Constraints from Provenance Studies of Mesoproterozoic To

Precambrian Research 259 (2015) 78–94

Contents lists available at ScienceDirect

Precambrian Research

jo urnal homepage: www.elsevier.com/locate/precamres

Proterozoic supercontinental restorations: Constraints from

provenance studies of Mesoproterozoic to Cambrian clastic rocks, eastern Siberian Craton

a,∗ b a c

Andrei Khudoley , Kevin Chamberlain , Victoria Ershova , James Sears ,

d c,e f a

Andrei Prokopiev , John MacLean , Galina Kazakova , Sergey Malyshev ,

f g h i

Anatoliy Molchanov , Kåre Kullerud , Jaime Toro , Elizabeth Miller ,

j,k a,l l

Roman Veselovskiy , Alexey Li , Don Chipley

Geological Department, St. Petersburg State University, 7/9 University Nab., St. Petersburg 199034, Russia

Department of Geology and Geophysics, University of Wyoming, 1000 E. University Ave., Dept. 3006, Laramie, WY 82071, USA

Department of Geosciences, University of Montana, Missoula, MT 59812, USA

Diamond and Precious Metal Geology Institute SB RAS, Lenin Avenue 39, Yakutsk 677980, Republic Sakha (Yakutia), Russia

Southern Utah University, 351 West University Boulevard, Cedar City, UT 84720, USA

All Russian Geological Research Institute (VSEGEI), Sredniy Prospect 74, St. Petersburg 199106, Russia

Department of Geology, Faculty of Science and Technology, University of Tromsø, 9037 Tromsø, Norway

Department of Geology & Geography, West Virginia University, Morgantown, WV, USA

Department of Geological and Environmental Sciences, Stanford University, Stanford, CA 94305, USA

Geological Department, Moscow State University, 1 Vorob’evy Gory, Moscow 119899, Russia

Schmidt Institute of Physics of the Earth RAS, B. Gruzinskaya 10, Moscow 123995, Russia

Department of Geological Sciences and Geological Engineering, Queen’s University, Kingston, Ontario K7L 3N6, Canada

a r t i c l e i n f o a b s t r a c t

Article history: The Mesoproterozoic–Neoproterozoic sedimentary succession of the eastern part of the Siberian Craton

Received 28 April 2014

consists of several unconformity-bounded, kilometer-scale siliciclastic-carbonate cycles. The overlying

Received in revised form

Lower Cambrian rocks are often compositionally similar to the uppermost units of the Neoproterozoic

26 September 2014

succession.

Accepted 1 October 2014

Twenty-nine samples were collected for U–Pb detrital zircon study and 27 samples were analyzed

Available online 14 October 2014

for whole-rock Sm–Nd isotopes. In total, 1491 detrital zircon grains were dated and 1148 grains were

selected for provenance interpretation. Samples from the Uchur and Aimchan groups only contain detri-

Keywords:

tal zircons of Paleoproterozoic and Archean age. Samples from the Kerpyl Group located on the Siberian

Eastern Siberian Craton

Craton contain Paleoproterozoic and Archean grains as well, but samples from the Kerpyl Group in the

Mesoproterozoic - Lower Cambrian

U–Pb detrital zircon geochronology Sette-Daban Ridge have signiﬁcant numbers of Mesoproterozoic detrital zircons. Mesoproterozoic detri-

Sm–Nd isotopic study tal zircons predominate in samples from the Uy Group. In the northern part of the study area, samples

Provenance from the uppermost Neoproterozoic and Lower Cambrian strata contain numerous ca. 790–590 Ma detri-

Paleocontinent restoration

tal zircons, whereas in the southern part of the study area only Paleoproterozoic and Archean grains have

been found. The whole-rock Sm–Nd isotopic values of clastic rocks show that most samples have isotopic

signatures typical for the Siberian Craton basement, whereas some samples from the Kerpyl Group and

younger rock units have isotopic signatures typical of the Grenville Orogen.

Most of the Archean and Paleoproterozoic detrital zircons were eroded from the basement of the

Siberian Craton, although some ca. 2080–2030 Ma detrital zircons are likely to have a non-Siberian pro-

venance. However, rocks younger than ca. 1700 Ma are not known in the Siberian Craton basement and

all Mesoproterozoic and younger grains must therefore have a non-Siberian provenance.

The detrital zircon age distributions and whole-rock Nd isotopic signatures of many samples from

the Kerpyl Group and younger units are very close to those of the Grenville Orogen in North America,

∗

Corresponding author. Tel.: +7 9217573876.

E-mail address: [email protected] (A. Khudoley).

http://dx.doi.org/10.1016/j.precamres.2014.10.003

A. Khudoley et al. / Precambrian Research 259 (2015) 78–94 79

suggesting that erosion of the latter contributed to clastic deposition along the Siberian margin. Three pale-

ocontinental restorations proposed by Sears and Price (1978, 2003), Rainbird et al. (1998) and Pisarevsky

and Natapov (2003) are invoked to explain the occurrence of Grenville-age detrital zircons in the Siberian

sedimentary succession. The provenance of ca. 790–590 Ma detrital zircons is most likely to be located

within the Central Taimyr accretionary belt formed along the northern margin of the Siberian Craton in

the Neoproterozoic.

1. Introduction 2. Geologic setting and stratigraphy of Meso- to

Neoproterozoic rock units

The Siberian Craton is the largest structural unit of northeast

Asia, consisting of Archean to Paleoproterozoic basement and a The study area, located in eastern Siberia, occupies the east-

thick overlying Mesoproterozoic to Cenozoic sedimentary cover. It ern and central parts of the Siberian Craton and the foreland

is bordered by the Taimyr, Verkhoyansk, and Central Asian fold and of the adjacent Verkhoyansk Fold and Thrust Belt (Verkhoyansk

thrust belts to the north, east and south respectively, which display FTB), underlain by Archean and Paleoproterozoic crystalline base-

a series of extensional and compressional events related to the for- ment varying in age from ca. 3570 Ma to ca. 1700 Ma (e.g. Smelov

mation and break-up of paleocontinents from the Precambrian to et al., 2001, and references therein) (Fig. 1). Recent overviews

Mesozoic time. emphasize the distribution of ca. 2000–1850 Ma, 2600–2500 Ma

Since the study by Sears and Price (1978), many authors and 3100–2900 Ma rocks in the Siberian Craton basement that also

have discussed the relationship between the Siberia paleo- have Nd model ages (TDM) older than ca. 2100 Ma (Rosen et al.,

continent and other continents in the Precambrian. The most 2006; Smelov and Timofeev, 2007; Glebovitsky et al., 2008).

studied connection has been the one between Siberia and Lau- The Meso- to Neoproterozoic stratigraphy of the strata dis-

rentia, with differing reconstructions modeling a connection cussed here was established by Semikhatov and Serebryakov

between northern Laurentia and various parts of the Siberian (1983), and mainly followed by Shenﬁl (1991), and Melnikov et al.

Craton, including: northern Siberia (Hoffman, 1991; Pelechaty, (2005). This stratigraphy was signiﬁcantly revised as isotopic dat-

1996), eastern Siberia (Condie and Rosen, 1994), southeast- ing of magmatic and carbonate rocks was carried out (see overview

ern Siberia (Frost et al., 1998), and southern Siberia (Rainbird in Khudoley et al., 2007, and references therein). In this paper

et al., 1998; Gallet et al., 2000; Pavlov et al., 2002; Didenko we mainly follow the correlations presented by Khudoley et al.

et al., 2003). In the reconstructions proposed by Sears and (2007) with the incorporation of new data discussed here. How-

Price (1978, 2003), western Laurentia was connected to east- ever, available isotopic studies are still scarce and often insufﬁcient

ern Siberia, whereas some studies rule out a Laurentia–Siberia for reliable correlation; therefore the stratigraphic chart, proposed

connection (Smethurst et al., 1998). From 1999 to 2004 an inter- in this paper (Fig. 2) should be considered as a ﬁrst-order approxi-

national team addressed the problems concerning reconstruction mation only.

of the late Mesoproterozoic–Neoproterozoic Rodinia superconti- According to Semikhatov and Serebryakov (1983), the most

nent with Siberia forming a promontory of the supercontinent complete Meso- and Neoproterozoic succession is located along

