Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China

Journal of Asian Earth Sciences xxx (2014) xxx–xxx

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Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China Lu Zhang a, Qinyan Wang a, Nengsong Chen a,b,e,f,⇑, Min Sun b, M. Santosh c, Jin Ba d a

Faculty of Earth Science, China University of Geosciences, Wuhan 430074, China Department of Earth Sciences, The University of Hong Kong, Hong Kong Special Administrative Region Journal Center, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China d Institute of Geological Survey, Sichuan Province, Chengdu 610081, China e State Key-Lab of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan 430074, China f State Key-Lab of Continental Geodynamics, Northwest University, Xi’an 710069, China b c

a r t i c l e

i n f o

Article history: Received 6 February 2014 Received in revised form 15 May 2014 Accepted 15 May 2014 Available online xxxx Keywords: Geochemistry Zircon geochronology Tectonic evolution Tarim and North China Cratons Early-Paleoproterozoic

a b s t r a c t The Delingha paragneiss suite in the Quanji massif, southeastern Tarim Craton, is composed of mica schist, paragneiss, leptynite and quartzite, similar to the ‘khondalite suites’ described from elsewhere in the world. The mica schist is rich in Al2O3 (up to 26 wt%) and contains graphite and diagnostic minerals including sillimanite and garnet, with metamorphism under amphibolite-facies to locally granulite-facies conditions as manifested by association with amphibolite and granulite. The detrital zircon U–Pb ages and geochemical data indicate that the protolith materials of the Delingha paragneiss suite were mainly sourced from 2.20 to 2.45 Ga granites, felsic volcanic rocks and TTG, and were deposited at 2.17–1.92 Ga. The detrital zircon Hf and whole-rock Nd isotopes document important crustal growth at 2.5–2.7 Ga. The detrital zircon age spectra, the whole rock Nd and zircon Hf model ages, the low-maturity of the protolith, and short-distance transportation suggest that the detritus were derived from the underlying Delingha Complex and the lower Dakendaban sub-Group. The timing of magmatic activities in the source region, the depositional age and metamorphic histories of the Delingha paragneiss suite are all comparable to those recorded in the khondalite belt along northern margin of the Ordos Block in the North China Craton. Our study shows that the 2.2–2.45 Ga magmatic rocks were generated in arc or active continental margin settings, suggesting a prolonged subduction and accretion history prior to final amalgamation (2.5–1.8 Ga) to form the unified North China Craton and the assembly of the Tarim Craton in NW China. Ó 2014 Elsevier Ltd. All rights reserved.

1. Introduction The North China Craton (NCC) and Tarim Craton (TC) are two major Precambrian continental blocks in north–northwest China (inset in Fig. 1). The formation of unified NCC and the assembly of the TC with its surrounding micro-continental blocks or massifs, and the incorporation of the two continental blocks into the Columbia supercontinent occurred broadly coevally through subduction-accretion-collision processes during 2.2–1.8 Ga (Zhao et al., 2004; Santosh, 2010; Zhai and Santosh, 2011; Santosh ⇑ Corresponding author at: Faculty of Earth Science, China University of Geosciences, Wuhan 430074, China. Tel.: +86 27 87692420; fax: +86 27 67883001. E-mail addresses: [email protected], [email protected] (N. Chen).

et al., 2012, 2013; Zhao and Zhai, 2013). However, hot debates surround the tectonic history of the NCC and TC at 2.2–2.5 Ga, which is critical for understanding of the tectonic history of these two cratonic blocks (Zhao and Zhai, 2013; Kusky et al., 2007; Kusky, 2011; Zhai et al., 2005; Zhai and Peng, 2007; Zhai and Santosh, 2011; Santosh et al., 2010, 2012). The Quanji Massif (QM) to the southeast of TC is a cratonic fragment (Fig. 1) with Paleoproterozoic paragneissic rocks sporadically exposed as tectonic slices. Some of these paragneisses have been envisaged as khondalite or khondalitic gneiss, based on limited field and preliminary petrographic observations (Lu, 2002; Wan et al., 2006a; Wang, 2009; Chen et al., 2012, 2013; Gong et al., 2012). In this paper, we report results from our detailed investigations on the lithological association, petrography and geochemistry of

http://dx.doi.org/10.1016/j.jseaes.2014.05.014 1367-9120/Ó 2014 Elsevier Ltd. All rights reserved.

Please cite this article in press as: Zhang, L., et al. Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China. Journal of Asian Earth Sciences (2014), http://dx.doi.org/10.1016/ j.jseaes.2014.05.014

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L. Zhang et al. / Journal of Asian Earth Sciences xxx (2014) xxx–xxx

Fig. 1. Geological sketch map of the Tarim Craton, also showing distribution of the Quanji Massif and other neighboring microblocks including the Alxa (part of the Western Block of the NCC), Qilian and Qaidam blocks (modified from Lu et al. (2008b). The inset figure is after Zhao et al. (2005), showing the distribution of the Khondalite belt of the Western Block of North China Craton.

the Delingha paragneiss suite in the QM. Our study focuses on: (1) the nature of the protolith; (2) natures of the source rocks and the provenance; (3) tectonic settings for formation of the source rocks. Our results provide important constraints on the understanding of the Early Paleoproterozoic (2.2–2.4 Ga) evolution of the QM and NW China within the context of the global orogenic events at this time.

