New finds of middle and late jurassic radiolarians in the siliceous-clayey and clastic rocks of the Nadan'khada-Bikin terrane (Jurassic accretionary wedge, western Sikhote Alin) and

ISSN 1819�7140, Russian Journal of Pacific Geology, 2011, Vol. 5, No. 6, pp. 518–530. © Pleiades Publishing, Ltd., 2011.Original Russian Text © I.V. Kemkin, A.N. Filippov, 2011, published in Tikhookeanskaya Geologiya, 2011, Vol. 30, No. 6, pp. 43–56.

518

† INTRODUCTION

The Sikhote Alin fold system comprises many ter�ranes of the Jurassic accretionary wedge (Fig. 1),which was formed during 50 Ma due to the successiveunderplating of Paleopacific sequences of differentages and lithologies beneath the eastern margin of thePaleoasian continent in response to the subduction ofthe oceanic lithosphere [3–5, 9–13, 15, 20, 22, 23, 27,29]. The previous lithobiostratigraphic and structuralinvestigations revealed that these terranes are com�posed of multiply alternating tectonic slices made upof pelagic and hemipelagic sediments, detrital rocksformed in near�continental environments of theancient ocean, fragments of oceanic seamounts, andchaotic olistostrome complexes. The micropaleonto�logical analysis of the rocks from these slices made itpossible to reconstruct the fragments of primary suc�cession of accreted paleo�oceanic sediments [6–8, 17,18]. Their lower parts are composed of pelagic cherts,which are gradually replaced higher in the section firstby hemipelagic siliceous–clayey and then terrigenousrocks formed in near�continental environments. Suchstratigraphic successions, which were termed oceanicplate stratigraphy sequences [26, 28], reflect the sedi�mentation history on the oceanic plate since its initia�

† Deceased.

tion in the spreading ridge till its burial in the subduc�tion zone. Each of these successions bears certaininformation. For example, cherts characterize pelagicsedimentation; hemipelagic rocks (siliceous mud�stones, mudstones, and silty mudstones) reflect theapproach of the oceanic plate to the convergentboundary; and terrigenous varieties, which weredeposited in the trench, mark the onset of the oceanicplate’s subsidence in the subduction zone and, corre�spondingly, the subsequent accretion of its sedimen�tary cover fragments. Consequently, knowing the ageof the rocks from the upper parts of these siliceous–terrigenous successions in different tectonic slices ofthe accretionary wedge, we can determine the timingof the accretion in different oceanic fragments andstratify the wedge into tectono�stratigraphic units thatcharacterize the particular stages in its formation.Being correlated between each other, these units maybe used for reconstructing the accretion and formationhistory of the accretionary wedge and, thus, for speci�fying the structure of both the wedge proper and itsdistribution area.

Three section types are definable in the terraneunder consideration [12]: the Ulitka�type sectionscorresponding to the lower structural level of thewedge and composed of Middle–Upper Jurassic tran�sitional siliceous�to�terrigenous rocks, the structurally

New Finds of Middle and Late Jurassic Radiolarians in the Siliceous–Clayey and Clastic Rocks of the Nadan’khada–

Bikin Terrane (Jurassic Accretionary Wedge, Western Sikhote Alin) and Their Geological Significance

I. V. Kemkin and A. N. Filippov†

Far East Geological Institute, Far East Branch, Russian Academy of Sciences, pr. 100�letiya Vladivostoka 159, Vladivostok, 690022 Russia

e�mail: [email protected] September 25, 2010

Abstract—The lithostratigraphic analysis of the paleo�oceanic sediments in the Bikin segment of theNadan’khada–Bikin terrane of the Jurassic accretionary wedge revealed late Bajocian and early to middleBathonian radiolarians in the siliceous–clayey rocks constituting its southern part in the Perepelinaya–Cher�emshanka and Kedrovka areas. Siltstones from the central part of the Bikin segment in the upper reaches ofthe Vasil’eka River contain radiolarians of the terminal late Tithonian age. Combined with the known datesavailable for siliceous–clayey rocks from the western part of the Nadan’khada Alin Range and the Ulitka–Zolotoi Klyuch area, these data made it possible to define three stages in the formation of the Bikin segmentof the Nadan’khada–Bikin terrane of the accretionary wedge: the terminal Middle Jurassic, the late Titho�nian, and the Berriasian. The formation of this segment lasted approximately 25 Ma.

Keywords: siliceous–clayey rocks, radiolarians, Nadan’khada–Bikin terrane, Jurassic accretionary wedge,Sikhote Alin.

