STATE GEOLOGICAL MAP OF UKRAINEgeoinf.kiev.ua/kartograma/l37-7/pz_l37-7_eng.pdf · Lozovatka, Korsak, as well as eastern branches of Molochna River. Dnipro River basin includes the

MINISTRY OF ECOLOGY AND NATURAL RESOURCES OF UKRAINE STATE GEOLOGICAL SURVEY

STATE ENTERPRISE "PIVDENUKRGEOLOGIA"

PRYAZOVSKA COMPLEX GEOLOGICAL GROUP UKRAINIAN STATE GEOLOGICAL RESEARCH INSTITUTE

“UkrSGRI”

STATE GEOLOGICAL MAP

OF UKRAINE

Scale 1:200 000

CENTRAL-UKRAINIAN SERIES MAP SHEET L-37-VIІ (BERDYANSK)

EXPLANATORY NOTES

All additions and amendments of Scientific-Editorial Council are included Authors: B.V.Borodynya, I.L.Knyazkova, K.Yu.Esypchuk, E.B.Glevaskiy,

Zh.V.Chubar, T.Ya.Ivanenko Editor of Series: K.Yu.Esypchuk Editors: P.F.Gozhyk, B.Yu.Zosymovych, E.B.Glevaskiy Expert of Scientific-Editorial Council: R.M.Dovgan

English Translation (2007) B.I.Malyuk

Kyiv – 2004 (2008)

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State Geological Map of Ukraine. Scale 1:200 000. Series Central-Ukrainian. Map Sheet L-37-VII

(Berdyansk). Explanatory Notes. Kyiv: Ministry of Ecology and Natural Resources of Ukraine, SE "Pivdenukrgeologia", Pryazovska CGG, Ukrainian State Geological Research Institute “UkrSGRI”, 2004 (2008). – 136 pages, 15 Figures, 1 Table, 6 Annexes, References 124 sources.

Authors:

B.V.Borodynya, I.L.Knyazkova, K.Yu.Esypchuk, E.B.Glevaskiy, Zh.V.Chubar, T.Ya.Ivanenko

Editor of the Series

K.Yu.Esypchuk, Doctor of Geological-Mineralogical Sciences

Editors

P.F.Gozhyk, B.Yu.Zosymovych, E.B.Glevaskiy

Expert of Scientific-Editorial Council

R.M.Dovgan, leading geologist, Pravoberezhna Geological Expedition, SRGE "Pivnichgeologia"

English translation (2008)

B.I.Malyuk, Doctor of Geological-Mineralogical Sciences, UkrSGRI The work summarizes geological materials grounded on results of extended geological study of the map

sheet L-37-VII (Berdyansk) in the scale 1:200 000 conducted in 1991-2000. Explanatory notes to the set of maps which includes geological map and map of mineral resources of pre-

Quaternary units, geological map and map of mineral resources of Quaternary sediments, geological map and map of mineral resources of crystalline basement, stratigraphic column of the area, contain description of the series, suites and complexes of Archean, Proterozoic, Phanerozoic, as well as review of tectonics and history of geological development of the area. Mineral deposits and occurrences in crystalline basement and sedimentary cover are described, and perspectives of the area are appraised. Analysis of ecologo-geological environments is presented.

The set of maps can be used in the course of planning the geological exploration works in Western Pryazovya.

© B.V.Borodynya et al, 2004 (2008) © UkrSGRI, 2004 (2008)

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CONTENTS

Abbreviations used in the text ................................................................................................................................. 5 INTRODUCTION................................................................................................................................................... 6 1. STUDY DEGREE............................................................................................................................................... 8 2. STRATIFIED ROCKS...................................................................................................................................... 10

PRECAMBRIAN ............................................................................................................................................. 14 Archean Acrotheme ..................................................................................................................................... 14

Paleo-Archean (AR1) .............................................................................................................................. 14 Neo-Archean (AR3)................................................................................................................................. 17

Proterozoic Acrotheme ................................................................................................................................ 20 Paleo-Proterozoic (PR1) .......................................................................................................................... 20

PHANEROZOIC.............................................................................................................................................. 22 Mesozoic Eratheme...................................................................................................................................... 22

Jurassic System (J) .................................................................................................................................. 22 Cretaceous System (K)............................................................................................................................ 24

Cenozoic Eratheme ...................................................................................................................................... 28 Paleogene System (P).............................................................................................................................. 29 Neogene System (N) ............................................................................................................................... 31 Quaternary System (Q) ........................................................................................................................... 36

3. NON-STRATIFIED UNITS ............................................................................................................................. 46 Intrusive units ................................................................................................................................................... 47

Archean Acron............................................................................................................................................. 47 Neo-Archean ........................................................................................................................................... 47

Proterozoic Acron ........................................................................................................................................ 47 Paleo-Proterozoic .................................................................................................................................... 47 Meso-Proterozoic .................................................................................................................................... 51 Neo-Proterozoic ...................................................................................................................................... 52

Paleozoic-Mesozoic undivided .................................................................................................................... 53 Ultra-metamorphic units................................................................................................................................... 54

Archean Acron............................................................................................................................................. 54 Neo-Archean ........................................................................................................................................... 54

Proterozoic Acron ........................................................................................................................................ 55 Paleo-Proterozoic .................................................................................................................................... 55

Metasomatic rocks............................................................................................................................................ 57 4. WEATHERING CRUST AFTER CRYSTALLINE ROCKS........................................................................... 59 5. TECTONICS..................................................................................................................................................... 62

Lower tectonic level ......................................................................................................................................... 62 Folded and magmatic structures .................................................................................................................. 63 Fault structures............................................................................................................................................. 67

Upper tectonic level.......................................................................................................................................... 69 6. HISTORY OF GEOLOGICAL DEVELOPMENT........................................................................................... 71

Archean stage ................................................................................................................................................... 71 Proterozoic stage............................................................................................................................................... 72 Paleozoic stage ................................................................................................................................................. 74 Meso-Cenozoic stage........................................................................................................................................ 74

7. GEOMORPHOLOGY AND RELIEF-FORMING PROCESSES .................................................................... 76 8. HYDROGEOLOGY.......................................................................................................................................... 80 9. MINERAL RESOURCES AND REGULARITIES IN THEIR DISTRIBUTION ........................................... 85

Metallogenic zonation ...................................................................................................................................... 85 Combustible minerals ....................................................................................................................................... 86

Gaseous combustible minerals..................................................................................................................... 86 Natural gas .............................................................................................................................................. 86

Solid combustible minerals.......................................................................................................................... 86 Brown coal .............................................................................................................................................. 86

Metallic mineral resources................................................................................................................................ 86 Ferrous metals.............................................................................................................................................. 86

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Iron ores...................................................................................................................................................86 Non-ferrous metals.......................................................................................................................................88

Titanium ..................................................................................................................................................88 Copper .....................................................................................................................................................88 Nickel, copper .........................................................................................................................................89 Nickel ......................................................................................................................................................89

Rare metals...................................................................................................................................................89 Tungsten ..................................................................................................................................................89 Molybdenum ...........................................................................................................................................90 Niobium, tantalum, lithium .....................................................................................................................90 Niobium, tantalum...................................................................................................................................90 Rubidium, niobium, tantalum..................................................................................................................91 Rubidium, cesium....................................................................................................................................91 Zirconium................................................................................................................................................91

Precious metals ............................................................................................................................................91 Gold.........................................................................................................................................................91 Silver .......................................................................................................................................................92

Rare-earth metals .........................................................................................................................................93 Non-metallic mineral resources ........................................................................................................................93

Non-ore raw materials for metallurgy ..........................................................................................................93 Refractory raw materials .........................................................................................................................93 Flux raw materials ...................................................................................................................................94

Chemical raw materials................................................................................................................................94 Agro-chemical raw materials ..................................................................................................................94

Non-metal ore commodities .........................................................................................................................95 Abrasive raw materials ............................................................................................................................95 Electric- and radiotechnical raw materials ..............................................................................................95 Adsorptive raw materials.........................................................................................................................96

Facing-stone raw materials...........................................................................................................................96 Ornamental stone.....................................................................................................................................96

Construction raw materials...........................................................................................................................96 Glass and porcelain-faience raw materials ..............................................................................................96 Cement raw materials ..............................................................................................................................97 Quarry-stone raw materials .....................................................................................................................97 Sand and gravel raw materials.................................................................................................................97 Brick-tile raw materials ...........................................................................................................................97

Waters ...............................................................................................................................................................98 Underground waters .....................................................................................................................................98 Mineral sludge and mud...............................................................................................................................98

10. EVALUATION OF THE TERRITORY PERSPECTIVES ............................................................................99 11. ECOLOGO-GEOLOGICAL ENVIRONMENT ...........................................................................................101 CONCLUSIONS .................................................................................................................................................105 REFERENCES ....................................................................................................................................................107

Published.........................................................................................................................................................107 Unpublished (all in Russian)...........................................................................................................................108

Annexes ...............................................................................................................................................................113 Annex 1. List of deposits and occurrences indicated in the geological map and map of mineral resources in pre-Quaternary units .......................................................................................................................................113 Annex 2. List of deposits and occurrences indicated in the geological map and map of mineral resources in Quaternary sediments......................................................................................................................................121 Annex 3. List of deposits and occurrences indicated in the geological map and map of mineral resources of crystalline basement........................................................................................................................................123 Annex 4. List of deposits and occurrences indicated in the geological map and map of mineral resources in weathering crust ..............................................................................................................................................132 Annex 5. List of geological landmarks ...........................................................................................................134 Annex 6. List of organic remnants shown in "Geological map and map of mineral resources in pre-Quaternary units"...............................................................................................................................................................135

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Abbreviations used in the text

CSF - conventionally-safe factor DDD - Dniprovsko-Donetska Depression Derzhgeolkarta-200 - the State Geological Map in the scale 1:200 000 DGM-50 - Deep Geological Mapping in the scale 1:50 000 Donbas – Donetskiy Coal Basin DSS - Deep Seismic Sounding EGP - Exogenic Geological Processes EGSF-200/50 - Extended Geological Study of the Fields in the scale 1:200 000/1:50 000 GEE - Geological Exploration Expedition GPM-200 - Geological-Prognostic Mapping in the scale 1:200 000 IP - Induced Polarization LTC - Litho-Tectonic Complex LTZ - Litho-Tectonic Zone MTS - Magneto-Telluric Sounding NSC - National Stratigraphic Committee of Ukraine OPSZ - Orikhivsko-Pavlogradska Suture Zone PCM - Pryazovskiy Crystalline Massif SCMR – State Commission on Mineral Reserves SGE - State Geological Enterprise TAC - top admissible concentration TAL - top admissible level TIC - Territorial-Industrial Ccomplex TMZ - Tectono-Metallogenic Zone UkS - Ukrainian Shield VEP - Vertical Electric Profiling Acc – accessories ap – apatite Bi – biotite Cpx – clinopyroxene Ga – garnet Hb – amphibole Mgt – magnetite Opx – orthopyroxene Pl – plagioclase Q – quartz sdM – sulphides tr – traces zr – zircon æ – volume magnetic susceptibility σ – density in g/cm3

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INTRODUCTION The territory of map sheet L-37-VII (Berdyansk) in the administrative layout of Ukraine includes to

Berdyanskiy, Prymorskiy, Chernigivskiy, Pologivskiy and Kuybyshevskiy areas of Zaporizka Oblast1, and partially encompasses Volodarskiy and Pershotravneviy areas of Donetska Oblast. It is bounded by geographic coordinates 36o00'-37o06' E longitude and 46o40'-47o20' N latitude. Southern boundary of the mapped area coincides with the northern coast of Azov Sea.

In geological respect the map sheet area is located at the junction of two regional geostructures: south-eastern ledge of Pryazovskiy Block of Ukrainian Shield and eastern closure of Meso-Cenozoic Prychornomorska Depression. As a result, the area geology combines the rocks of crystalline basement which comprise the lower tectonic floor, and Mesozoic-Cenozoic sedimentary rocks in the upper tectonic floor. In addition, the latter is divided in two tectonic sub-floors: the lower just Mesozoic-Cenozoic one and upper Quaternary sub-floor.

Berdyansk (130.4 thousand inhabitants) and Prymorsk (13.9 thousand inhabitants) are the biggest towns in the area; town-like inhabited locations2 include Chernigivka, Kamysh-Zorya, Rozivka and Andriivka. Besides these, there are about 125 villages from 500 to 1000 and in some cases up to 5000 inhabitants each. All the locations are electrified and provided with telephone connections, and most - also with telegraphic one. In the towns and town-like locations there is established the water supply while in the villages water is being supplied by the shaft wells up to 10-15 m deep or so called "pools" which are being filled up with water delivered by special transport from boreholes located mainly in Lunacharskiy, Prymorskiy, Andriivskiy and Botiivskiy (the latter is on adjacent western map sheet) water scoops. The map sheet territory is crossed by two railroads: Berdyansk-Pology (125 km long, railway stations: Troyany, Elizavetivka, Nelgovka, Verkhniy Tokmak, Semenivka) and Volnovakha-Tokmak (154 km long, railway stations: Rozivka, Kamysh-Zorya, Stulneve). The biggest highways connect Berdyansk town with Mariupol (79 km), Melitopol (122 km), Tokmak (110 km) and Pology (99 km). Most of inhabited locations are also connected one another by asphalt-paved roads, rarely -gravel-paved roads, and some points only - by dirty roads which over summer rainfalls and spring-autumn seasons of bad roads become hardly-passable for auto-transport. Total length of paved roads is about 1700 km.

The sea transport is developed and the sea port Berdyansk is located in the map sheet. By the landscape-natural conditions the territory is divided into three parts: 1) northern part that belongs to Pryazovska Height – hilly, extensively eroded by river, gully and ravine

valleys, with altitudes from 100 to 324 m (Belmak Hill); 2) southern part comprising flat-wavy coastal plain with altitudes 20-100 m which is cut by fairly broad

(1-2 km) and shallow (up to 25-50 m) river and gully valleys with flat (up to 2-5o) slopes 3) area of Azov Sea with the steep (except the spits) coast from 3-5 to 20-37 m high. The beach of Azov

Sea is sandy, narrow (5-10 m). The banks of sand spits (Berdyanska and part of Obitochna) are low and their western sides are mudded and overgrown. Whole the coastal area is shallow-water.

Of the total map sheet square (5085 km2) the sea area occupies 556 km2, 1881.5 km2 (37% of the land portion) are used in agriculture, 442 km2 (8.7%) – in various building constructions, and 101.7 km2 (2%) are occupied by reserve and resort zones located in river and ravine valleys and covered by small forest or shrub massifs.

The field-protecting forest bands are widespread where major tree varieties include oak, ash-tree, acacia, and apricot. Over the non-arable lands such narrow-leaved plants as feather grass, fescue, mint-grass, etc. predominate; among the shrubs – blackthorn and dog-rose.

The wild animals include mainly foxes, rabbits, mouth-like rodents and jerboa, wild boars and roes. The bird population is abundant fairly variable. Azov Sea with low salinity is known with its fish diversity including goby, sea-roach, pike perch, plaice, sturgeon; dolphins are common in the sea.

The biggest river Berda (with Karatysh, Berestova and other branches) is up to 226 km long and flows into the Azov Sea to the east from Berdyansk town; by the river course, higher of Osypenko village, Berdyanske water reservoir (3.5 km2 in size) is established providing major water supplying of Berdyansk town. The Azov Sea basin also includes the rivers: Obitochna (with Kiltychiya, Chokrak, Sosykulak and other branches), Lozovatka, Korsak, as well as eastern branches of Molochna River. Dnipro River basin includes the river upper courses in the northern part of map sheet – Konka and Gaychur. Over the banks of most rivers mainly small 1 In Ukraine, the “Oblast” comprises major territorial administrative unit. In total, Ukraine includes 25 Oblasts plus the Crimean Autonomic Republic. Each Oblast consists of some higher-order administrative units hereafter entitled as “area” (Translator note). 2 In the Annexes 1-4, for simplicity, these town-type inhabited localities are indicated as “villages” (Translator note).

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cliffs of crystalline rocks are observed. River beds are shallow, mudded; a number of ponds are known in the area.

Climatic conditions are moderate-continental. The winters are mainly mild, low-snow with frequent melting and average temperature -4 … -8oC although the hard winters up to -30oC cold are known.

The soil is being frozen not deeper than 20 cm. The summer is hot and very dry with day temperatures +21 … +27oC, sometimes to +37 … +40oC. The rains are short-term, local, rainfall-type. Average amount of annual precipitates is 400-450 mm; their maximum falls to spring and autumn. Average wind speed is 6-7 m/s, and speed of summer dry winds may attain 15-20 m/s. The south-western and north-eastern winds are most persistent affecting sea-level changes.

About half of population lives in Berdyansk and Prymorsk towns; the first one is the well known resort and industrial centre, and both – the sites of summer vacations. Respectively, considerable part of population is employed in services. Some big plants operate in Berdyansk including agriculture machinery construction, petroleum refinery “Azmol”, “Sklovolokno” (glass wares), cable, tyre, and armoured concrete ones.

In Prymorsk town metallurgical, brick, mixed fodder, foodstuff, and bread-baking plants operate. Most population in the villages and town-like inhabited locations is employed in agriculture. Major farming standards include grain-crops and sunflower, with minor diversity of green-stuff, watermelon, muskmelon, grape, apricot, sweet-cherry and other fruits.

Degree of mineral resources development is low. Last century the high-grade iron ores in Korsak-Mogyla deposit and ceramic beryllium-bearing pegmatites at Eliseivka village used to be mined as well as a range of relatively small quarries for crushed stone were in production; of these latter some continue to operate nowadays in Novopoltavka, Ttudove, Stulneve, Kolarivka, and Andriivka villages. Granite quarry in Mogyla Saltychanska for small-scale dimension stones is about to be restored.

A range of perspective occurrences and deposits are known in the territory which could be mined in the near future: Novopoltavske (or Chernigivske) apatite and rare-metal deposit related to carbonatites; Surozke gold deposit with high-fineness flaky gold; Berdyanske lithium pegmatite deposit; Kuksungurske iron-ore deposit; Kolarivskiy lamproite-related diamond occurrence; Dragunske occurrence of abrasive quartz related to high-alumina gneisses, and some graphite occurrences on Berda River. Balka Velykogo Taboru deposit, the biggest one in Ukraine in term of the feldspar reserves, is located in the area centre; the distinct ornamental patterns of pegmatites in this deposit allow their exploitation for facing stones.

By conditions for carrying out the geological works the territory is considered to be suitable enough. Crystalline rocks of Precambrian basement are well exposed by the valleys of all rivers and gullies next 15-20 km from Azov Sea coast, and outcrops of Meso-Cenozoic cover rocks are also observed in the same localities. In watershed areas the mapping were conducted using minor (first tens and up to 50 m deep) drill-holes, and in the coastal area – by 100-200 m and even 500 m deep drill-holes. Thin Quaternary sediments are widespread and exposed over entire territory.

The set of geological maps is designed mainly by results of extended geological studies in the scale 1:200 000 performed over the map sheet territory in 1991-2000 under leadership of V.F.Rozdorozhniy, using results of geological mapping and prospecting provided by G.L.Kravchenko, G.G.Konkov, M.I.Lebedev, V.A.Tsukanov, R.M.Dovgan, M.F.Rusakov, V.M.Dralov, L.P.Gogol, O.O.Bochkov, V.P.Kryvonos, O.M.Makarenko, A.V.Strekozov, M.F.Dyukov, F.V.Shrubovych, I.A.Ignatkin, O.F.Makivchuk, O.M.Berezka, V.D.Nesmiyko, M.S.Ryabtsev, E.M.Laputskiy and others.

The set of the State Geological Maps in the scale 1:200 000 (“Geological map and mineral commodity map of pre-Quaternary units”, “Geological map and mineral commodity map of Quaternary sediments”, “Geological map and mineral commodity map of crystalline basement”) is prepared for publishing by B.V.Borodynya (group head), I.L.Knyazkova, K.Yu.Esypchuk, E.B.Glevaskiy, Zh.B.Chubar, T.Ya.Ivanenko. Edition of maps and explanatory notes is provided by E.B.Glevaskiy, V.Yu.Zosymovych and P.F.Gozhyk.

Methodic leadership over the works was carried out by S.M.Strekozov, Chief of Pryazovska GEE. The map design and preparation was facilitated by M.V.Geychenko, A.S.Drannyk, O.B.Bobrov, B.D.Vozgryn, M.V.Kozar. The map is designed on the ground of data available by January 1, 2003.

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1. STUDY DEGREE The first edition of geological map in the scale 1:200 000 over map sheet L-37-VII (Berdyansk) was

carried out in 1966 by results of report on the State geological-hydrogeological mapping in the scale 1:200 000, responsible executive G.L.Kravchenko, 1962. Up to now this map is valuable and meaningful.

Over the forty years passed since that time, four periods can be distinguished in the geological study of the map sheet L-37-VII (Berdyansk).

1st period, 1961-1967. Geologists from the State enterprises “Artemgeologia” and “Dniprogeologia” as well as Kyiv University G.G.Konkov, R.M.Polunovskiy, 1965; M.I.Lebedev, 1966, V.A.Tsukanov, 1967 had conducted by-sheet mapping over 11 sheets in the scale 1:50 000. In parallel, the limited prospecting was performed for asbestos (O.O.Bochkov, 1967), high-alumina raw materials (V.A.Ignatkin, 1961; F.V.Shrubovych, 1963), vermiculite (L.P.Gogol, 1964), base metals (P.I.Teteryuk, 1965). Structure of the territory was essentially clarified in this period. The ground has been provided for the ideas concerning territory perspectives for new mineral occurrences.

2nd period, 1968-1975. A great amount of geological prospecting works performed for rare elements in Sorokynska and Chernigivska tectonic zones. It were also conducted prospecting for iron ores (L.I.Kanygin, 1972-1973; I.L.Andrushchenko, 1974; V.P.Kryvonos, 1975), feldspar-quartz raw materials (L.P.Gogol, 1966), graphite and others, as well as diamonds (M.F.Strekozov, 1968, 1975; E.G.Krongauz, 1976). Starting from 1968, when prognostic metallogenic map was designed for rare and trace elements (N.G.Kasatkin et al), prospecting and evaluation works over map sheet L-37-VII (Berdyansk) were carrying out for these mineral types. L.F.Lavrynenko, 1968, 1973, 1974; D.Sh.Rozenberg, 1970 performed prospecting for Ti, Be, Li, Rb, Cs, TR in brittle rocks and pegmatites of Western Pryazovye. In Chernigivska tectonic zone, starting from 1969, when rare-metal and apatite mineralization was discovered, over next 18 years Bilozerska GEE was conducting ahead and detailed exploration of apatite ores; it was also evaluating rare-metal mineralization, and together with scientists from Moscow, Kyiv and Simferopol studying ore composition and mechanism of their formation, developing technical-economic substantiations for the ore conditions. These results are contained in numerous reports of E.M.Lapytskiy, 1971, 1973, 1976, 1978, 1980, 1981, 1985, 1991. At the same time, over the five southern sheets (L-37-38-B,D; -38-C; -37-C,D) where Precambrian is overlain by Meso-Cenozoic rocks, it was completed geological mapping in the scale 1:50 000 (R.M.Dovgan, 1972, 1975; A.I.Nekryach, 1975).

As a result of these works, it was designed for the first time the map of Meso-Cenozoic, the Quaternary sediments were mapped in details, prognosis for ferruginous quartzites in Orlovska and Inzivska sites was performed, and tectonics and hydrogeology of the studied map sheet were described.

3rd period, 1976-1985. Metallogenic maps were designed and stratigraphic schemes were adjusted. The works on geological mapping were performed under new quality level. In the areas of most prospective zones the deep geological mapping in the scale 1:50 000 (DGM-50) was applied. Responsible executives in these works were M.F.Rusakov, 1977; V.M.Dralov, 1979; M.F.Rusakov, 1981.

As a result of these works, it was subdivided for the first time the supracrustal units, igneous complexes, tectonics, mineral deposits described in details, and new prospecting sites were recommended (see “Schemes of materials used”).

In the same period, prospecting and exploration were completed in Kuksungurske and Korsatske iron ore deposits (O.M.Makarenko, 1978; V.P.Kryvonos, 1979), as well as the works for rare elements in Sorokynska tectonic zone, Sadova site (L.F.Lavrynenko, 1976, 1979; O.M.Koval, 1980, 1981), for diamonds (M.F.Strekozov, 1977; E.G.Krongauz, A.V.Dyukov, 1977, 1985), for amphibolites (O.O.Bochkov, 1978-1981), for marbles (A.A.Pastushenko, 1980; O.O.Bochkov, 1983), and for kaolines (E.N.Kachanov, 1981).

4th period, 1986-1999. Over the fourth period deep geological mapping DGM-200 was conducted (V.F.Kiktenko, 1987), detailed exploration of Novopoltavske apatite deposit was completed (E.M.Lapytskiy, 1991), it was performed prospecting for staurolite (P.G.Priymak, 1991), apatite (V.G.Latsko, 1990), gold (O.F.Makivchuk, 1994), eclogite- and lamproite-type diamonds (O.M.Stremovskiy, 1986; O.P.Knyazkov, 1989), and a number of research prognostic-reconnaissance works [74, 96, 111, 112, 113].

Scheduled geophysical surveys (electric, gravity, magnetic) in the scale 1:200 000 over the map sheet L-37-VII were carrying out since the mid 50th. In 1955-1960 the aerial geophysical mapping was provided by V.M.Pelyushenko, K.M.Sokolova, S.A.Piskunova, A.A,Klimerov, A.V.Gryshyn and others.

In 1960-1970 almost entire territory was covered by gravimetric survey in the scale 1:50 000 and magnetic survey in the scale 1:25 000. The works were performed by geophysicists M.A.Badygin, V.I.Smirnov, S.G.Solyar, A.D.Markov, V.I.Rozov, G.A.Avksentyev, V.P.Terin and others. As a result of these works, the data

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were obtained over the whole territory of extended studies providing integral patterns of the rock magnetization and density distribution. Besides that, detailed surveys also were done in the scale 1:2 000 – 1:5 000 and 1:10 000. These works were performed for geophysical background design in the course of prospecting works in Sorokynska and Chernigivska tectonic zones as well as in Korsatske and Kuksungurske deposits (V.P.Martynov).

In the beginning of 90th A.A.Irza has performed aerial gravimetric and magnetic surveys for geophysical background preparation to be further used in DGM-50 and DGM-200. By these works, new minor massifs of ultramafic rocks and sub-alkaline granites were found to be perspective for rare metals, the distribution fields of stratified and non-stratified rocks were adjusted, and new high-order faults were mapped. Electric survey was applied in the mapping of crystalline basement surface, prospecting for ore and non-ore minerals, in hydrogeological studies. Over the last 30 years the map sheet area is covered by the electric surveys using standard methods VEP, IP and their combination.

In Pryazovskiy Block the studies by deep seismic sounding (DSS) had been being carried out since 1960 to 1978. Study of the earth crust and upper mantle was aimed earth crust geotectonic zonation, upper mantle features and definition the rational direction for prospecting and exploration works. On the ground of DSS data, the Moho (M) and Conrad (C) surfaces were determined, the Moho surface map (V.B.Sologub, 1967; M.A.Bordulin, 1985) and upper mantle structure sketch (V.B.Sologub, 1985) were designed in the scales 1:1 000 000, 1:2 500 000.

Since 1980 the State Geophysical Expedition “Dniprogeofizika” participated in the studies of deep electric conductivity of Pryazovskiy block. Over next 15 years a number of magneto-telluric sounding (MTS) observations were performed in the south-east of the map sheet which had provided the ground for the section geo-electric properties and degree of their lateral changes. These results are described in details in the works of A.I.Ingerov. Re-processing of previous MTS data together with seismic data interpretation, taking into account reliability of gravi-magnetic field maps, had resulted in more detailed model of the deep structure in the south-western part of Pryazovskiy Geoblock.

Scheduled geochemical study of the map sheet commenced in 1957-1960. In the course of geological mapping in the scale 1:200 000 (G.L.Kravchenko, 1962) metallometric maps were designed although without anomalous content of elements.

In the course of geological mapping in the scale 1:50 000 (G.G.Konkov, 1961, 1965; N.I.Lebedev, 1966), due to outdated techniques of spectral analysis, responsible executives had failed in design of conditional geochemical maps. The first mathematic processing of spectral analysis data, computation of Clarks and anomalous values for 27 elements in various types of rocks and minerals, and element anomalous content maps were conducted in course of geological mapping (GM-50) by V.O.Tsukanov, 1967 and R.M.Dovgan, 1972, 1975. Results obtained later in 1975-1991 were proven to be more comprehensive. In parallel, the preparation works and deep geological mapping in the scale 1:50 000 (A.I.Nekryach, 1975; V.M.Dralov, 1979; M.F.Rusakov, 1977, 1981), as well as research geochemical works headed by O.M.Dudyk and S.M.Strekozov, 1991, were conducted.

As a result of mentioned works, the sites prospective for various minerals were predicted including ones for gold (O.F.Makivchuk, 1977). Analysis of the research works allowed evaluation of geochemical study degree in Berdyanska site. It was shown that due to irregular sampling, mainly in ore sections, as well as non-conditional analytical techniques prior to 1967, most part of the territory remained not studied in geochemical respect.

Ecological works over the studied territory were not performed. Engineering-geological studies, conducted by Bilozerska and Pryazovska GEE over last 30 years had provided indirect ecological features of the area.

In 1991-2000 in the course of DGM-200 [103] the sampling was performed over the map sheet by the grid 4 by 4 km (detalization 2 by 2 km in contaminated sites). The samples for radio-nuclides and heavy metals were taken from the soils and aeration zone, and in the coastal area of Azov Sea the beach sands were studied with radioactivity measurements. In addition, the waters in water reservoirs and discharge points were sampled as well as their bottom sediments. By these results the maps were designed.

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2. STRATIFIED ROCKS Stratified units over map sheet include Quaternary, Neogene, Paleogene (Cenozoic Eratheme),

Cretaceous and Jurassic systems (Mesozoic Eratheme) of Phanerozoic as well as metamorphic rocks of Paleo-Proterozoic, Neo- and Paleo-Archrean divisions of Precambrian.

According to the distribution of diverse-facies Phanerozoic sediments over the map sheet Chernigivsko-Berestovska, Chernigivsko-Stulnivska and Prymorska LTZs are distinguished, and distribution of diverse metamorphic units allows definition of Orikhivsko-Pavlogradska, Zakhidnopryazovska and Tsentralno-pryazovska LTZs (see "Scheme of crystalline basement litho-tectonic zonation" in the scale 1:1 000 000).

Cenozoic and Mesozoic sediments do form the sedimentary cover up to 90-100 m thick in the north-west of the map sheet and up to 300-800 m – in the south; the cover almost completely overlies Precambrian crystalline basement.

Metamorphosed and tightly-folded crystalline basement rocks belong to the lower tectonic level which is divided into three tectonic floors: Paleo-Proterozoic, Neo-Archean and Paleo-Archean.

Paleo- and Neo-Archean stratified rocks are most widespread in the geological map of crystalline basement. Paleo-Proterozoic metamorphic rocks are locally distinguished.

Generalized stratigraphic column is given below in descending order.

STRATIGRAPHIC SCHEME OF PRECAMBRIAN AND PHANEROZOIC ROCKS IN THE TERRITORY OF L-37-VII (Berdyansk) MAP SHEET

PHANEROZOIC

C e n o z o i c e r a t h e m e

Quaternary System

Holocene Division – H

eH - eluvial sediments vH - aeolian sediments cH - coluvial sediments aH - alluvial sediments dcH - deluvial-coluvial sediments pdH - proluvial-deluvial sediments adH - alluvial-deluvial sediments tH - technogenic (alluvial) sediments mHač - Azovo-Chornomorskiy Horizon. Marine sediments m11mHač - Azovo-Chornomorskiy Horizon. Marine and estuary-marine sediments

Undivided Upper Pleistocene – Holocene sediments (H-PIII) aPIII-H – alluvial sediments adPIII-H – alluvial-deluvial sediments edPIII-H – eluvial-deluvial sediments

Pleistocene

Neo-Pleistocene

Upper Branch (PIII) a1PIIIds – Desnyanskiy ledge. Alluvial sediments of the first over-flood terrace a2PIIIvl – Vilshanskiy ledge. Alluvial sediments of the second over-flood terrace a3PIIItb – Trubizkiy ledge. Alluvial sediments of the third over-flood terrace edPIII – eluvial-deluvial sediments

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vdPIIIpč – Prychornomorskiy climatolith. Aeolian-deluvial sediments ePIIIdf – Dofinivskiy climatolith. Eluvial sediments vdPIIIbg – Buzkiy climatolith. Aeolian-deluvial sediments ePIIIvt – Vitachivskiy climatolith. Eluvial sediments vdPIIIud – Udayskiy climatolith. Aeolian-deluvial sediments ePIIIpl – Prylutskiy climatolith. Eluvial sediments vd,ePIIIbg-pč – Buzkiy and Prychornomorskiy climatoliths. Undivided aeolian-deluvial and eluvial sediments e,vdPIIIpl-vt – Prylutskiy and Vitachivskiy climatoliths. Undivided eluvial, aeolian-deluvial sediments pdPIII – proluvial-deluvial sediments ed,dPIII – eluvial-deluvial and deluvial sediments

Undivided Middle and Upper Branches (PII-PIII) e,vdPII-III – eluvial, aeolian-deluvial sediments

Middle Branch (PII) a4Pčr – Cherkaskiy ledge. Alluvial sediments of the fourth over-flood terrace vdPIIts – Tyasminskiy climatolith. Aeolian-deluvial sediments ePIIkd – Kaydatskiy climatolith. Eluvial sediments a5PIIhd – Khadzhybeyskiy ledge. Alluvial sediments of the fifth over-flood terrace vdPIIdn – Dniprovskiy climatolith. Aeolian-deluvial sediments ePIIzv – Zavadivskiy climatolith. Eluvial sediments e,vdPII – eluvial, aeolian-deluvial sediments undivided

Lower Branch (PI) mPIzk – Zyukskiy Horizon. Marine sediments a6PIkn – Krukenytskiy ledge. Alluvial sediments of the sixth over-flood terrace vdPItl – Tyligulskiy climatolith. Aeolian-deluvial sediments ePIlb – Lubenskiy climatolith. Eluvial sediments a7PIdc – Donetskiy ledge. Alluvial sediments of the seventh over-flood terrace vdPIsl – Sulskiy climatolith. Aeolian-deluvial sediments ePImr – Martonoskiy climatolith. Eluvial sediments a8PIbk – Budatskiy ledge. Alluvial sediments of the eighth over-flood terrace vdPIpr – Pryazovskiy climatolith. Aeolian-deluvial sediments ePIsh – Shyrokynskiy climatolith. Eluvial sediments e,vdPI – Eluvial and aeolian-deluvial sediments undivided

Eo-Pleistocene

Upper Branch (EII) (a9EIIng) – Nogayska ledge. Alluvial sediments of the ninth over-flood terrace (vdEIIil) – Illichivskiy ledge. Aeolian-deluvial sediments (eEIIkr) – Kryzhanivskiy climatolith. Eluvial sediments

Lower Branch (EI) (vdEIbr) – Berezanskiy climatolith. Aeolian-deluvial sediments

Pliocene – Eo-Pleistocene sediments undivided a10N2-EIkz – Kyzyldzharskiy ledge. Alluvial sediments of the tenth over-flood terrace

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Neogene System (N)

Chernigivsko-Berestivska LTZ Prymorska LTZ

Pliocene (N2) N2cb – Sequence of red-brown clays. Sub-aerial sediments

A k c h a g y l s k i y r e g i o - s t a g e N2gp – Sequence of clays, sands. Estuary-marine

sediments

C i m m e r i a n r e g i o - s t a g e N2zp – Sequence of iron-enriched sandstones.

Shallow-water marine, estuary-marine sediments

Miocene (N1)

P o n t i a n r e g i o - s t a g e N1sg – Sequence of parti-coloured clays. Sub-aerial sediments N1v – Sequence of limestones. Shallow-water marine sediments

S a r m a t i a n r e g i o - s t a g e N1gp – Clayey-sandy sequence N1kt-gl – Katerlezski and Geliksovi layers undivided

(Upper Sarmatian) N1nm-dn – Novomoskovski, Vasylivski and Dnipropetrovski layers undivided (Middle Sarmatian) N1kz-zb – Kuzhorski and Zbruchski layers undivided (Lower Sarmatian)

K o n k s k i y r e g i o - s t a g e N1sz-kn – Sartaganski and Konkski layers undivided

Lower-Middle Miocene undivided

P o l t a v s k i y r e g i o - s t a g e N1-2np – Novopetrivska Suite

Paleogene System (P)

Eocene (P2) Alminskiy and Khadzhybeyskiy stages undivided P2gp – Clayey-sandy sequence P2al-hd – Alminska and Khadzhybeyska suites Simferopolskiy and Bakhchysarayskiy regio-stages undivided P2pg – Sequence of sands and clays P2pg – Sequence of sands and clays

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M e s o z o i c E r a t h e m e

Cretaceous System (K)

Upper Division (K2)

C a m p a n i a n s t a g e

Chernigivsko-Stulnivska LTZ Prymorska LTZ

K2p – Sandy sequence K2pm – Sequence of sandy rocks and marls

T u r o n i a n a n d C o g n a c i a n s t a g e s K2bd – Berdyanska Suite

S e n o m a n i a n s t a g e K2gn – Genicheska Suite

Lower Division (K1)

A l b i a n s t a g e

L u n a c h a r s k i y r e g i o - s t a g e K1ln – Lunacharska Suite

A p t i a n a n d A l b i a n s t a g e s u n d i v i d e d K1pg – Sandy-clayey sequence

A p t i a n s t a g e K1gp – Clayey-sandy sequence

Jurassic System (J)

Middle Division (J2)

B a t i a n s t a g e J2gp – Sequence of clays and sands

PRECAMBRIAN

Proterozoic Acrotheme

Paleo-Proterozoic (PR1)

Orikhivsko-Pavlogradska LTZ Tsentralnopryazovska LTZ Zakhidnopryazovska LTZ PR1db – Dibrovska Suite PR1sd – Sadova Sequence

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Archean Acrotheme

Neo-Archean (AR3)

T s e n t r a n l o p r y a z o v s k a S e r i e s AR3dm – Demyanivska Suite AR3tm – Temryutska Suite

O s y p e n k i v s k a S e r i e s AR3kb – Krutobalkinska Suite AR3ol – Olginska Suite

Paleo-Archean (AR1) AR1dr – Dragunska Sequence AR1dr2 – Upper sub-sequence AR1dr1 – Lower sub-sequence

Z a k h i d n o p r y a z o v s k a S e r i e s ( A R 1 z p ) AR1knk – Kainkulatska Sequence AR1vt – Verkhnyotokmatska sequence

Below is presented the description of geological stratons which are indicated in all three geological maps (“Geological map and mineral commodity map of pre-Quaternary units”, “Geological map and mineral commodity map of Quaternary sediments”, “Geological map and mineral commodity map of crystalline basement”) starting from the oldest rocks.

PRECAMBRIAN Archean Acrotheme Paleo-Archean (AR1) Pryazovian area comprises a part of Ukrainian Shield, particularly, its furthest south-eastern part, and is

mainly composed of metamorphic rocks (see “Geological map of crystalline basement”). Zakhidnopryazovska Series (AR1zp) is most widespread among the stratified metamorphic rocks of the

area occupying more than two thirds of its square. By lithological composition the Series is divided in two sequences: lower – Verkhnyotokmatska and upper – Kainkulatska.

Zakhidnopryazovska LTZ Verkhnyotokmatska sequence (AR1vt) is comprised of biotite-two-pyroxene plagiogneisses, amphibole-

clino- and amphibole-orthopyroxene mafic gneisses, and clino- and orthopyroxene and pyroxene amphibolites. These rocks fill up mainly Lozovatska anticline which surrounds Saltychanska dome-shaped structure from the west looking like the flat sub-longitudinal arch. Sporadically these rocks are also known inside this structure, mainly at its periphery.

The Sequence rocks are well-expressed in gravity and magnetic fields. They form a range of second-order anticline folds oriented mainly in the north-western and north-eastern directions: to the north-west from Kolarivka village, to the east from Nelgivka station, and to the east from Uspenivka village. Some isometric anticlines up to 1 (2-3) km in size are distinguished in the south of the map sheet, at Borysivka village outskirts, to the east from Shevchenko village, and in other places within Saltychanska structure.

In the north and south of the map sheet the Sequence is extended outside the sheet boundaries. In the map sheet area it is overlain by Kainkulatska sequence rocks although the contact with this sequence and the younger metamorphic rocks is tectonic.

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The Sequence rocks are exposed at the surface on the right bank of Tokmak River between Verkhniy Tokmak and Chernigivka villages, on the left bank of Tokmak River (next 0.5-2.0 km higher the mouth of Kainkulak River) and on the right bank of Kainkulak River, and together with granites occur in Novopoltavskiy crushed-stone quarry (Mogyla Synya). Rock dipping commonly is steep under the angles 70-80o.

In the Precambrian stratigraphic column of the L-37-VII map sheet the Sequence is the lowermost. Just its upper portions are exposed at the surface and thus definition of its total thickness is impossible. In view of geophysical data it may exceed 3 km.

Magnetic field above the Sequence rocks displays increased values in the range 500-1200 nT. The gravity field of residual gravity anomalies being recalculated to the height of 1.5 km varies in the range 0.25-0.5 mG; negative density values predominate whereas positive ones are locally observed in places where denser rocks are elevated to the surface or are adjacent to the Sequence (see “Scheme of anomalous magnetic field”, “Scheme of local gravity anomalies”, 1:500 000).

Average value of two-pyroxene plagiogneisses magnetic susceptibility is 270*10-5 CI units, density – 2.7 g/cm3; magnetic susceptibility of mafic gneisses is 5400*10-5 CI units, density – 2.97 g/cm3; pyroxene amphibolites – 2500*10-5 CI units and 2.97 g/cm3 respectively.

Macroscopically plagiogneisses are grey, often light-grey, gneissose, often banded rocks of the following mineral composition (%): oligoclase-andesine (50-70), quartz (10-25), pyroxenes (0-10), hornblende (0-7), biotite (5-25), microcline (0-10); accessories: magnetite, apatite, zircon; secondary: chlorite, sericite, epidote. Their average chemical composition does correspond to diorites-granodiorites.

Mafic gneisses and pyroxene amphibolites are grey and dark-grey, unclear-banded rocks. Mineral composition (%): andesine-bytownite (50-70), hornblende (10-25), biotite (0-10), hypersthene (0-10), clinopyroxene (5-15), often garnet is observed. By chemical composition the rocks do correspond to gabbro. Both gneisses and mafic gneisses by petrochemical features in various classification diagrams fall into the fields of mafic and intermediate igneous rocks.

As it is evidenced by composition of mineral assemblages and features of opaque rock-forming minerals [103], the Sequence rocks were metamorphosed under granulites facies conditions at moderate or slightly increased pressure, and then the rocks have undergone retrograde metamorphism under amphibolite facies conditions.

Radiological age was not determined directly for the Sequence rocks. In gneisses of Kainkulatska Sequence by U-Pb method the age value of 3350 Ma is received (time of their metamorphism), and in the adjacent area the lower part of Zakhidnopryazovska Series (ultramafic rocks of Novopavlivska Sequence) is dated to 3650 Ma while granitoids that cut the sequence – to 3370-3400 Ma [42].

Orikhivsko-Pavlogradska LTZ Kainkulatska Sequence (AR1knk). It is developed widely in comparison to Verkhnyotokmatska one and

is more intricate in composition. It is mainly composed of biotite, amphibole-biotite, biotite- and amphibole-pyroxene plagiogneisses and mafic gneisses as well as garnet-biotite and pyroxene amphibolites. In addition, ferruginous quartzite (up to 5-15 m) and eulisite (up to 5 m) layers and calciphyre (up to 0.5 m) interbeds are observed in places [97].

The widest areas of the Sequence rocks are confined to the periphery of Saltychanska dome-shaped structure as well as to the eastern part of Orikhivsko-Pavlogradska suture zone. In Lozovatska anticline these rocks fill up some linear second-order syncline folds, and in Bilotserkivska syncline – latitudinal anticline folds. The rocks are also developed in the eastern part of Zakhidnopryazovska LTZ, to the north-east from Sorokynska tectonic zone, and are also known in the latter (see “Tectonic scheme”).

The most complete section of the Sequence is observed in the lower course of Kainkulak River, in its right bank. Big outcrops of the Sequence occur on the left bank of Verkhniy Tokmak River nearby Chernigivka village and on the left bank of Yushanly River. The section is mainly composed of plagiogneisses and mafic gneisses which alternate without visible regularity and contain single layers and interbeds of other rocks. Layer thickness varies from first to tens of meters. They form the series of isocline folds with mainly steep (80-85o) rock dipping although in Saltychanska structure and in Bilotserkivska syncline fairly flat rock plunging occur (angles up to 20-10o and sub-horizontal).

It is thought the Sequence lies over the rocks of Verkhnyotokmatska Sequence although the contacts between the two are mainly tectonic. In Bilotserkivska syncline the Sequence rocks are unconformably overlain by garnet-biotite plagiogneisses of Dragunska Sequence, and in Sorokynska graben-structure (also with tectonic unconformity) – by Olginska Suite metabasites of Osypenkivska Series. In the east of the map sheet the Sequence with stratigraphic and angular unconformity is overlain by Temryutska Suite rocks of Tsentralnopryazovska Series. Thickness of the Sequence is estimated to 3000 m and more.

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Gneisses of Kainkulatska Sequence coincide with the positive magnetic field up to 500-700 nT, and mafic gneisses, amphibolites and ferruginous quartzite interbeds – linear anomalies up to 1000-2000 nT. The anomalies are also defined in the gravity field (up to +0.5 …+1.5 mG). Magnetic susceptibility of gneisses is 1126*10-5 CI units, mafic gneisses – 9130*10-5 CI units, ferruginous quartzites – 9200*10-5 CI units; their density is 2.68 and 2.92 g/cm3 respectively.

The Sequence gneisses and mafic gneisses by their petrographic and petrochemical features commonly do not differ from the similar rocks of Verkhnyotokmatska Sequence and also do correspond to the ortho-rocks. In Kainkulatska Sequence leucocratic biotite and garnet-biotite gneisses are developed which can be ascribed to the metamorphosed sedimentary rocks. Obviously, ferruginous quartzites were also formed from some sediments.

By metamorphic degree the Sequence rocks also belong to granulite facies with superimposed amphibolite retrograde metamorphism.

The first Archean radiological date (2860 Ma) for the Sequence rocks was obtained by K-Ar method on amphibole [24]. Further [42] age determination on zircons from gneisses by U-Pb isochrone method yielded 3350 Ma that corresponds to the time of metamorphism.

Zakhidnopryazovska LTZ Dragunska Sequence (AR1dr) is developed only in the north-east of the studied map sheet where

together with Kainkulatska Sequence it constitutes large (up to 20 by 45 km) Bilotserkivska syncline. By lithological composition the Sequence is subdivided in two sub-sequences – lower and upper.

Lower Sub-Sequence (AR1dr1) is mainly composed of amphibolites which alternate with garnet-biotite, garnet-sillimanite-biotite, garnet and biotite-amphibole plagiogneiss layers and minor pyroxene mafic gneiss interbeds. The rocks unconformably lie over the folded rocks of Verkhnyotokmatska and Kainkulatska sequences of Zakhidnopryazovska Series. The contacts are mainly tectonic with Shevchenkivskiy Complex plagiogranites developed along.

The column of the Sub-Sequence is well-studied during prospecting for corundum in the area of Zhukovka gully (left branch of Mokra Konka River) nearby Zrazkove and Dibrove villages [123]. Considerable portion of the column (up to 300 m) is exposed by the railway hollow in 1 km to the east from Verkhniy Tokmak-2 station. The total thickness of the Lower Sub-Sequence is estimated to 1200 m.

Magnetic field above the rocks of Lower Sub-Sequence is slightly differentiated in the range 300-800 nT and above the layers of magnetite-bearing amphibolites it is increased up to 1100 nT. Gravity field recalculated to the height of 1.5 km varies in the rage 0-1.0 mG. Average magnetic susceptibility of amphibolites is 867*10-5 CI units, plagiogneisses – 435*10-5 CI units; density, respectively, is 2.89 and 2.79 g/cm3.

Mineral composition of amphibolites (%): andesine (20-60), hornblende (35-75), biotite (0-7), in places garnet (up to 10) and quartz (up to 5); accessories: sphene, apatite and magnetite. By chemical composition the rocks correspond to the igneous rocks of mafic and intermediate composition.

Plagiogneisses are grey, pink-grey and dark-grey medium-diverse-grained rocks with well-expressed gneissose and banded structure. Their mineral composition is fairly variable (%): oligoclase-andesine (25-72), quartz (10-45), biotite (5-20), garnet (2-20), sillimanite (0-10), cordierite (0-12), corundum, graphite; accessory minerals – zircon, monazite, spinel, apatite, pyroxene, magnetite, hematite etc. In migmatitized varieties microcline appears.

Among plagiogneisses of diorite composition, the biotite (5-30% of biotite contained) and amphibole (up to 15-20% of hornblende) or their mixed varieties predominate. By chemical composition these rocks do correspond to the felsic and intermediate volcanics (andesites and dacites), and high-alumina gneisses – to metamorphosed sedimentary rocks (re-deposited weathering crusts). Besides metamorphism, these rocks underwent considerable ultra-metamorphic and metasomatic modifications. Processes of the first type are expressed in development of the pink granite veins from some centimeters to first meters thick. Obviously, corundum is of metasomatic origin; it is developed in sillimanite-bearing gneisses at the contact with Paleozoic essexite-shonkinite stocks. The rocks of this Sub-Sequence are favourable for corundum and sillimanite deposits formation.

The age of Lower Sub-Sequence was defined by zircon from gneisses exposed in the railway hollow nearby Verkhniy Tokmak-2 station (2530 Ma) [24], and by zircons from biotite-amphibole plagiogneisses exposed on the left bank of Mokra Konka River in 4 km to the north from Zrazkove village (2790 Ma) [3].

Upper Sub-Sequence (AR1dr2) is mainly composed of biotite and biotite-amphibole plagiogneisses with minor, relatively thin (up to 10-15 m) amphibolite layers. It conformably overlies the rocks of Lower Sub-Sequence and with the stratigraphic and angular unconformity is overlain by the rocks of Temryutska Suite of Tsentralnopryazovska Series. The most completed sections of the Sub-Sequence are observed in the upper

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course of Verkhniy Tokmak River nearby Verkhniy Tokmak village, and also on the right bank of Berda River to the east from Oleksiivka village. The total thickness of Sub-Sequence does not exceed 1000 m.

In magnetic (200-300 nT) and gravity (0-0.75 mG) fields the rocks in Sub-Sequence are actually not expressed.

Magnetic susceptibility of gneisses is 46-96*10-5 CI units, amphibolites – 2370*10-5 CI units; density is 2.63 and 2.88 g/cm3 respectively.

Among the Sub-Sequence rocks biotite gneisses predominate. These are dark-grey, medium- and fine-grained rocks with gneissose and banded structure. Their mineral composition (%): oligoclase (40-70), quartz (20-35), biotite (5-20), hornblende (3-15); accessories – apatite, zircon, magnetite. By chemical composition the plagiogneisses mainly correspond to intermediate and felsic igneous rocks although some sedimentary rocks metamorphosed under amphibolite facies may be developed among the biotite varieties. Amphibolites by chemical composition do correspond to the mafic igneous rocks (meta-basalts).

Ascription of Dragunska Sequence to Paleo-Archean, approved by the NSC in 2000, is fairly conventional and apparently requires adjustment. This is not supported by above data on isotopic age of Lower Sub-Sequence while for the Upper Sub-Sequence such data are lacking at all. It can be only contended confidently that this Sequence is transitional between Zakhidnopryazovska (Paleo-Archean) and Tsentralnopryazovska (Neo-Archean) series, that is, it can be ascribed either to the Upper Paleo-Archean or Lower Neo-Archean, and, most probable, to Meso-Archean.

Neo-Archean (AR3) Neo-Archean rocks are known in the east and west of the map sheet and include Osypenkivska and

Tsentralnopryazovska series. Their distribution area is not great – up to 15% of the mapped territory and encompasses mainly the eastern part of the map sheet (see “Geological map of crystalline basement”).

Zakhidnopryazovska LTZ Osypenkivska Series (AR3os) is subdivided in two suites – Olginska, mainly meta-volcanogenic, and

Krutobalkinska meta-sedimentary. These suites constitute the deeply eroded Sorokynskiy greenstone belt in the east of the map sheet. Outside this belt but on extension of its longitudinal branch (area of Osypenko village) just a few up to 2 km long remnants of Olginska Suite rocks are known. The Series is studied in the exposed part of the belt in the banks of Berdyanske water reservoir, as well as in the numerous drill-holes. Its total thickness is up to 1.2 km. From the south-east to north-west thickness of the Series decreases and in the north nearby Andriivka village it does not exceed first hundreds of meters.

In geophysical fields the Series rocks differ in increased magnetization and density caused by ultramafic and ferruginous rocks in the middle part of the column. Average magnetic susceptibility of Olginska Suite attains 5839*10-5 CI units, and Krutobalkinska – 324*10-5 CI units. Their density is 2.92 and 2.77 g/cm3 respectively.

Neo-Archean age of the Series rocks is defined through its cutting by Osypenkivskiy Massif tonalites whose zircons yield 2.79 Ga age.

Olginska Suite (AR3ol). According to formational analysis data [5], three volcano-plutonic rock associations (upward) are distinguished in the Suite: lower meta-tholeiite-gabbro-diabase, meta-komatiite-dunite-harzburgite and upper meta-tholeiite-gabbro-diabase. Lower meta-tholeiite-gabbro-diabase association occupies the lowermost position in the Suite column and is characterized by essentially volcanogenic composition while mafic extrusives predominate (up to 90-95% by volume). It is developed over entire periphery of Sorokynskiy greenstone belt being symmetrically replicated in both its limbs. Its thickness in different parts of the belt varies from 45 to 200 m. It is composed of amphibolites, meta-basalts, komatiite meta-basalts, meta-diabase flows, and various quartz-plagioclase-chlorite, quartz-plagioclase-chlorite-actinolite schists connected by gradual reciprocal transitions.

Meta-komatiite-dunite-harzburgite association symmetrically surrounds the marginal parts of Sorokynskiy belt over entire its length. The boundary with lower association in the section is set by abrupt appearance of abundant ultramafic meta-volcanics which are clearly expressed in physical fields by linear positive magnetic and gravity anomalies and comprise the distinct marker horizon. It is developed in the band (exposure width 25-342 m) composed mainly of ultramafic rocks (various chlorite-actinolite, actinolite, tremolite-actinolite as well as serpentine-talc and serpentine-talc-carbonate schists) which are tightly paragenetically linked with mafic volcanics (quartz-plagioclase-chlorite-actinolite schists, amphibolites). In ultramafic volcanics, according to some authors [5], the staking is reconstructed of komatiite lava flows with characteristic spinifex textures. The latter are identified among so called porphyry serpentinites. Their

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phenosrysts include chloritized and serpentinized olivine chaotically distributed in the aggregate of carbonate, talc, serpentine, chlorite and tremolite.

Upper meta-tholeiite-gabbro-diabase association displays distinct composition reflected in essentially pyroclastic mode of mafic (up to 80% by volume) and intermediate-mafic (up to 20%) meta-volcanics. Lower boundary of the association is marked by appearance of abundant intermediate volcanics, strongly reduced amount of ultramafic interbeds and sharp facial change of volcanics from extrusive to pyroclastic (lava-pyroclastic). Mineral composition (in various proportions): quartz+actinolite+chlorite+plagioclase+(epidote). In upward direction the inward (in both syncline limbs) decreasing in thickness of meta-basite and increasing one of meta-sedimentary rocks occur.

Besides volcanogenic rocks, over the whole section of Olginska Suite the litho-facial replacements of these rocks by diverse meta-sedimentary (garnet-biotite-amphibole-quartz sandstones) and ferruginous-quartzite (magnetite and cummingtonite-magnetite quartzites) rocks are observed. The maximum thickness of the latter is defined in the northern part of the belt, in Andriivska site, where it attains first tens of meters.

Plutonic counterparts of associations (dykes and sills) respectively include metamorphosed gabbro-diabases and dunite-harzburgites, and in the schist portion – meta-gabbro-diabases. The rocks are metamorphosed coevally with meta-volcanics and together with the latter constitute paleo-volcanic units.

In lateral direction the Suite column is not persistent by composition and thickness. All known contacts of the Suite with underlaying granitized granulites of Kainkulatska Sequence are tectonic. However, the thick (150 m) batch of meta-sedimentary rocks [38] (two-mica granites with relicts of blasto-psammite textures) that occurs at the Suite bottom (right bank of Berda River, north-eastern limb of belt) coupled with the difference in degree of metamorphism and ultra-metamorphism of Olginska Suite rocks (normally epidote-amphibolite facies) with underlaying granulites or migmatites allows supposing its laying over Zakhidnopryazovska Series with tectonic unconformity. Total thickness of the Suite is up to 700 m.

Average mineral composition of the Suite main rocks types is as follows (%): amphibole-hornblende (50-75), albite-oligoclase (15-30), quartz (up to 16), biotite (up to 10), cummingtonite (0-10), magnetite (up to 10), actinolite, epidote, sphene (up to 5), apatite (2). In places zircon is observed (single grains). Magnetic susceptibility is 120*10-5 CI units, density – 2.96 g/cm3. Amphibole schist of ultramafic composition (%): tremolite (12-69), anthophyllite (0-8), olivine relicts (0-10), actinolite (0-20), serpentine (2-5 to 68-75), chlorite (1-15), carbonate (0-24), talc (0-45), ore mineral (2-13). Magnetic susceptibility is 5839*10-5, density – 2.92 g/cm3.

The rocks of Olginska Suite are favourable for localization of gold mineralization and spodumene pegmatites which control tantalum-niobium and lithium mineralization.

Krutobalkinska Suite (AR3kb). It is developed in the core portion of the belt – mainly in its broadest section of latitudinal extension. The Suite constitutes the core of wedge-shaped syncline overturned to the north-east. Here dipping angles are mainly steep (up to 75-80o). The stratotype Suite section is located on the right bank of Berdyanske water reservoir between Sobacha and Kruta gully mouths.

The Suite column is rhythmic and includes four rhythms at least. At the base meta-sedimentary rocks occur (from sandstones to disputable gravelites) which thickness varies from 30 to 50m; high-alumina (staurolite-, andalusite-, cordierite- and sillimanite-bearing) two-mica and biotite, garnet- and graphite-bearing schist interbeds are contained. In the mentioned high-alumina schists the following mineral content is most variable: garnet (0-65% and more), quartz (10-60%), biotite (0-40%). Muscovite content varies in the range 0-20%, plagioclase – 10-30%, staurolite – 0-10%, sillimanite – 0-10%, andalusite – 0-3%, tourmaline – 0-5%, graphite – 0-3% and iron oxides – 0-25%.

Total thickness of the Suite is about 500 m. The Suite transgressively and probably with angular unconformity overlies the rocks of Olginska Suite.

