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Precambrian Research 252 (2014) 209–222

Contents lists available at ScienceDirect

Precambrian Research

jo ur nal homep ag e: www.elsev ier .com/ locate /precamres

etrital zircon ages of Proterozoic meta-sedimentary rocks andaleozoic sedimentary cover of the northern Yili Block: Implicationsor the tectonics of microcontinents in the Central Asian Orogenic Belt

ongsheng Liua,b, Bo Wanga,b,c,∗, Liangshu Shua,b, Bor-ming Jahnc,d, Yoshiyuki Lizukac

State Key Laboratory for Mineral Deposits Research, School of Earth Sciences and Engineering, Nanjing University, 210046 Nanjing, ChinaCollaborative Innovation Center of Continental Tectonics, Northwest University, Xi’an, ChinaInstitute of Earth Sciences, Academia Sinica, 11529 TaipeiDepartment of Geosciences, National Taiwan University, 10617 Taipei

r t i c l e i n f o

rticle history:eceived 22 January 2014eceived in revised form 10 July 2014ccepted 26 July 2014vailable online 4 August 2014

eywords:etrital zircon U–Pb ageeta-sedimentary rocks

rovenancesianshanentral Asian Orogenic Belt

a b s t r a c t

The Central Asian Orogenic Belt (CAOB) is one of the largest accretionary orogens in the world. It wasformed mainly by amalgamation of island arcs, accretionary wedges and microcontinents. Revealing theorigins of the Precambrian continental blocks is essential for the understanding of the tectonic frameworkand geodynamic evolution of the CAOB. In this paper we present detrital zircon U–Pb ages of Precam-brian meta-sedimentary rocks and late Paleozoic undeformed sandstone from the northern Yili Block,Chinese North Tianshan, in order to better understand the regional tectonic evolution. Two mica-schistsamples from the Wenquan Metamorphic Complex (WMC) show similar zircon age distribution pat-terns with peaks at ∼0.43 Ga, ∼0.54 Ga, ∼0.65–0.68 Ga, ∼0.74–0.79 Ga, ∼0.89–0.92 Ga, ∼1.3–1.55 Ga and∼1.69–1.70 Ga, respectively. Minor age peaks of ∼1.1 and ∼2.2 Ga are also separately recognized in indi-vidual samples. A phyllite from the Mesoproterozoic Changcheng System yielded detrital zircon agesmainly ranging from 855 to ∼1500 Ma with a single peak at ∼906 Ma. According to the analysis of agedata and corresponding CL images of the dated zircon grains, protoliths of the mica-schists and phylliteshould have deposited later than 645 Ma and 850 Ma, respectively, and were subjected to medium- tolow-grade metamorphism during mid-late Silurian time. The good agreement between the age patternsof the meta-sediments and those of the nearby granitic and high-grade metamorphic rocks of the WMCindicates that the detrital zircon grains were mainly derived from the local metamorphic/crystallinebasement. Occurrence of much older zircons (∼1.0–2.2 Ga) in the mica-schists and absence of such zir-con populations in the phyllite suggest that (1) the protoliths of the mica-schists and phyllite had distinctsources and were deposited at different time, and (2) Mesoproterozoic to Paleoproterozoic rocks prob-ably existed in the northern Yili Block. Three undeformed sandstone samples yielded consistent singleage peak at ∼368–376 Ma and contain only a few Proterozoic detrital zircon grains. The peak age is inagreement with ages of neighboring late Paleozoic arc magmatic rocks in the Chinese North Tianshan.Thus, the sandstone was probably deposited during latest Devonian to earliest Carboniferous time in a

forearc or interarc basin, around which Proterozoic basement was not exposed or completely isolated. Acomparison between the zircon age patterns of the northern Yili Block and the surrounding cratons andmicrocontinents leads us to conclude that (1) the northern Yili Block had a Proterozoic basement similarto that of the Chinese Central Tianshan and Kyrgyz North Tianshan, and (2) these microcontinental blocksshare the same origin as the Tarim Craton, but are distinguished from the Siberian Craton.

© 2014 Elsevier B.V. All rights reserved.

∗ Corresponding author at: Xianlin Avenue 163#, Qixia District, Nanjing 210046,hina. Tel.: +86 25 89690862.

E-mail addresses: bwang@nju.edu.cn, burh cw@yahoo.com (B. Wang).

ttp://dx.doi.org/10.1016/j.precamres.2014.07.018301-9268/© 2014 Elsevier B.V. All rights reserved.

1. Introduction

Continental fragments are main constituents of accretion and

collisional orogenic belts. The origin and crustal evolution of thecontinental units play an important role in the understanding ofthe tectonics and geodynamic processes of orogenic belts. The Cen-tral Asian Orogenic Belt (CAOB; Fig. 1A; Jahn et al., 2000; Jahn,

210 H. Liu et al. / Precambrian Research 252 (2014) 209–222

Fig. 1. (A) The sketch map of Eastern Asian showing the tectonic position of the Central Asia (after Jahn, 2004). CAOB, Central Asian Orogenic Belt; EEC, East European Craton;K lt shoN lified

X

2iicrrsmstaNtpG2eol22eWelin

ZN, Kazakhstan. (B) Simplified geological map of the western Chinese Tianshan Beorth Tianshan Fault; MTSZ, Main Tianshan Shear Zone; NF, Nalati Fault. (C) SimpBGMR, 1988a, 1988b, 1993). The location of the sampling is shown with a star.