DOI: 10.1134/S1819714011060066

RUSSIAN JOURNAL OF PACIFIC GEOLOGY Vol. 5 No. 6 2011

NEW FINDS OF MIDDLE AND LATE JURASSIC RADIOLARIANS 519

uppermost Khor�type successions consisting of LowerJurassic siliceous mudstones, and the intermediateUssuri�type sequences (presumably the Middle Juras�sic in age). New finds of Middle Jurassic radiolariansin siliceous–clayey rocks from the southern part of theBikin segment and their Late Jurassic taxa in siltstonesfrom its central area allow the age and structure of theupper parts of oceanic sections in the Nadan’khada–Bikin terrane to be specified with better substantiateddiscrimination of the three tectono�stratigraphic unitsand the corresponding stages of the accretionarywedge’s development.

REGIONAL POSITION OF THE STUDIED AREA AND ITS INVESTIGATION HISTORY

The Nadan’khada–Bikin terrane extends along thenorthwestern margin of the wedge�shaped salient ofthe Bureya–Jiamusi–Khanka superterrane in theform of a NE�trending band up to 60 km wide and350 km long (Fig. 1). In the west and southeast, it isseparated from the latter and, partly, the Samarka ter�rane of the Jurassic accretionary wedge by theDakhechjen and Mishan–Fushun–Alchan faults,respectively. Its northern boundary with the Kha�barovsk terrane of the Jurassic accretionary wedgecoincides with the Laolikhe fault. The boundary withthe Early Cretaceous Zhuravlevka–Amur terrane ofthe near�continental pull�apart turbidite basin is rep�resented by a large tectonic fracture extending parallelto the Mishan–Fushun–Alchan fault. The UssuriRiver valley divides the terrane in two segments: thesouthwestern (the Nadan’khada in China) and north�eastern (Bikin).

The Nadan’khada–Bikin terrane is composed ofstacks of tectonic slices represented by Triassic–Juras�sic cherts, some of which enclose lenses of Upper Tri�assic limestones; Middle–Upper Jurassic to LowerCretaceous terrigenous rocks; and olistostromes withblocks and fragments of Upper Paleozoic limestones,basalts, and Triassic cherts (Fig. 2). The central part ofthe Bikin terrane contains widespread meimechite–picrite volcanics, while the northwesternNadan’khada Range hosts Mesozoic Zhaokhe ophio�lites [12, 20, 21, 24, 36]. All these volcanogenic–sili�ceous–terrigenous rocks are deformed into different�amplitude compressed asymmetrical folds of north�eastern (or near�meridional to northwestern in thesouthwestern part) strike (Fig. 2). In the central andeastern parts of the area under consideration, the axialsurfaces of the folds are characterized by the north�western vergence and southeastward inclined foldingplane. In the western part of the area, the axial surfacesof folds are, in contrast, inclined southeastward, whilethe folding plane gently dips in the northwesterndirection. The inversion of the axial fold surfaces in thecentral and eastern parts of the area is determined bythe flexural bending of the layers in the Jurassic accre�tionary wedge in response to the sinistral displacementof the Bureya–Jiamusi–Khanka superterrane margin

along the Mishan–Fushun–Alchan fault. Thus, judg�ing from the general structural position of the rocksconstituting the Nadan’khada–Bikin terrane (thegeneral dip of the layers, the vergence of the axial foldsurfaces, and the incline of the folding plane in differ�ent areas), its central and northeastern parts are com�posed of rocks constituting tectonic slices from thelowermost level of the terrane, while the southeastern,southwestern, and western parts consist of rocks repre�senting slices from its upper level (Fig. 3).

According to [1], siliceous mudstones outcroppingin the quarry developed along the Ignat’evka–Nizh�nemikhailovka road near the bridge across the Pere�pelinaya River (Area 1 in Fig. 2) in the southern part ofthe Bikin segment of the terrane (upper reaches of theCheremshanka and Perepelinaya rivers) contain the

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Fig. 1. Teranes of central Sikhote Alin and the adjacentregions (modified after [29]).(1) Bureya–Jiamusi–Khanka superterrane: (BR) Bureya,(KHN) Khanka, and Jiamusi (JM) blocks; (2) segments (ter�ranes) of the Jurassic accretionary wedge: (SM) Samarka,(NB) Nadan’khada–Bikin, (KHB) Khabarovsk, (BD)Badzhal; (3) Zhuravlevka–Amur (ZHR) Early Cretaceousterrane of the near�continental pull�apart turbidite basin;(4) Kema (KM) terrane of the Barremian–Albian island arcsystem; (5) Kiselevka–Manoma (KS) terrane of the Hau�terivian–Albian accretionary system; (6) left�lateral strike�slip faults including the following (encircled letters): (CSA)Central Sikhote Alin, (AR) Arsen’ev, (MFA) Mishan–Fushun (Alchan), (KCH) Katen–Chuken, (KR) Kurskii,(L) Laolikhe, (D) Dakhechjen; (AM) Amur and (KU)Kukan fault zones; (7) thrusts.