(Li et al., 2008) following ideas discussed earlier by Pisarevsky the southeastern margin of the Siberian Craton and correspond-

and Natapov (2003). However, just a few years later, new stud- ing parts of the Verkhoyansk FTB. The Meso- and Neoproterozoic

ies provided support for a southern Siberia–northern Laurentia succession here is divided into the following six widely recognized

connection (Evans and Mitchell, 2011; Metelkin et al., 2012) and units: the Uchur Group, Aimchan Group, Kerpyl Group, Lakhanda

an eastern Siberia–western Laurentia connection (MacLean et al., Group, Uy Group and Yudoma Group (Fig. 2). According to Rus-

2009; Sears, 2012). sian stratigraphic nomenclature the ﬁrst ﬁve groups are Riphean,

These contrasting reconstructions result from a paucity of com- whereas the Yudoma Group is Vendian in age (e.g. Melnikov et al.,

parative geological data. At least three concurrent models of the 2005; Khudoley et al., 2007). The Uchur, Aimchan and Kerpyl groups

Siberian Craton basement age and composition are widely dis- are unconformity-bounded, kilometer-scale siliciclastic-carbonate

cussed (Rosen, 2003; Smelov and Timofeev, 2007; Glebovitsky transgressive cycles. Signiﬁcant unconformities are documented at

et al., 2008), casting doubt on any restoration based on matching the base of the Yudoma Group and at the base of its upper unit

basement structures from different continents. Provenance stud- as well. Smaller-scale siliciclastic-carbonate transgressive cycles,

ies appear to be more useful, giving direct information on the mainly composed of carbonates occur in the Lakhanda and Yudoma

age of eroded rocks and constraining the relationship between groups. The Uy Group is clastic and its lower part contains sev-

uplifted crustal blocks and the potential source of clastics, but eral coarsening-upward cycles several hundred meters thick. Most

only a few provenance studies of Meso- and Neoproterozoic of these formations contain indicative sedimentary structures of a

rocks of Siberia have been published to date (Rainbird et al., shallow marine depositional environment and only the Uy Group

1998; Khudoley et al., 2001; MacLean et al., 2009; Chumakov contains evidence for deeper-water gravity-mass-ﬂow sedimenta-

et al., 2011a, 2011b; Gladkochub et al., 2013; Letnikova et al., tion.

2013). Two distinct southern and northern areas are recognized, based

Since the early 2000s, many authors of this paper have been on variations in regional stratigraphy (Fig. 2). In the south, the Aim-

involved in a series of projects which included U–Pb detrital zircon chan and Uy groups are truncated westward across the platform

and whole-rock Sm–Nd dating of clastic Meso- and Neoproterozoic and, farther to the west, the Yudoma Group truncates the Kerpyl

rocks in the eastern and central parts of the Siberian Craton. The Group and unconformably rests on the Uchur Group or crystalline

main subject of this paper is to discuss these studies with an empha- basement. A recent U–Pb detrital zircon study of the lowermost

sis on their consequences for paleocontinental reconstruction. The clastic unit, previously described as a part of the lower Mesopro-

main focuses of this study are the Meso- to Neoproterozoic clas- terozoic succession and penetrated by Srednemarkhinsk 2250 Well

tic rocks that rim the Siberian Craton, but Lower Cambrian clastic in the central part of the Siberian Craton (Fig. 1), revealed that it

rocks were studied in a few locations as well. contains detrital zircon grains as young as 740 ± 5, 710 ± 4, and

80 A. Khudoley et al. / Precambrian Research 259 (2015) 78–94

Fig. 1. Distribution of the Mesoproterozoic to Neoproterozoic sedimentary basins in Siberian Craton and location of the sampled sections (after Shenﬁl, 1991; Surkov and

Grishin, 1997; Khudoley et al., 2007).

689 ± 3 Ma (Kochnev et al., 2013). Furthermore, basal conglomer- Mukun Group, has shown occurrence of detrital zircon grains as

ates are compositionally similar to the Neoproterozoic diamictites young as ca. 1000 Ma pointing to local occurrence of a Neoprotero-

from southern Siberia (Kochnev et al., 2013). If this lower clas- zoic clastic unit that has not previously been recognized (Fig. 2)

tic unit is indeed Neoproterozoic in age, the commonly accepted (Kuptsova et al., 2011).

widespread distribution of Mesoproterozoic rocks across central

Siberia (e.g. Melnikov et al., 2005) may be an overestimation, as 3. Provenance study

upper Neoproterozoic rocks correlated with the Yudoma Group

typically rest directly on crystalline basement. The basal diamictite 3.1. Sampling and analytical procedure

unit has not been reported along the eastern margin of the Siberian

Craton suggesting that deposition of the Yudoma Group and its cor- Within the study area, 29 samples for the U–Pb detrital zircon

relatives was time transgressive, commencing in different parts of study and 27 samples for the Sm–Nd whole-rock isotopic study

the Siberian Craton at different times. On the southeastern margin were collected (Online Attachment 1). U–Pb dating of detrital zir-

of the Siberian Craton, the Yudoma Group unconformably overlies cons is important for the understanding of the provenance history

the Ingili alkaline intrusion, which has yielded a U–Pb zircon age of of clastic sediments, as the age of individual grains can often be

654 7 Ma (Figs. 1 and 2) (Yarmolyuk et al., 2005). used to interpret the age of the source rock. Over the past 20 years,

In the northern part of Siberia, the stratigraphy of Meso- and detrital zircon geochronology has become the most powerful tool

Neoproterozoic rocks is more complicated reﬂecting deposition in for provenance study and also for the estimation of the maximum

mostly isolated sedimentary basins (Fig. 2). A recent carbon and depositional age of clastic rock units (e.g. Gehrels, 2012 and refer-

oxygen isotopic study by Khabarov and Izokh (2014) showed that ence therein). However, whilst zircons are numerous within felsic

the exposed section in the Kharaulakh Mountains (frontal ranges rocks, they are much rarer in maﬁc or ultramaﬁc rocks. By con-

of the Verkhoyansk FTB) is not older than ca. 800 Ma. According trast, Sm–Nd isotopic ratios in clastic rocks are very sensitive to

to U–Pb baddeleyite dating the thick Sololy sill from the Olenek the presence of juvenile rocks in the source region (e.g. McLennan

uplift is as old as 1473 24 Ma (Wingate et al., 2009), suggesting et al., 2003, and references therein). We therefore used both U–Pb

that most of the succession is early Mesoproterozoic in age. The detrital zircon and Sm–Nd whole-rock isotopic studies to obtain

sedimentary succession in the Khastakh 930 Well has been corre- the most complete information on the age and composition of the

lated with that of the Olenek uplift in different ways (Grausman, provenance regions for the clastic sediments studied.

1995; Melnikov et al., 2005). Following the similarity in the detrital U–Pb detrital zircon ages were determined using different

zircon age distribution, discussed later in this paper, we provision- equipment (Online Attachment 1). Eight samples (X04-15-3, X04-

ally correlate the Khaipakh Formation of the Khastakh 930 Well 16-2, X04-23, X04-24, X04-33, X04-34, Mls-1, TT-3) were studied

(Grausman, 1995) with the Uktinsk Formation of the Kharaulakh using the SHRIMP-RG facility at Stanford University, 4 samples

Ridge (Fig. 2). The best exposed Meso- and Neoproterozoic section (309-322, 514-2, 571-3, 678) were studied using the SHRIMP-II

was documented along the margins of the Anabar Shield, where the facility at VSEGEI (St. Petersburg), and 7 samples (09AP117, Shein1,

upper part of the clastic succession (Mukun Group) was intruded Shein6, Shein9, Khast12, Khast19, Khast55) were studied using

by a sill dated as 1513 51 Ma (Sm–Nd isochron age, Veselovskiy Cameca IMS 1280 (NORDSIM, Stockholm). LA-ICP-MS equipment

et al., 2006) or 1493 34 Ma (U–Pb baddeleyite age, Khudoley et al., was used to study 10 samples (X04-15-3, X04-16-2, X04-18, X04-

2009). Overlying carbonates are cross-cut by a 1384 4 Ma maﬁc 19, X04-21, X04-23, X04-26, X04-33, C-3, TT-4) at Washington

dyke (U–Pb baddeleyite age, Ernst et al., 2000), pointing to an State University, 3 samples (07AP36, 07AP42, 07AP43) at Queen’s

early Mesoproterozoic age of the succession. However, the recent University, and 1 sample (99JT02) at Arizona Laser Chron Center.