Clastogenic 3.26 Ga zircons were selected from the Suite basal horizons [2]. Metamorphism of the Suite does correspond to epidote-amphibolite facies.

Staurolite deposit is located in the high-alumina rocks of the Suite. At the present knowledge the rocks of meta-rhyodacite formation are also ascribed to the Suite; these

rocks occupy the uppermost position in the column of Osypenkivska Series and are encountered almost in all parts of Sorokynkiy belt. Composition of volcanics varies from andesite-dacites to rhyolites with rhyodacite and rhyolite predomination. Paleo-type analogues of these rocks include quartz porphyries and quartz albitophyres, variously sheared, sericitized. By these reasons diverse quartz-plagioclase-sericite, quartz-biotite-chlorite-sericite and quartz-sericite schists are widely developed. The rocks unconformably overlie Olginska and Krutobalkinska suites. Radiogenic dating of these rocks is lacking yet. Gold mineralization is spatially related to meta-rhyodacite formation [5].

19

Tsentralnopryazovska Series (AR3cp). It includes metamorphic rocks of Temryutska and Demyanivska suites. The first Suite is developed in its stratotype area – Berestovska syncline in the east of the map sheet while Demyanivska Suite, reversely, in the west, nearby Korsatskiy Fault, in the small allochthonous block.

Tsentralnopryazovska LTZ Temryutska Suite (AR3tm). The Suite is mainly composed of biotite-amphibole, amphibole-two-

pyroxene, two-pyroxene, garnet-biotite, graphite-biotite, biotite-sillimanite plagiogneisses, pyroxene-bearing mafic gneisses, ferruginous and barren quartzites, as well as marbles and calciphyres. The rocks are exposed along Berda River and its branches to the east from Kalaytanivka village (Glyboka and Kalaytanivska gullies), nearby the mouth of Kosolapova gully and along Glodivska gully, along Berestova, Karatyk and Temryuk (Mogyla Visla) rivers, between Starchenkove and Karla Marksa villages. These rocks constitute the large north-north-east-trending Berestovska syncline which north-western and south-western margins are cut by Katerynivskiy and Mykolaivskiy deep-seated faults. Along these breaks the Suite contacts with plagiogneisses of Kainkulatska and Dragunska sequences.

Four sequences are distinguished in the Suite column (upward): carbonate-graphite-garnet, ferruginous-quartzite-amphibolite, gneiss and garnet-sillimanite. The first one is up to 300 m thick and is traced over tens of kilometres in the east and west of syncline. It is mainly composed of calciphyres, marbles, diopside rocks, graphite and garnet plagiogneisses. In the second sequence four-five 10-90 m thick ferruginous quartzite layers alternate with the layers of garnet-biotite and biotite-amphibole-pyroxene plagiogneisses and amphibolites; total thickness of this sequence is up to 900 m. The next gneiss sequence (mainly biotite gneisses and plagiogneisses) is up to 300 m thick. Upper sequence is established in the central part of syncline and is composed of garnet-sillimanite-graphite-biotite plagiogneisses of about 300 m total thickness (see “Geological map of crystalline basement”).

In magnetic field continuous positive anomalies up to 500 nT do correspond to the mafic gneisses and amphibolites, and up to 10-200 nT – to gneisses. In gravity field the lengthy chains of positive anomalies up to 0.9-1.5 mG (mafic gneisses and amphibolites) are set on the background of 0.0-0.9 mG corresponding to the gneiss layers. Average magnetic susceptibility of amphibolites and mafic gneisses is 2960*10-5 CI units, slightly mafic plagiogneisses – 385*10-5 CI units, felsic plagiogneisses – 62*10-5 CI units, marbles – 284*10-5 CI units, ferruginous quartzites – 37600*10-5 CI units. Rock density is 2.9 g/cm3, 2.68 g/cm3, 2.62 g/cm3, 2.82 g/cm3, 3.28 g/cm3, respectively.

Mineral composition of the rocks (%): mafic gneisses: andesine (30-57), hornblende (13-43), diopside (1-17), hypersthene (1-7), biotite (0-3); amphibolites: andesine (40-50), hornblende (40-65), clinopyroxene and biotite (up to 5); plagiogneisses: oligoclase (20-60), quartz (10-30), biotite (5-25), graphite (0-30), garnet (0-25), amphibole (0-15), sillimanite and cordierite also occur in places. Barren quartzites mainly contain (%) quartz (60-98) with minor oligoclase (0-15), microcline (1-10), muscovite (up to 10) and biotite (up to 3). Ferruginous quartzites (%): quartz (30-71), magnetite (12-30), orthopyroxene (20-35), clinopyroxene (up to 3), grunerite, hornblende, garnet. Rarely eulizites occur where quartz content (%) is 20-36, orthopyroxene – 20-37 at relatively low magnetite content (10-25).

By petrochemical features most of Temryutska Suite belongs to sedimentary rocks metamorphosed under granulite facies conditions. Only amphibolites, mafic gneisses and few slightly mafic plagiogneisses can be ascribed to the ortho-range.

Directly for the rocks of Tsentralnopryazovska Series the age is not determined. Their cutting (?) is observed by 2.8 Ga plagiogranites conventionally ascribed to Shevchenkivskiy Complex.

The Suite rocks contain economic reserves of graphite, ferruginous quartzites and high-alumina minerals, as well as skarn-like rocks with scheelite mineralization.

Zakhidnopryazovska LTZ Demyanivska Suite (AR3dm). It is developed in Korsatskiy block only where it constitutes the section of

the same-named ferruginous-quartzite deposit and is fairly well exposed. Total thickness of the Suite is about 500 m. The contacts with underlaying migmatized rocks of Zakhidnopryazovska Series are tectonic.

Three rock batches are distinguished in the Suite: sub-ore, ore and supra-ore ones. Sub-ore batch is quite reduced. The thin (up to 20 m) layers of garnet-biotite gneisses as well as “low-ferruginous” quartzites (apparently of tectonic origin) in the western limb of Korsak-Mogylska syncline are frequently attributed to this unit. Normally the ironiferous batch occurs in contact with migmatized or granitized pyroxene-hornblende host mafic gneisses.

20

The iron-ore batch is up to 200 m thick. Eulisites are widely developed at the footwall and hanging-wall of the batch. Ferruginous quartzites that predominate in the column do form up to five layers (in flexure of the eastern limb). Commonly these are two-pyroxene-magnetite varieties with subordinated garnet-biotite gneisses, amphibolized mafic granulites and minute marbles. Ferruginous quartzites are dark-grey and black banded rocks. Banding is caused by intercalation of quartz-magnetite, quartz-pyroxene-magnetite, quartz-amphibole-magnetite, quartz, amphibole or pyroxene beds. Under microscope the mineral composition is as follows (%): quartz – 50-75, magnetite – 10-42, diopside – 0-10, blue-green hornblende (often developed after pyroxene) – 0-10, ice-colour or slightly-greenish cummingtonite (grunerite) – 0-40, biotite (developed after pyroxene or amphibole) – 0-10, brownish-red garnet – 0-20, very rarely oligoclase (# 20-27) – 0-7; accessories: apatite, pyrite, pyrrhotite. By chemical composition, besides high-grade (Fe2O3 – 38.99; FeO – 10.8), the low-grade (Fe2O3 – 16.18; FeO – 1.76) quartzites of the same mineral composition are distinguished.

In the petrochemical plots the scattering of high-grade and low-grade quartzite points is fairly considerable. They often fall in the field of sandy-clayey sediments and products of their metamorphism and partially in the fields of mafic and intermediate igneous rocks. The Show index (DF) calculated for low-grade quartzites to be 13.15 that corresponds to the para-rocks.

Magnetic susceptibility of the ferruginous quartzites is 12480*10-5 CI units, density – 3.08 g/cm3. Supra-ore batch is divided in two parts and is intersected in DH 5 (depth 1155 m) in the core of Korsak-

Mogylska syncline. Lower part (up to 100 m thick) is of mixed composition and comprises intercalation of garnet-biotite, sillimanite and cordierite gneisses; the upper part (180 m thick) is the batch of mesocratic clinopyroxene-bearing hornblende-plagioclase gneisses.

Plagiogneisses include garnet-biotite, sillimanite-garnet-biotite, in places with cordierite varieties of the following average composition (%): plagioclase – 20-25, quartz – 10-20, sillimanite – 0-10, biotite – 7-20, muscovite – 0-4, garnet – 1-8, graphite – 0-3, cordierite – 0-10; accessories: zircon, apatite, monazite; secondary: chlorite, sericite.

Amphibole biotite-pyroxene-bearing plagiogneisses under microscope have the following mineral composition (%): oligoclase-andesine – 25-40, quartz – 10-15, orthoclase-microcline – 5-10, biotite – 1-10, hornblende – 5-15, diopside – 0-8, epidote – 0-7; accessories: apatite, sphene, zircon, in places rutile, monazite, garnet, xenotime; secondary: carbonate – 0-5, chlorite. Similar rocks are also known in the sub-ore part of the section. Moreover, they are typical for the rim of Saltychanskiy dome and apparently belong to Zakhidnopryazovska Series.

In average biotite plagiogneisses from supra-ore batch are of the following composition (%): quartz – 15-45, sodium oligoclase (# 28) – 30-40, potassium feldspar – 5-20, biotite – 5-25, muscovite – signs; in traces – amphibole, diopside, garnet, in places graphite in smoothed interbeds; accessories: apatite, sphene, zircon, ore minerals.

Magnetic susceptibility of biotite plagiogneisses is 133*10-5 CI units, density – 2.64 g/cm3. Korsak-Mogylskiy block is well-expressed in magnetic and gravity fields. Above the ferruginous

quartzite deposit magnetic field value attains 50000 nT. Residual gravity anomaly (gres) being recalculated to 1.5 km is of 1.5 mG value.

Radiological are is not studied for the rocks of Demyanivska Suite. Among the Suite rocks the ferruginous quartzites frequently occur that form iron-ore deposits. Proterozoic Acrotheme Paleo-Proterozoic (PR1) It is comprised of metamorphic rocks – Dibrovska Suite and Sadova Sequence that have been deposited

in different litho-tectonic zones. Dibrovska Suite is defined only in the west of the map sheet in the eastern part of Orikhivsko-Pavlogradska zone, and Sadova Sequence is only preserved in the south-eastern rim of Saltychanskiy dome (south-east of the map sheet) where it stacks up the Archean column of Sorokynskiy greenstone belt.

Orikhivsko-Pavlogradska LTZ Dibrovska Suite (PR1db). It constitutes so called fault-side monoclines in the eastern fragment of

Orikhivsko-Pavlogradska zone. The monoclines (Kuksungurska, Inzivska, Orlivska and other less studied) that adjoin Korsatskiy Fault are composed of relatively thin (up to 300-400 m, rarely to 1000 m) mixed sequence of variable composition by lateral and in the column. The basement of the Suite comprises migmatized and granitized gneisses of Kainkulatska Sequence which are overlain by the Suite, probably with tectonic

21

unconformity. It is evidenced by the difference in degree of metamorphism (respectively, granulite and epidote-amphibolite or amphibolite facies) and ultra-metamorphism of the sequences under comparison (see “Geological map of crystalline basement”).

The Suite column is most studied in the Kuksungurskiy junction “wedge” of latitudinal and longitudinal monoclines that correspond to Kuksungurske deposit. Here, in the latitudinal band, over biotite-amphibole migmatites with relicts of amphibolites and biotite-amphibole gneisses, does lie the lower productive batch of Dibrovska Suite composed of ferruginous quartzites and schists that form one-to-four layers from 10-15 m to 200 m thick. These are mainly biotite-bearing, amphibole (cummingtonite, actinolite, hornblende) and (or) pyroxene-magnetite rocks of variable composition. The Femagn. content in ferruginous quartzites varies from 20.6 to 40.5%. According to O.M.Makarenko [93], the heavy concentrate at Kuksungur Hills contains magnetite, martite, hornblende, hypersthene, talc, calcite, biotite, apatite, pyrite, chalcopyrite, pyrrhotite, quartz, garnet, pentlandite. Average mineral composition of these rocks under microscope is as follows (%): quartz – 30-55, cummingtonite – up to 10-30, enstatite – 0-8, blue-green hornblende – 0-5, diopside – from single grains to 10; accessories: apatite, garnet, sulphides; of secondary minerals carbonate (up to 10-15) and chlorite (up to 5) are frequently observed; in traces actinolite, grunerite and graphite occur.

Subordinated marble, garnet-biotite and sillimanite gneisses, graphite-bearing in places, lie between the ferruginous-siliceous rocks.

Phlogopite-olivine-diopside amphibole-bearing marbles are locally developed. Their average mineral composition is as follows (%): carbonate – 40-80, diopside – 0-25, phlogopite – 0-10, muscovite – 0-3, olivine (often serpentinized) – 0-20, plagioclase – 0-10, quartz – 0-5, spinel – 0-5, rarely microcline – up to 1; accessories: rutile, zircon, apatite, sphene, magnetite, pyrite, graphite, garnet; secondary: chlorite, talc, serpentine, limonite.

Magnetic susceptibility of marbles is 46*10-5 CI units, density – 2.8 g/cm3. Ferruginous-siliceous rocks are characteristic for the upper parts of productive batch. Supra-ore batch of

the Suite is also mixed in composition and is similar to aforementioned interbeds between ferruginous-quartzites but thickness of marbles, garnet-biotite and high-alumina gneisses is higher – first tens of meters. Thickness of the batch exceeds 100 m.

The Suite composition changes in the eastern part of Kuksungurske deposit. The para-rocks (garnet-biotite gneisses) are only found at the section top while the ferruginous rocks alternate mainly with amphibolites. This makes similar the eastern section type of the deposit with the section of Orlivska zone where clinopyroxene-magnetite quartzites alternate with clinopyroxene amphibolites and meta-ultrabasites (amphibolized pyroxenites, serpentinites etc.).

Amphibolites are most studied in the eastern part of Kuksungurske deposit. Average mineral composition of these rocks is as follows (%): oligoclase, andesine – 30-60, hornblende

– 40-65, clinopyroxene – 0-10, biotite – 0-10, microcline – 1-20, in places quartz – up to 5, magnetite – 0-5, apatite – from single grains to 3; accessories: sphene, zircon; secondary: sericite, carbonate, epidote, chlorite and iron hydroxides.

Radiological age of the rocks is not studied. The Suite rocks are favourable for iron-ore and graphite deposits formation. Zakhidnopryazovska LTZ Sadova Sequence (PR1sd) is known only in the southern part of Sorokynskiy greenstone belt, in 6-8 km

long tectonic block which adjoins the marginal fault bounding the south-western limb of the belt, and is studied only by drill-holes (see “Tectonic scheme”).

Symmetric structure of the block composed of this Sequence allows assumption on the section twinning [38]. If the block structure is considered to be syncline, the Sequence of about 400 m thick could be divided in two batches: lower – meta-terrigenous and upper – graphite-carbonate. The lower batch includes quartzite-schists, two-mica schists, often graphite-biotite with andalusite. The typical blasto-psammite textures are characteristic for the rocks of this batch.

Mineral composition of muscovite-feldspar barren quartzites (quartzite-schists) is as follows (%): quartz – 60-98, oligoclase (# 20) – 7-20, potassium feldspar – 0-15, biotite – 0-2, muscovite – 0-10; accessories: apatite, zircon, ilmenite, magnetite; secondary: chlorite, sericite, iron hydroxides.

Average density of quartzites is 2.63 g/cm3, magnetic susceptibility – 153*10-5 CI units. The average mineral composition of graphite-muscovite-biotite, silicified biotite-graphite schists is as

follows (%): plagioclase – 0-50, quartz – 0-60, graphite – 7-30, biotite – 10-30, muscovite – 0-7, sulphides – up to 5-10; secondary: sericite. Average density of graphite schists is 2.62 g/cm3, magnetic susceptibility – 29*10-5 CI units.

22

There are also observed thin (up to 10 m) layers of marbles and calciphyres. The upper batch is composed of mainly phlogopite-tremolite marbles with subordinate beds of graphite-bearing schists. Micro-breccias of graphite-bearing silicate-carbonate rocks with enclaves of microcline-diopside skarn-type rocks are characteristic.

The mineral composition of the marbles is as follows (%): calcite – 90-98, dolomite – 0-8, diopside – 0-7, tremolite – 1-7, phlogopite – 0-3, muscovite – 0-1, quartz – 0-2; accessories: graphite, magnetite, sphene, tourmaline, rutile, apatite, sulphides.

Average density of marbles is 2.72 g/cm3, magnetic susceptibility – 7*10-5 CI units. Calciphyres are more widely distributed. Their mineral composition (%): calcite – 53-78, tremolite – 4-

17, diopside – 0-3, microcline – 0-5, quartz – 0-3, phlogopite – 5-25, actinolite – 0-15, magnetite – 0-12, graphite – 0-2; accessories: sphene, rutile, tourmaline.

Average density of calciphyres is 2.83 g/cm3, magnetic susceptibility – 39*10-5 CI units. Mineral composition of diopsidites (diopside metamorphic rocks) is as follows (%): diopside – 55-95,

quartz – 0-3, phlogopite – 1-13, microcline – 1-17, carbonate – 0-10, tremolite – 0-7; accessories: sphene – from single grains to 1, graphite, magnetite – from single grains to 1; secondary: aggregate of talc, sericite, carbonate after diopside or tremolite, scapolite, chlorite.

Average density of diopsidites is 2.8 g/cm3, magnetic susceptibility – 67*10-5 CI units. The Sequence unconformably lies over the rocks of Olginska Suite and is metamorphosed under

epidote-amphibolite facies conditions. Isotopic age is not known. In the graphite schists of this Sequence A.M.Snizhko had determined the complex of micro-phitofossils similar to those in Gdantsivska Suite of Kryvorizka Series.

The Sequence rocks host graphite deposits.

PHANEROZOIC Phanerozoic Eonotheme in the map sheet area includes Mesozoic and Cenozoic erathemes. The territory

belongs to Pryazovskiy area [31] where litho-tectonic zones are distinguished with different sedimentation conditions: Chernigivsko-Stulnivska, Prymorska and Chernigivsko-Berestovska (see “Tectonic scheme in the scale 1:500 000” to the geological map of pre-Quaternary units).

Mesozoic Eratheme In the map sheet territory the Mesozoic rocks are developed in two different LTZs – Chernigivsko-

Stulnivska (north) and Prymorska (south) which correspond to the different paleo-geographic and paleo-tectonic environments of sedimentary rocks formation. Jurassic and Cretaceous systems are distinguished in Mesozoic Eratheme (see “Geological cross-section by line A1-A3”).

Jurassic System (J) Middle Division (J2) B a t i a n s t a g e Chernigivsko-Berestivska LTZ Sequence of clays and sands (J2gp). In the territory of L-37-VII (Berdyansk) map sheet Jurassic System

is comprised of Middle Jurassic sequence of clays and sands encountered in Novomykhaylivska Depression and developed only in Chernigivsko-Stulnivska LTZ. The rock distribution area is located in between Novomykhaylivka and Kryzhchyne villages. The Sequence lies directly over Precambrian rocks, particularly, over residual products of weathering crust after crystalline rocks. In turn, it is overlain by Neogene clays and sands or by Quaternary sediments. Southern boundary of Middle Jurassic Sequence is caused by Novomykhaylivskiy Fault (Fig. 2.1). The footwall altitudes vary from +40 m (in the core of Depression) to +130 m (at the northern boundaries). Maximum thickness of the Sequence is encountered in the core part of Novomykhaylivska Depression where it attains 106.7 m.

23

Fig.

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24

The facial composition of the Sequence corresponds to the lagoon and lake-swamp sedimentation environments. By lithology these are light-grey, greenish-grey, argillite-like, micaceous clays, fine-banded due to involved fine-grained sandy material, in places pyritized, with fauna and coalified fossil remnants, rarely with siderite concretions. In the lower parts the clays are mainly beidellite in composition, and in the upper part – montmorillonite one.

The sand interbeds (particularly, at the Sequence bottom in the core part of Depression) 2-5 m thick are encountered. The sands are quartz, diverse-grained, with coalified fossil detritus. Rarely interbeds of thin dark-grey, horizontally-layered, essentially quartz (up to 50%) micaceous with clayey-ironiferous cement aleurolites are observed.

The age of the Sequence is determined by palinological studies. The spore-pollen complex is found in the clays with Coniopteris sp., Cyathea sp., Phlebopteris sp., P. exarnatus Bolch., as well as Selaginella rotundiformis K-M. and others [91] suggesting for Middle Jurassic age of the rocks. I.M.Yamnychenko had determined fauna of Ferganoconcha sibirica Tcheri., Ferganoconcha shabarovi Tcheri., Anisocardia sp. [91] which were abundant in the Early-Middle Jurassic times.

Cretaceous System (K) Cretaceous System includes reduced Lower and Upper divisions composed of marine and continental

facies rocks. Sedimentation environments in the southern and northern parts of the territory were essentially different

in Cretaceous time. In Chernigivsko-Stulnivska LTZ Cretaceous rocks include Lower Cretaceous sandy-clayey sequence (Aptian and Albian undivided) of Upper Cretaceous sandy sequence. In Prymorska LTZ the Lower Cretaceous sediments include clayey-sandy sequence (K1gp) (being correlated with Aptian stage) and Lunacharska Suite (being correlated with Albian stage); Upper Cretaceous sediments include Genicheska (being correlated with Senomanian stage) and Berdyanska (Turonian-Cognacian undivided) suites and sequence of sandy rocks and marls (Campanian age).

Lower Division (K1) A p t i a n s t a g e Prymorska LTZ Clayey-sandy Sequence (K1gp). In the map sheet territory it is encountered in Berdyanskiy Graben and

belongs to Prymorska LTZ. The northern boundary of Sequence distribution is tectonic (coincides with Berdyanskiy normal fault) and is set along the line of Novopetrivka-Novovasylivka-Shevchenko villages. The Sequence lies directly over Precambrian basement and is overlain by Genicheska and Berdyanska suites (Upper Cretaceous Division) and Neogene sediments. The footwall and hanging-wall are stair-like due to block motions. Altitude of the footwall plunging toward the sea varies from -870 m to -360 m. Maximum thickness of the Sequence is 25 m (see “Map of pre-Quaternary units”, DH 64 (column)).

In Berdyanskiy Graben the Sequence is comprised of the continental (north-western part) and coastal-marine facies which boundary is set nearby Lunacharske village (Fig. 2.2).

At the bottom of continental-facies section ash-grey, sandy, oblique-layered clays with abundant coalified fossil remnants are observed. Higher up the clays are being changed by secondary kaolines and kaolineous sandy clays that further are replaced by kaolineous diverse-grained sands with numerous coalified fossil remnants and pyrite bunches. At the Sequence top there are encountered ash-grey feldspar-quartz sandstones, fine-grained with siliceous-clayey cement, with coalified fossil remnants, and glauconite and pyrite inclusions. Thickness of the continental-facies sediments is 16 m.

According to the data of S.Ya.Egorova, in the clays and sands the spores Gleicheniaceae, Schizaceae and Selaginella і Licopodium and pollen Cedrus are determined suggesting for the sediments formation under conditions of swamped land in the wet and hot climate.

The coastal-marine facies are more widely distributed and occupy almost entire Berdyanskiy Graben. By lithology this is uniform sandy sequence with minute thin interbeds of secondary kaolines and clays. The sands are grey to dark-grey, fine-grained, quartz with glauconite traces, non-carbonate, with coalified fossil remnants, as well as with ilmenite, zircon, garnet, rutile, and tourmaline grains in the heavy fraction.

Sandstones with silica clay-montmorillonite cement, from 0.5 to 12.0 m thick are much rarely observed. The clays are dark-grey, thin-layered, micaceous. Thickness of the sediments varies from 0.8 to 25.0 m

(in the eastern and southern directions).

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The age of sediments is determined by palinological studies provided by A.A.Mikhelis and V.I.Uziyuk [59]. The following spore-pollen complex is determined: spores – Gleicheniaceae, Coniopteris sp., Cyathea sp., Coniogramma, Pteridium, Anemia, Lygodium, Sphagnum; pollen – Cedrus sp., Podocarpaceae, Pinaceae, Caytonia sp., Naxidiaceae.

A l b i a n s t a g e Lunacharska Suite (K1ln) is known in Prymorska LTZ, in the eastern marginal part of Obitochnenskiy

Graben, in crystalline basement dimples. In Berdyanskiy Graben occurrence of the Suite is possible but not supported by fauna. The Suite is composed of spongolites with minor interbeds of sandstone and marine-facies silica-clay-like clays (Fig. 2.2).

Spongolites are dark-grey to black rocks, massive, non-carbonate, unclear-layered due to fine-grained sand interbeds. Siderite ore occurrences are para-genetically linked with spongolites. Sandstones are ask-grey, fine-grained, quartz with glauconite, non-carbonate. Silica-clay-like clays occur at the bottom of the section. These are dark-grey, massive, carbonate rocks with considerable traces of mica and opal, with fauna imprints (brachiopod, foraminifera, sponge spicules, radiolarian). Thickness of Lunacharski sediments is 20 m.

The rocks age is determined by L.F.Plotnikova [59] by foraminifera complex: Parmula cf.asiatica Furss., Anomalina cf. slavutichi Kart., Gavelinella cf. biinvoluta Mjatl.

A p t i a n a n d A l b i a n s t a g e s u n d i v i d e d Chernigivsko-Berestivska LTZ Sandy-clayey Sequence (K1pg) is established in Stulnivska and Chernigivska depressions, in crystalline

basement dimples, and is ascribed to Chernigivsko-Stulnivska LTZ. By facial appearance the Sequence is divided in two batches: lower continental and upper coastal-

marine ones (Fig. 2.1). The lower batch lies directly over the weathering crust after crystalline rocks. The footwall altitudes vary from +65.0 m to +130.0 m. Thickness of the batch in Chernigivska Depression is 18.0 m, in Stulnivska Depression – 35.0 m.

In Stulnivska Depression the lower batch is composed of dark-grey, quartz, diverse-grained sands, at the bottom – gravelous, with coalified fossil remnants, as well as with secondary kaolines. Thickness of kaoline seams is 1.0-3.0 m.

In Chernigivska Depression the column is similar but interbed thickness attains 8.0 m. The upper batch is encountered in Chernigivska Depression only. These are sands, clays and sandstones

of coastal-marine, lagoon facies. The sands are dark-grey to black, quartz, diverse-grained, with glauconite, rarely micaceous, with coalified fossil remnants. The clays are dark-grey, coaliferous, with glauconite. Sandstones are grey, greenish-grey, with glauconite, cement is siliceous. Total thickness of the Sequence is 37.0 m.

In the rocks A.K.Kolomiytseva had determined the spore-pollen complex: Gleichenia laeta Bolch., Gl. stellata Bolch., Gl. umbanata Bolch., Gl. angulata Bolch., as well as Coniopteris sp., Selaginella sp., Hausmania sp Weakly-preserved fauna remnants are observed.

Upper Division (K2) Upper Cretaceous sediments are widespread in both LTZs under consideration. In Chernigivsko-

Stulnivska LTZ these comprise Campanian sandy sequence. In Prymorska LTZ these include Genicheska Suite (Senomanian), Berdyanska Suite (Turonian-Cognacian undivided) and Campanian sequences of sandy rocks and marls. Lack of many subdivisions in the section is caused by the vertical block motions and sediments erosion at the elevated parts of the territory (see “Geological cross-sections by line B1-B4”).

S e n o m a n i a n s t a g e Prymorska LTZ G e n i c h e s k i y r e g i o - s t a g e Genicheska Suite (K2gn) is developed over entire Berdyanskiy Graben (Prymorska LTZ). With

discontinuity it lies over Lower Cretaceous rocks, in places over weathering crust after crystalline rocks, and is

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overlain by Berdyanska Suite and the sequence of sands and marls. The footwall plunges in the eastern direction, its altitudes vary from -131 m to -950 m. Thickness of the Suite attains 80 m (Fig. 2.3).

Coastal-marine facies comprise the sandy sediments with interbeds of clays, marls, tripoli, silica clays and spongolites (the latter – in the western edge of Graben only). In the northern part of Graben carbonate sediments lie at the column bottom.

The sands are grey, greenish to bright-green, glauconite-quartz, diverse-grained, non-carbonate, with minute fauna fragments. In the heavy fraction the following minerals are found: ilmenite, zircon, siderite, glauconite, phosphorite, pyrite.

Sandstones are greenish-grey, fine-grained, essentially quartz, glauconite-quartz with clayey cements, with fauna little fragments and imprints.

The clays are dark-grey with greenish shade, sandy, thickness up to 6 m. Marls are light-grey to white, sandy in places, composed of fine-grained calcite (57-80%) and clayey

material (15-20%), with minute foraminifera and ostracoda fragments; thickness from 3 to 14 m. Tripoli and silica clays are light-grey, greenish-grey, from 4 to 27 m thick. Spongolites are grey with greenish shade, aleurite-clayey, with glauconite gains. The Suite age is determined by L.F.Plotnikova and A.P.Vasyutyna [59] by foraminifera: Anomalina

senomanica Brotz., Anomalina globosa Brotz., A. berthelini Kell., Tritaxia tricarinata Reuss. T u r o n i a n a n d C o n g a c i a n s t a g e s u n d i v i d e d Berdyanska Suite (K2bd) is encountered within Berdyanskiy Graben. With discontinuity it lies over

Genicheska Suite and is overlain by the Campanian sequence of sandy rocks and marls, in places by Neogene sediments. The Suite distribution area is bounded in tectonic mode; the footwall plunges in southern and eastern directions, their altitudes vary from -100 m to -860 m. Thickness varies from 27 m to 120 m (see “Map of pre-Quaternary units”, DH 64 (column).

In facial respect, the Suite is composed of marine (limestones, marls, chalk) and coastal-marine (tripoli, sands, sandstones) facies. Marine sediments are confined to the Suite lower part and are encountered in the central, southern and western parts of Graben (Fig. 2.4).

Limestones often are chalk-like, essentially calcite, light-grey, massive, micro-grained rocks containing up to 1% of fine quartz and glauconite grains, as well as flint and mollusc fragments. Thickness of limestones attains 30 m.

The marls are developed in the central and western parts of Berdyanskiy Graben. These are light-grey, massive, sandy rocks with abundant flint kernels, organogenic detritus, rarely with quartz and crystalline rock fragments. White opal is observed by fractures. Thickness of the marls attains 26 m.

The chalk is encountered in the central and western parts of Graben. This is white uniform rock with a few sandy material and flint fragments. Main mass of the rocks is composed of organogenic detritus, single glauconite, quartz and mica grains occur. Thickness is up to 10 m. The chalks and marls contain up to 10-15 cm thick interbeds with flint kernels.

Tripoli (diatomite) rocks are known mainly in the northern part of Graben. These are light-grey to white, spotty in places, light rocks with flint kernels up to 5 cm in size. Siliceous aggregates of opal-chalcedony composition with minor sponge spicules comprise up to 15%. Thickness of tripoli attains 20 m.

The sands and sandstones constitute upper part of the Suite section. The sands are light-grey, fine-grained, quartz, calcareous, with glauconite traces, up to 32 m thick. Sandstones are grey, light-grey, fine-grained, quartz, with minor feldspar and glauconite grains, cavernous, brittle, with calcareous-siliceous cement. At the bottom the black flint fragments occur. Siderite ore occurrences are para-genetically linked with sandstones. Thickness of sandstone layer is up to 91 m.

The marls and sandstones are favourable for flammable gas occurrences. A.P.Vasyutyna [59] had determined in marls and chalks: foraminifera Reusella turonica Akim.,

Anomalina globosa (Brotz.), A. kelleri Mjatl.,A. ammonoides (Reuss.) (Lower Turonian); macro-fauna Liostrea cf. boncheroni (Cog.), Lima cf. cretasea Woods. (Cognacian-Santonian).

C a m p a n i a n s t a g e The rocks are encountered in Chernigivsko-Stulnivska and Prymorska LTZ (the north and south of the

map sheet respectively). Sequence of sandy rocks and marls (K2pm). In Prymorska LTZ is fills up both Berdyanskiy and

Obitochnenskiy grabens. It transgressively lies over Precambrian rocks, Lower Cretaceous sediments and Berdyanska Suite. In Berdyanskiy Graben the footwall plunges in the southern direction, its altitudes vary from -

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200 m to -630 m; in Obitochnenskiy Graben – from -226 m to -280 m. Thickness of the Sequence is 50-200 m and 50-70 m respectively.

The rock lithology of the Sequence does correspond to coastal-marine and shallow-water marine sedimentation environments – sands, sandstones, limestones and marls (Fig. 2.5).

The marls are widespread in the buried portion of Berdyanskiy Graben. These are grey, light-grey, massive, sandy rocks with mollusc imprints and shells. In places sponge spicules, coral imprints, belemnite cores, as well as coalified fossil remnants occur. The marls contain up to 40-73% of carbonate, up to 20-25% of clay material, and 5-7% of fragments. Almost 50% of the rock is composed of organogenic detritus. Sandy material includes glauconite and quartz. Thickness of the marls attains 114 m (in the south of Graben). The marls and sandstones are favourable for flammable gas occurrences.

Limestones are developed in both grabens. These are light-grey organogenic oolite rocks with traces of sandy and clayey material, with shell remnants, quartz and black flint fragments. Thickness is up to 13 m.

The sands are greenish-grey, fine-medium-grained, quartz, non-carbonate, with thin interbeds (up to 0.5 m) gravel-pebble material of quartz, flints and shell fragments. As it is revealed from mineralogical studies, the sands contain ilmenite, zircon, leucoxene, siderite and glauconite. In the marginal part of graben the sands are coarse-grained up to gravelous. Thickness is up to 55 m.

Sandstones are widely developed and often intercalate with marls, limestones and sands. These are grey with greenish shade, fine-grained, quartz, glauconite-quartz rocks, massive, with clayey-carbonate cement, with shell imprints. Siderite ore occurrences are para-genetically linked with sandstones. Thickness of sandstones is up to 30 m.

In the northern part of Berdyanskiy Graben silica clay and silica-clay-like clay 6-9 m thick interbeds are encountered.

According to A.P.Vasyutyna [59], in some drill-holes the Suite is divided in two zones by foraminifera complexes established. The lower zone (38-44 m thick) composed of marls and sandstones, contains the following foraminifera: Anomalina variata Plotn., A. clementiana (Orb.), Cibicides aktulagayensis Vass.The upper zone (up to 100 m thick) composed of marls with sandstone interbeds, contains the following foraminifera: Anomalina сomplanata Reuss., A. midwagensis (Plumm.), Cibicides nuricatus Lipn., Globorotalites emdyensis Vass.

Chernigivsko-Berestovska LTZ Sandy sequence (K2p). In Chernigivsko-Stulnivska LTZ this Sequence is defined in Chernigivska and

Stulnivska depressions. In Chernigivska Depression it is divided in two parts. In the lower part the terrigenous sediments are developed – greenish-grey diverse-grained quartz sands with glauconite, and grey, dark-grey, horizontally-layered clays. The upper part is composed of white silica clays and silica-clay-like rocks with glauconite (Fig. 2.1). With discontinuity the Sequence lies over Irshanska Suite rocks and over weathering crust after Precambrian rocks; the footwall altitudes vary from +90 m to +140 m. It is overlain by Neogene, Paleogene and Quaternary sediments. Thickness varies from 5 to 30 m.

In Chernigivska Depression ilmenite placers are para-genetically linked with the sandy rocks of sea basin coastal line. Discovery of zircon placers is also possible.

The Sequence is not characterized by fauna. In places weakly-preserved fauna occurs. The rock age is determined by analogy with fauna-supported sediments in Tarasivka village area [91].

In Stulnivska Depression the Sequence with discontinuity lies over the rocks of Irshanska Suite and over weathering crust after Precambrian rocks. These are terrigenous rocks: grey, greenish-grey, quartz, diverse-grained sands and gravelites at the bottom, as well as sandstones of similar composition, with kaolineous or ironiferous cement. Mentioned sandstones are confined to the section bottom and siderite ore occurrences are para-genetically linked with these rocks.

In Stulnivska Depression A.F.Samarska [91] had determined in the Sequence rocks the following micro-fauna: Bolivinoides delicatulus Cush., Globigerina sp., Bolivina planta Car., Anomalina baltica (Brotz.). According to A.A.Mikhelis data, the sediments contain spore-pollen complex where pollen Oculopollis sp., Zonganulopollis sp., Triporopollenites sp. predominate. The complex also includes Pseudovacuopolis sp., Plicapollis sp., Trudopollis sp., Cedrus sp., Pinus sp., and spore Sphagnum sp., Ligodium sp.

Cenozoic Eratheme Cenozoic rocks in the L-37-VII (Berdyansk) map sheet are comprised of Paleogene, Neogene and

Quaternary systems.

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Paleogene System (P) Paleogene System is known in Prymorska and Chernigivsko-Stulnivska LTZ (see “Geological cross-

sections by lines A1-A3 and B1-B4” in the “Map of pre-Quaternary units”). Paleogene column in both zones is incomplete, it is not subdivided in details due to lack of palinological data, and comprises Eocene only. In Prymorska LTZ occurrence of undivided Eocene Alminska and Khadzhybeyska suites is confirmed by fauna; these units lie over the Sequence of sands and clays which is defined by lithologo-facial features and in time is coeval to undivided Simferopolskiy and Bakhchysarayskiy horizons. In Chernigivsko-Stulnivska LTZ, upon lithology comparison of studied sediments and those in adjacent areas it was defined the sequence of sands and clays overlain by the clayey-sandy sequence.

Eocene S i m f e r o l o p s k i y a n d B a k h c h y s a r a y s k i y r e g i o - s t a g e s u n d i v i d e d Sequence of sands and clays (P2pg). In Prymorska LTZ the Sequence is developed in both Berdyanskiy

and Obitochnenskiy grabens. In Berdyanskiy graben with discontinuity it lies over Upper Cretaceous sequence of sandy rocks and marls; the footwall in stair-like mode plunges in southern direction, its altitudes vary from -140 m to -400 m. It is overlain by Neogene sediments. In Obitochnenskiy Graben the Sequence with interruption lies over Upper Cretaceous sequence of sandy rocks and marls and over weathering crust after Precambrian rocks; in this case the footwall also in stair-like mode plunges in southern direction, and its altitudes vary from -170 m to -250 m. It is overlain by undivided sediments of Alminska and Khadzhybeyska suites (see “Geological cross-sections by lines A1-A3 and B1-B4” in the “Map of pre-Quaternary units”).

The Sequence includes continental facies: intercalation of grey, dark-grey feldspar-quartz, diverse-grained sands, dark-greenish-grey to black kaolineous clays and white sandy secondary kaolines (Fig. 2.6). All rocks contain individual remnants and entire interbeds of coalified fossils. In the central part of Berdyanskiy Graben, where sands predominate, thickness of sediments attains 16 m; in the south, where kaolines predominate, rock thickness attains 79 m. The highest total thickness of the section (in the south of Berdyanska sandbank) attains 184 m. In the rocks A.A.Mikhelis had determined the spore-pollen complex: Betula sp., Corylus sp., Alnus sp., Triciporopolenitessp., Triatriopollenitessp.

At the same time, in Chernigivsko-Stulnivska LTZ sea basin regression occurred with formation of swamps and plant development. Due to further erosion the Sequence is preserved in Stulnivska Depression only where it is reduced in thickness. With discontinuity it lies over Upper Cretaceous sediments; the footwall altitudes vary from +33 m to +70 m. It is overlain by Neogene rocks and Eocene clayey-sandy sequence.

The Sequence comprises intercalation of dark-grey to black, with coalified fossil detritus, from 0.8-3.0 m thick clays, feldspar-quartz sand interbeds (up to 1 m thick), and brown coal (up to 1.5 m thick) which occurrence is indicated in the map. The highest thickness attains 54 m.

The rock age is defined taking into account the rocks position in the column and by litho-facial features. A l m i n s k i y a n d K h a d z h y b e y s k i y r e g i o - s t a g e s u n d i v i d e d Prymorska LTZ Alminska and Khadzhybeyska suites undivided (P2al-hd). This straton is established in Obitochnenskiy

Graben only. With discontinuity it lies over Eocene clayey-sandy sequence (P2pg) and over weathering crust after Precambrian rocks; the footwall plunges in southern direction with altitudes from -130 m to -170 m (see “Geological cross-section by line B1-B4” in the “Map of pre-Quaternary units”).

The rock facies changes in western and eastern directions from marine to coastal-marine are observed (Fig. 2.7). Marine facies include greenish-grey, calcareous, sandy clays, in places pyritized, with shell remnants, and calcareous sandstones.

The coastal-marine facies include greenish-grey to dark-grey, sandy, in places kaolineous clays, with coalified fossil remnants; quartz, coaliferous sands are encountered only in the southern part of the distribution area. Thickness of sediments attains 35 m.

Rock age is determined by D.E.Makarenko by fauna remnants: Chamys idoneus Wood., Vulsella sp., Pseudomissium corneum Sow.; and by E.Ya.Kraeva by foraminifera: Сibicides pygmeus Hantk., Acarinina rotundimarginata Subb., A. bullbroki Boll., Globigerina eocenica Targ.

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Chernigivsko-Stulnivska LTZ Clayey-sandy sequence (P2gp) is developed in the north of studied area in Chernigivsko-Stulnivska

LTZ, particularly, in Stulnivska and Chernigivska depressions. In Stulnivska Depression the Sequence with discontinuity lies over Upper Cretaceous sediments and

over Eocene clayey-sandy sequence; the footwall altitudes vary from -40 m to -100 m. It is overlain by Neogene and Quaternary rocks (see “Geological cross-sections by line A1-A3” in the “Map of pre-Quaternary units”).

Coastal-marine and lagoon facies are intricate in composition. At the bottom coarse-grained and gravelous sands and sandstones occur, in places with siliceous, ironiferous cement. Higher up in the section appear greenish-grey clays with coalified fossil remnants, then 1-20 m thick kaoline-bearing quartz and quartz-feldspar sands and sandstones with clay interbeds. Total thickness of sediments attains 38 m.

In Chernigivska Depression the Sequence is developed in the narrow band in the eastern part with tectonic boundaries by Chernigivskiy normal fault. With discontinuity the rocks lie over Upper Cretaceous sediments; the footwall altitudes vary from +117 m to +168 m. The rocks are overlain by Neogene and Quaternary sediments.

The coastal-marine facies include grey quartz diverse-grained sands, gravelites, breccias and conglomerates with granite fragments and carbonate-clayey cement (Fig. 2.1). Thickness of these rocks in Chernigivska Depression attains 20 m.

The rock age is defined taking into account the rocks position in the column and by litho-facial features. Neogene System (N) Sections of Miocene and Pliocene divisions of Neogene in the studied map sheet are somewhat reduced.

Whole area of Prymorska LTZ is covered with Neogene rocks that comprise marine facies. To the north of the line Mykolaivka-Novovasylivka-Novopetrivka villages up to the northern boundary of the map sheet there are developed the separated sediment remnants of Neogene internal-continental basins formed in the common paleo-geographic environments and united in Chernigivsko-Berestovska LTZ. It should be noted that the boundary between these two units was not stable in the Neogene time.

Miocene In Chernigivsko-Berestovska LTZ Miocene includes Novopetrivska Suite of Poltavska Series

(undivided Lower-Middle dividions of Miocene), sandy-clayey sequence and sequence of parti-coloured clays. In Prymorska LTZ Middle Miocene sediments are developed – undivided Sartaganski and Konkski layers, as well as Upper Sub-Division – layers of Sarmatian regio-stage and limestone sequence of Pontian regio-stage.

Lower and Middle Miocene undivided Chernigivsko-Berestivska LTZ P o l t a v s k i y r e g i o - s t a g e Poltavska Series Novopetrivska Suite (N1np). Starting from Early Miocene the territory to the north of the line

Mykolaivka-Novovasylivka-Novopetrivka villages had the common sedimentation environments and history of development thus these rocks are ascribed to the so called Chernigivsko-Berestovska LTZ. Continental sedimentation environments predominated over this territory in Early-Middle Miocene and respective sediments are combined in Novopetrivska Suite.

Some areas of the Suite rocks development are known in Chernigivsko-Berestovska LTZ. The biggest ones are located in Novomykhaylivska, Chernigivska and Stulnivska depressions; the boundaries of the Suite rocks in places are controlled by faults. With discontinuity the Suite lies over weathering crust after Precambrian rocks, as well as over Jurassic (Novomykhaylivska depression) and over Paleogene and Upper Cretaceous (Chernigivska and Stulnivska depressions) rocks (Fig. 2.1). The Suite footwall altitudes vary from +160 m (Novomykhaylivska depression) to +110 m (Stulnivska depression). And the footwall altitudes of some small

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rock enclaves developed along the southern boundary of Chernigivsko-Berestovska LTZ are +30 … +20 m. The sediments are overlain by Pliocene and Quaternary rocks.

The rocks were forming in the continental environments (internal basins, rivers, streams). In lithology, the Suite comprises intercalation of secondary kaolines, white kaoline sandy clays and light-grey, quartz, diverse-grained (from aleuritic to coarse-grained), high-clayey sands, gravels and gravelites. Sands and clays often contain iron-enrichment stains. Thickness of the Suite attains 40 m.

The Suite does not contain any fauna. Rock age is defined through comparison with the studied sections of Novopetrivska Suite in the neighbouring areas.

Middle Miocene In the map sheet Middle Miocene includes undivided Sartaganski and Konkski layers in Prymorska

LTZ. Prymorska LTZ Sartaganski and Konkski layers undivided (N1sr-kn). Formation and erosion of these layers in

Prymorska LTZ strongly depended on tectonic activity of the area. The rocks with discontinuity lie over Paleogene and Cretaceous sediments. The northern boundaries of the layers are extended out Berdyanskiy Graben up to Novovasylivka village while over remaining territory after Sarmatian transgression just a few sites (in between Lozovatka and Obitochna rivers and to the west of Prymorsk town) are preserved. The footwall plunges in the southern direction with altitudes ranging from -110 m to -300 m (see “Geological cross-section by line B1-B4” in the “Map of pre-Quaternary units”).

Undivided Sartaganski and Konkski layers include coastal-marine (carbonate and terrigenous) facies (Fig. 2.8). Carbonate sediments comprise grey organogenic limestones that alternate with dark-grey detrito-quartz sandstones; the rocks are encountered mainly in around Obitochnenskiy Graben. Thickness of limestones attains 3.7 m. Terrigenous sediments in Berdyanskiy Graben include grey, dark-grey, thin-layered, calcareous clays and grey, feldspar-quartz, diverse-grained, calcareous sands that alternate with gravel-pebble interbeds (0.1-1.7 m). Thickness of the sands is up to 5 m. Total thickness of Konkski layers is 27 m.

The age of Konkski sands is determined by V.G.Kulichenko based on molluscs: Modiolus incrassatus (Orb.), M. buglovensis (Orb.), Cardium andrussovi Sok., Ervilia pussila Phil., E. trigonula Sok., Mactra ex gr. basteroti Mauer., Corbula michalskii Sok., and others.

Upper Miocene S a r m a t i a n r e g i o - s t a g e Sarmatian regio-stage of Upper Miocene in Prymorska LTZ includes three sub-regio-stages. Pontian

regio-stage in the studied area is not divided. In Chernigivsko-Berestovska LTZ in Sarmatian time was forming the clayey-sandy sequence of internal-continental basins, and in Pontian time – terraces of ancient rivers and parti-coloured clays.

L o w e r S a r m a t i a n s u b - r e g i o - s t a g e Kuzhorski and Zbruchski layers undivided (N1kh-zb). The northern boundary of these layers is set by the

line Inzovka-Obitochniy-Banivka-Shevchenko-Novovasylivka-Osypenko villages. With discontinuity the layers lie over Cretaceous, Paleogene and Konkski sediments and over weathering crust after Precambrian rocks. In turn, the rocks are overlain by Cimmerian and Middle Sarmatian sediments. The footwall is irregular, stair-like, plunging in the south-eastern direction with altitudes from -50 m to -250 m.

Coastal-marine facies of incipient sea transgression comprise grey, dark-grey, fine- and medium-grained quartz sand with shell fragments, with interbeds of gravelous sands, sandstones with carbonate cement, organogenic limestones, as well as dark-grey thin-layered clay (Fig. 2.9). Minor occurrences of flammable gases are linked with clayey-sandy rocks.

The final period of sedimentation is comprised of dark-grey to black clays, thin-layered due to fine-grained quartz sand, often with fragments of minor thin-wall shells. The interbeds of calcareous sandstones and sandy limestones occur in places. Thickness of clayey sequence varies from 5 to 39 m. Abundant organic remnants in the clays suggest for warm climate in time of sedimentation. Total thickness of the layers is up to 70.0 m.

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The rock age is determined by V.G.Kulichenko based on Lower Sarmatian fauna: Ervilia dissita (Eichw.), Ervilia trigonula Sok. According to Z.N.Satanovska, the micro-fauna is as follows: Quinqueloculina reussi (Bogd.), Articulina problema Bogd., Elphidium macelum (E. et M.), Nonion bogdanowicsi Volosh.

M i d d l e S a r m a t i a n s u b - r e g i o - s t a g e Novomoskovski, Vasylivski and Dnipropetrovski layers undivided (N1nm-dn). These sediments in the

most part of Prymorska LTZ are eroded and preserved only to the east of Osypenko village, where the rocks are traced in the narrow band in the eastern direction outside the studied map sheet, and in Berdyanskiy Graben. The sediments transgressively lie over Precambrian and Lower Sarmatian rocks and are overlain by the sequence of iron-enriched sandstones. The footwall altitude is in the range from -20 m to -30 m, and in Berdyanskiy Graben – from -100 m to -180 m.

The sediments comprise the shallow-water marine facies (Fig. 2.10). These are light-grey, essentially calcite oolite limestones with large shell remnants, shelly limestones; the interbeds of greenish-grey thin-layered clays and quartz sands with fauna remnants also occur. Total thickness of the layers is up to 35 m.

Middle Sarmatian rock age is determined by V.G.Kulichenko based on fauna: Cardium ex gr. ingratum Koles., Cardium absoletum Eichw., Mactra fabreana Orb., Mactra vitaliana Orb., Paphia gregaria Goldf., Hidrobia pseudocaspia Sinz. Yu.M.Pylypenko had determined in the rocks the spore-pollen complex: Ulmus sp., Zelkova sp., Quercus sp., Betula sp., Salvinia sp.

U p p e r S a r m a t i a n s u b - r e g i o - s t a g e Katerlezski and Geliksovi layers undivided (N1kt-gl) are preserved from erosion over Cimmerian

transgression only in depressions of Prymorska LTZ and in the map sheet area are developed from Gyunivka village to Berdyanske village. Their southern boundary coincides with the northern boundary of Akchagylski sediments. The layers unconformably lie over Precambrian rocks and are overlain by Pliocene or Quaternary sediments.

Being locally developed, the rocks of shallow-water marine facies are fairly intricate in composition (Fig. 2.9). Grey clays with iron-enrichment stains, greenish-grey diverse-grained quartz sands, diverse-grained sandstones with calcareous cement and shell remnants, yellowish-white organogenic limestones, and marls alternate in various combinations and with essential thickness variations. Total thickness of the layers is up to 24.0 m.

In the limestones V.G.Kulichenko had determined Mactra ex gr. caspia Eichw., Mactra bulgarica Toul. Chernigivsko-Berestivska LTZ Clayey-sandy sequence (N1gp) is developed in the individual enclaves over entire Chernigivsko-

Berestovska LTZ. It unconformably overlies Precambrian rocks and their weathering crust, and in Novomykhaylivska Depression – Middle Jurassic rocks filling up the dimples in relief. It is overlain by Quaternary loams. The footwall altitudes in the north attain +162 m, and in the south – +36 m.

The Sequence is composed of the coastal-marine facies rocks. These are grey feldspar-quartz, slightly-calcareous, diverse-grained to gravelous sands with interbeds of carbonate-cement sandstones, and grey, dark-grey, greenish-grey, sandy clays with carbonate and gypsum inclusions. Total thickness of these rocks is up to 28.2 m.

P o n t i a n r e g i o - s t a g e Prymorska LTZ Sequence of oolite and shelly limestones (N1v) is developed in the north-eastern part of Prymorska LTZ,

on the slopes of Berda River in between Mykolaivka and Osypenko villages, and in the individual enclaves. The southern boundary of sediments coincides with the northern boundary of the Akchagylskiy regio-stage sequence of clays and sands. The Sequence unconformably overlies Precambrian rocks and their weathering crust, as well as undivided Miocene Katerlezski and Geliksovi layers. The Sequence footwall altitudes vary from +36.0 m in the north to +3.8 m in the south of its distribution area. It is overlain by red-brown clays and Quaternary loams.

The Sequence is composed of the shallow-water marine facies rocks: oolite and shelly limestones alternate with clays, sands and sandstones (Fig. 2.10).

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35

Limestones are white, grey with brown iron-enrichment stains, sandy, clayey, cavernous oolite or shelly

(composed entirely of mollusc shells and blue-green algae). The clays are grey with greenish shade, with brown stains, sandy, carbonate, mainly montmorillonite in

composition. The sands are greenish-grey with brownish shade, quartz with minor feldspars, clayey, diverse-grained

with limestone and shell fragments. The age of sediments is determined by V.G.Kulichenko and G.I.Molyavko by fauna: Dreissensia

rotiformis Dech., D. simplex Barb., Congeria novorossica Sinz., Prosodacna ex gr.litoralis Sichw., Monodacna pseudocatilus Barb., Didacna sp.

Thickness of sediments attains 25 m. Chernigivsko-Berestivska LTZ Sequence of parti-coloured clays (N1sg) is locally developed in the northern part of Chernigivsko-

Berestivska LTZ, specifically, to the east of Novomykhaylivka village. The site of rocks development is isometric – up to 1 km in diameter. The Sequence unconformably overlies Precambrian crystalline rocks and their weathering crust, as well as Miocene clayey-sandy sequence. The Sequence footwall altitudes vary in the range from +164 m to 180 m. It is overlain by the sequence of red-brown clays and Quaternary sediments.

The clays are parti-coloured, kaolineous, sandy, in places at the bottom quartz pebble and carbonate newly-formed aggregates occur. The clays were forming in continental basins, fairly shallow-water and periodically drying up.

The Sequence age is defined on the ground of stratigraphic analysis of the Sequence position in the Neogene column and lithological comparison with the sequence of parti-coloured clays established in the neighbouring (from the north) territory. Thickness of the Sequence attains 4 m.

Pliocene (N2) In Prymorska LTZ Pliocene rocks include the sequence of iron-enriched sandstones that corresponds to

Cimmerian regio-stage, and the sequence of clays and sands that corresponds to Akchagylskiy regio-stage. Undivided Pliocene sediments comprise the sequence of red-brown clays.

C i m m e r i a n r e g i o - s t a g e Prymorska LTZ Sequence of iron-enriched sandstones (N2zp). Distribution of this sequence (Prymorska LTZ) is caused

by transgression of Cimmerian sea which was expanding from the south; irregular northern boundary of sediments passes in the west Lozovatka village, Glyboka gully, and Borysivka, Novovasylivka and Osypenko villages. The rocks transgressively lie over Precambrian crystalline rocks and their weathering crust, undivided Kuzhorski and Zbruchski layers, and undivided Novomoskovski, Vasylivski and Dnipropetrovski layers. The Sequence footwall genTy plunges in the southern and south-eastern directions with altitudes from -25 m to -100 m. The rocks are overlain by the Akchagylska sequence of clays and sands.

The sediments were forming in the shallow-sea environments, with frequent bottom level variations under the general trend to its deepening (Fig. 2.11). In Prymorska LTZ two horizons are conventionally distinguished. The lower one is composed of iron-enriched, greenish-brown, diverse-grained to gravelous sandstones (so called “tobacco” iron ores). Rounded fragments are composed of quartz, iron hydroxide and chamosite oolites, feldspar (up to 5%), and amphibole (up to 5%). The iron hydroxide and chamosite oolites display concentric structure and normally quartz or gypsum grains occur inside. Oolite content varies in the range 5-40%.

The oolites, up to 0.6-1 mm in size, are extensively oxidized. Cement is contact-porous, carbonate-chlorite. Fine-grained brown carbonate (siderite) is contained in amount up to 4-7%. Chlorite is dark-green, iron-enriched (chamosite). Amount of cement attains 40-50%. Sandstones are layered due to involved interbeds of mollusc shells, massive sandstone with siderite cement, clays, rarely greenish-grey, fine-grained, quartz sand, in places cemented with ironiferous-clayey cement to weak sandstone. Chamosite ore occurrences are related to the ironiferous sandstones. Thickness of sandstones in lower horizon varies in the range 1.3-24 m. Thickness of

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siderite layer, which is confined to the most subsided parts of Prymorska LTZ, in places attains 8-10 m (2-6 m in average).

Above sandstones throughout lies dark-grey aleuritic clay with brown stains of iron enrichment, thin-layered due to sand interbeds. Thickness of the clays varies from 2 to 21 m.

Upper horizon is composed of grey aleuritic micaceous clays, 2-24 m thick, which are replaced in the northern direction by grey, greenish-grey feldspar-quartz fine-grained sands 2-24 m thick. Interbeds of sandstones with ironiferous cement and with vivianite are encountered.

The Sequence age is defined by lithological and paleontologic studies. V.M.Semenenko had determined the following fauna: Dreissensia rotiformis Dech. var.akmanaica Andrus., D. angusta Reuss., D. brussina Dech., D. theodori Andrus., Archicardium subacardo Andrus., Didacna crassatella Dech., D. karpinskyi Andrus., Paradacna stratonis Andrus., Monodacna donacoides Andrus., M. sokolovi Andrus.

Thickness of the Sequence attains 50 m. A k c h a g y l s k i y r e g i o - s t a g e Sequence of clays and sands (N2gp) is more widely developed than Cimmerian sequence of iron-

enriched sandstones because of Akchagylske sea transgression in Prymorska LTZ which had encompassed almost entire zone (Fig. 2.12). It unconformably lies over sediments of the sequence of iron-enruched sandstones, over Precambrian crystalline rocks and their weathering crust, and close to the eastern margin of the map sheet – over undivided Miocene Novomoskovski, Vasylkivski and Dnipropetrovski layers. In Berdyanska sandbank and in the lower portion of Berda River valley the sediments are eroded in Quaternary time. The footwall altitudes vary from -11 m to -45 m. The rocks are overlain by alluvial sediments of the tenth terrace. Clays and sands were deposited in shallow-water marine estuary-type environments which changed by river deltaic environments in time. Two lithological horizons are encountered in the section: lower sandy and upper clayey ones.

The sands are yellow- and bluish-grey, with brown interbeds, quartz, fine-grained, calcareous, non-layered, in places oblique and wavy layering is observed due to interbeds of clays and coarse-grained sands. In some places sandstones alternate with bluish- and dark-grey aleurolites and thin-layered clays. By mineralogical studies, the rocks contain ilmenite, zircon, minute gold signs. Thickness of the sands attains 22 m.

The clays of upper horizon are yellow- and dark-grey, often spotty, with iron and manganese hydroxide stains, montmorillonite-hydro-micaceous, sandy, at the bottom in places with shell fragments and carbonate bunches. Thickness of the clays varies in the range 2-25 m.