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Bajocian–Bathonian radiolarian assemblage identi�fied by E.A. Dorukhovskaya under a binocular micro�scope. The last researcher determined the Middle–Late Jurassic radiolarian assemblage from the silt�stones outcropping 3 km southwest of the previouslocality as well. We collected additional material andspecified the age by an electron microscopic study ofthe microfauna. Late Jurassic radiolarians were alsofound in siliceous–clayey rocks from the central partof the Bikin segment of the terrane on the watershedbetween the Vasil’evka River and the Pad PervayaRavine [16]. Recently, siltstones from the last areayielded the first radiolarians terminal late Tithonian inage. All these data made it possible to outline morereliably the formation period of the tectono�strati�

graphic units and correlate them with the coeval com�plexes outcropping in the Zolotoi and Shichang(China) creek valleys.

STRUCTURE AND AGE OF THE SILICEOUS–CLAYEY AND TERRIGENOUS SEQUENCES

IN THE BIKIN SEGMENT ACCORDING TO NEW FINDS OF MIDDLE AND LATE

JURASSIC RADIOLARIANS

The geological mapping in the southern part of theBikin segment of the Nadan’khada–Bikin terrane [1]defined the Lower Triassic–Upper Jurassic siliceoussequence of the Burlit allochthon and the Middle–Upper Jurassic olistostrome sequence (Fig. 4).

Folding plane

Fold

Axial plane

Distribution area of rocks constituting

Distribution area of rocks constituting

Distribution area of rocks

Folding plane

Fold

Axial plane

constituting the lowerstructural level

the middle structural level

the upper structural level

Fig. 3. Spatial geometry of the main structural attitude elements in rocks of the Nadan’khada–Bikin terrane.

Fig. 2. The schematic geological structure of the Nadan’khada–Bikin terrane with indication of the areas subjected to the lithos�tratigraphic investigation of siliceous–clayey rocks (modified after [2, 19, 36]).(1) Quaternary sediments; (2) Neogene basalts; (3) Cenozoic terrigenous terrestrial sediments; (4–7) volcanics: (4) Paleogeneandesites, (5) Late Cretaceous andesitic tuffs, (6) Late Cretaceous rhyolites and their tuffs, (7) Albian–Cenomanian basalts andandesites; (8–12) terrigenous shallow�water facies: (8) Albian, (9) Aptian–Albian, (10) Berriasian (?)–Valanginian, (11) Titho�nian–Berriasian, (12) Late Triassic; (13–15) rocks of the Nadan’khada–Bikin terrane of the Jurassic accretionary wedge:(13) terrigenous, (14) siliceous, (15) volcanogenic; (16) blocks of Upper Paleozoic limestones; (17) layers of Upper Triassic lime�stones among cherts; (18) volcano�sedimentary rocks of the Middle Cretaceous accretionary wedge of the Kiselevka–Manomaterrane; (19) Early Cretaceous granites; (20) Late Cretaceous granodiories; (21) metamorphic rocks; (22) Early Mesozoic(?) ophiolites of the Zhaokhe complex; (23) Middle Paleozoic ophiolites of the Dakhechjen complex; (24) faults; (25) areas ofthe lithostraigraphic study of siliceous–clayey rocks (encircled numbers): (1) Perepelinaya–Cheremshanka, (2) Kedrovka,(3) Vasil’evka–Pad Pervaya, (4) Zolotoi, (5) Shichang.

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According to the last researchers, the siliceoussequence 250–350 m thick is made up of cherts andsiliceous mudstones alternating with subordinatebasalts and dolomites. They noted that the cherts andsiliceous–clayey rocks contain Early Triassic con�odonts as well as Middle Triassic and Middle–LateJurassic radiolarians. The olistostrome sequence1200–1300 m thick consists of massive siltstones andtheir varieties with signs of roiling blocks and frag�

ments of cherts, sandstones, basalts, and Paleozoiclimestones. The siltstones are intercalated with sand�stones and basaltic flows. Middle–Late Jurassic radi�olarians are found in the matrix of the sequence.

The fragments of these sequences were studied inthe outcrops along the Ignat’evka–Nizhne�mikhailovka road between the Perepelinaya River andthe Cheremshanka–Ilyukhina Rechka river watershed(Area 1 in Fig. 2, Fig. 5a). Their attitude parameters,