U–Pb detrital zircon study of a clastic unit penetrated by wells in Most samples were studied using LA-ICP-MS and SHRIMP technolo-

the southeastern part of the Anabar Shield and interpreted as the gies, and in order to ensure consistency between data from the

A. Khudoley et al. / Precambrian Research 259 (2015) 78–94 81

Fig. 2. Meso-Neoproterozoic stratigraphic chart for the eastern Siberian Craton. Ages in italics are from this study. Data source for compiled sections: Rainbird et al. (1998),

Ovchinnikova et al. (2001), Ernst et al. (2000), Semikhatov et al. (2000, 2003), Melnikov et al. (2005), Yarmolyuk et al. (2005), Veselovskiy et al. (2006), Khudoley et al. (2007,

2009), Kochnev et al., 2013, Khabarov and Izokh (2014) and references therein. Local stratigraphic unit names: Uc – Uchur Group, Am – Aimchan Group, Kr – Kerpyl Group, Lh

– Lakhanda Group, Us – Uy Group, Jd – Yudoma Group, Uk – Uktinsk Formation, Es – Eseleekh Formation, Nl – Neleger Formation, St – Sirtchan Formation, Hr – Kharayutekh

Formation, Hp – Khaipakh Formation of the Khastakh 930 Well, nn – noname unit, Hb – Khorbusuonka Group, Mk – Mukun Group, Bl – Billyakh Group, Sr – Staraya Rechka

Formation.

two instruments, we analyzed thirty-six grains from four samples 1280. Following Gehrels (2012) we used a −10% to 30% discordance

(X04-15-3, X04-16-2, X04-23, X04-33) by both instruments. Mea- cutoff for zircons studied by LA-ICP-MS to preserve the relative

surements were taken from the same spots on twenty-six grains proportion of zircons with different ages. Grains with common Pb

and from different spots on ten grains. Two of the analyses did content above 5% and with 1 error >100 Ma were also ﬁltered.

207 206 206 238

not yield interpretable results; the other thirty four Pb/ Pb Interpreted ages are based on the Pb/ U ratio for grains with

206 238 207 206

dates are equivalent within 2 error. Therefore, we assume that Pb/ U ages younger than 1000 Ma, and the Pb/ Pb ratio

206 238

there is little or no instrument bias between the datasets from the for grains with Pb/ U ages older than 1000 Ma. After ﬁltering,

two instruments (MacLean, 2007). The analytical procedures, data 1148 grains were selected for interpretation and discussion. Two

tables and concordia plots for each sample are presented in ﬁles samples (07AP-42 and Shein6) each contained one dated zircon

combined in Online Attachment 2. in each sample that was obviously younger than the depositional

A total of 1491 detrital zircon grains were dated. Individual grain age (ca. 470 Ma and 425 Ma, respectively) and these were also

ages were ﬁltered by discordance, with the ﬁlter being set at −5% excluded from the discussion. Sample 571-3 was collected from

to 10% discordance for zircons studied by SHRIMP or Cameca IMS the Mukun Group that is cut by dykes dated as 1384 ± 4 Ma (Ernst

82 A. Khudoley et al. / Precambrian Research 259 (2015) 78–94

Well successions, located in the internal parts of the Siberian Craton

(Fig. 4). The stratigraphy and facies changes of the Meso- and Neo-

proterozoic rocks of this area were discussed in detail by Khudoley

et al. (2001).

3.2.1. Lower Mesoproterozoic: Uchur Group

The easternmost succession located in the Sette-Daban Ridge

is represented by samples X04-24 and X04-26 (Figs. 2 and 4).

Sample PN-1 from Khudoley et al. (2001) is also included. Sam-

ples X04-24 and PN-1 are arkosic sandstones from the same

lowermost exposed unit and are from approximately the same

stratigraphic horizon. Sample X04-26 is a quartzose to subarkosic

sandstone with a dolomitic matrix and is from the upper part of

the Uchur Group. In total, 71 grains were used to produce the

probability plot. The detrital zircon age distribution is character-

ized by a signiﬁcant, almost unimodal, Paleoproterozoic age peak

at 2060–2055 Ma, with only two Archean grains between 2900 and

2750 Ma and a few grains younger than 2000 Ma (Fig. 5A). Deposi-

tional age of the lower unit is constrained by the age of the youngest

detrital zircon grain at 1717 ± 32 Ma (2, Khudoley et al., 2001),

whereas the youngest grain in the upper part of the Uchur Group

Fig. 3. Detrital zircon age probability plot and concordia plots for the sample Shein1.

A – concordia plot for all grains with the 32-point (gray ellipses) discordia identifying is 1521 31 Ma.

an upper intercept age at 2721 7 Ma, B – probability plot for grains that meet The succession located in the frontal ranges of the Verkhoyansk

concordance criteria,.

FTB is represented by a sample from the Ebeke-Khayata Ridge (X04-

33, Fig. 5B), whereas the succession located in the internal part

et al., 2000) and ca. 1500 Ma (Veselovskiy et al., 2006; Khudoley of the Siberian Craton is represented by a sample from the Uchur

et al., 2009). The youngest detrital zircon grain in sample 571-3 has Depression (309–322, Fig. 5C). Fifty-three and 26 grains respec-

207 206

been dated in two spots, yielding Pb/ Pb ages of 1341 41 Ma tively were used to produce the probability plots. Both samples

(spot 571-3.25.1, 4.7% discordance) and 1574 22 Ma (spot 571- are red arkosic to lithic sandstones. The detrital zircon population

3.25.2, 29.8% discordance). However, the grain has a high U content in X04-33 (platform margin) is very similar to that in the Sette-

(ca. 1600 ppm) and contains several fractures showing evidence of Daban Ridge succession displaying an almost unimodal distribution

alteration and, therefore, we did not use this grain for the maximum with a Palaeoproterozoic age peak at 2055–2050 Ma. In the Uchur

depositional age estimation. Depression, the detrital zircon population also has a prominent

Several samples with a high proportion of discordant grains Paleoproterozoic age peak but at 1980 Ma, with a few grains dated

have concordia plots with a clustered distribution. For example, at 2300–2200 Ma and 2850–2500 Ma.

the sample Shein1 contains 64 dated grains, but only 28 of them

met concordance criteria (Fig. 3A and B). However, the concor- 3.2.2. Middle Mesoproterozoic: Aimchan Group

dia diagram indicates broadly modern-day Pb loss for grains with Two samples from the Sette-Daban and Ebeke-Khayata ridges

207 206

Pb/ Pb age ranging from 2740 Ma to 2620 Ma. Although only were analyzed, X04-21 and X04-34 respectively. Both sam-

13 out of the 32 grains met the concordance criteria, the 32-point ples are quartz sandstones from the lowermost sandstone units

discordia identify an upper intercept age at 2721 7 Ma (Fig. 3A). above the unconformity between the Aimchan and Uchur groups

Although the probability plots contain only grains that met the (Figs. 2 and 4). Sample X04-21 has a dolomitic matrix. Fifty-seven

concordance criteria, a study of the clustered distribution of zircon grains were used to produce the probability plot for the Sette-

grains was also used to identify the provenance more precisely. Daban Ridge succession (X04-21). Paleoproterozoic detrital zircons

For the following discussion, we produced probability plots predominate with prominent peaks at 2050 Ma and 1980 Ma and a

combining together samples from the same area which sit within few Archean grains at 3250–2700 Ma (Fig. 6A). The three youngest

a similar part of the stratigraphy and have a similar detrital zir- grains have a weighted average age of 1696 ± 28 (2) Ma, which

con age distribution. Data from papers by Rainbird et al. (1998) and does not deﬁnitively constrain the depositional age. In the Ebeke-

Khudoley et al. (2001) were incorporated as well. Khayata Ridge succession, only 32 grains were used to produce

Sm and Nd isotopes were analyzed in the Institute of Geology the probability plot (X04-34, Fig. 6B). Both Paleoproterozoic and

and Geochronology of Precambrian of the Russian Academy of Sci- Archean grains are abundant in the detrital zircon population.

ences, St. Petersburg. The analytical procedure and data tables for Among the Paleoproterozoic grains, age probability peaks occur

these analyses are presented in Online Attachment 3. To enlarge at 2055 Ma, whereas Archean grains are distributed from 2950

the data set, data from Podkovyrov et al. (2007) and Kuptsova et al. to 2550 Ma with the most prominent age probability peak at

(2011) were incorporated as well. 2740–2735 Ma. In sample X04-34, 30 grains, including those with

high discordance, deﬁne a discordia that has an upper intercept

3.2. U–Pb detrital zircon data: Southern area with concordia at 2027 17 Ma.

In the southern area (Fig. 2) samples from the Sette-Daban Ridge, 3.2.3. Upper Mesoproterozoic: Kerpyl Group

Ebeyke-Khayata and Kyllakh ridges, Uchur Depression, and Shein The Sette-Daban Ridge succession, located within the Verkhoy-

1P Well were analyzed. Three successions with differing stratig- ansk FTB, is represented by sample X04-23. Data from sample TT-2,

raphy and structural setting are recognized: (1) the Sette-Daban previously reported by Khudoley et al. (2001) were also included.

succession, located within the Verkhoyansk FTB, (2) the Ebeke- Both samples are subarkosic sandstones and were taken from the

Khayata and Kyllakh successions, located in the frontal ranges of basal part of the succession just above the pre-Kerpyl unconformity

the Verkhoyansk FTB where deformed sedimentary cover of the (Figs. 2 and 4). In total, 115 grains have been used to produce the age

Siberian Craton is exposed, (3) the Uchur Depression and Shein 1P probability plot. Fifty-one grains (44% of the total population) are

A. Khudoley et al. / Precambrian Research 259 (2015) 78–94 83

Fig. 4. Correlation chart for the Mesoproterozoic and Neoproterozoic sedimentary units of the southern area showing location of samples for U–Pb detrital zircon dating and

facies and thickness changes of rock units. Uc – Uchur Group, Am – Aimchan Group, Kr – Kerpyl Group, Lh – Lakhanda Group, Us – Uy Group, Jd – Yudoma Group.

