New data on detrital zircons from the sandstones of the lower Cambrian Brusov Formation (White Sea region, East-European Craton): unravelling the timing of the onset of the Arctida–Baltica

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New data on detrital zircons from the sandstonesof the lower Cambrian Brusov Formation (White Searegion East-European Craton) unravelling the timingof the onset of the ArctidandashBaltica collisionNB Kuznetsovab EA Belousovac AS Alekseevd amp TV Romanyukeb

a Tectonics Geological Institute of the Russian Academy of Science Moscow Russiab Department of Theoretical Foundations and Exploration of Oil and Gas Gubkin RussianState University of Oil and Gas Moscow Russiac Australian Research Council Centre of Excellence for Core to Crust Fluid Systems (CCFS)and GEMOC National Key Centre Department of Earth and Planetary Sciences MacquarieUniversity Sydney NSW 2109 Australiad Geological Department Lomonosov Moscow State University Moscow Russiae Schmidt Institute of Physics of the Earth Russian Academy of Sciences Moscow RussiaPublished online 06 Nov 2014

To cite this article NB Kuznetsov EA Belousova AS Alekseev amp TV Romanyuk (2014) New data on detrital zircons fromthe sandstones of the lower Cambrian Brusov Formation (White Sea region East-European Craton) unravelling the timing ofthe onset of the ArctidandashBaltica collision International Geology Review DOI 101080002068142014977968

To link to this article httpdxdoiorg101080002068142014977968

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New data on detrital zircons from the sandstones of the lower Cambrian Brusov Formation(White Sea region East-European Craton) unravelling the timing of the onset of the

ArctidandashBaltica collision

NB Kuznetsovab EA Belousovac AS Alekseevd and TV Romanyukeb

aTectonics Geological Institute of the Russian Academy of Science Moscow Russia bDepartment of Theoretical Foundations andExploration of Oil and Gas Gubkin Russian State University of Oil and Gas Moscow Russia cAustralian Research Council Centre ofExcellence for Core to Crust Fluid Systems (CCFS) and GEMOC National Key Centre Department of Earth and Planetary SciencesMacquarie University Sydney NSW 2109 Australia dGeological Department Lomonosov Moscow State University Moscow Russia

eSchmidt Institute of Physics of the Earth Russian Academy of Sciences Moscow Russia

(Received 27 March 2014 accepted 26 September 2014)

The basement of the northeastern periphery of the East-European Craton (ЕЕС) is composed of volcanic-sedimentarysequences volcanic rocks granitoids and rare ophiolite complexes Geochronological data constrain their age from ca 750to 500 Ma and there is a consensus that these rocks represent relicts of a late NeoproterozoicndashCambrian Pre-UralidesndashTimanides orogeny Combining new integrated isotopic (U-Pb Lu-Hf) and trace-element data (TerraneChronereg approach)on detrital zircons from sandstones of the lower Cambrian Brusov Formation in the Mezen basin (White Sea region in thenortheastern periphery of the EEC) with available studies on detrital zircons from Neoproterozoicndashmiddle Cambrian (meta)sedimentary units of the northeastern periphery of the EEC allow us to conclude that (1) the onset of the ArctidandashBalticacollision can now be constrained to the time interval between ca 540 and 510 Ma and (2) the Ediacaranndashearly CambrianMezen sedimentary basin was a basin on the Timanian passive margin of Baltica up to 540 Ma but was not a foreland basinof the Pre-UralidesndashTimanides orogen

Keywords ArctidandashBaltica collision Mezen sedimentary basin White Sea region Neoproterozoic Ediacaran Cambriandetrital zircons U-Pb dating Hf and trace-element systematics

Introduction

The basement of the northeastern periphery of the East-European Craton (ЕЕС) is composed of complexes withvolcanic-sedimentary rocks volcanic rocks granitoidsand rare ophiolites (Beliakova and Stepanenko 1991Scarrow et al 2001 Soboleva 2004 Soboleva et al2004 2012a 2013 Remizov and Pease 2004 Udoratinaet al 2006 Andreichev et al 2007 Andreichev 2010)The metamorphic grade of these rocks varies betweengreenschist facies up to blueschist-eclogitic and amphibo-lite facies (Beckholmen and Glondy 2004 Glodny et al2004) and they are variably (at some places very strongly)deformed (Roberts and Siedlecka 2002 Larionov et al2004 Roberts and Olovyanishnikov 2004 Kuznetsovet al 2007a 2007b Kuznetsov 2008) A number of com-plexes are exposed in the Polar Urals the Timan HillsKanin peninsula and the northeastern edge of the Kolapeninsula (Figures 1 and 2) Samples were collected bothfrom exposed surface and from boreholes for detailedstudies (Kostyuchenko and Romanyuk 1997 Gee et al2000 Dovzhikova et al 2004 Baluev 2006Kostyuchenko et al 2006 Dovzhikova 2007 Kuznetsovet al 2007a) More than 250 isotopic dating analyses

(a summary of U-Pb dating of magmatic zircons andtheir inherit cores results of dating by Rb-Sr or Sm-Ndisochronic and others methods see Supplementary Table l[httpdxdoiorg101080002068142014977968] sam-ple designations see in Figure 2) obtained recently on thecrystalline complexes of ca 750ndash500 Ma age (Kuznetsovet al 2007a 2010a Orlov et al 2011 Soboleva et al2012b) There is a consensus that these rocks are relicts ofa late NeoproterozoicndashCambrian orogeny This orogeny(or its partsstages) is referred to as the TimanndashVarangerBelt (Roberts and Siedlecka 2002) Timanide orogen(Puchkov 2003 Gee and Pease 2004) Pre-UralidesndashTimanides orogen (Kuznetsov et al 2007a 2010a) andothers The relicts of the Pre-UralidesndashTimanides orogenyhave been revealed in the basement of the vast area fromthe Pechora basin and northern parts of the western Uralsto the Svalbard archipelago and from the north edge of theKola Peninsula to the central part of Novaya Zemlyaarchipelago (Figure 2)

During the last 20 years the tectonic origin of the Pre-UralidesndashTimanides orogeny has been actively discussedwith two main models challenging each other The firstmodel is abbreviated further as the TAMB model

Corresponding author Email kouznikbormailru

International Geology Review 2014httpdxdoiorg101080002068142014977968

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Pale

ozo

ides o

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Complexes of the Meso andNeoproterozoic accretionarybelts and collisional orogens

Complexes of thePaleoroterozoic

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ogue

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tern

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Figure1

Map

ofthemainbasementcomplexes

andstructures

oftheEast-Europ

eanCraton(EEC)andits

periph

eryinclud

ingblocks

ofconsolidated

basementriftstructuresand

NeoproterozoicandPalaeozoicfold-thrustbeltsmodified

from

Kuznetsov

etal(201

0a)

LatePalaeop

roterozoicndashearly

Neoproterozoiccomplexes

oftheEEC

mod

ified

from

Bog

dano

vaet

al(200

8)NeoproterozoicndashmiddleCam

briancomplexes

Pre-U

ralid

esndashT

imanides

attheeasternandno

rth-easternperiph

eryof

theEECafterKuznetsov

etal(200

7a)

Configu

ratio

nof

theWhite

Sea

RiftSystem

(WS)afterBaluev(200

6)Insetcontou

rsof

EECproto-craton

sKolaKareliaSarmatiaandVolga-U

ralia

afterRom

anyu

ketal(201

3)

Black

linendashcontou

rof

Figure2

Yellow

symbo

lsmarklocalitiesof

samples

with

stud

ieddetritalzircon

s(starwith

number6ndashthis

stud

y)nu

mbers

oflocalitiesinside

symbo

lscorrespo

ndto

numbers

inFigures

28

9and10Abbreviations

ofgraniticmassifs

(white

letters)SSalma

Vy

Vyborg

RRiga

KKorosten

KNKorsun-Novom

irgorod

Nu

Nov

o-Ukrainsk

Ma

Mazury

2 NB Kuznetsov et al

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Figure 2 Tectonic classification of the Pre-UralidesndashTimanides Blue dashed lines ndash approximate southwestern and northeasternboundaries of the Pre-UralidesndashTimanides orogen (Kuznetsov et al 2010a) The scheme is based on maps from Bogdanov and Khain(1996) and Khain (1999) Configuration of White Sea Rift System after Baluev (2006) Uplifts and anticlinoria A Amderma K Kara OOchenyrd M Manytanyrd E Engane-Pe Kh Kharbei Kha Kharamalataou Ly Lyapin Kv Kvarkush U Uraltau B Bashkir(including Taratash) E Ebeta Black circles ndash boreholes Letters in red are abbreviations corresponding to sample designations inSupplementary Table 1 Yellow symbols mark localities of samples with studied detrital zircons (star with number 6 ndash this study)numbers inside symbols correspond to numbers of localities in Figures 1 8 9 and 10

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(Timanian Active Margin of Baltica) and interprets theorogeny as a supra-subduction long-lived orogenic systemthat was active during the late Neoproterozoic on thecurrently active northeastern Timanian margin of thepalaeocontinent Baltica (see Gee and Pease 2004Kostyuchenko et al 2006) (Figure 3) The second modelis known under the abbreviation ABC (ArctidandashBalticaCollision) and was developed by Kuznetsov et al (2007a2010a) who suggested that this orogen is collisional andformed during the convergence between the Arctida andBaltica palaeocontinents (Figure 4) This collision resultedin the suturing of the composite Arct-Europe (Arctida +Baltica) palaeocontinent The relict of the suture zonebetween Arctida and Baltica (Pechora suture) is representedby the Pechoro-Ilych-Chiksha fault zone in the basement ofthe Pechora basin (Kuznetsov et al 2007a) In a number ofrecent articles (Kuznetsov 2006 Kuznetsov et al 2007a2010a 2010b 2014 Orlov et al 2011) it was argued thatthe Timanian (more exactly the VarangerndashTimanianndashUralian) margin of Baltica was a passive margin until thetime of the collision while the overriding Bolshezemelmargin of Arctida was a long-lived active margin(Kuznetsov et al 2009a 2009b) Available geochronologi-cal data for crystalline complexes of the Pre-UralidesndashTimanides orogen allows the approximate estimation thatthe Arctida-Baltica collision had to occur at a point in timeclose to the CambrianndashPrecambrian boundary

In this article we present new data (TerraneChronereg

approach) on detrital zircons from sandstones of the lowerCambrian Brusov Formation Mezen Basin White Searegion of the EEC These new data are combined withresults from previous reports on detrital zircons fromNeoproterozoicndashCambrian (meta)sedimentary rockslocated in the northeastern periphery of the EEC Thisallows us to test the TAMB and ABC models and to betterconstrain the timing of the initiation of the Arctida-Balticacollision

Background of testing of the TAMB and ABC models

The EEC is broadly divided into basements and coversequences Basement rocks have been traditionallyassigned to the early Precambrian (Archaean andPalaeoproterozoic in age Mints et al 2010 and referencestherein) while the cover sequences are late Precambrian(Mesoproterozoic and Neoproterozoic in age) or youngerHowever this two-part basement-cover subdivision is notapplicable to the western parts of the EEC where highlymetamorphosed and deformed complexes may be signifi-cantly younger in age up to 900 Ma (Bogdanova et al2008 and references therein) It is important to note that nocrystalline complexes younger than 900 Ma are knownwithin the portion of the basement of the EEC that isinterpreted as representing the Precambrian palaeoconti-nent Baltica (Figure 1) Thus any crystalline complexes of

the Pre-UralidesndashTimanide orogen that contain magmaticor metamorphic zircons with ages of 750ndash500 Ma repre-sent a unique provenance signal which we call the Pre-UralidesndashTimanides provenance signal (pU-T signal) andwhich could not have been derived from any other crystal-line complexes within Baltica