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Fig. 4. The geological map of the southern Bikin segment of the Nadan’khada–Bikin terrane (based on materials from [1]).(1) Pliocene basalts of the Shufan Formation; (2) Eocene–Miocene detrital rocks with brown coals; (3) Alchan Formation(upper Albian): tuffs, andesite lavas and lava breccias, tuffaceous conglomerates; (4) Strel’nikovo Formation (middle–upperAlbian): sandstones, siltstones, gravelstones, rare conglomerates; (5) undivided Assikaev Formation: (Aptian–middle Albian):sandstones, siltstones, gravelstones; (6) Norian sandstones, siltstones, tuffaceous siltstones, conglomerates, and tuffites withintercalations of ash tuffs and hard coals; (7) Middle–Upper Jurassic siltstones and sandstones; (8–10) Jurassic accretionarycomplex: (8) Middle–Upper Jurassic olistostrome sequence, (9) blocks of Upper Paleozoic limestones, (10) Lower Triassic–Upper Jurassic siliceous sequence; (11) granites; (12) granodiorites; (13) thrusts; (14) normal faults; (15) other faults; (16) atti�tude elements; (17) railway road; (18) motor road; (19) areas of detailed investigations (encircled numbers): (1) Perepelinaya–Cheremshanka, (2) Kedrovka.



textural–structural features, and composition wereinvestigated both in outcrops and polished specimensand thin sections. Radiolarians extracted with a weaksolution of hydrofluoric acid were picked manuallyfrom the residues to be examined and photographedunder a scanning electron microscope. The results ofthese investigations made it possible to specify thecomposition, structure, and age of the rocks formed inthe paleo�oceanic environments.

The cherts and siliceous mudstones outcrop in aquarry located west of the bridge across the Perepeli�naya River, where their lower boundary is tectonic andcomplicated by an odinite dike (Fig. 5b, 1). The chertsup to 20 m thick are light gray to gray, thin� tomedium�platy, and with intercalations (up to 5 mm) ofgray siliceous mudstones. The Carnian–Norian radi�olarian taxa Capnodoce sp., Capnuchosphaera sp.,Plafkerium sp., and Emiluvia sp. (identifications byE.S. Panasenko) are found in cherts from the middlepart of the member. The siliceous mudstones 10 mthick are greenish gray and red�brown and contain upto 60% radiolarian skeletons and rare silt�sized quartzgrains. The red�brown varieties constitute a lens up to2 m thick with vague boundaries in the upper part ofthe member. Abundant radiolarians originate from sil�iceous mudstones (plate, Fig. 6). The co�occurrenceof the species Stichocapsa robusta Matsuoka, Pro�tunuma turbo Matsuoka, Stichocapsa decora Rust, andTricolocapsa plicarum Yao, which first appeared in thelate Bajocian, and Cyrtocapsa mastoidea Yao, Unumatypicus Ichikawa et Yao, and Unuma latusicostatus(Aita), which became extinct in the late Bajocian [25],constrains the age of the host rocks within the lateBajocian.

The dark gray silty mudstones are exposed by anexcavation on the watershed between the Perepelinayaand Cheremshanka rivers (Fig. 5b, 2). They are incontact along the fault with red�brown cherts and con�tain 30–40% silt�sized quartz and subordinate plagio�clase fragments. Some samples exhibit discrete gentle�wavy bedding due to the presence of numerous rockclasts in thin bands. Silty mudstones enclose rare bedsof hyalobasaltic clastic lavas and sandy siltstones withfragments of volcanics and cherts. The apparent thick�ness of the rocks is 30–35 m.

In the Cheremshanka–Ilyukhina Rechka riverwatershed, the lower part of the section is representedby a member (up to 30 m) of light gray tuffaceous siltymudstones with beds of silty tuffites (Fig. 5b, 3). Thetuffites contain up to 30% silt�sized quartz and subor�dinate plagioclase grains, irregularly scattered psam�mitic (up to 2–3 mm) angular clasts of basic volcanicsand cherts, and irregularly shaped inclusions of sili�ceous tuffites. The upper part of the section (120–130 m) is composed of dark gray bedded radiolariansilty mudstones. The detrital material in the rocks isrepresented by silt�sized quartz and plagioclase clastsfrequently covered by a ferruginous film (up to 50%).The bedded structure is determined by the oriented

arrangement of the rock fragments and clay mineralsas well as by the enrichment of some microlaminaewith carbonaceous matter. Radiolarian skeletons con�stitute 20–30% of the silty mudstones. Their MiddleJurassic assemblage is obtained precisely from thisrock variety (plate). Based on the co�occurrence ofStichocapsa decora Rust, the first appearance level ofwhich corresponds to the late Bajocian, and Hsuumbelliatulum Pessagno et Whalen, which became extinctin the middle Bathonian, the silty mudstones are cor�related with the late Bajocian–middle Bathonian [25].Inasmuch as the siliceous siltstones that underlie theserocks are dated back to the Late Bajocian, they aremost likely early–middle Bathonian in age.