004) is a result of long-lasting accretion orogenic processes, andts formation have become one of the most attractive issues in thenternational geologic community. Numerous studies have beenonducted in the past decades, but many disputed issues stillemain and have hindered understanding of the paleogeographiceconstruction and tectonic evolution of the CAOB. The controver-ies mainly focus on three aspects: (1) accretion process and itsechanism, including two competitive models, of which one is a

ingle arc-trench system with continuous subduction and accre-ion of oceanic components (including oceanic plateaus, islandrcs, seamounts and ophiolites) (Sengör et al., 1993; Sengör andatal’in, 1996), and the other is an archipelago model with mul-

iple arc/back-arc basin systems and different oceanic subductionolarities and ages (Mossakovsky et al., 1993; Windley et al., 2007;eng et al., 2009, 2011; Jiang et al., 2010, 2012; Levashova et al.,009; Long et al., 2010a; Glorie et al., 2011; Yuan et al., 2011; Xiaot al., 2010, 2013; Eizenhöfer et al., 2014); (2) time-space patternsf accretion orogeny, namely, the timing of the collision and theocations of suture zones (e.g., Gao et al., 1998, 2009; Shu et al.,002, 2004, 2011; Xiao et al., 2004, 2008, 2013; Wang et al., 2008,011a; Cai et al., 2010, 2011a, 2011b, 2012a, 2012b, 2014; Charvett al., 2011; Han et al., 2010; Hegner et al., 2010; Yin et al., 2010;ang et al., 2011d; Zhang et al., 2011a; Kröner et al., 2012; Wilhem

t al., 2012; Choulet et al., 2012, 2013); and (3) the nature and evo-ution of the continental blocks with Precambrian basement, thats, whether continental blocks belong to independent microconti-ents (Allen et al., 1993; Windley et al., 2007) or where continental

wing the distribution of Proterozoic rocks (Modified from Wang et al., 2009). NTF,geological map of the Salimu area, northern part of the Yili Block (modified from

fragments separated from and re-amalgmated with various cra-tonic plates (Sengör and Natal’in, 1996; Kheraskova et al., 2003;Turkina et al., 2007; Shu et al., 2002, 2004, 2013; Zhou et al., 2010;Charvet et al., 2007, 2011; Wang et al., 2008, 2011a; Levashova et al.,2011)?

Recently, an increasing amount of geochronological, geochemi-cal and isotopic data have been published to constrain the Paleozoicaccretion and amalgamation tectonics of the CAOB, but studies onthe nature and evolution of the continental basements within theCAOB are relatively minor (Hu et al., 2006, 2010; Kröner et al., 2007,2013; Chen et al., 2009, 2012; Sun et al., 2009; Wang et al., 2014). Onthe basis of U–Pb ages and Hf isotopic compositions of detrital zir-con grains from the late Paleozoic sedimentary rocks, some authorsrecognized evidence of contamination or reworking of Precam-brian crust during the Paleozoic magmatism that occurred duringthe building of the CAOB (Rojas-Agramonte et al., 2011, 2013; Maet al., 2012a, 2012b). However, the limited and discrete outcrops ofPrecambrian rocks cannot afford comprehensive cognition of thecontinental blocks and their correlation with sources of detritalzircon grains in Paleozoic sediments.

In the past few years, our research group has carried out exten-sive investigations on the Wenquan Metamorphic Complex (WMC;Wang et al., 2011b, 2012, 2014) that is located in the north-

ern Yili Block, Chinese North Tianshan (Fig. 1B and C). The WMCis composed mainly of high-grade metamorphic rocks and low-grade meta-sedimentary rocks that were previously assigned tothe Paleo- to Mesoproterozoic basement rocks (XBGMR, 1993).

Resea

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H. Liu et al. / Precambrian

he WMC extends westward into the central Kazakhstan oroclineWindley et al., 2007; Alexeiev et al., 2011) being one of the majorontinental components of the CAOB. Thus, a detailed study ofhese metamorphic rocks is essential for understanding the forma-ion and evolution of the crustal basement of the Yili-Kazakhstanontinental assemblage.

Studies of detrital zircons have become a powerful tool torace the provenances of sedimentary rocks (e.g., Sircombe, 1999;awood et al., 2003). In the past decades, the zircon U–Pb ages ofhe Siberian Craton, Tarim Craton and the microcontinents withinhe CAOB (such as Altai, Mongolia, Chinese Central Tianshan, Kyr-yz North and Middle Tianshan) have been extensively determinedSun et al., 2008; Jiang et al., 2011; Lei et al., 2011; Long et al.,011a, 2011b, 2011c; Ma et al., 2012a, 2012b; Rojas-Agramontet al., 2011, 2013; Kröner et al., 2013). In this paper, we presentetrital zircon ages for the meta-sedimentary rocks from the north-rn Yili Block, and attempt to draw implications for the nature andectonics of the continental blocks in SW of the CAOB. In addition,etrital zircons from the Paleozoic sedimentary cover were dated

n order to examine the paleogeographic situation of the study areauring mid-Paleozoic time.

. Geological background

The Central Asia Orogenic Belt (also called Altaids by Sengört al., 1993) is confined by the Eastern European Craton (EEC) to theest, the Pacific Ocean to the east, the Tarim-North China blocks to

he south and the Siberian Craton to the north (Fig. 1A). The Siberianraton was aggregated by several Archean terranes during Paleo-roterozoic (∼1.8–2.1 Ga) and became relatively stable since theesoproterozoic time (Rosen, 2002; Gladkochub et al., 2006 and

eferences therein). The Tarim Block is a continental block with aeoarchean to Paleoproterozoic metamorphic and crystalline base-ent, and it had been active in most of the Neoproterozoic to early

aleozoic time (Hu et al., 2000; Zhao et al., 2002; Guo and Zhang,003; Guo et al., 2005; Zhang et al., 2007; Lu et al., 2008; Long et al.,010b, 2011b, 2011c; Shu et al., 2011; Xu et al., 2013; Lei et al., 2012;hao and Cawood, 2012; Ge et al., 2013).

The CAOB is a typical accretionary orogen formed by progres-ive amalgamation of microcontinents, island arcs, seamounts, andccretionary complex during late Neoproterozoic to late PaleozoicMossakovsky et al., 1993; Sengör and Natal’in, 1996; Kheraskovat al., 2003; Degtyarev and Ryazantsev, 2007; Kröner et al., 2007;indley et al., 2007; Xiao et al., 2004, 2008, 2010; Wong et al.,

010; Yuan et al., 2010). The Kazakhstan microcontinent, Altai-ongolia Range and Tianshan Belt are major constituents located in

he southwest of this vast orogenic collage (Fig. 1A). The Kazakhstanicrocontinent consists of several sub-units with Precambrian

asement unconformably overlain by Paleozoic sequences. Thesenits, separated from each other by early Paleozoic volcanic arcsnd/or accretionary belts (Windley et al., 2007; Biske and Seltmann,010; Alexeiev et al., 2011; Kröner et al., 2012) include three Pre-ambrian blocks named Kokchetav – Kyrgyz North Tianshan, Ishim

Kyrgyz Middle Tianshan, and Aktau-Chinese North TianshanAlexeiev et al., 2011; Wang et al., 2011b, 2012, 2014). The Pre-ambrian basement within the Kyrgyz North Tianshan belt consistsainly of granitic gneisses with ages ranging from Neoproterozoic

o Archean (Kröner et al., 2007, 2013 and references therein). Theyrgyz Middle Tianshan unit is dominated by Paleozoic carbonatelatform deposits, fine-grained marine sediments and a supposednderlying Proterozoic basement (Degtyarev, 2003; Alexeiev et al.,

011; Rojas-Agramonte et al., 2013).