If (in accordance with the TAMB model) the north-eastern Timanian margin of Baltica was an active marginduring the late Neoproterozoic (ie the Pre-UralidesndashTimanides orogeny was a long-lasting succession of sub-duction-related events on the northeastern active Timanianmargin of Baltica) then some erosional products of thisorogeny containing the pU-T signal should have accumu-lated in sedimentary basins within Baltica (Figure 3)

If (in accordance with the ABC model) the north-eastern Timanian margin of Baltica was a passive mar-gin during the late Neoproterozoic up to the time of theArctida and Baltica collision then no pU-T signalshould be found in any late Neoproterozoic sedimentaryunits (which are autochthonous to the crystalline com-plexes of Baltica) on the northeastern margin of Baltica(Figure 4(A))

Thus the U-Pb ages of detrital zircons from (meta)sedimentary units distributed along the northeastern edgeof the EEC and covering a time span from the lateNeoproterozoic to the early Palaeozoic would providecrucial information allowing us to test the TAMB andABC models Generally the absence of the pU-T signalwould be an argument in favour of the ABC model whilewidespread presence of the pU-T signal would be suppor-tive of the TAMB model

According to the ABC model the Bolshezemel marginof Arctida was a long-lived active margin during the lateNeoproterozoic similar to the present-day Japan or South-Kuril subduction systems with volcanic arcs and back-arcbasins Because the bulk composition of magmatic rocksoriginating at volcanic arcs is of intermediate composition(ie andesites diorites quartz-diorites tonalities etchenceforth collectively termed lsquodioritesrsquo) with a lowercontent of SiO2 (less than 65) detrital zircons sourcedfrom erosional products of the Bolshezemel supra-subduc-tion accretion-type orogen should reflect bulk parentalrocks as lsquodioritesrsquo Also there should be an input ofjuvenile material (εHf 0) ie material that was directlymelted from mantle (Figure 4(A)) in the erosional pro-ducts of volcanic arcs

Within the ABC model Arctida and Baltica are thoughtto have collided during the earliest Cambrian forming thePre-UralidesndashTimanides orogen by suturing these two con-tinents (Figure 4(B)) The sedimentary complexes of theTimanian passive margin of Baltica together with frag-ments of oceanic-type crust of a back-arc basin(s) werecaught in the collisional zone and mixed with supra-sub-duction complexes of a volcanic island arc(s) of the activeBolshezemel margin of Arctida into a thrust-fold belt of the


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Figure 3 An illustration of the TAMB model (A B) Cartoon representations of interpreted setting of the northeastern margin of theFennoscandian Shield (after Roberts and Siedlecka 2002) redrawn with minimal simplifications (A) Suggested scenario during terminalRiphean to early Vendian time showing the continental margin oceanic basin bimodal arc and microcontinental blocks with inferrednortheastward subduction and early magmatism (B) Telescoping and accretion of these diverse elements against the Baltican margin inthe middle to late Vendian during and immediately following the Timanian orogenic event A reversal of subduction polarity is inferredfollowing slab break-off which led to the intrusion of late to postorogenic late Vendian calc-alkaline granites (CndashG) Cartoonrepresentations of the early Neoproterozoic to middle Palaeozoic tectonic evolution of the northeastern margin of the East EuropeanCraton (after Kostyuchenko et al 2006) (H) Schematic SWndashNE cross-section across the Pechora Basin during the Devonian (after Peaseet al 2004) Compare Timan Izhma Pechora and Bolshezemel zones with Figure 2 The late Neoproterozoic intrusion of post-tectonicgranitoids is interpreted to have occurred during passive margin sedimentation further west along the Baltoscandian margin of Baltica


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orogen In addition magmatism during the collision wouldhave generated large volumes of I- S- and A-type grani-toids intruding those amalgamations Collisional magma-tism then should have generated zircons with traceelemental signatures typical of zircons derived from rockswith a high SiO2 (more than 65) content (henceforthcollectively termed lsquogranitesrsquo)

Thus during the pre-collisional stage from ~750 to~540 Ma lsquodioritesrsquo might dominate the pU-T signal

amongst the other types of the parental rocks for detritalzircons while during the collisional stage from ~540 to500 Ma an essential input of zircons originating frommore felsic rocks (lsquogranitesrsquo) can be expected

When the collisional orogen had developed to a newhigh-standing uplift its erosional products started to betransported onto Baltica Given that no crystalline com-plexes younger than 900 Ma exist within basement ofBaltica (Figure 1) the pU-T signal could not appear in

Figure 4 A cartoon for the ABC model (A) Pre-collisional stage (~750ndash540 Ma) (B) collisional stage (540ndash510 Ma)Notes 1 ndash crust of continental type (a) basement of Baltica (b) basement of Arctida (c) possible fragments of continental crust of unknown origin in thebasement of volcanic arc(s)2 ndash crust of oceanic type (a) of Pechora ocean (a) (b) metamorphosed under low temperature and highultra-high pressure into a subduction zone(s)(c) generated into a back-arc basin(s)3 ndash volcanic and volcanic-sedimentary complexes of volcanic arc(s)4 ndash intrusive complexes (a) with higher (gt65) content of SiO2 (b) with lower (lt65) content of SiO25 ndash sedimentary complexes (a) autochthonic to Baltica basement and deposited before Arctida-Baltica collision (b) deposited within the Bolshezemelactive margin of Arctida (c) deposited within Arct-Europe after Arctida-Baltica collision6 ndash mantle7 ndash direction of plate movements8 ndash flux of erosional products9 ndash locations of samples studied for detrital zircon U-Pb ages abbreviations correspond to abbreviations of diagrams in Figures 8ndash10


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the sedimentary strata (which are autochthonic to thecrystalline complexes) of Baltica before the Pre-UralidesndashTimanide collisional orogen was createduplifted and started to erode Thus the oldest age ofthe (meta)sediments containing the pU-T signal repre-sents an upper time limit for the beginning of theArctida-Baltica collision On the other hand the young-est age of (meta)sedimentary rocks that do not containthe pU-T signal can be considered an estimated lowertime constraint for the onset of the Arctida-Balticacollision

The sampling of rock separation and imaging ofdetrital zircons

Neoproterozoic and Cambrian sedimentary complexes onthe northeastern periphery of the EEC are exposed in sev-eral localities (Figure 1) Neoproterozoic strata occur in themiddle and northern segments of the Western Urals in theTiman Hills the Kanin peninsula as well as in theVaranger Rybachiy and Sredniy peninsulas which arelocated on the northeastern edge of the Kola peninsula Avast sedimentary depocentre the Mezen basin existed inthe northeastern periphery of Baltica during the Ediacaranand early Cambrian (Martin 2000 Alekseev et al 2005Fedonkin et al 2007 Maslov et al 2008 2009) Parts of itssedimentary sequence are exposed as outcrops on theZimniy Bereg of the White Sea (Grazhdankin 2004Llanos et al 2005) and in the near-Ladoga region(Dronov et al 1995 2005 Kuznetsov et al 2011) aswell as having been intersected by several boreholes

The ALROSA-Pomorie company drilled the AL303borehole near the western edge of the Mezen basin (64deg38ʹ47 N 41deg50ʹ21 E approximately 60 km eastward fromArkhangelsk) Underneath a carbonate unit of theMoscovian Stage (Middle Pennsylvanian) the AL303 wellpenetrated a lower Cambrian succession of the PadunGroup (Figure 5) In the southeastern White Sea regionthe Padun Group is subdivided into three formations indescending stratigraphic order represented by (1) theBrusov Formation with up to 230 m of mostly red-colouredsandstones (2) the Nyugus Formation which contains 80ndash90 m of red-coloured clays with numerous interbeds ofbioturbated sandstones and siltstones and (3) the ZolotitsaFormation which is represented by about 100 m of mostlyred sandstones

The organic annulated tube-form problematic fossilsSabellidites cambriensis Yanishevsky were found in themiddle part of the Nyugus Formation both in bore holesand in outcrop (Alekseev et al 2005) This species is verycommon in upper Ediacaran (upper Vendian) and lower-most Cambrian strata of the EEC (Kirsanov 1968Sokolov 1968 Orlowski 1985 Ivantsov 1990) especiallyin the basal Cambrian Lontova Formation in the vicinityof Saint Petersburg (Yanishevsky 1926) Furthermore the

PrecambrianCambrian Global Boundary StratotypeSection and Point of the International Commission onStratigraphy located in Newfoundland falls within theSabellidites cambriensis zone (Landing et al 1989)Another problematic tubular fossil Platysolenites anti-quissimus Eichwald that has been considered as represent-ing agglutinated foraminifera (Lipps and Rozanov 1996Streng et al 2005) occurs in the middle of the NyugusFormation This species is almost exclusively confined tothe lower Cambrian Lontova Horizon in the EEC(Rozanov 1983) Furthermore sandstones of the BrusovFormation that occur as outcrops along the Bolshaya YuraRiver and in the aforementioned bore holes are burrowedby numerous large trace fossils Skolithos and

Figure 5 Generalized regional stratigraphic scheme for the south-eastern part of the White Sea region after Grazhdankin (2004)Alekseev et al (2005) and Maslov et al (2008 2009) The starindicates the stratigraphic position of the studied sample (09ndash325)from the lower Cambrian Brusov Formation Padun GroupNote that results of a study on a sample from the EdiacaranTamitsa Formation are shown as diagram B10 in Figure 9


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Diplocraterion which are typical for the Cambrian(Grazhdankin and Krayushkin 2007)

A fragment of core sample 09-325 had a diameter of~90 cm a length of ~65 cm and a weight of ~1 kg Itwas taken at a depth of 379 m in borehole AL303 andbelongs to the Brusov Formation This sample consistedof a yellow-reddish poorly sorted and poorly cementedquartz sandstone that was manually disintegrated inwater The dispersed material was washed to removeclay-size cement material and subsequently driedMaterial with a density less than 29 g cmminus3 wasremoved by heavy liquid (bromoform) separation Thefinal gt29 g cmminus3 heavy mineral concentrates weremainly composed of zircon garnet and apatite grainsZircons were further separated using MI heavy liquidthen handpicked mounted in epoxy discs and polishedThese zircon grains were imaged using CL imaging thatwas used to identify detrital domains within the grainsSample mounts were additionally imaged by back-scat-tered electron imaging to exclude grains with metamicti-zation Furthermore the zircons grains were studiedusing the TerraneChronereg approach at the GEMOCCCFS centre Macquarie University Sydney

The isotopic methods of studies of the detrital zircons(TerraneChronereg approach)

The TerraneChronereg approach combines three micro-analytical techniques applied to collect U-Pb ages Hf-isotope and trace-element compositions on individualgrains This combination makes it possible to determinefor each grain not only the age but also the nature andsource of the host magma and distinguish whether theyderived from crustal or from juvenile mantle material(Griffin et al 2004 2006 2007 Veevers et al 2005Belousova et al 2006 2009 2010) The integratedanalysis applied to suites of detrital zircon gives amore distinctive and easier to interpret picture of crustalevolution in the provenance area rather than age dataalone

U-Pb zircon dates were obtained using a New Wave213 nmNdndashYAG laser in a He ablation atmosphere coupledto an Agilent 7500cs ICP-MS More details of the analyticaltechniques can be found in Jackson et al (2004) The207Pb206Pb ratios were used to determine grain ages