As a whole, the primary succession of paleo�oce�anic sediments outcropping along the Ignat’evka–Nizhnemikhailovka road in the area from the Pere�pelinaya River to the Cheremshanka–IlyukhinaRechka river watershed is interpreted as consisting ofthree members: the Lower Triassic–Middle Jurassic(?) gray and red�brown platy cherts, the upper Bajo�cian greenish gray siliceous mudstones with lenses oftheir red�brown variety (approximately 10 m), and thelower–middle Bathonian bedded silty mudstones130–150 m thick. The lower part of the member (up to30 m thick) is represented by tuffaceous silty mud�stones with clastic hyalobasalt flows and tuffite beds.No sedimentation contacts between defined membersare observable.

The similar composition and age were determinedfor the rocks exposed in the quarry on the right side ofthe Kedrovka River along the Vladivostok–Kha�barovsk road (area 2 in Fig. 2, Fig. 7), where greeneshgray siliceous mudstones approximately 15 m thickcontain the late Bajocian–early Bathonian radiolarianassemblage as well (Fig. 6, Sample Al�9). The siltymudstones are gray to greenish gray with lenticular androunded chert fragments up to 3 cm across constitut�ing 10–30% of the rocks. The thickness of the memberis approximately 100 m.

New age dates were also obtained for the terrige�nous rocks from the central part of the Bikin segmentin the Vasil’evka River–Pad Pervaya area (area 3 inFig. 2). Earlier, Late Jurassic radiolarians were foundin the silty mudstones intercalated with siltstones inthe watershed of the Vasil’evka River–Pad PervayaRavine [16]. A representative radiolarian assemblagewas also extracted from dark gray siltstones outcrop�ping for 60 km along the Bikin–Lermontovka Settle�ment road in the upper reaches of the Vasil’evka River(plate, Fig. 6). The age of this assemblage is con�strained by the first appearance of Pseudodictyomitracarpatica (Lozyniak) and the extinction level of Eucyr�tidielum pyramis (Aita) [25]. Host siltstones weredeposited in the terminal late Tithonian. Thus, in thisarea, the section is represented by Middle Triassic–Middle Jurassic cherts, Upper Jurassic clayey rocks,and upper Tithonian siltstones.

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Fig. 5. (a) Schematic position of the examined outcrops along the Ignat’evka–Nizhnemikhailovka road: (1) quarry located westof the bridge across the Perepelinaya River, (2) excavation on the watershed between the Perepelinaya and Cheremshanka rivers,(3) excavation on the watershed between the Cheremshanka and Ilyukhina Rechka rivers. (b) sketches of examined outcrops.(1) sandstones; (2) silty mudstones; (3) tuffaceous silty mudstones; (4, 5) siliceous mudstones: (4) greenish gray, (5) red�brown;(6, 7) cherts: (6) gray to greenish gray, (7) red�brown; (8) hyaloclastites; (9) odinite dikes; (10) faults; (11) attitude elements;(12) sampling sites for the radiolarian analysis, their numbers (numerator) and ages (denominator); (13) talus; (14) quarry (a)and excavations (b).

Vorona R.



Radiolarian taxa identified in the siliceous–clayey rocks and siltstones of the Bikin segment of the Nadan’khada–Bikin terrane

Radiolarian speciesSamples

Khor�2 Khor�3 A436 A03P�1/3 A02P�1/5 A02P�1/6 A02P�3/5 Al�9 Sv�3 Sv�5

Archaeodictyomitra apiarum (Rust) +Archaeodictyomitra exigua Blome + + +Archaeodictyomitra exellens (Tan) +Archaeodictyomitra minoensis (Mizutani)

cf.

Archaeodictyomitra rigida Pessagno + + + + + +Archaeodictyomitra vulgaris Pessagno +Archicapsa pachyderma Tan Sin Hok cf. cf. cf. + + + cf.Cinguloturris cylindra Kemkin et Rudenko

+

Cyrtocapsa mastoidea Yao cf. +Dictyomitrella kamoensis Mizutani et Kido

+ + + + + + cf. cf.

Eucyrtidielum pyramis (Aita) cf. cf.Eucyrtidiellum unumaense Yao cf. + + +Hsuum belliatulum Pessagno et Whalen cf.Hsuum mirabundum Pessagno et Whalen cf. cf.Napora saginata Takemura +Parahsuum offwerence (Pessagno et Whalen)

+

Parvicingula dhimenaensis s.l. Baum�gartner

+ cf. cf. cf.