The sequence age is determined by V.M.Semenenko over lithological and paleontologic studies. The following fauna is found in the sediments: Dreissensia theodori kubanica Krest., D. ex gr. angusta Reuss., D. theodori Andrus., Prosodacna cf.misera Ebers., Valvata naticina Menka.

Undivided Pliocene sediments Sequence of red-brown clays (N2čb) is developed almost throughout the studied map sheet. In

Chernigivsko-Berestivska LTZ some minor separated enclaves occur, mainlt at the watersheds. In Prymorska LTZ the Sequence is developed along the northern margin but is eroded in the river valleys. It unconformably lies over Precambrian crystalline rocks and their weathering crust, as well as over sediments of Novopetrivska Suite and undivided Miocene sediments. Sequence is overlain by Quaternary loams.

The sediments of this straton were formed in sub-aerial environments as the products of eluvial and deluvial processes. Clays and sands of red-brown Sequence are distinctly coloured and besides the red-brown colouring, the brick-red, yellow-brown with greenish shade stains are known. The clays are dense, plastic, sandy, with sliding planes, with newly-formed carbonate bunches, iron-manganese oolites and gypsum druses; at the bottom the clays are changed by fine-grained sandy loams.

The sands are quartz, quartz-feldspar, fine-medium-grained, clayey, up to 2-3 m thick; the rocks occur only along the southern margin of Sequence distribution.

The Sequence does not contain any fauna. In view of its geological setting and distinct lithology red-brown clays are ascribed to Pliocene rocks.

Thickness of the Sequence attains 16.1 m. Quaternary System (Q) Quaternary sediments are developed almost throughout over the map sheet L-37-VII and are absent

only at the watersheds with denudation remnants and on the steep slopes of Berda, Korsak, Kyltychiya,

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Lozovatka, Obitochna, Tokmak and other rivers, where due to denudation and erosion processes pre-Quaternary rocks are exposed at the surface.

Location of the map sheet most parts within Pryazovska Height and in the back-glacier zone defines prevailing development of continental sub-aerial rocks in the territory, which are subdivided into loess-loam brown- and red-coloured formations. These two include not only sub-aerial but also associated rocks and by this reason in the studied area eluvial, deluvial, coluvial, sub-aqueous as well as complex genetic types occur in spatial relations (see “Geological map of Quaternary sediments”).

Continental sub-aerial sediments cover more than 95% of the territory constituting almost all geomorphologic elements.

On the Azov Sea coast, within Pryazovska Lowland, marine Quaternary sediments are widely developed.

The Quaternary sediments mainly unconformably lie over their underlaying rocks and comprise the upper tectonic floor of the Meso-Cenozoic level. Development of this floor continues nowadays.

By lithology, among the continental sediments at watershed and inter-river sites loess-like loams and clays predominate which alternate with the former soils. In the lower part of Quaternary column the clayey rocks of red-brown-coloured formation occur. In the river valleys the sands and sandy loams are widely developed besides the loams and clays. The sands, mudstones and clays predominate among marine sediments.

Thickness of Quaternary sediments increases from the north to south, in direction of the regional relief lowering, from parts of meter to 78.5 m. Thickness increasing is also observed at the watersheds in comparison to the river valleys where Quaternary sediments are partially eroded. The local thickness changes are related to the relief of underlaying surface, as well as the neo-tectonic block motions.

Stratigraphic subdivision of Quaternary sediments is performed applying the complex of method of which litho-stratigraphic and geomorphologic ones were the major one, and using the relevant paleontologic data.

In the course of map design for Quaternary sediments the data were used obtained in the large-scale geological mapping which were accompanied by the mapping of Quaternary sediments, as well as the complex mapping data conducted in the melioration purposes. The published data concerning basic geological sections and geology of Quaternary sediments in Pryazovya and other regions of Ukraine also were used [17, 18, 26, 28, 29], as well as available handbooks on studies of Quaternary sediments, “Legend of Derzhgeolkarta-200” and “Stratigraphic scheme of Quaternary sediments in Ukraine” approved in 1993 [31, 32].

In the territory of the suited map sheet the Quaternary sediments are ascribed to Lower and Upper Pleistocene, Lower, Middle and Upper Neo-Pleistocene, and subdivided into three types of simple, complex and combined genesis that is indicated in the “Geological map of Quaternary sediments”, in stratigraphic-genetic column, cross-sections, tectonic scheme and typical lithologo-stratigraphic sections (columns). The major mapping elements have included Quaternary sediments in the limits of the branch for sub-aerial, the ledge – for sub-aqueous, and the horizon – for marine genetic types. According to the accepted standards, the Holocene soil rocks are not shown in the map. In the typologic columns subdivision of sub-aerial sediments is provided up to the climatolith if possible.

Description of Quaternary sediments is given in compliance with the territory zonation performed with regard to its geological-tectonic and paleo-geographic features. Almost entire map sheet territory is ascribed to the southern loess region of the back-glacier zone (A) where the continental formations are developed. The narrow sea coast band is included into the coastal region and the Azov Sea area (B) with prevailing development of marine facies of Quaternary sediments. In the regions the following areas are distinguished: Pryazovskiy (A-1) and Northern Coast (B-1), as well as sub-areas: Northern (A-1-a) and Siuthern (A-1-b). The Northern sub-area encompasses Pryazovian crystalline massif and its slopes and corresponds to Pryazovska Height. The Northern Coast area and Southern sub-area belong to the northern limb of Azovsko-Kubanska Depression and correspond to Pryazovska Lowland (see “Scheme of structure-geomorphologic zonation” in the scale 1:500 000).

Absolute age of Quaternary (Neo-Pleistocene) sediments in Northern Pryazovye is based on the thermo-luminescent determinations [103].

Pliocene – Eo-Pleistocene alluvial sediments undivided (a10N2 – E1kh) Alluvium of the tenth (Kyzyldzharska) terrace, which is developed in almost continuous band along the

northern coast of Azov Sea, and is absent only in Berda River valley and in the mouth part of Lozovatka River valley, is ascribed to the undivided rocks of Upper Pliocene Beregivskiy Horizon and Lower Eo-Pleistocene Berezanskiy climayolith (see “Scheme of Quaternary sediments structure”). The width of mentioned band varies from 5-20 km in the east, through 8 km in the centre, to 16 km in the west of the map sheet. To the north of this

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band the Pliocene-Quaternary sediments are observed in some enclaves 0.5-3 km in size in the valleys of Korska, Lozovatkam Obitochna and Berda rivers.

The mentioned sediments lie mainly over the Upper Pliocene (Novovasylivska and red-brown clay sequences) and older rocks and are buried beneath the younger Quaternary sediments – from Eo-Pleistocene to Holocene inclusive. In Azovsko-Kubanska Depression the footwall of tenth terrace alluvium descends from the northern distribution boundary to the south, with respective altitude variations from 0.2-7.2 m to -23 … -29 m; on the slopes of Pryazovska Height the footwall ascends to the altitudes 6.7-59 m. Lithological composition of these sediments is two-folded. The upper layer is composed of red-brown, brown, grey, violent, greenish-violent clays, loams and sandy loams with interbeds of diverse-grained sands, iron-enrichment and gel stains, with inclusions of mud, gravel and pebble of crystalline rocks, newly-formed carbonate bunches, various iron-manganese oxide occurrences. The lower 2-33 m thick layer includes grey, yellowish- and greenish-grey, diverse-grained, quartz-feldspar sands with inclusions of pebble, gravel, semi-rounded re-deposited carbonate concretions. In the southern part these are brown, orange-brown, red-brown, brick-red, fine- and coarse-grained, quartz, quartz-feldspar sands with inclusions of gravel, gruss, pebble, boulders of granites, plagiogneisses and other crystalline rocks, 1.0-8.5 m thick. In the northern part these are red-brown-coloured sands, loams and clays. The sands are clayey, loams and clays are very sandy, 1.5-35.0 m thick, with inclusions of weakly-rounded fragments of crystalline rocks and newly-formed carbonate aggregates 3-7 cm in size (Berda River valley). The following fauna is found in these sediments: Elasmotherium sp., Archidiscodon cf. gromovi Gar., Cricetus sp., Spalax sp., Pliomys kretzoi Kow., Villanyia petenyii Meh., Microtinae gen., Mimomys cf. reidi Hint., Acridiscodon meridionalis Nesti.

Eo-Pleistocene (E) L o w e r B r a n c h ( E I ) Lower-Pleistocene rocks include Berezanski aeolian-deluvial sediments (vdE1br): brownish-yellow

sandy loams with numerous sliding planes covered with iron and manganese oxide films and dendrites, with carbonate tubes; grey clays with slight greenish shade and red stains, dense, with sliding planes, diverse-grained quartz sand parcels, minor carbonate concretions and beans (up to 4 mm), iron and manganese oxides. Thickness of these sediments is 1.1-2.8 m. Berezanski sediments overlies Pliocene sequence of red-brown clays and are overlain by Upper Eo-Pleistocene Kryzhanivski rocks.

U p p e r B r a n c h ( E I I ) Upper Eo-Pleistocene rocks more widely distributed and include sub-aerial and sub-aqueous genetic

rock types ascribed to Kryzhanivskiy and Illichivskiy climatoliths (see “Typical lithologo-stratigraphic sections”).

Kryzhanivskiy climatolith (eEIIkr). Eluvial sediments 1.6-9.6 m thick include red-brown, brick-red clays, in places loams of lumpy texture, dense, viscous, at the bottom – inclusions of rounded quartz and feldspar fragments with numerous stains and beans of iron and manganese oxides along sliding planes, contain carbonate concretion and bunches.

Illichivskiy climatolith (vdEIIil). Aeolian-deluvial sediments 0.2-2.7 m thick comprise bluish-greenish and brownish-grey clays, in places heavy loams, sandy, calcareous, dense. contain carbonate concretions with numerous stains and beans of iron and manganese oxides.

Nogayskiy ledge (a9EIIng). Sub-aqueous sediments include alluvium of Nogayska (ninth) terrace. Two layers are distinguished.

Upper layer comprises brown-, red-brown, sandy, dense clays, same-coloured loams, medium to heavt, sandy, contain inclusions of re-deposited carbonates with newly-formed bunches, stains and beans of iron and manganese oxides. Sands are grayish-yellow, grayish-green, with iron-enrichment stains, diverse-grained (2-10 m thick).

Lower layer is composed of brown to red-brown clays, in places greenish, sandy, contain gravel inclusions, quartz and feldspar pebble, carbonate bunches; the sands are grey, yellowish-grey, brownish-grey, quartz-feldspar, diverse-grained with semi-rounded grains, 4.5 m thick. Total thickness of terrace alluvium varies from 0.8 to 27.4 m. Alluvial sediments contain the mammal remnants: Archidiscodon meridionalis Nesti, Mimomys intermedius (Newt.), Allophaiomys pliocaenicus Korm., Lagurodon arankae Kretz., Eolаgurus sinlicidens (Young.), Lagurus sp., Microtinae gen., Citellus sp.,Cricetussp.

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Neo-Pleistocene (P) In the map sheet territory Neo-Pleistocene sediments are developed throughout except the older rocks

exposure sites, and in Berdyanska and Obitochna sandbanks where they are eroded. Neo-Pleistocene sediments are divided into Lower, Middle and Upper Neo-Pleistocene branches (see “Geological map of Quaternary sediments”).

L o w e r B r a n c h ( P I ) In the most elevated part of Northern sub-area (A-1-a) Lower Neo-Pleistocene sediments are locally

developed at some watersheds and their slopes and comprise sub-aerial rocks. In the southern and western directions in the river valleys appear sub-aqueous sediments which are widespread in the Southern sub-area (A-1-b). In Azov Sea coast and Obitochna sandbank marine sediments are developed (see “Scheme of structure-geomorphologic zonation”).

The continental sediments are subdivided into six climatoliths: Shyrokynskiy, Pryazovskiy, Martonoskiy, Sulskiy, Lubenskiy and Tyligulskiy which constitute three ledges: Budatskiy, Donetskiy and Krukenytskiy. Marine sediments are ascribed to Zyukskiy horizon of Evksinskiy supra-horizon (see “Scheme of Quaternary sediments correlation”).

The footwall of Lower Neo-Pleistocene sediments regularly descends from the north to south in the direction of regional relief lowering with respective altitude changes from +320 to +20 m.

Shyrokynskiy climatolith (vdPIsh). Eluvial sediments (0.5-6.5 m thick) are red-brown, rarely brown with reddish shade clays and heavy loams, in places sandy, transitional to clayey-sandy loams, calcareous, with inclusions of diverse-grained polymictic sand, contains carbonate concretions, by jointing planes – films and stains of iron and manganese oxides.

Pryazovskiy climatolith (vdPIpr). Aeolian-deluvial sediments (0.3-6.1 m thick) includes loess-like light- and yellowish-brown medium and heavy loams, calcareous, contain minor and coarse (up to 5-8 cm) carbonate concretions, by jointing planes – films and stains of iron and manganese oxides.

Budatskiy climatolith (a8PIbk). Alluvial (eighth) terrace is two-folded: upper part – brownish-grey, light- and dark-brown with yellowish shade heavy loams to clays, sandy, with wavy horizontal layering, in places contain inclusions of weakly-rounded crystalline rock fragments, carbonate concretions, frequent stains of iron and manganese oxides; lower part – light-brown sandy loams, light-grey with greenish shade sands, in places light-brown fine-medium-grained sands, feldspar-quartz, with inclusions of semi-rounded gravel fragments, crystalline rock pebble, and re-deposited carbonates. Total thickness of terrace alluvium varies from 3.6 to 18.0 m.

Martonoskiy climatolith (ePImr). Eluvial sediments (0.2-0.0 m thick) are reddish-brown, brown, heavy, dense loams, in places lumpy, calcareous clays, contain carbonate concretions and gypsum druses, by jointing planes the films and stains of iron and manganese oxides occur.

Sulskiy climatolith (vdPIsl). Aeolian-deluvial sediments – loess-like light- and yellowish-brown, medium and heavy loams, calcareous, contain minor and coarse (up to 5-8 cm) carbonate concretions, by jointing planes – films and stains of iron and manganese oxides (thickness – 0.3-6.1 m).

Donetskiy ledge (a7PIdc). Alluvial (seventh) terrace is two-folded: in the south the upper part comprises brownish-grey, light-brown clays, often with interbeds of sand and same-coloured sandy loam; the lower part – brownish-grey, grey, diverse-grained sands with inclusions of gravel, pebble, in places crystalline rock gruss. Total thickness of alluvium varies from 0.4 m to 15.2 m. Detailed studies over terrace sediments both in drill-holes and coastal cliff exposures allows consideration the seventh terrace to be the marker horizon.

Lubenskiy climatolith (ePIlb). Eluvial sediments (0.2-6.0 m thick) are light- and dark-brown heavy loams and clays, coarse-lumpy, high-calcareous. In the coastal cliff Lubenskiy former soil is traced quite confidenTy to the west from Obitochna River and actually comprises the marker horizon.

Tyligulskiy climatolith (vdPItl). These aeolian-deluvial sediments include pale-yellow, brownish-yellow, light-brown loess-like medium and heavy loams, macro-porous, carbonate, with iron-manganese oxide stains, single gypsum bunches, and carbonate concretions 1-6 cm in diameter. Thickness of terrace is 0.1-7.2 m.

Krukenytskiy ledge (a6PIkn). Alluvial (sixth) terrace composed of grayish-brown clays with inclusions of minor pebble and gravel, with interbeds of diverse-grained sand; grey quartz fine-grained sands, with interbeds of brown clay, inclusions of weakly-rounded fragments of crystalline rocks. Thickness of terrace alluvium is 4.9 m.

The Lower Neo-Pleistocene sub-aerial sediments located in paleo-depressions do also contain sub-aerial sediments of complex origin. For instance, at the watershed, close to upper course of Kiltychiya River, in the drill-hole the sub-aerial Lower Neo-Pleistocene sediments (e,vdPI) are intersected in the interval 9.0-20.3 m

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(altitudes 171.5-160.2 m) which overlie the crystalline rocks of Kolarivskiy Complex and are overlain by undivided Middle-Upper Neo-Pleistocene eluvial and aeolian-deluvial sediments. The rocks include yellowish-brown with slight reddish shade, light-brown, rarely red-brown loams, slightly macro-porous, aggregate-lumpy, with discrete stains of iron-manganese oxides. At the bottom the loams contain carbonate concretions up to 5 cm in diameter (up to 30-50% by rock volume), in places aggregates of fine gypsum crystals, abundant iron-manganese oxide stains. There is no clear division into eluvial and loess-like layers. Thickness of described sediments is 11.3 m.

Marine Lower Neo-Pleistocene sediments of Zyukskiy horizon (mPIzk) constitute the marine terrace developed to the south of Prymorsk town in the coastal band 10 km long and 2 km wide. Terrace sediments are exposed in the abrasion coastal cliff below the Middle Neo-Pleistocene sub-aerial rocks. In Obitochna sandbank Zyukski sediments lie beneath Holocene marine and estuary-marine sediments, above alluvium of tenth terrace. Footwall altitudes of Zyukska terrace varies in the range 6.6-10 m and decrease to the south.

Upper part of terrace section is composed of brown, of various shade, from light to dark, high-carbonate loams with newly-formed carbonate bunches and concretions, with inclusions of re-deposited carbonates. Mollusc fauna is encountered in the loams. Below lie sandy clays and muds, grey, dark-grey, greenish- and bluish-grey. Lower part of the section is composed of diverse-grained clayey sands which at the bottom contain inclusions of pebble and gravel of crystalline rocks, sandstones and re-deposited carbonate concretions. Thickness of these sediments varies from 4.1 to 9.5 m and is 4.5 m in average.

The age of marine terrace is supported by fauna. In DH 45ig are found the remnants of: Didacna cf. crassa (Eichw.), Didacna sp. Dreissena polymorpha Pall., Micromelania caspia Eichw., M. dimidiata Eichw.,Valvata piscinalis Mull., Theodoxus fluviatilis L. T. tilis L., Monodacna sp., Corbicula fluminalis Eichw., Viviparus cf. fasciatus Mull.,Clessiniola variabilis Eichw., Adacna sp., Micromelania sp., Caspia gmelini Dyb.

M i d d l e B r a n c h ( P I I ) Middle Neo-Pleistocene sediments (e,vdPII) are developed mainly at the watershed covering Lower

Neo-Pleistocene and older rocks and are throughout overlain by Upper Neo-Pleistocene and Holocene sediments. The local erosion windows are characteristic for these sediments. Middle Neo-Pleistocene sediments constitute the loess-loam sequence and are subdivided into Zavadivskiy, Dniprovskiy, Kaydatskiy and Tyasminskiy climatoliths which correspond to the warm and cold phases and include sub-aerial, sub-aqueous, eluvial, complex and combined genetic types.

Zavadivskiy climatolith (ePIIzv). Eluvial sediments (0.2-7.5 m thick in the north) are brown, chestnut, yellowish-brown loams, medium to heavy, nut-lumpy, calcareous with minor carbonate concretions, discrete iron-manganese oxide stains; in the south (0.3-6.4 m thick) these are reddish-brown, brown, dark-brown heavy loams, clays, coarse-lumpy, dense, with sliding planes, and newly-formed carbonate concretions of various shape.

Dniprovskiy climatolith (vdPIIdn). Aeolian-deluvial sediments in the northern part of map sheet comprise yellowish-brown, brown, brownish-grey loess-like medium loams, slightly macro-porous, 0.3-6.6 m thick, with crystalline rock fragments, carbonate concretions, scarce iron-manganese stains. In the southern part these are pale-yellow, pale-grey, loess-like light and medium loams, calcareous, highly macro-porous, with newly-formed carbonate tubes and minor druses, with minute gypsum druses (thickness 0.5-5.7 m).

Khadzhybeyskiy ledge (a5PIIhd). Alluvial (fifth) terrace is two-folded: in the south the upper part comprises grey, greyish-brown clay with carbonate beans and iron-manganese oxide dissemination; the lower part – grey, grayish-yellow, yellow diverse-grained, quartz, in places clayey sands with minor quartz pebble (thickness up to 5.7 m); in the north these are dark-grey, blue-grey, yellowish-brown with bluish shade heavy loams and clays with sand interbeds, below – brown with yellowish shade diverse-grained sands (thickness up to 5.9 m).

Kaydatskiy climatolith (ePIIkd). The former soils include dark-brown, brown heavy loams, in places humus, carbonate, lumpy clays, often with abundant carbonate aggregates, gypsum crystals (0.2-5.5 m thick in the north), and black-earth-like, medium-loamy, brownish-grey, grey calcareous soils, with newly-formed carbonate tubes and minor concretions (thickness 0.2-5.6 m in the south).

Tyasminskiy climatolith (vdPIIts). Aeolian-deluvial sediments in the northern part (0.2-2.4 m thick) include yellow-brown, yellow-grey, pale-yellow loams, calcareous, with discrete iron-manganese stains, and pale-yellow, brown-yellow, light-brown loess-like, light, calcareous, macro-porous loams with scarce gypsum druses in the southern part.

Cherkaskiy ledge (a4PIIcr). Alluvial (fourth) terrace is two-folded: in the north the upper part consists of dark-grey, grayish-brown loams and sandy loams with carbonate concretions; the lower part – grey, grayish-yellow, diverse-grained, quartz, in places clayey sands up to 10.4 m thick; in the northern part – light-grey, fine-

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and coarse-grained quartz-feldspar sands with minor fragments of quartz and crystalline rocks, red-brown loams and clays with inclusions of gypsum, gravel and pebble, thickness 10-2.4 m.

Age of Khadzhybeyski and Cherkaski rocks is revealed from the age of overlaying sediments. In the geological map the boundary of alluvium distribution is shown as probable since in the modern relief these terraces are not expressed in geomorphologic respect.

M i d d l e a n d U p p e r b r a n c h e s u n d i v i d e d ( P I I - I I I ) These sediments (e,vdPII-III) are developed in the north of L-37-VII map sheet in most elevated

watersheds and their slopes and lie over Lower Neo-Pleistocene, Neogene sediments and Precambrian crystalline rocks, and are overlain by Holocene soils. These include light-, yellow-brown and brown-grey, non-layered, light and medium, carbonate, aggrefate-lumpy, slightly macro-porous loams with inclusions of polymictic sand and gruss of crystalline rocks which amount increases downward. In places worm-holes occur filled with humus, with scarce iron-manganese oxides, minor carbonate bunches up to 1 cm in diameter. Thickness of these rocks varies from 1.1 to 17.2 m (7.5 m in average).

Two facies are clearly distinguished in the genetic types of Pleistocene sediments (by the international scale): lower Eo-Pleistocene red-brown clayey-loamy (ePIsh) and upper Neo-Pleistocene (with Pryazovskiy climatolith) pale loess-loamy.

Thickness of the facies varies in a wide range from 0 to 16 m for red-brown facies and from 0 to 36.3 m for loess-loamy one at the general thickness increasing.

In Pryazovya territory, located in between Molochna and Lozovatka rivers, detailed studies of absolute age of Quaternary sediments by thermo-luminescent method were conducted. Absolute age of Upper Neo-Pleistocene from Prylutskiy to Buzkiy climatoliths inclusive is determined in the interval 25-160 thousand years, Middle Neo-Pleistocene – 160-400 thousand years, Lower Neo-Pleistocene – 0.4-1.0 Ma.

U p p e r B r a n c h ( P I I I ) Of all Neo-Pleistocene branches the Upper Neo-Pleistocene sediments are most widespread and studied.

They constitute the upper portion of loess-loamy facies and comprise the alternation of former soils and loess-like rocks formed in warm and cold phases respectively.

In the studied map sheet these sediments, together with other Quaternary sediments, constitute the major forms of modern relief – watersheds and their slopes, over-flood terraces, as well as river and gully valley slopes. With the clear contact they lie over the rocks of Middle and Lower Neo-Pleistocene, Eo-Pleistocene, Pliocene, Miocene and over the older Meso-Cenozoic sediments and Archean-Proterozoic crystalline rocks.

Upper Neo-Pleistocene sediments are subdivided into six climatoliths: Prylutskiy, Udayskiy, Vytachivskiy, Buzkiy, Dofinivskiy and Prychornomorskiy which in pairs are combined in three ledges – Trubizkiy, Vilshanskiy and Desnyanskiy composed of sub-aerial, sub-aqueous, complex and combined genetic types.

In the course of mapping of sub-aerial sediments the Upper Neo-Pleistocene rock sequence is divided in two parts. Prylutski, Udayski and Vytachivski sediments (e,vdPIIIpl-vt) are included in the lower part, that is, eluvial rocks (ePIII) lie at the top and bottom being separated by aeolian-deluvial (vdPIII) rocks. They are developed at the watersheds and their slopes. Altitude of Prylutsko-Vytachivski sediments footwall is highest close to the northern map sheet boundary attaining 254.7 m and then descends in the southern and south-seatern directions, as well as outward from the watersheds to river and gully valleys (see “Typical lithologo-stratigraphic sections”).

In the map sheet south Prylutsko-Vytachivski sediments (e,vdPIIIpl-vt) are exposed in the sea coastal cliff. Their footwall altitudes here are 10-20 m. Eluvial medium and heavy loams with minor loess-like loams predominate in the column. Thickness of these sediments is quite variable and its highest value in the Southern sub-area is 8 m. Average thickness of Prylutsko-Vytachivski sediments is 3.5 m.

Upper part of Upper Neo-Pleistocene sub-aerial sequence includes Buzki, Dofinivski and Prychornomorski sediments (vd,ePIIIbg-pc). In the north these sediments are developed at some watershed areas covering Prylutsko-Vytachivski sediments and in places of lacking the latter – lie over older Quaternary and pre-Quaternary sediments up to Precambrian crystalline rocks. The hanging-wall of Buzko-Prychornomorski sediments actually coincides with the modern earth surface since it is covered only by thin Holocene soils.

Buzko-Prychornomorski sediments are mainly composed of loess-like, light, medium and heavy loams which various combinations and setting are shown in the “Geological map of Quaternary sediments” and supplementary geological cross-sections.

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In the map sheet territory most widespread are loess-like loams which in places become sandy on the watershed slopes.

Buzko-Prychornomorskiy climatolith (vd,ePIIIbg-pc). These sediments complete the column of Neo-Pleistocene sub-aerial rocks. Their thickness is variable and at the watersheds it attains maximum value of 6.2 m. Average thickness is 3.3 m (see “Scheme of Quaternary sediments structure”).

In the northern part of map sheet Prylutskiy climatolith (ePIIIpl) is mapped at the bottom of Upper Neo-Pleistocene section. This is former soil (thickness from 0.1 to 5.0 m) composed of yellowish-brownish-grey medium and heavy loams, nut-lumpy, carbonate, with rounded and semi-rounded fragments of crystalline rocks. In the southern part Prylutskiy soil comprises brown-grey, dark-brown, medium and heavy loams, slightly-calcareous, often gypsum-enriched, with carbonate concretions and bunches (thickness 0.2-4.4 m).

Udayskiy climatolith (vdPIIIud). These are more locally developed aeolian-deluvial sediments; in the north these are loess-like medium loams, light-brown, macro-porous, carbonate, with minor fragments of crystalline rocks and newly-formed carbonates, 0.2-3.2 m thick; in the south – pale-yellow, yellowish-brown and pale-brown loess-like medium loams, macro-porous, with vertical jointing, iron-manganese oxide stains, newly-formed carbonates, 0.3-3.5 m thick.

Vytachivskiy climatolith (ePIIIvt). Eluvial sediments comprise the same-named former soil: light-brown, yellowish- and grayish-brown, medium and heavy loams, lightly macro-porous, nut-lumpy, with iron-manganese oxide stains, carbonate bunches. Thickness in the northern part is 0.2-5.5 m. In the map sheet southern part (thickness – 0.2-4.5 m) these are brown, dark-brown, brownish-grey, medium and heavy loams, lumpy, high-calcareous, gypsum-enriched, with iron-manganese oxide beans.

Buzkiy climatolith (vdPIIIbg). These are aeolian-deluvial sediments composed of pale-yellow, pale-grey, loess-like medium loams, slightly macro-porous, carbonate, with vertical jointing, iron-manganese oxide stains, in places with carbonate bunches. In the northern part their thickness varies from 0.4 to 4.1 m (1.3 m in average).

In the Southern sub-area Buzki rocks include pale-yellow, bright-yellow, brownish-yellow loess-like light and medium loams, macro-porous, carbonate, with vertical jointing, in places with fine-crystalline gypsum druses. Thickness of Buzki sediments varies in the range 0.3-4.4 m (2.1 m in average).

Dofinivskiy climatolith (ePIIIdf). Eluvial rocks in the sub-aerial sediments are common likewise Buzki ones. In the north, Dofinivskiy former soil is composed of brown-grey, brownish-yellow, medium loams, carbonate, aggregate-lumpy, with humus films, in places with iron-manganese stains, and bunch carbonate (thickness 0.1-3.5 m). In the south, these are dark-brown, medium and heavy loams, fine- and medium-lumpy, carbonate, with newly-formed carbonate tubes, bunches of fine-crystalline gypsum, and scarce iron-manganese stains (thickness 0.2-3.5 m).

Prychornomorskiy climatolith (vdPIIIpc). These aeolian-deluvial sediments cap Neo-Pleistocene loess-loam sequence and throughout are overlain by Holocene soil. In the north, the rocks include pale-yellow, pale-grey, light, medium loess-like loams, macro-porous, calcareous, with vertical jointing, carbonate bunches, and iron-manganese stains (thickness 0.2-4.6 m). In the south, these are pale-yellow, pale, light-brown, light, medium loess-like loams, highly macro-porous, with vertical jointing and newly-formed carbonate (thickness 0.3-5.6 m).

In the Northern sub-area, on the closed slopes of river and gully valleys, are relatively widespread eluvial-deluvial and deluvial (ed,dPIII) Upper Neo-Pleistocene rocks. They are developed along the slopes by bands up to 2 km wide. Lithology of deluvial sediments depends on the underlaying rock composition. The rocks are brown-yellow and light-yellow loams, uniform, with inclusions of crystalline rock fragments which amount increases toward the bottom and downward the slopes. Thickness varies from 0.2 to 13.7 m, in average 4.4 m.

Upper Neo-Pleistocene eluvial-deluvial (edPIII) sediments up to 1.1 m thick are locally developed providing the oval enclaves up to 0.5-3.2 km in size at the watersheds in the Northern sub-area, often surrounding the denudation remnants of Precambrian crystalline rocks. They are composed of yellowish-grey, grayish-pale, light, carbonate loams, slightly macro-porous, with inclusions of quartz sand with almost non-rounded grains, and gravel of crystalline rocks, with brittle carbonate bunches up to 0.5 cm in diameter, minor iron-manganese oxide beans. The rocks lie over weathered surface of Precambrian crystalline rocks and are overlain by Holocene soil.

Upper Neo-Pleistocene alluvial sediments comprise the third (Trubizka), second (Vilshanska) and first (Desnyanska) over-flood terraces which are being traced in the valleys of major rivers in separated narrow bands. It is not possible to show these terraces in the map over entire sub-area since width of each terrace does not exceed 100-150 m. By these reasons the rocks together with Holocene alluvial sediments are described as undivided Upper Neo-Pleistocene – Holocene units.

Trubizkiy ledge (a3PIIItb). Alluvial (third) terrace is two-folded. Upper part includes greyish-brownish-yellow, brownish-yellow, dark-brown, in places greenish-white, medium to heavy loams, carbonate, with interbeds of muds, clays, sandy loams and sands, newly-formed carbonate and iron-manganese oxides. Mud is

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grey with minor gravel and quartz, granite pebble. This layer contains brown stains of iron-enrichment. Lower part includes light-grey, yellowish-grey, in places greenish-grey, diverse-grained quartz-feldspar sands with slight layering, with minor weakly-rounded gravel and crystalline rock pebble. Thickness is up to 27.4 m.

The age of Trubizkiy alluvium is supported by its normal setting at the hanging-wall of Vytachivskiy former soil. At the eastern margin of L-37-VII map sheet, nearby Kulykove village, from deluvial sediments of Prylutsko-Udayskiy time, which are changed by the third terrace alluvial sediments and are exposed in the Azov Sea coastal cliff, A.I.Shevchenko and O.V.Grygoryev (1967) had collected the rodent remnants Pitymys ex gr. gregаlis, Microtus ex gr. lagurus, Alactagulus acontion, Spalax sp., Microtinae gen (without roots, with cement). Listed minor mammals the authors had ascribed to Kulykovskiy Upper Neo-Pleistocene complex.

Vilshanskiy ledge (a2PIIIvl). Alluvial sediments of second terrace are defined in the lower course valleys of Lozovatka, Obitochna, Kiltychiya and Berda rivers. Width of alluvium band is 0.4-1 km. Lithology is variable and irregular by strike. In the vertical section alluvium is divided in two parts. Upper part is mainly composed of loams, muds, rarely sand interbeds. Loams normally are brownish-yellow, brown, medium to heavy, carbonate, in places with mud and sand interbeds, contain inclusions of gravel, pebble, aggregates, beans and stains of iron-manganese oxides, carbonate tubes and concretions. Muds are yellowish-bluish-grey, sandy, in places with minor fragments of mollusc shells. Sands are brownish-grey, feldspar-quartz, diverse-grained, mainly fine-grained, with inclusions of gravel and gruss, often clayey.

In the lower part of Vilshanskiy alluvium grey, dark-grey, in places with greenish shade, diverse-grained, mainly medium- and coarse-grained, quartz and feldspar-quartz sands predominate, with inclusions of weakly-rounded gravel and pebble. Rarely greenish-grey sandy clays with sand interbeds occur. Whole alluvium sequence display brown stains of iron enrichment.

Desnyanskiy ledge (a1PIIIds). Alluvial sediments constitute the first over-flood terrace and are developed mainly in the Southern sub-area, in the valleys of Obitochna, Kiltychiya and Berda rivers, in the separated short (up to 3 km) and narrow (0.2-1 km) bands. By lithology Desnyanskiy alluvium is divided in two parts: upper mud-loamy and lower – sandy.

Upper Neo-Pleistocene sediments of proluvial-deluvial origin (pdPIII) are developed in the coastal area of Azov Sea. These sediments fill up ancient (buried) gullies and are traced in the coastal exposures. They include brown, light-brown, medium and light loams, at the bottom – sandy with minor re-deposited carbonate concretions, 1.2-18.2 m thick in the south of map sheet.

Upper Neo-Pleistocene – Holocene undivided (PIII-H) The sediments of eluvial-deluvial, alluvial and alluvial-deluvial genetic types are ascribed to undivided

Upper Neo-Pleistocene – Holocene rocks. Eluvial-deluvial (edPIII-H) sediments of this age are developed in the limited enclaves and bands in the

steep open slopes of river valleys and gullies in the Southern sub-area. The bands are extended along the slopes and their width does not exceed 1-2 km. The sediments lie over Precambrian crystalline rocks, normally nearby outcrops of the latter.

By lithology, eluvium-deluvium includes brown, yellow-brown, crumbly, uniform loams, with inclusions of abundant non-rounded sand, gruss, gravel and fragments of crystalline rocks. Thickness of these sediments varies from 0.5 to 5 m increasing downward the slopes, in average 2.9 m.

Alluvial sediments are defined in the territory of Pryazovian crystalline massif where the river and gully beds are weakly developed by width. Thus, it is ascribed to undivided alluvial sediments (aPIII-H) the Holocene alluvium of the flood-land, as well as locally developed alluvium in the first, second and third over-flood terraces. Alluvium band width in the river upper courses is about some tens of meters increasing downward the course to 300-800 and more meters.

Two piles are distinguished in the vertical section. The upper one comprises dark-grey, greyish-yellow loams, medium, carbonate, with inclusions and interbeds of pebble and gravel of crystalline rocks. Lower pile is mainly composed of grey diverse-grained feldspar-quartz sands with interbeds of grey muds and bluish-grey clays. Inclusion amount notably increases to the section bottom. Alluvial sediments display oblique bedding. Thickness of alluvium varies from 0.6 to 13.6, in average 7.2 m.

Undivided Upper Neo-Pliocene – Holocene alluvial-deluvial sediments (adPIII-H) are confined to the gullies. In their lower courses the fragments of first, second and third terraces occur. Width of undivided alluvium bands attains 200-300 m. Gully bottom sediments include dark-grey muddy loams, in the lower part – sandy, with interbeds of sandy loams and sands, with inclusions of weakly-rounded particles of sand, gravel, gruss of crystalline rocks. Thickness of alluvium-deluvium does not exceed 5 m.

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Holocene (H) Holocene sediments comprise a variety of genetic rock types including continental (eluvial, coluvial,

alluvial, aeolian, deluvial-coluvial, proluvial-deluvial, alluvial-deluvial), marine and estuary-marine sediments. Holocene eluvial (eH) sediments are developed almost throughout and are absent only at the steep,

cliffy slopes of river and gully valleys and sea coast, and comprise the modern soils. At the watersheds and high terraces mainly thin low-humus back-earths are developed with humus content up to 5%. The soils are dark-grey, grainy-lumpy and nut-lumpy, with eluvial layer enriched in carbonate bunches. Thickness of the soil is up to 1 m. In the river flood-lands and first over-flood terrace the alkaline, salty and alkaline-salty soils are developed with humus layer thickness up to 0.8-1 m. At the gully bottom and over alluvial sediments of higher terraces the black-earth-alkaline soils are developed comprised mainly of heavy loams 1-1.5 m thick. On the gully and river valley slopes underwent erosion, as well as at the watersheds eroded soils are developed – removed and semi-removed black-earths up to 0.8 m thick. In composition the soils correspond to the light and medium loams.

Holocene coluvial (cH) sliding, collapse-talus sediments are developed in the coastal area of Azov Sea where the cliffy coast is formed. These are diverse displaced by gravity and mixed through the sliding and collapse-talus processes Quaternary rocks of various origins (eluvial, aeolian-deluvial, alluvial and alluvial-deluvial). They are composed of loams, clays, sandy loams, sands, pebble-stones. Collapse-talus sediments are developed along the foot of abrasion ledges and slide-break walls. Width of these sediments normally does not exceed some tens of meters. Thickness may attain 3-5 m. Slide rocks comprise the slide bodies. Thickness of the slide accumulations attains 20 m.

Deluvial-coluvial (dcH) sediments are developed in the coastal slope of Berdyanska sandbank and in the right slope of Berda River valley. They are being mapped in the bands 2.2-140 km long and 200-600 m wide. Formerly they were the same collapse-talus and slide rocks. But due to termination of abrasion processes and Berda River bank erosion the slope stabilization occurred. By lithology deluvium-coluvium consists of loams, sandy loams, sands, sandy clays, pebble-stones. In comparison to coluvial sediments they are more compressed. Thickness of deluvium-coluvium is 2.3-13.3 m.

Proluvial-deluvial (pdH) sediments are developed in Beryanska sandbank and were formed due to activity of temporary water streams upon extensive rainfalls and subsequent removal of eroded clays and loams from the gully that cut the hard-rock slope of Berdyansk town to the flat sandbank surface. Proluvial-deluvial sediments comprise the typical fan cone 1.4 by 1.4 km in size over the handing-wall of Holocene marine, estuary-marine sediments. They are composed of brown loams, sandy loams, with inclusions of gruss and gravel of crystalline rocks. Their thickness attains 5.5 m.

Holocene alluvial (aH) sediments are widely developed at the bottom of Lozovatka, Obitochna, Kiltychiya and Berda river valleys comprising flood-land terraces which width varies from 200 m (Lozovatka River, Novooleksiivka village) to 4700 m in the mouth part of Berda River. The flood-land sediments lie over alluvial sediments of the first and tenth alluvial terraces, over Neogene sediments and Precambrian crystalline rocks. Upper part of alluvium consists of various loams with interbeds of clays, muds, sandy loams, rarely sands, grey, dark-grey, greenish-grey, with yellow, brown-yellow stains of iron enrichment. Thickness varies from first meters to 9-15 m.

Lower part of the flood-land sediments consists of grey, dark-grey with greenish shade quartz-feldspar clayey sands with interbeds of clays, muds, sandy loams. At the bottom of alluvium gravel and pebble of crystalline rocks, sandstones and rounded carbonate concretions occur, thickness 0.2-0.9 m.

Thickness of alluvial sands varies from 2 to 12.5 m. Total thickness of Holocene alluvium varies from 4.2 to 33.0 m attaining maximum values in the mouth part of Berda River.

Holocene alluvial-deluvial (adH) sediments are confined to the gully bottom, mainly on the Southern sub-area. In the remaining territory of the map sheet they are included into undivided Upper Neo-Pleistocene – Holocene rocks. In the mouth parts of major gullies – Petrivska, Mokra and others – alluvium-deluvium band width attains 200-300 m. The sediments include grayish-yellow, yellowish-brown, brownish-grey, mainly medium loams, with interbeds of sands and sandy loams. At the section footwall inclusions of gravel and pebble of crystalline rocks and re-deposited carbonates are observed. Thickness of alluvium-deluvium varies from 0.8 to 7.3 m (4.4. m in average).

Holocene aeolian (vH) sediments are encountered in the sea coastal areas in Obitochna sandbank, in the islands nearby Berdyanska sandbank, where they form low (up to 3 m) heaps of marine sands, not overgrown with plants. They include yellowish-grey fine-grained quartz sands 0.5-30 m thick. The rocks were formed through blowing of dry beach sands in Holocene time.

Holocene technogenic (tH) sediments are developed wide enough. These include the mounds, remnants of military constructions, as well as numerous units resulted from extensive modern human activities: removed

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overburden rocks dumps, seaport embankment in the coast, waste storages and precipitation tanks in Berdyansk town area.

The mounds are thrown up over the graves some thousand years ago. Material for the mound construction was Holocene soil. The mound diameter at its foot may attain 200 m. Thickness of technogenic mound sediments depends on the mound height and attains 7 m. In places of 230 years old military constructions (Lantseve, Kalaytanivka villages) the soil ramparts preserved up to 10 m wide, 5-6 m high, and 400-500 m in diameter.

Nearby numerous quarries for crystalline rock mining there are the dumps of overburden, mainly Quaternary sub-aerial rocks and weathered crystalline rocks. The waste from the rock crushing also comes to the dumps. The dump size attains 200 by 100 m in the plane and 20-30 m thick.

In the sea coast embankment seaport constructions are ascribed to technogenic sediments. Holocene marine sands were used as the material for these facilities. The size of seaport constructions is 600 by 200 m.

The technogenic sediments also include the storages of domestic and industrial waste, liquid waste precipitation ponds and tanks in the western outskirt of Berdyansk town of commonly considerable size – 1 by 0.5 km and 0.5 by 0.5 km.

Holocene marine and estuary-marine (m,lmHač) sediments of Azovo-Chornomorskiy horizon are developed in the narrow band along the modern coast of Azov Sea, outside Obitochna and Berdyanska sandbanks. The width of marine sediment band (mHač) is commonly from some to 50 m and only in the western part of Berdyanska sandbank base it increases to 1 km. The rocks include white, light-grey, diverse-grained, quartz-feldspar sands with minor opaque minerals. The sands contain abundant broken mollusc shells, especially in the beaches. Along the beach back sides are observed the gravel and minor pebble of crystalline rocks, sandstones, limestones and carbonate concretions.

In places shell material predominates over sandy one providing interbeds up to 2.1 m thick. Some minerals contained in Holocene marine sediments contain radioactive elements (zircon, apatite, monazite and others). In the beach, due to the sea wave activity, the layer of dark and grey heavy concentrate is formed up to some centimeters thick which causes increased background in term of gamma and beta radiation that exceeds the sanitary standards. Thickness of marine sediments in the beach developed over the hard-rock coast, attains 4.8 m (at the base of Berdyanska sandbank).

Marine, estuary-marine sediments of Azovo-Chornomorskiy horizon are developed in Berdyanska and Obitochna sandbanks and comprise intercalation of marine sands and estuary-marine sediments themselves. The latter are composed of dark-grey to black sandy muds where mollusc shells and their detritus are contained.

The muds that cover bottoms of periodically drying estuaries are used in “Berdyansk” resort in medical purposes. Thickness of marine, estuary-marine sediments in the middle part of Berdyanska sandbank attain its maximum over entire studied area – 78.5 m.

To the south from the southern margin of the map sheet, in Obitochna sandbank, in Holocene marine, estuary-marine sediments the mollusc shells are found which are characteristic for Holocene Azovo-Chornomorskiy horizon. Of these, V.M.Semenenko had determined: Cardium edule L., C. exiguum Gm. In L., Chione gallina (L), Paphia rugata (B. D. D.), Abra ovata (Phil), Corbula (Lentidium) mediterranea (Costa), Cerithidium pusillum (Teffr), Mytilus sp., Theodoxus pallasi (Zindh), Rissoa splendis (Eichw.) that confirms Azovo-Chornomorskiy age of these sediments in the studied map sheet.

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3. NON-STRATIFIED UNITS These units include ultra-metamorphic, intrusive and metasomatic rocks of Archean and Proterozoic

age. In the map of crystalline basement the non-stratified units occupy less than 60% of territory and in the map of pre-Quaternary units – less than 20%. Crystalline rocks are mainly developed in Zakhidnopryazovska LTZ where they include Archean Sorokynskiy ultramafic complex and Proterozoic Novosilska association of mafic and ultramafic rocks, Obitochnenskiy gabbro-diorite-granodiorite, Chernigivskiy carbonatite, Kolarivskiy lamproite, Dyke complexes, and Volnovasko-Elanchytska and Zirchanska associations of Mesozoic minor intrusions, as well as Tokmatskiy, Shevchenkivskiy, Anadolskiy and Saltychanskiy granitoid ultra-metamorphic complexes.

Herein, the Complex includes those intrusive rocks whose age is defined precisely by isotopic geochronology methods and which are recorded in the correlation stratigraphic scheme by NSC of Ukraine.

The Association includes igneous rocks whose age is not defined precisely yet and which are not properly recorded in the stratigraphic scheme by NSC.

The time-based scheme of non-stratified units developed in the L-37-VII (Berdyansk) map sheet territory is as follows (ultra-metamorphic complexes are indicated with asterisk):

Paleozoic-Mesozoic undivided PZ-MZzk – Zirkska Association. Sub-alkaline gabbroids. PZ-MZvel - Volnovasko-Elanchytska Association. Trachytes. andesites, trachy-andesites, trachy-

basalts. Proterozoic Acron Neo-Proterozoic PR3d – Dyke Complex. Diabases, konga-diabases, lamprophyres, hornblendites Meso-Proterozoic PR2km – Kamyanomogylskiy Complex. Aplitoid granites, biotite-albite-microcline, rare-earth

pegmatites Paleo-Proterozoic PR1kl – Kolarivskiy Complex. Olivine lamproites PR1sl* - Saltychanskiy Complex. Albite metasomatites, albite pegmatites, albite aplitoid granites PR1cr – Chernigivskiy Complex. Calcite and dolomite carbonatites. Nepheline syenites PR1an* - Anadolskiy Complex. Aplites, muscovite-biotite leucocratic granites, granodioritic porphyry-

blastic granites PR1ob – Obitochenskiy Complex. Gabbro, gabbro-diorites, amphibolites, amphibole granodiorites PR1ns – Novosilska Association. Peridotites, pyroxenites, hornblendites, actinolitites Archean Acron Neo-Archean AR3sv* - Shevchenkivskiy Complex. Biotite-amphibole granodiorites, amphibole-biotite diorites,

quartz diorites, plagiogranites, plagio-migmatites AR3tk* - Tokmatskiy Complex. Charnockites, enderbites AR3sr – Sorokynskiy Complex. Ultramafics, komatiites, serpentinites, tremolitites. Description of intrusive and ultra-metamorphic units is given below separately.

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Intrusive units Archean Acron Neo-Archean Sorokynskiy Complex (sAR3sr). It is comprised of ultramafic dykes which cut meta-komatiites of Neo-

Archean Olginska Suite within Sorokynska tectonic zone (see “Tectonic scheme of crystalline basement”). However, they do not interact with rocks of overlying Krutobalkinska Suite of Osypenkivska Series and these relations define the time bounds of the Complex.

One of these dykes (50-100 m thick) is exposed in Berda River valley, in 2.5 km to the south from Rodionivka village (mouth of Sobacha gully and Blakynti Skeli ravine). By drill-holes and trenches this dyke is traced over about 5 km in latitudinal direction. The dyke is sub-vertical with steep (85-90o) dipping to the south.

Another dyke is encountered in Sadova site and is traced in gravity and magnetic fields by azimuth NW 315o over about 7 km. Magnetic field over both dykes is 500-1000 nT, residual gravity field – 0.5-1.5 mG. Magnetic susceptibility of ultramafic rocks is 5280*10-5 CI units, density – 2.75 g/cm3.

Among ultramafic rocks the porphyry serpentinites, serpentinized peridotite komatiites, chloritized and tremolitized peridotite komatiites and tremolitites are distinguished. The first rock type is characterized by dark-grey to black colouring and massive uniform porphyry structure caused by occurrence of white carbonate inclusions (pseudomorphs after olivine – up to 15%) on the background of prevailing (50-66%) serpentine; chlorite and phlogopite (up to 20%) and ore mineral (8-15%) occur in minor amounts.

In komatiites quite often olivine (up to 25%) and pyroxene (up to 10%) relicts are observed and also phlogopite (5-10%) and actinolite-tremolite (5-20%) occur; major minerals include serpentine (30-88%), carbonate (5-30%), chlorite (10-30%) and ore minerals (3-20%).

In the last rock variety of spotty silver-grey and black colouring tremolite and serpentine predominate in association with minor olivine relicts as well as phlogopite, chlorite, talc, bowlingite, carbonate and magnetite.

By petrochemical features, Sorokynski ultramafic rocks are high-magnesium (MgO content in places exceeds 30%), very low-titanium and alkali, Ca/Al ratio > 1; by Al2O3/TiO2 ratios they are close to komatiites of Barberton type.

There is no isotopic age dating for these rocks yet. However, the fact of their cutting by veins of confidently dated Shevchenkivskiy Complex granodiorites (2800 Ma) and relations with the rocks of Osypenkivska Series unequivocally suggest for their emplacement in Neo-Archean.

Proterozoic Acron Paleo-Proterozoic Novosilska Association (uPR1ns). It was established for the first time in the course of EGSF-200 [103].

Previously these rocks were considered to be the ancient Archean xenoliths distributed in the rocks of gneiss-migmatite sequence. Over EGSF-200 the data were obtained on the complex structure of these bodies and their cutting contacts with the country rocks. In addition, the data were also obtained on the old age of these intrusions since they are being cut by veins of plagioclasites, pegmatites and Proterozoic diabase dykes.

Novosilska Association includes the mafic and ultramafic rocks that form minor stock-like intrusions (250-500 m in diameter) confined to the central part of Saltychanskiy Dome. The rocks are well-exposed in Obitochna River valley nearby Novosilske village, remnants of Koza and Dakhno khutors, and along almost entire interval of this river from Chokrak River mouth in the south to Bila gully in the north. Novosilska intrusion is exposed in the right bank of large pond in 2.8 km higher Sosykulak River mouth. Six crescent-shaped bodies are distinguished, each 5-20 m thick and up to 100 m long, composed of hornblendites, actinolitites, tremolitites with distinct cluster-like actinolite-tremolite-asbestos aggregates. The ultramafic bodies are separated by conformable gabbro and gabbro-diorite bodies apparently formed through the layering in the single magma chamber because of no evidences for the contact changes between the rocks.

In the intrusion of Bila gully, tremolitites are lacking whereas hornblendites and the rocks of gabbro and gabbro-diorite composition predominate. Intrusions are cut by plagioclasite and quartz veins (up to 40 cm thick). On Berda River, nearby Sadove and Karla Marksa villages, the inner portions of intrusions are composed of peridotite and amphibolized pyroxenite, and outer ones – of hornblendite; these rocks are cut by syenite-pegmatite dykes up to 5 m thick.

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In physical fields the rocks of given association are variously expressed. Less altered ultramafic varieties are exhibited in magnetic field of 1000-2000 nT and residual gravity field of 1.0-1.5 mG while highly altered varieties provide low values in both magnetic and gravity fields, 50-200 nT and 0.1-0.2 mG respectively (see “Scheme of anomalous magnetic field” and “Scheme of local gravity anomalies” in the scale 1:500 000).

Magnetic susceptibility of olivine hornblendites is 773*10-5 CI units, feldspar hornblendites – 75*10-5 CI units, tremolite actinolitites – 5170*10-5 CI units, tremolitites – 15650*10-5 CI units, gabbro-diorites – 4730*10-5 CI units; density is 3.07 g/cm3, 3.05 g/cm3, 3.10 g/cm3, 3.0 g/cm3, 2.83 g/cm3 respectively.

Mineral composition of peridotites (variously altered) is as follows (%): olivine – 1-10, clinopyroxene – 0-8, orthopyroxene – 0-7, tremolite – 20-50, serpentine – 0-30, anthophyllite – 0-10, magnetite – 2-25, iddingsite – 0-5. By chemical composition two groups are distinguished: enriched in MgO (in excess of 25%) and those with its moderate MgO content (15-25%) and slightly enriched in SiO2 (44-47%).

Composition of amphibolized pyroxenites is as follows (%): hornblende – 45-80, diopside – 8-35, enstatite – 0-1, biotite – 0-10, oligoclase – 0-10. Magnesium content is low (13%) and SiO2 – relatively high (up to 50%).

Mineral composition of olivine- and pyroxene-bearing hornblendites (%): hornblende – 70-98, olivine – 0-8, clinopyroxene – 0-4, andesine – 0-5, magnetite and ilmenite – up to 10, biotite – up to 3. Feldspar hornblendites are composed of (%): hornblende – 55-97, oligoclase-andesine – 7-25, biotite – up to 2, microcline – 0-13, clinopyroxene – up to 1, quartz – up to 5.

Mineral composition of tremolite actinolitites (%): actinolite – 65-98, tremolite – up to 20, antophyllite – 0-27, microcline – 0-10, oligoclase – 0-5, magnetite – up to 15. Nearby Andriivka village in Bila gully chlorite actinolitites and tremolitites are encountered. In these rocks abundant chlorite (15-50%) and tremolite (47-92%) occur as well as antophyllite (up to 15%) and magnetite (2-15%). Talc tremolitites are enriched in MgO (28%).

Mineral composition of gabbro and gabbro-diorites is as follows (%): hornblende – 45-60, andesine – 20-35, biotite, clinopyroxene, tremolite, antophyllite, quartz, magnetite – up to 5-15.

Described rocks attracted attention of geologists for a long time as the locators of various mineral deposits. Directly they can be used as the raw material for petrurgy. Pyrope is found close to the intrusion within similar rocks (at Andriivka village) that assumes their perspectives in term of diamond prospecting. In the rocks and associated eluvial-deluvial sediments increased contents of gold and PGM are determined.

Radiological age of the rocks is not determined. However, their relationships with diorites of Obitochnenskiy Complex suggest for their genetic link (to be earliest magmatic phase) and their ascription to Paleo-Proterozoic.

Obitochnenskiy Complex (n, nd, d PR1ob). This Complex includes diorites, gabbro-diorites and gabbro which form a range of massifs and vein bodies mainly within Saltychanskiy Dome being exposed in the valleys of Obitochna, Chokrak, Kiltychiya and Lozovatka rivers. The rocks (except vein ones) are conformable in relation to the gneisses of Zakhidnopryazovska Series, granitoids of Shevchenkivskiy Complex and migmatites developed after the latter. It is observed that the rocks surround the oval (syncline and dome-shaped) second-order structures. Rarely the cutting contacts of diorites with host rocks are observed (see “Geological map of crystalline basement”).

The gabbro comprises the most melanocratic rocks. Opaque mineral content (amphibole, clinopyroxene) is about 60-70% by rock volume. Content of SiO2 is 49%. Gabbro-diorites contain less opaque minerals (up to 40%). And SiO2 content is about 55%. Gabbro and gabbro-diorites are developed in the core of intrusive bodies. Diorites are observed by periphery of the bodies comprising the “rim” around melanocratic gabbro and gabbro-diorite.

Mineral composition of diorites is as follows (%): plagioclase # 45-55 – 40-60, hornblende – 30-50, biotite – 1-7, quartz – up to 3-5, clinopyroxene – up to 5; gabbro-diorites: plagioclase # 40-70 – 50-60, biotite – 5-7; quartz diorites: plagioclase # 30-45 – 50-65, hornblende – 20-30, quartz – 5-10, biotite – up to 10; granodiorites: plagioclase # 20-35 – 40-55, hornblende – 10-15, quartz – 15-20, biotite – 10-15, microcline – 10-20; micro-diorites: plagioclase – 30-60, quartz – 3-20, biotite – up to 15, hornblende – up to 10.

Hornblende in diorites is bluish-green with iron-magnesium index 30-50% and high aluminum content in tetrahedron coordination. By chemical composition the rocks of this Complex are mainly ascribed to plutonic rocks of intermediate range and normal alkalinity. Somewhat high chromium content (106 g/t) and low – zirconium (121 g/t) and yttrium (20 g/t) are noted. From similar rocks of Shevchenkivskiy Complex the given ones differ in a bit lower strontium content (550-600 g/t in comparison to 600-800 g/t in Shevchenkivskiy case).

The gradual transitions are observed between all rock types included in the Complex, that is, individual intrusive phases are not distinguished except the vein one to which micro-diorites, micro-tonalites and plagioclasites are ascribed. However, it was noted above that mafic and ultramafic rocks of Novosilska Association can be considered as the first phase in intrusion.

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In magnetic field the rocks of Obitochnenskiy Complex are expressed with positive anomalies from 50 to 400 nT, and in the gravity field – from 0.3 to 0.8 mG.

Magnetic susceptibility of diorites is 500-1000*10-5 CI units, gabbro-diorites – 4250*10-5 CI units, micro-diorites and micro-tonalites – 23*10-5 CI units, plagioclasites – 12*10-5 CI units. Density is 2.7-2.8 g/cm3, 2.84 g/cm3, 2.7 g/cm3, 2.61 g/cm3 respectively.

The age of Obitochnenskiy Complex rocks is not determined using confident methods. Available data include K-Ar determination by hornblende yielded 2020-2150 Ma [24] and U-Pb one by zircon yielded discordant values of 1840 and 2200 Ma [38].

Chernigivskiy Complex (u1, x2, qx2, jx3, al, c4 PR1cr). It includes typical comagmatic counterparts of carbonatite complexes: alkaline ultramafic rocks, ijolite-melteigites, nepheline syenites, the rocks of syenite-nordmarkite-tweitosite series, carbonatites and others. Alkaline syenites and carbonatites are most widespread. Nepheline syenites and alkaline pyroxenites are subordinated to above ones. Remaining rock varieties (olivinites, peridotites, ijolite-melteigites) are observed as inclusions in carbonatites or in the thin single bodies (carbonatite kimberlites, essexites etc.). Besides mentioned igneous rocks, the Complex also includes alkaline (essentially sodium) metasomatites – fenites. They form exo-contact aureole (up to 100 m) in the country rocks and are also developed inside the massif where they replace the remnants of primary rocks. The rocks of Chernigivskiy Complex are overlain by the platform cover with sedimentary rock thickness up to first tens of meters.