2. Geological background The Quanji Massif is exposed southwest to the Western Block of the North China Craton (WBNCC) and in the east of the Tarim Craton (TC) (Fig. 1). The QM extends WNW–ESE for nearly 500 km, and is separated from the Paleozoic South Qilian belt by the Da-Qaidam – Qinghai Lake Fault in the north and from the Qaidam Block by the early Paleozoic north Qaidam high- to ultrahigh-pressure metamorphic belt in the south. The Precambrian basement of the QM is composed of the metamorphosed Paleoproterozoic Delingha Complex (DC), Dakendaban Group and the Mesoproterozoic Wandonggou Group (Lu, 2002; Lu et al., 2002) as well as some metamorphosed mafic and felsic plutons, unconformably covered by the Nanhua-Sinian Quanji Group and other early Paleozoic to Mesozoic strata. The DC is composed of metamorphosed granitoids with lenticular enclaves of amphibolite and mafic granulite. The granitoids were mostly emplaced at 2.37–2.39 Ga, with minor at 2.2 Ga (e.g. Lu, 2002; Lu et al., 2006a, 2008a; Ba et al., 2012; Gong et al., 2012). Some of the amphibolite enclaves yielded TIMS zircon U–Pb ages of 2410 Ma (Lu, 2002) and the mafic dykes intruded the DC at 1.85–1.83 Ga (Lu et al., 2006b, 2008b; Liao et al., 2014). The Dakendaban Group is divided into the lower and upper Dakendaban sub-Groups (LDG and UDG, respectively) (Chen et al., 2012). The LDG is distributed in the northeastern part of Wulan area and is composed of upper amphibolite-facies volcano-sedimentary rocks formed at 2.20–2.32 Ga (Chen et al., 2012). The UDG is mainly exposed near the Delingha town and is predominantly made up of paragneisses, thus term Delingha paragneisses is used in this paper. The detrital zircon ages from the sediments and the timing of first metamorphic event suggest

that the protoliths of these paragneisses were possibly deposited at 2.2–1.92 Ga (Wan et al., 2001, 2006a; Lu, 2002; Huang et al., 2011; Chen et al., 2012). The basement of the QM experienced three regional metamorphic events in the Proterozoic. The first metamorphic event reached upper amphibolite-facies with locally granulite-facies conditions, accompanied by pervasive anatexis. The metamorphism is medium-P/T type and characterized by clockwise P–T path with loading and heating at the prograde stage, followed by decompression after the metamorphic peak and cooling at the final retrograde stage (e.g. Wang, 2009; Chen et al., 2013). The timing of the metamorphism and anatexis has been well constrained. In the Delingha region, metamorphic zircons from the high-grade amphibolite and the paragneiss-associated granulite enclaves within the 2.37 Ga granite yielded a LA-ICP-MS U–Pb age of 1913 ± 38 Ma (Zhang et al., 2011) and a MC-LA-ICP-MS U–Pb age of 1.90 Ga (oral communication, Professor Li, 2013; Zhang et al., 2001), respectively. The anatectic zircons from the granitic leucosomes of the UDG yielded a LA-ICP-MS U–Pb age of 1924 ± 15 Ma (Wang, 2009; Wang et al., 2009). In the Wulan region, the metamorphic zircons from the amphibolites and the anatectic zircons from the granitic leucosomes within the amphibolite and felsic gneiss of the LDG, yielded LA-ICP-MS U–Pb ages of 1948 ± 17 Ma and 1960 ± 43 Ma, and 1946.8 ± 7.8 Ma and 1960 ± 17 Ma, respectively (Chen et al., 2009, 2013). A conventional TIMS U–Pb age of 1939 ± 21 Ma was also reported for zircons from the leucosomes of the felsic gneiss (Lu, 2002; Lu et al., 2006b, 2008b). The second metamorphic event occurred with two stages of low-P/T type amphibolite facies (at 1.85–1.82 Ga) and medium-P/T type amphibolite facies (at 1.82–1.80 Ga), respectively. The two metamorphic stages were considered to take place in an arc-related environment and possibly related to arc-continent or continent–continent collision setting, respectively (Chen et al., 2013), and thus this metamorphic event was probably a result of the final amalgamation of the Quanji Massif with nearby continental block(s), which could be part of the assembly of the global Columbia supercontinent (Chen et al., 2007a, 2009, 2013; Lu et al., 2008b; Wang, 2009). The third metamorphic event under greenschist-facies conditions occurred at the end of the Mesoproterozoic as recorded by a whole-rock Rb-Sr isochron age of 1022 ± 64 Ma for the Wandonggou Group (Yu et al.,

Please cite this article in press as: Zhang, L., et al. Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China. Journal of Asian Earth Sciences (2014), http://dx.doi.org/10.1016/ j.jseaes.2014.05.014

L. Zhang et al. / Journal of Asian Earth Sciences xxx (2014) xxx–xxx

1994), which was considered as the response to the global Rodinia supercontinent assembly. 3. Geology and petrography of the Delingha paragneiss suite The Delingha paragneiss suite is exposed in the area adjacent to the northeastern Delingha City (Fig. 2), and occurs in fault contact with gneisses of the Delingha Complex or covered by Quaternary sediment. The suite can be subdivided into North, Middle and South units along a North–South cross-section (Fig. 3). Representative lithologies of the Delingha paragneiss suite are listed in Table 1. The North unit comprises thick-layered quartzite with minor mica schist, quartz schist, gneiss and garnet-rich rocks as well as amphibolite (Fig. 3). The quartzite occurs as layers generally 1–20 m thick (Fig. 4a), shows white, gray, dark gray or brown color, medium-grained texture, and is composed dominantly of quartz (P90%) with subordinate muscovite, biotite, microcline, garnet, and accessory detrital zircon and monazite (Fig. 4a and b). The mica schist shows brown color, schistose structure, porphyroblastic texture, and contains porphyroblast garnets (35%) and matrix quartz (8%), biotite (45%) and plagioclase (15%). The garnet porphyroblasts are 1–2.5 cm in diameter, and enclose mica, quartz, and reaction remnants of staurolite (Fig. 4a and c), with later intergrowth of plagioclase and biotite on the absorbed edges. The quartz schist is dark gray, shows schistose structure, medium to coarse grained texture, and contains quartz (50–75%) and biotite + muscovite (10–25%), subordinate garnet (5–10%), sillimanite (10%), graphite (2%), and accessory zircon and apatite. The gneiss is composed of plagioclase (40–45%), quartz (35–40%), and biotite (10%), subordinate garnet (5–15%) and muscovite (4–8%) and accessory zircon, apatite, monazite and opaque minerals. Two generations of garnets have been identified (Wang et al., 2009), suggesting a complex metamorphic history. The first generation garnet grew as porphyroblasts generally with embayed edges and inclusions of quartz, plagioclase and/or biotite; the second generation occurs as individual fine-grained subhedral to euhedral crystals in the matrix, or as thin rims on the edges of the first generation garnet and also along the contacts between the matrix biotite and plagioclase. The quartz garnet rocks are embedded within the thick-layered quartzite, and usually show dark gray or dark brown color with garnet (70–85%) and biotite (10–25%) with or without plagioclase (10%) and minor quartz (5%), graphite (3%) and opaque minerals of ilmenite and limonite (2–5%)