Trace element abundances in igneous zircons areshown to be sensitive to the source rock type and crystal-lization environment (Belousova et al 2002) The concen-trations of 26 trace elements in zircons from a wide rangeof different rock types reveal distinctive elemental abun-dances and chondrite-normalized trace-element patternsfor specific rock types The trace-element abundance inzircons increases from ultramafic through mafic to graniticrocks The average REE content is typically less than50 ppm in kimberlitic zircons up to 600ndash700 ppm in

carbonatitic and lamproitic zircons up to 2000 ppm inzircons from mafic rocks and can reach percentage levelsin zircons from granitoids and pegmatities Relatively flatchondrite-normalized REE patterns with chondrite-nor-malized YbSm ratios ranging from 3 to 30 characterizezircons from kimberlites and carbonatites while YbSmvalues gt100 are commonly only observed in zircons frompegmatites ThU ratios typically range from 01 to 1 butcan be 100ndash1000 in zircons from some carbonatites andnepheline syenite pegmatites The geochemical signaturescharacteristic for zircon from different rock types can beeasily identified with the help of the program CARTwhich is based on principles of multivariate statisticalanalysis (see details in Belousova et al 2002) The trace-element result of an unknown zircon grain is run through atree and ends up in a terminal node which has beenassigned a class label Three class labels (rock types)were recognized as parental rocks for the here-studiedzircons from the Brusov Formation (1) lsquogranitesrsquo (iegranitoids with relatively high (gt65) SiO2 content) (2)lsquodioritesrsquo (ie granitoids with relatively low (lt65) SiO2

content) and (3) lsquosyenitesrsquo (ie syenite)Hf isotopes can yield information on the isotopic

source of the magmatic parent rock for each zircon andenables distinction between juvenile or evolved magmasIn this study we have investigated the in situ Hf isotopiccomposition of zircons whose U-Pb ages were previouslydetermined Analyses were undertaken with a New WaveMerchantek UP-213 laser attached to a Nu Plasma multi-collector ICP-MS The analytical methods for zircon Hfisotope determination are described in detail in Griffinet al (2000) Crustal model ages (TDMc) and εHf havebeen calculated (see Griffin et al 2004 2006 Belousovaet al 2010 Howard et al 2011 and references therein)

In a plot of εHf vs U-Pb age (see Figure 8) the positiveεHf values in zircons (position of data points between chon-dritic unfractionated reservoir (CHUR) (εHf = 0) anddepleted mantle (DM) lines) indicate that magmatisminvolved a juvenile source while its negative values suggestthe contribution of older (isotopic mature) crustal materialin the protolith that was responsible for the formation ofmagmas during its melting which were parental relative tozircons TDM gives a minimum age for the source materialof the magma from which the zircon crystallized TDMcassumes that its parental magma was produced from anaverage continental crust (176Lu177Hf = 0015) that origin-ally was derived from the DM Accuracy of TDMc isca 100 Ma

Results of studies of detrital zircons from the lowerCambrian sedimentary rocks of the Brusov Formationof the Mezen basin

U-Pb ages (Supplementary Table 2) and trace-element con-tents (Supplementary Table 3) were obtained for 57 zircon


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grains (60 analyses) while Lu-Hf isotope analyses(Supplementary Table 4) were run on 45 of these grainsCores and rims were studied separately in three large zircongrains and analyses revealed similar U-Pb ages for coresand rims 2361 plusmn 80 and 2456 plusmn 166 for grain N831809 plusmn 50 and 1806 plusmn 80 for grain N93 and 1818 plusmn 90and 1797 plusmn 46 for grain N95 Thus no older inheritedinclusions were revealed One analysis of the U-Pb systemof the grains exhibited large error and six analyses showeddiscordance Dgt 10 (Figure 6) These grains were

excluded from further consideration The remaining 53analyses yielded 206Pb207Pb ages ranging from 2751 plusmn 44to 1011 plusmn 44 Ma (Figure 7) The studied zircons can besubdivided into three distinct age groups The most numer-ous Mesoproterozoic group (37 dZr) has a prominent peakat ca 1160 Ma on the probability density plot Two othergroups are substantially smaller from middle to latePalaeoproterozoic (7 dZr) and early PalaeoproterozoicndashNeoarchaean (9 dZr) and do not show any clear andsharp peaks on the probability density plots Note the

Figure 6 Concordia diagram for detrital zircons from sandstones of the lower Cambrian Brusov Formation of the Padun Group (sample09-325 AL303 well) southeastern part of the White Sea region of the EEC

Figure 7 Histogram and probability density plot (red curve) for U-Pb isotopic ages of detrital zircons from sandstones of the lowerCambrian Brusov Formation of the Padun Group (sample 09-325 AL303 well) southeastern part of White Sea region


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absence of any detrital zircons with ages that fall within theca 750ndash500 Ma time interval ie the complete absence ofthe pU-T signal

The trace-element data obtained for 45 zircon grainswere processed using the CART classification (Belousovaet al 2002 Griffin et al 2004) two grains (both Archaeanin age) might have originated from lsquosyenitesrsquo five grains(all of Mesoproterozoic age) from lsquogranitesrsquo and the other38 grains (~80) from lsquodioritesrsquo (Figure 8(A))

Analysis of Lu-Hf isotope systematics revealed a widerange of εHf values from +82 to ndash101 One analysisexhibited an εHf value of minus161 but this grain is character-ized by a high discordance (17) in the U-Pb system anddoes not allow a reliable estimation of εHf and TDMcMany detrital zircons are characterized by a significantcontribution of an older crustal component which isreflected in their Lu-Hf isotopic system (εHf 0 datapoints in Figure 8(A) below the CHUR line)

The model ages of the substrate (TDMc) vary from3590 to 1420 Ma (Figure 8(A)) Note that two clusters areoutlined one with very old TDMc ages of 3600ndash3000 Maand another with ages younger than 2600 Ma (2600ndash1400 Ma) No zircons with TDMc ages of 3000ndash2600 Ma (which are the bulk ages of Archaean proto-cratons within EEC) were found On the contrary ninegrains (20) revealed TDMc ages within the 2600ndash2200 Ma time interval which is non-typical for the base-ment of EEC

Summary and discussion of the available studies ondetrital zircons from NeoproterozoicndashmiddleCambrian (meta)sedimentary units of the northeasternperiphery of the EEC

Detrital zircons from NeoproterozoicndashCambrian (meta)sedimentary units of the northeastern periphery of theEEC which represent the southwestern parts (Balticaside) of the Pre-UralidesndashTimanides orogen have beenstudied from at least seven localities geographically scat-tered along the whole length of the orogen (Figure 1localities 1ndash7) There are five studied samples fromanother side (Arctida side) of the Pechora suture betweenArctida and Baltica (Figure 1 locality 8) For three of thestudied samples trace-element and Hf-isotope data areavailable besides the U-Pb ages (Figure 8)

A summary of U-Pb ages for detrital zircons fromthe samples representing the Baltica side is presented inFigure 9 The depositional ages of all studied samplesspan the whole NeoproterozoicndashCambrian time intervalThe detrital zircon age distribution spectra demonstratethat there is no pU-T signal during the lateNeoproterozoic to early Cambrian (Figure 9 diagramsB5ndashB10) The youngest sedimentary unit for which thissignal has been found within Baltica (Kuznetsov et al2011 Orlov et al 2011) is the middle Cambrian Sablino

Formation (~510 Ma) (Figure 9 diagram B11) in thesouthern near-Ladoga region Thus during accumulationof this sedimentary unit the Pre-UralidesndashTimanidesorogen had undoubtedly become a high-standing upliftof the Arct-Europe continent and was being intensivelyeroded This implies that the ~510 Ma date representsan upper time limit for the beginning of the Pre-UralidesndashTimanides orogeny and ArctidandashBalticacollision

The youngest unit in which the absence of pU-T signalhas been recognized (Figure 9 diagram B10) is the lowerCambrian Brusov Formation of the Mezen basin (Figure 1locality 6 results of this study) Thus the ~540 Ma date(the lower boundary of Cambrian) now represents the bestestimate as the lower constraint for the onset of the Pre-UralidesndashTimanides orogeny In summary the onset of theArctidandashBaltica collision can now be constrained to thetime interval between ca 540 and 510 Ma

We have further tested the ABC model with respect tothe following aspects (1) what was the main direction(Arctida vs Baltica) of clastic transport from the Pre-UralidesndashTimanides orogen (2) Do U-Pb ages of zirconsand combined characteristics of the zircons (U-Pb ages ofzircons model ages of zircons and the type of theirparental rocks) that are available for three samples fit tofeatures of pre-collisional and collisional stages of the Pre-UralidesndashTimanides orogeny (3) Is it possible to obtaininsight into the source regions

Ages of detrital zircons from the upper CambrianndashLowerOrdovician Pogurey and Manitanyrd formations (Figure 10diagrams A4 and A5) in the Polar Urals (Figure 1 locality 8)corresponding to the Arctida side of the Pre-UralidesndashTimanides orogen reveal signals (Miller et al 2011Soboleva et al 2012b) that are practically identical to ageochronological image of the Pre-UralidesndashTimanides oro-gen (Figure 10 diagram pU-T) with a prevailing dominanceof ages in the range 750ndash500 Ma and minor input of oldercomponents sourced from basement rocks of the Arct-Europe continent This implies that the Pogurey andManitanyrd formations mostly formed from erosional pro-ducts of the collisional Pre-UralidesndashTimanides orogenwhich represented a key regional tectonic structure duringthe late Cambrian ndash a high-standing mountain system likelysimilar to the present-day Alps

Erosional products of the Pre-UralidesndashTimanidesorogen were transported both onto the Baltica side andonto the Arctida side of Arct-Europe However the pU-T signal forms a minor input into late Cambrian strataon the Baltica side (Figure 9 diagrams B12 and B13)whereas the pU-T signal is the dominant input into moreor less synchronously deposited sedimentary units onthe Arctida side (Figure 10 diagrams A4 and A5)This allows us to propose that the majority of the ero-sional material of the Pre-UralidesndashTimanides orogenhad been shed onto the Arctida side of Arct-Europe


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Figure 8 A comparison of Hf-isotopic and trace-element systematics for detrital zircon grains from (A) the lower Cambrian BrusovFormation (B) the lower Neoproterozoic Dzhezhim Formation (Kuznetsov et al 2010a) (C) the Ediacaran()ndashlower Cambrian Engane-Pe-Formation (Kuznetsov et al 2010a) The numbers of localities are in brackets (see Figures 1 and 2) Abbreviations B1 B11 A3correspond to those in Figures 4 9 and 10 A principle of TDMC calculation for grains is shown by the dashed line in (B)


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Figure 9 A summary of U-Pb isotopic ages of detrital zircons from (meta)sedimentary rocks of Neoproterozoicndashearly Palaeozoic unitsfrom the northeastern periphery of the EEC for the Baltica side of the Pre-UralidesndashTimanides orogen Green bars on the time axis (in themiddle of the figure) show approximate time intervals of the stratigraphic units The numbers of localities are in brackets (see Figures 1and 2) Abbreviations B1ndashB13 correspond to those in Figures 4 and 8B1 ndash Kuznetsov et al (2010a 2010b)B2 ndash Andreichev et al (2013)B3ndashB8 ndash Nicoll et al (2009) and Roberts and Siedlecka (2012)B9 ndash Maslov et al (2011 2012)B10 ndash Kuznetsov et al (2014)B11 ndash this studyB12ndashB13 ndash Kuznetsov et al (2011) and Orlov et al (2011)


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Upon secondary resedimentation these materials mighthave reached very distant parts of this continent andlater appeared within Arct-Laurussia and Arct-LaurasiaThis hypothesis (Kuznetsov 2006) finds support in agestudies of detrital zircons from Palaeozoic and earlyMesozoic (Triassic) sedimentary units deposited onArctica the pU-T signal has been detected in manylocalities up to very distal Canadian Arctic archipelagoAlaska and Chukotka (Miller et al 2006 Lorenz et al2008 Amato et al 2009 Anfinson et al 2012a 2012b2013)