Geophysical fields over the area of this Complex rocks display mosaic patterns. In magnetic field these are the spots up to 1000-1500 nT on the background of 500-600 nT, and in residual gravity field on the background of 0-7 mG there are observed rounded or elongated (1.5-2 km) anomalies with negative Δg values up to 1-2 mG (see “Scheme of anomalous magnetic field” and “Scheme of local gravity anomalies” in the scale 1:500 000).

Magnetic susceptibility (in CI units) of alkaline pyroxenites is 1178*10-5, nepheline syenites – 323*10-5, alkaline syenites – 954*10-5, carbonatites (average) – up to 436*10-5. Density (g/cm3) is 2.98, 2.65, 2.71 and 3.1 respectively.

Most of described rocks constitute dyke-like bodies developed in the arch-shaped extension fault gently convexed to the west. Carbonatites and allied rocks within this fault are extended over about 30 km and their total thickness in the widest sections is 600-700 m. The fault under review sub-conformably follows up concentric structure in around Saltychanskiy Dome – shear-type “break-apart” in the eastern limb of Lozovatska anticline. The arch-shaped structure of the Complex is split (with slight horizontal displacement) by Stulnivskiy Fault in two almost same-length massifs or blocks. The Northern one – Novopoltavskiy – s extended in the north-eastern direction, and in the north it joins Chernigivsko-Vyacheslavskiy Fault, and in the south, next 3 km from Stulnivskiy Fault, it is in tectonic contact (junction by normal) with pink granite body of the same strike ascribed to Anadolskiy Complex. The Southern massif (Begim-Chokrakskiy) of south-eastern extension is also tectonically pinched out in the north and south.

Likewise Chernigivskiy Complex, in the similar arch fashion the different by origin (vein, porphyry-blastic, anatectic etc.) Anadolski granites are distributed in the area and their integrated contour likely surrounds the southern massif and in this way separates the two. It is notable that Anadolski granites are not displaced by Stulnivskiy Fault. Apparently this suggests for Novopoltavskiy and Begim-Chokrakskiy massifs filled not the single and then split arch structure but two contiguous extension zones set up after granite formation.

The rocks of carbonatite complex were discovered in 60th for the first time in the course of geological mapping in Novopoltavskiy massif (M.I.Lebedev [91]) but carbonatites themselves were identified much later in 70th in the course of prospecting and exploration works (E.M.Lapitskiy, V.A.Barkhotov and others [86-90]). Later on Begim-Chokrakskiy massif was discovered (M.F.Rusakov and others [105]). The comprehensive analysis of geological setting, composition and genesis of the rocks are given elsewhere [14, 28], based mainly on the most studied Novopoltavskiy massif. Using these results, below the brief description of major rock types is presented in the order of general succession of their emplacement.

Alkaline ultramafic rocks comprise heterogeneous rock group where just the alkaline pyroxenites are of individual importance and formed prior to other rocks of the Complex. The following rock succession is defined:

1) Alkaline pyroxenites that form dyke-like bodies up to 60 m thick. Their mineral composition (%): clinopyroxene (aegirine 9-20%) – 60-100, magnetite – 2-15, ilmenite – 1-15, amphibole – 0.5-5, biotite – 0.5-10, calcite – 0.5-5, apatite – 0.5-5, sphene – 0.5-5. Accessories: zircon, orthite, graphite, sulphides.

2) Segregation or vein (?) rocks – tweitosites, genetically linked with syenite series. Their mineral composition (%): clinopyroxene (aegirine – up to 15%) – 70-80, apatite – 10-25, perthite and quartz – up to 5, as well as amphibole, biotite, calcite. Accessories: orthite, sphene, pyrochlore-hatchettolite, magnetite, sulphides, zircon and barite.

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3) Segregation inclusions in carbonatites formed together with the latter. Their composition depends on type of carbonatites. Among such inclusions the following are defined: clinopyroxene-amphibole-biotite ultramafic rocks, phlogopite glimmerites, peridotites, olivinites etc.

Ijolite-melteigites (commonly melteigites) are known only as xenoliths in carbonatites. Their mineral composition (%): clinopyroxene (aegirine – 14-22%) – 40-70, nepheline – 25-50, calcite – 0.5-20, hortonolite – 0-15, amphibole – 0-15, biotite – 0-5, apatite – 1-5. Accessories: zircon, monazite.

Nepheline syenites constitute thick (about 150 m) dyke-like body in the northern part of Novopoltavskiy massif. Their mineral composition (%): albite – 60-80, nepheline – 5-40, biotite – 5-25, calcite – 2-10, microcline – up to 5, apatite – 0.1-5. Accessories: zircon, hornblende, hatchettolite, niobium rutile.

The rocks of syenite-nordmarkite series are most widely distributed. Thickness of their individual bodies attains 100 m. Normally these are coarse-crystalline pegmatoid rocks. Their mineral composition depends on numerical relations between alkaline feldspars, aegirine-bearing clinopyroxenes and quartz. Minor and accessory minerals are sphene, apatite, orthite, amphibole, biotite, calcite, molibdenite, pyrochlore-hatchettolite. Among the rocks of this series most widespread are alkaline syenites which contain 10-15% of clinopyroxene.

The common feature of all silicate rocks in the Complex is mandatory occurrence of primary-magmatic carbonates which highlight their comagmatic nature and carbonatite affinity.

Carbonatites that form the dyke series of various thicknesses (often about 50-60 m) include the group of widely distributed rocks of the Complex. These rocks contain at least 50% of carbonates. By composition of the latter the rocks are subdivided into calcite (soevites and alvikites), calcite-dolomite and dolomite (beuforcites) varieties as well as transitional rock to kimberlites – kimberlite carbonatites. All these varieties are considered to be the mantle intrusive-magmatic rocks. It is supported by C, O, Sr isotopic composition of carbonatites – δavg

13C = -5.8 ‰; δavg

18O = +8.3‰; 87Sr / 86Sr = 0.7006, as well as by findings in these rocks the chilled contacts, fluidal textures, melted inclusions in minerals etc. Carbonatites were emplaced in discrete mode. It is evidenced by changes in their mineral assemblages from phase to phase – with increasing carbonate magnesium content of each next phase (from soevites to beuforcites) changes the composition of silicates. In soevites silicates include amphibole, clinopyroxene and biotite (together – up to 40%), in beuforcites – olivine and phlogopite (together – up to 35%), and in alvikites both calcium and magnesium-iron silicates occur. In typical alvikite varieties their content is 10%. In all types of carbonatites apatite content varies from 2-4 to 14%, and in phosphorites it ups to tens of percents. The latter rocks comprise essentially apatite or apatite-magnetite enclaves in beuforcites up to first meters thick. Accessory minerals determined in all mentioned rock types: pyrochlore-hatchettolite, columbite, zircon, monazite, sphene, ilmenite, sulphides. In addition, orthite and magnetite are found in soevites, and cerium fergusonite, baddeleyite, gahnite, pleonaste and graphite – in beuforcites.

Besides described carbonatites, in the southern part of Novopoltavskiy massif the vertical dykes (up to 10 m thick) of kimberlite carbonatites are encountered. They are quite locally developed and occupy first percents of carbonatite spaces. These are melanocratic breccia-like phlogopite-olivine(serpentine)-calcite rocks containing 25-50% of carbonates. Their accessory minerals include zircon, baddeleyite, pleonaste. In contrast to carbonatites, they do not contain niobium- and REE-bearing minerals (see “Geological map of crystalline basement”).

Thus, based on above description as well as experimental and petrologic data on carbonatite complexes in general, it can be concluded that primary magmas were alkaline-ultramafic melts formed at sub-crustal depth through the partial melting of mantle source. Concerning Chernigivskiy Complex itself, the following simplified scheme for carbonatites and allied rocks formation can be drawn:

melteigite+CO2+carbonatite+nepheline syenite and (or) alkaline syenite+fenitising fluid of sodium composition

This process of mantle carbonatization and formation of carbonatite and allied melts depended on the depth since solubility of carbon dioxide increases with pressure increasing. This is why it is thought that carbonatite melts are being formed at the depth more than 80 km where CO2 solubility attains 40 wt. %. It is also known that with pressure (depth) increasing sequentially calcite, dolomite, ankerite and other carbonatites are formed. This succession does correspond to the sequence of Chernigivskiy Complex carbonatite emplacement – soevites, alvikites, beuforcites. Obviously, in theory (in the scheme above) the “own” nepheline and/or alkaline syenites/nordmarkites as well as fenites should correspond to each carbonatite type. Mentioned syenite melts, being lighter in comparison to carbonatite ones, would be accumulated at the roofs of melting regions and, respectively, should be first ones entered the faults getting open. These are exactly the rock relationships observed in the Complex: both nepheline syenites and rocks of syenite-nordmarkite series are being cut by all types of carbonatites. However, the subdivision of syenite-nordmarkite series into the rocks that correspond to carbonatites of different phases was failed and this is why they were described above as pre-carbonatite rocks. The same “generalization” also concerns fenites. The latter ones are well divided into four phases by degree of

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country rocks re-working (fourth-phase fenites after granitoids have composition of alkaline syenite) which correspond to the integral metasomatic process related to development of the Complex as a whole.

Established succession of magmatite emplacement by the order of their formation depth increasing – from crustal Anadolski granites to mantle magmatites of carbonatite complex – defines not only the depth of the arch-system faults in Western Pryazovya but also the distinct downward mode of its sequential opening.

Isotopic age of carbonatite complex rocks on zircons from beuforcites is 2.09 Ma [41]. The same age is also obtained by K-Ar method on micas and amphiboles. Besides carbonatites, in the studied area the similar age is attributed to the hornblendite dykes of alkaline-ultramafic composition that form the north-west-trending belt [15] and REE-bearing Saltychanski granites.

Kolarivskiy Complex (PR1kl). It is established for the first time in the course of EGSF-200 in 1992 [103]. Lamproites of various composition do form the minor (up to 200-500 m in diameter) pipe-like stocks of which the first one (“Mriya”) was discovered nearby Kolarivka village. Similar bodies are known in the upper course of Komyshuvata gully (left branch of Kyltychiya River) close to Zelenivka and Orlivka villages, in upper courses of Mokra Konka, Velyka Tokmachka and Kainkulak rivers. At the outskirts of Kolarivka and Zelenivka villages the stocks of mica kimberlites up to 10 m in diameter are encountered in the plagiogneiss and migmatite country rocks (see “Geological map of crystalline basement”).

In the core part of “Mriya” pipe the olivine lamproites occur which to the periphery are changed by amphibole-phlogopite lamproites comprising main part of the body. In the north-western periphery the phlogopite-amphibole lamproites (cortlandites) are distinguished. In the rounded xenoliths (up to 10-12 cm) olivine-serpentine rocks are observed. The vein phase is comprised of the mono-mineral hornblendite dykes 1-8 m thick.

Magnetic susceptibility of amphibole-phlogopite lamproites is 3030*10-5 CI units, serpentinites – 180*10-5 CI units; rock density is 2.82 and 3.10 g/cm3 respectively.

Amphibole-phlogopite lamproites are dark-greenish-grey, massive, medium-fine-grained rocks with poikilo-dia-blastic prismatic-grained, cluster-ray texture and the following mineral composition (%): light-green amphibole (tremolite) – 18-40, ice-coloured amphibole (cummingtonite) – 3-27, phlogopite – up to 64, clinopyroxene relicts – up to 10-20, magnetite – up to 8, ilmenite – up to 2; accessories – apatite, zircon, moissanite, corundum, spinel, rutile, garnet, graphite; secondary minerals: chlorite, serpentine, epidote, carbonates. By chemical composition these are sub-alkaline mafic rocks with SiO2 – up to 48%, K2O – up to 3.6%, MgO – up to 21.5%, CaO – 7.2%, Al2O3 – 6%. The rocks display high content of chromium (14 g/t) and nickel (7 g/t) as well as cobalt and copper (up to 0.5 g/t).

Mineral composition of phlogopite-amphibole lamproites is as follows (%): amphibole – 20-70, phlogopite – 25-35, olivine – 10-20; accessories: apatite, zircon, sphene, staurolite, barite, sulphides; secondary: serpentine, bowlingite, talc, carbonates, chlorite.

Mineral composition of olivine lamproites (%): olivine and replacing it serpentine – 30-70, orthopyroxene – up to 20, phlogopite – 8-15, magnetite – 10-15, tremolite, actinolite – up to 10. Secondary minerals: biotite, bowlingite, chlorite, epidote, sphene; accessory: cromium-magnetite, picro-ilmenite, chrom-spinelides.

Mineral composition of vein hornblendites (%): amphiboles (hornblende, actinolite, tremolite) – 55-92, phlogopite – 5-30, plagioclase – 3-5, quartz – up to 1; accessories: ilmenite, apatite, sphene, magnetite, garnet, zircon; secondary: serpentine, carbonates, chlorite.

Phlogopite age from lamproites at Kolarivka village determined by K-Ar method is 1950-1970 Ma. Age of granites that cut above rocks, determined by U-Pb method on zircon is 1720 Ma.

The rocks of the Complex are thought to be perspective for diamond deposits and gold mineralization. Vermiculite occurrences are genetically linked with weathering crust.

Meso-Proterozoic Kamyanomogylskiy Complex (ig2, r2 PR2km). In the map sheet area the vein bodies of the Complex are

developed comprised of pegmatites, pegmatoid granites and granite-aplites. In the most extent these ones are encountered in Temryuk and Karatyuk river basins, as well as in the middle course of Berda River and in Berestova River basin (area of Zakharivka, Sachky, Sadove, Vesele, Storozhove, Kalaytanivka, Karla Marksa and other villages). It is characteristic for pegmatites the low body thickness (up to 10 m) and sub-vertical setting. Increased radioactivity (up to 100-500 gammas) comprises the distinct feature of pegmatites and pegmatoid granites caused by radioactive zircon, monazite and orthite content in the rocks. Small places of the Complex pegmatites are known at Andriivka village (Chervona Gora deposit). Here meat-red microcline pegmatites constitute the bodies up to 30 m thick. In Chabanska gully these rocks cut the bodies of Saltychanskiy Complex white granites (see “Geological map of crystalline basement”).

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Pegmatites are pink, meat-red or pink-grey coloured, with coarse-grained or pegmatoid texture. Average mineral composition of these rocks is as follows (%): microcline-perthite – 50-70, albite-oligoclase – 5-10, quartz – 25-40, biotite – 0-10; accessories: zircon, orthite, fluorspar, magnetite, hematite, monazite, beryl, cassiterite, tourmaline; secondary: iron hydroxides.

In heavy concentrate from meat-red pegmatites are determined (g/t): magnetite – 21, biotite – 2111.7, amphiboles – 1041.6, monazite – 2276, zircon – 719, apatite – 898, ilmenite – 10, pyroxene – 19, tourmaline, chlorite, moissanite, iron hydroxides – single grains.

By petrochemical features the pegmatites, granite-pegmatites and granite-aplites of the Complex are high-alumina al’ = 21.28, sub-alkalic (Na2O+K2O) = 8.49, potassium-sodium series rocks, Na2O/K2O = 0.85, fractionation coefficient Kf = 0.92.

In comparison with all-period granites (after R.Daly) and other complexes, the vein granitoids of the Complex display decreased content of CaO, MgO, Fe2O3 and slightly increased content of alkalis at clear potassium predomination over sodium. Relative acidity Ac of pegmatites is lower than one of vein granites and aplites.

Vein bodies of granite-aplites are less developed. They are observed in single bodies in the south-eastern part of the map sheet.

The mineral composition of pink, pink-light-grey fine-medium-grained vein granite-aplites in average is as follows (%): microcline-perthite – 35-60, oligoclase, albite-oligoclase – 10-25, quartz – 20-40, biotite – 01-5, muscovite – 0-3; accessories: zircon, monazite, apatite, magnetite, garnet, ilmenite; secondary: sericite, iron hydroxides, pelitemorphic aggregate, chlorite.

In heavy concentrate from pink vein granite-aplites are determined (g/t): magnetite – 18,773, ilmenite – single grains, biotite – 19,357, carbonate – 3,803, amphibole – 13,852, zircon – 321, sulphides – 36,051, feldspar, in places in intergrowth with quartz – 892,905, apatite – 9,953, sphene – 1,721, monazite – 1,995, leucoxene – 273, iron hydroxides, hematite, epidote, garnet, rutile, tourmaline – single grains.

Density of vein pink granite is 2.65 g/cm3, magnetic susceptibility – 68*10-5 CI units. In physical fields the vein bodies are not distinguished due to their small size.

Concerning mineral resources, the pegmatites were mined as radioactive ore in the end of 40th – beginning of 50th by quarries in Temryuk River basin. Zircon, monazite and orthite were extracted from the ores. Nowadays the pegmatites are not economic.

Neo-Proterozoic Dyke Complex (b, qb, c, u PR3d). The rocks of Neo-Proterozoic Dyke Complex occur in veins, dykes

and stocks and are developed over almost entire map sheet territory. The bodies are composed of hornblendites, glimmerites (biotitites), biotite-amphibole-plagioclase lamprophyres, diabases and konga-diabases.

Hornblendites and glimmerites (uPR3) are encountered in Kolarivskiy, Andriivskiy and Elyseivskiy quarries and in outcrops on Obitochna (Shevchenko village) and Kiltychiya rivers and in other places where the rocks occur in dykes from 0.1 to 10 m thick. They cut pegmatites of Saltychanskiy Complex and, in turn, are cut by lamprophyre stocks and pipes. Magnetic susceptibility of hornblendites is 6680*10-5 CI units, density – 3.1 g/cm3.

In many dykes hornblendites alternate with glimmerite bands up to 10-15 cm thick. Mineral composition of hornblendites (%): hornblende – 75-90, sphene – 5-18, biotite – 0-15, plagioclase (# 25-29) – 0-15; accessories: apatite, magnetite and titanomagnetite, ilmenite, zircon, orthite. By chemical composition they belong to low- and medium-alumina ultramafites-mafites of potassium or potassium-sodium series and by TiO2 and alkalis content are similar to Yakutia kimberlites. Probably, it was not casual that in hornblendite from Andriivskiy quarry the 0.15 mm in size diamond crystal was found [113]. From the other hand, these rocks are mainly related to Chernigivskiy carbonatite complex (see “Geological cross-section by line A1-A4” to the “Geological map of crystalline basement”).

Mineral composition of glimmerite (%): biotite, rarely phlogopite – 40-79, hornblende – 0-25, oligoclase – 5-10; secondary minerals: chlorite, actinolite, muscovite, epidote, zeolites; accessories: sphene, orthite, fergusonite, corundum, ilmenite, magnetite, rutile, monazite, garnet. By chemical composition these are intermediate rocks of normal and sub-alkaline, mainly potassium range, medium-alumina (correspond to trachy-basalts).

Biotite-amphibole-plagioclase and biotite-plagioclase lamprophyres (cPR3) are much less developed. Their minor stocks (up to 10-30 m) or dykes (up to 10 m) are encountered in Andriivskiy and Kolarivskiy quarries, in Khvostyanka gully and nearby Lantsevo village on Berda River.

Magnetic susceptibility of lamprophyres is 4300*10-5 CI units, density – 2.88 g/cm3.

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By mineral composition they correspond to spessartite or minette: oligoclase-andesine (from 3-10 to 58%), orthoclase, microcline, and sometimes anorthoclase (from 0-5 to 25-40%), hornblende, tremolite or actinolite (from 0-10 to 12-25%), biotite (2-23%), quartz (0-10%); accessories: apatite, zircon, magnetite, sphene, pyrite, rutile, moissanite, spinel, corundum; secondary: chlorite, sericite. By chemical composition they belong to medium-alumina rocks of potassium series, sub-alkaline range.

The age of these rocks is not determined. By their relationships with the rocks of Saltychanskiy and Kolarivskiy complexes the age is taken approximately at 1.8 Ga.

Diabases, dolerites and konga-diabases (qbPR3) do form extended dykes (kilometers and tens of kilometers) oriented mainly in sub-latitudinal and north-western direction and confined to the deep-seated faults (Sorokynskiy, Elyzavetinskiy, Stulnivskiy and others), rarely isometric pipe-like bodies.

The longest dyke is found in the zone of Stulnivskiy Fault and is traced over about 50 km at 10-20 m thickness; it is exposed in the quarry of Bila gully where it cuts the rocks of Novosilska Association; to the west and east it is traced by drill-holes [104] up to Komyshuvatka gully and Sorokynska zone where it changes its strike to south-eastern up to Rodionivka village where it becomes sub-latitudinal again.

Another dyke more than 8 km long is also traced in latitudinal direction from outskirts of Gyunivka and Radolivka villages through Mogyla Saltycha to Chabanska gully in Andriivka village.

In magnetic field these dykes are clearly expressed with narrow elongated anomalies up to 500 nT. Pipe-like diabase bodies are expressed in residual gravity field by positive anomalies up to 0.1 mG.

Magnetic susceptibility of diabases is 1390*10-5 CI units, density – 3.01 g/cm3. Mineral composition (%): andesine (# 42-50) – 40-57, augite – 27-42, olivine – up to 10, magnetite – up

to 10, quarts – up to 2, in konga-diabases – up to 7-10, feldspar – up to 10, hornblende – up to 5, biotite – up to 5, rarely 15, orthopyroxene – up to 25, in dolerites sometimes titanaugite – up to 35; accessories: apatite, rutile, sphene, ilmenite; secondary: chlorite, epidote, sericite, carbonate, serpentine, iddingsite, actinolite, tremolite. By chemical composition they correspond to mafic and intermediate rocks of normal range.

Radiological age of diabases is determined by whole-rock K-Ar method to 1450 Ma [24]. Paleozoic-Mesozoic undivided Zirkska Association (enPZ-MZzk). For the first time it is defined in Eastern Pryazovya in the course of

DGM-50 over Volodarska field (V.F.Rozdorozhniy, 1986-1990). Association includes rounded in the plane three-four-phase intrusions of sub-alkaline gabbroids (first phase – pyroxenites, second – essexites-shonkinites, third – micro-syenites, and fourth – carbonatites). Intrusions positioned in the map sheet limits (upper course of Mokra Konka River) are two-phase. The second phase (shonkinite-essexite) is extensively developed and constitutes actually entire volume of intrusive bodies while much less abundant third phase comprises thin (up to 1-2 m) micro-syenite dykes (see “Geological map of crystalline basement”).

In the course of EGSF-200 [103] three minor (from 500 to 1400 m) stock-like intrusions of shonkinite-essexites and micro-syenites are mapped higher by Mokra Konka River nearby Zhukovka gully and Dibrova and Zrazkove villages. Two of these bodies cut the rocks of Archean Lower Dragunska sub-sequence and the third one (Mogyla Ryasna mound) – the rocks of Verkhnyotokmatska Sequence. At the contact with country rocks the chilling zones up to 0.5 m thick are found. In the exo-contacts crushing zone after host plagiogneisses is developed (10-15 cm) followed by the pink micro-syenite zone (up to 10 cm). In the host plagiogneisses also abundant corundum occurs formed after sillimanite due to thermal influence of intrusion.

In physical fields the rocks are expresses by high magnetization – 1000-1200 nT and gravity anomalies (up to 0.5 mG).

Mineral composition of shonkinite-essexites (%): augite or titanaugite – 20-30, andesine (# 34-36) – 24-36, orthoclase and microcline – 10-20, biotite – 5-10, hypersthene – up to 5, olivine – up to 1; secondary minerals: chlorite, serpentine, bowlingite, iddingsite, uralite; accessories: apatite, magnetite. By chemical composition these are intermediate medium-alumina rocks of potassium series, sub-alkaline range.

Quartz micro-syenites that form thin dykes (up to 1-2 m) are composed of microcline-perthite (30-60%), oligoclase (20-25%), quartz (10-20%), albite (up to 5%), biotite (up to 5%), amphibole (up to 5%) and muscovite (1-3%). These are high-alumina intermediate rocks of potassium-sodium series, sub-alkaline range, with high enough content of SiO2 (64%) and alkalis (Na2O+K20 = 8%), agpaite coefficient – 0.84.

The age of shonkinite-essexites is determined by whole-rock K-Ar method to 296 Ma that corresponds to Carboniferous time [24].

Volnovasko-Elanchytska Association (t, a, ta, tb, wb PZ-MZvel). It is defined in Eastern Pryazovya in the course of DGM-50 over Kalmiuska field (V.V.Vasylchenko, 1989-1995). Volcanic units and trachy-andesite and andesite dykes were ascribed to the Association. In the limits of L-37-VII map sheet it includes andesite

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volcanic units as well as dykes of trachytes, trachy-andesites, andesites, andesite porphyries, picrite basalts, rhyolites and quartz porphyries.

Association is comprised of a wide range of young dyke rocks developed in around Saltychanskiy Dome. These include picrite basalts, trachy-basalts, andesites and trachy-andesites, trachytes, quartz porphyries. They form the bodies from tens of centimeters to 20 m thick which cut age-different rocks of Precambrian basement. Their strike is mainly sub-latitudinal and dipping is close to vertical. Besides the dyke bodies, the isometric ones occur, probably, paleo-volcano necks (core portion of Saltychanskiy Dome). The major dyke of trachy-andesites is traced over about 35 km (thickness 15-20 m) between Belmanka, Bilotserkivka, Starchenkove villages.

In the physical fields these dykes are not expressed. Magnetic susceptibility of trachy-andesites is 170*10-5 CI units, density – 2.83 g/cm3.

Mineral composition of picrite-basalts (%): andesine-labrador – 30-40, chlorite – 10-27, carbonate – 3-15; phenoctysts-vesicles are composed of calcite (up to 10%), chlorite (2-7%) and ore mineral.

Trachy-basalts (%): phenocrysts: andesine-labrador – 10-25; in groundmass: andesine – 24-67, actinolite hornblende – 8-15, diopside – up to 10, biotite – up to 10, quartz – 2-5, magnetite – 5-15.

Trachy-andesites (%): phenocrysts: oligoclase – 2-10, amphibole – up to 10, orthoclase – 2, clinopyroxene – up to 3, quartz – up to 1; groundmass: amphibole – up to 15, biotite – up to 5, oligoclase-anorthoclase – 40-60, clinopyroxene – 1-15, apatite – single grains up to 5.

Trachytes (%): phenocrysts: microcline – 2-5, oligoclase-albite – 2-5, quartz – up to 7, magnetite – up to 3, mica – up to 1; groundmass: albite – 30-55, orthoclase – 10-30, glass – up to 36, diopside – up to 15, phlogopite – up to 10.

Rhyolites and quartz porphyries (%): phenocrysts: plagioclase, orthoclase, quartz (aggregate of grains – up to 5-17); groundmass: feldspar and quartz – 70-80, biotite – up to 5, hornblende.

There are some rock isotopic age determinations by K-Ar method: andesites (210-235 Ma) and orthopyres (270 Ma) from dykes in Mokra Konka River area nearby Kinkski Rozdory [24]; andesite porphyry (320, 80 and 70 Ma) from drill-hole at Partyzany village [58]. In Eastern Pryazovya for these rocks the age of 340 Ma is obtained [24].

Ultra-metamorphic units Archean Acron Neo-Archean Tokmatskiy Complex (c, en AR3tk). It includes high-temperature pyroxene-bearing granitoids (enderbites

and charnockites) of ultra-metamorphic origin developed mainly in Tokmak River basin after the rocks of Zakhidnopryazovska Series. In Novopoltavskiy crushed-stone quarry (Mogyla Synya) they form isometric bodies up to 10 m across which occur within mafic gneisses and linked with these rocks by gradual transitions. In the same area, by geophysical data, amoeba-like 1.3 by 3 km in size body of chranockitoids is defined which occurs within plagiogneisses and mafic gneisses of Verkhnyotokmatska Sequence. It is marked by low-intensity (200-400 nT) magnetic field. In residual gravity field it is expressed by negative (0-1 mG) values. More often enderbites and charnockites are observed in leucosome of banded migmatites developed after the rocks of Zakhidnopryazovska Series.

Average composition of enderbites (%): plagioclase (#35-40) – 50-65, quartz – 10-25, hypersthene – 5-10, clinopyroxene – up to 5, hornblende and biotite – up to 10, K-feldspar – up to 10; accessory minerals: apatite, zircon, ilmenite, pyrite, sphene, garnet, rutile, barite, fluorspar, topaz. In charnockites microcline-perthite content may attain 55% and plagioclase (#20-22) content decreases to 25-30%. Iron-magnesium index of hypersthene is 38-55%, clinopyroxene – 28-48%, hornblende – 35-56%, biotite – 34-36%.

Content of SiO2 in enderbites is 61-65%, in charnockites – up to 69%; alkalis – 5-7% at sodium predomination over potassium in the former rocks and reversely – in the latter. Iron-magnesium index of enderbites (50-52%) is slightly higher than one of charnockites (46-48%).

From zircon isotopic dating the age of Tokmatskiy Complex enderbites is estimated to 2700-2800 Ma. Shevchenkivskiy Complex (gd, d, qd, pg, m AR3sv). It includes diorites, quartz diorites, granodiorites,

plagiogranites and plagiomigmatites developed mainly in Saltychanskiy Dome and in Berestovska Syncline. As it was pointed above, there are some difficulties in distinction between the rocks of diorite composition included in Shevchenkivskiy and Obitochnenskiy complexes. Of course, Archean age of the former and Proterozoic age of the latter is confident but the rock age determinations are scarce. The geochemical criteria are more

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accessible, particularly, increased Sr content in Obitochnenski diorites in comparison to Shevchenkivski ones but these numeric data are also limited. Diorites of Shevchenkivskiy Complex commonly associate with tonalites and plagiogranites whereas Obitochnenski – with gabbro, gabbro-diorites and granodiorites. And in spite of these observations the distribution of mentioned rock types in the map remains quite conventional. The rocks of Obitochnenskiy Complex are mainly confined to the core portions of Saltychanskiy Dome while Shevchenkivskiy Complex rocks – to its periphery. The outcrops of the latter are observed on Obitochna and Kiltychiya rivers at Shevchenko, Olenivka, Andriivka, Novotroitske, Sofiivka villages, on Lozovatka River at Kolarivka and Yuryivka villages, on Berda River at Osypenko, Kalaytanivka, Zakharyivka, Sadove, Vesele villages, on Karatyuk and Temryuk rivers (see “Geological cross-section by line A1-A4” to the geological map of crystalline basement).

In magnetic field these rocks are expressed with slight positive anomalies up to 100-200 nT, and in residual gravity field – by negative gravity values (-0.25 … -0.75 mG). Magnetic susceptibility of plagiogranites is 724*10-5 CI units, density – 2.65 g/cm3.

Mineral composition of plagiogranites (%): oligoclase-andesine – 35-70, quartz – 25-32, biotite – 1-5; accessories: magnetite, apatite, zircon, orthite, ilmenite, garnet, pyrite. By chemical composition the rocks are similar to enderbites of Tokmatskiy Complex and correspond to high-alumina rocks of normal-range potassium-sodium series.

Likewise plagiogranites massifs, granodiorites are developed mainly in the east of studied map sheet. Granodiorites constitute the rounded in the plane bodies from 2 to 5 km across that slightly only cut the country rocks. The roof portions of these massifs often occur at the depth about some hundred meters below the surface and are weakly exposed. Diameter of visible granodiorite outcrops is several hundred meters attaining maximum of 2 km (Troitskiy, Osypenkivskiy and other massifs).

Characteristic feature of granodiorites that are exposed at the surface is their slight albitization and K-feldsparization with muscovite development that makes the rocks close to apogranites [4]. In case of granodiorite occurrence within the country rock plagiogneisses metasomatic alteration is developed in the latter of which silicification is the major.

Plagiomigmatites are widespread in Saltychanskiy Dome. By structure-texture features the banded and shadowed varieties are distinguished. Most widespread are banded plagiomigmatites where melanosome is composed of biotite gneiss of Verkhnyotokmatska Sequence (thickness of interbeds from some millimeters to tens of centimeters), and neosome – of aplitoid or pegmatoid plagiogranites and diorite. Neosome interbeds commonly are parallel to the schistosity of melanosome and cutting veins are observed in places. Less abundant are amphibole and amphibole-biotite layered migmatites where melanosome is composed of amphibole and amphibole-biotite plagiogneisses and very rarely the migmatites with substratum of pyroxene-bearing gneisses occur.

The shadowed migmatites display the spotty or unclear-banded structure. The boundary between melanosome and leucosome in unclear, smoothed and these two differ one another by mineral composition.

The age of Shevchenkivskiy Complex plagiogranites is determined by U-Pb method on zircon to 2780 Ma, granodiorites – 2800 Ma, and diorites – 2850 Ma [41].

Proterozoic Acron Paleo-Proterozoic Anadolskiy Complex (ig, g, gd, m PR1an). It includes pink and pink-grey diverse-grained, often

porphyry-like biotite and muscovite-biotite leucocratic granites developed in Lozovatska anticline structure, mainly in the rim of Chernigivskiy carbonatite massif. These granites are exposed in quarry at Mogyla Synya, on Tokmak River at Mogylyany and Chernigivka villages, on Yushanly River at Zelenivka and Bogorodytske village outskirts. In the map sheet L-37-VII territory the following varieties of Anadolskiy Complex rocks are distinguished: medium-grained granites and granodiorites with red K-feldspar porphyry-blasts; pink aplite-pegmatoid granites that are gradually changed by migmatites; pink fine-grained and meat-red coarse-grained granites with black quartz that form the veins with sharp contacts.

The low values of magnetic (-50 … -300 nT) and residual gravity (-0.25 … -1.0 mG) fields do correspond to the above granites. Their magnetic susceptibility is 41-46*10-5 CI units, density – 2.62 g/cm3.

The mineral composition of the first type granites and granodiorites is as follows (%): plagioclase (albite-oligoclase) – 20-42, microcline and microcline-perthite – 15-35, quartz – 20-25, biotite – 5-10, hornblende – up to 7; accessories: apatite, zircon, orthite, ore minerals. Their chemical composition is characterized by relatively low SiO2 content (68.35%), slightly increased MgO (1.41%) and low Na2O (3.83%) and K2O (3.72%) content.

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Mineral composition of most widespread granites of the second type (%): microcline – 37-55, plagioclase – 8-40, quartz – 25-42, biotite – 0-6, muscovite – up to 5, hornblende – up to 2 (in marginal facies only). In chemical composition the high SiO2 (72-75%) and alkalis (Na2O – 3.5-4%, K2O – 4.5-5.5%) contents are characteristic.

Mineral composition of vein granites (%): oligoclase – 10-40, microcline – 25-60, quartz – 30-35, biotite – 5-10, muscovite – up to 10; accessories: apatite, zircon, sphene, orthite, garnet, monazite, ore minerals.

In geochemical respect granites of Anadolskiy Complex are characterized by increased content of Rb (269 g/t), Pb (29 g/t), Ва (823 g/t), La (91 g/t) and Се (127 g/t).

Anadolski migmatites are exposed in Chokrak and Yushanly river basins, to the west of Zamostya village, in Kainkulak and Tokmak river mouths, and in the central part of Bilotserkivska syncline. Here plagiogneisses had undergone the inter-layer injection by pink granite matter. Thickness of injection veins is up to first centimeters, in places up to 10-20 cm. Close to the veins the paleosome is essentially K-feldspatized and transformed into migmatites. However, in general amount of neosome veins does not exceed 25% of the rock volume. Besides green biotite and chlorite ice-coloured muscovite is widely developed. Visually these are the rocks with clear coarse-banded structure caused by alternation of pink microcline bands with light-grey cream quartz-biotite-plagioclase bands. The rocks are heterogeneous, the relicts of host biotite gneisses are scattered in the rock like spots and shadows with unclear smoothed boundaries. Average mineral composition of migmatites (%): albite-oligocalse, oligoclase – from 2-10 to 20-30, microcline – 20-45, biotite – from 3-5 to 15-20, muscovite (normally developed after biotite and plagioclase) – 0-9; accessories: magnetite, ilmenite, zircon, apatite, sphene; secondary: chlorite, sericite, epidote. Chemical analyses of migmatites vary depending on paleosome and neosome mineral composition. The spectrum of trace-elements in migmatites is exactly the same of the paleosome and neosome ones. In the maps of magnetic field and residual gravity anomalies the migmatites display transitions from negative values in case of high neosome content to positive values when the latter is low.

In genetic respect these are typical ultra-metamorphic rocks formed through metasomatic re-working and partial melting of Archean gneisses and granitoids in Early Proterozoic.

Ascription of all described granites to Anadolskiy Complex whose petrotype is defined in Eastern Pryazovya (Anadolskiy massif), is somewhat conventional since granites of the first and two last types notably differ from the petrotype ones; perhaps, in the future it would be more suitable to distinguish these rocks in separate association or complex. It is only known that these are one of the youngest orogenic granites in Pryazovya. The information on their isotopic dating in the map sheet is lacking. The age of Anadolski granites in Eastern Pryazovya by U-Pb dating on zircon is estimated to 2085+25 Ma [24].

Saltychanskiy Complex (PR1sl). The grey and pink-grey fine-medium-grained biotite granites with orthite traditionally are ascribed to this Complex; they form four minor massifs (from 0.3 by 0.4 to 1 by 3 km2 in size) at the outskirts of Saltychiya (Mogyla Saltychiya or Kamyana), Radolivka and Gyunivka villages. Now we propose some expansion of the Complex ascribing to it the granites of Andriivskiy petrotype defined by V.F.Rozdorozhniy [103]; most of large pegmatite fields in Western Pryazovya are related to these granites. The rocks under discussion are exposed at the western outskirt of Andriivka village, in Chabanska gully, at Ivanivka, Elyseivka (Bagy gully), Vyboeve, Karla Marksa and Mykolaivka villages (Berda River basin) where they also constitute minor (up to 1-4 km across) stock-like intrusions.

Earlier K.Yu.Esypchuk [20] had argued that Krasnokutski granites, that control lithium-bearing pegmatites of Shevchenkivske deposit, comprise the non-orthite analogs of Saltychanskiy Complex granites.

At the present knowledge of the territory aforementioned granite ascription is thought to be temporary since Saltychanski and Andriivski granites, being similar in radiological age, are somewhat different in mineralogical composition (in Andriivski granites plagioclase is more felsic, there is no accessory orthite characteristic for Saltychanski granites, and accessory garnet occur) and petrochemical features (in Andriivski granites: Na2O+K2O = 7%, Na2O/K2O = 4; in Saltychanski granites: Na2O+K2O = 8%, Na2O/K2O = 0.6); Andriivski pegmatites display rare-metal and ceramic specialization, Saltychanski – rare-earth one. It should be noted that further definition of white albite-oligoclase-microcline two-mica granites of Andriivskiy type and related pegmatites into the separated complex is fairly possible.

In the physical fields granites of Saltychanskiy Complex are expressed by negative or low positive values of magnetic field (-100 … +100 nT) and negative residual gravity field (0.25-1 mG). Magnetic susceptibility of Saltychanski orthite granites is 534*10-5 CI units, Andriivski granites – 68*10-5 CI units; density – 2.65 and 2.63 g/cm3 respectively.

Mineral composition of Saltychanski granites (%): microcline – 20-35, oligoclase – 20-50, quartz – 25-30, biotite – 8-20, muscovite – up to 7, hornblende (in contact zones only) – up to 10; accessory minerals: orthite – up to 3, sphene, zircon, magnetite, britholite, apatite, monazite, ilmenite.

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Mineral composition of Andriivski granites (%): microcline-perthite – 25-45, oligoclase – 12-40, albite – up to 30, quartz – 25-35, biotite – 1-10, muscovite – up to 8, garnet – up to 4; accessories: monazite, magnetite, pyrite, apatite, garnet, rutile, moissanite.

By chemical composition Andriivski granites, in comparison to Saltychanski ones, are somewhat enriched in SiO2 (74% and 70% respectively), Na2O and depleted in K2O (1.5% and 5%); the latter is explained by superimposed albitization. Granites with sodium predomination over potassium are also known in the central part of Saltychanskiy massif.

Age of biotite from Saltychanski granites is determined by K-Ar method to 1900 Ma; by U-Pb method on orthite and sphene received age values are 1900, 1960 and 2130 Ma. Age of biotite from Andriivski granites is determined by K-Ar method to 2060 Ma.

Concerning ore specialization, the pegmatites of this association are mainly of ceramic type. At the same time, the bunches containing columbite-tantalite mineralization are encountered in pegmatites. In addition, the bodies of albite-spodumene pegmatites (Kruta Balka deposit) are discovered in Sorokynska tectonic zone.

Metasomatic rocks Three groups of metasomatic rocks are distinguished in the map sheet territory: 1) skarn-like rocks and

epidosites; 2) alkaline metasomatites; 3) secondary quartzites and argillizites. Skarn-like rocks and epidosites are grey, greenish- or pink-grey, from very dark, almost black to light,

spotty, fine-grained, quite strong, with conchoidal fracture rocks of fairly variable mineral composition. These include pyroxene-garnet-plagioclase and pyroxene-garnet-amphibole-plagioclase, garnet-epidote-quartz, epidote-quartz and essentially epidote rocks. They are locally developed in lend-like and sheet-like interbeds from first to some tens of meters thick and up to 100 and more meters long. The host rocks include gneisses and migmatites of Zakhidnopryazovska and Tsentralnopryazovska series, in places granitoids of Shevchenkivskiy and Anadolskiy complexes.

V.F.Rozdorozhniy [103] considered these rocks to be eclogites. Previously they were described as metamorphic rocks – deeply metamorphosed carbonate-clayey rocks of primary sedimentary origin. Nowadays these rocks are unequivocally treated to be metasomatites of skarn origin formed through influence of granitizing fluids over calcium-enriched metamorphic rocks: crystalline limestones, calciphyres, metamorphosed marls or amphibolites.

Skarnoids are observed in exposures on the right bank of Karatyuk River (in 1 km to the north-west from Sadove village, in 100 m higher the dam), on the right bank of Berda River (in 1 km to the south from Berestova River mouth, between Karla Marksa and Mykolaivka villages), on the left bank of Tokmak River (at the north-eastern outskirt of Chernigivka village and in 200 m higher of Kainkulak River mouth), on the left bank of Chokrak River (to the west from Panfilivka village), on the left bank of Yushanly River (nearby Boyove village), in the quarry at south-eastern outskirt of Zelenivka village, and many other places. Normally almost all of mentioned rock varieties are observed in a single outcrop displaying some kind of zonation. The earliest are amphibole-pyroxene-plagioclase rocks then garnet appears which replaces pyroxene; further epidote is developed which replaces all early formed minerals, then quartz and sometimes scapolite.

On the right bank of Obitochna River, higher up the mouth of Sosykulak River, in front of Dakhno khutor remnants, the quartz-epidote rocks with garnet are known for a long time and are described by G.L.Kravchenko [73]. In our mind, these rocks comprise one of the deepest stages of amphibolite skarnation under influence of granitizing fluids related to Obitochnenska and Saltychanska intrusions.

Plagioclase which amount varies in the range 10-75% has the composition of andesine-labrador-bitovnite although in highly-epidotized and silicified varieties it downs to oligoclase-albite, completely disappears, and in places is replaced by microcline. Hornblende content may attain 30% although most often it is absent. Clinopyroxene (up to 20%) is bright-green diopside with сNg = 40–60°; Ng = 1.710–1.765; +2V = 55–70°; f = 30–87%. It is replaced by pink garnet of grossularite-andradite composition which content does not exceed 10-15%. Epidote content normally does not exceed 25-30% although in some varieties it forms almost mono-mineral rock (epidosite) or is associated with quartz (quartz-epidote rock). Scapolite (up to 15-20%) is comprised of marialite (Na-scapolite) with 78-80% of meionite (Ca-scapolite) compound. Quartz is developed in marginal zones of skarnoid units in spindle-shaped elongated grains; elongated relicts of aggregate composed of plagioclase, sphene and epidote are preserved between the latter quartz grains. The rock may be changed by secondary quartzite.

Magnetic susceptibility of pyroxene- and garnet-bearing rocks is 946-500*10-5 CI units, density – 3.05-2.99 g/cm3.

In the fault zones and exo-contacts of granite intrusions the epidote rocks of other type are observed – green or pink-green (with microcline), rarely almost black rocks which fill up tectonic fractures in the host rocks

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or almost completely replace the latter. Commonly these rocks occur in Sorokynska tectonic zone, on Berda River, and on Tokmak and Kainkula rivers, in zones of cataclasis and milonitization.

Epidote-chlorite-albite metasomatites, defined by V.O.Tsukanov [117] under the name helsinkites, are developed in sub-latitudinal zones of conformable extension faults which bound Obitochnenska granodiorite-diorite intrusion from the north (upper course of Obitochna River).

Helsinkites of Pivdennoobitochnenske field are confined to the arc-shaped extension fault within quartz diorites and tonalites of Saltychanskiy massif. In magnetic field the rocks are well expressed by negative anomaly. Thickness of the zone of altered rocks attains 700 m. They are traced by drill-holes and geophysical data over the distance of 10 km (the rock are not exposed anywhere). From periphery to the centre of the zone the following rock changes are observed: 1) cataclased diorites and tonalites with epidotized hornblende; 2) chlorite-epidote rock (30-40% by volume) with relicts of altered plagioclase and hornblende as well as newly-formed quartz. albite and K-feldspar; 3) helsinkites composed of albite (up to 60%), epidote (30-70%) and chlorite (up to 15%); in coarse albite grains relicts of primary epidotized plagioclase are observed; 4) chlorite-epidote-albite rock (each mineral content is 10-20-70% respectively) with quartz veinlets (up to 5-10%) and hollows filled with prehnite and calcite. Thickness of the zones varies in a wide range.

Helsinkites of the incipient stages of metasomatism differ from unaltered rocks by increased content of SiO2, Fe2O3 and K2O. Aluminum, iron oxide, calcium, magnesium and sodium content in the rocks are decreased. Albite-prehnite rocks of the final stage are highly enriched in sodium, aluminum and water.

The time of helsinkite formation does correspond to the final post-magmatic development stage of Obitochnenskiy Complex intrusions (Late Paleo-Proterozoic).

Fenites, developed in the rim of Chernigivskiy carbonatite massif and described above in review of respective complex, are ascribed to the group of alkaline metasomatites.

Products of silica metasomatism include secondary quartzites and argillizites. The first ones are already partially mentioned as the final stage of high-calcium rocks skarnation process. But most widely these rocks are developed in the eastern part of the area where the separate process of acid metasomatism within Katerynivskiy and Mykolaivskiy faults is superimposed onto Archean gneisses and plagiogranites which previously were crushed and cataclased. Feldspar quartzites, which are exposed and mined in Mogyla Vysla quarry, comprise highly fractured rocks composed mainly of quartz with relicts of feldspars and mica, extensively kaolinitized in the upper part. In the exo-contacts of thick body (more than 150 m) quartzites are iron-enriched. Occurrence of gold in quartzites from hundredth gram per ton to visible particles up to 0.1 mm in size is characteristic [73].

Similar secondary quartzites are also exposed in Bogdan Hill, in Sklyana Golova ravine, on Berestova River nearby Sadoviy khutor.

Argillizites or chlorite-quartz-kaolinite rocks are observed together with secondary quartzites and in separate dyke-like bodies in Lozovatka River valley (Lysycha gully).

Mineral composition of quartzites (%): quartz – 70-95, plagioclase – up to 5 (in places up to 8-10), microcline – up to 10 (in places up to 20), muscovite – up to 15, biotite – up to 4, sillimanite – up to 12. Accessory minerals: apatite, magnetite, hematite, ilmenite, pyrite, zircon, monazite, rutile.

Composition of argillizite (%): kaolinite – 45-75, quartz – 30-40, K-feldspar – 10-15, chlorite – 3-8, iron hydroxides – 2-8; accessories: magnetite, zircon, apatite.

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4. WEATHERING CRUST AFTER CRYSTALLINE ROCKS Weathering crust comprises a complex of rocks formed over transformation of igneous, metamorphic

and sedimentary rocks in continental environments under influence of various weathering factors. In the area, this is a layer of variable thickness that lies between Meso-Cenozoic and crystalline basement rocks. The upper surface (crust hanging-wall) corresponds to the basement surface relief whereas the lower surface (crust footwall) defines the depth of chemical and physical disintegration processes developed in basement rocks. Since the relief formation was controlled by the mode of tectonic motions, climate, hydrodynamics of the water flows, water chemical composition, and wind erosion, the thickness of weathering crust varies for different places. Due to extensive erosion in Cretaceous tine, the crust is absent in the area of Lower Cretaceous rocks development in the south and south-west of Prychornomorska Depression. It is also lacking in the beds and valleys of modern rivers. In a whole, erosion sites comprise 25% of the studied area territory.

In the “Map of weathering crust thickness isopachs” three levels are conventionally distinguished (Fig. 4.1) that correspond to the thicknesses 0-10, 10-20 and more than 20 m.

The first level (0-10 m) is a basic one and in spatial respect it defines the fields of weathering crust development in general. These crust thicknesses spatially are related to the watershed ridges as well as with lower portions of river valley and gully slopes and water-collecting hollows.

The second level (10-20 m) is observed higher of the first one. This level exposure sites are located in the mid and upper watershed portions as well as the mid and upper river courses due to slightly reduced hydrodynamics of the water flows. Second-level weathering crust is more locally developed.

The third level (20 m and more) is even more locally developed. It is related to the graben-like structures – Stulnivska and Chernigivska depressions, Obitochnenskiy graben etc. In some drill-holes thickness of weathering crust exceeds 20-30 m.

Two types of weathering crust are distinguished by the forming conditions and morphological features – aerial and linear ones. The first type is developed predominantly. The second one is observed in the weakened zones of tectonic breaks and rock contacts where the atmospheric and surface water infiltration prevailed over considerable time. In places the aerial crust gets the linear-aerial appearance when the broken rocks plunge down being elongated in the narrow bands.

Three zones are distinguished in the weathering crust column. Zone of incipient products is observed over entire studied area (Fig. 4.1). Zone of transitional products

is less developed and is confined to the small sub-isometric, oval or irregularly-shaped sites. Zone of the final weathering products is preserved quite locally. It should be noted, that incomplete weathering crust profile in the map sheet L-37-VII (Berdyansk) is caused by erosion and subsequent re-deposition of the upper crust horizons. It is evidences by occurrence of high-kaoline clays with slightly rounded quartz grains in Poltavski and Sarmatian sediments [104].

The rock diversity in the crystalline basement of the studied map sheet had caused the various degree of rock weathering despite of the uniform climate conditions. Degree of weathering however depends not only on the rock composition but also on the primary rock structure-texture patterns and tectonic environments. Quartzites and other mono-mineral fine-grained and massive rocks underwent the least weathering. And essentially feldspar, biotite, tremolite, actinolite schists, ultramafic rocks, amphibolites, ferruginous quartzites and other rocks are most weathered.

Litho-genetic types of weathering crust are being defined depending on composition and complexity of the primary rocks. The typomorphic crust section with distinct final weathering products is formed after each primary rock (rock complex) through the sequential modifications. For instance, relatively thick, well-expressed, almost free of clay material disintegration zone is formed after metamorphic and igneous rocks of felsic composition. And after mafic and ultramafic rocks this zone is being developed under reduced rate. Actually these rocks undergo extensive chemical weathering “skipping” the stage of typical disintegration.

In case of aerial weathering crust, it is most widespread after granitoid rocks when all three zones are developed (upward):

1. Zone of incipient weathering products (disintegration zone) where degree of disintegration increases upward. It is composed of crushed stone, gruss, in places sand. Structure-texture patterns and primary mineral composition of the rocks are completely preserved. Maximum thickness is up to 40 m.

2. Zone of transitional weathering products (hydromica-kaoline). In this zone the primary rocks are being transformed into the clayey-sandy mass without their structure-texture patterns breaking. Feldspars are being pelitized, micas – hydrated; and other opaque minerals are being serpentinized, chloritized and destroyed.

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Fig. 4.1. Sketch geological map and map of mineral resources of weathering crust 1 – sites of lacking weathering crust; 2-4 – planar-type weathering crust zones: 2 – zone of final weathering products; 3 – zone of transitional weathering products (hydro-micas); 4 – zone of incipient weathering products (disintegration); 5 – linear-type weathering crust zones; 6 – boundaries of weathering crust zones; 7 – isopachs of weathering crust (drawn through 10 m); 8-10 – strato-isohypses of crystalline basement relief: 8 – positive, 9 – zero, 10 – negative; 11-13 – faults: 11 – deep-seated; 12 – major; 13 – minor.

MINERAL RESOURCES

GROUP SUB-GROUP COMMODITY MINERAL DEPOSITS OCCURRENCES METALS FERROUS Iron Fe

NON-METAL ORE COMMODITIES

ADSORPTIVE RAW MATERIALS Vermiculite

vrад

NON-METALS CONSTRUCTION

RAW MATERIALS

GLASS AND PORCELAIN-FAIENCE

RAW MATERIALS

Primary kaoline

example: 87number by listmineralfield of use

;; vr

ad

example: number by listsymbol of valuablecomponent

;

- for metallic minerals

155

- for non-metallic minerals

Deposit (occurrence) symbol includes:

STUDY DEGREE OF DEPOSITS AND OCCURRENCES

deposits with exploredeconomic reserves

underexplored deposits assessed non-perspective occurrencesunderexplored occurrences

ECONOMIC DEVELOPMENT OF DEPOSITS

never been mined

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3. Zone of the final products – clayey (kaolinite-montmorillonite). It is characterized by the strong chemical transformation of primary mineral composition, structure and texture of the rocks, with formation of kaoline or montmorillonite with minor hydromica. Transitions between the zones are gradual, smoothed.

Depending on the mineral composition of the primary rocks underwent weathering the following mineral varieties of weathering crust are distinguished:

1. Kaolinite – it is formed after granites, migmatites, biotite gneisses and plagiogneisses. 2. Kaolinite-montmorillonite – after amphibolites, amphibole-biotite, amphibole gneisses and

plagiogneisses. 3. Nontronite-montmorillonite – after mafic gneisses. 4. Limonite – after ferruginous quartzites. Just the kaolinite and nontronite-montmorillonite crust types are widely developed over the studied

area. Deposits and occurrences of siderite ores, vermiculite and kaoline are associated with the weathering crusts.

Vermiculite-bearing weathering crust is most studied. In is developed in the right bank of Lozovatka River, at the western outskirt of Kolarivka village, within “Mriya” pipe and some pipe-like bodies in Komyshuvatka gully to the east of Andriivka village.

The lower crust boundary altitudes vary from +10 m to +30 m; thickness of the crust – from 6 to 30 m. Disintegration zone is intersected in almost all drill-holes that had intercepted lamproites. The crust

exposures are encountered in the quarry nearby Kolarivka village. The crust is composed of crumble lamproites retaining the primary structure-texture patterns. The rock is extensively cut by the dense network of variously-oriented fractures filled up with iron hydroxides providing the rock brown-rusty colouring. The clay minerals and chlorite are observed both in fractures and the rock groundmass. Thickness of disintegration zone varies from 1.5 to 21.5 m.

By mineralogical analyses data, disintegration zone of Kolarivskiy Complex lamproites contains (in average, g/t): magnetite – 77,000, rutile – single grains, pyroxenes – 165,000, amphiboles – 374,000, phlogopite – 77,000, apatite – single grains, olivine – 64,000, sulphides – minute grains, chlorite – 33,000, iron hydroxides – 44,000, rock fragments – 166,000. Average chemical composition of lamproite weathering crust in disintegration zone (%): SiО2 – 46.1, Al2O3 – 6.14, Fe2O3 – 5.48, FeО – 3.2, TiО2 – 0.54, P2O5 – 0.185, MnО – 0.115, CaО – 6.05, MgО – 22.8, SO3 – 0.075, K2O – 2.6, Na2O – 1.7, LOI – 5.44, sum – 100.4.

Zone of transitional dismembering (transitional weathering products) stacks up profile of the lamproite weathering crust but the size of its development sites is much less in comparison with ones of disintegration zone. It is composed of sandy-clayey, in places with fine gruss, brownish-green crumble rock mass. The rounded dark crystals of olivine and amphibole and silver mica flakes (vermiculite-hydrophlogopite) are embedded in the clayey mass. Amount of the latter varies from first percents to 80%. With increasing the mica content the size of its flakes rises from 1 mm to 1 cm. Under eluvial process the mineral grains lose their luster, get blurred and become dully, brittle, opaque minerals get faded. Phlogopite is getting hydrated and chloritized, it does form vermiculite-like aggregates. In parallel to the changes of lamproite physical properties and mineral composition the rock texture-structure patterns are also getting changed and become less prominent. The rock colour in this zone is mainly brownish-greenish-grey. Chemical composition of weathering crust in hydration zone (%): SiО2 – 39.8, Al2O3 – 4.15, Fe2O3 – 7.32, FeО – 1.18, TiО2 – 0.30, P2O5 – 0.12, MnО – 0.11, CaО – 5.80, MgО – 27.0, SO3 – 0.068, K2O – 0.14, Na2O – 1.0, LOI – 12.91, sum – 99.9. Potassium and in lesser extent sodium are extensively removed from the zone of transitional dismembering. Then silica, alumina, titanium and calcium are being removed but in less amount. Ferrous oxide goes into iron oxide form but iron remains unmovable in general. Likewise, magnesium is actually being retained on site. Losses on ignition essentially increase suggesting for considerable growth of clayey minerals amount in weathering crust. Thickness of the zone is up to 13 m.

Zone of the final dismembering (clayey weathering products) of lamproite rocks in the area is absent due to erosion and denudation but its former existence is revealed from the re-deposited weathering crust – secondary one.

Besides the aerial weathering crust the thick linear one is encountered in the area in relation with Chernigivska fault zone. Thickness of the crust here attains 400 m and more; discontinuous and incomplete profile of the crust is also noted in case of all zones mixing and formation the uniform clayey-gruss pile. More detailed description of weathering crust after alkaline-ultramafic in Chernigivska tectonic zone is given elsewhere in numerous reports of E.M.Lapytskiy [86-90].

The age of weathering crust in the studied map sheet L-37-VII (Berdyansk) is Meso-Cenozoic. And the exposure of crystalline basement coupled with the weak development of sedimentary cover over the territory facilitates development of weathering processes at present time as well.

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5. TECTONICS In tectonic respect the map sheet territory belongs to Pryazovskiy mega-block of Ukrainian Shield

where it occupies mainly its south-western part and is characterized by the complex structure of the Earth crust (see “Model geological section” by the line A1-A4).

The models of the deep crustal structure are based on the numeric interpretation of DSS and other geophysical data [39]. On this ground, mainly by the speed parameters for various crystalline rock types, the sketch sections were designed for the consolidated Earth crust of Ukrainian Shield. According to the model, the crust consists of three “layers” (downward) which conventional composition is defined by the speed of longitudinal waves (Vp, km/s): “granite” – 5.7-6.4, “diorite” – 6.4-6.8, and “basalt” – 6.8-7.6.

Over the map sheet territory this crustal section does correspond to so called transitional type of crust with the following crustal thickness (km) and “layer” percentage: 1) “granite” – 10 (25%), “diorite” – 22 (55%) and 3) “basalt” – 8 (20%). This allows assumption that from the depth 10-15 km [36, 39], that is, at the lower sub-sphere bottom of Saltychanskiy Dome the crust apparently consists of granitized mafic granulites which in petrophysical respect do correspond to so called conventional “diorites”. This assumption is supported by the fact that almost over entire map sheet (except its south-eastern corner) the deep magnetic heterogeneity is projected which is considered to be typical for the lower part of granulite belts [39]. This treatment of the crustal structure is in agreement with the structure of Moho surface. Evidently, the area of eroded Saltychanskiy Dome is associated with the lowest depth of this surface – 35 km whereas thickness of the western rim of the Dome and the eastern flank of Orikhivsko-Pavlogradska zone is 40 km and more.