Parvicingula mashitaensis Mizutani cf.Parvicingula nanoconica Hori et Otsuka cf.Pseudodictyomitra carpatica (Lozyniak) + cf.Pseudodictyomitra nuda Shaaf +Protunuma turbo Matsuoka + + + + +Sethocapsa funatoensis Aita cf. cf.Stichocapsa convexa Yao cf.Stichocapsa cribata Hinde + + +Stichocapsa decora Rust + cf. cf. +Stichocapsa japonica Yao cf. cf. + + + +Stichocapsa rodusta Yao cf. cf. cf.Thanarla brouweri (Tan) + +Transhsuum brevicostatum (Ozvoldova) + + + + + cf. cf.Transhsuum maxwelli (Pessagno) cf. + + + + + + cf.Tricolocapsa fusiformis Yao cf. + cf. +Tricolocapsa plicarum Yao cf. +Wrangellium puga (Shaaf) cf.Unima latusicostatus (Aita) +Unuma typicus Ichikawa et Yao + +

Note: Samples Khor�2, Khor�3, A436, A02P�1/3, A02P�1/5, and A02P�1/6 originate from the quarry located west of the bridge acrossthe Perepelinaya River (Area 1). Sample A02P�3/5 is from the excavation on the watershed between the Cheremshanka and Ily�ukhina Rechka rivers (Area 1). Sample Al�9 was taken in the quarry on the right bank of the Kedrovka River (area 2). Samples Sv�3and Sv�5 were collected from the outcrop along the Bikin–Lermontovka Settlement in the upper reaches of the Vasil’evka River(area 3).

TECTONO�STRATIGRAPHIC UNITS AND FORMATION STAGES

OF THE NADAN’KHADA–BIKIN TERRANE OF THE JURASSIC ACCRETIONARY WEDGE

The new data on the age and composition of the

paleo�oceanic sediments allow us to distinguish twotectono�stratigraphic units corresponding to the for�mation stages of the southern Bikin segment of theNadan’khada–Bikin terrane (an element of the Juras�sic accretionary wedge). These tectono�stratigraphiccomplexes differ in the composition of the tectonic

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KEMKIN, FILIPPOV

Plate I

1

23

45

6 7

8 9 10

11 1213 14

1516 17 18 19



blocks and the age of their constituting rocks as well asin the nature and composition of the mélange matrix[19].

The tectono�stratigraphic complex with blocks ofLower Triassic–Middle Jurassic (?) cherts, upperBajocian siliceous mudstones, and lower Bajocian–middle Bathonian silty mudstones intercalated withhyalobasaltic clastic lavas and tuffite is distributed inthe Perepelinaya–Cheremshanka watershed and theKedrovka River basin, where it constitutes, in consis�tency with the general structural patterns, the upperstructural level of the Bikin segment of the terrane.The upper Bajocian–middle Bathonian siliceous–clayey rocks of this complex indicate the arrival of theoceanic plate to the convergent boundary. Accordingto the geological mapping [1], the terrigenous rocksare the Middle–Late Jurassic in age. At the same time,recent data on the distribution of the Jurassic radiolar�ian taxa [25] imply that their assemblage extractedfrom these rocks and consisting of Stylocapsa lacrima�lis Matsuoka, Gongylothorax sakawaensis Matsuoka,Stichocapsa robusta Matsuoka, Stichocapsanaradaniensis Matsuoka, Stylocapsa hemiscostataMatsuoka, Tricolocapsa plicarum Yao, and otherscharacterizes the Bathonian–Callovian period, whichcorresponds to the onset of the accretion of paleo�oceanic complexes constituting the upper structurallevel of the Bikin segment of the terrane.

Another tectono�stratigraphic complex is definedin the Vasil’evka River–Pad Pervaya Ravine area,where it constitutes the middle structural level of theBikin segment of the terrane. Its terrigenous rocks(siltstones) are reliably dated back to the terminal lateTithonian, which corresponds to the onset of the sub�sidence of the paleo�oceanic succession in the sub�duction zone and its partial accretion. The paleo�oce�anic rocks of this complex are represented by MiddleTriassic–Middle Jurassic cherts and Upper Jurassicclays developed in this area [16].

The previously obtained data specify the structureof the Nadan’khada–Bikin terrane of the Jurassicaccretionary wedge.

The fragment of the section with gradual transi�tions from cherts to siliceous–clayey and, further, ter�rigenous rocks that compose the lower structural levelof the Bikin segment of the terrane was examined onthe watershed between the Ulitka River and ZolotoiKlyuch Creek (area 4 in Fig. 2) [19]. It includes Mid�

dle Triassic–Upper Jurassic (?) cherts with lenses ofupper Carnian–lower Norian pelitomorphic lime�stones, which are replaced upward the section bygreenish gray siliceous mudstones. On the left side ofthe Zolotoi Klyuch Creek, they contain a poorly pre�served radiolarian assemblage consisting of Archaeo�dictyomitra cf. minoensis (Mizutani), Podobursa sp.,Pseudodictyomitra cf. primitiva Matsuoka et Yao,Spongocapsula cf. perampla (Rust), Stichocapsa ex gr.cribata Hinde, and Xitus sp. The species Archaeodicty�omitra minoensis was initially described from theTithonian siliceous rocks of the Hida–Kanayama areain Japan [35]. Subsequently, its stratigraphic range waswidened to the mid�Oxfordian–uppermost Tithonian

N

S

80 m

Al�9

0

1

2

3

4

5

J2baj2�bat1

Fig. 7. Sketch of the quarry located in the right bank of theKedrovka River along the Vladivostok–Khabarovsk road.(1) silty mudstones; (2) siliceous mudstones; (3) cherts; (4)faults; (5) sampling site for the radiolarian analysis, itsnumber (numerator) and age (denominator).