A summary of U-Pb ages for detrital zircons from theEdiacaran()ndashlower Cambrian Engane-Pe and BedamelFormations in the Engane-Pe uplift area Polar Urals isshown in Figure 10 (diagrams A1ndashA3) One sample fromthe Engane-Pe uplift was studied by the TerraneChronereg

approach (see details in Kuznetsov et al 2009a 2009b2010a) The presence of zircons interpreted to representfirst cycle grains derived from tephra of earlyNeoproterozoic age that carry Mesoproterozoic TDMc(Figure 8(C)) allowed the interpretation that the Engane-Pe Formation was deposited on the slope ofManyukuyakha back-arc basin close to the Bolshezemelsubduction zone (Figure 4(A) A3) The basin was latersquashed into the collisional zone between Arctida andBaltica Together with a prevailing of lower SiO2 contentmaterial (lsquodioritesrsquo) and a minor input of lsquobasitersquo andlsquogranitersquo zircons as well as a fixing of juvenile materialthis three-component signal (U-Pb ages as well as Lu-Hfand trace element signatures) corresponds to a pre-colli-sional stage of pU-T signal

Comparative analyses of detrital zircon data fromstrata older than late Neoproterozoic allows us to obtaininsights into an earlier tectonic history of the region of theTimanian margin of Baltica According to widely acceptedpalaeotectonic reconstructions this region was a passivemargin of the supercontinent Rodinia (Li et al 2008) or anintracratonic basin of Rodinia (Evans et al 2009) begin-ning during the latest Mesoproterozoic or earlier Itappears that this region remained magmatically inactivewhen Baltica separated from Rodinia during the earlyNeoproterozoic This idea is supported by the absence ofzircons with ages younger than ca 1000 Ma in earlyNeoproterozoic strata (Figure 9 diagrams B1ndashB5) alongthe whole VarangerndashTimanian margin of Baltica ie noprovenance signals from local magmatic sourceseventsthat are clearly unrelated to the Baltica basement havebeen found

A comparison using three parameters of detrital zircons(U-Pb ages as well as Lu-Hf and trace element signatures)from the Brusov Formation (accumulated on the Timanianmargin of Baltica deposition age of ca 540 Ma) and theearly Neoproterozoic (Olovyanishnikov 1998) DzhezhimFormation (accumulated within the Baltic part of Rodiniadeposition age of ca 1000ndash960 Ma) reveals that the

Figure 10 U-Pb isotopic ages of detrital zircons from (meta)sedimentary rocks of some Neoproterozoicndashearly Palaeozoicunits of the Western Polar Urals (Figure 1 locality 8)Geochronological image of the Pre-Uralides-Timanides orogeny(a summary of crystalline complex ages is listed inSupplementary Table 1) is shown in diagram pU-TAbbreviations A1ndashA5 correspond to those in Figures 4 and 8A1 and A2 ndash Soboleva et al (2010)A3 ndash Kuznetsov et al (2009a 2009b 2010a)A4 and A5 ndash Soboleva et al (2012b)


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detrital material that accumulated in these two units isessentially different (Figure 8(A) and (B))

Studied samples from the Dzhezhim Formation con-tain a significant proportion of Palaeoproterozoic detritalzircons with a juvenile Hf-isotope signature (positive εHf)This suggests that the sedimentary basin in which theDzhezhim Formation accumulated existed for at least700 million years within Rodinia (ie between the assem-blage of Columbia (Nuna) and the cratonization of theEEC at 2200ndash1650 Ma on the one hand and the accumula-tion of the Dzhezhim Formation ~1000 Ma on the other)Yet it was mostly filled by erosional products fromPalaeoproterozoic collisional orogens andor fromreworked sedimentary sequences containing products ofthe initial destruction of those Palaeoproterozoic orogensThose Palaeoproterozoic orogens sutured Archaean proto-cratons into the supercontinent Columbia and their relictscompose now the basement of the EEC (Piper 2000 2007Rogers and Santosh 2002 Zhao et al 2002 2011Lahtinen et al 2005 Daly et al 2006 Сlaesson et al2006 Korja et al 2006 Houmllttauml et al 2008 Bogdanovaet al 2008 Bingen et al 2008b Meert 2012) (Figure 1)This is consistent with previous reports on the amount ofearly Palaeoproterozoic juvenile zircons found inPalaeoproterozoic sedimentary units of northeasternFennoscandia (ie erosional products of the LaplandndashKola orogen and Svecofennian province) that are basedon integrated isotopic (U-Pb Sm-Nd and Lu-Hf) investi-gations (Timmerman and Daly 1995 Bridgwater et al2001 Tuisku and Huhma 2006 Lahtinen et al 2010Andersson et al 2011 Beyer et al 2012)

Trace-element data available for detrital zircons fromthe Dzhezhim Formation suggest that they are derivedfrom a variety of rock types but lsquogranitesrsquo represent aprevailing source (possibly re-melted continental crustwithin the collisional zones) lsquoDioriticrsquo zircons with juve-nile Hf signatures (εHf 0) might be derived from theearly Palaeoproterozoic volcanic arcs caught into the colli-sional zones TDMc for Palaeoproterozoic zircons withεHf 0 vary from ca 3000 to 2500 Ma an age rangethat closely resembles the bulk ages of Archaean proto-cratons that make up the EEC

The MesoproterozoicndashNeoproterozoic assemblage ofRodinia at ca 1300ndash900 Ma (Grenvillian orogeny) and theEEC-intraplate magmaticmetamorphic events (Neymarket al 1994 Aringhaumlll et al 2000 Andersson et al 2002 2009Bogdanova et al 2004 Bingen et al 2008a) are practicallynot represented in the Dzhezhim Formation This means thatthemain source of detritus (Archaean and Palaeoproterozoic)to the Dzhezhim Formation was from the closest northeast-ern parts of the Baltic shield and central areas of the EECand that only a minimal input (Mesoproterozoic) was derivedfrom distant parts of Rodinia

In contrast Palaeoproterozoic zircons are very rare andno Palaeoproterozoic grains with juvenile Hf-isotope

composition have been found in the Brusov Formation(Figure 8(A)) which accumulated ~400 million years laterthan the Dzhezhim Formation Detrital zircons in this unit arepractically exclusively represented by grains typical for lsquodior-itesrsquo with only two grains being classified as lsquosyeniticrsquo andtwo as lsquograniticrsquo Numerous predominantlyMesoproterozoic detrital zircons consist of equal amountsof grains with mantle (εHf gt 0) and more evolved crustal(εHf lt 0) Hf-isotope signatures The bulk of theMesoproterozoic lsquodioriticrsquo juvenile zircons were derivedfrom magmas emplaced in a non-cratonic setting and mostprobably formed in volcanic arcs It is rather unlikely thatMesoproterozoic zircons with a contribution of older (isoto-pically mature) crustal material in the protolith might besourced from the Baltica-intraplate magmaticmetamorphicevents given that their TDMc have EEC atypical values of2500ndash2000 Ma and do not show the typical EEC values of3000ndash2500 Ma This observation allows us to argue thatthese Mesoproterozoic zircons most likely originate fromthe Mesoproterozoic orogens that sutured Rodinia ie theGrenvillian (Sveco-Norwegian within Baltica) and other oro-gens The implication is that the Brusov Formation receivedinput of detritus not only from nearby provinces but also avery essential input from some ultimately very distalsources Together with the absence of the pU-T signal theseare indications that at the time of the Brusov Formationaccumulation the Mezen basin had not yet been transformedinto a foreland basin of the Pre-UralidesndashTimanides orogenand the orogen itself had not yet been eroded

Conclusions

New integrated isotopic (U-Pb Lu-Hf) and trace-elementdata measured on detrital zircons from sandstones of thelower Cambrian Brusov Formation in the Mezen basin(White Sea region) in combination with previously availablestudies on detrital zircons from other Neoproterozoicndashmid-dle Cambrian (meta)sedimentary units of the northeasternperiphery of the EEC allow us to conclude the following

(1) The absence of the pU-T signal in lateNeoproterozoic (meta)sedimentary units (authoch-tonous to the basement of the EEC) of the north-eastern periphery of the EEC is an argument infavour of the ABC model

(2) The onset of the ArctidandashBaltica collision can nowbe constrained to the time interval between ca 540and 510 Ma

(3) Erosional products of the Pre-UralidesndashTimanidesorogen had been transported mostly onto theArctida side of the Arct-Europe palaeocontinent

(4) A comparison using three parameters (U-Pb ages aswell as Hf-isotope and trace-element signatures) ofdetrital zircons from the Brusov Fm (accumulated atthe Timanian passive margin of Baltica deposition


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age of ca 540 Ma) and the Dzhezhim Formation(accumulated within the Baltic part of Rodiniadeposition age of ca 1000 Ma) shows that the detri-tal material accumulated in these units is essentiallydifferent The main flux of detritus to the DzhezhimFormation derived principally from the closest north-eastern parts of the Baltic shield and central areas ofthe EEC (Palaeoproterozoic and Archaean material)with only a minimal input from distal parts ofRodinia (Mesoproterozoic material) On the con-trary the Brusov Formation received detrital inputnot only from nearby provinces but also an essentialinput component from ultimately very distal sources(Mesoproterozoic orogens)

(5) The absence of the pU-T signal in the BrusovFormation and the presence of bulk detrital zirconssourced ultimately from very distal provinces suggestthat at the time of accumulation of the BrusovFormation the Mezen basin had not yet been trans-formed into a foreland basin of the Pre-UralidesndashTimanides orogen

AcknowledgementsThe authors are very grateful to Stephanie Kovach and ChristianHallmann and reviewers Sergey Pisarevsky and Todd LaMaskinfor their careful reading of the text Their comments and editingof the English greatly improved the manuscript

FundingThis work was partly supported by Programme N 6 of the Divisionof Earth Sciences of the Russian Academy of Sciences by RFBR(project N 12-05-01063) by grant 2330 of the Ministry ofEducation and Science of Russia (Gubkin Russian StateUniversity of Oil and Gas) and contract 14Z50310017 of theMinistry of Education and Science of Russia (Schmidt InstitutePhysics of the Earth Russian Academy of Science) The analyticaldata were obtained using instrumentation funded by DESTSystemic Infrastructure Grants ARC LIEF NCRIS industry part-ners and Macquarie University This is contribution 512 from theARC Centre of Excellence for Core to Crust Fluid Systems (httpwwwccfsmqeduau) and 965 in the GEMOC Key Centre (httpwwwgemocmqeduau) Funding for preparation of this manu-script and compilation of Supplementary Table 1 (base date ofages of the crystalline complexes of the Pre-Uralides-Timanides)was provided by RSCF grant 14-27-00058 (KE Degtyarev)

Supplemental dataSupplemental data for this article can be accessed at httpdxdoiorg101080002068142014977968

ReferencesAringhaumlll K-I Connelly JN and Brewer TS 2000 Episodic

rapakivi magmatism due to distal orogenesis Correlation of169ndash150 Ga orogenic and inboard ldquoanorogenicrdquo events in

the Baltic Shield Geology v 28 p 823ndash826 doi1011300091-7613(2000)28lt823ERMDTDgt20CO2

Alekseev AS Grazhdankin DV Reimers AN MinchenkoGV Krayushkin AV Larchenko VA Ushakov VNand Stepanov VP 2005 New data on the upper limit ofthe age of the ore-hosting strata Arkhangelsk diamondiferousprovince in Zinchuk NN ed Geology of Diamonds ndashPresent and Future (of 50-th Anniversary of Mirnyi andDiamond Mining Industry in Russia Voronezh VoronezhState University p 235ndash241 (in Russian)