In other words, both surface and deep structure of the studied area do not contradict to the accepted model of crystalline basement, and, in addition, structure of its surface is well expressed in sub-concentric patterns of anomalous magnetic and gravity fields.

It is also important for the super-deep (mantle) structure of the map sheet that almost entire its territory coincides with the projection of so called north-east-trending lineament E-E’ [39] defined by the features of asthenosphere surface. Obviously, occurrence of diverse deep magmatites – carbonatites as well as diamond-bearing rocks in the studied area is related just to these deep-structure features.

Likewise other regions of Ukrainian Shield, two tectonic levels different in composition and structure are distinguished in the area: lower – crystalline basement, and upper – platform cover composed of horizontal strata of crumble rocks.

Lower tectonic level It is mainly composed of granitoids and gneisses that were formed and modified at the considerable

deep (up to 25 km) crustal levels under conditions of ductile deformations in the age interval up to 1.5 Ga. On the ground of structure, chrono-statigraphic, petrologic and other relationships of crystalline rocks it is thought that over that time the Earth crust was forming, growing and re-building many times. Its final structure at the present erosion slice is shown in the map of crystalline basement. Four first-order various-scale structures are distinguished in the map. In the list below each next structure involves even the younger rocks. And the general feature of all these units is their significant re-building in Proterozoic as it is evidenced from widely developed Proterozoic ultra-metamorphism and magmatism. Thus, the major tectonic elements in the studied area include:

1. Saltychanskiy Dome (Oval) of concentric structure, up to 40 km in diameter, is mainly composed of age-different (Archrean and Proterozoic) granitoids. It occupies the central part of the map sheet.

2. Heterogeneous folded envelope of Saltychanskiy Dome. It is mainly composed of metamorphic rocks of various Archean and, in lesser extent, Proterozoic series.

3. Berestovska Syncline – the fragment of heterogeneous envelope of Manguskiy oval of Central Pryazovya.

4. Eastern flank of Orikhivsko-Pavlogradska suture zone composed of both Archean basement (extensively migmatized) and Proterozoic metamorphic sequences that form narrow linear structures of various orientations.

Two latter first-order tectonic units are presented by their marginal parts only and occupy up to 30% of the map sheet area.

Below the major structures of the lower tectonic level are considered.

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Folded and magmatic structures The doubled title of Saltychanskiy Dome (oval) is revealed from the centroclinal dipping of involved

rocks in almost all exposures. It is especially clear expressed in the dome core on Chokrak and Obitochna rivers. At the first look, these tectonic patterns contradict to the definition of structure which is considered to be the dome but this can be reliably explained from the point of view that widely-accepted deep erosion of Pryazovskiy geo-block (especially in comparison with adjacent Middle-Dniprean one) resulted in elimination the upper sub-sphere of the former dome and only its lower portion is being mapped in the studied area [16].

The most extensive granitization and migmatization processes, in comparison to other first-order structures, comprise the second important feature of the structure under discussion. This is why Zakhidnopryazovska Series, shown in the map, is observed here mainly in substratum of migmatites and extensively migmatitized rocks and very rarely – in thin lenses within numerous granitoid complexes of the deeply-eroded dome.

Internal structure of Saltychanskiy Dome is fairly complex and for the first time it was considered by some authors [117, 43] on the ground of geological mapping in the scale 1:50 000. According to these and other data, there are widely developed almost isometric syncline structures up to 10 km in size by long axis. They are mainly composed of migmatites of plagiogranitoid composition. Besides the central part of the Dome where these structures are most developed, they are also known in its west and south-west nearby Nelgivka and Partyzany villages, as well as in the north of the Dome. From the point of view mentioned above these migmatite “synclines” also should be considered as eroded second-order domes. The positive structure in Saltychanskiy Dome is preserved only in its south-east comprising Andriivskiy second-order dome composed of migmatitized gneisses and mafic gneisses of Verkhnyotokmatska Sequence. This suggests for lesser erosion degree in this part of the Dome. Indirectly this is also supported by the relatively good preservation of Sorokynskiy greenstone belt only in this part of the Dome’s envelope.

Sub-concentric structure of the Dome is defined by the numerous massifs of Archean and Proterozoic granitoids, mainly of Shevchenkivskiy and Obitochnenskiy complexes. They are similar in composition and tectonic setting and, therefore, it is not excluded that actually part of Shevchenkivskiy Complex belongs to Obitochnenskiy one or its renewed varieties. More older dating of granitods ascribed to Shevchenkivskiy Complex is also possible. The problem can be solved only through further isotopic dating.

In the “Tectonic scheme of crystalline basement” the granitoid massifs are entitled with own names. All these ones are relatively small (up to 85 km2), are elongated along structural elements of the Dome (maximum length – up to 20 km at width of the first kilometres) and in general highlight the sub-concentric structure of the Dome. Normally these massifs are located by periphery of aforementioned eroded second- or higher-order domes, and, certainly, of Saltychanskiy Dome itself. That is, they occur mainly in the inter-dome sites between melanocratic amphibole granite-gneisses, amphibolites, meta-ultramafites etc., or at the boundary of the Dome with the metamorphic envelope. Almost throughout the strike and dip elements of granitoids and the country rocks are similar while the direct contacts are sharp or gradual in places. The typical cutting chill contacts of tonalites with metamorphic country rocks are known only in the least eroded south-eastern part of Saltychanskiy Dome (Osypenkivskiy massif). This tectonic setting and bedding elements of Shevchenkivskiy Complex massifs are characteristic for migmatites of Archean granite-dome regions in general. It is thought that these are resulted from “floating” of so called migmatite diapirs – concentrators of the light most granitized rocks (mainly migmatites of granite composition). Uplift of such diapir and “break-through” essentially mafic metamorphites (as revealed from Zakhidnopryazovska Series rocks) led to the formation of Saltychanskiy Dome. This was the complex multi-phase process which included:

1. Floating up and coalescence of numerous granite diapirs (modern high-order domes). 2. Generation of higher temperature magmas (diorite, granodiorite) in between the domes within

melanocratic and thus relatively competent metamorphites resulted in formation of auto- or allochthonous massif. In relation to migmatites of the floating granite diapers, these massifs could be older, contemporaneous or even later. However, due to the ductile (essentially melted) state of matter in granite diapirs even younger, relatively to them, magmatites of Shevchenkivskiy Complex were not able to form the cutting contact with the rocks of respective migmatites domes. At the same time, compression conditions emerged between the floating diapirs led to the formation in diorites, granodiorites and other rocks of many massifs the distinct oriented gneiss-like structures conformable to the dome boundaries. All these processes occurred at the deep crustal levels. For instance, if we assume close to the sphere shape of Saltychanskiy Dome then at its diameter of 40 km even upper portions of its lower sub-sphere do correspond to the depth 15-20 km at least.

At the height of the upper sub-sphere of Saltychanskiy Dome the Osypenkivskiy massif only probably formed. It is located in the same-named third-order block which is separated from the major Dome part by

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Malynivskiy fault and comprises its south-eastern extension providing general pear-like shape of Saltychanska structure. Tonalites of Osypenkivskiy massif are most homogeneous among the granitoids of this complex: they contain acute xenoliths of metamorphic rocks and form typical chilled contacts with the rocks surrounding this part of the Dome – amphibolites of Olginska Suite; the massif is elongated along this contact. Magmatic structures of all other complexes in the Dome, mainly stock – and dyke-like bodies, are much less in size in comparison to ones described above. The cutting relationships with country rocks are typical for these bodies while these ones in some extent follow structure of the country rocks. The bodies of Andriivskiy massif do fit the sub-concentric structure of the Dome in most extent.

Heterogeneous folded envelope of Saltychanskiy Dome is resulted from the intricate process of the Dome formation. The rocks of six Paleo- and Neo-Archean subdivisions are developed in the numerous structures of this envelope. Of these ones Verkhnyotokmatska Sequence was deposited prior to the beginning of Dome formation. Two others, Kainkulatska and Dragunska sequences, do correspond to the early and late periods of the first (Paleo-Archean) phase of the Dome formation while the metamorphic rocks of Sorokynskiy greenstone belt apparently correspond to the period of Neo-Archean merging of the crust formed in Western and Eastern Pryazovya. Proterozoic stratons (except the minor blocks composed of Sadova Sequence and Dibrovska Suite) are almost not preserved and the rocks of this age include mainly ultra-metamorphites (poly-migmatites) and magmatites.

Lozovatska anticline defined during geological mapping in the scale 1:50 000 [117] is the major structure in the envelope. It surrounds Saltychanskiy Dome from the west and north-west over the distance of more than 70 km being 10 km wide in the south and up to 25 km in the north where it swells and bifurcates through the merging with the envelope of another dome outside the map sheet territory. Thus, the anticline axis changes its strike from north-western in the south to south-eastern in the north. Extensively migmatized granulites of Zakhidnopryazovska Series are folded into the steep, perhaps, isoclinal fold with the limb range from ten meters to first kilometres, and steep (80-85o) dipping mainly to the east and north-east in the eastern limb and to the south-west in the western limb. The dipping direction of the axis plane in these folds often is being changed to the reverse one by strike.

Some higher-order mainly isometric (dome-like) structures (up to first kilometres wide) can be distinguished in Lozovatska anticline. Normally their cores (in the north) are composed of pink granites. Minor (< 1 km) domes are also typical to the west of Zelenivka village, as well as a range of similar structures that are being well mapped by observations in minor quarries on Lozovatka River in between Yuryivka and Kolarivka villages. Their cores are commonly composed of biotite migmatites and in places (on Lozovatka River) – of amphibole agmatites. In the core portions of these structures the rock bedding is more flat than in granulites and varies from 40-45o in the cores to 50-70o in the limbs.

Tectonic setting, structure and composition of Korsak-Mogylskiy high-order block, where Korsak-Mogyla iron-ore deposit is located, requires special consideration. The block is situated between two first-order structures – the eastern flank of Orikhivsko-Pavlogradska zone and the envelope of Saltychanskiy Dome. This minor (5.9 by 2.4 km) block composed of both Demyanivska Suite and Zakhidnopryazovska Series rocks directly adjoins Korsatskiy fault and formally belongs to the south-western limb of Lozovatska anticline. At the same time, in the western envelope of Saltychanskiy Dome this structure looks like “isolated” or the similar iron-ore occurrences are unknown from this site.

The asymmetric brachy-syncline structure of Korsak-Mogyla deposit is revealed from drilling data. The steeply-dipping ferruginous-siliceous rocks in its western and eastern limbs differ in composition and thickness. Increased rock thickness in the eastern limb (2.5-3 times) is caused by the fault-side flexure where epigenetic high-grade ores are located. The ferruginous horizon in the western limb is composed of tectonized coarse-grained massive or gneissose ferruginous quartzites. Tectonites after ferruginous rocks are also developed in the eastern syncline limb. In general, both the Suite column (intercalation of ferruginous rocks with mainly ortho-rocks) and its bedding are similar to those of other iron-ore deposits of Western Pryazovya which comprise the fault-side monoclines to the west of Korsak-Mogyla. By these reasons it should be explained why the rocks of Korsak-Mogylskiy block are ascribed to Demyanivska Suite instead of Dibrovska Suite.

The major differences in composition between Korsak-Mogyla deposit and similar ones of Kuksungurska or Kamyanomogylska groups include granulite metamorphic degree and occurrence of thick batch (180 m) of mesocratic clinopyroxene-hornblende-plagioclase gneisses (retrograde intermediate-mafic granulites typical for Zakhidnopryazovska or Tsentralnopryazovska series) in the supra-ore part of the column. Similar rocks are also widely developed in Manguskiy block of Eastern Pryazovya – the stratotype area of Demyanivska Suite of Mariupolske iron-ore deposit whose column is often being correlated with Korsak-Mogysliy one. However, it cannot be refused that the monotonous retrograde granulite batches known both in the supra- and sub-ore parts of Korsak-Mogyla column may comprise the basement of contrasted Demyanivska Suite (by analogy with Dibrovska Suite in fault-side monoclines in the west of map sheet). These relationships

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are supported by essential difference in the age between Zakhidnopryazovska Series and Demyanivska Suite, and also by apparent allochthonous laying of Korsak-Mogylskiy block over granulites of Lozovatska anticline.

Bilotserkivska syncline replaces Lozovatska anticline in the northern envelope of the Dome. This is also composite structure up to 50 km long and up to 30 km wide extended in latitudinal direction it includes three anticlines – Oleksiivska, Tytovska and Lantsivska. The latter separates Bilotserkivska syncline in two parts – smaller south and greater north ones. The southern limb of first structure at the same time comprises the limb of north-eastern extension of Lozovatska anticline whereas southern syncline is open toward the envelope which is shared with adjacent dome outside the map margins. In other words, formation of the trough where Dragunska Sequence was depositing is caused by uplift of adjacent domes. Perhaps, its formation commenced as far back as initial stages of granitoid domes floating up. It is evidenced by unconformable laying and composition of Dragunska Sequence, particularly, development of high-alumina gneisses (apparently derived from re-deposited weathering crust) in the lower part. In addition, Dragunska Sequence differs from underlaying rocks of Zakhidnopryazovska Series in metamorphic degree which does not exceed amphibolite facies and much less deformation degree. In contrast to the linear folding in Lozovatska anticline, Bilotserkivska syncline and its complicating folds are actually brachy-form structures with fairly moderate for Archean structures in Pryazovya dipping angles which normally do not exceed 50-60o. Of course, these features also require their explanations. It is thought that the rocks of Zakhidnopryazovska Series were transformed into granulites prior to the Dome formation. It is seen that formation of granite-dome associations under the modern models is resulted from the melting of water-saturated oceanic crust (metamorphites of Verkhnyotokmatska Sequence do correspond to this crust) due to the crust sinking into the over-heated mantle. It is therefore clear that in the lower parts of the Dome (which actually were mapped in the studied area), that is, at the depth of 20 km at least beneath the former surface, the remnants of the former oceanic crust should be transformed into granulites and only within granitoids of the Dome itself they were later retrograded under amphibolite facies conditions. In contrast to Verkhnyotokmatska Sequence, metamorphism of Dragunska Sequence had occurred in the final period of granitoid domes floating up, that is, at the phase of their growth and coalescence accompanied by capturing the sequences deposited in the inter-dome troughs. Obviously, these conditions were relatively shallow-deep but they also did correspond to the level of amphibolite-facies ultra-metamorphism and metamorphism as it is evidenced by mineral assemblages in Dragunska Sequence.

Sorokynska tectonic zone or the same-named greenstone belt [17, 18] surrounds Saltychanskiy Dome from the east. It is mainly composed of Archean rocks of Osypenkivska Series which unconformably (with clastic sediments at the base) lie over granulites of Zakhidnopryazovska Series. And in spite of Osypenkivska Suite does not have direct contacts with Dragunska Sequence, it is considered to be younger in view of the known regional tectonic relationships. It should be noted that Sorokynska zone not only surrounds Saltychanskiy Dome by periphery but, likewise typical greenstone belts of Middle Dniprean region, it also fills up the space between the second-order domes in the south-eastern periphery of Saltychanskiy Dome. It is Osypenkivskiy Dome in the east and Andriivskiy dome further to the west. The diagonal (in relation to the strike of major structure) inter-dome extensions are large enough. In the western envelope of Osypenkivskiy Dome, in between Osypenko and Novotroitske villages, the length of such longitudinal branch is 7 km. Thus, these relationships strongly contradict to the definition of Sorokynska structure as tectonic zone. And if one take into account also the age of Osypenkivska Series, typical mafic-ultramafic rocks at the column base and relatively low metamorphic grade (epidote-amphibolite facies predominates), these data coupled with tectonic conformity with granite domes, stressed above, would explain why Sorokynska structure is currently classified as greenstone belt similar to Gaychurskiy belt in the map sheet adjacent from the north, as well as similar greenstone structures in the Middle-Dniprean geo-block.

Sorokynskiy greenstone belt is fairly well studied in the exposed sites mainly on the coast of Berdyanske water reservoir, as well as in other sites by numerous boreholes drilled in different years in the course of prospecting for various mineral occurrences (gold, lithium, iron, copper, asbestos etc.) located in the Belt. As one can see in the map, the belt comprises narrow (up to 1 km wide) band of metamorphites which are directly or through the minor country rock blocks are bounded by sub-parallel faults. The general extension of the Belt is north-western (300-330o). Sub-latitudinal section of the Belt is observed in the area of Osypenkivskiy Dome northern envelope. Here the Belt width is greatest – 2-2.5 km.

Plicative structures of the Belt are relatively simple and in general they are well expressed in the anomalous gravity and magnetic fields due to the rocks properties in the column lower part. By geophysical and numerous drill-hole data, over the most its length the Belt comprises undulating tight (keel-like) linear syncline overturned mainly to the north-east. Rock dipping is steep (65-90o) and only south-western and southern. Besides more than 1.2 km thick Archean metamorphites of Osypenkivska Series, in the southern part of the Belt (Sadova site) by drilling the meta-clastic rocks, marbles, diopsidites, muscovite-biotite quartzites, graphite-bearing schists and other rocks of Proterozoic Sadova Sequence are encountered that stacks up Archean column.

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The mode of their development comprises the tectonic plate up to 9 km long. The normal thickness of Sadova Sequence is up to 400 m.

Besides aforementioned rocks, in the Belt or just nearby in the country rocks Proterozoic granites and rare-metallic pegmatites are also known. Thick cutting bodies of the latter are observed in the widest sub-latitudinal part of the Belt where among the host rocks ultramafites predominate. It is assumed [18] that these rocks were emplaced into this site from other parts of the Belt in Proterozoic due to ductile properties of serpentinites and their squeezing facilitated formation of the hollows subsequently sealed with pegmatite melts.

Analysis of the rock metamorphism also contributes to the ideas on the Belt structure although metamorphic degree of Archean and Proterozoic rocks in the southern part of the Belt is almost the same. However, over entire Belt in the direction from south-east to north-west increasing of metamorphism from epidote-amphibolite to amphibolite facies is observed. The latter facies is developed nearby the northern pinch of the Belt. Further by strike of the Belt, in the northern envelope of second-order Andriivskiy Dome, metamorphic modifications attain the granulite degree (skialites in granites). In the same direction the rock column of the Belt is getting simpler. Particularly, there is no Sadova Sequence to the north of Sadova site. Further to the north-west thickness of Krutobalkivska Suite decreases and to the north of the widest Belt section the rocks of Olginska Suite predominate in the column. These observations confirm ideas pointed above with regard to increasing of erosion degree in Saltychanskiy Dome and its Archean envelope from south to the north.

Berestovska syncline comprises the envelope fragment of the Manguskiy Oval adjacent to the Saltychanskiy Dome and located in the neighbouring (from the east) map sheet. This syncline, like above Bilotserkivska and Sorokynska structures, was forming over the late stage of the durable period of granite-dome tectonics onto already developed crust of Pryazovskiy geo-block. However, in contrast to mentioned structures, Berestovska syncline was formed later and probably it corresponds to the time of partial destruction of the crust. It is evidenced from:

1. Discontinuous, with two-straton interruption, laying of Temryutska Suite over Kainkulatska Sequence of Zakhidnopryazovska Series.

2. Wide development of quartzites and high-alumina gneisses in Temryutska Suite – probable metamorphosed rocks of re-deposited weathering crust of that time.

3. The crustal “weakness point” inheritance by the depositing trough of Temryutska Suite – inter-dome boundaries caused the characteristic crescent shape. Specifically, in the south Berestovska syncline adjoins with the envelope of Saltychanskiy Dome and Manguskiy Oval and almost merges Sorokynskiy Belt, and in the north it likely drives a wedge between Bilotserkivska syncline and Manguskiy Oval.

4. Apparent link of primary depositing trough with con-sedimentation faults. This is indirectly confirmed by the wide development of mafic granulites (former basaltoids) in Temryutska Suite.

Berestovska syncline is almost triangular in the plane, irregularly compressed structure, bounded by the faults. Disharmonic folding is characteristic for its widest part and is most expressed in the western limb through the ductile rocks of the lower carbonate-graphite batch (see “Structure of carbonate and graphite-bearing horizons” in the map). Probably, this is resulted from divergence of country rock contours in the west and east. Perhaps, by these reasons in the north and south of syncline, where country rock contours are sub-parallel, the syncline itself is narrow (first kilometres) with linear folding. In the centre it is 5-6 times wider due to ductile squeezing of the rocks from the narrow parts of structure. This is why the disharmonic folding in non-competent rocks is developed in this place.

Erosion degree of Berestovska structure composed of granulites is much greater than in the adjacent Sorokynska and Bilotserkivska ones. It is in agreement with ideas on the uplift of Eastern Pryazovya blocks relatively to the Western Pryazovya ones by the fault system of so called Tsentralnopryazovska zone which includes the faults that bound Berestovska syncline from the west. Complexity of Berestovska syncline is caused by numerous high-order structures of which granite-dome ones composed of Archean (Shevchenkivskiy Complex) and Proterozoic granitoids are being best mapped. By these reasons the rock dipping varies in a wide range – 40-90o. The high-order synclines are also known; of these ones structure composed mainly of marbles of lower carbonate-graphite batch in the eastern limb of Berestovska syncline is most studied. These rocks are well-exposed in Glyboka gully nearby Kalaytanivka village.

Orikhivsko-Pavlogradska suture zone (OPSZ or the same-named band) in the map sheet area is represented by its large eastern fragment. In the east it is bounded by Korsatskiy Fault, and in the west and south it extends outside the map sheet. By internal structure this part of suture zone is transitional from sub-longitudinally oriented tight folds of metamorphites or their fragments and a range of lensed essentially granitoid high-order blocks of Orikhivsko-Pavlogradska band to the typical sub-concentric granite-dome structure of Pryazovskiy geo-block itself.

It was assumed by Academician M.P.Semenenko as far back as 40th of the last century that this unit belongs to the structure of Orikhivsko-Pavlogradska band. Further on this territory was extensively studied in

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relation to the exploration of numerous iron-ore deposits, geological mapping in the scale 1:50 000 and scientific researches. However, up to now their internal structure is quite disputable. Most often the eastern flank of OPSZ is being qualified as Korsatskiy synclinorium [43]. The fragment under present discussion comprises its eastern part. The western limb of this synclinorium (Kamyanomogylska strip of ferruginous quartzites and associated rocks) is located outside the map sheet. In the structure design of OPSZ eastern fragment the statements of two alternative concepts were used. The laying of Dibrovska Suite metamorphites over Archean basement (granulites of Kainkulatska Suite migmatized and granitized prior to deposition of Dibrovska Suite) does match the first concept [19]. From the second one [43] the statement is taken on difference between the productive sequences in Kuksungurske deposit (and Kamyanomogylska strip as well) included into Dibrovska Suite and productive sequences in Korsak-Mogyla deposit. The metamorphic rocks of the latter are ascribed to Demyanivska Suite and their tectonic setting is reviewed above in the envelope structure of Saltychanskiy Dome. Thus, the following data are taken into account in structure design of OPSZ eastern fragment:

1. The major rock set in the zone includes migmatites with remnants of amphibolites, often pyroxene-bearing, or (in the eastern part) mafic granulites; this set comprises migmatized and granitized granulites of Kainkulatska Sequence.

2. By drilling and geophysical data, the metamorphic rocks united in Dibrovska Suite, do form the single variously-oriented strips within aforementioned migmatized rocks: sub-longitudinal and latitudinal up to 10 km long and up to 2 km wide, which meet one another under the angle close to normal. In the west of studied map sheet (nearby Petrivka village) this is Kuksungurskiy “wedge” that corresponds to the same-named iron-ore deposit. In the south, at Inzivka and Orlivka villages, similar latitudinal strips are studied which join Kamyanomogylska strip outside the map sheet limits.

3. Interpretation of Dibrovska Suite relationships with the migmatized rocks supports an idea on its laying over already granitized Kainkulatskiy basement. It is evidenced by: a) relatively slight granitization of Dibrovska Suite rocks expressed mainly along the contacts with the “country rocks”; b) wide development of quartzites and high-alumina gneisses – the indicator of interruptions in formation of tectonic floors in the zone; c) difference in metamorphic degree between the basement and Dibrovska Suite: the first one contains granulite skialites whereas the second is metamorphosed under amphibolite or epidote-amphibolite conditions; in addition, the tectonites often occur along the contacts of the strips.

Thus, from the above discussion it can be concluded that aforementioned metamorphic strips should be classified as the fault-side monoclines in places complicated by the high-order flexure folds. Kuksungurske iron-ore deposit comprises the typical and best studied representative of these structures. Its southern latitudinal strip tectonically pinches out over the first kilometers outside the map sheet margins, and its sub-longitudinal strip (based on detailed maps of anomalous magnetic field) in the north meets Kamyanomogylska strip and in the south with some interruptions is traced by relatively slight anomalies toward Orlivska strip [19]. Just the minor part of these strips are well-studied, particularly, their direct junction in the radius of almost 4 km. The latitudinal section comprises the monocline plunging to the north. Productive ferruginous quartzite sequences and other rocks are gripped between migmatites and the contacts with the latter commonly are tectonic. Thickness and composition of metamorphic rocks are quite variable by strike. Sub-ore portion of the Suite here is almost not preserved and ferruginous quartzites are tectonized.

The longitudinal monocline of Kuksungurske deposit is steeply inclined to the west and is also extensively tectonized. Its junction with the latitudinal strip is observed along the thick (tens of meters) milonite suture.

Tectonic and metasomatic transformations in the strips were multi-phase and had various magnitudes – from injection migmatites and agmatites and widespread microclinization to muscovitization, epidotization etc. Transformations of the ferruginous rocks are characteristic: besides various tectonites after these rocks there are also encountered the microcline granites contaminated by ferruginous rocks that contain up to 10-20% of magnetite, and in the southern strip the epigenetic chlorite-epidote-magnetite ores are also described.

Fault structures Almost all first-order faults shown in the “Tectonic scheme of crystalline basement” coincide with the

contours of the same-ranked to them tectonic elements described above, for instance, the limits of major second-order blocks – Orikhivsko-Pavlogradska suture zone, Western Pryazovya and Eastern Pryazovya, or the limits of relatively minor structure – Sorokynskiy greenstone belt. Therefore, formation depth of these faults at some development stages may correspond to the forming conditions of major tectonic elements in the map sheet, that is, to the depth of mid crust at least for respective time. This statement often is supported by ductile dislocations of migmatites and igneous bodies located in the fault zones. However, the fault zones were developing over long

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time – up to recent and by these reasons the age- and depth-different tectonites (most often brittle dislocation products) are concentrated in the fault zones.

Let us consider first of all the faults responsible for Pryazovskiy mega-block division into the second-order blocks. These include Korsatskiy Fault and the faults of so called Tsentralnopryazovska zone – Mykolaivskiy and Katerynivskiy.

Korsatskiy Fault of north-western and sub-longitudinal extension is traced from the Azov Sea coast up to the northern limit of the studied map sheet and further outside it joins Zakhidnopryazovskiy Fault. The latter one, in general opinion, comprises the eastern margin of Orikhivsko-Pavlogradska strip while the wedge-shaped block in between Zakhidnopryazovskiy and Korsatskiy faults, as it was pointed above, does correspond to the transitional zone from Orikhivsko-Pavlogradska band to the structures of Pryazovskiy mega-block itself. Thus, in the map sheet area Korsatskiy Fault separates the mentioned zone from the southern (Saltychanskiy) block of the western Pryazovskiy mega-block. It comprises tectonic boundary of the major structure in the envelope of Saltychanskiy Dome – Lozovatska anticline – and due to differences in composition of adjoining rock complexes (retrograde granulites in Lozovatska anticline and migmatite complex in the eastern fragment of Orikhivsko-Pavlogradska zone) the fault is well-expressed in geophysical fields. The Fault initiation time apparently is Archean since the Fault corresponds to the boundary of enveloped Saltychanskiy Dome with the similar dome in the west of Pryazovskiy mega-block, and the major rock set in the eastern fragment of Orikhivsko-Pavlogradska zone is the same – the rocks of Zakhidnopryazovska Series re-worked under ultra-metamorphism. However, major tectonic motions here took place in Proterozoic. It is evidenced by the fault-wall transformations in monoclines composed of Dibrovska Suite and by the age of Orikhivsko-Pavlogradska zone. Later processes in the fault zone at some places are marked by low-temperature metasomatites (albitites for instance) and typical brittle deformations. The latter are known from exposed thick (up to 50 m) crushed rocks on Tokmak River nearby Kainkulak River mouth and other places. The southern part of the Fault is commonly known as Berdyanskiy normal fault.

Katerynivskiy and Mykolaivskiy faults in the east of map sheet comprise the western tectonic margin of superimposed Berestovska syncline and their primary nature apparently is con-sedimentation and their initiation time is obviously Neo-Archean. These faults meet and cross one another at the right angle following weakened inter-dome boundaries.

Katerynivskiy Fault is best expressed in the north-east of the map sheet over the distance of about 35 km. Actually this is 2-4 km wide tectonic zone where the rocks are extensively cataclased and silicified. In the distinct metasomatites of the zone – feldspar quartzites – the gold signs are permanently observed. Proterozoic period of the Fault development is marked by its intersection with the south-western extension of the internal sub-zone of Orikhivsko-Pavlogradska zone and by rare-metal pegmatites (Mogyla Visla) located in the east of map sheet and Kamyanomogylskiy Complex apogranite massifs (in the map sheet adjacent from the east).

Mykolaivskiy Fault is being sub-parallel to the faults of Sorokynskiy greenstone belt and almost coincides with these faults (it is traced in 3.5-8 km to the north-east). This probably suggests for unique weakness inheritance of this particular inter-dome section where inter-block destruction and Western and Eastern Pryazovya block junction periodically occurred. The Fault is well-expressed in magnetic field and in outcrops it is reliably traced by numerous tectonite zones in Berda River valley – nearby Mykolaivka village, to the south of Tytove village and other places.

The most first-order faults in the map sheet are located in around Saltychanskiy Dome forming semi-regular hexahedron appeared probably due to the Dome floating up in Archean. From the west to east clockwise these are Chernigivsko-Vyacheslavskiy, Stulnivskiy, faults of Sorokynskiy greenstone belt, Malynivskiy and Berdyanskiy faults. In the south-east of the hexahedron, outside its boundaries, Saltychanskiy Dome is complicated by Osypenkivskiy block which is least eroded as it was pointed above. The block is elongated along the southern edge of Sorokynskiy belt and is bounded by Berdyanskiy and Elizavetivskiy faults in addition. All mentioned faults are well-expressed in magnetic and gravity fields and actively evolved later. For instance, in the north of the Dome Stulnivskiy Fault had split Chernigivskiy carbonatite massif in two blocks. Often the faults contain thick bodies of Paleo-Proterozoic pegmatites (Sorokynska fault zone), Neo-Proterozoic rocks of Dyke Complex (Stulnivskiy and Elizavetivskiy faults), and Chernigivskiy and Berdyanskiy faults at some their sections are known as Meso-Cenozoic normal faults.

Later than the faults in the Dome envelope, perhaps in Proterozoic, the cutting faults were set up. Of these ones Elizavetivskiy Fault is the largest. In diagonal direction (from south-east to north-west) it crosses Saltychanskiy block and controls Proterozoic dykes of diabases, feldspar hornblendites and lamprophyres. In view of the fact that Berdyanskiy normal fault is displaced along Elizavetivskiy Fault in the south of map sheet, the latter was actively developing in Meso-Cenozoic.

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The faults that control deposits and numerous mineral occurrences are of particular interest. First of all, these are so called con-sedimentation faults or fault zones, as well as the breaks directly or indirectly accompanied by exotic igneous rocks – carbonatites, kimberlites etc.

The oldest (initiated in Archean) in this group are the faults that bound Sorokynskiy greenstone belt and belong to the fault system which surrounds Saltychanskiy Dome.

From the paleo-tectonic point of view, these faults apparently correspond to the margins of the basin with oceanic-type crust (Olginska Suite) and the continental crust of that time. It is not clear yet whether the basin was residual or the rifting one. The latter assumption is argued by meta-clastic rock occurrence in the lower part of Olginska Suite. But the mapped faults in Sorokynska zone and numerous associated mineral occurrences were formed later in Neo-Archean, over the basin closure, or even during Proterozoic activization. It is thought that subducted oceanic crust of this basin provided the major source for the ore concentrations. Just the oceanic crust is characterized by increased Clarks of many ore components (including gold) that were extracted from the buried crust and transported into the newly-formed greenstone belt. Later on, the fault zone actively evolved in Proterozoic as it is evidenced by deposition and metamorphism of Sadova Sequence, as well as by emplacement of numerous rare-metal pegmatite veins. Most of the faults at this development stage of Sorokynskiy belt are classified as up-throw strike-slips [17, 18].

Con-sedimentation nature of Katerynivska fault zone and Mykolaivskiy Fault is already discussed above. Besides numerous mineral occurrences the epigenetic graphite deposits are confined to these faults.

The elements of sub-concentric faults in the north-western envelope of Saltychanskiy Dome were followed by Proterozoic igneous rocks of Chernigivskiy carbonatite complex which form the elongated (up to 30 km) arch structure. In its northern part the apatite deposit is known, and in its southern extension – numerous bodies of Kolarivskiy Complex diamond-bearing rocks.

The north-western fault direction both in Saltychanskiy block and other areas is thought to be perspective for diamond-bearing rocks prospecting. This statement is based, for instance, on the fact that lamproite diamond-bearing pipes are encountered along the southern section of Chernigivsko-Vyacheslavskiy fault and to the west (nearby Zelenivka village) and to the east (Kolarivka village area) of this fault. Lamproite-like rocks are known in the faults of the same direction: on the northern extension of Mykolaivskiy Fault outside the map sheet, and to the south of Kuybyshevskiy fault.

Besides described faults, in the studied area are also widely developed the higher-order breaks that are being traced over first kilometers. They are mainly arranged in en echelon manner within one of the fault systems: longitudinal, latitudinal or diagonal. The latter system faults are best expressed in the landscape.

Upper tectonic level The upper tectonic level (platform cover) overlies crystalline basement with clear angular and

stratigraphic unconformity. Characteristic features include relatively simple column structure with horizontal or very flat rock bedding. At the same time, tectonic patterns of Jurassic, Cretaceous-Paleogene and Neogene sediments separated by stratigraphic discontinuities are somewhat different reflecting various tectonic regimes over Jurassic, Cretaceous-Paleogene and Neogene periods.

Respectively, Jurassic, Cretaceous-Paleogene and Neogene tectonic floors are distinguished. Jurassic tectonic floor is developed only in the north-western part of the map sheet where it constitutes

the oval fault-side Novomykhaylivska Depression elongated in sub-latitudinal direction. Its length is about 13.5 km, maximum width – up to 6 km. The deepest portion (800-100 m) is located in the south of mentioned area, close to the fault [61]. To the north structure is gradually getting flatter. In the north-western part of the map sheet Jurassic sediments apparently used to be more developed. But the Late Cimmerian phase of Alpine orogenesis had caused the territory uplift and erosion of Jurassic sediments. They are preserved in Novomykhaylivska Depression only.

Cretaceous-Paleogene tectonic floor in the north-western and southern parts of the studied territory fills up the dimples in crystalline basement and does form the negative structures evolved in the course of sedimentation, that is, con-sedimentation structures. Their size varies from some to first tens of square kilometers.

In the north-western part of the territory these negative structures often are tongue-shaped, and in the southern part they are mainly elongated in sub-longitudinal direction. The rock dipping angles in the limbs of these structures attain 1-2o. In their distribution some link with Precambrian sub-longitudinal faults (Korsatskiy, Chernigivskiy etc.) is observed affirming the block structure of crystalline basement.

Stulnivska Depression is located to the south of the same-named fault (Vladivka, Stepove, Mokriy Stav villages). Depression width from the north to south is up to 8 km, the length – up to 10 km. Maximum depth is 90-100 m. It is filled with Cretaceous and Paleogene sediments.

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Chernigivska Depression is located to the west from the same-named normal fault and is elongated in longitudinal direction up to 14 km. Depression width attains 8 km, maximum depth – 100 m. The basement surface is irregular, stair-like. Depression is composed of Cretaceous and Paleogene sediments.

In the southern part of the map sheet the sediments of Cretaceous-Paleogene tectonic floor comprise the slope of Prychornomorska Depression with gentle dipping to the south. This plunging (by series of sub-latitudinal faults parallel to Berdyansliy normal fault) is better expressed on the crystalline basement surface and is much less prominent in the overlaying Neogene sediments. The monocline is complicated by various higher-order structure forms, various in morphology and genesis, of which the local depressions (Obitochnenskiy and Berdyanskiy grabens) and breaks are widespread. The monocline plunges to the south under the angles 1-3o. The northern edges are bounded by normal faults.

Berdyanskiy Graben is located in the south-east of the map sheet in the area of Berdyanska sandbank. Here crystalline basement is buried to the depth from 50 m in the north to 900 m in the south. The Graben size is 22 km in the direction from the north to south, and 28 km – from west to east. Structure is filled with Cretaceous and Paleogene sediments.

Obitochnenskiy Graben is located in the south-west of the map sheet (Obitochnenska sandbank). The Graben dimensions: 12 km from north to south and 9 km – from west to east, maximum depth – 300-400 m. Basement surface is irregular, stair-like. This structure also is composed of Cretaceous and Paleogene sediments.

Neogene tectonic floor in the studied territory lies almost horizontally: in Chernigivsko-Berestovska LTZ – as single enclaves with maximum thickness of sediments up to 50 m; in the northern edge of Prychornomorska Depression (southern slope of Ukrainian Shield) – as the broad band along the Azov Sea coast where its thickness gradually increases southward up to 150 m.

Besides the mentioned regional plicative dislocations, the fragments of the fault dislocations, which often coincide with the regional faults in crystalline basement, are identified in the Cretaceous, Paleogene and Neogene sedimentary piles by the complex of methods. Apparently these features are related to the ancient fault renewal in Cenozoic. It is exemplified by the fault fragments that often coincide with the zone of Korsatskiy regional fault – Chernigivskiy, Stulnivskiy, Berdyanskiy branches and other local faults.

Quaternary sediments are also transected by neo-tectonic faults. Close to the western map sheet margin the fault is observed along the gully in the right slope of Yushanly River valley. This is normal fault of north-eastern extension. Vertical displacement by the fault attains 11.6 m. Another fault is found in the north-east of the territory along the bottom of Gruzenka gully. The fault strike is north-north-eastern. The fault in Blagovishchetsi village (close to the northern margin of the map sheet) is extended in sub-longitudinal direction. In the topographic map this fault is expressed in the erosion ledge. Two north-east-trending 6 km and 12 km long faults are encountered in the south-eastern part of the map sheet. The dimple in the modern relief is confined to one of these faults (1.4 km to the west of Rozy village). And the active land-slide is confined to another fault on the right bank of Berda River valley. The faults obviously are of Holocene age.

Study of neo-tectonic motions in the map sheet territory suggests for the modern vertical block movements along the bounding Precambrian faults of sub-latitudinal direction (Stulnivskiy, Elizavetivskiy, Berdyanskiy).

Zakhidnopryazovskiy ledge of crystalline basement displays the uplift trend. The magnitude of positive motions decreases from the north to south. The far northern block that

includes Bilotserkivska syncline is involved in the greatest uplift and the far southern block at the boundary with Prychornomorska Depression is being uplifted in the least extent. As a result, erosion basis is being changed leading to the formation of a range of erosion-accumulation terraces.

The northern edge of Prychornomorska Depression in Neogene-Quaternary time undergoes some motions with general subsidence. These motions are accompanied by Neogene sea transgressions and regressions with respective deposition of age-different sediments which overlie one another with stratigraphic discontinuity.

Since Upper Neo-Pleistocene commenced the slow subsidence of the northern edge of Prychornomorska Depression at the speed about 1 mm per year, and accumulation of thick (up to 20-49 m) alluvial sediments. The sea transgression essentially contributes to the formation of morphology in the southern part of the territory.

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6. HISTORY OF GEOLOGICAL DEVELOPMENT The history of geological development for the region of Ukrainian Shield and Prychornomorska

Depression can be restored in the general outlines. In the earth crust formation of the region which includes the studied territory the four stages can be

distinguished that essentially differ one another by the crust formation “mode” and duration. These include Archean, Proterozoic, Paleozoic and Meso-Cenozoic stages.

Two first stages encompass considerable part of the time – from ~3.5 to ~2.0 Ga. Over this period the continental crust was mainly formed and, after some authors [32, 46], laterally merged into Sarmatia meso-continent; the basement of Ukrainian Shield comprises only small part of the latter. Sarmatia was just one of three meso-continents which later (prior to 1.86-1.87 Ga) had merged into the single Eastern-European Craton [46]. Ukrainian Shield comprises the relatively young structure of this Craton and it was detached out from the Craton in the beginning of the plate development stage (in Riphean) when the continent was split through the formation of aulacogenes. The reliable evidences for this development period are not found in the studied map sheet. Probably some dykes of respective age correspond to this period.

In Paleozoic the eastern part of Ukrainian Shield, particularly, Pryazovskiy mega-block, was the internal massif between Herzinian structures of Donbas and modern basement of Scythian Plate. Over that time the crust of Pryazovskiy mega-block was mainly eroding and comprised the source region for thick clastic sequences in the mentioned structures although the Permian-Carboniferous igneous occurrences (sounds of events in Herzinian fold belts that bound mega-block) are known in the maps sheet territory.

In Mesozoic-Cenozoic over the map sheet territory, besides the denudation, the deposition of thin sedimentary cover in marine and continental environments also occurred. Interchange of these environments, that is, sea transgressions and regressions, coincide with the events in the Tethys mobile belt.

In the Quaternary time, despite of location the map sheet territory outside the continental glaciation, the climate changes related to the alternating glaciation and inter-glaciation periods provided the major factors affecting sedimentation.

Archean stage Paleo-Archean metamorphites of Zakhidnopryazovska Series comprise the oldest stratified rocks in the

map sheet. The rock lithologies, especially in the lower part of the column and even in case of superimposed ultra-metamorphism, are being agreeable correlated with the oceanic crust. Specifically, the Series includes two-pyroxene-plagioclase mafic granulites, or amphibolites after these rocks, which are similar to the modern oceanic tholeittes by chemical composition. The correspondence in composition between the mentioned rocks, of which Archean ones are more iron-enriched, was emphasized by many authors [43]. Comparability of Zakhidnopryazovska Series granulites with oceanic crust is in agreement with occurrence of meta-sedimentary rocks – ferruginous quartzites, biotite-garnet gneisses, calcareous-siliceous schists etc., that probably represent the first layer of the ancient oceanic crust. Development of the felsic and intermediate rocks in the same sections is explained either by superimposed ultra-metamorphic processes or by occurrence in Zakhidnopryazovska Series the rocks that belong to other (post-oceanic) stages of crustal development.

The above arguments indicate that the key point in the accepted concept for the geological development of the region comprises an assumption on the primary oceanic crust whose further transformations resulted in formation of continental crust. This approach to the model of continental crust formation is used for a long time and is analyzed in many works of K.Condie, S.R.Taylor, C.M.MacLennan, V.E.Khain and others. From petrologic and calculation results [37] it is also thought that parameters of Archean oceanic crust (low thickness, short time and thus the density) essentially differ from the parameters of the later crust of the same-type, even Proterozoic one. By these reasons, in contrast to the later periods, in Archean the oceanic crust had been transforming into the continental one not in the subduction geodynamic environments but in relatively shallow-depth (50-60 km) submergence zones. It is concluded [37] that these zones were resulted from Archean crust thin plates “accretion and splitting” with subsequent their subsidence into the over-heated mantle above its downward convective flows. In this way the water-saturated basalts of oceanic crust had been being melted, fractionated but did not derive the intermediate melts, which are typical for Phanerozoic or modern arcs, and did produce the lighter plagiogranitoids instead. The latter were floating up through the accreted oceanic plates and formed the domes. The sketch for plagiogranitoid domes formation is presented above in the section “Tectonics”. And here it should be emphasized that according to the accepted model neither in the dome envelope nor, furthermore, in the dome itself one can expect any the normal stratigraphic section of the ancient

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oceanic crust and, therefore, the section of Zakhidnopryazovska Series as well. This is because in the course of accretion and submergence the thin plates of oceanic crust were repeatedly intercalated tectonically, stacked and partially eliminated. Probably, by these reasons neither rock succession nor thickness of Zakhidnopryazovska Series does correspond to the actual parameters of the ancient oceanic crust. More or less reliable stratification of Archean sequences is probably possible starting from the stratigraphic level of Dragunska Sequence which was depositing over granite-dome basement.

From the actualistic positions described environments of continental crust formation can be principally compared with the island arc environments only since in both cases the continental crust is formed through the transformation of oceanic crust. However, since the Archean arcs differ from the later ones in geodynamics and composition it seems to be better define them as primitive or proto-island arcs.

Certainly, in the modern erosion section of these arcs the upper volcanic floor is absent. It is eroded and in the map sheet just the proto-arc deep level is mapped composed of mainly ultra-metamorphic and igneous rocks. In view of isotopic age of the proto-arc rocks it was forming over 0.7 Ga at least. It was the complex and probably not only constructive process. For instance, in Neo-Archean, roughly at the boundary between Archean blocks of Western and Eastern Pryazovya, the rifting basins were initiated that correspond to the modern Sorokynskiy greenstone belt and Berestovska syncline. Most extensive opening is observed in Sorokynskiy belt. Olginska Suite at the column base, besides the typical ophiolites of komatiite-tholeiite composition also includes meta-clastic horizons. This suggests first of all for the Suite formation over already established continental crust, and, secondly, for the extension of rifting process in the basin up to the oceanic-type crust formation. In Berestovska syncline ophiolites are not found but here the meta-basaltoids (mafic granulites) of Temryukska Suite do mark fairly extensive extension processes, probably within so called disseminated rifting. Closure of rifting troughs, folding and emplacement of Shevchenkivskiy Complex granitoids do mark the final merging of the blocks of Archean proto-arc and Pryazovskiy mega-block. This event is dated by the age of Shevchenkivskiy Complex granitoids – 2.7-2.8 Ga. However, it looks likely that not only these granitoids comprise the proto-arc stage granite formation in the map sheet territory. Perhaps, the older granitoids are not identified yet. Among the Neo-Archean stratified rocks the “witnesses” – coarse-clastic rocks of molassoid type – of the final phases of proto-arc blocks merging are not preserved. Probably, the thick (up to 0.5 km) meta-terrigenous rocks of Krutobalkinska Suite correspond to the initial period of this process.

Of course, both the map sheet territory and entire Pryazovskiy mega-block comprise only the fragments of the Archean proto-arc. According to [17, 45] this arc was extended far to the north (in the modern coordinates) and included the eastern part of Voronezhskiy crystalline massif within so called Kursko-Pryazovskiy micro-continent.

Proterozoic stage Proterozoic rocks contribute to almost all major tectonic units in the map sheet L-37-VII but are locally

developed and respectively shown in the geological map of crystalline basement. The total square of these rocks does not exceed 5% of the territory although it is not excluded that the role of ultra-metamorphic transformation of this particular stage for the map sheet geology is underestimated yet. Occurrence of Proterozoic material is especially probable in the migmatite (poly-migmatite) complexes. In these units the superimposed Proterozoic processes are confidently identified only by development of potassium feldspars since Archean potassium granites are not known either in the map sheet area or the mega-block as a whole.

The data available demonstrate that both studied area and entire Pryazovskiy mega-block were extensively eroded over the post-Proterozoic times. It was already emphasized in tectonic review of Saltychanskiy Dome and Sorokynskiy greenstone belt; in the latter case only narrow (deep) keel-shaped folds are preserved in comparison with the similar structures in the adjacent Middle Dniprean region [17, 18].

The high degree of crystalline basement erosion in the map sheet is also confidently argued by composition and structure of Proterozoic massifs of Chernigivskiy carbonatite complex. In contrast to the most of similar and associated rock units, the massifs are elongated and, therefore, it is thought [14] that the upper ring portion of the central type is eroded. Leaving behind for a while the mineralogical details of carbonatite complex, it should be noted that by these data it is defined to be the deepest of the alkaline rock massifs in the Ukrainian Shield and by mineralogical barometry its erosion degree attains 20 km [14, 28].

It is the common feature that stratified Proterozoic rocks are known only in the west and east of the map sheet whereas igneous rocks (except vein granites and migmatites) are mapped only to the east of Korsatskiy Fault. Furthermore, the igneous rocks of intermediate composition (Obitochnenskiy Complex) are encountered mainly in the central part of the map sheet, within Saltychanskiy Dome.

There are certain regularities in the distribution of metamorphic rocks as well. In the west they constitute the fault-side monoclines (Dibrovska Suite) which are tectonically interlaced with migmatized rocks

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of Archean “country rocks” and probably by these reasons are preserved from erosion. In the east Paleo-Proterozoic rocks of Sadova Sequence stack up the column of Sorokynskiy greenstone belt. Occurrence of Proterozoic rocks within granulites of Berestovska Syncline is also not excluded since similar units in Manguskiy Oval (directly to the east of the map sheet margin) display the concordant values of Proterozoic age on zircons from mafic granulites and charnockitoids [41]. It therefore can be concluded that the zone of rifting troughs between the Western and Eastern Pryazovya blocks that had been being initiated in Archean was continuing to develop in Proterozoic and by these reasons Proterozoic granulites are preserved in these sites despite of the deep erosion.

Obviously, the data presented are not sufficient enough to develop the integrated model of Proterozoic crustal history in the region. However, it is important to note that the data available are in agreement with the models designed on the ground of information from Pryazovskiy mega-block as a whole [22]. By these models, the proto-arc (Kursko-Pryazovskiy micro-continent) originated in Archean was then evolving in Proterozoic in geodynamic environments of the active continental margin and the collision ones. In the definition of these environments the following key points and data were taken into consideration:

1) Contrasted Proterozoic environments in two adjacent mega-blocks – Middle Dniprean and Pryazovskiy of which the crust of the former mega-block, in contrast to the latter one, did not undergo considerable transformation in Proterozoic.

2) Encountering in Pryazovskiy mega-block the lateral zonation of Proterozoic magmatism (mainly in Obitochnenskiy, Khlibodarivskiy and Anadolskiy complexes) which is typomorphic for the active continental margins. It comprises the gradual eastward increasing of the igneous rock alkalinity (from diorites-granodiorites to sub-alkaline potassium granites and quartz syenites) and decreasing in the same direction the zircon isotopic age in the rocks of these complexes over the interval ~2.4-2.1 Ga at least. This is the kind of zonation which is quite similar to the typical one [23] and which defines the direction of oceanic lithosphere subduction in the inter-mega-block basin from the west to east (in the modern coordinates).

3) Occurrence of suture zone – Orikhivsko-Pavlogradska strip – in between the Middle Dniprean and Pryazovskiy mega-blocks which is classified as the zone of micro-continent collision.

From the above positions the history of geological development in the region is thought to be as follows:

1) The basin with oceanic-type crust existed in Proterozoic between the mega-blocks; the basin was continuously closing due to oceanic lithosphere submerging beneath Pryazovskiy mega-block. As a result of this process the active continental margin was formed. It is preserved in the central part of the map sheet and comprises the zone of carbonate-alkaline magmatism (Obitochnenskiy Complex) of the former volcano-plutonic belt.

2) The basin closure was completed by collision of mega-blocks. In this period the eastern flank of Orikhivsko-Pavlogradska suture zone, adjacent to the frontal portion of Pryazovskiy mega-block, had underwent significant tectonic transformations. For instance, the primary sub-concentric granite-dome structure in the internal part of the mega-block was breaking that time (likewise before during convergence). Instead, in the upper part of the crust the stacking of Archean basement plates ovethrusted one another had occurred, and the sediments of the ancient continental terrace of micro-continent (Dibrovska Suite), as well as probably the relicts of the oldest Archean oceanic crust obducted through the micro-continent convergence, were buried between the stacked plates [16, 19]. Amagmatic patterns of this frontal zone of the mega-block, where no Proterozoic igneous rocks are mapped except vein units and migmatites of probably collision stage, is explained by its direct proximity to the paleo-subduction zone. The time of complete mega-blocks collision is marked as 2.1 Ga by the age of alkaline rocks in Malotersyanskiy massif in Orikhivsko-Pavlogradska band [41]. In the map sheet area this geodynamic environment is reflected in the rocks of Chernigivskiy carbonatite complex which are same-aged and allied to the rocks of Malotersyanskiy massif. The massifs of Chernigivskiy Complex, as well as the numerous potassium granite bodies of similar in age Anadolskiy Complex, are located at the boundary between the frontal zone and volcano-plutonic belt of the active continental margin – the regional weakened zone in the mega-block used by the collision magmatites.

3) Distribution of Proterozoic metamorphites in the eastern part of the map sheet – Sadova Sequence and other possible rocks of this age – does correspond to the boundary between zones of carbonate-alkaline and alkaline magmatism in the lateral igneous zonation of the mega-block. In Phanerozoic active continental margins occurrence of extension zones in this position is considered to be typical [22] that confirms the taken concept for Proterozoic crustal evolution in the region.

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Paleozoic stage Pryazovskiy mega-block comprises the narrow (up to 150 km wide) region of crystalline rocks of

Ukrainian Shield which is pinching out in this area and is surrounded by the Late Precambrian – Paleozoic structures of Dniprovsko-Donetskiy Aulacogene and the basement of Scythian Plate. Thus it is not surprising that Late Paleozoic (340-260 Ma) igneous rocks of Volnovasko-Elanchytska and Zirkska associations (stocks and dykes of mafic and intermediate, often sub-alkaline composition) are encountered in the map sheet territory. According to the paleo-tectonic and paleo-geographic reconstructions [23] in Late Devonian time commenced the major opening period of Dniprovsko-Donetskiy Aulacogene – the died branch of triple rifting system, which two active rifts had formed the south-western margin of the Eastern-European Platform. In other words, in that period the mega-block territory comprised peninsula bounded by rifting basins. According to [23], subduction zone was formed about 340 Ma along the modern southern margin of the Eastern-European Platform, Herzinian fold belt was formed in the Middle-Late Carboniferous time through the collision with island arcs in the basement of Scythian Plate and then in the Permian time the folding in Donbas had occurred. Thus, the Permian-Carboniferous igneous rocks of the mentioned associations reflect events occurred that time in around of Pryazovskiy mega-block – the internal massif in the system of Herzinian fold belts.

Meso-Cenozoic stage Jurassic rocks developed in Novomykhaylivska Depression comprise the oldest sediments in the studied

area. The rocks (sequence of clays and sands) gently plunge (5-10o) to the south. It is not excluded that formerly Carboniferous rocks overlain Precambrian rocks and then upon erosion they provided the source material for Jurassic sediments.

Over the Late Cimmerian (Andean) orogenic phase at the Jurassic and Cretaceous boundary the Stulnivska and Chernigivska depressions were formed in Chernigivsko-Stulnivska LTZ; the lake-swamp sedimentation regime (sandy-clayey sequence) was established in these depressions in Early Cretaceous time. At the end of Early Cretaceous, due to the Austrian phase of tectogenesis, Precambrian rocks of the northern and central parts of the territory were uplifted to the surface and up to the Campanian time no sedimentation occurred there.

In Prymorska LTZ the sea transgression continued that had commenced in the Aptian time. It caused the clayey-sandy sequence formation (Lunacharska, Genicheska and Berdyanska suites).

In the Campanian time the sea transgression attained its maximum and apparently whole territory was covered by the sea basin waters. This caused deposition of marine sediments both in Chernigivsko-Stulnivska and Prymorska LTZs (sequence of sandy rocks and marls).

At the Cretaceous-Paleogene boundary, due to Laramian phase of tectogenesis (67 Ma), entire map sheet territory uplift occurred and the area became the land. In this period (up to Middle Eocene) the extensive denudation and weathering crust formation occurred.

The Cenozoic period was dominated by marine and continental sediments formation which distribution depended on the relief of crystalline basement surface. Paleogene sedimentation commenced since Middle Eocene when the southern slope of the Shield was covered by sea basin waters and expansion of transgression to the north suppressed crystalline basement uplift. In the coastal areas the kaolineous (coaliferous in places) clays and sands were depositing. At the same time, in the elevated portion of Pryazovskiy block the continental sedimentation regime occurred and sequence of sands and clays as well as Eocene clayey-sandy sequence were depositing filling up the Stulnivska and Chernigivska depressions in the north-west of the map sheet.

At the Paleogene-Neogene boundary the Savska phase of orogenesis (26 Ma) actively appeared in the map sheet area. It is reflected in the stratigraphic discontinuity between respective sediments in both Chernigivsko-Stulnivska and Prymorska LTZs. Erosion of the older rocks was fairly significant. In Neogene (Middle and Late Miocene) the different conditions of sedimentation in the north and south of the map sheet retained. Starting from the Middle Miocene due to slow subsidence over the southern part of the territory the sea transgression occurred in Prymorska LTZ. Lithology of the sediments reflects the frequent changes in the conditions of sedimentation from the coastal-marine to marine ones both by depth and by strike. In other words, on the background of general subsidence the vertical variations of the sedimentation surface occurred. In Chernigivsko-Berestovska LTZ in Middle Miocene the river-bed, flood-land and lake facies sediments were depositing in the continental environments (Novopetrivska Suite). In Late Miocene the denudation stage (Early-Middle Sarmatian) had changed by the stage of marine lagoon sedimentation (Late Sarmatian).

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At the Sarmatian-Pontian boundary in Late Miocene the Antychna phase of orogenesis (12 Ma) released in general uplift of the map sheet territory caused lacking of Meotychniy stage sediments.

Starting from the Pontian time, the territory of Chernigivsko-Berestovska LTZ became the land with continental sedimentation environments. In Prymorska LTZ the sea basin expanded in Early Pontian and Pliocene with the denudation and erosion phase in Late Pontian.

At the Neogene-Quaternary boundary the Volakhska phase of Alpine orogenesis emerged (~2 Ma). That time the physico-geographic situation over the Earth had changed abruptly. Conditions for Quaternary sediments deposition appeared.

The geological history over Quaternary epoch is characterized by the rhythmic climate variations and changes of paleo-geographic conditions; the changes were directed and distinct for each particular rhythm – cold or warm one. The continental glaciations and inter-glacial periods over the territory of entire Ukraine and the Eastern-European Platform as a whole were the major events in the Quaternary history. The map sheet location in the back-glacial zone (sub-zone of the southern loess areas) provided formation of the loess-like loams and clays over the cold periods and the loamy and clayey former soils – over the warm ones. Simultaneously the river-bed deepening occurred where alluvial sediments were depositing.

The modern period of the territory developments is characterized by formation of eluvial, eluvial-deluvial and alluvial sediments throughout in the area.

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7. GEOMORPHOLOGY AND RELIEF-FORMING PROCESSES In accordance with the geomorphologic zonation of Ukraine the territory of map sheet L-37-VII

(Berdyansk) encompasses Azovsko-Prydniprovska Height and Prychornomorska Lowland [7] (see “Scheme of structure-geomorphologic zonation”).