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(Fig. 4d). The garnet- and iron-rich rocks contain subordinate limonite and goethite, cummingtonite (Fig. 4e) and biotite in addition to garnet as the major component (>40%) (Table 1). The mica quartz schist and the gneiss commonly show irregular granitic leucosomes. The anatectic zircons from the leucosomes were dated to be 1924 ± 15 Ma using the LA-ICP-MS U–Pb method, which is considered as the timing of the anatexis immediately following the metamorphic peak (Wang et al., 2008; Wang, 2009). The Middle unit consists predominantly of leptynite, quartz schist, quartzite and gneiss with minor graphite schist (Fig. 3). The leptynite, quartzite and schist occur as 0.5–30 cm interlayers, with local 1–3 cm rhythmic layering (Fig. 5a). The quartz schist shows gray color, and is composed of quartz and muscovite, with subordinate feldspars, graphite and opaque limonite (Fig. 5a and c). The schist is dominantly composed of muscovite (up to 90%) with subordinate quartz and minor limonite and graphite (Fig. 5c). The leptynite contains predominant K-feldspar and quartz (P90%), subordinate muscovite and graphite, with or without plagioclase and biotite (Fig. 5b and d), and accessory minerals of zircon and apatite. A previous dating on 35 detrital zircon grains from the K-feldspar leptynite yielded an age spectrum with a mono-peak age of 2.19 Ga (e.g. Huang et al., 2011). The feldspar mica schist is intercalated within the leptynite layers (Fig. 5e), and shows dark gray color, medium-grained texture and contains 50–60% muscovite, 20–30% sodium–plagioclase, The muscovite occurs as porphyroblast-like lenses (usually >1 cm) with assemblage of fined-grain muscovite flakes and fibrous sillimanite, wrapped by large muscovite sheets (Fig. 5f). The matrix shows intergrowth of subordinate fined-grain limonite and muscovite flakes and albite or Na-plagioclase. The South unit is composed of dominant mica schist, quartz schist and graphite schist with minor gneiss as well as amphibolite (Fig. 3). The mica schist and quartz schist display transgressive relation with the development of granitic leucosomes. The gneiss shows the same features as those in the North and Middle units. The mica schist shows gray to dark-gray color, schistose structure, and contains biotite + muscovite (50–60%), sillimanite (10–20%), quartz (10–15%), and subordinate plagioclase + K-feldspar (5–10%), and garnet (5–10%), with or without graphite (2–5%) (Fig. 6a and b). The quartz schist shows the same structure and texture as those of the mica schist, and contains the same major minerals but greater content of quartz (>50%) than mica (<50%) with subordinate staurolite + kyanite (5–10%). Two generations of garnet are developed in the quartz schist;

Fig. 2. Geological sketch map showing part of the Quanji Massif in Delingha area. Note that the Delingha paragneiss suite (the upper Dakendaban Group, Pt1D2) is in fault contact with and occurs as a tectonic slice thrusting on the Delingha monzonitic granitic gneiss of the Delingha complex. The symbol below Delingha City represents the urban area of that city.

Please cite this article in press as: Zhang, L., et al. Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China. Journal of Asian Earth Sciences (2014), http://dx.doi.org/10.1016/ j.jseaes.2014.05.014

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L. Zhang et al. / Journal of Asian Earth Sciences xxx (2014) xxx–xxx

Fig. 3. A cross-section along road cut on the western edge of the Delingha paragneiss suite showing the distribution of the three main lithologic units and fault contact with the Delingha monzonitic granitic gneiss. Also shown are the localities of the three samples of detrital zircon dating from each unit as well as the formation line of the western side of the tectonic slice of the Delingha paragneiss suite.

Table 1 Mineral compositions and modes (volume%) of representative rocks from the Delingha paragneisses. Units

Sample

Type

North North North North

CN09-4 CN07-11-2 LZR-1 LZR-3

North North North North North Middle

04DLH-08 04DLH-11 06DLH-05 06DLH-10 06DLH-11 06DLH-16 and CN0727-1 CN09-6 06DLH-17 12DLH-1 CN07-27-2 CN29-1

Quartzite Garnet-rich schist Quartz garnet rock Garnet- and iron-rich rock Quartz feldspar gneiss Quartz feldspar gneiss Quartz feldspar gneiss Quartz feldspar gneiss Quartz feldspar gneiss Quartz feldspar leptynite Mica quartz schist Mica schist Mica schist Mica schist Mica graphite schist

South South South Middle South

Sil

Ky

Sta 5–10

5–8 <5 10

5

<5

5–10 <5 <5

6–10

10–15 15–20 5

Grt

Bi

25–35 80–85 40–50

35–45 5–10 10–15

10–15 10–15 5–10

8–10 10–15 8–10 10–15 10–15

5–10

5–10 5–10

15–20 30–40 30–40

Ms

Pl

5–8 5

Kf

Qtz

Cum

90–95 5–10 5–10

5–10

20–30 5–10 5 10–15 10–15 <5 5–15

20–25 25–30 50–60 40–50

10–15 5–10 10–15 10–25 35–40 15–20

50–60 10–15 10–15 25–35 10 30–35

35–40 30–40 25–30 25–30 25–30

5–10 <5 <5 20–30

<5 <5 <5 <10 5–10

50–60 10–15 10–15 5–15 10–15

Gra

5 5–10

Opa 3 5 10–15 2 2 1

2

5 2

<5 25–30

<10 <2

Mineral abbreviations: Sil – sillimanite, Ky – kyanite, Sta – staurolite, Grt – garnet, Bi – biotite, Ms. – muscovite, Pl – plagioclase, Kf – potassium feldspar, Qtz – quartz, Cum – cummingtonite, Gra – graphite (identified under reflected light), Opa – opaque minerals, predominantly of metal minerals, with or without graphite under transmitted light.