Data source: Semikhatov and Serebryakov (1983), Khudoley et al. (2001, 2007) and Melnikov et al. (2005).

Mesoproterozoic in age showing an age distribution with promi- 99JT02) were collected (Figs. 2 and 4). Data from sample MM-1,

nent peaks at 1200 Ma, 1495 Ma, and 1560–1555 Ma (Fig. 7A). Fifty previously reported by Rainbird et al. (1998), were also used in our

ﬁve grains (48%) are of Paleoproterozoic age, with the most promi- compilation. Sandstone composition varies from greywacke and

nent peak at 2035–2030 Ma and several subordinate peaks ranging lithic sandstone to arkose and subarkose. All studied samples are

from 1950 to 1820 Ma. Only 9 grains (8%) are Archean, ranging in quite immature in composition.

age from 2900 to 2550 Ma. The four youngest grains overlap in In total, 185 grains were used to produce the age probability plot.

age within 1 error and yield a weighted average age at 1120 ± 17 Mesoproterozoic grains predominate, comprising 71% of the whole

(2 ) Ma, providing a maximum age for the host sediments. population (Fig. 8) with peaks at 1085–1080 Ma, 1155–1150 Ma,

The Kyllakh Ridge succession, located in the frontal ranges of the 1245–1240 Ma, 1395–1390 Ma and 1465–1460 Ma. Paleoprotero-

Verkhoyansk FTB with deformed sedimentary cover of the Siberian zoic and Archean grains are subordinate, displaying much smaller

Craton, is represented by samples TT-3 and TT-4. Both samples are peaks at 1655–1650 and 2715–2710 Ma.

red subarkosic sandstones from the lower clastic unit of the Ker- The Uy Group comprises several locally recognized strati-

pyl Group. In total, 76 grains were used to produce the probability graphic units with a debatable correlation (e.g. Semikhatov and

plot (Fig. 7B) with only Paleoproterozoic and Archean grains doc- Serebryakov, 1983; Khudoley et al., 2001; Melnikov et al., 2005,

umented. Paleoproterozoic grains predominate with a major peak and references therein). In the easternmost exposures, the upper-

at 1960 Ma on the probability plot, whilst Archean grains range in most unit consists of red lithic sandstones (Mayamkan Formation)

age from 3300 to 2550 Ma and form a peak at 2725–2720 Ma. where the youngest individual grain yields an age of 1070 ± 40 Ma

(Rainbird et al., 1998). In the central part of the basin, the 6 youngest

3.2.4. Upper Mesoproterozoic–Lower Neoproterozoic: Uy Group grains from sample C-3 within the uppermost sandstone beds of

The Uy Group is exposed only in the Verkhoyansk FTB succes- the Uy Group have ages overlapping within 1 error and yield a

sion in the Sette-Daban Ridge, where 3 samples (C-3, Mls-1 and weighted average age of 920 45 (2 ) Ma.

84 A. Khudoley et al. / Precambrian Research 259 (2015) 78–94

Fig. 6. Southern area, middle Mesoproterozoic Aimchan Group: detrital zircon prob-

ability versus age plot for samples from Sette-Daban (A) and Ebeke-Khayata (B)

ridges. See location in Figs. 1 and 4.

intercept age of 2027 ± 16 Ma. Only 3 grains are Archean in age,

ranging from 3500 to 2600 Ma. The detrital zircon population in

the upper Yudoma Group has a similar distribution with peaks at

1995 and 2070–2065 Ma, with a few Archean grains ranging in age

from 2850 to 2550 Ma. However, the upper Yudoma Group sample

(X04-16-2, Fig. 9B) contains a cluster of late Neoproterozoic detrital

zircon grains, among which the 3 youngest grains with ages that

overlap within 1 error yield a weighted average age of 605 ± 17

(2 ) Ma. The detrital zircon age distribution in the Lower Cambrian

sample (X04-15-3, Fig. 9C) is characterized by an almost unimodal

Fig. 5. Southern area, lower Mesoproterozoic Uchur Group: detrital zircon proba- wide Paleoproterozoic age peak at 1985–1960 Ma, with only a few

bility versus age plot for samples from Sette-Daban Ridge (A), Ebeke-Khayata Ridge

Paleoproterozoic grains ranging in age from 2200 to 2100 Ma and

(B), and Uchur Depression (C). See location in Figs. 1 and 4. Data from sample PN-1

a few Archean grains ranging in age from 2900 to 2650 Ma.

(Khudoley et al., 2001) are included.

The Shein 1P Well succession is located within the Siberian Cra-

ton and is represented by 3 samples (Shein1, Shein6 and Shein9).

In total, 122 grains were used to produce the probability age plot

3.2.5. Uppermost Neoproterozoic (Yudoma Group) and Lower

Cambrian (Fig. 9D). Fifty-two percent of the total detrital zircon popula-

tion are Paleoproterozoic grains with several age peaks between

The Yudoma Group and its correlatives were studied in the

2050 Ma and 1900 Ma. Archean grains comprise 35% of the total

Verkhoyansk FTB (Sette-Daban Ridge) and central part of the

population ranging in age from 3150 to 2500 Ma and displaying

Siberian Craton (Shein 1P Well) successions (Figs. 2 and 4). In the

a prominent peak at 2735 Ma. Thirty-two grains (including those

Sette-Daban Ridge, the Yudoma Group is separated into two parts

that are highly discordant) from the sample Shein1 identify a chord

by an unconformity. The Lower Cambrian sedimentary units and

a with a 2721 ± 7 Ma upper intercept age (Fig. 3A). Mesoprotero-

the upper Yudoma Group are lithologically similar and form a single

succession. zoic grains (12%) are almost uniformly distributed from 1550 to

1100 Ma, whilst the youngest grain yielded an age of 860 ± 9 Ma.

The Sette-Daban succession is represented by samples X04-18,

19 (lower Yudoma Group), X04-16-2 (upper Yudoma Group) and

X04-15-3 (Lower Cambrian) (Fig. 4) with 70, 61 and 60 grains ana- 3.3. U–Pb detrital zircon data: Northern area

lyzed respectively and used to produce the age probability plots.

The detrital zircon population in the lower Yudoma Group dis- In the northern area (Fig. 2) samples are available from the

plays peaks at 1990 and 2070–2065 Ma (Fig. 9A). However, all 39 Kharaulakh Ridge, Khastakh 930 Well and along the eastern and

grains from sample X04-19 identify a discordia line with an upper northern margins of the Anabar Shield. The Kharaulakh Ridge

A. Khudoley et al. / Precambrian Research 259 (2015) 78–94 85

Fig. 7. Southern area, upper Mesoproterozoic Kerpyl Group: detrital zircon proba-

bility versus age plot for samples from Sette-Daban (A) and Kyllakh (B) ridges. See

location in Figs. 1 and 4. Data from sample TT-2 (Khudoley et al., 2001) are included.

succession has approximately the same structural setting as the

Ebeke-Khayata and Kyllakh Ridge successions being located in

the frontal ranges of the Verkhoyansk FTB. The two other sample

locations (Khastakh 930 Well and Anabar Shield) characterize the

central part of the Siberian Craton. Structural and stratigraphic cor-

relatives of the Sette-Daban Ridge are not exposed in the northern

Verkhoyansk FTB. The stratigraphic setting of the studied samples

is shown in Fig. 10. Additional details on the stratigraphy and facies

changes of the Meso- and Neoproterozoic rocks of this area were

discussed by Sears et al. (2004), Melnikov et al. (2005) and Khudoley

et al. (2007).