Amato JM Toro J Miller EL Gehrels GE Farmer GLGottlieb ES and Till AB 2009 Late ProterozoicndashPaleozoic evolution of the Arctic Alaska-Chukotka terranebased on U-Pb igneous and detrital zircon ages Implicationsfor Neoproterozoic paleogeographic reconstructionsGeological Society of America Bulletin v 121 no 9ndash10p 1219ndash1235 doi101130B265101

Andersen T Graham S and Sylvester AG 2009 The geo-chemistry Lu-Hf isotope systematics and petrogenesis ofLate Mesoproterozoic A-type granites in southwesternFennoscandia The Canadian Mineralogist v 47 p 1399ndash1422 doi103749canmin4761399

Andersson U Neymark LA and Billstroumlm K 2002Petrogenesis of the Mesoproterozoic (Subjotnian) rapakivicomplexes of central Sweden Implications from U-Pb zirconages Nd Sr and Pb isotopes Transactions of the RoyalSociety of Edinburgh Earth Sciences v 92 no 3 p 201ndash228 doi101017S0263593300000237

Andersson UB Begg GC Griffin WL and Hogdahl K2011 Ancient and juvenile components in the continentalcrust and mantle Hf isotopes in zircon from Svecofennianmagmatic rocks and rapakivi granites in SwedenLithosphere v 3 no 6 p 409ndash419 doi101130L1621

Andreichev VL 2010 Evolution of the base of the Pechoraplate according to the isotope-geochronological data[Doctoral thesis] Ekaterinburg Institute Geology andGeochemistry 46 p (in Russian)

Andreichev VL Larionov AN and Livinenko AF 2007New Rb-Sr and U-Pb data on the age of granitoids from theSyadatayakbinskaya intrusion (Polar Urals) Lithosphere no1 p 147ndash154 (in Russian)

Andreichev VL Soboleva AA and Gehrels GE 2013 U-Pb age of Detrital Zircons from the Upper PrecambrianTerrigenous section of North Timan Doklady EarthSciences v 450 no 2 p 592ndash596 doi101134S1028334X13060093

Anfinson OA Leier AL Dewing K Guest B Stockli DFEmbry AF and Hibbard J 2013 Insights into thePhanerozoic tectonic evolution of the northern Laurentianmargin Detrital apatite and zircon (UndashTh)He ages fromDevonian strata of the Franklinian Basin Canadian ArcticIslands Canadian Journal of Earth Sciences v 50 p 761ndash768 doi101139cjes-2012-0177

Anfinson OA Leier AL Embry AF and Dewing K2012a Detrital zircon geochronology and provenance ofthe Neoproterozoic to Late Devonian Franklinian BasinCanadian Arctic Islands Geological Society ofAmerica Bulletin v 124 no 3ndash4 p 415ndash430doi101130B305031

Anfinson OA Leier AL Gaschnig R Embry AF DewingK and Colpron M 2012b U-Pb and Hf Isotopic data fromFranklinian Basin Strata Insights into the nature ofCrockerland and the timing of accretion Canadian ArcticIslands Canadian Journal of Earth Sciences v 49 no 11p 1316ndash1328 doi101139e2012-067


Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014

Baluev AS 2006 Geodynamics of the Riphean Stage in theEvolution of the Northern Passive Margin of the EastEuropean Craton Geotectonics v 40 no 3 p 183ndash196doi101134S0016852106030034

Beckholmen M and Glondy J 2004 Timanian blueschist-facies metamorphism in the Kvarkush metamorphic base-ment Northern Urals Russia in Gee DG and Pease Veds The Neoproterozoic Timanide Orogen of EasternBaltica The Geological Society London Memoirs v 30p 125ndash134 doi101144GSLMEM20040300111

Beliakova LT and Stepanenko VJ 1991 Magmatism andgeodynamics of the Baikalide basement of the Pechora syne-clise Izvestia AN SSSR Serie Geologich no 12 p 106ndash117 (in Russian)

Belousova E Griffin W OrsquoReilly SY and Fisher N 2002Igneous zircon Trace element composition as an indicator ofsource rock type Contributions to Mineralogy and Petrologyv 143 no 5 p 602ndash622 doi101007s00410-002-0364-7

Belousova EA Griffin WL and OrsquoReilly SY 2006 Zirconcrystal morphology trace element signatures and Hf isotopecomposition as a tool for petrogenetic modelling ExamplesFrom Eastern Australian Granitoids Journal of Petrology v47 no 2 p 329ndash353 doi101093petrologyegi077

Belousova EA Kostitsyn YA Griffin WL Begg GCOrsquoReilly SY and Pearson NJ 2010 The growth of thecontinental crust Constraints from zircon Hf-isotope dataLithos v 119 p 457ndash466 doi101016jlithos201007024

Belousova EA Reid AJ Griffin WL and OrsquoReilly SY2009 Rejuvenation vs Recycling of Archean Crust in theGawler Craton South Australia Evidence from U-Pb andHf-isotopes in Detrital Zircon Lithos v 113 p 570ndash582doi101016jlithos200906028

Beyer EE Brueckner HK Griffin WL and OrsquoReilly SY2012 Laurentian Provenance of Archean Mantle Fragmentsin the Proterozoic Baltic Crust of the NorwegianCaledonides Journal of Petrology v 53 p 1357ndash1383doi101093petrologyegs019

Bingen B Andersson J Soderlund U and Moller C 2008aThe Mesoproterozoic in the Nordic countries Episodes v31 no 1 p 29ndash34

Bingen B Nordgulen O and Viola G 2008b A four-phasemodel for the Sveconorwegian orogeny SW ScandinaviaNorwegian Journal of Geology v 88 p 43ndash72

Bogdanov NA and Khain VE editors 1996 Tectonic map ofthe Barents Sea and the Northern part of European RussiaMoscow Institute of the Lithosphere RAS

Bogdanova SV Bingen B Gorbatschev R Kheraskova TN Kozlov VI Puchkov VN and Volozh YA 2008 TheEast European Craton (Baltica) before and during the assem-bly of Rodinia Precambrian Research v 160 p 23ndash45doi101016jprecamres200704024

Bogdanova SV Pashkevich IK Buryanov VB Makarenko IB Orlyuk MI Skobelev VM Starostenko VI andLegostaeva OV 2004 The 180ndash174 Ga gabbro-anortho-site-rapakivi Korosten Pluton in the Ukrainian Shield A 3-Dgeophysical reconstruction of deep structure Tectonophysicsv 381 no 1ndash4 p 5ndash27 doi101016jtecto200310023

Bridgwater D Scott DJ Balagansky VV Timmerman MJMarker M Bushmin SA Alexeyev NL and Daly JS2001 Age and provenance of Early Precambrian metasedi-mentary rocks in the Lapland-Kola Belt Russia Evidencefrom Pb and Nd isotopic data Terra Nova v 13 no 1 p32ndash37 doi101046j1365-3121200100307x

Claesson S Bibikova EV Bogdanova S and Skobelev V2006 Archaean terranes Paleoproterozoic reworking and

accretion in the Ukrainian Shield East European craton inGee DG and Stephenson RA eds European LithosphereDynamics Geological Society of London Memoirs v 32 p645ndash654 doi101144GSLMEM2006320138

Daly JS Balagansky VV Timmerman MJ and WhitehouseMJ 2006 The Lapland-Kola orogen Palaeoproterozoiccollision and accretion of the northern Fennoscandian litho-sphere Geological Society London Memoirs v 32 p 579ndash598 doi101144GSLMEM20060320135

Dovzhikova E Pease V and Remizov D 2004Neoproterozoic island arc magmatism beneath the PechoraBasin NW Russia Gff v 126 no 4 p 353ndash362doi10108011035890401264353

Dovzhikova EG 2007 Late Precambrian magmatism of Pri-Pechora faule zone (Central part of the Pechera bassin) [PhD thesis] Syktyvkar Institute of Geology 24 p (inRussian)

Dronov AV Koren TN Popov LE Tolmacheva TJu andHolmer LE 1995 Uppermost Cambrian and LowerOrdovician in Northwestern Russia Sequence stratigraphysea level changes and bio-events in Cooper JD Droser ML and Finney SC eds Ordovician Odyssey Short Papersfor the Seventh International Symposium on the OrdovicianSystem The Pacific Section Society for SedimentaryGeology (SEPM) Las Vegas Nevada p 319ndash322

Dronov A Tolmacheva T Raevskaya E and Nestell M2005 Cambrian and Ordovician of St Peterburg Region inThe 6th Baltic Stratigraphical Conference August 23ndash25pre-conference Excursion lsquoCambrian and Ordovician of StPetersburg Regionrsquo Field Guidebook St Petersburg StPetersburg State Univ and Baltic StratigraphicalAssociation 64 p (httpwwwpaleocitycomuploadsarti-clesOrdvician_Field_Guide_Dronovpdf)

Evans DAD 2009 The palaeomagnetically viable long-livedand all-inclusive Rodinia supercontinent reconstruction inMurphy JB Keppie JD and Hynes AJ eds AncientOrogens and Modern Analogues London GeologicalSociety London Special Publications v 327 p 371ndash404doi101144SP32716

Fedonkin MA Simonetta A and Ivantsov AI 2007 Newdata on Kimberella the Vendian mollusc-like organism(White Sea region Russia) Paleoecological and evolutionaryimplications in Vickers- Rich P and Komarower P edsRise and Fall of the Vendian Biota Geological Society ofLondon Special Volume v 286 p 157ndash179 doi101144SP28612

Gee DG Beliakova L Pease V Larionov A andDovzhikova E 2000 New Single Zircon (Pb-Evaporation)Ages from Vendian Intrusions in the basement beneath thePechora Basin Northeastern Baltica Polarforschung v 68p 161ndash170 hdl 10013epic29803d001

Gee DG and Pease V editors 2004 The NeoproterozoicTimanide Orogen of eastern Baltica IntroductionGeological Society London Memoirs v 30 p 1ndash3doi101144GSLMEM20040300101

Glodny J Pease V Montero P Austrheim H and Rusin A2004 Protolith ages of eclogites Marun-Keu ComplexPolar Urals Russia Implications for the pre- and earlyUralian evolution of the northeastern European continentalmargin in Gee DG and Pease V eds TheNeoproterozoic Timanide Orogen of Eastern Baltica TheGeological Society London Memoirs v 30 p 87ndash105doi101144GSLMEM20040300109

Grazhdankin DV 2004 Late Neoproterozoic sedimentation inthe Timan foreland in Gee DG and Pease V eds The


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nloa

ded

by [

171

672

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1] a

t 06

44 0

8 N

ovem

ber

2014

Neoproterozoic Timanide Orogen of Eastern Baltica TheGeological Society London Memoirs v 30 p 37ndash46doi101144GSLMEM20040300104

Grazhdankin DV and Krayushkin AV 2007 Trace fossilsand the Upper Vendian boundary in the southeastern WhiteSea region Doklady Earth Sciences v 416 no 1 p 1027ndash1031 doi101134S1028334X07070100

Griffin WL Belousova EA and OrsquoReilly SY 2007TerraneChron analysis of Zircons from Western AustralianSamples Record (Geological Survey of Western Australia)v 4 52 p

Griffin WL Belousova EA Shee SR Pearson NJ andOrsquoReilly SY 2004 Archean crustal evolution in the north-ern Yilgarn Craton U-Pb and Hf-isotope evidence fromdetrital zircons Precambrian Research v 131 p 231ndash282doi101016jprecamres200312011

Griffin WL Belousova EA Walters SG and OrsquoReilly SY2006 Archaean and Proterozoic crustal evolution in theEastern Succession of the Mt Isa district Australia U-Pband Hf-isotope studies of detrital zircons Australian Journalof Earth Sciences v 53 p 125ndash149 doi10108008120090500434591