The Aktau-Chinese North Tianshan unit extends eastward fromhe center of the Kazakhstan orocline to the northern part of theili Block (Alexeiev et al., 2011; Wang et al., 2012, 2014) which

rch 252 (2014) 209–222 211

is actually a triangular area and bordered by two late Paleozoicsuture zones named as the North Tianshan Suture to the Northand the Central Tianshan Suture to the South, respectively (Wanget al., 2008, 2011a; Charvet et al., 2011). Both suture zones werereworked by Permian post-orogenic wrench faults, namely, theNorth Tianshan Fault (NTF) and the Nalati Fault (NF) (Fig. 1B; Wanget al., 2008, 2009). The northern part of the Yili Block is mainly occu-pied by Borohoro Range, where widely outcropped late Paleozoicmagmatic and sedimentary rocks formed in an active continentalmargin setting (e.g., Gao et al., 1998; Wang et al., 2006, 2007, 2009;Han et al., 2010).

The Precambrian crystalline and metamorphic basement of theYili Block occurs mainly along its northern and southern bound-aries (Fig. 1B). The Wenquan Metamorphic Complex (WMC) isone of the major exposures of basement rocks developing at thenorthern margin of the Yili Block (Fig. 1B and C). The WMC was pre-viously considered to be Paleoproterozoic in age (XBGMR, 1988a,1988b) but is recently subdivided into pre-Neoproterozoic, Neo-proterozoic and early Paleozoic subunits on the basis of newlypublished geochronological data (Fig. 2; Hu et al., 2006, 2010;Wang et al., 2011b, 2012, 2014; Li et al., 2013; Huang et al., 2013).The pre-Neoproterozoic subunit is composed of medium to high-grade meta-volcanic and meta-sedimentary rocks, but ages of theirprotoliths remain uncertain although Mesoproterozoic Nd modelages were obtained (Hu et al., 2000, 2006). Neoproterozoic subunitincludes gneissic granite and migmatite; both were formed by par-tial melting of supracrustal rocks (Hu et al., 2006, 2010; Wang et al.,2014). Early Paleozoic subunit consists of arc-type intermediate tomafic intrusive rocks (Hu et al., 2008; Wang et al., 2012; Huang et al.,2013). The WMC was tectonically overprinted in the late Siluriandue to early Paleozoic accretionary orogeny (Wang et al., 2011b).

3. Sedimentary sequences and sampling

The sedimentary sequences in the Wenquan area can be rec-ognized as three lithotectonic units (Figs. 1C and 2). Unit one (I)is mainly represented by Precambrian meta-sedimentary rocksincluding mica-schist and paragneiss with lenses of marble (Fig. 2);the meta-sedimentary rocks are associated with mafic and felsicmeta-volcanic rocks (amphibolite and quartzite, respectively). Theboundary between rock types is generally parallel to the folia-tion. Occasionally, intrusive contact can be observed between themeta-sedimentary rocks and the Neoproterozoic gneissic S-typegranite and migmatitic dikes (Fig. 2; Wang et al., 2014). How-ever, ambiguous or tectonic contact is commonly observed. TheUnit I can be further subdivided into two subunits based on thedifferent grades of metamorphism, namely, a relatively higher-grade subunit (I-1) that is closely associated with migmatite, anda lower-grade subunit (I-2) free from migmatization (Fig. 2). Agesof protoliths of the meta-sedimentary rocks were previously con-sidered as Paleoproterozoic (constituents of the Wenquan Group)according to regional comparison of rock facies (XBGMR, 1993) oras Mesoproterozoic on the basis of whole-rock Nd model ages (Huet al., 2006). Deformation fabrics (such as mylonitic foliation andstretching/mineral lineation) are well preserved in the paragneiss,quartzite and mica-schist (Figs. 3A and 4). The fabrics might havebeen produced during the early Paleozoic accretionary orogeny ortectonic overprint (Wang et al., 2011b).

Unit II is composed of low-grade meta-sedimentary rocks,including slate, phyllite and crystalline limestone (Fig. 2). This unitis separated by a reverse fault from the tectonically overlying Wen-

quan Group (Fig. 1C). The meta-pelitic rocks and carbonate werepreviously assigned to the Mesoproterozoic Changcheng System(XBGMR, 1993), but their precise deposition age remains undated.The slaty cleavage in the meta-pelites is steeply south-dipping, and

212 H. Liu et al. / Precambrian Research 252 (2014) 209–222

F an arc the la

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ig. 2. Column diagram of the metamorphic and sedimentary rocks in the Wenquoordinate of the relative probability diagrams is not in a uniform scale considering

as refolded by a north-verging thrusting (Fig. 3B and C) that isrobably related to late Paleozoic accretionary tectonics of the Chi-ese North Tianshan (Wang et al., 2006, 2011b). Unit III is madef upper Paleozoic limestone, sandstone and conglomerate. Thesendeformed and non-metamorphic rocks overly unconformablypon the meta-pelitic rocks of the Unit II (Figs. 1C, 2 and 3C and D),

nd intruded by late Paleozoic high-K granitic plutons (Fig. 1C).

Two mica-schist samples (W33 and W52) were collected fromubunit I-2 of the Wenquan Metamorphic Complex (Figs. 1C and 2).n these rocks, flat muscovite grains and elongated quartz and

ea, northern Yili Block and compilations of the detrital zircon ages. Note that therge difference of data numbers for different samples.

feldspar ribbons align consistently to show a preferred orientationthat forms the major foliation and lineation (Figs. 3A and 4). Onephyllite (07-4b) was sampled from the low-grade metamorphicsedimentary unit (II) of the Changcheng System (Figs. 1C, 2 and 3D).Three additional samples (07-3c, 07-3d and 07-3e) were taken fromthe upper Paleozoic sedimentary cover (Unit III) (Figs. 1C, 2 and 3D),

therein, two samples (07-3c and 3d) are fine-grained sand-stone, and the other one (07-3e) is coarse-grained sandstone(greywacke). The detailed sample descriptions are presentedin Table 1.