the first generation occurs as porphyroblasts with embayed edges, and the second shows fine-grained euhedral crystals or thin rims on resorbed edges of the first generation garnet porphyroblasts or along the contacts between the plagioclase and biotite. The sillimanite occurs as fibrous crystals, cross-cutting the biotite, or together with the assemblages of fine-grained euhedral staurolite and kyanite replacing the muscovite porphyroblasts. The graphite schist occurs as 3–5 m wide layers within the quartz mica schists (Fig. 6c). The rocks show gray to dark-gray color and fine-grained texture, and contain major graphite (up to 20–30%), muscovite (20–35%) and quartz (30–40%). The graphite crystals display crenulation with the muscovite flakes (Fig. 6d). The amphibolites occur as lenticular bands of 1–17 m thick and several to tens of meters long (Fig. 3). They show dark green color, gneissic structure and medium-grained texture, with hornblende (50%) and plagioclase (45%) as the major minerals and biotite and garnet as minor minerals, and accessory phases include sphene and ilmenite. Some of the lenticular amphibolites show weakly developed leucosomes on the outcrops, suggesting their protolith was generated prior to the medium-P/T type metamorphism at 1.92 Ga (Chen et al., 2013), thus formed at 1.92–2.19 Ga. However, some amphibolite lenses are free of leucosomes and yielded LA-ICP-MS U–Pb age of 1836 ± 17 Ma on metamorphic zircons, suggesting that their protolith was produced at 1.92–1.84 Ga. A recent study suggested that both 1.92–1.84 Ga and 1.92–2.19 Ga amphibolites are metamorphosed equivalents of basic dykes and

basalts, respectively (Hassan et al., in preparation, unpublished data). In order to understand the nature of the protolith and the source rocks, and the tectonic settings for formation of the source rocks in the provenance, whole-rock samples were selected from rocks of the North, Middle and South units of the Delingha paragneiss, and major- and trace-elements and Nd isotope compositions were analyzed. Representative samples were also collected from each of the three units for zircon U–Pb and Hf isotope analyses.

4. Analytical methods Whole-rock major elements were determined at the Material Research Center of the Wuhan University of Technology and the State Key Laboratory of Geological Processes and Mineral Resources of China University of Geosciences in Wuhan, respectively using an Axios advanced X-ray fluorescence spectroscopy. The results are presented in Supplementary Data Table 2. The analytical precisions are better than 5% for the major elements. Wholerock trace elements were measured by using Agilent 7500a ICP-MS at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences in Wuhan. The samples were digested by Hf + HNO3 in Teflon bombs for ICP-MS analyses, as described by Liu et al. (2008a). The rock standards AGV-2, BHVO-2, BCR-2 and GSR-1 were used as external standards. The

Please cite this article in press as: Zhang, L., et al. Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China. Journal of Asian Earth Sciences (2014), http://dx.doi.org/10.1016/ j.jseaes.2014.05.014

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Fig. 4. Outcrop photos and photomicrographs of representative rocks from the North unit. (a) Outcrop photo showing the thick-layered quartzite with minor garnet mica schist and garnet and biotite-bearing quartzite; (b) Photomicrograph showing mineral compositions of the garnet-bearing quartzite with predominant equant-grained quartz, minor porphyroblast garnet and flaky limonite (parallel nicols); (c) Photomicrograph showing island-like staurolite remnants inside the porphyroblastic garnet (Sample CN07-11-2; crossed nicols); (d) Photomicrograph showing subhedral flaky graphite associated with limonite (Sample LZR-1; reflected light); (e) Photomicrograph showing garnet- and iron-rich rocks containing sieve-textured garnet and prismatic cummingtonite (Sample LZR-1; parallel nicols). Mineral abbreviations: Grt – garnet; Qtz – quartz; Lm – limonite; Pl – plagioclase; Sta – staurolite; Gra – graphite; Cum – cummingtonite.

precisions are better than 5% and the accuracies are better than 10%. Detailed analytical procedures were described by Liu et al. (2008a). Nd isotope compositions were analyzed by using Nu Plasma HR MC-ICP-MS at State Key-Lab of Continental Geodynamics of the Northwest University, Xi’an, China. The measured 143Nd/144Nd ratios were normalized to 146Nd/144Nd of 0.7219. The La Jolla and GBW04411 Nd standards were measured during the course of analyses, yielding a 143Nd/144Nd ratio of 0.511842 ± 10 (2r), and 143 Nd/144Nd = 0.512740 ± 8, respectively. In this study, eNd(t) values were calculated using (143Nd/144Nd)CHUR = 0.512638, (147Sm/144Nd)CHUR = 0.1967 and k147Sm = 6.54  10 12 a 1. Depleted mantle Nd model ages (TDM1) were calculated using a present-day depleted mantle 143Nd/144Nd ratio of 0.513151 and 147 Sm/144Nd ratio of 0.21357. In order to exam the influence of the fractionation of Sm and Nd, two-stage Nd model ages (TDM2) were calculated using average continental crust 147Sm/144Nd values of 0.118 (Jahn and Condie, 1995). Zircon grains were separated employing heavy liquid and magnetic techniques and then hand-picked under a binocular microscope, enclosed in epoxy resin and polished to about half their thickness. Cathodoluminescence (CL) images of the zircons were taken at the Institute of Geology and Geophysics, Chinese Academy of Sciences in Beijing, using the MiniCL by Gatan

Company, Germany, mounted on LEO1450VP Scanning Electron Microscopy, which was used to investigate their internal structures, and in order to choose spot sites for analyses of trace elements, U–Pb and Hf isotopes. Trace element analyses and U–Pb dating for zircons from samples CN07-27-1 and CN09-6 were conducted by LA-ICP-MS at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan. ICP-MS ELAN 7500a and GeoLas 2005 laser-ablation system equipped with a 193 nm ArF-excimer laser were used for the experiments. The analysis was carried out with beam sizes of 24 lm and 32 lm, respectively, 6 Hz repetition rate. Off-line selection and integration of background and analytical signals, and time-drift correction and quantitative calibration for trace element analyses and U–Pb dating were performed using in-house software ICPMSDataCal (e.g. Liu et al., 2008b, 2010). Concordia diagrams and weighted mean calculations were made using Isoplot/Ex.ver3 (Ludwig, 2003). The reference glass SRM 610 and Si were analyzed as external and internal standards, respectively, for trace element content calibration (Liu et al., 2010). The preferred values of element concentrations for the USGS reference glass are from the GeoReM database (http://georem.mpch-mainz.gwdg.de/). The trace element concentrations in zircon standard 91500 obtained at both beam sizes of 24 and 32 lm are generally consistent with the