In geomorphologic and morpho-structure respect the northern part of studied area, which belongs to the Western Pyazovskiy block of Ukrainian Shield, is expressed in the relief with the Pryazovska Height (positive morpho-structure). Its southern part, which belongs to Azovsko-Kubanska Depression, comprises the lowland (negative morpho-structure). In the neo-tectonic development stage the mentioned Height underwent the variously-oriented but mainly positive tectonic motions whereas the Lowland – mainly negative motions being compared to the Height.

The boundary between the mentioned morpho-structures apparently follows the zero contour line of crystalline basement surface and almost coincides with the development contour of the Late Pliocene marine sediments of Novovasylivska Sequence naturally separating these morpho-structures.

The relief of Pryazovska Height in the studied area resembles one in the bed of sedimentary rocks, that is, denudation surface of crystalline rocks and their weathering crust. The highest altitudes in the Height are confined to the northern boundary of the map sheet. From this area, the watershed surfaces gradually plunge to the south and south-west up to the flat-wavy Pryazovska Lowland. Within the Height the watersheds comprise the separated heights being one of the clear indicators for denudation patterns of the sedimentary cover floor.

Occurrence in the watersheds the denudation remnants composed of crystalline rocks and dependence of the river valley morphology on the relief of crystalline basement provides another distinct feature of the relief in Pryazovska Height. At the slope foots and in the bottoms the crystalline rock outcrops including cliffs, flat bars and rapids in the river courses are frequently observed and in places the valleys look like the small canyons.

Complete lacking of horizontal or semi-horizontal sections in between the rivers comprises the distinct feature of the Height. Actually the areas between the rivers are the combinations of slopes with variable shape, inclination and morphology related to the structure of crystalline basement, as well as lithology and thickness of Quaternary and Meso-Cenozoic sediments in sedimentary cover. This indicates the denudation nature of the crystalline basement surface and the long-term period required for this surface preparation.

Pryazovska Height is cut by relatively deep and dense erosion system. The valley depth here often attains 70-100 m suggesting for extensive neo-tectonic uplifts.

Geological structure of the Height is complex. Almost throughout the crystalline basement occurs above the local erosion basis. On the weathered surface of crystalline rocks with considerable discontinuity unconformably and not throughout lie mainly continental sandy-clayey Paleogene and Neogene sediments up to 30 m of total thickness. In the north-western part in the local depressions (Chernigivska, Novomykhaylivska and Stulnivska) the Mesozoic (Jurassic and Cretaceous) sediments are developed. Actually over entire territory the blanket of Quaternary continental sediments occur; these rocks participate in all geomorphologic elements of the relief (see “Tectonic scheme” to the geological map of Quaternary sediments).

Pryazovska Lowland is limited from the north by the boundary of exposed Pryazovskiy massif crystalline rocks and Late Pliocene marine sediments, and from the south – by Azov Sea. This is accumulative lowland plain on the Neogene basis almost everywhere covered by alluvium of Eo-Pleistocene terraces, and in the river valleys – by Neo-Pleistocene and Holocene alluvium. In the coastal area throughout Quaternary marine sediments occur.

The surface of the inter-river areas is most elevated in the north where altitudes attain 80-100 m. To the south and south-west they gradually decreases up to the sea coast scarp with maximum values up to 35-40 m and 4-2…0.4 m in the sub-horizontal plain of the sea coast.

The Lowland is cut by shallow valleys of rivers and gullies which depth attains 30 m and more. The watershed areas comprise weakly-eroded wavy surfaces. The relief of Pryazovska Lowland is caused by geological structure and especially by neo-tectonic stage of development. Influence of crystalline basement on the relief formation essentially decreases along with it stair-like plunging beneath Meso-Cenozoic sediments which thickness in Berdyanska sandbank attains 875 m.

The width of river valleys attains 1.5-2.0 km. The valley slopes are more flat. The surface inclination at the watersheds is less than one in the Height.

Eight genetic types of relief are distinguished based on results of structure-geomorphologic zonation and geomorphologic studies in the course of the large-scale geological mapping [58, 59]: structure-denudation, denudation, accumulative-denudation, accumulative, erosion-accumulative, plain, marine and estuary-marine, gravitation and aeolian.

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Structure-denudation relief is connected with watersheds and is defined in some sites where denudation remnants are preserved in places. These sites comprise the fragments of primary watersheds. Their surface is covered by thin eluvial-deluvial Late Eo-Pleistocene loams with inclusions of crystalline rock gruss and gravel, and by Holocene soil.

Seven major sites are shown in “Structure-geomorphologic scheme”. The sites are oval-shaped, isometric, rarely elongated. The size varies from 1-1.4 to 2-3.4 km across. Average surface inclination angle is 5o. In three sites the denudation remnants are observed comprising the hills composed of crystalline rocks and partially covered by modern soil-plant layer. The remnant altitudes are as follows: 324 m (Belmek-Mogyla hill), 307 m (Synya hill) and 138 m (Korsak-Mogyla hill). Age of structure-denudation relief is apparently pre-Neogene [71].

Accumulative-denudation relief comprises watershed-slope, inclined, partitioned accumulative-denudation plain on Precambrian, rarely Mes0-Cenozoic basement with the cover of Quaternary loess-like rocks (area A-I-a) and in Pryazovska Height it occupy the watersheds and their slopes. The maximum heights are observed in the northern part and attain 300 m, decreasing southward up to 80 m. The inclination toward the river valleys and gullies is also observed.

This relief type is widespread at the watersheds. The relief of the plain is close to the relief of crystalline rock surface and was formed as a result of long-term denudation over period from Mesozoic to Quaternary. In Quaternary time the surface of denudation plain was covered by the red-brown clayey and loess-like loamy sequences of 5-30 m total thickness. The share of Neogene sediments gradually increases from the north to south.

The Quaternary sediments had essentially smoothed the crystalline basement relief irregularities providing soft appearance of the relief. The age of relief is defined in the range from Late Paleogene to Early Neogene. It is thought that the crystalline basement relief was formed over this period. Over Neogene and Quaternary relief-forming stages residual relief was refreshed and through accumulation of aeolian-deluvial sediments and relief-forming processes had got its present features. On the southern slopes of the Height the inter-river areas gradually decrease getting the characteristic wavy soft profiles.

The denudation relief type is known on the slopes of accumulative-denudation plains cut by ravine-gully network (area A-I-a). On the slopes of river and gully valleys the open hard-rock slopes, in places covered by eluvium-deluvium, and closed deluvial slopes are distinguished. Deluvial closed slopes of Upper Quaternary accumulation are widespread in Pryazovska Height. They are developed on the right and left slopes of the river and gully valleys. The width of deluvial closed slopes varies from some tens and hundreds of meters to 2-3 km. Average inclination angles are 15-20o. Although the edge of the slope is poorly expressed, the closed slopes are being well defined in processing of satellite images. The surface of the slopes is cut by gullies and ravines. Proximity of crystalline rock surface causes relatively shallow depth of ravine and gully network. Deluvial cover is composed of loams, in places with considerable amount of crystalline rock fragments. Thickness of deluvium is 2-6 m.

The open hard-rock slopes are related to the crystalline rock exposures at the surface. In places they sharply rise above the valley bottom and form the cliffs. Average inclination angles of the open slopes are 30-45o. In places the open slopes are covered by thin (1-2 m) eluvial-deluvial sediments with inclusion of abundant gruss, gravel and crystalline rock fragments. The denudation of hard rocks comprises the major factor of the open slopes formation.

In Pryazovska Lowland the denudation relief type is represented by the closed slopes only. Due to wide development of alluvial terraces over the gully and ravine slopes the areas of both relief types often coincide and by these reasons the denudation relief type is not shown in the “Structure-geomorphologic scheme”.

Accumulative relief is developed in Pryazovska Lowland, particularly, in its Pryazovska accumulative lowland plain (on the Neogene basis) and in one specific area – Pryazovska slightly-inclined weakly-cut accumulative plain with the cover of Quaternary loess-like rocks (area A-I-b). This area comprises the lowland plain with general surface inclination to the south and south-west and occupies the watershed sites. The wavy-hill surface of the plain is caused by the valley-gully network. Average altitudes of the surface are 30-40 m. Maximum ones are confined to the watersheds in the northern part of the plain where they attain 50-60 m.

The geological base of this plain includes up to 50 m thick marine sediments of Late Miocene Novovasylivska sandy-clayey sequence and undivided up to 33 m thick Pliocene-Quaternary sediments of Kyzyldzharska (tenth) alluvial terrace.

Pryazovska sub-horizontal accumulative plain of the sea coast (area B-I) encompasses the Azov Sea coast and include the plain marine and estuary-marine accumulative relief type of the sea sandbanks and coast. Surface of the plain is sub-horizontal with altitude variations 0.4-0.8 m in the beach and up to 3.5 m in the sandbanks. In geology of the coast and sandbanks, besides Cretaceous, Paleogene and Neogene sediments, the Early Pleistocene and Holocene marine sediments also participate.

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Erosion-accumulative relief is fairly widespread and is related to the Quaternary activity of water flows in river valleys and gullies. This relief type is expressed in the numerous river alluvial terraces.

In Pryazovska Height the valleys of Berda, Tokmak, Yushanly, Krushanly, Korsak, Obitochna, Lozovatka, Kiltychiya, Berestova, Karatyuk, Mokra Konka rivers and their branches are developed in the crystalline rocks and display dendrite patterns in the plane. Directions of the river valleys coincide with the general inclination of the plain surface and depend on the geology and tectonics of the territory. Connection of the river and gully valleys with tectonic faults is evidenced by: the strait-line valley sections with abrupt turns by 90o and more (valleys of Lozovatka River at Yuryivka, Kolarivka villages; Chokrak River at Elizavetovka, Dolynske villages etc.); cross-like location of the branches; opposite-directed, transverse valleys joined at the watersheds by the common saddle (Saltych and Yushanly rivers). In the zones of tectonic faults essential valley widening occur [71, 117].

In Pryazovska Lowland the part of river system (Lozavatka, Obitochna, Kiltychchya) belongs to the equal-stream type of consequent setting resulted in sharp asymmetry of river basins and valleys. The river valleys display the slope asymmetry: the right slope is very flat and broad whereas the left slope is relatively narrow and steeper. The valley of Berda River is also asymmetric: its right slope in the lower river course is steeper whereas the left slope is flat and is weakly cut by slightly-expressed gullies. The valleys of many rivers are developed in the crumbly rocks of the loess-loamy sequence. Most of the minor and medium shallow gullies by their morphology belong to the steppe gullies. They are V-shaped and have narrow flat or concave bottoms 5-50 m wide. Their slopes are flattened. The major gullies have asymmetric slopes and flat bottoms 50-400 m wide.

The total number of alluvial terraces is 11, specifically: one Late Pliocene, one Late Eo-Pleistocene, eight Neo-Pleistocene terraces, and one Holocene. In addition, there is Early Pleistocene (Zyukska) sea terrace developed in the Azov Sea coast. Description of erosion-accumulative relief is given below for each terrace starting from the oldest ones. Formation of terraces is related to the neo-tectonic activity in the area resulted in the erosion basis changes.

The fans in ravines and gullies composed of proluvial-deluvial sediments comprise the variety of erosion-accumulative relief. The biggest fan is located at the base of Berdyanska sandbank being extended over 2.2 km along the sandbank. Surface of the fan cone is inclined to the south with the bar drops to 1.5 m. Other fan cones are minor in size (up to 5-10 m across) and thickness (up to 0.5 m).

Accumulative marine and estuary-marine relief is developed in the sea coast and includes the coastal beach band and Early Neo-Pleistocene sea terrace.

Berdyanska sandbank is triangular-shaped. The sandbank surface is irregular, lowland, complicated by the lakes and estuary tongues, which are periodically flooded by the sea, as well as by the minor coastal arcs and sand dunes. The altitudes of sandbank surface vary from 0.4 m along the coastline to 4-5 m at the base of sandbank. The eastern flank of the sandbank is somewhat elevated in comparison to the western one due to storm coastal arcs as well as the beach sand winding and formation of the sand-aeolian relief forms – heaps and dunes. Their height varies from 0.5 to 2 m.

Obitochna sandbank includes its base about 40 km long and 3.4 km wide. The sandbank surface is low, flat, and complicated by estuaries up to 3 km long and up to 0.6 km wide. Some minor coastal arcs and sand dunes are observed on the surface. The surface altitudes vary from -0.4 m (by coastline) to +3 m (heaps). Marine and estuary-marine sediments of the sandbank are of Holocene age. Their thickness is 5-8 m.

The bars which separate the estuaries from the sea are developed on the sandbanks and are up to 300-400 m wide. They are composed of the same rocks as the sandbanks themselves.

At the western coast of Berdyanska sandbank a range of minor sand islands are developed comprising the elevated bars.

The sand beaches normally are narrow – from some meters up to 10-15 m, rarely 25 and more meters, and are developed along the coastline of sandbanks, bars, islands and sea coast. The beaches are composed of diverse-grained sands with inclusions of fine pebble, crystalline rock fragments and rounded carbonate concretions. Abundant fragments and solid mollusc shells are observed in the beaches. In places the weakly-expressed coastal bars occur in the beaches. The sandbanks and other accumulative relief forms are of Holocene age.

Gravitation relief is developed in the sea coast and in the right valley slope of Berda River lower course; it includes abrasion-accumulative sliding and abrasion-collapse types.

The sea coast bench is developed along the Azov Sea coastline. By degree of wave processes impact on the formation of the bench morphology it is divided into the coast bench under abrasion and the died coast bench. Abrasion coast bench at present undergoes active abrasion in stormy weather. Its morphology is being formed mainly due to the active sliding and collapse-sliding processes. In those places where these processes are

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terminated the beach abrasion bench is complicated by the former (stabilized) slides expressed here as the terraces.

The abrasion coast bench is defined in those parts of Azov Sea where the coast undergoes abrasion impact only. These are the coast sections which adjoin the river and gully mouths, as well as the sections of relatively low coast up to 20 m high.

The abrasion coast bench is very steep everywhere. By numerous vertical fractures the rocks in the bench are split into the block of various sizes. From time to time, some of these blocks are being disconnected of the hard-rock coast, then they get detached and, collapsing, form the heaps at the bench foot. Over the sea storms the heap material is being disintegrated and removed by the coastal flows. At the same time, the tidal hollows and cauldrons are being formed in the abrasion wall (cliff), mainly pursuing the vertical fractures. The depth of some hollows attains 2-3 m. Upon the storms the 2-3 m wide bench is exposed at the cliff foot being composed of the tenth terrace clays. In the sections of abrasion coast the beach normally is absent. In places it comprises narrow band from some meters to 5-10 m wide.

The sea coast bench, undergoes abrasion and complicated by the active slides, does occupy the lengthy coastal sections between Obitochne village and Berdyansk town, and further to the east of Novopetrivka village.

The coast geology in these sites, where thick (up to 20-22 m) Quaternary loams overlie the alternating alluvial watered sands, loams and clays, coupled with permanent coastal abrasion, facilitate development of the huge (by length and width) frontal slides.

The died coast bench is defined at the base of Obitochna and Berdyanska sandbanks. Sea-wave processes here do not approach the bench and do not affect formation of its morphology; these are the reasons why the coast bench is considered died one. At present its morphology is influenced by deluvial processes, and partially erosion ones. Through the integrated action of above processes the bench got relatively flat, overgrown throughout and very close to the steep slopes of the river valleys and gullies. The height of died bench may attain 15-18 m at the base of sandbanks and up to 30 m on the right slope of Berda River in its lower course.

The active slides are known mainly in the coast of Azov Sea and in its abrasion bench. The slides are observed in the sections where the coast is composed of intercalating sandy-clayey sediments of the tenth, ninth and seventh terraces, partially watered and undergo the sea abrasion. By shape, the slides are mainly frontal, rarely circum-like. Slipping down of the slide bodies often is released over the clays of tenth terrace alluvium.

Detachment walls of the slides, composed of Quaternary loess-like rocks, commonly are almost vertical. Their height depends on thickness of these rocks and may attain 15-20 m. The slide bodies consist of the stair-like down-slipping blocks distributed over the slope. Surface of some blocks is inclined toward the detachment wall. The slide body is cut by numerous open fractures of various length and depth. Fractures are most abundant in the tongue part of the slide. On the individual block slipping directly to the zone of sea-wave processes they get eroded and released material is being removed by the coastal flows.

Aeolian relief comprises heaps and dunes and is developed along the beaches in Berdyanska and Obitochna sandbanks as well as in bars and islands. The height of these aeolian units is low – from 0.5 to 2-3 m.

Technogenic relief forms include quarries, dumps, pond dams, waste polygons, and ancient mounds. The relief formation in the studied area is controlled by endogenous and exogenic processes. Influence

of endogenous processes includes vertical tectonic movements: positive and negative. By means of repeating geodesic survey it is established that the northern, most elevated part of the area is going up at more than 3 mm per year speed whereas sea coast moves down at about 1 mm per year speed [7]. Exogenic geological processes provide the relief smoothing in the regional respect. Erosion and denudation processes predominate over the Height. Development of accumulative processes is characteristic for the Lowland.

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8. HYDROGEOLOGY The territory of map sheet L-37-VII (Berdyansk), according to the hydrogeological zonation (Fig. 8.1)

belongs to the two first-order hydrogeological areas: fracture waters of Ukrainian basin (its south-eastern part – Pryazovskiy Crystalline Massif (PCM) which by geological zonation belongs to Chernigivsko-Berestovska LTZ) and Prychornomorskiy artesian basin (Azovo-Kubanska depression – Prymorska LTZ). The distinct hydrogeological conditions are encountered in the junction zone of PCM with Azovo-Kubanska depression comprising the system of faults and block structures.

Within the limits of PCM the north-eastern closure of Prychornomorska Depression was distinguished including Stulnivska, Novomykhaylivska and Chernigivska depressions.

The geological, geomorphologic and climatic factors define variability of underground waters distribution, forming conditions, chemical composition, feeding and discharging.

Fig. 8.1. Sketch hydrogeological map. See next page for the legend.

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Water-bearing horizon of Holocene – Upper Pleistocene alluvial and alluvial-deluvial sediments (a,adPIII-H) is developed in the river flood-lands and gully bottoms deeply cut into the hard rocks. Water-bearing rocks include sands with interbeds and lenses of clays, muds, loams and sandy loams, in places gravel is observed at the bottom. Depth of the ground water table is up to 2 m. Water saturation is irregular with borehole yields from 0.01 to 0.84 l/s. Water mineralization varies from 0.9 to 41.1 g/dm3, normally 1-3 g/dm3. By type, waters are chloride-sodium and sulphate magnesium-calcium-sodium. Due to low water saturation, high mineralization and hardness the waters of this horizon are not suitable for the centralized water supplying but it is used by the local inhabitants for the housing needs and in places for drinking.

Water-bearing horizon of Holocene marine and estuary-marine sediments (m,lmH) is developed in Berdyanska sandbank and along the Azov Sea coast within the limits of modern sea beach. It is composed of sands with clay and mud lenses. At the base in places gravel and pebble occur. The water table depth is up to 0.9 m. Borehole yields attain 9.1 l/s. Mineralization of underground waters varies from 5.7 to 33 g/dm3. Waters are mainly chloride magnesium-calcium-sodium and chloride sodium. Regime of this water-bearing horizon depends on the feeding conditions and the Azov Sea level variations.

Water-bearing horizon of Akchagylskiy regio-stage clayey-sandy sediments (N2gp) is developed in the broad band from 7 to 20 km wide along the Azov Sea coast. It is composed of sands with clay and sandstone interbeds of total thickness from 5.0 to 49.5 m. Water table varies in the range 0.1-42.0 m below the surface. Piezometric table altitudes vary from 21.3 to 2.5 m going down from the north to south and from watersheds to the river and gully valleys. The pressure figures are 8-30 m, rarely 10-15 m. Yield varies in the range 1-3 l/s. Waters are slightly-saline with mineralization 1.1-2.3 g/dm3, rarely the brines occur which mineralization attains 51 g/dm3; normally the are waters with 1.5 g/dm3. By chemical composition waters are mainly hydrocarbonate-chloride-sulphate, magnesium-calcium-sodium, the brines – chloride sodium.

Waters of this horizon do not match the standard requirements for the centralized water supplying but in the local arid climate they are being used for drinking and provide the major supplying source over entire area of its development.

The waters are being exploited everywhere by single boreholes and the group scoops with output 25-100 m3/day for water supplying of enterprises, villages and medical institutions located on the Azov Sea coast. Aiming improvement the water supplying of Berdyansk town, in the area of Lunacharske village the water reserves are explored and approved by categories B+C1. Deposit is entered into exploitation in 1972 and is in production to date.

Water-bearing horizon in iron-enriched sandstones of Cimmerian regio-stage (N2zp) does form the band along the modern coast of Azov Sea, a bit further to the south from the boundaries of water-bearing horizon in Akchagylska clayey-sandy sequence and in places the boundaries of two horizons coincide. In the areas of Kutsa Berdyanka and Lozovatka rivers and Sukha gully the iron-enriched sandstones lie to the south of clayey-sandy sequence. The water-bearing rocks include diverse-grained sands and sandstones. Their thickness varies from 3.0 to 44.5 m. Depth of the horizon hanging-wall varies from 26.6 m to 92.2 m and increases toward the sea and watersheds. The waters are pressurized. Pressure value varies from 14 to 68 m. Yield mainly is 0.5-1.0 l/s. By chemical composition chloride sodium waters predominate, chloride-sulphate, sulphate-chloride and other water types are less common. Mineralization varies from 1.1 to 37.7 g/dm3, normally – 2-3 g/dm3.

Water-proof sequence of Cimmerian regio-stage red-brown clays (N2cb) is locally developed along the sites composed of Meso-Cenozoic sediments, pinching out in the river valleys (Prymorska LTZ) or at the depression boundaries and watersheds (Chernigivsko-Berestovska LTZ). Southern limit of water-proof sequence coincides with the limit of Akchagylskiy regio-stage clayey-sandy sequence. Thickness attains 16.1 m. This sequence separates the waters of alluvial-deluvial sediments from underlaying horizons of Neogene (Prymorska LTZ), Paleogene and Cretaceous (Chernigivska depression), and Precambrian (Chernigivsko-Berestovska LTZ).

Water-bearing horizon of Pontian regio-stage oolite and shelly limestones (N1v) is developed in minor enclaves in the north-eastern part of Prymorska LTZ. The southern boundary lies to the north of the Akchagylskiy regio-stage Novovasylivska sequence boundary, and its northern boundary actually coincides with the northern edge boundary of Azovo-Kubanska Depression (area of Osypenko village). It is composed of limestones and sands with clay interbeds; is intersected by drill-holes [58]. In the northern part clays and sands predominate being gradually substituted by limestones to the south. Borehole yield is normally 0.5 l/s. By chemical composition the underground waters are chloride-sulphate, sodium-calcium, with mineralization 2.0-4.4 g/dm3.

Water-bearing horizon in undivided Katerlezsko-Geliksovi layers of Sarmatian regio-stage (N1kt-gl) is developed in Prymorska LTZ and in the narrow band is observed along the slope of Prychornomorska Depression. Water-bearing rocks include fine-grained sands, sandstones and limestones. Water-bearing horizon is pressurized-non-pressurized. The table of underground waters is free and waters become pressurized at the foot of river valley slopes. Borehole yields are 3-4 l/s. Mineralization varies from 0.8 to 19.3 g/dm3, normally – 2

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g/dm3. By chemical composition the waters are chloride-hydrocarbonate-sulphate, magnesium-sodium-calcium and chloride-sodium. Underground waters do not match requirements of the standard No. 2874-82 “Drinking water” for the centralized water supplying.

In the arid conditions these waters, as an exception, can be used for the housing-drinking water supplying of minor consumers under permission from sanitary-epidemiologic authorities.

Water-bearing horizon in undivided Novomoskovsko-Dnipropetrovski layers of Sarmatian regio-stage (N1nm-dn) is developed in Prymorska LTZ, in Berdyanska sandbank, and in the south-east part of the map sheet. Water-bearing rocks include fine-grained sands and limestones. Water-bearing horizon is pressurized-non-pressurized. The underground waters contained in Novomoskovsko-Dnipropetrovski layers, are pressurized up to 110 m in the limits of Berdyanskiy Graben. Borehole yield is 3-4 l/s. Mineralization varies from 0.8 to 19.3 g/dm3, normally – 2 g/dm3. By chemical composition the waters are chloride-hydrocarbonate-sulphate, magnesium-sodium-calcium and chloride sodium. The underground waters do not match requirements of the standard No. 2874-82 “Drinking water” for the centralized water supplying.

Water-bearing horizon in clayey-sandy sequence of Sarmatian regio-stage (N1gp). In the limits of Cgernigivsko-Berestovetska LTZ this horizon is developed in separated places. It is composed of diverse-grained sands that overlie the crystalline rocks. The sites are locally developed and are not considered as the separate water-bearing horizon. Borehole yield is 1-2 l/s.

Mineralization varies from 0.8 to 19.3 g/dm3, mainly – 3 g/dm3. By chemical composition the waters are chloride-hydrocarbonate-sulphate, magnesium-sodium-calcium and chloride sodium. The underground waters do not match requirements of the standard No. 2874-82 “Drinking water” for the centralized water supplying.

Water-proof sequence of undivided Kuzhorski and Zbruchski layers of Sarmatian regio-stage (N1kz-zb) is traced in the solid band 2-10 km wide along the coast of Azov Sea. The northern boundary of Kuzhorsko-Zbruchski layers follows the centre of northern edge of Azovo-Kubanska (Prychornomorska) Depression, at the south-western outskirt of Inzivka village, then, respectively, up to the line of faults, along the left slope of Lozovatka River valley, and further close to Obitochna, Banovka, Shevchenko, Novovasylivka, Osypenko villages. It is composed of dark-grey to black argillite-like clays, with minor grey sand.

Sands, especially at the base of clays, are 1-5 m thick. Thickness increases in southward direction up to 70 m, mainly being in the range 5-39 m. This sequence comprises the regional water-proof between the water-bearing horizons in Cimmerian (N2zp) and underlaying Konkski (N1sr-kn and N1np) regio-stages, and in sandbank – between Cimmerian (N2zp) and Sarmatian (N1nm-dn) regio-stages. In this way, the feeding and discharging conditions and chemical composition of underground waters in the listed horizons are separated. In addition, the water system is divided into the infiltration and elision pressurized branches.

Water-bearing horizon in undivided Sartagansko-Konkski layers of Konkskiy regio-stage (N1sr-kn) is known in the enclaves in Prymorska LTZ. It is composed of clayey sands. Water table depth varies from +2.3 m to -44 m. Waters are pressurized; pressure value is up to 96-98 m. Borehole yield is 0.005-1.93 l/s. By quality the waters vary from the fresh to salty with mineralization from 0.8 to 22.3 g/dm3. Water types: chloride-sulphate, chloride sodium. The underground waters do not match requirements of the standard No. 2874-82 “Drinking water” for the centralized water supplying. The water-bearing horizon is perspective for mineral water prospecting.

Water-bearing horizon in Novopetrivska Suite of Poltavskiy regio-stage (N1np) is developed in depressions of Chernigivsko-Berestovska LTZ. Water-bearing rocks comprise diverse-grained kaolineous sands. Previously the horizon was not studied and requires additional works.

Water-bearing complex in Eocene sediments (P2). It is developed in the depressions of Chernigivsko-Stulnivska LTZ and Prymorska LTZ. In Stulnivska and Chernigivska depressions the water-bearing rocks include sands, weakly-cemented sandstones, conglomerates and gravelites. Water tables are set at the depths from 11.3 to 43 m below the surface providing the pressure value of 27-31 m. Borehole yield varies from 0.48 to 3.07 l/s. By chemical composition the waters are chloride-sulphate calcium-magnesium-sodium with mineralization 3.8-7.5 g/dm3. In Prymorska LTZ the water-bearing horizon in Eocene sediments is developed in the limits of Berdyanskiy and Obitochnenskiy grabens. Water-bearing rocks include sands and marls up to 93 m thick. Water table is set at the depths from +3.1 to -45 m below the surface providing the pressure value from 15 to 300 m. Specific borehole yield varies from 0.5 to 2 l/s. By chemical composition the waters are chloride-sodium with mineralization from 10 to 45.9 g/dm3. Increased content of bromine and iron is determined in the waters. Due to high mineralization the waters are not suitable for housing-drinking water supplying.

Water-bearing complex in Lower-Upper Cretaceous sediments (K1-2) is developed in Prymorska LTZ, in Berdyanskiy and Obitochnenskiy grabens, and in the narrow band along the coast. Underground waters are pressurised. Pressure value varies from 13 to 42.7 m. Table depth is +1.0 … -37.3 m. Borehole yield varies from 0.21 to 77.41 l/s. By chemical composition the waters are chloride-sulphate with mineralization from 0.7 to 17

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g/dm3 which increases as the complex surface plunges down. The fresh waters are being used for drinking water supplying.

In Prymorska LTZ the water-bearing rocks include sands, sandstones and marls. Water content is not too high and is variable in comparison to the sediments in the northern depressions. Specific borehole yields vary from thousandth to 0.75 l/s, in sandbank – mainly 0.6 l/s. Water-bearing complex is pressurised. Water tables are at the depths +3.5 … -6.1 m below the surface providing pressure height of 121-557 m. By chemical composition the waters are chloride sodium with mineralization up to 60 g/dm3. In DH 748g [109] with bromine mineral water which is being exploited for medical needs of “Lazurniy” sanatorium (Berdyansk town) reserves by categories A+B are approved in 1980. This complex is perspective for bromine, bromine-iron, iron-bromine, iodine-bromine and other mineral waters.

Water-bearing horizon in Upper Cretaceous sandy sequence (K2p) is developed in the limits of Stulnivska and Chernigivska depressions in Chernigivsko-Berestovska LTZ. Water-bearing rocks include sands, sandstones, silica clays, and at the footwall – gravelites. Thickness of this sequence attains 30 m. Water table is free and the waters become pressurized at the slope parts of river valleys. Previously the horizon was not studied and requires additional works.

Water-bearing horizon in Middle Jurassic sediments (J2) is defined for the first time. It is developed in the limits of Novomykhaylivska Depression in the north-western part of the territory, and is composed of sands, argillites and aleurolites. Thickness of horizon varies from 25 m to 119 m. Depth of water-bearing horizons varies from 35 to 110 m. At the bottom the crystalline rocks occur, and at the top – Novopetrivska sequence.

Water-bearing horizon is pressurised. Pressure value is 24-74.4 m. Water table is set at the depth 6.8-25.6 m below the surface. Specific borehole yield is 0.02-0.0006 l/s. Filtration coefficient is 0.005-0.23 m/day. By mineralization the waters are slightly-saline – 1.3-2.0 g/dm3. By chemical composition the waters are sulphate sodium-magnesium. Previously the horizon was not studied and requires additional works. At the higher yield the waters can be used for housing-drinking water supplying.

Water-bearing horizon in fractured Archean-Proterozoic crystalline rocks and their weathering crust (AR-PR1) is developed throughout in the area. The water-containing sequence belongs to the most weathered and fractured zone of crystalline rocks. Specific borehole yield is 0.008-219.58 m3/day under depression 39.5-3.0 m. Quality of underground waters varies both by lateral and by depth. Mineralization varies from 0.2 to 11 g/dm3 in the area of crystalline massif and significantly increases in the northern slope of Prychornomorska Depression attaining 60 g/dm3. By chemical composition sulphate and chloride-sulphate waters predominate, and chloride sodium waters are developed in the south. Normally the water are hard, total hardness is 18-57 mg-equiv./dm3. The brine-like waters are encountered in Berdyanska sandbank; they may contain economic concentrations of bromine, iodine, boron, rare and alkali-earth elements. By temperature these waters are classified as warm thermal waters. Due to high mineralization the waters do not match requirements of the standard No. 2874-82 “Drinking water” for the centralized water supplying. However, in case of lacking other sources the waters can be used for housing-drinking water supplying by individual enterprises.

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9. MINERAL RESOURCES AND REGULARITIES IN THEIR DISTRIBUTION

Metallogenic zonation By the list of mineral types and their abundance, Pryazovska metallogenic province which includes

considerable part of the studied area, is highly ranked in metallogenic zonation of Ukraine. Taking into account tectonic zonation, evidences, criteria and regularities of mineral resources

distribution, three tectono-metallogenic zones (TMZ) are distinguished in the crystalline basement (see “Scheme of metallogenic zonation” to the geological map of crystalline basement).

The central part of the map sheet (about 80% of the territory) is occupied by Zakhidnopryazovska TMZ which metallogenic features are defined by deposits of iron ores, apatite, gold and ceramic pegmatites as well as numerous occurrences of nickel, copper, tungsten, molybdenum, gold, silver and diamonds.

Seven ore (ore-bearing) camps are distinguished in this TMZ with their clear conjunction to the metamorphic-igneous rock complexes.

In the central part of the zone, occupied by Saltychanskiy Dome, two major camps are distinguished: Andriivsko-Elyseivskiy camp of ceramic pegmatites divided into Elyseivske and Andriivske fields; Novosilskiy platinum-copper-nickel-bearing camp with closely-spaced copper and nickel occurrences confined to the mafic-ultramafic rocks of Novosilska Association, and geochemical specialization marked by increased platinum-group element concentrations.

In the envelope of Saltychanskiy Dome, where potassium ultramafites and lamproites of Kolarivskiy Complex are widely developed, the diamond occurrences are found which are combined in Lozovatskiy and Komyshuvatsko-Konkskiy diamond-bearing camps.

In Lozovatska Anticline Krushanly-Korsatskiy iron-ore camp is distinguished; its metallogenic features are defined by development of the iron-ore economic stratified deposits and occurrences, as well as nickel occurrences.

Chernigivskiy apatite-rare-earth-rare-metal and Sorokynskiy gold-rare-earth-rare-metal ore-bearing camps are related to the linear tectono-magmatic structures of Zakhidnopryazovska TMZ. Particularly, Chernigivskiy ore camp includes large Novopoltavske deposit and Begim-Chokratske apatite occurrence; both are confined to carbonatites of the rare-earth-rare-metal specialization.

Rare-metals and gold deposits are known in Sorokynskiy ore camp. Occurrences of rare-earth metals, copper, lead, silver are encountered, as well as staurolite deposit (fluorspar substitute in ferrous metallurgy).

Metasomatic rocks, abundant in Zakhidnopryazovska TMZ, are accompanied by molybdenum, tungsten, rare-earth element and rare-metal occurrences.

From the west and east Zakhidnopryazovska TMZ is surrounded by Orikhivsko-Pavlogradska and Tsentralnopryazovska TMZs respectively.

Paleo-Proterozoic iron-ore deposits and occurrences define metallogenic features of Orikhivsko-Pavlogradska TMZ. In addition, occurrences of tungsten, rare-metals, rare-earths and nickel are encountered in the southern part of the zone.

Metallogenic features of Tsentralnopryazovska TMZ are defined by metamorphogenic graphite deposits and iron-ore occurrences formed in Neo-Archean metallogenic epoch. The tungsten occurrences related to plagiogranites of Shevchenkivskiy Complex are also ascribed to the latter epoch. In addition, rare-earth deposits and copper, gold and diamond occurrences are known in the zone.

In total, 115 deposits and occurrences (annexes 3, 4) are encountered in the crystalline basement in the territory of map sheet L-37-VII (Berdyansk); by mode of their formation metamorphic, magmatic, metasomatic and residual (weathering crust) genetic types are distinguished. In Meso-Cenozoic platform cover 42 sedimentary deposits and occurrences (annexes 1, 2) are found, of which the most important ones include placer gold deposit and numerous deposits of construction materials.

Description of mineral deposits and occurrences is given below for particular types of mineral resources.

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Combustible minerals Gaseous combustible minerals Natural gas Flammable gas occurrences are encountered in Berdyanska sandbank (IV-4-113)3 and in the area of

Orlivka village (IV-1-107). They are confined to the Cimmerian sands and sandstones, Lower Sarmatian clays and Upper Cretaceous sands, sandstones, limestones and marls. Occurrences are located in the northern slope of Prychornomorska Depression filled with Meso-Cenozoic sediments up to 1000 m thick. By chemical analysis data, gas is mainly methane, in some cases hydrogen predominate.

Yield of the flammable gas is low, 0.06 m3/hour in average, except occurrence at Orlivka village where gas yield is 0.5-1.0 m3/hour. Occurrences are not studied.

Solid combustible minerals Brown coal Brown coal in Veselovskiy occurrence (I-1-9) is confined to the Eocene sequence of sands and clays

which fill up Stulnivska Depression. It is located in the area of Vesele and Stepove villages. The bodies are sheet- and lens-shaped with horizontal or flat bedding. Just one bed is encountered. It thickness increases from the mold periphery to the centre from 1.0 m (in the north) and 3.0 m (in the west) to 7.0-8.6 m (in the centre). The coal ash content is 27.8-30.1%, volatiles – 35.4-54.8%, heating value – 4074-6417 calories. The depth varies from 48.5 to 66.6 m. Occurrence is not studied, and in view of its low size (3.5 km2) it is of no value so far.

Metallic mineral resources Ferrous metals Iron ores Iron-ore deposits and occurrences are subdivided into some genetic types by the forming conditions and

age of mineralization. The ferruginous-siliceous rocks of various metamorphic degrees are most widespread in the area; litho-stratigraphic factor provides the major control of ore mineralization.

Beside that, in some places of the area the iron-ore occurrences in weathering crust after crystalline rocks and in Meso-Cenozoic sedimentary sequence are known.

By composition and structure-texture features the iron ores of crystalline basement include two technological types: easy-beneficiating magnetite and medium-beneficiating silicate-magnetite quartzites.

In easy-beneficiating magnetite quartzites magnetite and quartz comprise the major minerals with minor opaque minerals.

Magnetite iron content in magnetite quartzites varies in the range 28-38% in average being decreased to 24-28% in the ores due to dilution by barren rocks.

Characteristic features of easy-beneficiating magnetite quartzites include magnetite grains easy separation which is started at the ore crushing to 1 mm and is completed with full separation at crushing to 0.074 mm, and high quality of concentrate with iron content 70-72.25% which is obtained by two-stage scheme of magnetic beneficiation.

In case of silicate-magnetite quartzites, the magnetite iron content in the ores is much less coupled with high content of opaque minerals and their intergrowth with magnetite and quartz. The latter feature negatively affects the technological properties of ores providing low separation of magnetite grains and low quality of concentrate with iron content in the range 65-68%.

The ores of economic value are related to Paleo-Proterozoic Dibrovska Suite and Neo-Archean Demyanska Suite of Tsentralnopryazovska Series. 3 Hereafter, indices in parentheses provide location of mineral deposits and occurrences in the maps where numbers in Roman comprise map left-border layout, first Arabic number – map top-border layout, and second Arabic numbers indicate the objects themselves (Translator note).

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The iron-ores associated with Dibrovska Suite are developed in Kuksungurske deposit and Inzivskiy and Orlivskiy occurrences located in Kamyanomogylskiy iron-ore camp of Orikhivsko-Pavlogradska LTZ.

Kuksungurske deposit (III-1-77) is the leading one in the mentioned camp. Deposit is prepared for economic exploitation and ore reserves are approved by SCMR of USSR in 1980 for open-cast mining to the depth 500 m below the surface. Overburden hard rocks can be used for the crushed-stone manufacturing [76].

The iron-ore batch is composed by 85-95% of cummingtonite-magnetite quartzites with medium-fine-banded structure and essential predomination of magnetite and quartz. The barren rocks include biotite and garnet-biotite gneisses, low-ore and non-ore magnetite-pyroxene quartzites and granites that form thin interbeds and lenses and dilute the magnetite iron content in the ore to 25.4% in average. In the upper part of iron-ore batch the extensively granitized garnet-sillimanite-cordierite-graphite-bearing biotite gneisses are developed which at the column top (3-5 m) are substituted by fine-grained mafic gneisses and sideroplesite quartzites. Thickness of the batch varies from 5-15 to 200 m.

In deposit, the rocks are observed in the bend-shaped narrow fault-side monocline; the strike varies from latitudinal (over 4 km distance in the southern part) to sub-longitudinal (over 3 km distance in the north).

Major ore reserves are located in the Central block where iron-ore body is exposed at the surface under sub-latitudinal strike over the distance 1700 m with average thickness 100 m. The dipping varies from northern at the angles 65-75o in the west through vertical in the body centre to the southern one at the angles 75-85o in the east.

The ore body in Meridional block adjoins the Central block being extended in the northern direction over the distance 1260 m at the average thickness 85 m with dipping to the west at the angles 65-85o. In sulphidized quartzites and host garnet-biotite gneisses of Meridional block the gold is encountered with the grade up to 1 g/t by spectrometry data and 0.228 g/t by fine assay data [78].

The Western block is located at the junction of the latitudinal and sub-longitudinal monoclines with rock dipping to the north-west at the angles 60-70o. The ore body length is 350 m at the thickness up to 230 m.

Interim block is located in between the Central and Western ones being separated from them by faults. This block strongly differs from the others by geology. The ores are observed in thin beds separated by thick gneiss layers; between the iron-ore and garnet-bearing batches the interbeds of carbonate rocks appear – marbles, calciphyres and graphite schists with high graphite carbon content (5.79-10.38%). The length of the block is 900 m at the thickness up to 120 m; rock dipping is to the north and north-west at the angle 45o.

The columns of Orlivskiy-1 (IV-1-155) and Inzivskiy (IV-1-151) occurrences are similar to ones in the Western block of Kuksungurske deposit at the lower thickness of iron ores and higher thickness of overburdern sedimentary rocks that essentially suppresses their perspectives. In the Inzivskiy occurrence the tungsten and uranium mineralization is encountered by drill-holes within cataclased and silicified rocks. The tungsten content (by spectrometry data) varies is the range 0.01-0.3%, and uranium content (chemical analysis) attains 0.08%. Mineralization is accompanied by increased concentration of copper – up to 0.2% and lead – up to 0.005%. Thickness of ore intervals varies from 2.8-5.8 to 71.0 m [59, 95].

The second mining-important object is Korsatske deposit (III-1-79) of iron ores confined to Demyanska Suite of Tsentralnopryazovska Series. Deposit is located in the far west of Zakhidnopryazovska TMZ.

Two sub-longitudinal strips of ferruginous quartzites are distinguished in the deposit: western (first-fifth hills) and eastern (sixth and seventh hills). The first one comprises the large up to 300 m thick lens of massive quartz-magnetite quartzites extended over 3 km at the steep dipping to the west-south-west. In ferruginous quartzites Fe2O3 content is 44%, FeO – 2%; in low-grade ones – 20% and 5% respectively.

The eastern strip (in 500 m from western) is also traced over 3 km. Several 40-50 m thick layers of ferruginous quartzites are distinguished separated by garnet-biotite, sillimanite-biotite and biotite gneisses beds. In this strip ferruginous quartzites are more fine-grained, banded-textured, and hypersthene-bearing. Content of Fe2O3 is 48%, FeO – 1-1.5%.

At the sixth hill the bodies of high-grade hydrogoethite-martite ores from some centimeters to 4-5 m thick with more than 50% of iron content are associated with the weathering crust after ferruginous quartzites. This part of deposit is already mined to the depth of 45 m in the beginning of XX century.

In comparison to Kuksungurskiy type, in Korsatski ores magnetite content is lower and it is in the intergrowth with opaque minerals which abundance essentially increases. In spite of this, the ore bodies Korsatske deposit are economic due to close-spaced reserves and much less overburden rocks. In addition, prospecting interest is provided by encountered zones of cataclasm, sulphidization and silicification where silver content is determined by fine assay from 12 to 140 g/t at the gold grade variances from 0.016-0.7 up to 3.0 g/t (fine assay too) [78].

In Temryutsko-Troitskiy iron-graphite ore camp of Tsentralnopryazovska TMZ the magnetite ores of Temryukska Suite are observed in minor bodies (occurrences I-4-24, II-4-62, II-4-68, III-4-146) within

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amphibole-pyroxene mafic gneisses and graphite-bearing gneisses [70, 71, 100]. The ores are two-pyroxene-magnetite with average magnetite iron content up to 25.5%.

In Zakhidnopryazovska TMZ occurrences of ferruginous quartzites in the mafic and ultramafic rocks are known in Kainkulatska Sequence of Zakhidnopryazovska Series (І-3-18, І-3-19, ІІ-1-31, ІІ-1-32). The ores occur in thin (up to 10 m) bodies of limited length (first hundreds of meters); average magnetite iron content is up to 30% [66, 71, 91, 95].

Occurrences are not studied and in view of their small scale are considered to be not economic. In addition, in the course of geological mapping [59] Orlivskiy-2 (IV-1-155) and Lunacharskiy (IV-1-

157) occurrences of siderite in kaoline weathering crusts are discovered in the south-western and southern parts of the map sheet. Thickness of the bodies varies from 2.4 to 10.9 m; their depth is 130 and 300 m below the surface. Soluble iron content is 16.3-20.6%. Besides iron, in these occurrences increased titanium content is determined in relation to ilmenite (4.7-30.4 kg/m3). Due to the significant depth eluvial bodies are not economic.

In the sedimentary sequence iron is related to siderite in Cretaceous sediments and goethite-hydrogoethite ores of Kerchenskiy type in Cimmerian rocks.

Occurrences of siderite ores (IV-2-108, IV-3-111) in the southern part of map sheet are weakly studied [59]. Due to the significant they are considered to be not economic.

Occurrence in Stulnivska Depression (I, II-1-10) is related to 0.7-21.0 m thick horizon of siderite-enriched glauconite-quartz sands, sandstones and clayey spongolites in Campanian sandy sequence. Soluble iron content varies from 12 to 40%. Depth is in the range 59.4-219.2 m below the surface [91].

Occurrence of Kerchenskiy-type ores (IV-1-109) is located in the southern part of the map sheet [59]. It includes three beds of iron-enriched sandstones separated by clay and sand interbeds. Thickness of the beds varies from 0.2 to 21 m. Goethite is iron-concentrator, together with chamosite and hydrogoethite it forms concentrically-zoned oolites 1-2 mm in diameter (5-36%). Siderite is contained in limited amount comprising cement in oolites or feldspar-quartz sands. Soluble iron content varies from 15.1 to 51.3%. Ore bodies occur at the depths 40-100 m being aerially distributed over more than 60 km along the Azov Sea coast to the south of Lozuvatka, Dmytrivka and Osypenko villages. Occurrence is weakly studied.

Non-ferrous metals Titanium The mineral sand placer occurrences are known in the map sheet territory: ilmenite – Chernigivskiy (I-

1-3) and ilmenite-monazite – Gondzhugovskiy (III-4-123), Nogayskiy (IV-3-126), Novopetrivskiy (IV-4-128) and Berdyanskiy (IV-4-133).

The first one is confined to Upper Cretaceous sands which fill up Chernigivska Depression. The sands lie over Lower Cretaceous sediments or crystalline rocks and are overlain by 3-60 m thick Paleogene, Neogene and Quaternary sediments. Occurrence is not studied; it belongs to the sedimentary deposits of platform depressions.

Remaining occurrences are ascribed to the modern coastal-marine sediments of Azov Sea. Placer length varies from 0.5 to 2.0 km, width – 5-7 m. Thickness of productive sands is 0.1-1.5 m. Ilmenite content is 2.42-150 kg/m3, monazite – 0.073-2.0 kg/m3, zircon – 0.1-0.156 kg/m3. Occurrences are not studied and their perspectives are not defined.

Copper Copper occurrences are related to the brecciation zones of Obitochnenskiy Complex diorites and

sulphidized metamorphic rocks in Zakhidnopryazovska TMZ. Zubivskiy occurrence (II-2-33) is located in the upper course of Tokmak River. It is confined to

metasomatically altered (albitized, K-feldspatized, chloritized, epidotized and prehnitized) diorites of Obitochnenskiy Complex at the contact with gneisses of Kainkulatska Sequence. Mineralization comprises irregularly-distributed malachite which forms the aggregates up to 2 cm in size, and limonitized sulphides. Copper content varies in the range 0.12-0.67% [105]. Thickness of the zone is 25.9 m, strike – north-east along 0.5 km, dipping to south-east at the angle 65o.

Similar figures are also observed in Yuryivskiy occurrence (III-2-143) where at the surface copper content (by spectrometry) is up to 1%, and low-grade malachite mineralization is encountered in metasomatically altered diorites of Obitochnenskiy Complex [117].

Fairly interesting copper occurrence Botsman Gora (II-4-65) is located on the right bank of Berestova River to the south of Vyboeve village. Malachite and azurite as well as fine dissemination of covellite and

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chalcopyrite are encountered in the crushing zone after secondary quartzites. Zone thickness is up to 2 m, copper content – 1.46%, zinc – 0.02%, lead – 0.002 %.

Described occurrences are prospective for the gold-quartz-sulphide mineralization. Copper occurrence of Gusarka gully (I-3-17) in metamorphic rocks is confined to biotite gneisses of

Dragunska Sequence; up to 1% of copper content and 0.1% of zinc are determined by spectrometry [66, 71]. Perspectives of occurrence are not clear.

Nickel, copper The complex nickel-copper occurrence of Bila gully (II-2-35) is encountered in ultramafic rocks of

Novosilska Association in Zakhidnopryazovska TMZ. Sulphidization is found in zones of brecciation, cataclasm, with extensive tremolitization of peridotites

and hornblendites. Sulphides and malachite are major minerals of ore. Nickel content varies in the range 0.1-0.47%, copper – up to 1.51%. Gold is also determined – up to 0.05 g/t [103]. Thickness of ore intervals is 3-4 m.

Occurrence is weakly studied and is thought to be perspective for gold and platinoids mineralization. Nickel Nickel occurrences (IІ–3-44, ІІ-3-46, ІІ-3-53, ІІ-3-61) are encountered in ultramafic rocks of

Novosilska Association in Zakhidnopryazovska and, in lesser extent, Orikhivsko-Pavlogradska TMZs. Besides nickel, in occurrences often cobalt is noted under non-economic content; by these reasons cobalt is not considered herein.

Sulphidization is found in zones of metasomatically altered peridotites and hornblendites. Major minerals of ore include pentlandite, pyrrhotite, chalcopyrite, valeriite, cubanite and pyrite. Nickel content varies in the range 0.1-1.2%, copper – up to 1.51%. In some occurrences (II-3-53, II-3-61) are determined: gold – up to 0.15 g/t, silver – up to 10 g/t [104], and platinum – up to 0.2 g/t [97]. It should be noted that the scale of mineralization and content of associated valuable components characteristic for this association are weakly studied.

Some occurrences are ascribed to ones of unclear perspectives due to weak study: occurrence (IV-1-156) in meta-ultramafic rocks of Dibrovska Suite with nickel content 0.05-0.5% [59], and occurrence (III-4-104) in meta-basites within granodiorites of Osypenkivskiy Massif with nickel content 0.26-0.46% [58].

Rare metals Tungsten Specialized works for tungsten in the map sheet area were not conducted although the mapped rock

complexes unequivocally suggest for possible occurrence of tungsten and molybdenum economic concentrations. Firstly, this is a wide development of intermediate rocks (diorites, granodiorites, gabbro-diorites) favourable for stockwork-type molybdenum, copper and tungsten mineralization, and, secondly, development of fault tectonics and associated host rock metasomatic alteration.

Tungsten, together with other metals, is encountered in the zones of metasomatic alteration after the rocks, different in genesis, composition and age. In occurrences (I-2-141, II–3-54, II–4-74) tungsten is related to plutonogenic-hydrothermal rocks of gold-sulphide-quartz association confined to the north-west-trending zones of cataclasm and silicification. Tungsten content is up to 3% by spectrometry data. By mineralogical study scheelite is determined in amount from single grains up to 5.12-22.4 g/t. Besides this, silver – from 9 to 20 g/t and gold – up to 0.185 g/t are determined. Occurrences are not studied but perspective.

In Kirovskiy occurrence (II-4-69) within pyroxene-magnetite quartzites of Temryukska Suite the 18.4 m thick batch of cataclased pyroxene-garnet-quartz rocks with fine scheelite dissemination (up to 400 g/m3) is defined. Tungsten content varies from 0.06 to 0.1%. Mineralization is located close to the contact of plagiogranites with carbonate rocks. It is accompanied by sporadic malachite mineralization with copper content up to 0.67%. Occurrence is perspective and belongs to the skarn quartz-scheelite-type mineralization of scheelite ore formation [71].

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Molybdenum Dolynskiy molybdenite occurrence (III-2-83) is characteristic for molybdenum-porphyry ore formation

and is confined to the silicified intervals (thickness – 1.0 m; 1.3 m) in diorites of Obitochnenskiy Complex [117]. Molybdenite is observed in fine flakes and aggregates up to 1 mm distributed along fractures in quartz. Molybdenum content (by chemical analysis) varies in the range 0.084-0.232%. Occurrence is perspective.

Another important source of molybdenum can be graphite bodies of the carbonaceous formation. In the studies of graphite deposits [63, 77] it was noted the molybdenum content in the range 0.07-0.2% (by spectrometry data); this corresponds to the mineralization of economic value.

Niobium, tantalum, lithium These metals are contained in the complex ores of pegmatite deposit and in occurrences of rare-metal

formation being characteristic for Pivdennosorokynske gold-rare-earth-rare-metal ore field (B-4-2) located in the south-eastern part of Zakhidnopryazovska TMZ (see “Scheme of metallogenic zonation”).

In the mentioned ore field Kruta Balka deposit (III-4-99) of lithium pegmatites is explored [58, 84]. Besides Li, pegmatites also contain economic concentrations of Nb and Ta.

Rare-metal pegmatites are located mainly in meta-ultramafites, rarely in granodiorites, mica and amphibole schists. In the first case pegmatites are of quartz-albite-microcline composition, and in the second one – quartz-albite with muscovite, rarely biotite.

The veins are zoned. The central part is composed of coarse-block quartz with rare coarse crystals of pink microcline. In the footwall quartz core is gradually replaced by the zone of block light-pink or grey microcline. In places between these two zones the transitional zone is developed; it is composed of fine-flaky muscovite or is enriched in bunches and batches of its coarse crystals. In other places this transitional zone is muscovite-quartz-albite or essentially albite or cleavelandite in composition while vein marginal parts are composed of quartz and albite.

Three ore-bearing zones are distinguished in deposit: lower, middle and upper. The upper zone is observed at the hypsometric level from +36 to -36 m. Two pegmatite veins are encountered, 7.2-25.5 m and 4.1-5.9 m thick, traced to the depth over 240 and 60 m respectively. Concentration of rare metals increases by dipping and varies in the range (%): Li2O – 0.008-4.0, Ta2O5 – 0.001-0.268, Nb2O5 – 0.001-0.036, Cs2O – 0.001-0.041, Rb2O – 0.006-0.094. Ore minerals include spodumene, columbite, tantalite, cassiterite, sulphides.

Middle zone is observed at the hypsometric level from +15 to -160 m. One pegmatite body is encountered, from some to 70 m thick, plunging to the south-east at the angles 10-15o; it is traced over 220 m. Metal content (%): Li2O – 0.02-6.55, Ta2O5 – 0.001-0.176, Nb2O5 – 0.001-0.06. Ore minerals: spodumene, tantalite, niobotantalite, triphylite-lithiophyllite, sulphides.

Hypsometric level of the lower zone varies from -97 to -195 m; it is traced over the distance of 180 m from north-west to south-east at width 70 m. Some sheet-like pegmatite bodies, from 3 to 30 m thick, slightly inclined to the east are encountered. Metal content (%): Li2O – 0.02-1.43, Ta2O5 – 0.001-0.018, Nb2O5 – 0.001-0.009, Cs2O – 0.001-0.033. Ore minerals: spodumene, columbite, niobotantalite, tantalite, tapiolite, microlite, eschynite.

In the pegmatite body No. 1 the beryl crystal up to 2 cm in size is found. The finding is of no practical value.

The wasteless beneficiation technology is developed for the ores of this deposit to get the rare-metal concentrates and associated feldspar, quartz and mica production.

In the studies of rare-metal mineralization increased gold concentrations are encountered in the zones of sulphidization and brecciation of metamorphosed mafic and ultramafic rocks (gold grade attains 3.2 g/t). Since Kruta Balka deposit is in the same tectonic setting as Surozke gold deposit adjacent from the south-east, it should be noted that both deposits can be studied together aiming their subsequent complex development.

Niobium, tantalum Both metals are contained in two pegmatite occurrences of rare-metal formation and one placer

columbite occurrence. Osypenkivskiy (III-4-106) and Sadoviy (III-4-148) pegmatite occurrences are located in

Pivdennosorokynske gold-rare-earth-rare-metal ore field (B-4-2). Host meta-ultramafites of Olginska Suite and granodiorites of Shevchenkivskiy Complex are cut by the series of vertical microcline, microcline-albite and albite pegmatite bodies of Saltychanskiy Complex. Thickness of pegmatite bodies varies from 1.1 to 20-30 m.

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Rare-metal content in Sadova site: Ta2O5 – 0.0075-0.158%; in Osypenkivskiy occurrence: Nb (by spectrometry) – 0.2%.

In both occurrences increased gold content is encountered. Gold content of quartz-tourmaline rocks in Sadova site is 0.1-1 g/t.

Since both occurrences are located in the same tectonic setting and close to Kruta Balka deposit, they are thought to be perspective for rare-metal mineralization.

Columbite placer occurrence (III-2-119) is found in deluvial sediments in the right slope of Chokrak River, close to ceramic pegmatite deposit Mogyla Zelena where the samples are known with columbite content up to 1.98 kg/m3. Thickness of the placer is 1.3 m, columbite content – up to 0.2 kg/m3. Occurrence is of no economic value.

Rubidium, niobium, tantalum Rare-metal occurrences of Dovzhyk gully (III-4-96) and Blakytni Skeli (III-4-102) are encountered in

aplite-like granites and pegmatites of Saltychanskiy Complex located in metamorphic rocks of Osypenkivska Series. Ore body thickness is 0.2-1.5 m, extension is sub-latitudinal, dipping is steep to the south.

Columbite content in biotite schists of Dovzhyk gully (III-4-96) is 860 g/m3. In aplite-like granites are determined (by spectrometry): Rb – 0.41%, Nb – 0.145%.

By chemical analysis, the metal content in pegmatites of Blakytni Skeli (III-4-102): Ta2O5 – 0.017%, Cs2O – 0.003%, Rb2O – 0.07%. By mineralogical analysis, the mineral content: columbite – 123 g/t, beryl – 227 g/t. Ore minerals: spodumene, columbite, tantalite. In meta-ultramafites gold (0.1-0.3 g/t) and silver (4.0 g/t) are determined.

Occurrences are located in the central part of Pivdennosorokynske gold-rare-earth-rare-metal ore field (B-4-2) and are considered to be perspective for rare-metal mineralization.

Rubidium, cesium Occurrence of Krymska gully (III-4-93) like all previous pegmatite objects of rare-metal formation is

located in Pivdennosorokynske gold-rare-earrth-rare-metal ore field (B-4-2). It is confined to albitite vein with columbite crystals up to 3 mm in size. Albitites are observed in meta-ultramafites of Olginska Suite where the zones of alkaline metasomatism are also known in other intervals. From spectrometry data, rubidium content is more than 0.1%, cesium – up to 0.055%. Increased concentrations are also determined (chemical analysis): Ta2O5 – 0.005%, Nb2O5 – 0.01%.