Fig. 9. Southern area, uppermost Neoproterozoic Yudoma Group and Lower Cam-

brian: detrital zircon probability versus age plot for samples from Sette-Daban Ridge

(A–C) and Shein 1P Well (D). See location in Figs. 1 and 4.

Fig. 8. Southern area, upper Mesoproterozoic–lower Neoproterozoic Uy Group:

detrital zircon probability versus age plot for samples from Sette-Daban Ridge. See

location in Figs. 1 and 4. Data from sample MM-1 (Rainbird et al., 1998) are included.

86 A. Khudoley et al. / Precambrian Research 259 (2015) 78–94

Fig. 10. Correlation chart for the Mesoproterozoic and Neoproterozoic sedimentary units of the northern area showing location of samples for U–Pb detrital zircon dating and

facies and thickness changes of rock units. Uk – Uktinsk Formation, Es – Eseleekh Formation, Nl – Neleger Formation, St – Sirtchan Formation, Hr – Kharayutekh Formation,

Hp – Khaipakh Formation, Hb – Khorbusuonka Group, Mk – Mukun Group, Bl – Billyakh Group, Sr – Staraya Rechka Formation.

Data source: Semikhatov and Serebryakov (1983), Grausman (1995), Melnikov et al. (2005), Khudoley et al. (2007) and Khabarov and Izokh (2014).

3.3.1. Lower Mesoproterozoic: Mukun Group

Clastic rocks of the Mukun Group were studied along the eastern

and northern margins of the Anabar Shield (Figs. 1 and 10). All sam-

ples (514-2, 571-3, 678) are red quartzose to subarkosic sandstones

located just above the unconformity between the crystalline base-

ment of the Siberian Craton and the overlying sedimentary cover.

In total, 84 zircon grains were used to produce the age probability

plot (Fig. 11).

Detrital zircon ages range from 2900 to 1600 Ma. Approxi-

mately 82% of the total zircon population is Paleoproterozoic in

age, whereas 18% of the grains are Archean. The most prominent

peak is documented at 1965 Ma, with smaller peaks at 1720 Ma

and 2705–2700 Ma. All grains that are signiﬁcantly younger than

1900 Ma are present only in sample 678, where the 8 youngest

Fig. 11. Northern area, lower Mesoproterozoic Mukun Group: detrital zircon prob-

grains have ages that overlap within 1 error and yield a weighted

ability versus age plot for samples from the Anabar Shield margins. See location in

average age of 1681 ± 28 Ma.

Figs. 1 and 10.

A. Khudoley et al. / Precambrian Research 259 (2015) 78–94 87

Fig. 13. Northern area, uppermost Neoproterozoic Yudoma Group and Lower Cam-

Fig. 12. Northern area, upper Neoproterozoic Khaipakh and Uktinsk formations:

brian: detrital zircon probability versus age plot for samples from Kharaulakh Ridge

detrital zircon probability versus age plot for samples from the Kharaulakh Ridge

(A) and Khastakh 930 Well (B). See location in Figs. 1 and 10.

3.3.2. Neoproterozoic: Uktinsk and Khaipakh Formations On the Kharaulakh Ridge, all samples are quartzose to sub-

Neoproterozoic clastic rocks were studied in the Kharaulakh arkosic sandstones. Several peaks with ages at 800–580 Ma,

Ridge (Uktinsk Formation, sample 09AP117) and in the Khastakh 1320 Ma, 2140–2070 Ma, 2560 Ma and 2870 Ma are documented

930 Well (Khaipakh Formation, samples Khast12 and Khast19) (Fig. 13A). In the Khastakh 930 Well, sample Khast55 is a lithic

(Figs. 2 and 10). The stratigraphic correlation of these units is ques- sandstone. Approximately 80% of the total population are detrital

tionable and they could be as young as uppermost Neoproterozoic zircons of Neoproterozoic age, forming a prominent peak at 715 Ma

(Melnikov et al., 2005; Khabarov and Izokh, 2014). All samples are and smaller peaks at 600–595 Ma and 645–640 Ma (Fig. 13B). A few

quartz sandstones. In total, 56 and 66 grains from the Kharaulakh Paleoproterozoic grains ranging in age from 2150 to 1900 Ma and a

Ridge and Khastakh 930 Well respectively were used to produce few Archean grains ranging in age from 2900 to 2650 Ma are present

the probability age plots (Fig. 12A and B). as well.

Detrital zircon age distributions in the Kharaulakh Ridge and

within the Khastakh 930 Well are very similar. Approximately

3.4. Sm–Nd whole-rock isotopic study

70% of the whole populations is Paleoproterozoic in age, whilst

30% of the populations is Archean. In both areas, the most promi-

The same sandstone units sampled for the U–Pb detrital zir-

nent peaks are documented at 1860–1850 Ma for Paleoproterozoic

con study were also sampled for the Sm–Nd isotopic study. The

grains and 2735–2730 Ma for Archean grains. A subordinate peak at

same sample was often studied by both methods or, at least, closely

1990–1985 Ma is also documented for the Kharaulakh Ridge sam-

located samples were selected for the analyses (Figs. 4 and 10,

ple and at 1925–1920 Ma and 2035–2030 Ma for samples from the

Online Attachment). Data by Podkovyrov et al. (2007) and Kuptsova

Khastakh 930 Well. In sample Khast12, 31 grains (including those

et al. (2011) were also incorporated into this study. Most of the

that are highly discordant) deﬁne a chord that has an upper inter-

studied samples are sandstones. Podkovyrov et al. (2007) tested

cept with concordia at 2739 ± 22 Ma.

both sandstone and shale samples and did not found signiﬁcant

variations between the two. Results of the study are presented in

ε ε

3.3.3. Uppermost Neoproterozoic (Kharayutekh Formation) and Fig. 14 and are interpreted in terms of Nd(t) (i.e. Nd at the time of

Lower Cambrian deposition), along with Nd model age TDM.

Clastic rocks of the Kharayutekh Formation were studied in the In the southern area, all samples from the lower and middle

Kharaulakh Ridge (samples 07AP36, 07AP42, 07AP43), whereas the Mesoproterozoic rocks (Uchur and Aimchan groups) have Nd(t)

Lower Cambrian succession was studied in the Khastakh 930 Well that fall within the ﬁeld of the Siberian Craton basement with

(sample Khast55) (Figs. 2 and 10). In total, 28 and 46 grains were TDM ranging from late Archean to early Paleoproterozoic. However,

analyzed from the Kharaulakh Ridge and Khastakh 930 Well respec- Nd(t) values vary signiﬁcantly within the upper Mesoproterozoic

tively to produce the age probability plots. and lower Neoproterozoic rocks. Samples from the Kerpyl Group

88 A. Khudoley et al. / Precambrian Research 259 (2015) 78–94

for the Siberian Craton basement and correspond to Archean TDM

␧

(Fig. 14). In the uppermost Neoproterozoic rock units, Nd(t) val-

ues are relatively high (−10.9 and −14.1) but still lie within the

Siberian Craton basement ﬁeld. However, the Lower Cambrian sam-

ple from the Khastakh 930 Well (Khast55) has a positive Nd(t)

(+1.8) value and lies signiﬁcantly above the Siberian Craton base-

ment ﬁeld (Fig. 14).

4. Discussion

4.1. Tectonic and magmatic events within the Siberian Craton

and adjacent areas: Siberian and non-Siberian provenance

Detrital zircon age distribution diagrams and their peaks reﬂect

stages of tectonic and magmatic activity in the provenance area and

may be used to better understand the tectonic and magmatic evo-

lution of source regions. This interpretation is more complicated

if detrital zircons came from older sediments and not magmatic

or metamorphic rocks, but the immature composition and/or rel-

atively high Nd(t) values in our samples suggest that reworking

of older sediments was not important during deposition of most

of the studied clastic units. The most mature quartz sandstones

are typically found in the uppermost Neoproterozoic rock units

throughout the Siberian Craton; however they often contain detri-

tal zircons that are close in age to the depositional age of the host

sediments (e.g. ca. 605 Ma detrital zircon grains in sample X04-16-

2 or ca. 540–580 Ma grains in sample5 07AP42) pointing to erosion

of magmatic rocks as well. Therefore, we infer that detrital zircon

ages mainly reﬂect the age of magmatic and metamorphic rocks in

the provenance, although some input from older sediments can-

not be ruled out. To ease correlations between studied samples, all

detrital zircon age distribution diagrams (Figs. 5–9 and 11–13) are

plotted together at the same scale (Fig. 15).