Please cite this article in press as: Zhang, L., et al. Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China. Journal of Asian Earth Sciences (2014), http://dx.doi.org/10.1016/ j.jseaes.2014.05.014

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Fig. 5. Outcrop photos and photomicrographs of representative rocks from the Middle unit. (a) Outcrop showing rhythmic layering made up of leptynite and quartz schist bandings with very thin layers of mica schist (after Fig. 2b by Wang et al., 2009). (b) Outcrop showing muscovite K-feldspar leptynite (sample CN07-27-1), which clearly displays pink color due to large volume of microcline without iron-bearing mineral limonite. (c) Micro bandings of mica schist and leptynite. Such leptynite usually shows gray color on outcrop (e.g. Fig. 5a) because of some flaky limonite (parallel polarized light). (d) Muscovite K-feldspar leptynite (e.g. Fig. 5b) showing mineral compositions of predominant quartz, microcline with minor muscovite (parallel polarized light). (e) Outcrop showing thin interlayer of mica schist within the leptynite (f) Porphyroblast-like muscovite lens showing intergrowth with fibrous sillimanite wrapped by large flaky muscovites and limonites. Mineral abbreviations: Kf – K-feldspar; Ms. – muscovite; Mi – microcline; Sil – sillimanite; others are the same as those in Fig. 4.

LA-ICP-MS working values within 10% relative deviation as well as those reported by Belousova et al. (2009). Zircons 91500 (Wiedenbeck et al., 1995) and GJ-1 (Jackson et al., 2004) were used as internal and external standards respectively for U–Pb dating, and was analyzed twice every five analyses. Time-dependent drifts of U–Th–Pb isotopic ratios were corrected using a linear interpolation (with time) for every five analyses according to the variations of 91500. Because the common Pb is low in these standards, no common Pb correction was made. The obtained mean 206Pb/238U ages for the zircon GJ-1 is 599.1 ± 4.1 Ma (2r, n = 10) for beam size of 24 lm, and 594.3 ± 6.3 Ma (2r, n = 4) for beam size of 32 lm, well consistent with the reported or recommended value (GJ-1: 206Pb/238U age 599.8 ± 1.7 Ma (2r), Jackson et al., 2004) within analytical error. Hf isotopic analysis was carried out on zircon domains near the spots where U–Pb dating was done by Neptune Plus MC-ICP-MS (Thermo Fisher Scientific, Germany) in combination with a Geolas excimer ArF laser ablation system (Lambda Physik, Göttingen, Germany) at the State Key Laboratory of Geological Processes and Mineral Resources of China University of Geosciences, Wuhan. Spot laser ablation was adopted in this study with a 20 s background acquisitions and 50 s sample data acquisitions, a beam size of 44 lm, laser pulse frequency of 6 Hz. Detailed analytical procedures were described by Hu et al. (2012). The 179Hf/177Hf and 173Yb/171Yb

ratios were used to calculate the mass bias of Hf (bHf) and Yb (bYb), which were normalized to 179Hf/177Hf = 0.7325 and 173Yb/171Yb = 1.1248 (Blichert-Toft and Albarede, 1997) using an exponential correction for mass bias. Interference of 176Yb on 176Hf was corrected by measuring the interference-free 173Yb isotope and using 176 Yb/173Yb = 0.7876 (McCulloch et al., 1977) to calculate 176 Yb/177Hf. Similarly, the relatively minor interference of 176Lu on 176 Hf was corrected by measuring the intensity of the interference-free 175Lu isotope and using the recommended 176 Lu/175Lu = 0.02656 (Blichert-Toft and Albarede, 1997) to calculate 176Lu/177Hf. Off-line selection and integration of analyte signals, and mass bias calibrations were performed using ICPMSDataCal (Liu et al., 2010). Zircon U–Pb and Lu–Hf isotope analyses for sample CN09-4 were carried out in situ using a Resolution M-50-HR type 193 nm excimer laser ablation system of Resonetics, attached to Nu Plasma HR multi-collector ICP-MS, in the Department of Earth Sciences, the University of Hong Kong. Spot laser ablation was adopted in this study with a beam size of 30 lm for U–Pb and 55 lm for Hf isotopic analyses, laser pulse frequency of 6 Hz, and energy density of 5 J/cm2. The ablated sample materials were transported by helium carrier gas mixed with a small amount of argon and nitrogen. Analytical time for each spot was 100 s, which consisted of

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Fig. 6. Outcrop photos and photomicrographs of the South unit. (a) Outcrop photo showing obvious acicular or fibrous Sillimanite bundles in the mica schist; (b) Photomicrograph of mica schist showing sillimanite bundles in preferred orientation, which displays the main gneissosity or schistosity of such type of rocks (parallel nicols); (c) Outcrop photo of graphite schist showing prominent schistosity; (d) Photomicrograph of graphite schist showing flaky graphites occurring as crenulation foliation with muscovite flakes (Sample CN07-29-1, reflected light). Mineral abbreviations: Sil – sillimanite; Bi – biotite; Ms. – muscovite; Lm – limonite; Gra – graphite; others are the same as those in Figs. 4 and 5.