Griffin WL Pearson NJ Belousova E Jackson SE VanAchterbergh E OrsquoReilly SY and Shee SR 2000 TheHf isotope composition of cratonic mantle LAM-MC-ICPMS analysis of zircon megacrysts in kimberlitesGeochimica Et Cosmochimica Acta v 64 p 133ndash147doi101016S0016-7037(99)00343-9

Houmllttauml PH Balagansky V Garde AA Mertanen SPeltonen P Slabunov A Sorjonen-War P andWhitehouse M 2008 Archean of Greenland andFennoscandia Episodes v 31 no 1 p 13ndash19

Howard KE Hand M Barovich KM Payne JL andBelousova EA 2011 U-Pb Lu-Hf and SmndashNd isotopicconstraints on provenance and depositional timing of meta-sedimentary rocks in the western Gawler CratonImplications for Proterozoic reconstruction modelsPrecambrian Research v 184 no 1ndash4 p 43ndash62doi101016jprecamres201010002

Ivantsov AY 1990 New data on ultrastructure of sabelliditids(Pogonophora) Paleontological Journal no 4 p 125ndash128(in Russian)

Jackson SE Pearson NJ Griffin WL and Belousova EA2004 The application of laser ablation-inductively coupledplasma-mass spectrometry to in situ U-Pb zircon geochronol-ogy Chemical Geology v 211 p 47ndash69 doi101016jchemgeo200406017

Khain EV and Leonov YG editors 1999 InternationalTectonic Map of Europe scale 15 000 000 4 sheets + 1sheet with inset and legend Saint-Petersburg VSEGEIhttpccgmorgenmaps110-carte-internationale-tectonique-d-europehtml

Kirsanov VV 1968 New data on Precambrian stratigraphy ofcentral part of Russian Platform Izvestiya Akademii NaukSSSR Seriya geologicheskaya no 4 p 98ndash113 (inRussian)

Korja A Lahtinen R and Nironen M 2006 TheSvecofennian orogen A collage of microcontinents andisland arcs Geological Society London Memoirs v 32 p561ndash578 doi101144GSLMEM20060320134

Kostyuchenko S Sapozhnikov R Egorkin A Gee DGBerzin R and Solodilov L 2006 Crustal structure andtectonic model of northeastern Baltica based on deep seis-mic and potential field data in Gee DG and StephensonRA eds European Lithosphere Dynamics Geological

Society of London Memoirs v 32 p 521ndash539doi101144GSLMEM20060320132

Kostyuchenko SL and Romanyuk TV 1997 Nature of theMezen gravity maximum Izvestia Akademii Nauk SSSRFizika zemli no 12 p 3ndash22

Kuznetsov NB 2006 The Cambrian Baltica-Arctida collisionpre-Uralide-Timanide orogen and its erosion products in theArctic Doklady Earth Sciences v 411 no 2 p 1375ndash1380doi101134S1028334X06090091

Kuznetsov NB 2008 The Cambrian pre-Uralide-Timanideorogen Structural evidence for its collisional originDoklady Earth Sciences v 423 no 2 p 1383ndash1387doi101134S1028334X08090122

Kuznetsov NB Alekseev AS Belousova EA RomanyukTV Reimers AN and Tselrsquomovich VA 2014 Testingthe Models of Late Vendian Evolution of the NortheasternPeriphery of the East European Craton Based on the FirstUPb Dating of Detrital Zircons from Upper VendianSandstones of Southeastern White Sea Region DokladyEarth Sciences v 458 no 1 p 1073ndash1076 doi101134S1028334X14090311

Kuznetsov NB Kulikova KV and Udoratina OV 2007bStructural patterns of Pre-Uralides in the Enganepe Uplift(Polar Urals) as a reflection of the Cambrian collision ofBaltica and Arctida Doklady Earth Sciences v 415 no 1p 695ndash700 doi101134S1028334X07050078

Kuznetsov NB Natapov LM Belousova EA Griffin ULOrsquoReilly S Soboleva AA Kulikova KV Udoratina OV and Morgunova AA 2009a First results of isotopicdating of detrital zircons from the clastic rocks of the Pre-Uralides-Timanides complexes Contribution in the LatePrecambrian stratigraphy of the Enganepe Uplift WesternPolar Urals Doklady Earth Sciences v 424 no 1 p 41ndash46 doi101134S1028334X09010097

Kuznetsov NB Natapov LM Belousova EA Griffin ULOrsquoRelly SY Kulikova KV Soboleva AA andUdoratina OV 2010b The First Results of UPb Datingand Isotope Geochemical Studies of Detrital Zircons fromthe Neoproterozoic Sandstones of the Southern Timan(Djejim-Parma Hill) Doklady Earth Sciences v 435 no 2p 1676ndash1683 doi101134S1028334X10120263

Kuznetsov NB Natapov LM Belousova EA Griffin WLand OrsquoReilly SY 2009b First isotopic data on detritalzircons from the Engane-Pe Uplift (western Polar Urals)Implications for the primary tectonic position of the Pre-Uralides-Timanides Doklady Earth Sciences v 426 no 1p 567ndash573 doi101134S1028334X09040138

Kuznetsov NB Natapov LM Belousova EA O`Reilly SY and Griffin WL 2010a Geochronological geochemicaland isotopic study of detrital zircon suites from lateNeoproterozoic clastic strata along the NE margin of theEast European Craton Implications for plate tectonic mod-els Gondwana Research v 17 no 2ndash3 p 583ndash601doi101016jgr200908005

Kuznetsov NB Orlov SY Miller EL Shazillo AVDronov AV Soboleva AA Udoratina OV andGehrels G 2011 First results of UPb dating of DetritalZircons from early Paleozoic and Devonian Sandstones ofthe Baltic-Ladoga Region (South Ladoga Area) DokladyEarth Sciences v 438 no 2 p 759ndash765 doi101134S1028334X11060316

Kuznetsov NB Soboleva AA Udoratina OV Hertseva MV and Andreichev VL 2007a Pre-Ordovician tectonicevolution and volcano-plutonic associations of theTimanides and northern Pre-Uralides northeast part of the


Dow

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1] a

t 06

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ovem

ber

2014

East European Craton Gondwana Research v 12 no 3 p305ndash323 doi101016jgr200610021

Lahtinen R Huhma H Kontinen A Kohonen J andSorjonen-Ward P 2010 New constraints for the sourcecharacteristics deposition and age of the 21ndash19 Ga meta-sedimentary cover at the western margin of the KarelianProvince Precambrian Research v 176 p 77ndash93doi101016jprecamres200910001

Lahtinen R Korja A and Nironen M 2005Palaeoproterozoic tectonic evolution in Lehtinen MNurmi PA and Raumlmouml OT eds Precambrian Geologyof Finland ndash Key to the evolution of the Fennoscandianshield Developments in Precambrian Geology AmsterdamElsevier Science v 14 p 481ndash532

Landing E Myrow P Benus AP and Narbonne GM 1989The Placentian Series Appearance of the oldest skeletalizedfaunas in southeastern Newfoundland Journal ofPaleontology v 63 no 6 p 739ndash769

Larionov AN Andreichev VL and Gee D 2004 TheVendian alkaline igneous suites of northern Timan Ionmicroprobe U-Pb zircon ages of gabbros and syenite inGee DG and Pease V eds The NeoproterozoicTimanide Orogen of Eastern Baltica The GeologicalSociety London Memoirs v 30 p 69ndash74 doi101144GSLMEM20040300107

Li ZX Bogdanova SV Collins AS Davidson A DeWaele B Ernst RE Fitzsimons ICW Fuck RAGladkochub DP Jacobs J Karlstrom KE Lu SNatapov LM Pease V Pisarevsky SA Thrane K andVernikovsky V 2008 Assembly configuration and break-up history of Rodinia A synthesis Precambrian Research v160 p 179ndash210 doi101016jprecamres200704021

Lipps JH and Rozanov AY 1996 The Late Precambrian-Cambrian agglutinated fossil Platysolenites PaleontologicalJournal v 30 no 6 p 679ndash687

Llanos MPI Tait JA Popov V and Abalmassova A 2005Palaeomagnetic data from Ediacaran (Vendian) sediments ofthe Arkhangelsk region NW Russia An alternative apparentpolar wander path of Baltica for the Late ProterozoicndashEarlyPalaeozoic Earth and Planetary Science Letters v 240 p732ndash747 doi101016jepsl200509063

Lorenz H Gee DG and Simonetti A 2008 Detrital zirconages and provenance of the Late Neoproterozoic andPalaeozoic successions on Severnaya Zemlya Kara ShelfA tie to Baltica Norwegian Journal of Geology v 88 p235ndash258

Martin MW 2000 Age of Neoproterozoic Bilatarian Body andTrace Fossils White Sea Russia Implications for MetazoanEvolution Science v 288 no 5467 p 841ndash845doi101126science2885467841

Maslov AV Grazhdankin DV Podkovyrov VN IsherskayaMV Krupenin MT Petrov GA Ronkin YL Gareev EZ and Lepikhina OP 2009 Provenance composition andfeatures of geological evolution of the Late Vendian forelandbasin of the Timan orogen Geochemistry International v 47no 12 p 1212ndash1233 doi101134S0016702909120052

Maslov AV Grazhdankin DV Podkovyrov VN Ronkin YL and Lepikhina OP 2008 Composition of sedimentprovenances and patterns in geological history of theLate Vendian Mezen basin Lithology and MineralResources v 43 no 3 p 260ndash280 doi101134S002449020803005X

Maslov AV Vovna GM Kiselev VI Krupenin MT andRonkin YL 2011 First U-Pb Dates for Detrital Zirconsfrom Deposits of Serebryanka Group (Upper Proterozoic

Middle Urals) Doklady Earth Sciences v 439 no 1 p933ndash938 doi101134S1028334X11070257

Maslov AV Vovna GM Kiselev VI Ronkin YL andKrupenin MT 2012 U-Pb systematics of detrital zirconsfrom the Serebryanka Group of the Central Urals Lithologyand Mineral Resources v 47 no 2 p 160ndash176doi101134S0024490212020046

Meert JG 2012 Whatrsquos in a name The Columbia(PaleopangaeaNuna) supercontinent Gondwana Researchv 21 no 4 p 987ndash993 doi101016jgr201112002

Miller EL Kuznetsov N Soboleva A Udoratina O GroveMJ and Gehrels G 2011 Baltica in the CordilleraGeology v 39 no 8 p 791ndash794 doi101130G319101

Miller EL Toro J Gehrels G Amato JM Prokopiev ATuchkova MI Akinin VV Dumitru TA Moore TEand Cecile MP 2006 New insights into Arctic paleogeo-graphy and tectonics from U-Pb detrital zircon geochronol-ogy Tectonics v 25 TC3013 (19 p) doi1010292005TC001830

Mints MV Suleimanov AK Babayants PS Belousova EA Blokh YI Bogina MM Bush VA Dokukina KAZamozhnaya NG Zlobin VL Kaulina TV Konilov AN Mihai`lov VO Natapov LM Piusp VB Stupak VM Tihotckii` SA Trusov AA Philippova IB andShur DI 2010 Deep structure evolution and mineraldeposits of the Early Precambrian basement of the EastEuropean Platform interpretation of the materials on the1_EU geotraverse and profiles 4B and TATSEIS(GEOKART Geos Moscow 2010) v 1 and 2 (in Russian)

Neymark LA Amelin YV and Larin AM 1994 Pb-Nd-Srisotopic and geochemical constraints on the origin of the154ndash156 Ga Salmi rapakivi granite-anorthosite batholith(Karelia Russia) Mineralogy and Petrology v 50 p 173ndash193 doi101007BF01160146