H. Liu et al. / Precambrian Research 252 (2014) 209–222 213

Fig. 3. Field photographs of the meta-sedimentary rocks and overlying undeformed sedimentary cover in the northern Yili Block. (A) mica-schist of the Wenquan Group withs hangcL able cs

4

zmmta

TD

teep foliation and shallow lineation, (B) re-folded slaty cleavage in phyllite of the Cate Devonian-early Carboniferous conglomerate, and (D) overview of unconformampling.

. Analytical procedures

The samples were crushed and milled into powders, from whichircon grains were separated using conventional heavy liquid and

agnetic techniques and then by handpicking under binocularicroscope. Subsequently, selected zircon grains free from frac-

ure and inclusion were mounted in epoxy resin, then polishednd coated with gold. Cathodoluminescence (CL) images of the

able 1etailed sampling information, brief descriptions and summary of dating results for the s

Sample Coordinates Rock Brief description

W33 N44◦53′58′′

E80◦34′59′′Mica-schist Foliation: 300◦∠80◦

Mineral or stretching line270◦∠25◦

W52 N44◦53′55′′

E80◦38′17′′Mica-schist Foliation: 355◦∠70◦

Sub-horizontal lineation07-4b N44◦52′42′′

E80◦41′43′′Phyllite Slaty cleavage re-folded

07-3c N44◦52′15′′

E80◦40′10′′Fine-grainedsandstone

Undeformed and unconfooverlying on the phyllite

07-3d Idem Fine-grainedquartzsandstone

Undeformed

07-3e Idem Coarse-grainedsandstone

Undeformed, coarse-grain

heng System, (C) unconformable contact between schistose phyllite and overlyingontact between the phyllite and undeformed sandstone showing the locations of

zircon grains were obtained using a JSM-6360LV thermal emis-sion (W-filament) low-vacuum type scanning electron microscopeequipped with Gatan mini-CL detector at the EPMA Lab of the Insti-tute of Earth Sciences, Academia Sinica (Taipei).

The U–Pb isotopic ratios of representative zircon grains wereanalyzed at the State Key Laboratory for Mineral Deposits Researchat Nanjing University using Agilent 7500a ICP-MS coupled to aNew Wave 193 nm laser ablation system with an in-house sample

edimentary rocks, northern Yili Block.

Age range (Ma)

ation:Similar age spectra, age populations at: 410–430 Ma,540 Ma, 650–680 Ma, 740–790 Ma, 890–920 Ma,1.3–1.55 Ga, and 1.69–1.7 Ga

Age peaks at 906 Ma

rmably Age peak: 376 Ma

Age peak: 369 Ma

ed texture 368.9 ± 2.7 Ma

214 H. Liu et al. / Precambrian Resea

Fig. 4. Microscopic photographs of mica-schists from the Wenquan MetamorphicCgt

cdcaa(sscC1ab2

rpwac

5

5

sc

omplex showing obvious orientation of flat mica and elongated quartz and feldsparrains (A, B), and visible recrystallization of quartz crystals (B) indicating mediumo high temperature ductile deformation.

ell. The details of the analytical procedures are similar with thatescribed by Jackson et al. (2004). The U–Pb fractionation wasorrected using zircon standard GEMOC GJ-1 with a 207Pb/206Pbge of 601 ± 12 Ma, and analytical accuracy was controlled usingnother zircon standard Mud Tank with an age of 735 ± 12 MaBlack and Gulson, 1978). The U–Pb ages were calculated with theoftware Glitter. Since 204Pb could not be measured due to lowignal and interference from 204Hg in the gas supply, common leadorrection was carried out using the Excel® embedded programomPbCorr#3 (Andersen, 2002). For zircon crystals older than000 Ma, 207Pb/206Pb apparent ages are better considering largemounts of radiogenic Pb, and thus used to plot relative proba-ility diagrams; whereas for zircon grains younger than 1000 Ma,06Pb/238U apparent ages are more reliable due to low content ofadiogenic Pb and low uncertainty of common Pb correction. Therogram ISOPLOT 3.1 (Ludwig, 2001) added-in for Microsoft Excel®

as used for age calculation and Concordia plotting. Uncertaintiesre quoted at 1� for individual analyses and at 2� (with 95%onfidence level) for weighted mean ages, respectively.

. Zircon U–Pb LA-ICP-MS analytical results

.1. Mica-schists from the Wenquan Metamorphic Complex

A total of 54 and 84 zircon grains were dated for mica-schistamples W33 and W52, respectively (Table S1; Fig. 5). Most zir-on crystals are sub-rounded to sub-euhedral, with length/wide

rch 252 (2014) 209–222

ratios of 1–2. CL images show that the majority of zircon crystalshave core-mantle (or rim) structure in which the cores are generallybright with or without magmatic oscillatory zoning, and the rimsare usually darker showing no oscillatory zoning (Fig. 5A and B).Subordinate amount of grains show homogeneous dark to black CLimages without oscillatory zoning. On the 207Pb/235U vs. 206Pb/238Udiagrams (Fig. 5C and E), most analyses plot on or close to the Con-cordia, but some zircons of the sample W33 show significantly highapparent age errors (Fig. 5C; Table S1).

On the basis of detailed analysis of inner texture and ana-lytical isotopic ratios, four types of zircons can be recognized,namely, (1) zircons with concordant apparent ages and low ageerrors, (2) zircons with highly discordant apparent ages and vari-able age errors, (3) zircons with extremely high 207Pb/206Pb (andoccasionally 207Pb/235U) age errors (>10%) and usually also dis-cordant apparent ages, (4) zircons with slightly high 207Pb/206Pbage errors only and concordant 207Pb/235U and 206Pb/238Pb appar-ent ages (Table S1). The analytical results of the second and thirdtype zircons are geologically meaningless, and thus were not con-sidered in the discussion of provenances and relative probabilityplots. Whereas, the data of the fourth type of zircons, althoughwith slightly high 207Pb/206Pb age errors, their 207Pb/206Pb appar-ent ages are generally consistent with 207Pb/235U and 206Pb/238Uapparent ages when they are older than 1000 Ma, or alternatively,their 207Pb/235U and 206Pb/238U apparent ages are quite consistentwhen the ages are younger than 1000 Ma (Table S1). Thus, theseanalyses were used together with the data of the first type of zir-cons to plot relative probability diagrams, and further included inthe provenance discussion.