early 40 s background acquisitions (including gas blank and laser valve off) and later 60 s sample data acquisition. The masses of Hf isotope acquisition are from 172Hf and 179Hf. 176Hf/177Hf isotopic ratios were normalized to 179Hf/177Hf = 0.7325, using exponential correction for mass bias (Patchett and Tatsumoto, 1980). The isobaric interference of 176Yb and 176Lu on 176Hf was corrected by monitoring 172Yb and 175Lu, using the new ratios of 176Yb/172Yb and 176Lu/175Lu of 0.5887 and 0.02655 respectively (Vervoort et al., 2004). The 176Lu decay constant 1.865  10 11 yr 1 (Scherer et al., 2001) was used to calculate initial 176Hf/177Hf ratios. The chondritic values of 176Hf/177Hf (0.282772) and 176Lu/177Lu (0.0332) reported by Blichert-Toft and Albarede (1997) were used for the calculation of eHf values. The depleted mantle Hf model age (TDM1) was calculated using an isotopic liner growth model, projecting the initial ratio of 176Hf/177Hf = 0.279718 at 4.55 Ga, and a present-day 176Hf/177Hf = 0.283250, 176Lu/177Hf = 0.0384 (Griffin et al., 2000). Two-stage zircon Hf model ages (TDM2) are calculated using Lu/Hf = 0.015 for the average continental crust (Griffin et al., 2002). Off-line processing of the U–Pb raw data was performed also using the in-house software ICPMSDataCal (e.g. Liu et al., 2008b, 2010). Concordia diagrams and weighted mean calculations were also made using Isoplot/Ex.ver3 (Ludwig, 2003).

5. Results 5.1. Zircon U–Pb geochronology Zircon U–Pb isotopic ratios and the calculated age results are listed in Supplementary Data Tables 2–4 for the muscovite-bearing quartzite sample (sample CN09-4) from the North unit, the K-feldspar leptynite sample (sample CN07-27-1) from the Middle unit, and the mica quartz schist sample (sample CN09-6) from the South unit, respectively. CL images of the representative zircon grains are presented in Fig. 7. Th/U vs age plots and chondrite normalized REE patterns for the zircon grains from samples CN07-27-1 and CN09-6 are shown in Figs. 8 and 9, respectively.

5.1.1. Sample CN09-4 from the North unit Detrital zircon grains from this sample are mostly euhedral prismatic crystals with slightly corroded edges and clear oscillatory zoning (Fig. 7a). All the 62 analyses yielded concordant ages ranging from 2233 to 2494 Ma (Supplementary Data Table 2, Fig. 10a). The relative probability plot of the concordant 207 Pb/206Pb ages shows a major age peak at 2.38 Ma and two minor peaks at 2.45 Ga and 2.24 Ga (Fig. 10b), which are consistent with the results previously reported for the detrital zircons from a quartzite (sample CN07-1, Fig. 3) near the northern border of the North unit (e.g. Chen et al., 2012). 5.1.2. Sample CN07-27-1 from the Middle unit Detrital zircons from this sample are prismatic crystals with slightly corroded edges and oscillatory zoning (Fig. 7b). Thirty-six U–Pb analyses have been reported previously (Huang et al., 2011), and 15 more analyses were conducted in this study (Supplementary Data Table 3). Among the total 51 data, 43 give concordant ages ranging from 2067 to 2280 Ma (Supplementary Data Table 3), with Th/U values >0.4 (Fig. 8a) and REE patterns typical of the igneous zircons (Fig. 9a). On the Concordia plot, the data points are clustered as two populations; the old population has concordant ages in the range of 2.16–2.25 Ga, and the young population in range of 2.06–2.16 Ga, with mean ages of 2.19 Ga and 2.12 Ga, respectively (Fig. 10c). These spectra are shown on the histograms, but the relative probability plot of concordant 207 Pb/206Pb ages shows a single peak at 2.17 Ga due to high uncertainties (>40 Ma) for most single 207Pb/206Pb age (Fig. 10d, Supplementary Data Table 3), consistent with the single peak age (2.19 Ga) previously obtained by Huang et al. (2011). 5.1.3. Sample CN09-6 from the South unit Detrital zircons from this sample show prismatic shape as stubby or rounded grains. Most of the crystals are subangular with minor sub-rounded grains and the majority show oscillatory zoning (Fig. 7c). Fifty analyses on 50 zircon grains yielded Th/U values

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Fig. 7. Representative Cathodoluminescence (CL) images for zircons from (a) the muscovite-bearing quartzite (sample CN09-4), (b) the K-feldspar leptynite (sample CN0727-1) and (c) the mica quartz schist (sample CN09-6). The solid line circles mark the spot site for age dating, and the yellow dashed line circles for Lu–Hf isotopic analyses.

Fig. 8. (Th/U) vs.

207

Pb/206Pb diagram for the zircons from (a) the K-feldspar leptynite (sample CN07-27-1) and (b) the mica quartz schist (sample CN09-6).

Fig. 9. Chondrite-normalized REE patterns for the zircons from (a) the potassium- feldspar leptynite (sample CN07-27-1) and (b) the mica quartz schist (sample CN09-6). The chondrite-normalized values are from Sun and McDonough (1989).

mostly >0.3 with REE patterns also typical of the igneous zircons (Fig. 9b). The data show 48 concordant ages ranging from 2209 to 2529 Ma (Supplementary Data Table 4, Figs. 8b and 10e). The

relative probability plot of the 48 concordant 207Pb/206Pb ages shows a major peak at 2.45 Ga with two very minor peaks at 2.38 Ga and 2.20 Ga (Fig. 10f).

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Fig. 10. (a) and (b) Concordia diagrams of U–Pb zircon and histogram-relative probability plots of 207Pb/206Pb ages with 90% or higher concordance for zircons from the muscovite-bearing quartzite (sample CN09-4), (c) and (d) the K-feldspar leptynite (sample CN07-27-1) and (e) and (f) the mica quartz schist (sample CN09-6).