Nicoll GR Tait JA and Zimmerman U 2009 Provenanceanalysis and tectonic setting of Neoproterozoic sedimentson the Varanger Peninsula Northern Norway in RodiniaSupercontinents Superplumes and Scotland Fermormeeting Edinburg Scotland Programme and abstractsp 68

Olovyanishnikov VG 1998 Upper Pre-Cambrian of the Timanand Kanin peninsula Ekaterinburg UrDep RAS 164 p (inRussian)

Orlov SY Kuznetsov NB Miller EL Soboleva AA andUdoratina OV 2011 Age Constraints for the Pre-Uralide-Timanide Orogenic Event Inferred from the Study of DetritalZircons Doklady Earth Sciences v 440 no 1 p 1216ndash1221 doi101134S1028334X11090078

Orlowski S 1985 Lower Cambrian and its trilobites in the HolyCross Mts Acta Geologica Polonica v 35 no 3ndash4 p 231ndash250

Pease V Dovzhikova E Beliakova L and Gee DG 2004Late Neoproterozoic granitoid magmatism in the basement tothe Pechora Basin NW Russia Geochemical constrainsindicate westward sudduction beneath NE Baltica in GeeDG and Pease V eds The Neoproterozoic TimanideOrogen of Eastern Baltica The Geological Society LondonMemoirs v 30 p 75ndash85 doi101144GSLMEM20040300108

Piper JDA 2000 The Neoproterozoic Supercontinent Rodiniaor Palaeopangaea Earth and Planetary Science Letters v176 no 1 p 131ndash146 doi101016S0012-821X(99)00314-3

Piper JDA 2007 The Neoproterozoic supercontinentPalaeopangaea Gondwana Research v 12 p 202ndash227doi101016jgr200610014


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2014

Puchkov VN 2003 Uralides and Timanides Their structuralrelationship and position in the geological history of theUral-Mongolian fold belt Russian Geology andGeophysics v 44 no 1ndash2 p 28ndash39

Remizov DN and Pease VL 2004 The Dzela complexPolar Urals Russia A Neoproterozoic island arc in GeeDG and Pease V eds The Neoproterozoic TimanideOrogen of Eastern Baltica The Geological SocietyLondon Memoirs v 30 p 107ndash123 doi101144GSLMEM20040300110

Roberts D and Olovyanishnikov VG 2004 Structural andtectonic development of the Timan orogen in Gee DGand Pease V eds The Neoproterozoic Timanide Orogen ofEastern Baltica The Geological Society London Memoirsv 30 p 47ndash57 doi101144GSLMEM20040300105

Roberts D and Siedlecka A 2002 Timanian orogenic defor-mation along the northeastern margin of Baltica NorthwestRussia and Northeast Norway and AvalonianndashCadomianconnections Tectonophysics v 352 no 1ndash2 p 169ndash184doi101016S0040-1951(02)00195-6

Roberts D and Siedlecka A 2012 Provenance and sedimentrouting of Neoproterozoic formations on the VarangerNordkinn Rybachi and Sredni peninsulas North Norwayand Northwest Russia A review Norges GeologiskeUndersoslashkelse Bulletin v 452 p 1ndash19

Rogers JJW and Santosh M 2002 Configuration ofColumbia a Mesoproterozoic supercontinent GondwanaResearch v 5 no 1 p 5ndash22 doi101016S1342-937X(05)70883-2

Romanyuk TV Kuznetsov NB Maslov AV Belousova EARonkin YL Gorozhanin VM and Gorozhanina EN2013 Geochemical and Lu-Hf (LAndashICPndashMS) Systematic ofDetrital Zircons from Lower Neoproterozoic LemezaSandstones Southern Urals Doklady Earth Sciences v 453no 2 p 1200ndash1204 doi101134S1028334X13120222

Rozanov AY 1983 Platysolenites in Urbanek A andRozanov AY eds Upper Precambrian and CambrianPaleontology of the East European Platform WarsawWydawnictwa Geologiczne p 94ndash100

Scarrow JH Pease V Fleutelot C and Dushin V 2001 Thelate Neoproterozoic Enganepe ophiolite Polar UralsRussia An extension of the Cadomian arc PrecambrianResearch v 110 p 255ndash275 doi101016S0301-9268(01)00191-7

Soboleva A Udoratina O Miller EL Kuznetsov N GroveM and Gehrels G 2010 Magmatic source rocks for lateNeoproterozoic ndash early Cambrian sediments of the EnganepeUplift western Polar Urals [abs] AGU Fall Meeting 13ndash17Dec San Francisco CA Abstract D T31A-2134

Soboleva AA 2004 Volcanites and associated granites of theSub-Polar Urals Ekaterinburg UrO RAN 146 p (inRussian)

Soboleva AA Karchevskii AF Efanova LI Kuznetsov NB Grove M Sobolev ID and Maurin MV 2012aEvidence for Late Riphean Granite Formation in the Polar

Urals Doklady Earth Sciences v 442 no 2 p 181ndash187doi101134S1028334X12020080

Soboleva AA Kudryashov NM and Dorokhov NS 2004The U-Pb age of Granitoids from the Narodinsk Pluton theNear-Polar Urals Transactions (Doklady) of the RussianAcademy of Sciences Earth Science Section v 397 no 6p 804ndash807

Soboleva AA Kuznetsov NB Miller EL Udoratina OVGehrels G and Romanyuk TV 2012b First Results of U-Pb Dating of Detrital Zircons from Basal Horizons ofUralides (Polar Urals) Doklady Earth Sciences v 445 no2 p 962ndash968 doi101134S1028334X12080156

Sokolov BS 1968 Vendian and early Cambrian Sabelliditida(Pogonophora) of the USSR Problems of PalaeontologyInternational Geological Congress XXIII Session Reportsof Soviet Geologists for the Meeting of the InternationalPalaeontological Union p 73ndash79 Publishing HouseldquoNaukardquo Moscow (in Russian)

Streng M Babcock LE and Hollingsworth JS 2005Agglutinated protists from the Lower Cambrian of NevadaJournal of Paleontology v 79 no 6 p 1214ndash1218doi1016660022-3360(2005)079[1214APFTLC]20CO2

Timmerman MJ and Daly JS 1995 Sm-Nd evidence for lateArchaean crust formation in the Lapland-Kola MobileBelt Kola Peninsula Russia and Norway PrecambrianResearch v 72 no 1ndash2 p 97ndash107 doi1010160301-9268(94)00045-S

Tuisku P and Huhma H 2006 Evolution of MigmatiticGranulite Complexes Implications from Lapland GranuliteBelt Part II Isotopic dating Bulletin of the GeologicalSociety of Finland v 78 p 143ndash175

Udoratina OV Soboleva AA Kuzenkov NA Rodionov NV and Presnyakov SL 2006 Age of Granitoids in theManrsquokhambo and Ilrsquoyaiz Plutons the Northern Urals U-PbData Transactions (Doklady) of the Russian Academy ofSciences Earth Science Section v 407 no 2 p 284ndash289

Veevers JJ Saeed A Belousova EA and Griffin WL2005 U-Pb ages and source composition by Hf-isotope andtrace-element analysis of detrital zircons in Permian sand-stone and modern sand from southwestern Australia and areview of the paleogeographical and denudational history ofthe Yilgarn Craton Earth-Science Reviews v 68 p 245ndash279 doi101016jearscirev200405005

Yanishevsky M 1926 On tube-form worms from CambrianBleu Clay Ezhegodnik Russkogo PaleontologicheskogoObschestva v 4 for 1922ndash1924 p 99ndash113 (in Russian)

Zhao G Cawood PA Wilde SA and Sun M 2002 Reviewof global 21ndash18 Ga orogens Implications for a pre-Rodiniasupercontinent Earth-Science Reviews v 59 no 1ndash4 p125ndash162 doi101016S0012-8252(02)00073-9

Zhao G Li S Sun M and Wilde SA 2011 Assemblyaccretion and break-up of the Palaeo-MesoproterozoicColumbia supercontinent Record in the North ChinaCraton revisited International Geology Review v 53 no11ndash12 p 1331ndash1356 doi101080002068142010527631


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New data on detrital zircons from the sandstones of the lower Cambrian Brusov Formation(White Sea region East-European Craton) unravelling the timing of the onset of the

ArctidandashBaltica collision

NB Kuznetsovab EA Belousovac AS Alekseevd and TV Romanyukeb

aTectonics Geological Institute of the Russian Academy of Science Moscow Russia bDepartment of Theoretical Foundations andExploration of Oil and Gas Gubkin Russian State University of Oil and Gas Moscow Russia cAustralian Research Council Centre ofExcellence for Core to Crust Fluid Systems (CCFS) and GEMOC National Key Centre Department of Earth and Planetary SciencesMacquarie University Sydney NSW 2109 Australia dGeological Department Lomonosov Moscow State University Moscow Russia

eSchmidt Institute of Physics of the Earth Russian Academy of Sciences Moscow Russia

(Received 27 March 2014 accepted 26 September 2014)

The basement of the northeastern periphery of the East-European Craton (ЕЕС) is composed of volcanic-sedimentarysequences volcanic rocks granitoids and rare ophiolite complexes Geochronological data constrain their age from ca 750to 500 Ma and there is a consensus that these rocks represent relicts of a late NeoproterozoicndashCambrian Pre-UralidesndashTimanides orogeny Combining new integrated isotopic (U-Pb Lu-Hf) and trace-element data (TerraneChronereg approach)on detrital zircons from sandstones of the lower Cambrian Brusov Formation in the Mezen basin (White Sea region in thenortheastern periphery of the EEC) with available studies on detrital zircons from Neoproterozoicndashmiddle Cambrian (meta)sedimentary units of the northeastern periphery of the EEC allow us to conclude that (1) the onset of the ArctidandashBalticacollision can now be constrained to the time interval between ca 540 and 510 Ma and (2) the Ediacaranndashearly CambrianMezen sedimentary basin was a basin on the Timanian passive margin of Baltica up to 540 Ma but was not a foreland basinof the Pre-UralidesndashTimanides orogen

Keywords ArctidandashBaltica collision Mezen sedimentary basin White Sea region Neoproterozoic Ediacaran Cambriandetrital zircons U-Pb dating Hf and trace-element systematics

Introduction

The basement of the northeastern periphery of the East-European Craton (ЕЕС) is composed of complexes withvolcanic-sedimentary rocks volcanic rocks granitoidsand rare ophiolites (Beliakova and Stepanenko 1991Scarrow et al 2001 Soboleva 2004 Soboleva et al2004 2012a 2013 Remizov and Pease 2004 Udoratinaet al 2006 Andreichev et al 2007 Andreichev 2010)The metamorphic grade of these rocks varies betweengreenschist facies up to blueschist-eclogitic and amphibo-lite facies (Beckholmen and Glondy 2004 Glodny et al2004) and they are variably (at some places very strongly)deformed (Roberts and Siedlecka 2002 Larionov et al2004 Roberts and Olovyanishnikov 2004 Kuznetsovet al 2007a 2007b Kuznetsov 2008) A number of com-plexes are exposed in the Polar Urals the Timan HillsKanin peninsula and the northeastern edge of the Kolapeninsula (Figures 1 and 2) Samples were collected bothfrom exposed surface and from boreholes for detailedstudies (Kostyuchenko and Romanyuk 1997 Gee et al2000 Dovzhikova et al 2004 Baluev 2006Kostyuchenko et al 2006 Dovzhikova 2007 Kuznetsovet al 2007a) More than 250 isotopic dating analyses