Consequently, 37 out of 54 zircon ages of the sample W33 wereselected to plot a relative probability diagram (Fig. 5D), whichshows multiple age peaks at ∼0.65, ∼0.74, ∼0.92, ∼1.46–1.55, 1.7and ∼2.22 Ga. In addition, minor age peaks at ∼0.43, ∼0.54, 1.1,∼1.25 and ∼1.9 Ga are also visible (Fig. 5D). In the sample W52, 77out of 84 zircon grains yielded reliable data, and the relative prob-ability diagram defines several age peaks at ∼0.43, ∼0.55, ∼0.69,∼0.79, 0.89, 1.11, 1.3–1.5 and 1.69 Ga (Fig. 5F).

5.2. Low-grade meta-pelite of the Changcheng System

Sixty-five zircon grains from meta-pelite sample (07-4b) wereanalyzed. The dated zircon grains are generally prismatic andsub-euhedral. CL images of most grains are quite dark, and theoscillatory zoning is generally visible but is often affected by vari-able surface- and/or zoning-controlled alteration similar to thatdescribed by Vavra et al. (1996). Overgrowth rim can occasion-ally be observed in a few zircon grains (Fig. 6A, spot No. 11). Mostanalyses plot on or close to the Concordia, but many others are dis-cordant showing relative young 206Pb/238U apparent ages and quiteold 207Pb/206Pb ages (Table S1; Fig. 6B), and are therefore geolog-ically meaningless. Thus, 33 out of 65 analyses were used to plota relative probability diagram that shows a predominant age peakat 906 Ma and a minor peak at 965 Ma (Fig. 7C). In addition, twoMesoproterozoic zircon grains (∼1.15 and ∼1.5 Ga) are also foundin this sample.

5.3. Undeformed upper Paleozoic sandstones

From the upper Paleozoic sedimentary sequence (Unit IIIin Fig. 2), a total of 20 grains were analyzed for the coarse-grained sandstone (07-3e), and 18 out of 20 analyses yieldedconcordant and consistent apparent ages, therefore a mean age

of 368.9 ± 2.7 Ma (MSWD = 1.12) is calculated (Fig. 7A). Remainingtwo zircon grains (Nos. 7 and 17 in Table S1) yielded discordantapparent ages probably due to high common Pb (No. 7 cannot beplotted on Fig. 7A). The CL images of the dated zircon grains show

H. Liu et al. / Precambrian Research 252 (2014) 209–222 215

Fig. 5. Representative CL images (A, B), Concordia diagrams (C, E) and relative probability plots (D, F) of the detrail zircon U–Pb ages for the mica-schist samples W33 andW

br

pa

52 from the Wenquan Metamorphic Complex, northern Yili Block.

right concentric oscillatory zoning without obvious overgrown

im (Fig. 7B), and only few zircon grains have core-rim structure.

Two fine-grained sandstones (07-3c, 3d) contain plenty ofrismatic and euhedral zircon grains, which show bright CL imagesnd dense concentric oscillatory zonings (Fig. 7B) indicating a

felsic magmatic origin according to Corfu et al. (2003). Inherited

cores can be occasionally observed, but secondary overgrownrim is absent (Fig. 7B). The zircon U–Pb analytical results of thesetwo samples plot mostly on or close to the Concordia (Fig. 7Cand E), and the corresponding apparent ages were used to plot

216 H. Liu et al. / Precambrian Resea

Fig. 6. Representative CL images (A), Concordia diagram (B) and relative probabilityplot (C) of the detrail zircon U–Pb ages for the phyllite from the Changcheng System,northern Yili Block.

rsacfas1z

degrees over the pre-existing zircon grains, or resulted from mix-ture between overgrown rims and old cores, but are not likely torepresent ages of pre-depositional detrital zircons with metamor-

elative probability diagrams (Fig. 7D and F). The age spectra of twoamples are quite similar with consistent age peaks at ∼370 Mand minor peaks at ∼400 Ma. The major peak age (∼370 Ma) isonsistent with the mean age (369 Ma) of the detrital zirconsrom the coarse-grained sandstone (sample 07-3e). In addition,bout dozen analyses on the inherited cores (Fig. 7B) of eachample yielded older ages of ∼450 Ma, 650–700 Ma, 900–1100 Ma,300–1400 Ma, ∼1500 Ma, 1700–1800 Ma and one Neoarchean

ircon grain at 2.6 Ga (Fig. 7D and F).

rch 252 (2014) 209–222

6. Discussion

6.1. Significances of the detrital zircon U–Pb ages and constraintsto the depositional timing of protoliths of the meta-sedimentaryrocks

The high-grade metamorphic rocks of the Wenquan Metamor-phic Complex (WMC) were previously considered to be Paleopro-terozoic in age and to represent the basement of the Yili Block(XBGMR, 1988a, 1993; Hu et al., 2006). The low-grade meta-peliticrocks (phyllite) are assigned to the Changcheng System (1.8–1.4 Ga)according to the published geological map (XBGMR, 1988a). How-ever, recent studies suggest that orthogneiss and migmatite fromthe WMC formed in Neoproterozoic instead of Paleoproterozoic(Hu et al., 2010; Li et al., 2013; Wang et al., 2014), and were sub-jected to deformation and metamorphism during mid-late Silurian(Wang et al., 2011b). The ages of the meta-sedimentary rocks werepoorly constrained although they were assigned to the Paleopro-terozoic Wenquan Group (XBGMR, 1993). Our new detrital zirconU–Pb ages will provide the first constraints on the deposition agesof the protoliths of these meta-sedimentary rocks.

On the basis of a comprehensive analysis on the CL images andthe corresponding U–Pb analytical results of the detrital zircongrains from the two mica-schist samples (Table S1; Fig. 5), substan-tial amount of age data were obtained from zircons with relativelysmall sizes and showing obvious core-mantle (rim) textures andvariable degrees of alteration. Some ages are highly discordant orwith large age errors, which could be due to either common Pb orPb loss induced during metamorphism or metasomatism relatedto fluid-thermal activities, or could also be the result of significantmixture of dating different parts (core and rim) of zircon grains withdistinct origins. Thus, these unreliable data are geologically mean-ingless, and only concordant ages with relatively low age errors areconsidered to discuss their significances.