Occurrence is weakly studied and is perspective for rare-metal mineralization. Zirconium Zirconium occurrence of Saltychiya gully (II-2-36) is encountered in the bunch-shaped pegmatite body

(3 by 1.5 m) of biotite-quartz-plagioclase-microcline composition with zircon content 47.97 kg/t; associated minerals: thorite, apatite, pyrite and magnetite [104]. Occurrence is weakly studied.

Another Preslavskiy occurrence (IV-1-152) is located to the north-west from Preslava village and confined to metasomatically altered gneisses of Kainkulatska Sequence. Zirconium content is 0.5%; other elements: phosphorus – 10%, yttrium – 0.035%, and titanium – 4%. Occurrence is weakly studied, due to great depth (108 m) it is thought to be non-perspective.

Precious metals Gold Economic gold concentrations are encountered in relation with the gold-sulphide-quartz formation in

the zones of brecciation, sulphidization and silicification in crystalline rocks of various age and composition. In addition, gold is found in the sedimentary sequence of modern sediments.

By degree of metallogenic study Sorokynskiy gold-rare-earth-rare-metal ore camp (B-4) is distinguished where Surozke deposit (III-4-100) and some occurrences are encountered (II-3-48, II-3-58, III-4-103).

Surozke deposit is located on the right bank of Berdyanske water reservoir, on the both slopes of Sobacha gully. The host rocks include meta-komatiites, garnet-biotite schists and ferruginous quartzites of

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Olginska Suite (Osypenkivska Series) and ultramafic rocks of Sorokynskiy Complex. Five ore bodies are distinguished in deposit, from some centimeters to 1.5-2.0 m thick, located in thin (2-3 m) zones of cataclasm and milonitization, arranged en echelon in the zone of sub-latitudinal Skifskiy fault and in the endo-contacts of sub-vertical ultramafic dyke (50-100 m thick). Estimated gold grade is 1.4-12 g/t, and in the major ore body – 6.8 g/t. Increased gold grade (19-33.6 g/t) is observed in places of sulphide-quartz breccia development and in thin interbeds of chloritized and carbonatized tremolitites.

The ores are of gold-sulphide-quartz type. Most of gold (50-80%) is contained in cataclased quartz close to its contacts with sulphides, partially (5-15%) – in intergrowths with pyrite, pyrrhotite, chalcopyrite and magnetite, and remaining (10-30%) – in fractures of quartz with sulphides and other minerals. Large enough (up to 0.06-0.15 mm) gold particles are observed in quartz and partially also in sulphides; fine-dispersed gold (0.01-0.005 mm) is confined to pyrite and pyrrhotite aggregates.

Gold is high-fineness (926-933); traces of silver (6.63-7.34%) and Bi, As, Sb, Hg occur. Composite gold tellurides with Cd, Cu, Se are determined.

Ores of Surozke deposit, upon technological trials, are being beneficiated by gravity-flotation scheme with additional extraction of sulphide-associated gold (arsenopyrite, pyrrhotite, pyrite) by hydro-metallurgy and heap-leach cyanidation.

Deposit is studied to the depth 300 m. Formational studies conducted in deposit and other perspective sites of Sorokynska structure have

shown [5] that, without exceptions, all ore body intersections or highly-contrasted geochemical aureoles of gold and associated complex of micro-elements, are confined to the nearest exo-contacts of tonalite-plagiogranite formation massifs or the relict bodies of meta-rhyodacite formation with the rocks of meta-komatiite-tholeiite and schist-jaspilite-meta-tholeiite formation.

Geological setting of other occurrences in Sorokynske ore field is similar to that of Surozke deposit. Andriivskiy occurrence (II-3-48) is discovered in the zones of silicification and sulphidization of

ferruginous quartzites and meta-ultramafites with gold grade variations in the range 0.3-10 g/t. Sorokynskiy occurrence (II-3-58) is located in ferruginous quartzites where quartz veinlets with gold grade 1-3 g/t (gold spectrometry) and 0.932 g/t (fine assay) in association with silver (up to 20 g/t) are encountered.

Radyvonivskiy – Blakytni Skeli (III-4-103) gold, silver and copper occurrence is encountered in the contact zone of Olginska Suite amphibolites with granodiorites where extensive silicification and sulphidization are observed [114]. Gold is concentrated in vein quartz (up to 10 g/t), copper – in sulphides (0.24-1.45%). Accompanying elements include zinc – 0.06-0.6% and silver – 20-40 g/t. Ore zone is traced in the right bank of Berdyanske water reservoir from Blakytni Skeli ravine over more than 1300 m to the east.

Occurrences of Sorokynskiy ore field are perspective and require further studies. Berestovskiy gold occurrence (II-4-71) located in the right bank of Berestova River nearby the western

outskirt of Karla Marksa village is also prospective. Mineralization is confined to the fracturing zone of west-north-west extension adjoining Mykolaivskiy fault. Some 30-100 m thick bodies of muscovite-feldspar-quartz metasomatites (secondary quartzites or quartzitolites) are observed in the zone. In one of these bodies, 0.7-2.0 by 5 m in size, the bunches up to 25-30 cm across enriched in chalcopyrite, covellite and bornite are found; malachite, galena, molybdenite, bismuthine, sphalerite as well as native gold also occur. Native gold comprises elongated, hooked, branched, bar-like, and isometric, cavernous and cell-like particles 0.1-0.25 mm in size. Up to 40 gold particles are found in two samples. Gold fineness is 678-746.

In the zone, up to 500 m thick, extended over 1000 m, by geochemical data a range of similar ore bodies are distinguished, with thickness from 1.8 to 4.0 m. Occurrence is perspective and requires further studies.

In the sedimentary sequence, the gold encountered in Holocene alluvial sediments of Novovasylivska site (III-4, IV-4-127) is of practical value. The placer occurrence is located in Berda River valley, from the southern outskirt of Osypenko village to the river mouth, in the area of Novovasylivka, Staropetrivka and Novopetrivka villages. In the samples about 7-11 kg weight, the gold laminae 0.02-0.5 mm in size in amount of 11-110 mg/m3 are determined. The placer is not studied.

Silver Commonly silver comprises accompanying element in occurrences of gold-sulphide-quartz formation.

In some occurrences silver achieves specific value at the concentrations in excess of 30 g/t. In Balka Glyboka occurrence (III-3-90) epidotized and silicified rocks at the contact with the dyke of

feldspar hornblendites contain up to 53 g/t of silver with accompanying gold grade from 0.1 to 0.6 g/t. In Balka Kruta occurrence (III-4-98) in the silicification zone silver grade attains 600 g/t (fine assay). In

addition, lead (12%) and bismuth (0.06%) are determined. In pegmatites at this site the silver grate is estimated to 26 g/t.

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Silver occurrences are prospective and require further studies aiming discovery of gold-quartz-sulphide mineralization.

Rare-earth metals Increased concentrations of rare-earth elements are characteristic for the map sheet territory in relation

to the development of alkaline and sub-alkaline igneous rocks. Mineralization includes the following genetic types: rare-earth granites, rare-metal-rare-earth

pegmatites and rare-earth metasomatites. Mogyla Saltychiya orthite occurrence (II-2-39) is related to the rare-earth granites of Saltychanskiy

Complex. The mineral distribution over the rock is regular enough and its content attains 1%, in places more [117]. In Malynivskiy occurrence (II-3-142) in the up to 3 m thick vein of fine-grained leucocratic granite orthite content attains 0.8 kg/m3 [104]. In view of the wide development of Saltychanskiy Complex in the central part of Zakhidnopryazovska TMZ, aforementioned occurrences are prospective and require further studies.

Deposit (I-4-22) and occurrences (I-4-20, I-4-23, II-3-50) of cerium lanthanoids in Zakhidnopryazovska and Tsentralnopryazovska TMZs, as well as yttrium occurrence (II-3-47) in Sorokynska tectonic zone comprise the pegmatite type of mineralization.

Mineralization is observed in the lens-like 0.6-7 m thick north-west-trending pegmatite bodies of Kamyanomogylskiy Complex. Ore components include monazite (from 12 to 25 kg/m3) and zircon which content in Mogyla Visla deposit (I-4-23) is 10-15 kg/m3 [70, 72, 73].

Yttrium occurrence (II-3-47) is encountered in plagioclase pegmatite. Thickness of the vein is 0.7 m with yttrium content 0.35%. Rare-earth mineralization is represented by xenotime [104].

Occurrences of light lanthanoids (II-1-30, IV-1-152) and yttrium (I-1-139) are encountered in Orikhivsko-Pavlogradska and Zakhidnopryazovska TMZ in relation with the rare-earth metasomatites.

Petrivskiy yttrium occurrence (I-1-139) is considered to be perspective with increased yttrium content – 0.1% [61].

Occurrence Balka Krushanly (II-1-30) is intersected by drill-hole at the depth 218-224 m within extensively K-feldspatized and carbonatized biotite-pyroxene gneisses; by spectrometry lanthanum content is 0.5%, cerium – 0.1% [105]. Occurrence is weakly studied.

Preslavskiy occurrence (IV-1-154) is encountered in cataclased quartz metasomatites with drill-hole intercept of 5 m. Lanthanum content is 0.3%, cerium – 0.2%. Occurrence is not studied.

Non-metallic mineral resources Non-ore raw materials for metallurgy Refractory raw materials C l a y Petrivske deposit (III-1-78) is located in the right bank of Korsak River in the central part of Petrivka

village. Deposit includes kaolineous, white, often with light-grey, ochre-yellow and black shades, sandy clays of Novopetrivska Suite. Two 2-4 m thick clay layers are distinguished which were mined for manufacturing the high-quality refractory bricks.

S e c o n d a r y k a o l i n e Secondary kaolines of Novopetrivska Suite are developed in Chernigivska and Stulnivska depressions.

Mineral objects include Vladivske (Richne) deposit (I-1-8) and Novogrygorivske occurrence (I-2-11). They lie at shallow depth beneath Quaternary loams, in places (Begim-Chokrak River and Biloglynka gully) – above the basis of erosion. Thickness of kaoline bodies is 5-10 m and at Vladivka village only it increases to 21 m. Kaolines have refractory properties.

S i l l i m a n i t e a n d c o r u n d u m Dragunske deposit of sillimanite and corundum (I-2-12) is located in the northern part of map sheet in

the upper courses of Mokra Konka and Sukha Konka rivers.

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The 150-200 m thick batch of biotite, garnet-biotite, sillimanite-biotite and sillimanite-garnet-biotite gneisses is distinguished in the deposit. The rocks are ascribed to Archean Lower Dragunska sub-sequence which contains four 0.5-10 m thick layers of sillimanite- and corundum-bearing mafic gneisses. The rocks are traced over 300-400 m and contain 0.8-5.3%, in places up to 8% of sillimanite, and up to 15% of corundum. The latter is observed in the crystals from 0.1-0.5 to 5-7 mm in size. Major rock-forming minerals (%): microcline – up to 50, plagioclase – 5-20, biotite – 25-40; in places spinel (up to 1-10) and quartz (up to 1) occur [123].

Deposit is explored with economic reserves but was not mined yet. Flux raw materials S t a u r o l i t e In the map sheet area Osypenkivske staurolite deposit (III-4-97) is evaluated in the course of

prospecting works [101]. Deposit is confined to the central part of Sorokynska tectonic zone and is located in the western bank of Berdyanske water reservoir, in between Kryta and Krymska gullies. Staurolite-bearing schists are observed in five layers, from 10 to 250 m thick that occur in Krutobalkinska Suite gneisses of Osypenkivska Series. The rocks are traced in the north-western direction over 500-2700 m; rock dipping is south-western at 62-82o. Staurolite content in the schists varies from 2 to 40%. Besides staurolite, in various schist varieties biotite, muscovite, garnet and andalusite also occur. Reserve estimation is performed to the horizon 200 m. Developed beneficiation scheme allows receiving the staurolite, garnet and biotite concentrates. Deposit is out of production.

Chemical raw materials Agro-chemical raw materials A p a t i t e Apatite ores are known mainly in Chernigivskiy ore camp where are located the only Ukrainian

explored Novopoltavske apatite deposit (I-1-140) and Begim-Chokratskiy occurrence (II-1-29). In geological respect these objects are confined to Chernigivska and Begim-Chokratska fault-side

tectono-metasomatic zones sealed with the alkaline-ultramafic carbonatite formation rocks of Chernigivskiy Complex [13, 14, 28, 90].

Apatite mineralization is related to carbonatites of variable composition both by major minerals (calcite, dolomite, apatite, magnetite, phlogopite and olivine) and minor and accessory minerals (pyrochlore, fergusonite, columbite, beidellite and monazite).

Apatite, besides phosphorus, also contains rare earths with cerium-group lanthanoids strong predomination, fluorine and strontium. Ten major and some less thick elongated, lens-shaped ore bodies are distinguished. The ore bodies are overlain by sedimentary rocks up to 85 m thick.

Apatite is being well preserved during carbonatite weathering and is accumulated in the weathering crust. The latter comprise the transitional stage suggesting for the short-term weathering.

The ore beneficiation scheme is developed providing economically efficient apatite concentrate manufacturing. It prescribes the complex concentrate of rare and rare-earth metals and magnetite. Deposit is out of production.

In Begim-Chokratskiy occurrence eight ore bodies are encountered, from 0.1 to 12 m thick with sub-longitudinal strike and southern dip at the angles 45-55o. Thickness of weathering crust is 4.0-11.0 m. Overburden rock thickness is 2.5-4.5 m. The composition and concentration of ore elements are similar to those of Chernigivske deposit. Occurrence is perspective and requires further studies.

High apatite content is observed in amphibolites of Saltychiya village occurrence (II-2-37) encountered within medium-grained plagio-migmatites of Shevchenkivskiy Complex. Visible thickness is 2-3 m; apatite content attains 15-20%. Perspectives are not clear.

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Non-metal ore commodities Abrasive raw materials T e c h n i c a l d i a m o n d Diamond occurrences are concentrated in the envelope of Saltychanskiy Dome. They are confined to

the lamproites (potassium ultramafites) of Kolarivskiy Complex and the modern alluvial sediments. Lamproites are observed in the stock- and pipe-like bodies, from 10 to 500 m in size, and in the first

meters thick dykes that occur within igneous and metamorphic rocks of various age. Major diamond findings are known from three occurrences (III-1-75, III-2-88, III-2-89) in Kolarivskiy

(B-6-1) and one occurrence (III-3-91) in Andriivske (B-6-1) ore-bearing fields. In the first case the diamond crystals and fragments are found both in the hard rocks and in re-deposited

weathering crusts after lamproites developed in the “Mriya” pipe and anomaly No. 4 [103]. Diamond crystals are cube-octahedron in shape, yellow, yellow-green and grey-green colour and small size (0.01-0.25 mm).

In Andriivskiy occurrence (III-3-91) confined to 6 m thick, north-west-trending, sub-vertical lamproite dyke, just a single semi-transparent diamond fragment 0.15 mm in size is found.

It is characteristic for the lamproites of Andriivsko-Lozovatskiy diamond-bearing area the complete lacking of satellite minerals suggesting for new formational type of diamond-bearing rocks. Occurrences are prospective and require further studies.

In Zakharyivska diamond-bearing site, in Velyka Ternova gully occurrence (II-4-63), in two samples (5.6 and 6.7 kg) the crystal and the fragment of ice-coloured diamond 0.35 by 0.3 and 0.65 by 0.375 mm in size are found.

Komyshuvatsko-Konkskiy diamond-bearing camp includes Mokrokonkska ore-bearing site with Mokra Konka River occurrence (I-2-115) where 0.2 mm green diamond crystal together with pyrope and picroilmenite crystal is found in alluvial sediments, and Komyshuvatska site of lamproite magmatism development.

Sedimentary diamond occurrence (IV-4-138) is confined to the “beach” sands in the western part of Berdyanska sandbank; three crystals in the 460 kg sample are found [58]. In view of unfavourable geomorphology of the Azov Sea coastline this occurrence is considered to be not prospective.

Electric- and radiotechnical raw materials G r a p h i t e Graphite bodies are concentrated in Temryutsko-Troitske graphite-bearing field of

Tsentralnopryazovska TMZ. By geological prospecting works four deposits – Temryutske (I-4-25), Karatyutske (I-4-26), Sachkynske (II-4-64), Troitske (II-4-66), and two occurrences (I-4-28, II-4-72) are evaluated in the strip of Temryutska Suite graphite gneisses of Tsentralnopryazovska Series extended over 25 km along the western limb of Berestovska syncline and exposed along Temryuk, Karatyuk, Berda and Berestova rivers.

Deposits contain significant reserves of graphite ore for the open-cast mining that occur in the bodies from 3-5 to 230 m thick extended over the distance from 500 to 3500 m. Graphite carbon content in ore beds is 2.4-4.1%. The ore beds are separated by 15-80 m thick amphibole gneiss interbeds with low graphite content; in places these interbeds pinch out and graphite gneisses merge into the single thicker ore body. The ore bodies are also irregular in composition: in places carbon content is much higher and in other places it drops to one and even less percent.

The ores are easy-beneficiating by the technological scheme of Mariupol plant “Markograf”. Reserves are approved by category C2 and prognostic resources – by categories P1 and P2 to the depth 200 m. At present the ores are of no practical value.

Graphite occurrences are weakly studied. As it was mentioned above, economic concentrations of molybdenum and anomalous silver contents are encountered in graphite beds suggesting for the needs in further studies.

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Adsorptive raw materials V e r m i c u l i t e In the map sheet area Andriivske (II-3-45) and Radyvonivske (III-4-100) deposits and Temryutskiy (I-

4-21), Kirovskiy (II-4-70), Berestovskiy (II-4-73), Kolarivskiy (III-2-87), Mykolaivskiy (III-4-94) and Olginskiy (III-4-149) vermiculite occurrences are known.

Economic vermiculite concentrations are related to the weathering crust after high-mica metamorphic and igneous rocks. The ore bodies comprise the non-structured eluvium with vermiculite predomination in the upper part, and hydro-biotite, hydro-phlogopite and hydro-muscovite – in the lower part; under heating these ones are capable for 4-6 times volume expansion. Middle part has mixed vermiculite-hydro-biotite-phlogopite-muscovite composition.

The ore bodies occur at the depth 0-15 m, they are lens-shaped with maximum thickness 15-35 m being 150-750 m long and up to 400 m wide; average hydro-mica content is 16.5-25%.

Deposits are out of production. Facing-stone raw materials Ornamental stone G r a n i t e , g a b b r o i d s , m a r b l e In the map sheet territory shonkinite-essexites of Zirkska Association – Dragunske deposit (I-2-13),

granites of Saltychanskiy Complex – Mogyla Kamyana (II-2-38) and Andriivske (II-3-52) deposits, and carbonate rocks of Kalaytanivskiy occurrence (II-4-67) can be used for ornamental facing stone output.

In Dragunske deposit the fine-grained texture, fairly regular distribution of feldspar, pyroxene and amphibole grains, dark to black colour, and the block patterns define the wide spectrum of the commodity use. The rocks are exposed at the surface or are overlain by thin loam lenses. Deposit is in production since the end of XX century.

Saltychanski granites are the rocks of light-grey colour, irregular-medium-grained texture and massive structure. The saleable production output in deposit revealed from the studies of natural fracturing is 25-35% (30% - first-group blocks, 50% - second- and third-group blocks, 20% - fourth- and fifth-group blocks).

Carbonate rocks of Kalaytanivska site belong to Temryukska Suite. The marbles and calciphyres are observed in the 180-190 m wide fold extended over 400 m. Five beds of 11 m total thickness, in swells – up to 25-30 m are defined. Occurrence is perspective and requires further studies.

Construction raw materials Glass and porcelain-faience raw materials P r i m a r y k a o l i n e Novokazankuvatskiy occurrence (I-1-2) of primary kaoline is known in the map sheet territory. Kaoline

weathering crust is of dirty-white colour, up to 30 m thick, it lies beneath Quaternary loams at the depth 13.8 m. Kaoline does match requirements for porcelain-faience and refractory ware manufacturing. Occurrence is perspective and requires further studies.

P e g m a t i t e In the map sheet territory 15 deposits and a range of ceramic pegmatite occurrences are explored,

mainly in the central part of Saltychanska Dome structure, in Andriivsko-Elyseivskiy ore camp (II-2-40, II-2-41, II-2-42, II-2-43, II-3-49, II-3-56, II-3-57 etc.). Deposits comprise the series of contiguous veins of mica-quartz-feldspar pegmatites.

In the map sheet territory is located one of the major ceramic pegmatite deposits – Balka Velykogo Taboru (II-2-43) which contains up to 85% of explored ceramic pegmatite reserves in Ukraine. It is located in 0.5-2 km to the east of Elyseivka village. Here, over the square 1.8 km2 (1.2 by 1.5 km), in gneisses of

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Zakhidnopryazovska Series and granitoids of Shevchenkivskiy and Obitochnenskiy complexes 12 pegmatite veins from 6 by 150 m to 30 by 750 m in size are distinguished. The strike of most veins is north-western (300-315o) and dipping – south-western (210-225o). The veins display some zoning expressed in transition from aplite central zone through the grained and graphic pegmatites to the pegmatites with pegmatoid and block texture. The beneficiation plant may operate on the base of this deposit producing 100-200 thousand tons of concentrate per year.

Microcline concentrate can be used for manufacturing of housing and technical porcelain, semi-porcelain and window glass.

Cement raw materials S i l i c a c l a y Silica clays in Novosemenivske deposit (I-1-4) are encountered and explored in Upper Cretaceous

sediments. The ore body is irregular in composition with major silica clay and subordinate silica-clay-like sandstones and marls and variable thickness from 2.0 to 9/75 m. The overburden rocks comprise up to 9.5 m thick Quaternary loams. Deposit is explored with economic reserves but was not mined yet.

Quarry-stone raw materials I n t r u s i v e , m e t a m o r p h i c a n d s e d i m e n t a r y r o c k s Construction stone (aggregate and gravel) can be produced from: hornblendites of Novosilska

Association – Sadove deposit (I-4-27); granites and migmatites of Anadolskiy Complex – Stulnivske (I-1-5), Novopoltavske (I-2-14) and Berdyanske (III-3-92) deposits; granodiorites of Shevchenkivskiy Complex – Osypenkivske deposit (III-4-105); migmatized gneisses of Dragunska Sequence – Tsarekostyantynivske (I-3-15) and Kuybyshevske (I-3-16) deposits; migmatized gneisses and mafic gneisses of Zakhidnopryazovska Series – Zekenivske (III-1-76), Yuryivske (III-2-85) and Kolarivske (III-2-86) deposits. Commonly granites and migmatites of Anadolskiy Complex as well as migmatized gneisses of Dragunska Sequence are being mined.

Migmatites of Stulnivske deposit (I-1-5) are grayish-pink rocks and are cut by fracture systems into large blocks. In the quarry of Tsarekostyantynivske (I-3-15) deposit biotite-amphibole, pinkish-grey, migmatized gneisses are being mined; at the surface the rocks are destroyed to the gruss. The crushed rocks from these deposits are used in the road construction purposes.

Sandstones of Chernigivske (I-1-6) and Stulnivske-1 (I-1-7) deposits are less suitable for aggregate and gravel manufacturing. Thickness of the bodies varies in the range 1.5-5 m, they occur at the depth 0-5 m. Occupied square exceeds 100 hectares.

Sand and gravel raw materials Deposits of this group (III-4-120, III-4-121, IV-4-130 etc.) are widespread in the southern part of the

area and are related to the Quaternary System. The rocks involved can be used as the natural construction materials, fillers of construction liquids, inert additions to concrete and armed-concrete, ballast materials. Deposits were not mined yet.

Brick-tile raw materials Clays and loams are widely used for brick and tile manufacturing. They are confined to the Quaternary

sediments and are developed mainly in the southern and central parts of the map sheet. Numerous deposits (I-1-114, II-3-116, II-4-117 etc.) of this type are known. Deposits are composed of pale-brown, brown-yellow and red-brown loess-like loams of total thickness from 3.2 to 12-40 m. Some deposits are exhausted (II-4-117, III-1-118), one is in production (IV-4-129) and remaining was not mined yet.

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Waters Underground waters In the territory of L-37-VII map sheet deposits and occurrences of underground waters are known:

Lunacharske deposit of fresh waters (IV-3-110), Lazurne deposit (IV-4-112) and Radyvonivskiy occurrence (III-4-95) of mineral waters.

Lunacharske deposit is confined to the sequence of clays and sands of Akchagylskiy regio-stage which is developed in the 7-20 km band along the Azov Sea coast. Depth of water-bearing horizon footwall varies from 8 to 75 m. Waters are hydrocarbonate-chloride-sulphate, magnesium-calcium-sodium, and mineralization – 1.5 g/dm3. Waters do not match the standard requirements but in arid climate environments are used for water supplying over entire territory of their development.

Lazurne deposit is related to Upper Cretaceous sands developed in Berdyanskiy Graben. The waters contain distinct components and are bromine chloride-sodium in composition with mineralization 58.6 g/dm3. Medical value of the water is defined by bromine content from 24 to 137.6 mg/dm3 and the active components like iodine, iron, fluorine, arsenic, meta-boron and silica acids etc. Deposit is explored with economic reserves; the waters are used by the resorts and medical institutions of Berdyansk town.

In addition, some springs of mineral waters related to the rocks of crystalline basement are known. Of these, major Radyvonivskiy occurrence (III-4-95) of radon waters is located to the north of Radyvonivka village and is confined to extensively fractured gneisses of Kainkulatska Sequence. The waters are chloride-sulphate, mineralization – 7 g/dm3. Radon content is 4-5 ncn/dm3. Occurrence is not studied.

Mineral sludge and mud Two mineral sludge deposits are known in the area: Nogayske (IV-2-125) – Tsilyushche and Solone

lakes, and Berdyanske (IV-4-137) – Dovge, Gruzke, Chervone and other lakes. Square of the lakes is 1-2 km2, depth – up to 1 m, thickness of sludge layer – 0.4-1.6 m. Chemical composition of sludge is variable over many years. Major active components include radon, radium and bromine. Mineral sludge is used by the resorts and medical institutions of Berdyansk town.

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10. EVALUATION OF THE TERRITORY PERSPECTIVES The perspectives of the area are being appraised on the ground of analysis of geological structure and

distribution of mineral deposits and occurrences using the complex of prognostic factors and prospecting criteria for particular types of mineral resources. Recommendations for the directions of further works are concluded taking into account the perspectives appraised.

The following sites are distinguished by the degree of their perspectives: • high-perspective for the location of deposits in production, deposits with reserves prepared for

exploitation, deposits and occurrences of strategically important mineral types with economic and prognostic resources;

• medium-perspective, where iron and graphite ore deposits with economic reserves are located but these deposits are under-studied;

• low-perspective, where weakly-studied deposits as well as occurrences with favourable mineralization factors are located;

• unclear-perspective, where under-studied occurrences with favourable geological and tectonic setting and development of hydrothermal-metasomatic processes are located.

Major perspectives of the area concern the rare-earth, rare and precious metals. Of rare metals, tungsten is widespread although tungsten deposits are not encountered. Six occurrences

and 20 mineralization points are known confined to the plutonogenic-hydrothermal and skarn rocks; copper, gold and molybdenum also often occur in these places. Occurrences are accompanied by highly-contrasted anomalies in the crystalline rocks and by scheelite in the heavy concentrate samples. Areas occupied by diorites and gabbro-diorites of Shevchenkivskiy and Obitochnenskiy complexes and graphite-bearing gneisses of Temryukska Suite are perspective for molybdenum ores of stockwork and stratiform types. Widespread hydrothermal sulphidized rocks, molybdenum occurrences with economic grade (III-2-83) and aerial anomalies provide the reasons for further studies in these occurrences. Most perspective sites for molybdenum-tungsten mineralization include territories of Saltychanskiy Dome – Novosilskiy platinum-copper-nickel-bearing camp (B-2) and Berestovska Syncline – Temryuk-Troitskiy iron-graphite-ore camp (C-2) (see “Scheme of metallogenic zonation” to the “Geological map of crystalline basement”).

Pegmatites of Saltychanskiy Complex in Pivdennosorokynskiy gold-rare-earth-rare-metal ore field (B-4-1) and columbite pegmatites of Elyseivske ceramic pegmatite field (B-5-1) are perspective for niobium and tantalum.

Concerning the precious metals, prospecting interest in this direction has emerged in 70-80th of the last century upon the studies of some gold occurrences in Sorokynska tectonic zone and iron-ore deposits in Pryazovya provided by G.L.Kravchenko and I.I.Sakhatskiy [26, 27, 74]. Most studied is Sorokynska tectonic zone where the same-named gold-rare-earth-rare-metal camp is defined (B-4): besides Surozke deposit, six gold and silver occurrences are known here, of which five – in crystalline basement and one – in the sedimentary cover. Outside Sorokynska structure, in the basement, some precious metal occurrences are know (II-4-71, III-3-90) suggesting for positive specialization of the area in term of precious metals. Berestovskiy occurrence (II-4-71) is thought to be most perspective in view of widely developed silicification and sulphidization.

The perspectives for economic copper-nickel mineralization are defined. Five occurrences in Obitochnenske ore-bearing field (B-2-1) with increased content of platinum group metals allow prognosis for copper, nickel and platinum deposits in the Novosilskiy platinum-copper-nickel-bearing camp (B-2).

The diamond-bearing lamproites comprise the new rock type for the map sheet territory; three ore-bearing camps with different study degree are distinguished. Of these, most perspective is Andriivsko-Lozovatskiy diamond-bearing camp (B-6) where Kolarivske ore field (B-6-1) with three occurrences is defined and deposits with economic diamond concentrations are expected.

Graphite-bearing rocks of Tsentralnopryazovska TMZ, besides graphite, by spectrometry data are enriched in molybdenum and silver and can be treated as metamorphosed analogs of black-shale formation with additional prognosis for gold and PGM mineralization. These figures allow the new approach in perspective appraisal of graphite deposits in Temryuk-Troitskiy iron-graphite-ore camp (C-2).

Zakhidnopryazovska TMZ comprises the principal area of Ukraine where major reserves of ceramic pegmatites are concentrated. Their further growth depends on the industry needs. It should be noted that in the field of pegmatites (B-5-1) the heavy concentrate anomalies of columbite, tantalite and scheelite are defined suggesting for the needs in their extended studies aiming rare-metal objects prospecting.

Deposits related to the weathering crust and sedimentary cover are mainly small-scale and actually are of no practical value.

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Based on the mentioned features of the perspective fields and occurrences the following recommendations for their further studies are offered.

1) Geological-prognosis mapping should be conducted in the territory of L-37-VII map sheet aiming selection of the first-order targets for the exploration works.

2) In the map sheets L-37-26-B,D and L-38-B-a,b it is recommended conduction of extended geological study in the scale 1:50 000 (EGS-50) aiming solution the problem of age and litho-tectonic (formational) subdivision and identification of the stratified rocks of Temryutska Suite, definition the relationships between Zakhidnopryazovska and Tsentralnopryazovska series, and, in view of abundant mineral resources in the territory, definition controlling factors for gold, tungsten, molybdenum and diamonds.

3) In the map sheets L-37-25-D, -26-C, -37-B, -38-A the EGS-50 is also recommended: to study the internal structure, composition, development margins, metallogenic specialization and formational affinity of granitoids in Saltychanskiy Dome (Shevchenkivskiy and Obitochnenskiy complexes) and the mode of their interaction each other and with the host rocks; to study the minor intrusions of Novosilska Association, adjustment their composition, age and metallogenic specialization; to define the distribution patterns of potassium ultramafites and lamproites of Kolarivskiy Complex and to study their diamond-bearing potential.

4) To the orders of consumers the geological exploration for graphite, vermiculite, ceramic pegmatites, iron ores etc. should be conducted.

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11. ECOLOGO-GEOLOGICAL ENVIRONMENT The territory of L-37-VII (Berdyansk) map sheet, according to established zonation, encompasses two

regional structures: Prychornomorska Lowland and Azovo-Prydniprovska Height, which, in turn, are subdivided into diverse classes, types and varieties of landscapes.

The following classes of landscape are distinguished in Prychornomorska Lowland. Chloride-sulphate landscape class (solonetz, saline land) is covered with wet crumbly salt crust

underlain by sandy or sandy-loamy layer with abundant shells. At the depth 1-2 m the bitter-salty water occurs. The soil profile is highly chloride-enriched. Composition is classified as salty by anionic and cationic relations in water extract: Cl – 1 mg-equiv./dm3; SO3 - 0.2 mg-equiv./dm3. The pH reaction is alkaline – 7.6-8.5.

Calcium class (chestnut soils) is being formed mainly over heavy loess-like loams; it contains humus – 3-4% (A+B1 – 30-40 cm) and nitrogen – 0.19-0.25%. Absorption capacity is 23-27 mg-equiv. per 100 m of soil (after Gedroitz). Among adsorbed alkalis Ca2+ predominates in amount of ~97% of adsorbed capacity and from 2.7 to 3.4% possesses exchange Na+. Reaction of water extract is low-alkaline – pH 7.2-7.5. Maximum carbonate accumulation is observed at the depth 50-55 cm; boiling at 40-45 cm.

In Azovo-Prydniprovska Height the following landscape classes are distinguished: 1) Chloride-sodium (meadow-solonetz soils and saline lands) class is developed in case of close

location of mineralized ground waters. Salinity composition (after Yu.P.Lebedev) is as follows: Cl- > 2 mg-equiv.; Na+ > 2 mg-equiv. Water extract reaction is alkaline – pH 7.6-8.5.

2) Calcium (black-earth soils) class is developed beneath steppe and diverse-grass-steppe grassy plants. It is formed mainly over heavy high-carbonate loess-like loams. Total thickness of humus layer (A+B1) is 45-60 cm. Nitrogen content (0.2-0.5%) varies respectively to humus content. Absorption capacity is 30-70 mg-equiv. per 100 m of soil. Among exchange cations calcium predominates. Magnesium possesses 15-20% of total amount. Among adsorbed cations few Na+ and Mg2+ occur. The pH reaction is 7.0-8.5. Maximum accumulation of carbonates is observed below the humus layer and often including the layer of humus tongues.

In the studied area calcium class is most developed occupying about 75% of the territory. According to the soil-geographic zonation the studied territory belongs to sub-aerial belt and to IV area

– central forest-steppe and steppe; to Machorovicic zone – of common and southern steppe black-earth; to the province 33 – Southern Ukrainian.

The landscape type defines migration dynamics of harmful contamination components due to the planar and linear detachment and filtration. The following types are distinguished:

• elevated erosion-denudation plain with plakors and slopes; • low-elevated accumulative-denudation plain with plakors and slopes; • accumulative and denudation-accumulative alluvial plain: flood-land terraces and aqueous plains. The landscape types define the soil sorption properties and reflect major features of column lithology.

In the aeration zone the following types are distinguished: • sands over loams and clays; • loams over sands; • loams over carbonate rocks; • loams over sandy clays; • loams over clays; • loams over crystalline rocks. Geological-ecological studies have shown that the territory almost throughout underwent technological

impact. The natural landscapes, except saline lands in the mouth parts of Berda, Lozuvatka, Obitochna rivers are substituted by the landscapes partially modified by industrial activities and natural-technogenic landscapes. The first one includes the natural landscapes that underwent modifications changed the natural biologic exchange and at present reside under short-term antropogenic influence. These include gardens, vineyards, forest massifs, sites of perennial shrub-grassy meadow plants and the huge agro-landscapes (arable lands). Of the natural-technogenic landscapes (reside under permanent or long-term antropogenic influence) the major ones include the city and village agglomerations, irrigation systems, electric power lines >10 kW, quarries, road complexes, major highways. The general high level of technogenic charge is also evidenced by the great number of geological environment contamination sources. In Zaporizka Region the module of technogenic charge is 400-800 t/km2, in places – 4000-5000 t/km2.

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Fig. 11.1. Sketch ecologo-geological map.

1 – Ecological state of geological environment: a – extremely charged, b – charged, c – moderately charged, d – appropriate. 2 – Boundaries: a – territories with different integral ecological assessment; b – sites with assessment of changes or contamination by same-rank specific substances. 3 – Technogenic objects affecting geological environment: a – quarries, b – fuel shops, c – fertilizer and pest-killer storages, d – cattle burial grounds. e – animal farms and poultry-farms, f – irrigation systems. 4 – Contamination of geological environment components (blue – in underground waters, red – in soils, violet – in bottom sediments): a – spot anomalies; to the right – contaminating chemical elements; b – planar anomalies, in contour breaks - contaminating chemical elements, c – nitrate-nitrite contamination. 5 – Pseudo-formula of ecological assessment for geological environment. Indices: C’ – dangerous level of underground water contamination, D – moderate-dangerous level of soil contamination, F – low rate of dangerous processes (set forth in the factor descending order). Note: ecological state of this territory is almost completely related to the natural agents (high mineralization and hardness of underground waters, extensive exogenic geological processes etc.).

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Evaluation of ecological state includes impact of natural factors (neo-tectonics, underground water protection, thickness of aeration zone, EGP), technogenic factors (technogenic change of natural landscapes, module of technogenic charge), and natural factors modified under human influence (state of soils, bottom sediments, surface, ground and underground waters).

Emerged zones of neo-tectonic breaks may be the channels of diverse substance migration. Thickness of aeration zone, as criteria for the ground waters protection, varies from 1 m in the river

valleys to 10 m and more at the watersheds. Throughout in the area erosion (ravine-gully, planar removal), slide activization, re-working and

mudding of water reservoir bottoms, under-flooding of inhabited localities are developed being complicated by human activities.

The natural factors essentially modified by technogenesis which affect the ecological situation include state of soils, bottom sediments, surface and underground waters.

Organic contamination of soils is not encountered and pesticide content does not exceed TAC. High content of natural radio-isotopes is defined in the beach sands of ilmenite-zircon-monazite composition. Thorium (232Th) is the major radioactive element in sands.

Radiological situation in the studied area is considered to be satisfactory since g and b parameters are within the standard limits. Amount of heavy metals excess over TAC in the ground and underground waters is 5.5-113.4.

The waters are mainly sulphate of mixed cationic composition. Almost all ground waters are contaminated. Contaminants include iron, boron, bromine, strontium, cadmium and others. Throughout in the areas of private farming the water organic contamination is observed expressed in high nitrate content and oxidation degree. Of organic contaminants nitrates only are determined. Nitrate contamination is spread over 2020 km2 (40%) of the map sheet territory and of this amount 1806 km2 possesses the water-bearing horizon in fractured Precambrian crystalline rocks being non-protected.

It is estimated by sampling of the water-scoops that in the underground waters sum of heavy metals TAC excess is low.

In general, using evaluation criteria provided, contamination of surface and underground waters is high and in the map sheet it is spread over the square of 3890 km2 (see the map) although this contamination is of natural origin.

There are few unbroken landscapes in the map sheet and almost all of them are broken to the depth 5 m in towns and villages; more than 5 m – in the industrial zones and at the quarry sites; more than 50 m – in Stulnivskiy open pit.

Content of some elements (zinc, nickel, copper, strontium, vanadium etc.) exceeds the background values in the bottom sediments of ravine-gully system which are used for sewage and storage of housing wastes. In other cases the bottom sediments of surface water reservoirs and water flows reside at the geochemical background level except niobium anomaly located to the west from Begim-Chokratske rare-earth-rare-metal occurrence. Pesticide content of chemical chlorine-organic group in excess of TAC is determined at six points of bottom sediments.

The rocks of aeration zone are almost not contaminated. Ecological state in the studied area is very charged mainly due to natural factors: high mineralization

and hardness of underground waters, extensive development of EGP (abrasion of sea coast, slides etc.). Radioactive contamination is encountered in the beach sands. Influence area of Berdyanska industrial-urban agglomeration is considerable.

Taking into account the data presented, it is suggested to continue the ecological studies in places of encountered contamination aiming observations on changes in ecological state. It is required a survey over medical organizations to collect the information concerning sickness provoked by Cd, Pb, Cu, Co, V, Mn, Sr content in excess of admissible concentrations.

Aiming prevention the health hazard to the people on vacations at Azov Sea, the annual mapping is required for the ilmenite-zircon-monazite sands by means of radiation surveys on the sea beaches and sandbanks. In addition, regular sands reclamation and setting of caution marks are required.

Adjustment is required concerning data received during EGSF-200 over Berdyanske water reservoir (which is used for water supplying of Berdyansk town and surrounding villages) and neighbouring territory. In case of our data confirmation (Mo in bottom sediments; Zn, Cu, As – in soil; Fe and NO3 – in water) perhaps it should be considered the issue on establishment of sanitary protection zone of Berdyanske water reservoir with removal all the farms located in around.

It should be avoided formation of the ecologically-dangerous geochemical and bio-geochemical anomalies which may be caused by the waste use as fertilizer, irrigation with contaminated river waters, general technogenic contamination of environment and atmospheric pollutions.

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Table 11.1. Chemical element content in the components of geological environment (L-37-VII map sheet) Major parameters of chemical element distribution in soils, bottom sediments and surface waters

Element content

soils, mg/kg bottom

sediments, mg/kg

beach sands, mg/kg surface watersChemical

elements Danger class TAC

Back-ground (soils)

c min c max c min c max c min c max TAC, mg/l Barium 3 332 15 700 15 1000 15.5 700 0.1 Beryllium 2 1 2 1 2 1 2 0.0002 Lead 1 30 19 10 70 2 50 10 70 0.03 Tin 3 0.5 5 0.5 30 0.5 5 Titanium 3800 300 5000 700 5000 300 7000 0.1 Tungsten 3 1.5 3 1.5 20 1.5 3 0.05 (0.1) Manganese 3 1500 660 200 700 100 1000 200 1000 0.1 Niobium 2 24 5 30 10 1500 5 30 0,01 Gallium 8 5 20 5 20 5 20 Chromium 2 100 56 5 150 30 300 5 300 0.5 Nickel 2 150 20 1 70 5 100 1 200 0.1 Bismuth 2 1.5 1 2 0.5 20 1 2 0.1 (0.5) Cobalt 2 6 7 20 2 20 7 30 0.1 Molybdenum 3 1 0.5 2 0.5 3 0.5 2 0,25 Vanadium 3 150 46 1 100 5 100 1 200 0.1 Copper 2 30 22 3 50 10 315 3 70 1 Zinc 1 100 54 5 150 30 5000 5 150 1 Zirconium 470 150 500 50 500 150 500 Silver 0,03 15 30 15 70 15 30 0.05 Yttrium 23 2 30 1 50 5 30 Ytterbium 2,3 1 3 1 5 1 3 Lanthanum 23 10 30 5 70 10 30 Cerium 30 15 30 15 100 15 30 Phosphorus 750 300 700 150 5000 300 700 0.001 Strontium 3 150 150 150 70 1000 150 150 7 Scandium 8 3.5 7 3.5 10 3.5 7 Lithium 2 8 5 30 5 150 10 30 0,03 Fluorine 10 2 Mercury 1 2.1 0.04 Arsenic 3.5 3.5 3.5 3.5 0,05 pH 6.5-8.5 Mineralization 1000 Hardness Са 180 Mg 20 Na 200 NO

3 45 Cl 350 SO4 50 HCO3 29

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CONCLUSIONS The set of geological maps of L-37-VII (Berdyansk) map sheet in the scale 1:200 000, prepared for

second edition, provides the principally new ideas on geology and mineral resources of the studied territory. The principally new and most important results include:

a) for crystalline basement of Ukrainian Shield: • definition of new Paleo-Archean stratigraphic unit – Dragunska Sequence (AR1dr) and its

subdivision in two sub-sequences; • moving up the former Osypenkivska Suite into the Series with its subdivision in two suites: lower –

Olginska (AR3ol) and upper – Krutobalkinska (AR3kb); • definition of Neo-Archean Sorokynskiy ultramafic complex (sAR3sr); • definition of minor, up to 0.5-1.9 km in diameter, ultramafic-gabbro central-type intrusions in

Novosilska Association (sPR1ns); • ascription to Anadolskiy Complex (gPR1an) (by analogy with adjacent map sheet) the Nyzyanskiy

type granites; it is worthy to define them further in a separate complex; • definition of Andriivskiy type granites into separate group temporarily ascribed to Saltychanskiy

Complex (g2PR1sl); • subdivision of pegmatites in two types: rare-earth and rare-metal and, in turn, definition of rare-

metal (Ta, Nb, Li) and ceramic sub-types in the latter; • discovery of Kolarivskiy (iPR1kl) kimberlite-lamproite complex and diamond finding in the rocks

involved; • subdivision of Paleozoic minor bodies (dykes and sub-volcano necks) in two groups: sub-alkaline

gabbroides – Zirkska Association (enPZ-Mz-zk); trachytes, trachy-andesites and andesites – Volnovasko-Elanchytska Association (PZ-MZvel);

• new insight of map sheet geology, litho-tectonic and paleo-tectonic zonation. b) for sedimentary cover: • definition of three litho-tectonic zones (Chernigivsko-Stulnivska, Chernigivsko-Berestivska,

Prymorska) and their boundaries; • adjustment the distribution areas for all stratigraphic units of sedimentary cover in litho-tectonic

zones; • corrections for Meso-Cenozoic sediments over the map sheet in compliance with the current

Legend of “Derzhgeolkarta-200”, 1986 [31]; • definition and mapping the sub-aerial facies of Quaternary sediments and their subdivision (for the

first time) into climatoliths; • definition (for the first time) of water-bearing horizon in Middle Jurassic sediments in

Novomyklaylivska Depression of Chernigivsko-Berestivska LTZ. Adjustment of geological structure had allowed new metallogenic zonation of the territory and

reappraisal its perspectives making predictions not only for the minerals common in the area: iron, graphite, pegmatites, vermiculite, crushed stone, apatite and rare metals, but also for the new ones: diamond, gold, copper-nickel mineralization and facing stones, within new perspective fields of which major include Novosilskiy platinum-copper-nickel-bearing camp, Andriivsko-Lozuvatskiy and Kamyshuvatsko-Konkskiy diamond-bearing camps, and Temryuk-Troitskiy iron-graphite-ore camp. Both GPM-200 and EGSF-50 are recommended in these areas.

By ecological-geological studied conducted for the first time during extended geological works, it is defined that the map sheet territory throughout underwent the technogenic impact.

Ecological state in the studied area is very charged mainly due to natural factors: high mineralization and hardness of underground waters, extensive development of EGP (abrasion of sea coast, slides etc.). Radioactive contamination is encountered in the beach sands. Influence area of Berdyanska industrial-urban agglomeration is considerable. Chemical composition of all water types (surface, ground, underground) in regional respect does not match the current standards. Contaminants include iron, boron, bromine, strontium, cadmium etc. In the areas of private farming the water organic contamination is observed expressed in high nitrate content and oxidation degree.

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Despite of high information potential and precision of prepared maps some issues of geology are not solved unequivocally yet. These disputable questions mainly concern stratigraphy and magmatism of composite geological units, specifically:

1. The age of Tsentralnopryazovska Series requires adjustment since its granulite metamorphism suggests for older (Paleo-Archean) age.

2. Ascription of Dragunska Sequence to Paleo-Archean is conventional enough and also requires adjustment. The statement is not supported by presented isotopic dating of the lower sub-sequence.

3. Some difficulties exist in subdivision the rocks of diorite composition ascribed to Shevchenkivskiy and Obitochnenskiy complexes.

4. It is problematic combining in Saltychanskiy Complex the typical Saltychanski and Andriivski granites which differ in mineral composition and petrochemical features.

5. It is disputable ascription to Anadolskiy Complex the Nyzyanskiy type granites surrounding Chernigivskiy carbonatite massif.

6. In Prymorska LTZ the volume of Paleogene System requires adjustment (Paleocene sediments should be defined).

Solution of mentioned problems is possible through more precise geological mapping on the ground of prepared maps L-37-VII (Berdyansk).

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26. Kravchenko, G.L., Sakhatskiy, I.I., Rusakov, N.F., 1985. New data on gold occurrence // Geological Journal (Ukraine). – v.45, N 5. – p. 127-131. (In Russian).

27. Kravchenko, G.L., 1992. New data on gold occurrence in Burtychiya River basin and host rocks composition (Western Pryazovya) // Geological Journal (Ukraine). – N 4. – p. 110-120. (In Russian).

28. Krivdik, S.G., Tkachuk, V.I., 1990. Petrology of Alkaline Rocks of Ukrainian Shield. – Kyiv: Naukova Dumka Publishing. – 408 p. (In Russian).

29. Krivonos, V.F., 1999. On the link of kimberlite diamond bearing with their petrochemistry and age // In: Prognosis and Prospecting for Hard-Rock Diamond Deposits. – Simferopol. – p.84-87. (In Russian).

30. Kulish, E.A., Galiy, S.A., Komov, I.L., et al, 1998. Platinoid-bearing of geological complexes of Ukraine // In: Aspects of Minerageny of Ukraine. Kiev – p.329-346. (In Russian).

31. Legend of Geological Map of Ukraine in the scale 1:200 000. Central-Ukrainian Series. Explanatory Notes, 1996. – Kiev: Goskomgeologia Ukraine. – 27 p. (In Russian).

32. International Tectonic Map of Europe. 3rd Edition, 1998. The Map of Basement of Eastern-European and Western-European Platforms in the scale 1:10 000 000. Eds.: S.V.Bogdanova, R.M.Gorbachev (Eastern Europe); V.D.Brezhnev (Western Europe). – Sankt-Petersburg Map Factory, VSEGEI. (In Russian).

33. Melnik, V.I., 1961. Mineralogical composition of loess rocks and some basic sections of Ukraine // In: Quaternary Period. – Kiev: AS Uk.S.S.R. Publishing. – p.157-171. (In Russian).

34. Razdorozhniy, V.F., Vasilchenko, V.V., Borodynya, B.V., 2000. Precambrian igneous complexes of South-Western Pryazovya (Berdyanskiy sheet) // In: Precambrian Geology and Magmatism of Ukrainian Shield. – Kyiv. – p.92-96. (In Russian).

35. Rusakov, N.F., Kravchenko, G.L., 1986. To the question of structure of Chernigivskiy carbonatite massif (Pryazovya) // Geological Journal (Ukraine). – v.46, N 4. – p. 112-118. (In Russian).

36. Sollogub, V.B., 1980. Lithosphere of Ukraine. – Kyiv: Naukova Dumka Publishing. – 184 p. (In Russian).

37. Sorokhtin, O.G., Ushakov, S.A., 1991. Global Evolution of the Earth. – Moscow: MSU Publishing. – 446 p. (In Russian).

38. Stratigraphic columns of Precambrian of Ukrainian Shield, 1987. / K.E.Esipchuk, Ed. – Kyiv: Naukova Dumka Publishing. – 168 p. (In Russian).

39. Scheme of lithosphere deep structure in south-western part of Eastern-European Platform. Scale 1:1 000 000, 1992 / A.V.Chekunov, Ed. (In Russian).

40. Tsukanov, V.A., Esipchuk, K.E., 1970. On helsinkites of Western Pryazovya // In: Proc. NISKTU, N 5. (In Russian).

41. Shcherbak, N.P., Zagnitko, V.N., Artemenko, G.V., Bartnitskiy, E.N., 1995. Geochronology of major geological events in Pryazovskiy block of Ukrainian Shield // Geochemistry and Ore Formation. – v.21. – p.112-129 (In Russian).

42. Shcherbak, N.P., Artemenko, G.V., Stepanyuk, L.M., 1998. Stratigraphy of Archean of Ukrainian Shield. – Kyiv. – p.52-54. (In Ukrainian).

43. Eynor, O.L., Esipchuk, K.E., Tsukanov, V.A., 1980. Precambrian of Western Pryazovya. – Kiev University Publishing. – 184 p. (In Russian).

44. Yaskevich, T.B., 1999. Geology and gold mineralization of Sorokynska greenstone belt (Western Pryazovya). – Candidate Sci. Theses, Lviv. (In Ukrainian).

45. Glevasskiy, E.B., Glevasska, A.M., 2002. The Ukrainian Shield: Precambrian Regional Structure and Paleogeodinamics // Mineralogical Journal (Ukraine). – v.24, N 4.

46. Shcipansky, A.A., Bogdanova, S.V., 1996. The Sarmatian crustal segment: Precambrian correlation between the Voronezh Massif and Ukrainian Shield across the Dnieper-Donets Aulacogen // Tectonophysics, v.268 - P. 109–125.

Unpublished (all in Russian) 47a. Database “Geolkarta-200” of map sheet L-37-VII (Berdyansk), 2003. K. Geoinform. 47. Berezka, A.I., Reshetov, N.K., 1977. Report on complex hydrogeological and engineering-

geological mapping in the scale 1:50 000 in purposes of irrigation in the area between Berda and Kalmius rivers. Book 1. Text. – 240 p. // Artemovska GRRE, Artemovsk.

48. Bochkov, A.A., Bayrakov, V.V., Gogol, L.P., 1967. Geological report on results of prospecting works for antophyllite-asbestos in Western Pryazovya in 1964-1967. Book 1. Text. – 355 p. // Pryazovskaya GRE, Volnovakha.

109

49. Bochkov, A.A., Gogol, L.P., 1972. Report on prospecting-evaluation works for vermiculite in Andreevskoe and Radionovskoe deposits. Book 1. Text. – 224 p. // Pryazovskaya GRE, Volnovakha.

50. Bochkov, A.A., Kostenko, Yu.A., et al, 1983. Report on detailed marble prospecting in Kalaytanivskiy site in 1981-1983. Book 1. Text. – 259 p. // Pryazovskaya GRE, Volnovakha.

51. Brezitskiy, V.I., 1985. Report on prospecting for underground waters in Neogene and Cretaceous sediments for water supplying of Berdyansk town in 1981-1985. – 76 p. // Berdyanska KGIGP, Berdyansk.

52. Brezitskiy, V.I., 1986. Report on detailed exploration for mineral waters for “Niva” sanatorium, Berdyanskiy area, Zaporizka Region, conducted in 1985-1986. Book 1. Text. – 82 p. // Belozerska GRE, Berdyanska KGIGP, Berdyansk..

53. Brezitskiy, V.I., 1988. Report on works for study of regime, State recording and protection of underground waters from exhaustion and contamination in the territory of Zaporizka Region. Book 1. Text. – 62 p. // Berdyanska KGIGP, Berdyansk..

54. Brezitskiy, V.I., 1989. Report on prospecting for mineral drinking medical-table waters in Berdyanskiy area of Zaporizka Region in 1988-1989. Book 1. Text. – 70 p. // Berdyanska KGIGP, Berdyansk..

55. Veklych, M.F., Grigoryev, A.V., 1960. Paleo-geomorphologic forming conditions of Oligocene-Miocene kaolineous sequence in the eastern part of Mokrye Yaly River (Northern Pryazovya). Preliminary conclusion by IGN. Kiev. – 11 p.

56. Gogol, L.P., Borovikov, V.P., Gruba, V.I., et al, 1964. Geological report on prospecting works for vermiculite conducted in 1959-1963 in Pryazovya. Book 1. Text. – 363 p. // Pryazovskaya GRE, Volnovakha.

57. Grebenyuk, A.N., 1995. Report on prospecting and prospecting-evaluation works for quartzites for silica brick and ferroalloys in Pryazovya. Book 1. Text. – 84 p. // Pryazovskaya GRE, Volnovakha.

58. Dovgan, R.N., Izmaylov, S.G., Rusakov, N.F., et al, 1972. Report on the complex geologo-hydrogeological and engineering-geological mapping in the scale 1:50 000 in Prymorskiy geological area (Yaltinskiy site). Map sheets L-37-38-B,D; -37-39-A,B; -37-27-D (eastern half). Volume 1. Books 1, 2. Text. – 462 p., 405 p. // Artemovskaya KGRE, Artemovsk.

59. Dovgan, R.N., Fokin, K.I., Suyarko, M.P., et al, 1975. Report “Complex geologo-hydrogeological and engineering-geological mapping in the scale 1:50 000 in Prymorskiy geological area (Western site)”. Map sheets L-37-37-C,D; -38-C; -49-A. Book 1. Text. – 415 p. // Artemovskaya KGRE, Artemovsk.

60. Dovganyuk, P.D., 1989. Report on preliminary exploration of mineral waters for “Berdyansk” sanatorium. – 64 p. // Berdyanska KGIGP, Berdyansk.

61. Dralov, V.M., Isakov, L.V., Semerenko, A.Y., et al, 1979. Report on results of works on deep geological mapping in the scale 1:50 000 in the map sheets L-37-13-C,D; -37-25-A,B (Western Pryazovya) (Novopoltavskaya PGGK, 1975-1979). Volume 1. Text. – 400 p. // Novomoskovskaya GRE. Dnepropetrovsk.

62. Dyukov, A.V., 1985. Report on prospecting for diamonds in the junction zone of Donbass and Pryazovya (Verkhnekonkskiy, Kuybyshevskiy and other sites) in 1982-1985. Book 1. – 110 p. // Novomoskovskaya GRE. Novomoskovsk.

63. Zhylenko, L.A., Bochkov, A.A., 1984. Report on results of detailed prospecting for graphite ores in Karatyukskiy, Sachkinskiy and Troitskiy sites in 1981-1984. Book 1. Text. – 155 p. // Pryazovskaya GRE, Volnovakha.

64. Ignatkin, V.A., Shrubovich, F.V., 1961. Report on prospecting works for corundum conducted in the upper course of Konka River in 1959-1961. Book 1. Text. – 145 p. // Novomoskovskaya GRE. Novomoskovsk.

65. Kanygin, L.I., Usenkov, V.V., 1973. Report on results of preliminary exploration in the Central site of Kuksungur deposit. Book 1. Text. – 116 p. // Pryazovskaya GRE, Volnovakha.

66. Kiktenko, V.F., Pereverzev, S.I., Golinchuk, V.F., et al, 1987. Report on deep geological mapping in the scale 1:200 000 in Western Pryazovya over map sheets L-37-1-VII, M-37-XXXI (sheets M-37-133-A,B,C,D; -134-C; L-37-1-A,B,C,D; -2-A,B,C,D; -13-A,B,C,D; -14-A,B,C,D; -25-A,B) in 1982-1987 by Zapadnopryazovskiy GSO of Novomoskovska GRE. Book 1. Text. – 226 p. // Dnepropetrovsk.

67. Knyazkov, A.P., 1989. Report on prospecting for diamonds of non-kimberlite origin in Western Pryazovya (1985-1989). Book 1. Text. – 135 p. // Pryazovskaya GRE, Volnovakha.

68. Koval, E.M., Pavlyuchenko, R.A., Galitskiy, V.V., 1980. Report on results of detailed prospecting for rare metals in Sadoviy site conducted in 1977-1980. Book 1. Text. – 135 p. // Pryazovskaya GRE, Volnovakha.

69. Koval, E.M., Pavlyuchenko, R.A., Galitskiy, V.V., 1980. Report on results of prospecting for rare metals in the central part of Sorokinskaya tectonic zone. Book 1. Text. – 214 p. // Pryazovskaya GRE, Volnovakha.

110

70. Konkov, G.G., Polunovskiy, R.M., 1961. Report on results of the State complex geological mapping in the scale 1:50 000 over the map sheets L-37-15-C,D; -26-B; -27-A,B (Pryazovskiy crystalline massif). Volume 1. Text. – 504 p. // Artemovsk.