Amongst the detrital zircons of Archean age, peaks at

2900–2850 Ma and 2750–2700 Ma are most typical (Fig. 15). Detri-

tal zircon grains of 2850–2900 Ma are documented in almost all

Fig. 14. Whole-rock Nd isotope evolution diagram for Mesoproterozoic–Lower

Cambrian clastic rocks from the southern and northern areas of the eastern Siberia. samples in the northern area, but the nearest provenance area com-

White symbols – this study, black symbols – after Podkovyrov et al. (2007) for prising source rocks of this age is located in the western part of

southern area, and Kuptsova et al. (2011) for northern area. Dashed lines show

the Aldan Shield (Kotov, 2003). Detrital zircons of 2750–2700 Ma

approximate age of sampled units in accordance with stratigraphy presented in

have been found in both the northern and southern areas, form-

Fig. 2. Siberian Craton ﬁeld after Kovach et al. (2000), Smelov et al. (2001) and Rosen

ing peaks on the age distribution diagrams for almost all samples.

et al. (2006). Grenville Orogen ﬁeld after Dickin et al. (2009), McLelland et al. (2010)

and McNutt and Dickin (2012). Uc – Uchur Group, Am – Aimchan Group, Kr – Kerpyl They are most widespread in the samples from the internal part

Group, Lh – Lakhanda Group, Us – Uy Group, Jd – Yudoma Group, Nl – Neleger For-

of the Siberian Craton, where the Khast12 and Shein1 samples

mation, Hp – Khaipakh Formation, Hb – Khorbusuonka Group, nn – noname unit,

have signiﬁcant numbers of highly discordant detrital zircon grains

Mk – Mukun Group, Bl – Billyakh Group, Sr – Staraya Rechka Formation.

which have upper intercept ages with concordia at 2739 ± 22 and

2721 ± 7 Ma, respectively, likely pointing to the proximal location

ε − −

show variations in Nd(t) from 12.6 to 1.3 on the Siberian Craton of the provenance. However, rocks of such ages are not known to be

− −

and from 4.7 to 7.5 in the Sette-Daban Ridge. Most samples have typical for the Siberian Craton basement and have only been docu-

values that fall within the ﬁeld of the Siberian Craton basement, but mented previously in the western part of the Aldan Shield (Kotov,

ε −

one sample with Nd(t) = 1.3 (data by Podkovyrov et al., 2007) from 2003; Rosen et al., 2006; Smelov and Timofeev, 2007; Glebovitsky

the Siberian Craton margin has an isotopic signature that cannot be et al., 2008). However, most of the Siberian Craton basement is now

explained by erosion of the Siberian Craton basement. Shales from covered by thick sedimentary cover (Fig. 1) and it is quite possible

ε −

the Lakhanda Group have high Nd(t) values ranging from 2.4 to that basement rocks of these ages have been deeply buried beneath

+1.8, which are much higher than those expected for the Siberian younger sediments.

Craton basement and correspond to a late Paleoproterozoic–early Detrital zircons of Paleoproterozoic age form 2 prominent peaks

Mesoproterozoic TDM (Fig. 14). In the Uy Group, Nd(t) values range at 2080–2030 Ma and 2000–1950 Ma. A signiﬁcant number of

− −

from 6.2 to 2.4 and are located above the ﬁeld of the Siberian highly discordant detrital zircon grains in samples X04-34 and X04-

Craton basement. The uppermost Neoproterozoic (Yudoma Group) 19 identify discordia with almost the same upper intercept ages

and Lower Cambrian samples form 2 clusters where samples from of 2027 ± 17 Ma, likely pointing to the widespread distribution of

one cluster have very low Nd(t) values typical of the Siberian Cra- rocks of this age in the provenance region. Only one prominent peak

− −

ton basement (from 20.9 to 11.1), whereas samples from the is documented in most of the samples, but in rock units such as the

ε − −

other cluster have high Nd(t) values ( 1.0 and 3.5) and are located Aimchan and Yudoma groups of the Sette-Daban Ridge, both peaks

above the ﬁeld of the Siberian Craton basement. occur (Figs. 5, 9 and 15). The age peak at 2000–1950 Ma ﬁts pre-

In the northern area, all samples except for the uppermost cisely with the main magmatic and metamorphic event recognized

Neoproterozoic–Cambrian have low Nd(t) values that are typical throughout the Siberian Craton (Kotov, 2003; Rosen et al., 2006;

A. Khudoley et al. / Precambrian Research 259 (2015) 78–94 89

Fig. 16. Detrital zircon grains with location of shots, sample 678, Anabar Shield,

Mukun Group. A – grain 678.15.1, 1765 ± 42 Ma; B – grain 678.17.1, 1692 ± 47 Ma.

The available detrital zircon data therefore provides evi-

dence for both Siberian and non-Siberian provenance of the ca.

2080–2030 Ma detrital zircon grains. In the southern area, ca.

2050 Ma detrital zircon grains have been found in the internal

part of the Siberian Craton (Shein 1P Well), where they are likely

to have been derived from a local provenance (Figs. 9 and 15).

For the Uchur Group clastic rocks with almost uniform detrital

zircon age distribution and a prominent peak at 2060–2050 Ma

(Figs. 5 and 15), both facies transitions and paleocurrent data sup-

port a provenance from the Siberian Craton (Khudoley et al., 2001).

By contrast, samples from the Sette-Daban succession of the Ker-

pyl Group display a prominent peak at 2035–2030 Ma with only a

few grains of 2000–1950 Ma, whereas samples from the Siberian

Craton succession display a prominent peak at 1960 Ma and only

a few grains of 2080–2030 Ma (Figs. 7 and 15). This relationship

may be interpreted as evidence for an eastern (in present coor-

dinates), non-Siberian source of ca. 2080–2030 Ma detrital zircon

grains. Facies transitions within the Yudoma Group sandstone unit

with numerous 2070–2060 Ma detrital zircon grains also point to

an eastern non-Siberian provenance (Khudoley et al., 2001). In

the northern area, ca. 2080–2070 Ma detrital zircon grains have

been found on the Kharaulakh Ridge and in the Khastakh 930 Well

(Figs. 13 and 15), where they are likely to have been locally derived

from the Olenek uplift where granite intrusions close to this age

are exposed (Wingate et al., 2009).

Two prominent peaks at ca. 1850 and 1720 Ma docu-

mented in the Mukun Group, Khaipakh and Uktinsk formations

(Figs. 11, 12 and 15) across the northern area, are likely to have been

derived from a local provenance as granite intrusions of ca. 1850 Ma

are abundant across the northeastern part of the Siberian Craton

(Rosen et al., 2006). Detrital zircons of ca. 1720 Ma often consist

of elongated euhedral grains typical of felsic magmatic rocks, with

no evidence for a long transport distance or reworking (Fig. 16).

Rift-related felsic volcanics of similar age have also been reported

from the southeastern Aldan Shield and Prikolyma cratonic terrane,

Fig. 15. Comparison of the Mesoproterozoic–Lower Cambrian U–Pb detrital zircon

pointing to the craton-wide distribution of related magmatic and

age relative probability plots of samples from both southern and northern areas of

the eastern Siberia. Gray belts show distribution and age of the most widespread tectonic events (Khudoley et al., 2007, and references therein).

magmatic and tectonic events.