The oldest ages of ∼2.2–2.6 Ga and some Mesoproterozoicages of ∼1.4 Ga were obtained from zircon grains with dark andhomogenous CL images without oscillatory zoning, and were alsofrom the homogenous and bright cores of the zircon grains withdarker rims. These ages are probably indicative of Paleoprotero-zoic to Neoarchean and early Mesoproterozoic metamorphism.Many other Mesoproterozoic ages were obtained from inheritedcores of the zircon grains, whose CL images show typical magmaticoscillatory zoning or bright homogenous texture, suggesting thatthe cores of these zircon grains were formed during contempo-raneous magmatic and metamorphic events occurred in ∼1.7 and∼1.35–1.55 Ga. The latest Mesoproterozoic to Neoproterozoic ages(∼1.1, ∼0.92–0.89, 0.78–0.74 and ∼0.69–0.65 Ga) were obtainedfrom magmatic cores of zircon grains, indicating multi-staged mag-matic events of source areas.

All the Paleozoic ages (∼545–410 Ma) were obtained eitherfrom the dark rims of zircon grains, or from the zircons withhomogenously dark CL images, which are similar to the Proterozoicmetamorphic zircons. However, considering (1) obvious metamor-phic and deformation characteristics of the mica-schists (Fig. 4),and (2) common youngest peak ages of ∼430 Ma (Fig. 5D and F)from both mica-schist samples are consistent with the ages ofmetamorphism and cooling of the Wenquan Metamorphic Com-plex (mica Ar–Ar ages at 430–410 Ma; Wang et al., 2011b), itis reasonable to propose that a substantial amount of detritalzircons in these meta-sedimentary rocks were subjected to post-depositional metasomatism or alteration. Thus, the Paleozoic agesare most likely the result of metamorphic overprint with variable

phic origins.

H. Liu et al. / Precambrian Research 252 (2014) 209–222 217

F robabC

oct(s2lsS(

mw

ig. 7. Concordia diagrams (A, C and E), representative CL images (B) and relative parboniferous undeformed sandstones, northern Yili Block.

Consequently, the youngest detrital zircon grains of magmaticrigin in two mica-schist samples are of 780–650 Ma, which mayonstrain the maximum deposition age (<650 Ma) of the pro-oliths of the mica-schists. In addition, Middle to Late Ordovician447–466 Ma) arc-type magmatic rocks intruded in these meta-edimentary rocks (Hu et al., 2008; Wang et al., 2012; Huang et al.,013), and both were deformed and/or metamorphosed during

ate Silurian (430–410 Ma; Wang et al., 2011b). Hence, the depo-ition of the protoliths of the mica-schists must be earlier than lateilurian (>410 Ma) or is even likely earlier than Middle Ordovician

>470 Ma).

The low-grade meta-pelite (phyllite sample 07-4b) containsainly Neoproterozoic zircon ages, ranging from 990 to 840 Ma,ith a major age peak at 906 Ma (Fig. 6). The CL images of these

ility plots (D, F) of the dated detrital zircon grains from the Late Devonian to early

zircon grains generally show visible concentric or striped oscilla-tory zonings (Fig. 6A) which are similar to the zircon grains of felsicand mafic magmatic origins, respectively (Corfu et al., 2003). Onlyfew zircon grains show bright cores with oscillatory zoning sur-rounded by dark overgrown rims, and two Mesoproterozoic ages(∼1.15 and ∼1.5 Ga) were obtained from this kind of cores indicat-ing recycling of old magmatic zircon grains. The pelitic sample wasmetamorphosed under the lower green-schist facies condition dur-ing late Silurian (Wang et al., 2011b), and some zircon grains werevariously affected to yield discordant ages (Fig. 6B; Table S1). Even

though, many other analyses are generally concordant, and theyoungest concordant detrital zircon grains (∼850 Ma) with mag-matic origin can thus be used to constrain the maximum depositionage of the protolith (pelitic rock) of the phyllite. According to similar

2 Research 252 (2014) 209–222

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3ciozaasrslstal1

6No

mid(astlam2ad

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Fig. 8. Compilations of zircon U–Pb ages from the northern Yili Block and the neigh-boring tectonic units. Age data of the northern Yili Block (A) are from this study(Table S1) and those published in Hu et al. (2006, 2008, 2010), Wang et al. (2012,2014), Li et al. (2013) and Huang et al. (2013). Age data combined from igneous,detrital and metamorphic zircon grains from the Central Chinese Tianshan (Yanget al., 2006; Chen et al., 2009; Li et al., 2011; Wang et al., 2011c; Lin et al., 2011; Leiet al., 2011; He et al., 2012; Chen et al., 2012; Ma et al., 2012a, 2012b, 2013), andfrom the Tarim Block (Wu et al., 2009; Zhang et al., 2011b, 2012; Shu et al., 2011;Cao et al., 2011; Xu et al., 2013) are listed in Supplementary Table S2, and plottedin (B) and (C), respectively. Data from the Kyrgyz North Tianshan (Rojas-Agramonte

18 H. Liu et al. / Precambrian

easoning mentioned above for the mica-schists, the pelitic rockhould have deposited earlier than 430 Ma but later than 850 Manstead of in Mesoproterozoic as previously considered.

In addition, the mica-schists and phyllite have similar Neo-roterozoic magmatic zircon populations (915, 890 and 906 Ma);owever, the phyllite shows a distinct age spectrum from those ofhe mica-schists, i.e., it has no Paleozoic nor Meso-Paleoproterozoicetrital zircons (Figs. 2, 5 and 6). The absence of Paleozoic ages

s probably due to relatively weak deformation and low-gradeetamorphism that did not sufficiently reset the U–Pb isotopic

ystems of the zircon grains in the phyllite. The lacking of Meso-aleoproterozoic detrital zircon grains indicates that the protolithf the phyllite had not such sources, obviously different from thosef the protoliths of the mica-schists. This difference may be inter-reted as a result of synchronous sedimentation in distinguishedepositional environments, or can be explained by progressivehange of sedimentary facies with reducing input of older andeep-seated materials. Considering the proximity of the sampling

ocations of the mica-schists and phyllite, it is more reasonable toropose that the protoliths of the mica-schists and phyllite wereormed at different time and in distinct sedimentary environmentso that their source compositions are different.