Fig. 6. Some Middle Jurassic radiolarians from siliceous–clayey rocks of the Perepelinaya–Cheremshanka area and Late Jurassicradiolarians from the Vasil’evka–Pad Pervaya area.(1) Tricolocapsa fusiformis Yao, Sample Khor�3; (2) Tricolocapsa cf. plicarum Yao, Sample Khor�3; (3) Protunuma turbo Mat�suoka, Sample Khor�2; (4) Unuma latusicostatus (Aita), Sample Khor�2; (5) Stichocapsa cf. robusta Matsuoka, Sample A�436;(6) Unuma typicus Ichikava et Yao, Sample A�436; (7) Cyrtocapsa mastoidea Yao, Sample A�436, (8) Hsuum cf. belliatulum Pes�sagno et Whalen (Sample A02P�3/5); (9–10) Stichocapsa cf. decora Rust: (9) Sample A02P�1/6, (10) Sample Al�9; (11, 12) Cin�guloturris cylindra Kemkin et Rudenko, Sample Sv�3; (13) Pseudodictyomitra carpatica (Lozyniak), Sample Sv�3; (14) Eucyrtidi�ellum cf. pyramis (Aita), Sample Sv�3; (15) Archaeodictyomitra ex gr. apiarium (Rust), Sample Sv�3; (16) Archaeodictyomitraminoensis (Mizutani), Sample Sv�3; (17, 18) Pseudodictyomitra nuda Schaaf, Sample Sv�3; (19) Wrangellium puga (Schaaf),Sample Sv�5. All the bars are 10 µm.

528


KEMKIN, FILIPPOV

interval. The species Pseudodictyomitra primitiva is atype taxon of the synonymous radiolarian zone thatcorresponds to the Tithonian Stage and is establishedin Japan and the Northwest Pacific [33–35]. At thesame time, according to other researchers, the strati�graphic range of this species is substantially wider,spanning the upper Bathonian–upper Tithonian [25].The species Spongocapsula perampla is characterizedby a stratigraphic range corresponding to the mid�Bathonian–upper Tithonian [25]. Thus, the age of thesiliceous mudstones may now be estimated as rangingfrom the mid�Oxfordian to Tithonian. Additional

investigations are required to specify their age. At anyevent, these rocks are not younger than the Late Juras�sic (most likely, Tithonian), because the conformablyoverlying silty mudstones with beds of sandy siltstonescontain Early Berriasian buchias [14]. Further acrossthe Zolotoi Klyuch Creek valley, the section is contin�ued by sandstones and dark gray siltstones that formrhythms 20–40 cm thick with gravelstone intercala�tions. In the opinion of E.A. Kalinin, the gravelstonesenclose buchian shells redeposited from the lower Ber�riasian sediments [19]. Combined, all of these paleon�tological data indicate that the paleo�oceanic sedi�

Age

, M

a

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tem

Creta�

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ra

ss

icT

ria

ss

ic

Ser

ies

Lo

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Up

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Mid

dle

Stage

Berriasian

Tithonian

Kimmeridgian

Oxfordian

Callovian

BathonianBajocian

Aalenian

Toarcian

Pliensbachian

Sinemurian

HettangianRhetian

Norian

Carnian

Ladinian

Anisian

Olenekian

Induan

T e c t o n o � s t r a t i g r a p h i c c o m p l e x e s

Upper structural level Middle structural level Lower structural level

Lo

wer

Low

erU

pp

erM

idd

leceous

150

200

250

?

1 2 3 4 5 6 7 8

??

Fig. 8. Tectono�stratigraphic compexes of the Bikin segment of the Nada’khada–Bikin terrane.(1) cherts; (2) limestones; (3) siliceous mudstones; (4) mudstones; (5) siltstones with rare sandstone intercalations; (6) alternatingsiltstones and sandstones; (7) subduction mélange (olistostromes); (8) basic volcanics (basalts and hyaloclastites).



ments that form this tectono�stratigraphic unit arrivedat the subduction zone in the Tithonian (?). Judgingfrom the age of the terrigenous rocks, their accretionto the continent occurred in the Berriasian.