Magmatic rocks younger than ca. 1700 Ma are not widely dis-

tributed in the Siberian Craton basement and the Siberian Craton

therefore cannot represent a provenance for the numerous detrital

Smelov and Timofeev, 2007; Glebovitsky et al., 2008). In contrast zircons of this age found in the Kerpyl Group and younger rocks,

to the ca. 2000–1950 Ma rock units, magmatic and metamorphic both in the southern and northern areas. Two major clusters of

rocks of 2080–2030 Ma are very rare in the Siberian Craton base- non-Siberian detrital zircon populations with ages ranging from

ment and were found only locally (e.g. Rosen et al., 2006; Wingate 1650 Ma to 950 Ma and from 720 Ma to 590 Ma are recognized in

et al., 2009). the southern and northern areas respectively. Non-Siberian sources

90 A. Khudoley et al. / Precambrian Research 259 (2015) 78–94

for these strata are also suggested by Nd isotopic data, as a signiﬁ- Grenville Orogen (McLelland et al., 2010). Sm–Nd isotopic charac-

cant number of samples from the Kerpyl Group and younger units teristics of many samples from the Kerpyl, Lakhanda and Uy groups

have Nd isotopic signatures typical of Grenville Orogen or younger are also similar to those from the Grenville Orogen (Fig. 14, Dickin

crust (Fig. 14) and cannot be derived from erosion of the Siberian et al., 2009; McLelland et al., 2010; McNutt and Dickin, 2012). In

Craton basement. light of this data, we interpret the Grenville Orogen in North Amer-

The uppermost Neoproterozoic Yudoma Group clastic units doc- ica as the most likely provenance for the clastic rocks of the Kerpyl

ument an important tectonic event which resulted in a signiﬁcant and Uy groups.

shift of the clastic provenance during the latest Neoproterozoic The spatial distribution of Grenville-age detrital zircons in the

(Figs. 14 and 15). Clastic sediments in the Kerpyl and, especially, sedimentary successions along the eastern margin of the Siberian

Uy groups are dominated by detrital zircons with Mesoproterozoic Craton is not clear. In the northern area, rocks of the Uktinsk For-

ages, whereas clastic rocks of the Yudoma Group do not contain mation contain only Paleoproterozoic and Archean detrital zircons

Mesoproterozoic detrital zircons along the Siberian Craton mar- (Fig. 12A). Detrital zircon age distribution of the Uktinsk Formation

gin (Fig. 9A–C) and have only a small number in the central part is quite similar to that of the Kerpyl Group from the Kyllakh Ridge,

of the craton (Fig. 9D). In contrast to the underlying rock units, where only Paleoproterozoic and Archean grains were reported as

clastic rocks of the Yudoma Group are dominated by Paleopro- well (Figs. 7, 12 and 15). However, both the Kharaulakh and Kyllakh

terozoic detrital zircons. However, this shift in the detrital zircon ridges are located along the frontal thrusts of the Verkhoyansk FTB

age distribution only partly correlates with the Nd isotopic com- and have the same structural setting (Prokopiev and Deikunenko,

position of the same rocks, as rock samples of the Yudoma Group 2001; Khudoley and Prokopiev, 2007). If so, correlative strata of

occupy two different ﬁelds on the Nd(t) – stratigraphic age diagram the Sette-Daban Ridge, with numerous Grenville-age detrital zir-

(Fig. 14). Most samples fall within the ﬁeld of Paleoproterozoic cons, should be located to the east of the Kharaulakh Ridge where

and Archean crust, which correlates well with the predominance they would be buried beneath a thick succession of younger rocks.

of Paleoproterozoic detrital zircon grains in the sandstones. How- Similarly, correlative strata to the Uy Group, if existing in the north-

ever, two samples have high Nd(t) values that fall within the ﬁeld ern area, would also be expected east of the Kharaulakh Ridge but

of much younger crust typical of the Grenville Orogen (Fig. 14). are not exposed in the modern structure. However, a recent study

The absence of young detrital zircons is interpreted as a result of by Powerman et al. (2013) illustrated a widespread distribution

the erosion of juvenile rocks in the provenance area, which do not of Mesoproterozoic zircons along the southwest margin of Siberia

contain a signiﬁcant number of zircons but signiﬁcantly affect the (Yenisey Ridge) making a relationship between a Grenville-age pro-

Nd isotopic signature (e.g. Podkovyrov et al., 2007). These juve- venance and sedimentary basins along the eastern margin of the

nile rocks are most likely to consist of MORB-like basalts, which Siberian Craton quite complicated (Fig. 17). By contrast, available

are characterized by high Nd(t) values but contain very few zir- detrital zircon studies show no contribution of the Grenville-age

cons. Although maﬁc sills intruded into the Uy Group have quite magmatic rocks to the Neoproterozoic clastic succession deposited

high Nd(t) values (Khudoley et al., 2007), the absence of Meso- along the southern margin of the Siberian Craton (Chumakov et al.,

proterozoic detrital zircons suggests that the Yudoma Group does 2011a, 2011b), with exception of a few grains ranging in age from

not contain any clastics reworked from the older Uy Group. The ca. 1000 Ma to 1520 Ma (Gladkochub et al., 2013; Letnikova et al.,

maﬁc magmatic unit responsible for the shift in the Nd(t) values 2013). Available data on the tectonics of the Lake Baikal area

of 2 samples from the Yudoma Group is likely to be younger than and further to the south do not support the occurrence of the

the Uy Group age and represent an unknown magmatic and tec- Grenville Orogen there either (Demoux et al., 2009; Rytsk et al.,

tonic event so far undocumented on the southeastern margin of 2007; Kozakov et al., 2011, 2012; Rojas-Agramonte et al., 2011;

the Siberian Craton. Kröner et al., 2013). Therefore, despite a similarity in the detrital

zircon ages distribution, provenance areas of the Kerpyl and Uy

4.2. Non-Siberian provenance of clastic rocks and supercontinent groups of the Sette-Daban Ridge and their possible chronostrati-

restorations graphic equivalents on the Yenisey Ridge were not derived from

a single orogenic belt, but were derived from spatially separated

The upper Mesoproterozoic and lower Neoproterozoic Ker- continental blocks of similar age.

pyl and Uy groups, along with the Lower Cambrian clastic rocks, All published tectonic reconstructions which suggest that the

contain numerous 1650–950 Ma and 720–590 Ma detrital zircon Siberian Craton was not connected to other continental blocks

grains, which we interpret to have a non-Siberian provenance. In during the Proterozoic, or suggest a northern Siberia–northern

order to explain their widespread distribution we reviewed several Laurentia or eastern Siberia–northern Laurentia connection, do

paleocontinental reconstructions with reference to paleomagnetic not place southern Siberia close to the provenance of Grenville-

data. In contrast to many previous restorations, we do not dis- age detrital zircons and can therefore be ruled out by our data

cuss details of basement tectonics because of the existence of and are not considered further here (Hoffman, 1991; Condie and

several very different interpretations of the Siberian Craton base- Rosen, 1994; Pelechaty, 1996; Smethurst et al., 1998). Three pale-

ment (Rosen, 2003; Smelov and Timofeev, 2007; Glebovitsky et al., ocontinental restorations are proposed to explain the widespread

2008), which renders any reconstructions based on correlation distribution of Grenville-age detrital zircons in the Kerpyl and Uy

of the Archean and Paleoproterozoic provinces inconclusive and groups of southern Siberia (Fig. 18).

ambiguous. The restoration by Pisarevsky and Natapov (2003) was based on

The widespread distribution of non-Siberian 1650–950 Ma paleomagnetic data and presented on the Rodinia map (Li et al.,

detrital zircon grains in immature lithic sandstones requires a 2008), followed by Pisarevsky et al. (2008) and Didenko et al.

proximal source region. The three youngest age peaks on the age (2009). According to this restoration, Siberia was located at some

probability plot of the Uy Group (Fig. 8, 1085–1080, 1155–1150, distance from Laurentia with southern Siberia facing the northern

and 1245–1240 Ma) can be attributed to the Ottawan, Shawinigan margin of Laurentia and the presence of an unknown continen-

and Elzevirian orogenies of the Grenville Orogen in North Amer- tal block between them. Hypothetically, the unknown continental

ica (McLelland et al., 2010). A smaller peak at 985–980 Ma can be block may contain a signiﬁcant volume of North America – like

correlated to the Rigolet Phase, whereas older peaks at 1395–1390, Grenville age terranes. If so, it may explain the widespread distribu-

1465–1460, and 1655–1650 Ma ﬁt reasonably well with the age of tion of Mesoproterozoic zircons in sedimentary successions across

granite intrusions and metamorphic rocks also reported from the the southeastern and southwestern margins of Siberia. However,

A. Khudoley et al. / Precambrian Research 259 (2015) 78–94 91

Fig. 17. Cartoon representation of potential provenances of Grenville-age detrital zircons for the Kerpyl and Uy groups and their correlatives (ca. 1100–900 Ma) and of

Grenville-age and ca. 790–590 Ma detrital zircons for the Yudoma Group and Lower Cambrian clastic rocks (ca. 650–530 Ma).

no data on the composition of this inferred continental block is or are unknown along the eastern margin of the Siberian Craton.

available. A hypothetical continental terrane capable of supplying the south-

Sears and Price (1978) suggested that eastern Siberia was western margin of Siberia with Mesoproterozoic detrital zircons is

attached to the western margin of Laurentia, whilst a later mod- required in this restoration.

iﬁcation of the reconstruction placed Australia to the south of The restoration by Rainbird et al. (1998) corresponds well with