The undeformed and non-metamorphic sandstone samples (07-c, d, and e) from the upper Paleozoic sedimentary cover show aommon single age peak at ∼370 Ma (Figs. 2, 7D and F). The CLmages reveal that the euhedral zircon grains have fine and brightscillatory zoning without overgrown rim, indicating that theseircon grains are of magmatic origin and free of secondary alter-tion during diagenesis and later tectonics. A couple of youngerpparent ages of <300 Ma were yielded from two fine-grained sand-tone samples (Table S1), but all are discordant, thus they may notepresent additional young sources. Therefore, the maximum depo-itional age of these sandstones should be later than ∼368 Ma, i.e.,atest Devonian to early Carboniferous. This interpretation is con-istent with the previous age constraint (Lower Carboniferous) forhese undeformed sandstones on the basis of regional comparisonnd occurrence of plant fossils such as Archaeocalamites Scrobicu-atus (Schlotheim) Seward, and coral Neoclisiophyllum sp. (XBGMR,988a).

.2. Changing provenances in northern Yili Block through lateeoproterozoic to late Paleozoic and implications for the tectonicsf continental blocks in SW CAOB

As discussed above, the mica-schists from the Wenquan Meta-orphic Complex (WMC) and phyllite of the Changcheng System

n the northern part of the Yili Block were originally depositeduring late Neoproterozoic (<850–650 Ma) to early Paleozoic>430–410 Ma), instead of previously proposed Paleoproterozoicnd Mesoproterozoic, respectively (XBGMR, 1993). Among theources of the mica-schists (W33 and W52) and phyllite (07-4b),he Neoproterozoic detrital zircon grains display magmatic oscil-atory zoning on the CL images, and their ages (∼950–840 Ma)re comparable with those of the gneissic granite and associatedigmatite within the WMC (930–845 Ma; Hu et al., 2010; Li et al.,

013; Wang et al., 2014). Thus, the gneissic granite and migmatitere most likely the proximal provenances of the Neoproterozoicetrital zircon grains in these meta-sedimentary rocks.

The mica-schists also contain substantial zircon grains of Meso-o Paleoproterozoic ages. One possibility is that all these zirconrains are inheritances within the Neoproterozoic zircons since theeoproterozoic magmatic zircon grains include older cores dated

s Meso-Paleoproterozoic in age (Hu et al., 2010; Wang et al., 2014).f this is true, the phyllite that contains similar Neoproterozoicetrital zircons should also have Meso- to Paleoproterozoic zir-on compositions, but our data indicate that the phyllite is almost

et al., 2013 and references therein) and South Siberian Cratons (Rojas-Agramonteet al., 2011 and references therein) are plotted in (D) and (E), respectively.

free of these older zircons. Therefore, the Meso- and Paleoprotero-zoic zircon grains in the mica-schists could represent additionalsources that were only available during the sedimentation of theprotoliths of the mica-schists. These sources were probably erodedfrom the underlain basement rocks of the northern Yili Block,or alternatively derived from remote provenances through long-distance transportation. The first case is supported by occurrenceof Mesoproterozoic gneissic granites (1.4–1.3 Ga) within the WMC(Hu et al., 2006; A. Kröner, personal communication) and Nd modelages (1.7–2.1 Ga) of the high-grade metamorphic rocks in the WMCindicating the reworking of older crustal rocks (Hu et al., 2000,2010; Wang et al., 2014). In the second case, the Central ChineseTianshan, Kyrgyz North Tianshan and the Tarim Block are proba-ble source areas of the mica-schists since these tectonic units areclose to the northern Yili Block and also have records of Meso- andPaleoproterozoic magmatic and/or metamorphic zircons (Fig. 8; Huet al., 2000, 2006; Shi et al., 2010; Shu et al., 2011; Long et al., 2011b,2011c; Ma et al., 2012a, 2012b; Kröner et al., 2013). However, thenorthern Yili Block was probably separated from above-mentionedtectonic units during the Neoproterozoic (∼780–660 Ma) as provedby rifting-related magmatism (Lu et al., 2008). Thus, remote prove-nances are unlikely, and an in situ older basement is more favorablealthough further study is in need to test the existence of the under-

lain basement rocks, which are poorly exposed in the study area.

The undeformed Late Devonian to early Carboniferous sand-stones comprise a unique zircon population of ∼360–400 Ma in age,

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mea∼mt∼acpdnMmit

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H. Liu et al. / Precambrian

nd only minor Precambrian ages were obtained from the inheritedores that are occasionally observed in the fine-grained sandstoneamples (07-3c, d; Fig. 7B–F), suggesting a recycling of old materialsnto Late Devonian magmatic zircon grains instead of direct Pre-ambrian sources. According to available geological map (XBGMR,988a; Fig. 1) and the previous studies, late Paleozoic plutonic andolcanic rocks occur in the northern Yili Block, and these magmaticocks were mostly formed during 354–380 Ma in an active con-inental margin setting (Zhai et al., 2006; Wang et al., 2006, 2009;ong et al., 2010; Bai et al., 2011; Li et al., 2012). Thus, these arc-typeagmatic rocks in northern margin of the Yili Block could be the

ource of the detrital zircon grains in the undeformed sandstones.onsidering the unique characteristics of a single source (especiallyhe coarse-grained sandstone 07-3e; Table S1; Fig. 7A), it is possi-le that these sandstones were deposited in a sedimentary basinery close to the late Paleozoic North Tianshan magmatic arc (e.g.,

forearc or interarc basin), where the in situ Precambrian basemente.g., Neoproterozoic magmatic and metamorphic rocks) of the Yililock was not or rarely exposed, or alternatively, the exposed base-ent in adjacent areas might have been completely isolated from

he sedimentary basin. In order to test this interpretation, furtheredimentological and geochemical studies are in need to determinehe precise depositional environment of these sedimentary rocks.