In the road excavation 20 km west of the ShichangSettlement in the Chinese territory (Area 5 in Fig. 2),Middle Jurassic radiolarians were found in siliceousmudstones approximately 15 m thick [31, 32]. Theyare greenish gray rocks with beds of red�brown variet�ies (up to 20 cm thick) in the upper part of the memberand inclusions of Mn�rich varieties in its lower part[30]. Middle Jurassic radiolarians are represented bythe species Eucyrtidielum ptyctum (Riedel et Sanfil�ippo), Eucyrtidiellum unumaense Yao, Guexella nudata(Kocher), Stichocapsa convexa Yao, Tricolocapsa pli�carum Yao, Tricolocapsa tetragona Matsuoka, Tricolo�capsa cf. ruesti Tan, and Tricolocapsa (?) fusiformisYao. This assemblage was previously attributed to theBathonian–Callovian [31, 32]. According to therecent data on the distribution ranges of the constitut�ing species [25], it is the late Bajocian in age. Siliceousmudstones from this area of the Nadan’khada AlinRange are reliably correlated with siliceous–clayeyrocks of the Perepelinaya–Cheremshanka section.

Thus, new finds of radiolarians and previous mate�rials allow three tectono�stratigraphic complexes to beoutlined in the Bikin segment of the Nadan’khada–Bikin terrane of the Jurassic accretionary wedge,which form its different structural levels. These com�plexes differ from each other by both the age of the sil�iceous–terrigenous rocks and, correspondingly, theiraccretion time. For example, the age of the terrigenousrocks ranges from the Bathonian–Callovian to theearly Berriasian. This means that the siliceous–terrig�enous rocks constituting the terrane represent frag�ments of the sedimentary cover overlying different�ageareas of the paleo�oceanic plate or, in other words,fragments of different�age successions of the OceanicPlate Stratigraphy Sequence type accreted to theSikhote Alin structure. It should be noted that the agesof the rocks in the defined units and, correspondingly,the accretion time of the paleo�oceanic sequencesbecome successively younger from the upper structurallevel toward the lower one (Fig. 8). As a whole, theNadan’khada–Bikin terrane’s structure is character�ized by reverse stratification of its rocks: the lowerstructural level is composed of relatively youngerrocks, the upper level is represented by older rocks,and the middle one is correspondingly formed by vari�eties of intermediate age. At the same time, the pri�mary stratigraphic succession in each complex is nor�mal (from older to younger). Such a structure of theNadan’khada–Bikin terrane resulted from the succes�sive accretion of different�age and different�faciessequences of the oceanic lithosphere. During the sub�duction of the oceanic plate, fragments of its frontal(most remote from the spreading centers and, there�fore, older) areas became accreted in the first place.They are subsequently underlain by fragments ofyounger areas of the oceanic plate to form a packet of

tectono�stratigraphic slices. Thus, the true structure ofthe Nadan’khada–Bikin terrane is interpreted as asystematic repetition of complexly deformed frag�ments of the primary sedimentary cover sectionformed by different�age (i.e., differently remote fromthe spreading center) areas of the paleo�oceanic plate,not as irregular multiple alternation of tectonic slicescomposed of different�age and different�facies paleo�oceanic sediments. The age of the siliceous–clayeyrocks in the defined complexes indicates that theseareas approached the margin of the Paleoasian conti�nent in the late Bajocian–early Bathonian, the initial(?) Late Jurassic, and the Tithonian. The stages of thesubsequent accretion inferred from the ages of the ter�rigenous rocks correspond to the terminal MiddleJurassic, the late Tithonian, and the Berriasian. Judg�ing from these data, the formation period of the Bikinsegment of the Nadan’khada–Bikin terrane lastedapproximately 25 Ma.

CONCLUSIONS

The Middle Jurassic (late Bajocian–middle Batho�nian) radiolarians were found in the siliceous–clayeyrocks constituting the southern Bikin segment of theNadan’khada–Bikin terrane of the Jurassic accretion�ary wedge in the Perepelinaya–Cheremshanka andKedrovka river areas. The siltstones outcropping in thecentral part of the segment under consideration in theexcavation along the Bikin–Lermontovka Settlementroad in the Vasil’evka River’s upper reaches containradiolarians dating them back to the terminal lateTithonian. Combined with the previous data on theage of the siliceous–clayey rocks from the western partof the Nadan’khada Alin Range and the Ulitka River–Zolotoi Klyuch Creek area, these materials allowthree tectono�stratigraphic units and the correspond�ing formation stages to be outlined for the Bikin seg�ment of the Nadan’khada–Bikin terrane of the accre�tionary wedge: the terminal Middle Jurassic, the lateTithonian, and Berriasian. The terrane was formedduring a period approximately 25 Ma long.

ACKNOWLEDGMENTS

This work was supported by the grant of the FarEast Branch of the Russian Academy of Sciences(no. 09�III�A�08�403) and the Russian Foundationfor Basic Research (project no. 09�05�00041).

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New finds of middle and late jurassic radiolarians in the siliceous-clayey and clastic rocks of the Nadan'khada-Bikin terrane (Jurassic accretionary wedge, western Sikhote Alin) and

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