Siberia (Fig. 18) (Sears and Price, 2003). This restoration positions paleomagnetic data (Ernst et al., 2000; Pavlov et al., 2002; Evans

the southeastern margin of the Siberian Craton close to the south- and Mitchell, 2011; Metelkin et al., 2012). Magmatic events of

ern extension of the Grenville Orogen (Sears and Price, 2003; ca. 1710 Ma as well as ca. 740–720 Ma and 780 Ma from south-

Sears, 2012) but contradicts the paleomagnetic data presented by ern Siberia are well correlated with almost synchronous events in

Pisarevsky and Natapov (2003). Magmatic events at ca. 1720 Ma, northern Laurentia (Thorkelson et al., 2001; Harlan et al., 2003;

1500 Ma and 1384 Ma, as along with latest Neoproterozoic–Early Macdonald et al., 2010; Gladkochub et al., 2010), whilst Meso-

Cambrian rifting, are documented along both the eastern margin proterozoic magmatic events at ca. 1384 Ma and 1267 Ma are not

of the Siberian Craton and the western margin of the North Ameri- known from the southern Siberian Craton margin. The northern

can Craton (Sears and Price, 2003). However, the ca. 1005–930 Ma continuation of the Grenville Orogen to Greenland and further

magmatic event documented on the Sette-Daban Ridge (Khudoley north toward the proposed location of the Sette-Daban Ridge

et al., 2007) is a bit younger than the magmatic event described (Fig. 18) was argued by Pisarevsky and Natapov (2003), but recent

from the proposed counterpart in California (ca. 1080 Ma, Heaman studies of detrital zircons and conglomerates from Neoproterozoic

and Grotzinger, 1992), whilst magmatic events that occurred at ca. and Paleozoic rocks of Greenland and the Arctic islands support the

780–650 Ma and are widely distributed in western North America continuation of the Grenville Orogen toward northern Greenland

(Lund et al., 2010; Link and Christie-Blick, 2011; Mahon et al., 2014), and further north below the Arctic Ocean (Kirkland et al., 2009;

have a very small distribution (ca. 654 Ma, Yarmolyuk et al., 2005) Lorenz et al., 2013, and references therein). However, an unknown

Fig. 18. Cartoon representation of three possible paleocontinent restorations for Siberia and Laurentia to explain wide distribution of Grenville-age detrital zircons in Siberia.

White star – Sette-Daban Ridge, black star – Yenisey Ridge, black belt – Grenville Orogen. Question marks show possible northward (present coordinates) continuation of

the Grenville Orogen (Kirkland et al., 2009; Lorenz et al., 2013).

92 A. Khudoley et al. / Precambrian Research 259 (2015) 78–94

continental block that supplied the southwestern margin of the Sandstones from the Kerpyl and Uy groups contain numerous

Siberian Craton with Mesoproterozoic detrital zircons is again detrital zircons with ages ranging from 1650 Ma to 950 Ma. Crys-

required in this restoration. talline rocks of these ages are not known from the basement of the

In the southern area, clastic rocks of the Yudoma Group do Siberian Craton, but age peaks on the detrital zircon probability plot

not contain any Mesoproterozoic detrital zircons along the east- diagrams are well correlated with orogenic events in the Grenville

ern margin of the Siberian Craton, suggesting signiﬁcant changes Orogen of North America, which is considered as the most likely

to the provenance area. However, Mesoproterozoic detrital zircons provenance for detrital zircons in southeastern Siberia. The Nd iso-

have been found in the samples from Shein 1P Well, providing topic signature of many samples further supports derivation from

evidence that Mesoproterozoic detrital zircons were transported the Grenville Orogen as well. Paleocontinental restorations sug-

to the central part of the craton from the southwestern margin gested by Sears and Price (1978, 2003) and Rainbird et al. (1998)

(Yenisey Ridge), where older Neoproterozoic and Mesoproterozoic juxtapose the continuation of the Grenville Orogen to southeastern

rocks were eroded and reworked (Fig. 17). Siberia, but a separate Grenville-age continental terrane is required

In the northern area, sandstones from the Kharayutekh Forma- in order to supply sedimentary basins across southwestern Siberia

tion and the Lower Cambrian rock units contain numerous detrital with zircons of Grenville-age. The restoration by Pisarevsky and

zircons ranging in age from 790 to 590 Ma (Figs. 13 and 15). These Natapov (2003) include a hypothetical continental block between

ages correspond reasonably well with magmatic and metamor- Laurentia and Siberia, which may be a potential provenance for

phic events documented in the Central Taimyr accretionary belt Grenville-age zircons. However, no data on the composition of this

along Siberia’s northern margin (Vernikovsky and Vernikovskaya, hypothetical continent block is available.

2001; Vernikovsky et al., 2004). Moreover, the Sm–Nd isotopic sig- A comparison of detrital zircon ages and Nd isotopic data of the

nature of the Khast55 sample is very close to that of volcanic arc Yudoma Group samples suggest the occurrence of a maﬁc mag-

granites dated at ca. 750 Ma, suggesting that the Central Taimyr matic event which post-dates deposition of the Uy Group, as yet

accretionary belt was a likely provenance for Lower Cambrian sand- undocumented from the eastern Siberian Craton. In the northern

stones in the Khastakh 930 Well. However, the very immature lithic part of the Siberian Craton, detrital zircons from the Kharayutekh

composition of the sandstones provides evidence for a proximal Formation and Lower Cambrian sandstones, ranging in age from

provenance, and we therefore infer that the Central Taimyr accre- 790 to 590 Ma, have only been documented in the northern part of

tionary belt continued eastward beneath the present-day Laptev the study area. The most likely provenance for these zircons is ter-

Sea sedimentary basin. This provenance interpretation implies that ranes of the Central Taimyr accretionary belt, suggesting that these

the Central Taimyr terranes were accreted to the Siberian Craton terranes were accreted to the Siberian Craton but not to the Kara

(Vernikovsky and Vernikovskaya, 2001; Metelkin et al., 2012), but microcontinent during the Neoproterozoic.

not to the Kara microcontinent, which was located far away from

the Siberian Craton at this time (Proskurnin et al., 2014). An alter-

Acknowledgements

native interpretation is that ca. 790–590 Ma detrital zircons were

eroded from the southwestern margin of Siberia and surrounding

Study of A. Khudoley, V. Ershova and S. Malyshev were

terranes, where similarly aged magmatic rocks were documented

supported by St. Petersburg State University research grant

(e.g. Kuzmichev et al., 2001; Vernikovsky et al., 2004). However,

# 3.38.137.2014 and RFBR grant # 13-05-00943. V. Ershova

much of the Siberian cratonwas covered by a shallow marine basin

acknowledges Grant of President of Russia for Young Scientist MK-

during the latest Neoproterozoic (Vendian) and Early Cambrian,

2902.2013.5. Studies by K. Chamberlain, J. Sears and J. MacLean

with cycles of carbonate and evaporite deposition (e.g. Sukhov,

were funded by NSF grant # 0310186. Work by R. Veselovskiy was

1997; Melnikov et al., 2005). This paleogeographic setting would

supported by the Ministry of Education and Science of the Russian

make transportation of detrital zircons from the southwestern mar-

Federation (ordinance # 220, application # 2013-220-04-216). Lab-

gin of the Siberian Craton to its northern part rather difﬁcult.

oratory studies were partly supported by Shell, Cameco and Exxon.

The Nordsim ion microprobe facility operates as a Nordic infra-

structure regulated by The Joint Committee of the Nordic Research

5. Conclusion

Councils for Natural Sciences (NOS-N). This is Nordsim publica-

tion #384. Assistance of the Nordsim staff (Martin Whitehouse, Lev

The Mesoproterozoic to Lower Cambrian succession of eastern

Ilyinsky, Kerstin Lindén) is greatly appreciated. Comments by J. Bar-

Siberia contains many clastic rock units which document a long his-

net, S. Pisarevsky, N. Kuznetsov and anonymous reviewer improved

tory of successive tectonic and magmatic events in the surrounding

the manuscript.

areas. Twenty-nine samples for U–Pb detrital zircon dating and 27

samples for the whole-rock Sm–Nd isotopic study were collected.

In total, 1491 detrital zircon grains were dated and 1148 grains Appendix A. Supplementary data

were selected for the following provenance interpretation.

Amongst detrital zircons of Archean age, peaks at 2900–2850 Ma Supplementary data associated with this article can be found,

and 2750–2700 Ma are most widespread. Crystalline rocks of such in the online version, at http://dx.doi.org/10.1016/j.precamres.

ages are not typical of the presently exposed portions of the Siberian 2014.10.003.

Craton basement; therefore the detrital zircon data provides con-

straints on the ages of Siberian Craton basement rocks that are

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