5.2. Whole rock geochemistry 5.2.1. Major- and trace-elements Major and trace elements compositions for the representative rocks (garnet rich rocks, feldspar rocks and mica schists) are listed in Supplementary Data Table 5. The garnet-rich rocks show high Fe2Ot3 (22.3–59.3%), low SiO2 (30.9–50.9%), and highly variable Al2O3 (5.70–19.4%), consistent with mineral compositions, i.e. predominant biotite and garnet, minor staurolite, and lack of kyanite/ andalusite/sillimanite (Table 1). Sample LZR-3 contains the highest Fe2Ot3, corresponding to its high volume of opaque minerals (10–15%). The feldspar gneiss and leptynite have high contents of SiO2 (59.4–79.8%) and broadly variable Al2O3 (7.79–21.9%) and K2O (1.48–5.65%), moderate Na2O (0.63–2.60%), and CaO (0.35–1.87%), with Na2O + CaO = 1.86–4.15% (mostly P2.13%), correlating with the predominant plagioclase, potassium feldspar and quartz, with minor mica and garnet as well as with or without sillimanite, kyanite and staurolite (e.g. Wang, 2009). Except for

sample CN07-27-2, the other 7 mica schist samples show high content of SiO2 (58.7–64.6%), moderate to high Al2O3 (17.9–25.9%), moderate K2O (3.36–4.99%) and Fe2Ot3 (5.02–8.70%), and low Na2O (0.22–0.80%) and CaO (0.26–0.69%), with Na2O + CaO = 0.48–1.49% mostly 60.94%, correlating with the dominant mica (biotite and muscovite) and quartz with minor feldspars and garnet (Table 1), and with or without sillimanite, kyanite and staurolite. The sample CN07-27-2 has moderate content of Fe2Ot3 (6.06%), consistent with the presence of limonite with minor goethite. On the other hand, high K2O (3.98%) and Na2O (4.47%) and moderate CaO (1.28%) of this sample corresponding to high volume of muscovite and Na-plagioclase, but the quartz mode is low (Table 1) with corresponding low SiO2 content. The feldspar gneiss, leptynite, mica schist and garnet-rich rocks have Zr/TiO2 values mostly >200, and show sedimentary protolith on Zr/TiO2 vs. Ni plots (Winchester et al., 1980) (Fig. 11). On the Cr vs. Ni diagram (Taylor and Mclennan, 1985), all samples are plotted in a domain overlapping the areas of the post Archean and late

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respectively, totally ranging from 2.42 to 2.79 Ga (Supplementary Data Table 7, Fig. 13c), with one major peak at 2.66 Ga and two shoulders at 2.62 Ga and 2.76 Ga on the relative probability plot (Fig. 13d). Thirty Hf isotope analyses were carried out on the zircons from sample CN09-6. The analyses yielded 2 eHf(t) values <0, corresponding to TDM2 model ages of 2.93 and 2.98 Ga, and 28 eHf(t) values >0, ranging from +1.0 to +6.9, corresponding to TDM1 from 2.50 to 2.76 Ga (Supplementary Data Table 8, Fig. 13e). The relative probability plot of these model ages show a major peak at 2.72 Ga, two minor peaks at 2.96 Ga and 2.50 Ga, and one shoulder at 2.66 Ga on the relative probability plot (Fig. 13f).

Fig. 11. Ni vs. (Zr/TiO2) diagram for discrimination of sedimentary and igneous origins for the Delingha khondalite protolith (after Winchester et al., 1980).

Archean sediments, showing mixing of the protolith materials (Fig. 12a). The rocks of the Delingha paragneiss suite have high total REEs with an average of 246 ppm. The chondrite normalized REE patterns are similar for the mica schists, quartz schists, gneisses and leptynites, with enriched LREE, flat HREE and strong to moderate negative Eu anomalies (dEuN = 0.32–0.84) (Fig. 12b). Nevertheless, as shown on Fig. 12b, all samples exhibit REE patterns similar to those for the Post Archean average Australian shale (PAAS) (Taylor and McLennan, 1985).

5.2.2. Zircon Hf isotopes Hf isotopic compositions are presented in Supplementary Data Tables 6–8 for the zircons from muscovite-bearing quartzite (sample CN09-4) from the North unit, K-feldspar leptynite (sample CN07-27-1) from the Middle unit, and mica quartz schist (sample CN09-6) from the South unit (Fig. 3, Table 1), respectively. Forty Hf isotope analyses were conducted on the detrital zircons, from sample CN09-4, on which U–Pb ages were determined, and the results show eHf(t) values ranging from -1.1 to + 4.7 (Supplementary Data Table 6, Fig. 13a). Thirty-eight of the 40 analyses show positive eHf(t) with depleted mantle model ages (TDM1) in the range of 2.51–2.70 Ga; the rest 2 analyses have negative eHf(t) with TDM2 model ages of 2.99–3.00 Ga. The total model ages range from 2.51 to 3.00 Ga, with one major peak at 2.81 Ga, two minor peaks at 3.0 Ga and 2.65 Ga, and one shoulder at 2.9 Ga on the relative probability plot (Fig. 13b). Thirty-one Hf isotope analyses were conducted on the zircons from sample CN07-27-1, which yielded eHf(t) values ranging from 1.5 to +3.4, with 24 data >0 and the other 7 data 60, corresponding to 24 TDM1 model ages and 7 TDM2 model ages,

5.2.3. Nd isotopes Six analyses of Nd isotopes for whole rock samples from the Delingha paragneiss suite yielded eNd(t) values ranging from 5.93 to 1.48, and 147Sm/144Nd values ranging from 0.0944 to 0.1243 (Supplementary Data Table 9). Three samples show 147 Sm/144Nd values between the lower crust (0.151) and upper crust (0.105) (e.g. Taylor and Mclennan, 1985), but the other three are lower than that of the upper crust, suggesting that the Sm–Nd system for some of the samples had probably been disturbed and fractionated during the amphibolite facies metamorphism and anatexis at 1.92 Ga. In this case, two stage model ages (TDM2) are calculated for those whole-rock samples with 147 Sm/144Nd < 0.108 and those with 147Sm/144Nd > 0.128 for discussing their petrogenesis (e.g. Li et al., 1991), because the 147 Sm/144Nd ratios of these samples are considered to be reset and fractionated at 1.92 Ga. As shown in Supplementary Data Table 9, samples 06DLH-11, 06DLH-15 and 06DLH-17 have 147 Sm/144Nd values of 0.1129, 0.1099 and 0.1243, respectively, and show TDM1 of 2.82 Ga, 2.78 Ga and 2.92 Ga, respectively. The samples 06DLH-5, 06DLH-16 and 04DLH-11 have 147Sm/144Nd values of 0.1034, 0.0944 and 0.1043, respectively, with 147 Sm/144Nd < 0.108, and the calculated TDM2 ages of 2.83 Ga, 2.51 Ga and 2.67 Ga, respectively (Supplementary Data Table 9). Taken together, the total 6 samples have Nd model ages of 2.51–2.92 Ga with average of 2.76 ± 0.14 Ga, or 2.80 ± 0.09 Ga if the number of 2.51 Ga is excluded. 6. Discussion 6.1. Is the Delingha paragneiss suite of a khondalite? The term ‘‘khondalite’’ was firstly used by Walker (1902) for the garnet-sillimanite-(graphite) schist exposed in the Archean Eastern Ghats Group, Orissa State of India. The term has been accepted worldwide for a suite of metamorphosed continental shelf

Fig. 12. (a) Cr vs. Ni diagram showing time signatures of protolith deposits of the Delingha khondalite (after Taylor and Mclennan, 1985) (b) Chondrite normalized rare-earth element patterns, on which also shown is the REE pattern of the Post Archean average Australian shale (PAAS) (Taylor and Mclennan, 1985).