Our new U–Pb age data on the detrital zircons from theeta-sedimentary rocks in northern Yili Block document sev-

ral magmatic and metamorphic events occurred in the studyrea, including (1) successive magmatic activities during ∼2.2–2.6,1.1–1.0, ∼0.92–0.84, 0.79–0.74 and ∼0.69–0.65 Ga; (2) regionaletamorphism occurred in ∼2.15 and ∼1.4 Ga; and (3) simul-

aneous magmatic and metamorphic events at ∼1.95, ∼1.7 and1.3–1.5 Ga (Figs. 2, 5 and 6). The compiled age spectrum (Fig. 8A)nd corresponding geological events indicate that the continentalrust of the northern Yili Block probably formed during late Paleo-roterozoic to Mesoproterozoic although the available data cannotirectly explore these oldest basement rocks. Thereafter, the conti-ental crust underwent multi-staged growth and reworking duringesoproterozoic to Neoproterozoic, therein, the Neoproterozoicagmatism and metamorphism are the most predominant events

n the cratonization and configuration of the continental crust ofhe Yili Block (Hu et al., 2006, 2010; Wang et al., 2014).

According to the zircon age distribution patterns compiled withvailable data from the northern Yili Block and the neighboringectonic units within the CAOB (e.g., the Chinese Central Tianshan,yrgyz North Tianshan and Tarim Block) (Fig. 8), Paleoproterozoicircons are rare in the northern Yili Block but abundantly existn other units. In addition, the Kyrgyz North Tianshan has a pro-ounced age peak at ∼1.1 Ga (Fig. 8D), which may correspond tohe age of widespread Grenville-stage gneissic granites in Kyrgyzorth Tianshan (Alexeiev et al., 2011; Kröner et al., 2013). However,

uch late Mesoproterozoic zircon population is almost invisiblen the age spectra of the other tectonic units (Fig. 8A–C) probablyecause the old rocks are much less developed or alternatively,hey are barely exposed. Despite these minor differences, theorthern Yili Block has generally similar age distribution patternith those of the Chinese Central Tianshan, Kyrgyz North Tianshan

nd Tarim blocks (Fig. 8A–D). By contrast, the age spectra of theseontinental blocks are obviously different from that of the Southiberian Craton (Fig. 8E) which is characterized by pronounced latealeoproterozoic and late Archean age peaks, corresponding to thencient magmatic events (Rosen et al., 1994; Gladkochub et al.,006; Linnemann et al., 2008; Abati et al., 2010; Rojas-Agramontet al., 2011). Therefore, distinct from Siberian Craton, the northern

ili Block has a tectonic affinity with the other continental blocks

n the southwest of the CAOB, and these blocks might share aommon origin from the Tarim Block. This interpretation is con-istent with previous hypothesis that the continental fragments

rch 252 (2014) 209–222 219

including the Yili Block rifted during Neoproterozoic from theRodinia Supercontinent, in which the Tarim Block is one of themain constituents (e.g., Chen et al., 2004; Zhan et al., 2007; Xiaoet al., 2010). Moreover, available paleomagnetic data obtainedfrom central Kazakhstan and Mongolia also proved that thesemicrocontinents originally belonged to Tarim Block or relatedcontinental assemblages (Levashova et al., 2009, 2011).

7. Conclusions

(1) Mica-schists from the Wenquan Metamorphic Complex andphyllite of the Changcheng System in the northern YiliBlock contain similar early Neoproterozoic (∼915–890 Ma)detrital zircons with magmatic origin, and the youngestpre-depositional zircons are of ∼650 Ma for mica-schistsand ∼850 Ma for phyllite, respectively. In addition, post-depositional metamorphic zircons of ∼430 Ma were foundin the mica-schists. Thus, the protoliths of these meta-sedimentary rocks were likely deposited during latest Neopro-terozoic to late Silurian instead of previously considered Paleo-to Mesoproterozoic. The mica-schists have substantial Meso- toPaleoproterozoic zircon populations which are almost absent innearby phyllite, indicating that the protoliths of mica-schistsand phyllite had distinct source compositions and thereforedeposited at different stages.

(2) The principal provenances of the meta-sedimentary rocksin the northern Yili Block are the Neoproterozoic gneis-sic granite, migmatite (∼930–840 Ma) and meta-mafic rocks(∼780–650 Ma) in the Wenquan Metamorphic Complex. In situMeso- to Paleoproterozoic basement rocks and older rocks arenow rarely exposed but were probably sources of the protolithsof the mica-schists. The latest Devonian to early Carbonifer-ous undeformed sandstones contains unique source of LateDevonian magmatic rocks (∼370 Ma) that were derived fromproximal active magmatic arc in the northern margin of the YiliBlock.

(3) The detrital zircon age patterns and the morphological charac-teristics of zircon grains reveal major Proterozoic magmatic andmetamorphic events in the northern Yili Block. These events arealso documented in the neighboring Chinese Central Tianshan,Kyrgyz North Tianshan and Tarim blocks. Thus, an origin fromthe Tarim Block is favorable for the northern Yili Block and theother continental blocks within the SW of the Central AsianOrogenic Belt.

Acknowledgments

We appreciate kind help from Mr. B. Wu (NJU) in zircon LA-ICPMS dating. Mr. Fei Wang and Mr. Kongsen Li participatedin part of the field work and analysis of zircon geochronology.Prof. W.J. Xiao and another anonymous reviewer, and the EditorProf. G.C. Zhao are greatly appreciated for their detailed com-ments and constructive suggestions in improving our work. Thisstudy was financially supported by National Natural Science Foun-dation of China (41390445, 41172197, 41222019, 41311120069,40802043), the National Basic Research Program of China (973Program) (2007CB411301), Foundation for the Author of NationalExcellent Doctoral Dissertation of PR China (FANEDD, No. 201130),and Fok Ying Tung Education Foundation (131016). B.M. Jahn andB. Wang acknowledge the support of National Research Council(Taiwan) through grants NSC-100-2116-M-002-024 and NSC-101-2116-M-002-003. Supports of the Scientific Research Foundation

for Returned Overseas Chinese Scholars, State Education Ministry ofChina, and the Fundamental Research Funds for the Central Univer-sities are also appreciated. This study is a contribution to IGCP-592Project “Continental construction in Central Asia”.

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20 H. Liu et al. / Precambrian

ppendix A. Supplementary data

Supplementary data associated with this article can be found,n the online version, at http://dx.doi.org/10.1016/j.precamres.014.07.018.

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