71. Konkov, G.G., Polunovskiy, R.M., Belevtseva, A.I., et al, 1965. Geological report on results of complex geological mapping in the scale 1:50 000 over map sheets L-37-14-C (southern half), L-37-26-A,C,D; L-37-27-C (Tsentralnopryazovskiy area). Volume 1. Text. – 565 p. // Artemovsk.

72. Kravchenko, G.L., Dovgan, R.N., Baranova, N.I., 1960. Materials to the State geological map of USSR in the scale 1:200 000. Complex geological map of the sheets L-37-VII (Berdyansk), L-37-VIII (Mariupol) (Report of geological group # 5 on works in 1957-1960). Book 1. Text. – 647 p. // Artemovskaya GRE. Artemovsk.

73. Kravchenko, G.L., Dovgan, R.N., Izmaylov, S.G., et al, 1962. Materials to the State geological map of USSR in the scale 1:200 000. Complex geological map of the sheets L-37-VII (Berdyansk), L-37-VIII (Mariupol) (Report of geological group # 5 on works in 1957-1960). Book 1. Text. – 1208 p. // Artemovskaya GRE. Artemovsk.

74. Kravchenko, G.L., Sakhatskiy, I.I., Rusakov, N.F., 1986. Proposals on study of mineralization in Sorokinskaya tectonic zone. Recommendation of IGFM AS Uk.S.S.R. and PGO “Donbassgeologia”. – 7 p. // Kiev.

75. Krivonos, V.P., Titova, E.G., Krivonos, V.I., et al, 1975. Report on results of prospecting works for iron ores in Korsakskoe and Novoukrainskoe ore fields. Book 1. Text. – 237 p. // Pryazovskaya GRE, Volnovakha.

76. Krivonos, V.P., Krivonos, V.I., Galitskiy, V.V., 1979. Geological report on results of geological exploration conducted in Kuksungurskoe iron-ore deposit (Zaporozhskaya obl. Uk.S.S.R) performed in 1969-1979 with reserve estimation by 01.01.79. Book 1. Text. – 397 p. // Pryazovskaya GRE, Volnovakha.

77. Krivonos, V.P., Zhylenko, L.A., Latsko, V.G., et al, 1982. Report on results of general prospecting for graphite ores in Pryazovya in 1979-1982. Book 1. Text. – 157 p. // Pryazovskaya GRE, Volnovakha.

78. Krivonos, V.P., Lisogor, V.P., Grebenyuk, A.N., et al, 1986. Report on results of general prospecting for ferruginous quartzites of deep horizons and structure studies in Kuksungurskoe field in 1982-1986. Book 1. Text. – 138 p. // Pryazovskaya GRE, Volnovakha.

79. Krongauz, E.G., Astrakhantseva, A.S., 1972. Report on prospecting for diamonds conducted in 1966-1971 in the southern part of Uk.S.S.R. Book 1. Text. – 73 p. // Novomoskovskaya GRE. Novomoskovsk.

80. Krongauz, E.G., Dyukova, A.V., Astrakhantseva, A.S., 1977. Report on prospecting for diamond-bearing kimberlites and prognosis map design over Middle Pryazovya in 1975-1977. Book 1. Text. – 203 p. // Novomoskovskaya GRE. Novomoskovsk.

81. Lavrinenko, L.F., Rozenberg, D.Sh., 1968. Report on results of prospecting for tantalum, beryllium, lithium, rubidium, rare earths in Pryazovya in 1964-1968. Book 1. Text. – 275 p. // Pryazovskaya GRE, Volnovakha.

82. Lavrinenko, L.F., Rozenberg, D.Sh., 1973. Geological report on results of prospecting for tantalum in Pryazovya in 1971-1973. Book 1. Text. – 74 p. // Pryazovskaya GRE, Volnovakha.

83. Lavrinenko, L.F., Pavlyuchenko, R.A., Pastuchenko, A.A., et al, 1974. Geological report on results of prospecting-evaluation works for tantalum in Sorokinskaya tectonic zone and prospecting works in the central part of Sorokinskaya zone in 1973-1974. Book 1. Text. – 121 p. // Pryazovskaya GRE, Volnovakha.

84. Lavrinenko, L.F., Chebanenko, V.V., 1976. Geological report on results of prospecting-evaluation works conducted in “Balka Krutaya” rare-metal deposit (Zaporozhskaya obl. Uk.S.S.R.) in 1972-1976 with reserve estimation by 01.06.1976. Book 1. Text. – 90 p. // Pryazovskaya GRE, Volnovakha.

85. Lavrinenko, L.F., Porokhnenko, P.K., Luginina, E.N., et al, 1977. Report on project “Design of metallogenic map in the scale 1:200 000 of Ukrainian Shield over the territory of Pryazovskiy massif”. Book 1. Text. – 326 p. // Pryazovskaya GRE, Volnovakha.

86. Lapitskiy, E.M., Romaniy, O.D., 1973. Report on results of works for evaluation of tantalum and niobium mineralization in the area of Chernigovskiy fault (Western Pryazovya) conducted in 1972-1973. Book 1. Text. – 112 p. // Belozerskaya GRE. Mikhaylovka.

87. Lapitskiy, E.M., Ploskiy, A.P., Romaniy, O.D., 1976. Report on results of prospecting for rare-metal-phosphate raw minerals in metasomatites of Novopoltavskaya field in Chernigovskaya fault zone cinducted in 1973-1976. Book 1. Text. – 178 p. // Belozerskaya GRE. Mikhaylovka.

88. Lapitskiy, E.M., Shapovalov, V.V., Nikitin, V.V., 1981. Report on detailed prospecting for phosphate raw minerals in Chernigovskiy site of Zaporozhskaya Region in 1980-1981. Book 1. Text. – 234 p. // Belozerskaya GRE. Mikhaylovka.

111

89. Lapitskiy, E.M., Dorozhkina, L.V., 1985. Report on results of preliminary exploration in Chernigovskiy block of Novopoltavskoe deposit conducted in 1981-1985. Book 1. Text. – 293 p. // Belozerskaya GRE. Mikhaylovka.

90. Lapitskiy, E.M., Dorozhkina, L.V., Nikitina, V.N., et al, 1991. Detailed exploration of Novopoltavskoe apatite deposit. Report on results of works conducted in 1982-1991 with reserve estimation by 01.07.1991. Books 1-3. Text. – 532 p. // Belozerskaya GRE. Mikhaylovka.

91. Lebedev, N.I., Kalanta, I.V., Buyanovskaya, M.E., et al, 1966. Report on geological mapping in the scale 1:50 000 conducted by GSP-10 in 1961-1964 over map sheets L-37-13-C,D; -37-25-A. Volume 1. Text. // Dnepropetrovskaya GE, Dnepropetrovsk.

92. Makarenko, A.M., 1977. Report on prospecting for iron ores in the flanks of Korsakskoe ore field in Western Pryazovya in 1976-1977. Book 1. Text. – 167 p. // Pryazovskaya GRE, Volnovakha.

93. Makarenko, A.M., 1978. Report on prospecting for iron ores in Shovkayskiy block of Kuksungurskoe deposit in 1977-1978. Book 1. Text. – 156 p. // Pryazovskaya GRE, Volnovakha.

94. Makarenko, A.M., 1979. Report on results of preliminary exploration in the eastern block of Korsakskoe iron-ore deposit in 1977-1979. Book 1. Text. – 213 p. // Pryazovskaya GRE, Volnovakha.

95. Makarenko, A.M., 1979. Report on results of prospecting for iron ores in the fields of perspective magnetic anomalies of Western Pryazovya in 1978-1979. Book 1. Text. – 185 p. // Pryazovskaya GRE, Volnovakha.

96. Makivchuk, O.F., Sivoronov, A.A., Bobrov, A.B., et al, 1997. Preliminary report on project “Development of technologies for design of prognosis-metallogenic maps of gold mineralization in Sorokinskaya tectonic zone with definition of perspective sites”. Book 1. Text. – 369 p. // NPO “Zemlya”. Kiev.

97. Nekryach, A.I., Elkin, V.D., Semerenko, A.T., et al, 1975. Report on results of data generalization and preliminary field works conducted in 1975-1977 aiming preparation to the deep geological mapping in the scale 1:50 000 over map sheets L-37-13-C,D; -25-A,B. Book 1. Text. – 125 p. // Novomoskovskaya GRE. Dnepropetrovsk.

98. Nesmeyko, V.D., Plyasovskaya, V.V., Kharlamova, N.Ya., 1976. Report on results of complex hydrogeological and engineering-geological mapping in the scale 1:50 000 over map sheets L-37-37-A (southern half); B (southern half); C,D (western and northern parts); L-37-38-A (southern half); B (western half); C (northern half) in irrigation purposes in 1974-1976. Book 1. Text. – 220 p. // Dnepropetrovsk.

99. Pastushenko, A.A., 1980. Report on results of prospecting for marble and marbled limestones in Pryazovya in 1978-1980. Book 1. Text. – 80 p. // Pryazovskaya GRE, Volnovakha.

100. Polunovskiy, R.M., Belevtseva, A.I., 1969. Report on project “Stratigraphy, petrology and metallogeny of gneiss series in Central Pryazovya” to fence drilling in Tsentralnopryazovskiy area. Book 1. Text. – 645 p. // Artemovskaya KGRE, Pryazovskaya GRE. Artemovsk, Volnovakha.

101. Priymak, P.G., Pastushenko, A.A., Shaposhnikov, S.V., 1991. Report on prospecting-evaluation works for staurolite in Sorokinskaya tectonic zone in 1986-1991. Book 1. Text. – 211 p. // Pryazovskaya GRE, Volnovakha.

102. Priymak, P.G., Pastushenko, A.A., Kozina, E.D., et al, 1992. Report on detailed exploration in Sadovoe deposit of crushed stone (Donetskaya Region) in 1983-1992 with reserve estimation by 01.05.1992. Book 1. Text. – 155 p. // Pryazovskaya GRE, Volnovakha.

103. Razdorozhniy, V.F., Borodynya, B.V., Knyazkova, I.L., et al, 2000. Report on extended geological study of the field in the scale 1:200 000 over map sheet L-37-VII (Berdyansk) in 1991-2000 by Berdyanskiy GSO. Books 1-11. Text, graphic and text annexes. // Pryazovskaya GRE, Volnovakha.

104. Rusakov, N.F., Lapchuk, L.I., Terina, L.A., et al, 1977. Report on results of deep geological mapping in the scale 1:50 000 of Eliseevsko-Andreevskaya field. Map sheets L-37-25-D-b,d; -26-B; -26-D-a,d; -37-B-b; -38-A-a,b. Volume 1. Text. – 335 p. // Artemovskaya KGRE, Artemovsk.

105. Rusakov, N.F., Lapchuk, L.I., Sinitsa, A.N., et al, 1981. Report on results of deep geological mapping in the scale 1:50 000 of Chernigivskaya tectonic zone (Korsakskaya field). Map sheets L-37-25-C, D-a, c; -37-А-B-a, c. Volumes 1, 2. Text. – 199 p. // Artemovskaya KGRE, Artemovsk.

106. Ryabtsev, N.S., Melnikova, Yu.V., Tyazhlova, V.E., 1981. Report on hydrogeological and engineering-geological mapping in the scale 1:50 000 in the irrigation purposes over map sheets L-36-36-C-d, e; L-36-48-А-а, b, B-а, b; L-37-25-C, c, d, D-c, d; L –37-26-C-c, d, D-c; L-37-37-А-а, b, B-а, b; L-37-38-А-c, b in 1977-1981. Book 1. Text. – 155 p. // Pryazovskaya GRE, Novomikhaylovka, Dnepropetrovsk.

107. Ryabykh, V.A., Shapovalov, N.I., Ryabykh, E.A., et al, 1976. Report on exploration of underground waters for water supplying of Berdyansk town. Book 1. Text. – 96 p. // Berdyanskaya KGIGP. Berdyansk.

108. Ryabykh, V.A., et al, 1976. Report on prospecting for mineral waters for “Berdyansk” resort, Zaporozhskaya Region, conducted in 1975-1976. Book 1. Text. // Berdyanskaya KGIGP. Berdyansk.

112

109. Ryabykh, V.A., Dovganyuk, P.D., 1981. Report on detailed exploration of mineral waters for “Lazurniy” sanatorium of Berdyansk resort, Zaporozhskaya Region, conducted in 1979-1980. Book 1. Text. – 155 p. // Belozerskaya GRE, Novomikhaylovka.

110. Strekozov, N.F., Teteryuk, P.I., Gonshakova, V.I., 1975. Geological report on results of studies of diamond-bearing perspectives and kimberlite rocks in junction zone of Pryazovskiy crystalline massif with Donbass in 1973-1974. Book 1. Text. – 284 p. // Pryazovskaya GRE, Volnovakha.

111. Strekozov, S.N., Dudik, A.I., Krivonos, V.I., et al, 1991. Geological report on research project “Critical analysis of geologo-geochemical data aiming perspective appraisal of the fields in Pryazovya conducted in 1989-1991. Book 1. Text. – 210 p. // Pryazovskaya GRE, Volnovakha.

112. Stremovskiy, A.M., Knyazkov, A.P., Guskova, I.O., 1986. Report on project “Definition and study of high-potassium mafic rocks in Prydneprovye and Pryazovye areas” in 1985-1986. Book 1. Text. – 154 p. // Pryazovskaya GRE, Volnovakha.

113. Tarasyuk, O.N., Chashka, A.I., Smirnov, G.I., 1998. Study of composition and beneficiation capacity of kimberlites and other genetically linked rocks of Ukraine. Preliminary report on project 097 for 1997. Book 1. Text. – 112 p. // NPAP “Nedra”. UGIMR GK of Ukraine. Simferopol.

114. Teteryuk, P.I., 1965. Geological conclusion on results of geological prospecting for base metals in Volnovakhskaya metallogenic zone and south-western part of Pryazovskiy crystalline massif in 1962-1964. Book 1. Text. – 158 p. // Pryazovskaya GRE, Volnovakha.

115. Tyazhlov, G.T., 1970. Report on prospecting for underground waters in Chernigovskiy, Primorskiy and other southern areas of Zaporozhskaya Region. Map sheets L-37-25-A,B,C,D; -37-26-C; -37-37-A,B. Book 1. Text. – 69 p. // Belozerskaya GRE, Dnepropetrovsk.

116. Tyazhlov, G.T., 1978. Report on underground waters reserve estimation in Zaporozhskaya Region. Book 1. Text. – 100 p. // Belozerskaya GRE, Dnepropetrovsk.

117. Tsukanov, V.A., Esipchuk, K.E., Yavorskiy, N.I., et al, 1967. Report on geological mapping in the scale 1:50 000 over the map sheets L-37-25-C,D; -37-37-A,B; 37-38-A (Western Pryazovya). Volume 1. Text. – 483 p. // NISKGU. Kiev.

118. Shapovalov, N.M., 1970. Report on prospecting for underground waters for water supplying of Berdyansk town of Zaporozhskaya Region – 74 p. // Berdyanskaya KGIGP. Berdyansk.

119. Shapovalov, N.M., 1973. Report on exploration of underground waters for water supplying of Berdyansk town (with reserve estimation). Book 1. Text. // Berdyanskaya KGIGP. Berdyansk.

120. Shapovalov, N.M., 1974. Report on prospecting for underground waters for water supplying of Primorsk town of Zaporozhskaya Region. Book 1. Text. // Berdyanskaya KGIGP. Berdyansk.

121. Shatalov, N.N., 1987. Perspectives of precious metals prospecting in Pryazovskiy block of Ukrainian Shield in relation to the dyke complex. Recommendation. – 37 p. // Institute of Geophysics AS Uk.S.S.R. Kiev.

122. Shaposhnikov, S.V., Krivonos, V.P., Pastushenko, A.A., et al, 1990. Geological report on project “Compilation of results of previous geological prospecting for local prognosis of high-alumina raw materials in Pryazovya in 1989-1990. Book 1. Text. – 183 p. // Pryazovskaya GRE, Volnovakha.

123. Shrubovich, F.V., Ignatkin, V.A., Petrenko, P.N., 1963. Report on prospecting for corundum-sillimanite raw materials in Western Pryazovya and Middle Pryazovya. Book 1. Text. – 152 p. // Novomoskovskaya GRE. Novomoskovsk.

124. Entelis, N.D., Zhilenko, L.A., Zaritskiy, A.I., 1960. Geological report on results of prospecting for rare metals in Middle Pryazovya in 1956-1960. Book 1. Text. – 457 p. // Pryazovskaya GRE, Volnovakha.

113

Annexes

Annex 1. List of deposits and occurrences indicated in the geological map and

map of mineral resources in pre-Quaternary units

Cell index, number in

map

Mineral type, object name and its location

Deposit exploitation state or brief description of occurrence

Geological-economic type

Notes (references

cited)

1 2 3 4 5

Combustible minerals Gaseous

Natural gas Occurrence

IV-1-107

Orlivskiy, left bank of Lozuvatka River, Orlivka village

Gas is methane in composition, yield is low

Sedimentary 73

IV-4-113 Berdyanska sandbank, 2 km to the east of Berdyansk town

Gas measure – 0.7-2.2%, gas bearing – 1.98-6.5 m3/m3. Sedimentary 58, 73

Solid Brown coal Occurrence

I-1-9 Veselovskiy, Vesele village

One coal bed encountered, thickness varies from 1-3 to 7-8.6 m Sedimentary 91, 105

Metallic mineral resources Ferrous metals

Iron ores Deposit

III-1-77 Kuksungurske; Maryanivka village, Mogyla Kuksungur

Explored with economic reserves, was not mined yet Metamorpho-

genic 76

III-1-79 Korsatske; Mykhaylivka village, 2 km to SE

Explored with economic reserves, was not mined yet

Metamorpho-genic

75, 93, 94

Occurrence

I, II-1-10 Vladivskiy; right bank of Begim-Chokrak river, Stepove village

Square 14500 m2, avg. ore thickness 4 m, soluble iron content 25-40%, vol. weight 3.2 t/m3

Sedimentary 91, 105

I-3-18

Ocheretyanskiy; site of Ocheretyanka and Khvostyanka gullies flow into Berda river

Magnetite content from 25 to 55%. In single chip sample: Fe2O3 26.11%, FeO 17.18%

Metamorpho-genic 71

I-3-19 Trystanivskiy; right bank of Berda river, Lantseve village

Magnetite iron content 24-25% Metamorpho-genic 71

I-4-24

Temryutskiy; right bank of Temryuk river, 2 km to S from Starchenkove village

Magnetite iron content 23-29% Metamorpho-

genic 100

114

1 2 3 4 5

II-1-31 Krushanlynskiy; 1 km to SE from Mokriy Stav village

Oxide iron content 29.04-54.72%, magnetite iron content from 23 to 35.6% at 30% avg.

Metamorpho-genic 105

II-1-32 Tarasivskiy; Tarasivka village

Oxide iron content 30-40% Metamorpho-genic 117, 92

II-4-62 Sachkynskiy; 1.5 km to E from Sachky village

Magnetite iron content 28.9% Metamorpho-genic 100

Rare metals Tungsten

Occurrence

II-3-54 Samsonova gully; Andriivka village

Tungsten content 0.3%, rubidium 0.066%

Plutonogenic-hydrothermal 104

II-4-69 Kirovskiy; left bank of Berda river, Kalaytanivka village

Scheelite content 400 g/t (WO3 in scheelite 74.9%), tungsten 0.06-0.1% Skarn 71

II-4-74 Krymska gully; Mykolaivka village

Tungsten content 0.15-0.2%, silver 9-20 g/t


Molybdenum Occurrence

III-2-83 Dolynskiy; Chokrak river, Dolino village

Molybdenite content in polished section 3%, by chemical analysis molybdenum content 0.084-0.232%


Niobium, tantalum, lithium Deposit

III-4-99 Kruta Balka; to SW from Radyvonivka village

Explored with economic reserves, was not mined yet Pegmatite 58, 84

Niobium Occurrence

III-4-106 Osypenkivskiy; left bank of Berda river, W outskirt of Osypenko village

Niobium content 0.2% Pegmatite 111

Rubidium, niobium, tantalum Occurrence

III-4-96 Dovzhyk gully; right bank of Berda river, Radyvonivka village

Columbite content 860 g/m3. By spectrometry rubidium content 0.41%, niobium 0.145%

Pegmatite 58

III-4-102

Blakytni Skeli; left bank of Berda river, to S from Radyvonivka village

Tantalum content 0.017%, beryllium 0.023%, cesium 0.003%, rubidium 0.07%. By mineralogical analysis columbite content 123 g/t, beryl 227 g/t, gold 0.1-0.3 g/t, silver 4 g/t

Pegmatite 58, 93

Rubidium, cesium Occurrence

III-4-93 Krymska gully; to SW from Radyvonivka village

Rubidium content > 0.1%, cesium 0.055%, tantalum 0.05%, niobium 0.01%

Pegmatite 58

Zirconium Occurrence

II-2-36 Saltychiya river; W outskirt of Saltychiya village

Zircon content 47.97 kg/t

Pegmatite 104

115

1 2 3 4 5

Precious metals Gold

Deposit

III-4-101

Surozke; right bank of Berdyanske water reservoir, Sobacha gully, to N from Osypenko village

Explored, was not mined yet

Plutonogenic-hydrothermal

1, 26, 96, 5, 43, 103

Occurrence

II-3-48 Andriivskiy; Samsonova gully, to E from Andriivka village

Sulphide-quartz mineralized zones. Gold grade up to 10 g/t Plutonogenic-

hydrothermal 104, 27

III-3-58 Sorokynskiy; right bank of Burtychiya river, former Soroki khutor

Sulphide-quartz mineralized zones. Gold grade up to 3 g/t, silver 20 g/t Plutonogenic-

hydrothermal 71, 104,

27

II-4-71 Berestovskiy; Karla Marksa village, right bank of Berestova river

Native gold, copper content attains 0.91% Plutonogenic-


III-4-103

Radyvonivskiy; Blakytni Skeli; left bank of Berdyanske water reservoir, to S from Radyvonivka village

Sulphide-quartz mineralized zones. Gold grade up to 10 g/t, copper 0.24-1.45%, silver 20 g/t Plutonogenic-


18

Silver Occurrence

III-3-90

Glyboka gully; left bank of Obitochna river, to S from Shevchenko village

Quartz mineralized zones.

Silver content 41-53 g/t, gold occurs in amount of 0.6 g/t

Plutonogenic-hydrothermal 34, 121

III-4-98 right bank of Kruta gully; to SW from Radyvonivka village

Telluric silver content 600 g/t. By spectrometry lead content 12%, zinc 0.05%, bismuth 0.06%


Rare-earth metals Cerium, lanthanum

Deposit

I-4-22

Mogyla Visla; right bank of Temryuk river, Starchenkove village

Monazite occurs together with zircon, zircon content in rock 10-15 kg/t.

Minor mining in the past Pegmatite 70

Occurrence

I-4-20 Karatyutskiy; right bank of Karatyuk river, Bilotserkivka village

Monazite content 12.36 kg/m3, zircon 12.09 kg/m3 Pegmatite 72, 73

I-4-23 Temryutskiy; right bank of Temryuk river, to S of Mogyla Visla

Monazite content 12.36 kg/m3 Pegmatite 70

II-1-30

Krushanlynskiy; left bank of Krushanly river, 1 km to SE from Mokriy Stav village

Metasomatically altered rocks.

Lanthanum content 0.5%, cerium 0.1% Plutonogenic-hydrothermal 70

II-2-39

Mogyla Saltychiya; right bank of Saltychiya river, to W from Sakhno village

Rare earth content: dysprosium and lanthanum 4.66%, yttrium and ytterbium 3.49%, cerium 4.61%, titanium 1%, beryllium 0.05%

Endogenous 117

116

1 2 3 4 5

II-3-50 Chervona Girka; mouth of Bezimenna gully, Andriivka village

Monazite concentration attains 21739 g/t Pegmatite 104

Yttrium Occurrence

II-3-47

Kamyshuvata gully; Andriivka village

Yttrium content 0.35%.

By mineralogical data xenotime content 6994 g/t, monazite 291 g/t, uraninite 60 g/t, magnetite 102 kg/t

Pegmatite 104, 27

Non-metallic mineral resources Non-ore raw materials for metallurgy

Refractory raw materials Clay

Deposit

III-1-78 Petrivske; right bank of Korsak river, Petrivka village

Under-studied, was not mined yet Sedimentary 73

Secondary kaoline Deposit

I-1-8 Vladivske (Richne); Begim Chokrak gully, Vladivka village

Exhausted Sedimentary 73

Occurrence

I-2-11 Novogrygorivskiy; Biloglynka gully

Interbed thickness 5-16 m, development square 11 km2 Sedimentary 91

Sillimanite, corundum Deposit

I-2-12 Dragunske; to S from Zori khutor


Metamorpho-genic

91, 122, 123

Flux raw materials Staurolite Deposit

III-4-97 Osypenkivske; to W from Radyvonivka village



Chemical raw materials Agro-chemical raw materials

Apatite Occurrence

II-1-29 Begim-Chokrakskiy; Chernigovo-Tokmatske village

Eight carbonatite veins 0.1-12 m thick Endogenous 35, 105

II-2-37 Saltychiya village; western part

Apatite content 15-20% Endogenous 117

Non-metal ore commodities Abrasive raw materials

Technical diamond Occurrence

II-4-63

Velyka Ternova gully; to E from Sachky village, Velyka Ternova gully, right branch of Berda river

In two samples chromospinelides and three fragments of ice-colour diamond found Endogenous 67

117

1 2 3 4 5

III-1-75

Zelenivskiy; Lozovatka river, Zelenivka village

Fragment (0.32 by 0.25 by 0.22 mm) of ice-colour diamond in thermal decomposition products of lamproite non-magnetic fraction

Endogenous 103

III-2-88

Kolarivskiy; Lozovatka river, Kolarivka village, “Mriya” pipe

In deluvial-alluvial sediments and in lamproites of “Mriya” pipe more than hundred of diamond fragments encountered

Endogenous 103

III-2-89 Anomaly No. 4; SE part of Kolarivka village

One diamond grain is found in re-deposited weathering crust Endogenous 103

III-3-91 Andriivskiy; Andriivskiy quarry, Kiltychiya river, Andriivka village

In thermal decomposition products of lamproites from dykes 0.15 mm diamond fragment found

Endogenous 103

Electric- and radiotechnical raw materials Graphite Deposit

I-4-25 Temryutske; Temryuk river, Starchenkove village


genic 70, 77

I-4-26 Karatyutske; Karatyuk river, Sadove village


Metamorpho-genic 63, 70

II-4-64 Sachkynske; Berda river, Sachky village



II-4-66 Troitske; Karla Marksa village



Occurrence

I-4-28 Lugivskiy; Berda river, Lugove village

Total thickness of ore zone 13-140 m Metamorpho-genic 70

II-4-72 Berestovskiy; Berestova river, to SE from Karla Marksa village

Graphite content 8.92-9.47% Metamorpho-genic 71

Adsorptive raw materials Vermiculite

Deposit

II-3-45 Andriivske; Kamyshuvata gully, Andriivka village

Explored with economic reserves, was not mined yet Weathering crust 49

III-4-100

Radyvonivske; Berda river, Kruta gully, Radyvonivka village


Occurrence

I-4-21 Temryutskiy; Temryuk river, to S from Temryuk village

Vermiculite content 6.5-17.9% Weathering crust 73

II-4-70 Kirovskiy; right bank of Berda river, Kalaytanivka village

Vermiculite content 3.0-17.3% Weathering crust 56, 71

II-4-73 Berestovskiy; mouth part of Berestova gully


118

1 2 3 4 5

III-2-87 Kolarivskiy; right bank of Lozovatka river, Kolarivka village

Vermiculite content 16-32% Weathering crust 103

III-4-94 Mykolaivskiy; left bank of Berda river, down of Vodyana gully mouth


Facing raw materials Ornamental stone

Granite, gabbroids, marble Deposit

I-2-13 Dragunske; Mokra Konka river, to N from Zorya khutor

Explored with economic reserves, in production Endogenous 91, 123

II-2-38 Kamyana Mogyla; Saltychiya river, to W from Sakhno village

Explored with economic reserves, in production Endogenous 91

II-3-52 Andriivske; Chabanska gully, Andriivka village

Explored with economic reserves, was not mined yet Endogenous 103

Occurrence

II-4-67 Kalaytanivskiy; Berda river, Kalaytanivka village

Total thickness of calciphyres and marbles 11-30 m Metamorpho-

genic 50

Construction raw materials Glass and porcelain-faience raw materials

Primary kaoline Occurrence

I-1-2 Novokazankuvatskiy; Novokazankuvate village

Thickness of kaoline weathering crust by drill-hole 30 m Weathering crust 91

Pegmatite Deposit

II-2-40 Sosykulatske; Chokrak river, Dakhno khutor


II-2-41 Eliseivske; Chokrak river, Eliseivka village

Explored with economic reserves, was not mined yet Pegmatite 73, 105,

124

II-2-42 Dalnya Kamchatka ; Bagy gully, Eliseivka village


124

II-2-43

Balka Velykogo Taboru; right slope of Velykogo Taboru gully, Eliseivka village

Explored with economic reserves, in production Pegmatite 73, 105,

124


Explored with economic reserves, in conservation Pegmatite 73, 105,

124

II-3-51 Kamyana Skelya; Kiltychiya river, Andriivka village


124

II-3-55 Krynychne; Kiltychiya river, NW outskirt of Uspenivka village


124

II-3-56

Krasnogorivske; Kiltychiya river, NW outskirt of Uspenivka village

Explored with economic reserves, in conservation Pegmatite 73, 124

119

1 2 3 4 5

II-3-59 Uspenivska; Kiltychiya river, mouth part of Vodyana gully

Explored with economic reserves, in conservation Pegmatite 73

II-3-60 Verbove; right bank of Burtychiya river


III-2-80 Zelena Mogyla; Chokrak river, Elyseivka village

Exhausted Pegmatite 73, 105, 124

III-2-81

Obitochnenske; right bank of Obitochnenska river, in front of Shevchenko village


III-2-82 Balka Glyboka; bank of Chokrak river, Elyzavetivka village


124

III-2-84 Dolynske; right bank of Chokrak river, Dolynske village


Cement raw materials Silica clay Deposit

I-1-4 Novosemenivske; left bank of Kainkulak river, Novosemenivka village

Explored with economic reserves, in conservation Sedimentary 73

Quarry-stone raw materials Sandstone Deposit

I-1-6 Chernigivske; N outskirt of Chernigivka village

Explored with economic reserves, is mined for sand Sedimentary 73

I-1-7

Stulnivske-1; left bank of Tokmak river; 3.2 km to SW from Stulneve village

Explored with economic reserves, in conservation Sedimentary 73

Intrusive, metamorphic and sedimentary rocks

Deposit

I-1-5 Stulnivske; left bank of Tokmak river, Kamyanka village

Explored with economic reserves, is mined for crushed stones, gruss Metamorpho-

genic 73

I-2-14 Novopoltavske; watershed of Tokmak and Konka rivers

Explored with economic reserves, in production Metamorpho-

genic 73

I-3-15 Tsarekostyantynivske; to N from Trudove village

Explored with economic reserves, in production

Metamorpho-genic 73

I-3-16 Kuybyshivske; N outskirt of Trudove village


Metamorpho-genic 73

I-4-27 Sadove; Karatyuk river, Sadove village


III-1-76 Zelenivske; Lozovatka river, Zelenivka village



III-2-85 Yuryivske; Lozovatka river, Yuryivka village

Explored with economic reserves, in conservation


III-2-86 Kolarivske; Lozovatka river, Kolarivka village

Exhausted Metamorpho-genic 105

120

1 2 3 4 5

III-3-92 Beryanske; Kiltychiya river

Explored with economic reserves, in conservation Endogenous 73

III-4-105 Osypenkivske; Berda river, Osypenko village

Is mined for gruss in road construction purposes Endogenous 73

Waters

Underground waters

Fresh waters

Deposit

IV-3-110 Lunacharske; bank of Kutsa Berdyanka river

Explored with economic reserves, in production Artesian basins 107

Mineral waters

Deposit

IV-4-112 Lazurne; northern coast of Azov Sea

Explored with economic reserves, in production Artesian basins 109

Occurrence

III-4-95 Radyvonivskiy; 0.6 km to N from Radyvonivka village

Mineral waters similar to Moskovskiy type Fractured mineral

waters 109

121


map of mineral resources in Quaternary sediments


map




Notes (references

cited)

1 2 3 4 5

Metallic mineral resources Non-ferrous metals

Titanium Occurrence

III-4-123

Gondzhugivskiy placer; coast of Azov Sea

Placer; two sites of 500 m long each. Ore minerals: monazite, ilmenite

Sedimentary 58

IV-3-126 Nogayskiy placer; coast of Azov Sea, to S from Shevchenko village

Placer up to 2 km long and 8-10 m wide. Valuable components: ilmenite, monazite

Sedimentary 58

IV-4-128 Novopetrivskiy placer; coast of Azov Sea, to N from Berda river mouth

Placer up to 2 m long. Valuable components: ilmenite, monazite. Average monazite content 2 kg/m3

Sedimentary 58

IV-4-133 Berdyanskiy placer; eastern coast of Berdyanska sandbank

Placer. Valuable components: ilmenite. monazite Sedimentary 58

Rare metals Niobium, tantalum

Occurrence

III-2-119 Placer; Chokrak river, S outskirt of Elyseivka village

Thickness of deluvial sediments 1.5-5.0 m, columbite content up to 200 g/m3

Sedimentary 73


Occurrence III-4,

IV-4-127 Placer; Berda river, Novovasylivka village

Placer ; in alluvial sediments gold content 11-30 mg/m3 Sedimentary 103

Non-metallic mineral resources Non-metal ore commodities

Abrasive raw materials Technical diamond

Occurrence

I-2-115 Placer; Mokra Konka river, right bank, higher Zhukova gully mouth

In alluvial sediments found: one diamond crystal (0.2 by 0.2 mm), satellite – pyrope, picroilmenite

Sedimentary 79, 80

IV-4-138 Berdyanskiy placer; W part of Berdyanska sandbank

In beach sands three diamond crystals found Sedimentary 58

122

1 2 3 4 5

Construction raw materials Sand and gravel raw materials

Deposit

III-4-120

Osypenkivske-1; Osypenkivske-2; left bank of Berda river, Osypenko village

Explored with economic reserves, was not mined yet Sedimentary 58

III-4-121 Osypenkivske-3; NE outskirt of Osypenko village


III-4-122 Olginske; right bank of Berda river valley


IV-4-130 Blyzhnyomakartynske; to NE from Berdyansk town


IV-4-136 Berdyanske; E part of Berdyanska sandbank


Brick and tile raw materials Loam, clay

Deposit

I-1-114 Chernigivske; Chernigivka village


II-3-116 Andriivske; Kiltychiya river, to S from Andriivka village


II-4-117 Mykolaivske; upper course of Zalizna gully, Mykolaivka village


III-1-118 Petrivske; Shovkay river, Petrivka village


IV-2-124 Nogayske; Obitochna river, Prymorsk town


IV-4-129 Berdyanske; 3.5 km to N from Berdyansk town

Explored with economic reserves, in production Sedimentary 58

IV-4-131 Berdyanske-1; W part of Berdyansk town

Explored with economic reserves, in production Sedimentary 58

IV-4-132 Berdyanske-2; N part of Berdyansk town


IV-4-134 Berdyanske-3; W part of Berdyansk town


IV-4-135 Berdyanske-4; E part of Berdyansk town


Waters Mineral sludge and mud

Deposit

IV-2-125 Nogayske; Nogaysk town, Likuvalne and Solone lakes

Explored with economic reserves, in exploitation Sedimentary 73

IV-4-137 Berdyanske; Berdyanska sandbank

Explored with economic reserves, in exploitation Sedimentary 73

123

Annex 3. List of deposits and occurrences indicated in the geological map and map of mineral resources of crystalline basement


map




Notes (references

cited)

1 2 3 4 5


Iron ores Deposit

III-1-77 Kuksungurske; Maryanivka village, Mogyla Kuksungur


genic 76

III-1-79 Korsatske; 2 km to SE from Mykhaylivka village


genic 75, 93,

94

Occurrence

I-3-18

Ocheretyanskiy; site of Ocheretyanka and Khvostyanka gullies flow into Berda river

Magnetite content from 25 to 55%. In single chip sample: Fe2O3 26.11%, FeO 17.18%

Metamorpho-genic 71

I-3-19 Trystanivskiy; right bank of Berda river, Lantseve village

Magnetite iron content 24-25% Metamorpho-genic 71

I-4-24

Temryutskiy; right bank of Temryuk river, 2 km to S from Starchenkove village

Magnetite iron content 23-29% Metamorpho-

genic 100

II-1-31 Krushanlynskiy; 1 km to SE from Mokriy Stav village

Oxide iron content 29.04-54.72%, magnetite iron content from 23 to 35.6% at 30% avg.


II-1-32 Tarasivskiy; Tarasivka village

Oxide iron content 30-40% Metamorpho-genic 117, 92

II-4-62 Sachkynskiy; 1.5 km to E from Sachky village

Magnetite iron content 28.9% Metamorpho-genic 100

II-4-68 Kirovskiy; Kalaytanivka village

Magnetite iron content 25.5%, by mineralogical analysis magnetite content 304 kg/m3

Metamorpho-genic 71

III-4-144

Balka Kruta; upper course of Kruta gully, to W from Radyvonivka village

Content of FeO 13.96%, Fe2O3 34.34%Metamorpho-

genic 58

III-4-145 Radyvonivskiy; to W from Radyvonivka village

Content of FeO 17.6-28.67%, Fe2O3 2.58-15.15% Metamorpho-

genic 58

III-4-146 Mogyla Shol; 6.4 km to E from Radyvonivka village

Content of Fe2O3 25.61% Metamorpho-genic 58

III-4-147 Zasorina gully; to NE from Osypenko village

Content of FeO 22.87%, Fe2O3 15.10% Metamorpho-genic 58

124

1 2 3 4 5

III-4-150 Olginskiy; to W from Osypenko village

Two beds of ferruginous quartzites 1-4.3 m thick, 250-300 m long

Metamorpho-genic 58

IV-1-151 Inzivskiy; Lozovatka river, Inzivka village

Average iron content 36.4% Metamorpho-genic 59, 95

IV-1-153 Orlovskiy-2; left slope of Lozovatka river to S from Orlivka village

Siderite content 37.3-222.3 kg/t, ilmenite 13.6-225.0 kg/t Weathering crust 59

IV-1-155 Orlovskiy-1; to E from Orlivka village

Magnetic anomaly 4000 gamms Metamorpho-genic 59, 95

IV-3-157 Lunacharskiy; left slope of Kutsa Berdanka river, Lunacharske village

Kaoline enrichment with siderite to 342.2 g/t Weathering crust 59

Non-ferrous metals Copper

Occurrence

I-3-17 Gusarka gully; 2.8 km to E from Oleksiivka

Copper content 1%, zinc 0.1% Plutonogenic-hydrothermal 66, 71

II-2-33

Zubivskiy; left bank of Tokmak river, 1.6 km down of Verkhniy Tokmak village

Copper content 0.63% Plutonogenic-hydrothermal 105

II-2-34 Draganova gully; Obitochne village

Copper content 1.064% Not defined 105

II-4-65 Botsman-Gora; Vyboevo village

Copper content 1.46%, zinc 0.02%, lead 0.002%


III-2-143 Yuryivskiy; upper course of Bogorodytska gully, Yuryivka village

Copper content attains 1% Plutonogenic-hydrothermal 117

Nickel, copper Occurrence

II-2-35 Bila gully; Obitochne village, right bank of Bila gully

Copper content attains 1.51%, nickel 0.47%, chromium 0.17%. By gold spectrometry gold content 0.05 g/t

Magmatic-immiscible 117

Nickel Occurrence

I-1-1

Novomykhaylivskiy; 1 km to NE from Novomykhaylivka village

Nickel content 0.6%, chromium 0.16%, copper 0.02% Magmatic-

immiscible 61

II-3-44 Reven khutor Nickel content 0.17-0.3%, chromium 0.14-0.16%


II-3-46 Kamyshuvata gully; Andriivka village

Nickel content up to 0.5%, cobalt 0.03%, chromium 3%, tungsten 0.01%


II-3-53 Mogyla Zelena; Kiltychiya river, Andriivka village

Nickel content attains 0.36-0.6%, gold 0.02-0.1 g/t Magmatic-

immiscible 71

II-3-61 Ivanivskiy; Ivanivka village

Nickel content 0.09-1.2%, copper 0.58%, silver 10 g/t, gold 0.15 g/t


III-4-104 Osypenkivskiy; Osypenko village

Nickel content 0.26-0.46% Magmatic-immiscible 58

IV-1-156 Arapka village; left bank of Arapka gully, Preslav village

Nickel content from 0.05 to 0.5% Magmatic-immiscible 59

125

1 2 3 4 5 Rare metals

Tungsten Occurrence

I-2-141 Mogyla Dovga Popovka; to W from Vershyna-2 village

Tungsten content 0.2% Plutonogenic-hydrothermal 91

II-3-54 Samsonova gully; Andriivka village

Tungsten content 0.3%, rubidium 0.066%


II-4-69 Kirovskiy; left bank of Berda river, Kalaytanivka village

Scheelite content 400 g/t (WO3 in scheelite 74.9%), tungsten 0.06-0.1% Skarn 71

II-4-74 Krymska gully; Mykolaivka village

Tungsten content 0.15-0.2%, silver 9-20 g/t


Molybdenum Occurrence

III-2-83 Dolynskiy; Chokrak river, Dolino village

Molybdenite content in polished section 3%, by chemical analysis molybdenum content 0.084-0.232%


Niobium, tantalum, lithium Deposit

III-4-99 Kruta Balka; to SW from Radyvonivka village


Niobium, tantalum Occurrence

III-4-148

Sadova site; upper course of Zasorina and Gondzhugova gullies, Osypenko village

Content of Ta2O5 0.0075-0.158%, gold 0.1-1.0 g/t Pegmatite 68

III-4-106

Osypenkivskiy; left bank of Berda river; W outskirt of Osypenko village

Niobium content in the range 0.2%

Pegmatite 111

Rubidium, niobium, tantalum Occurrence

III-4-96 Dovzhyk gully; right bank of Berda river, Radyvonivka village

Columbite content 860 g/m3. By spectrometry rubidium content 0.41%, niobium 0.145%

Pegmatite 58

III-4-102

Blakytni Skeli; left bank of Berda river, to S from Radyvonivka village

Tantalum content 0.017%, beryllium 0.023%, cesium 0.003%, rubidium 0.07%. By mineralogical analysis columbite content 123 g/t, beryl 227 g/t, gold 0.1-0.3 g/t, silver 4 g/t

Pegmatite 58, 93

Rubidium, cesium Occurrence

III-4-93 Krymska gully; to SW from Radyvonivka village

Rubidium content > 0.1%, cesium 0.055%, tantalum 0.05%, niobium 0.01%

Pegmatite 58

126

1 2 3 4 5 Zirconium

Occurrence

II-2-36 Saltychiya river; W outskirt of Saltychiya village

Zircon content 47.97 kg/t

Pegmatite 104

IV-1-152 Preslavskiy; W outskirt of Preslav village

Content of phosphorus 10%, zircon 0.5%, yttrium 0.035%, titanium 4.1%



Deposit

III-4-101

Surozke; right bank of Berdyanske water reservoir, Sobacha gully, to N from Osypenko village

Explored, was not mined yet

Plutonogenic-hydrothermal

1, 26, 96, 5, 43, 103

Occurrence

II-3-48 Andriivskiy; Samsonova gully, to E from Andriivka village

Sulphide-quartz mineralized zones. Gold grade up to 10 g/t Plutonogenic-


III-3-58 Sorokynskiy; right bank of Burtychiya river, former Soroki khutor

Sulphide-quartz mineralized zones. Gold grade up to 3 g/t, silver 20 g/t Plutonogenic-


27

II-4-71 Berestovskiy; Karla Marksa village, right bank of Berestova river

Native gold, copper content attains 0.91% Plutonogenic-


III-4-103

Radyvonivskiy; Blakytni Skeli; left bank of Berdyanske water reservoir, to S from Radyvonivka village

Sulphide-quartz mineralized zones. Gold grade up to 10 g/t, copper 0.24-1.45%, silver 20 g/t Plutonogenic-


18

Silver Occurrence

III-3-90

Glyboka gully; left bank of Obitochna river, to S from Shevchenko village

Quartz mineralized zones.

Silver content 41-53 g/t, gold occurs in amount of 0.6 g/t

Plutonogenic-hydrothermal 34, 121

III-4-98 right bank of Kruta gully; to SW from Radyvonivka village

Telluric silver content 600 g/t. By spectrometry lead content 12%, zinc 0.05%, bismuth 0.06%


Rare-earth metals Cerium, lanthanum

Deposit

I-4-22

Mogyla Visla; right bank of Temryuk river, Starchenkove village

Monazite occurs together with zircon, zircon content in rock 10-15 kg/t.

Minor mining in the past

Pegmatite 70

Occurrence

I-4-20 Karatyutskiy; right bank of Karatyuk river, Bilotserkivka village

Monazite content 12.36 kg/m3, zircon 12.09 kg/m3 Pegmatite 72, 73

127

1 2 3 4 5

I-4-23 Temryutskiy; right bank of Temryuk river, to S of Mogyla Visla

Monazite content 12.36 kg/m3 Pegmatite 70

II-1-30

Krushanlynskiy; left bank of Krushanly river, 1 km to SE from Mokriy Stav village

Metasomatically altered rocks.

Lanthanum content 0.5%, cerium 0.1% Plutonogenic-hydrothermal 70

II-2-39

Mogyla Saltychiya; right bank of Saltychiya river, to W from Sakhno village

Rare earth content: dysprosium and lanthanum 4.66%, yttrium and ytterbium 3.49%, cerium 4.61%, titanium 1%, beryllium 0.05%

Endogenous 117

II-3-50 Chervona Girka; mouth of Bezimenna gully, Andriivka village

Monazite concentration attains 21739 g/t Pegmatite 104

II-3-142

Malynivskiy; left bank of Burtychiya river, to W from Malynivka village

Content of orthite 2074 g/t, uranium thorosilicate 56.5 g/t, uranothorium 11.7 g/t, thorite 3.9 g/t, molybdenite 129 g/t

Pegmatite 104

IV-1-154 Preslavskiy; to SE from Orlivka village

Content of lanthanum 0.3%, cerium 0.2%, yttrium 0.003%


Yttrium Occurrence

I-1-139 Petrivskiy; right bank of Kainkula gully, Petrovske village

Content of yttrium 0.1%, lanthanum 0.01% Plutonogenic-

hydrothermal 61

II-3-47

Kamyshuvata gully; Andriivka village

Yttrium content 0.35%.

By mineralogical data xenotime content 6994 g/t, monazite 291 g/t, uraninite 60 g/t, magnetite 102 kg/t

Pegmatite 104, 27

Non-metallic mineral resources Non-ore raw materials for metallurgy

Refractory raw materials Sillimanite, corundum

Deposit

I-2-12 Dragunske; to S from Zori khutor


Metamorpho-genic

91, 122, 123

Flux raw materials Staurolite Deposit

III-4-97 Osypenkivske; to W from Radyvonivka village



Chemical raw materials Agro-chemical raw materials

Apatite Deposit

I-1-140

Novopoltavske; to N from Chernigivka village, to S from Grygorivka village

Explored with economic reserves, was not mined yet Endogenous 13, 14,

28, 90

128

1 2 3 4 5 Occurrence

II-1-29 Begim-Chokrakskiy; Chernigovo-Tokmatske village

Eight carbonatite veins 0.1-12 m thick Endogenous 35, 105

II-2-37 Saltychiya village; western part

Apatite content 15-20% Endogenous 117

Non-metal ore commodities Abrasive raw materials

Technical diamond Occurrence

II-4-63

Velyka Ternova gully; to E from Sachky village, Velyka Ternova gully, right branch of Berda river

In two samples chromospinelides and three fragments of ice-colour diamond found Endogenous 67

III-1-75

Zelenivskiy; Lozovatka river, Zelenivka village

Fragment (0.32 by 0.25 by 0.22 mm) of ice-colour diamond in thermal decomposition products of lamproite non-magnetic fraction

Endogenous 103

III-2-88

Kolarivskiy; Lozovatka river, Kolarivka village, “Mriya” pipe

In deluvial-alluvial sediments and in lamproites of “Mriya” pipe more than hundred of diamond fragments encountered

Endogenous 103

III-2-89 Anomaly No. 4; SE part of Kolarivka village

One diamond grain is found in re-deposited weathering crust Endogenous 103

III-3-91 Andriivskiy; Andriivskiy quarry, Kiltychiya river, Andriivka village

In thermal decomposition products of lamproites from dykes 0.15 mm diamond fragment found

Endogenous 103

Electric- and radiotechnical raw materials Graphite Deposit

I-4-25 Temryutske; Temryuk river, Starchenkove village


genic 70, 77

I-4-26 Karatyutske; Karatyuk river, Sadove village



II-4-64 Sachkynske; Berda river, Sachky village



II-4-66 Troitske; Karla Marksa village



Occurrence

I-4-28 Lugivskiy; Berda river, Lugove village

Total thickness of ore zone 13-140 m Metamorpho-genic 70

II-4-72 Berestovskiy; Berestova river, to SE from Karla Marksa village

Graphite content 8.92-9.47% Metamorpho-genic 71

129

1 2 3 4 5 Adsorptive raw materials

Vermiculite Deposit



III-4-100



Occurrence

I-4-21 Temryutskiy; Temryuk river, to S from Temryuk village


II-4-70 Kirovskiy; right bank of Berda river, Kalaytanivka village


II-4-73 Berestovskiy; mouth part of Berestova gully


III-2-87 Kolarivskiy; right bank of Lozovatka river, Kolarivka village


III-4-94 Mykolaivskiy; left bank of Berda river, down of Vodyana gully mouth


III-4-149 Olginskiy; to N from Olginka village

Vermiculite content 10% at vol. weight 356-795 kg/m3 Weathering crust 48

Facing raw materials Ornamental stone

Granite, gabbroids, marble Deposit

I-2-13 Dragunske; Mokra Konka river, to N from Zorya khutor

Explored with economic reserves, in production Endogenous 91, 123

II-2-38 Kamyana Mogyla; Saltychiya river, to W from Sakhno village

Explored with economic reserves, in production Endogenous 91

II-3-52 Andriivske; Chabanska gully, Andriivka village


Occurrence

II-4-67 Kalaytanivskiy; Berda river, Kalaytanivka village

Total thickness of calciphyres and marbles 11-30 m Metamorpho-

genic 50

Construction raw materials Glass and porcelain-faience raw materials

Primary kaoline Occurrence

I-1-2 Novokazankuvatskiy; Novokazankuvate village


Pegmatite Deposit

II-2-40 Sosykulatske; Chokrak river, Dakhno khutor


130

1 2 3 4 5

II-2-41 Eliseivske; Chokrak river, Eliseivka village


124

II-2-42 Dalnya Kamchatka ; Bagy gully, Eliseivka village


124

II-2-43

Balka Velykogo Taboru; right slope of Velykogo Taboru gully, Eliseivka village

Explored with economic reserves, in production Pegmatite 73, 105,

124



124

II-3-51 Kamyana Skelya; Kiltychiya river, Andriivka village


124

II-3-55 Krynychne; Kiltychiya river, NW outskirt of Uspenivka village


124

II-3-56

Krasnogorivske; Kiltychiya river, NW outskirt of Uspenivka village


II-3-57 Sorokynske; Burtychiya river, Durna gully mouth


II-3-59 Uspenivska; Kiltychiya river, mouth part of Vodyana gully


II-3-60 Verbove; right bank of Burtychiya river


III-2-80 Zelena Mogyla; Chokrak river, Elyseivka village

Exhausted Pegmatite 73, 105, 124

III-2-81

Obitochnenske; right bank of Obitochnenska river, in front of Shevchenko village


III-2-82 Balka Glyboka; bank of Chokrak river, Elyzavetivka village


124

III-2-84 Dolynske; right bank of Chokrak river, Dolynske village


Quarry-stone raw materials Intrusive, metamorphic and sedimentary rocks

Deposit

I-1-5 Stulnivske; left bank of Tokmak river, Kamyanka village

Explored with economic reserves, is mined for crushed stones, gruss Metamorpho-

genic 73

I-2-14 Novopoltavske; watershed of Tokmak and Konka rivers

Explored with economic reserves, in production Metamorpho-

genic 73

I-3-15 Tsarekostyantynivske; to N from Trudove village


Metamorpho-genic 73

131

1 2 3 4 5

I-3-16 Kuybyshivske; N outskirt of Trudove village


Metamorpho-genic 73

I-4-27 Sadove; Karatyuk river, Sadove village


III-1-76 Zelenivske; Lozovatka river, Zelenivka village



III-2-85 Yuryivske; Lozovatka river, Yuryivka village

Explored with economic reserves, in conservation


III-2-86 Kolarivske; Lozovatka river, Kolarivka village

Exhausted Metamorpho-genic 105

III-3-92 Beryanske; Kiltychiya river

Explored with economic reserves, in conservation Endogenous 73

III-4-105 Osypenkivske; Berda river, Osypenko village

Is mined for gruss in road construction purposes Endogenous 73

Waters

Underground waters

Mineral waters

Occurrence

III-4-95 Radyvonivskiy; 0.6 km to N from Radyvonivka village

Mineral waters similar to Moskovskiy type Fractured mineral

waters 109

132


map of mineral resources in weathering crust


map




Notes (references

cited)

1 2 3 4 5


Iron ores Occurrence

153 Orlovskiy-2; left slope of Lozovatka river to S from Orlivka village

Siderite content 37.3-222.3 kg/t, ilmenite 13.6-225.0 kg/t Weathering crust 59

157 Lunacharskiy; left slope of Kutsa Berdanka river, Lunacharske village

Kaoline enrichment with siderite to 342.2 g/t Weathering crust 59

Non-metallic mineral resources Non-ore raw materials

Adsorptive raw materials Vermiculite

Deposit

45 Andriivske; Kamyshuvata gully, Andriivka village


100



Occurrence

21 Temryutskiy; Temryuk river, to S from Temryuk village


70 Kirovskiy; right bank of Berda river, Kalaytanivka village


73 Berestovskiy; mouth part of Berestova gully


87 Kolarivskiy; right bank of Lozovatka river, Kolarivka village


94 Mykolaivskiy; left bank of Berda river, down of Vodyana gully mouth


149 Olginskiy; to N from Olginka village

Vermiculite content 10% at vol. weight 356-795 kg/m3 Weathering crust 48

133

1 2 3 4 5 Construction raw materials

Glass and porcelain-faience raw materials Primary kaoline

Occurrence

2 Novokazankuvatskiy; Novokazankuvate village


134

Annex 5. List of geological landmarks

Number Name Location Altitude, m Nature-protection

status Landmark type

1 Tokmak-

Mogyla (Synya Gora)

Novopoltavka village, 1.2 km to NE; ZO-ChA.

270 Local-rank nature landmark

Mineralogical, petrographic

2 Mogyla Visla Maryanivka village, 0.6 km to SE; DO-VoA.

129 Local-rank nature landmark


3 Mogyla Kuksungur

Starchenkove village, 0.42 km to S; ZO-PrA

118 Local-rank nature landmark since 1972, square 3 hectares

Stratigraphic

4 Korsak-Mogyla

Manuylivka village, 1.3 km to S; ZO-PrA


Stratigraphic

5 Elyseivskiy quarry

Elyseivka village, S outskirt; ZO-PrA



6 Skelya Sova Pymonova

Kalaytanivka village, SW outskirt; ZO-BeA

70 Local-rank nature landmark since 1972, square 0.5 hectare

Landscape

7 Granite Cliffs Mykolaivka village, 0.6 km to NW; ZO-BeA


Landscape

8 Mountain Ridge

Kalaytanivka village, 0.9 km to SE; ZO-BeA


Geo-morphologic

9 Granite Cliffs Mykolaivka village, 1.4 km to SE; ZO-BeA


Landscape

10 Crystal Cliff Radyvonivka village, 0.5 km to N; ZO-BeA


Landscape

11 Quartzite Cliff Radyvonivka village, 0.9 km to W; ZO-BeA


Landscape

12 Blakytni Skeli

Radyvonivka village, 2.3 km to S, left bank of Berda River; ZO-BeA

22 Local-rank nature landmark Landscape

Notes: all landmarks are located in Pryazovskiy block of Ukrainian Shield. ZO – Zaporizka Oblast, DO – Donetska Oblast, ChA – Chernigivskiy area, VoA – Volodarskiy area, PrA – Pryazovskiy area, BeA – Berdyanskiy area.

135

Annex 6. List of organic remnants shown in "Geological map and map of mineral

resources in pre-Quaternary units" Number in map

Drill-hole number

Author of report, paleontologist Remnant names Defined age

1 10238 M.I.Lebedev, 1966, I.M.Yamnichenko

Ferganoconcha sibirica Tcheri Ferganoconcha shabarovi Tcheri

Undivided Lower-Middle Jurassic

2 315 Tsukanov, 1967, O.V.Komarova

Mactra caspia Eichw. Mactra bulgarica Toul. Upper Sarmatian

3 1/160 G.L.Kravchenko, 1962 O.I.Mykolaivka

Dreissensia rostri formis Desh. var. akmanaica Andrus.

Cimmerian regio-stage

4 30/26 G.L.Kravchenko, 1962 L.A.Digas Cibicides aktulagayensis Vass. Upper Cretaceous

136

STATE GEOLOGICAL MAP OF UKRAINE

Scale 1:200 000

Central-Ukrainian Series Map Sheet L-37-VII (Berdyansk)

EXPLANATORY NOTES

Authors:

B.V.Borodynya, I.L.Knyazkova, K.Yu.Esypchuk, E.B.Glevaskiy, Zh.V.Chubar, T.Ya.Ivanenko

Editor of Series: K.Yu.Esypchuk

Editors:

P.F.Gozhyk, B.Yu.Zosymovych, E.B.Glevaskiy

Expert of Scientific-Editorial Council: R.M.Dovgan, leading geologist, Pravoberezhna Geological Expedition, SRGE “Pivnichgeologia”

Published according to the decision of Scientific-Editorial Council of the Department of Geology and Subsurface Use of the Ministry of Ecology and Natural Resources of Ukraine

on December 18, 2003 (Protocol No. 139)

Chief of Publishing Center O.K.Bobrovnikova Editor G.G.Golubeva Literature Editor L.G.Morgun Technical Editor K.N.Koliychuk Corrector I.A.Nagornykh Computer arrangement L.A.Svyntsova, A.V.Volkogon

English translation and computer arrangement B.I.Malyuk (2008)

Published by UkrSGRI. Registration Certificate Series DK No. 182 of 18.09.2000

Address: UkrSGRI Publishing Centre, 04114, Kyiv-114, Autozavodska Str., 78A

Tel.: 206-35-18; tel./fax: 430-41-76

STATE GEOLOGICAL MAP OF UKRAINEgeoinf.kiev.ua/kartograma/l37-7/pz_l37-7_eng.pdf · Lozovatka, Korsak, as well as eastern branches of Molochna River. Dnipro River basin includes the

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