(a summary of U-Pb dating of magmatic zircons andtheir inherit cores results of dating by Rb-Sr or Sm-Ndisochronic and others methods see Supplementary Table l[httpdxdoiorg101080002068142014977968] sam-ple designations see in Figure 2) obtained recently on thecrystalline complexes of ca 750ndash500 Ma age (Kuznetsovet al 2007a 2010a Orlov et al 2011 Soboleva et al2012b) There is a consensus that these rocks are relicts ofa late NeoproterozoicndashCambrian orogeny This orogeny(or its partsstages) is referred to as the TimanndashVarangerBelt (Roberts and Siedlecka 2002) Timanide orogen(Puchkov 2003 Gee and Pease 2004) Pre-UralidesndashTimanides orogen (Kuznetsov et al 2007a 2010a) andothers The relicts of the Pre-UralidesndashTimanides orogenyhave been revealed in the basement of the vast area fromthe Pechora basin and northern parts of the western Uralsto the Svalbard archipelago and from the north edge of theKola Peninsula to the central part of Novaya Zemlyaarchipelago (Figure 2)

During the last 20 years the tectonic origin of the Pre-UralidesndashTimanides orogeny has been actively discussedwith two main models challenging each other The firstmodel is abbreviated further as the TAMB model

Corresponding author Email kouznikbormailru

International Geology Review 2014httpdxdoiorg101080002068142014977968

copy 2014 Taylor amp Francis

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es b

een

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Dan

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n (~

147

ndash14

2 G

a) a

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tiona

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vent

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orog

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com

plex

es b

een

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Tele

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(~1

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15

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e ou

ter

boun

dary

of

scel

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tica)

b ndash

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ndar

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e bl

ocks

and

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de E

EC

bou

ndar

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of c

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con

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e bl

ocks

and

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tec

toni

c bo

unda

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of th

e M

esondash

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(16

ndash08

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with

in E

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ift s

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WS

ndash W

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Sea

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ndash K

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MR

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an M

ndash M

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n V

ndash V

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O ndash

Vol

yn-O

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SA

ndash S

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k ndashA

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ino

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ache

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La

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Con

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of

the

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of

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ndashUra

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ndashTim

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nd th

eir

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anal

ogue

s in

the

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tern

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ls T

iman

Hill

s P

aindashK

hoi M

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Kan

in V

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and

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y P

enin

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s V

ouga

ch Is

I an

d N

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a Z

emly

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chip

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o

Arc

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lexes (

~37

0ndash26

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a)

of

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no

scan

dia

V

olg

a-U

ralia a

nd

Sarm

ati

a

Cad

omid

esndashA

valo

nide

s

Ura

lides

(Eas

tem

Ura

ls)

Var

isci

des

(Wes

tem

and

Cen

tral

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ope

Sca

ndin

avia

n C

aled

onid

es (

mid

dle

and

uppe

r-m

ost n

appe

s of

Sca

ndin

avia

n C

aled

onid

es)

Figure1

Map


andstructures

oftheEast-Europ


periph

eryinclud

ingblocks

ofconsolidated



from

Kuznetsov

etal(201

0a)

LatePalaeop



oftheEEC

mod

ified

from

Bog

dano

vaet

al(200


briancomplexes

Pre-U

ralid

esndashT

imanides

attheeasternandno

rth-easternperiph

eryof


etal(200

7a)

Configu

ratio

nof

theWhite

Sea

RiftSystem

(WS)afterBaluev(200

6)Insetcontou

rsof

EECproto-craton


ralia

afterRom

anyu

ketal(201

3)

Black

linendashcontou

rof

Figure2

Yellow

symbo

lsmarklocalitiesof

samples

with

stud

ieddetritalzircon

s(starwith

number6ndashthis

stud

y)nu

mbers

oflocalitiesinside

symbo

lscorrespo

ndto

numbers

inFigures

28

9and10Abbreviations

ofgraniticmassifs

(white

letters)SSalma

Vy

Vyborg

RRiga

KKorosten

KNKorsun-Novom

irgorod

Nu

Nov

o-Ukrainsk

Ma

Mazury


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Conclusions







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Dow

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t 06

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ber

2014

Pale

ozo

ides o

f fo

ld-n

ap

pes b

elt

s in

th

e f

ram

ing

of

East-

Eu

rop

ean

Cra

ton

(E

EC

)

Me S

ondash a

nd

Neo

pro

tero

zo

ic f

illin

g o

f ri

fto

gen

ic s

tru

ctu

res (

rift

s au

loco

gen

s etc

) w

ith

in t

he E

EC

Me s

ondash a

nd

Neo

pro

tero

zo

ic c

om

ple

xes an

d r

are

rew

ork

ed

Arc

hean

ndashP

ale

op

rote

rozo

ic c

om

ple

xes o

f re

lics

of

accre

tio

nary

an

d c

ollis

ion

al b

elt

s o

f n

ort

hndashw

este

rn a

nd

weste

rn p

art

s o

f th

e E

EC



collisional orogens

Pale

op

rote

rozo

ic c

om

ple

xes o

f F

en

no

scan

dia

V

olg

a-U

ralia a

nd

Sarm

ati

a

No

nu

nif

orm

ly m

eta

m o

rph

osed

Neo

pro

tero

zo

ic t

o M

idd

le C

am

bri

an

co

mp

lexes

Pre

ndashU

ralid

esndashT

iman

ides o

fW

este

rn U

rals

an

d T

iman

ndashP

ech

ora

ndashB

are

nts

Sea R

eg

ion

an

d t

heir

ag

es a

nalo

gu

es o

f n

earndash

Ura

lian

part

of

EE

C a

nd

Scan

din

avia

(F

inm

ark

en

an

d t

he lo

west

un

its o

f th

e C

ale

do

nia

n n

ap

pes)

an

d C

ad

om

idesndash

Avalo

nid

es o

f th

e s

ou

thern

an

d S

E f

ram

e o

f E

EC

Pre

ndashUra

lides

ndashTim

anid

es a

ndash m

ostly

sed

imen

tary

com

plex

es

b ndash

volc

anog

enic

vol

cani

cndashse

dim

enta

ry a

nd s

edim

enta

ry c

ompl

exes

Und

iffer

entia

ted

com

plex

es b

een

rew

orke

d du

ring

Sve

cono

rweg

ian

(~1

14ndash0

90

Ga)

col

lisio

nal e

vent

s(S

veco

norw

egia

n or

ogen

y)

com

plex

es b

een

rew

orke

d du

ring

Dan

opol

onia

n (~

147

ndash14

2 G

a) a

ccre

tiona

ry e

vent

s(D

anop

olon

ian

orog

eny)

com

plex

es b

een

rew

orke

d du

ring

Tele

mar

kian

(~1

52ndash

148

Ga)

acc

retio

nary

eve

nts

(Tel

emar

kian

oro

geny

)

com

plex

es b

een

rew

orke

d du

ring

Got

hian

(~1

73ndash

155

Ga)

acc

retio

nary

eve

nts

(Got

hian

oro

geny

)

Mes

opro

tero

zoic

ano

rtho

site

-man

gerit

e-ch

arno

ckite

ndashgra

nite

(A

MC

G)

plut

onic

ass

ocia

tions

and

A-g

rani

tes

15

5ndash1

44 G

a (a

) 1

60ndash1

58

Ga

(b)

167

ndash16

5 G

a (c

)

Lapl

and-

Kol

a co

llisi

onal

oro

gen

(~1

98ndash1

91

Ga)

join

ed K

arel

ian

and

Kol

a P

roto

ndashCra

tons

(par

ts o

f Fe

nnos

cand

ia d

omei

n of

EE

C)

Vol

ynndashM

iddl

endashR

ussi

on o

roge

n (~

18ndash

17

Ga)

join

ed V

olgo

ndashSar

mat

ia a

nd F

enno

scan

dia

dom

ein

of E

EC

Vol

go-S

arm

atia

n or

ogen

(~2

1ndash2

0 G

a) jo

ined

Vol

gondashU

ralia

and

Sar

mat

ia d

omei

ns o

f E

EC

Und

iffer

entia

ted

com

plex

es o

f Fe

nnos

can

dia

(19

5ndash1

65 G

a) V

olga

ndashUra

lia a

ndS

arm

atia

(2

2ndash2

0 G

a)

The

gab

bro-

anor

thos

ite-g

rani

te (

Rap

aki

vi-li

ke)

plut

ons

(18

2ndash1

74-G

a)

Und

iffer

entia

ted

Mai

n fa

ults

(so

lid li

nes)

and

thei

r pr

opos

ed c

ontin

uatio

ns (

dash

ed li

nes)

a ndash

sut

ures

alo

ng th

e ou

ter

boun

dary

of

scel

eton

of

EE

C (

Bal

tica)

b ndash

bou

ndar

ies

of th

e bl

ocks

and

dom

eins

insi

de E

EC

bou

ndar

ies

of c

ollis

iona

l oro

gens

con

nect

ed th

e bl

ocks

and

dom

eins

tec

toni

c bo

unda

ries

of th

e M

esondash

and

Neo

prot

eroz

oic

(16

ndash08

Ga)

rift

s an

d au

laco

gens

with

in E

EC

(R

ift s

yste

ms

WS

ndash W

hite

Sea

KB

ndash K

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Bel

aya

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acog

ens

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ndash m

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e R

ussi

an M

ndash M

osco

wia

n V

ndash V

alda

y V

O ndash

Vol

yn-O

rsha

SA

ndash S

erno

vodc

k ndashA

bdul

ino

Pa

ndash P

ache

lma

La

ndash La

doga

gra

ben

Con

turs

of

the

outc

rops

of

Pre

ndashUra

lides

ndashTim

anid

es a

nd th

eir

age

anal

ogue

s in

the

Wes

tern

Ura

ls T

iman

Hill

s P

aindashK

hoi M

nts

Kan

in V

aran

ger

and

Ryb

achi

y P

enin

sula

s V

ouga

ch Is

I an

d N

ovay

a Z

emly

aar

chip

elag

o

Arc

hean

co

mp

lexes (

~37

0ndash26

0 G

a)

of

Fen

no

scan

dia

V

olg

a-U

ralia a

nd

Sarm

ati

a

Cad

omid

esndashA

valo

nide

s

Ura

lides

(Eas

tem

Ura

ls)

Var

isci

des

(Wes

tem

and

Cen

tral

Eur

ope

Sca

ndin

avia

n C

aled

onid

es (

mid

dle

and

uppe

r-m

ost n

appe

s of

Sca

ndin

avia

n C

aled

onid

es)

Figure1

Map


andstructures

oftheEast-Europ


periph

eryinclud

ingblocks

ofconsolidated



from

Kuznetsov

etal(201

0a)

LatePalaeop



oftheEEC

mod

ified

from

Bog

dano

vaet

al(200


briancomplexes

Pre-U

ralid

esndashT

imanides

attheeasternandno

rth-easternperiph

eryof


etal(200

7a)

Configu

ratio

nof

theWhite

Sea

RiftSystem

(WS)afterBaluev(200

6)Insetcontou

rsof

EECproto-craton


ralia

afterRom

anyu

ketal(201

3)

Black

linendashcontou

rof

Figure2

Yellow

symbo

lsmarklocalitiesof

samples

with

stud

ieddetritalzircon

s(starwith

number6ndashthis

stud

y)nu

mbers

oflocalitiesinside

symbo

lscorrespo

ndto

numbers

inFigures

28

9and10Abbreviations

ofgraniticmassifs

(white

letters)SSalma

Vy

Vyborg

RRiga

KKorosten

KNKorsun-Novom

irgorod

Nu

Nov

o-Ukrainsk

Ma

Mazury


Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014













Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014









Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014













Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014









Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014













Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014









Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014









Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014









Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014









Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014






Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014














Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014



Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014








Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014







Conclusions







Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





















Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014




























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014





























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014


























Dow

nloa

ded

by [

171

672

162

1] a

t 06

44 0

8 N

ovem

ber

2014

New data on detrital zircons from the sandstones of the lower Cambrian Brusov Formation (White Sea region, East-European Craton): unravelling the timing of the onset of the Arctida–Baltica

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