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Fig. 13. Histograms and relative probability plots for eHf(t) and TDM2 values of the zircons from the muscovite-bearing quartzite (sample CN09-4) (a and b), the K-feldspar leptynite (sample CN07-27-1) (c and d) and the mica quartz schist (sample CN09-6) (e and f).

sequence including quartzite, pelites and carbonates (Cooray, 1960; Cooray, 1962; Krishnan, 1968; Narayanaswami, 1975; Bates and Jackson, 1980; Barbey and Cuney, 1982; Qian et al., 1985; Chacko et al., 1987; Dash et al., 1987). Walton et al. (1983) suggested that the term khondalite should be used for a rock suite dominantly composed of garnet-quartz-sillimanite schist and garnet quartzite, graphite schist and marble. Geochemically, khondalites show distinctive features such as enrichment in Al and Si, depletion in alkali elements (Na and K), Cr and Ni, with MgO > CaO and K2O > Na2O. Their Al2O3 contents are highly variable, and can be <10 wt% for the felsic gneiss member (e.g. Lu et al., 1996 and the references therein). Quartzite and some leptynites of the khondalite suite contain only minor sillimanite, but garnet contents can be as high as 30–40 wt%; and some of the rocks have abundant sillimanite together with garnet, or cordierite (Santosh, 1987; Jiang, 1990; Lu et al., 1996). A study by Condie et al. (1992) indicates that the sillimanite-garnet gneisses, the Al-rich member of the khondalite suite from the Khondalite belt of the Western Block, NCC, in the Datong area, possess Al2O3 content of 14.0–21.0 wt%, with an average of 18.6 ± 2.83 wt%.

The Delingha paragneiss suite and other similar paragneisses have been suggested to be khondalites or khondalitic gneisses, considering that the mica schist, gneiss and leptynite are associated with garnet bearing quartzite, and contain high content of sillimanite and graphite in the mica schist, together with other metasedimentary gneiss and leptynite (Lu, 2002; Wan et al., 2006a; Wang, 2009; Chen et al., 2012, 2013; Gong et al., 2012). However, the presence of graphite was only speculated in these studies. Our present study revealed that the protoliths of the Delingha paragneiss are sedimentary rocks (Fig. 11). The thick-layered quartzite contains minor mica and feldspar with variable volume of garnet (Fig. 4b). The mica schist, mica quartz schist, feldspar gneiss and leptynite also contain variable amounts of garnet, sillimanite, kyanite and staurolite (Figs. 4c–e and 6a and b), particularly the mica schists in the South unit generally contain sillimanite up to 15–20% (Fig. 6a and b). Flaky graphite occurs in the rocks from all the three units (Figs. 4d and 5c and f). Furthermore, some rocks in the South unit even contain 25–30% graphite so that the rocks can be named as graphite schists (Fig. 6c and d). Geochemically, most mica schists contain Al2O3 ranging from 20 to 26 wt%

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(Supplementary Data Table 5), showing features similar to those of the sillimanite-garnet gneisses, i.e. the Al-rich rock member of the Khondalite belt of the Western Block, NCC (e.g. Condie et al., 1992; Lu et al., 1996). Furthermore, a slice of paragneiss suite elsewhere in the Delingha area was reported to be undergone upper amphibolite- to granulite-facies temperature condition (e.g. Zhang et al., 2001). We thus suggest that the rocks of the Delingha paragneisses represent a khondalite suite, in spite of the absence of graphitebearing meta-carbonate which could have been tectonically dismembered. 6.2. Nature of the source rocks and the sedimentary provenance(s) Chen et al. (2012) reported U–Pb and Hf isotope and trace element compositions of detrital zircons from one quartzite sample from the North unit of the Delingha paragneiss suite and discussed possible nature of protolith materials. In this study, we obtained mineral composition, whole-rock geochemistry and detrital zircon U–Pb and Hf isotope compositions for the different rock types in this suite in order to provide further constraints on the nature of the source rocks and the sedimentary provenance(s) for the protolith of these metamorphosed sedimentary rocks (e.g. Compston and Pidgeon, 1986; Lahtinen et al., 2002; Griffin et al., 2004; Kontinen et al., 2007). The presence of detrital potassium feldspar (majority is microcline) and plagioclase in the quartzite, quartz schist, gneiss and leptynite of the Delingha paragneiss suite indicate that the source region was dominated by felsic rocks of continental source (Table 1). We consider that it would not be reasonable to use the chemical index of alteration (CIA, Nesbitt and Young, 1982) and/or Chemical index of weathering (CIW, Harnois, 1988) to evaluate chemical alteration or weathering degrees for the protolith sediments in

our case, because it is hard to meaningfully evaluate the complex changes during transportation and mobility of K in the subsequent multiple amphibolite-facies metamorphism (e.g. Chen et al., 2013) and pervasive anatexis of the paragneiss (Wang et al., 2008; Chen et al., 2012). However, whole-rock immobile trace elements can better preserve information about compositional characteristics of the source rocks (Taylor and Mclennan, 1985; Cullers et al., 1988; McLennan and Taylor, 1991). On the diagram of La/Th vs. Hf, two of the three samples of garnet-rich rocks are plotted in the acidic arc source field and the remaining one (sample CN0711-2) is plotted near the tholeiitic ocean island source field (Fig. 14a). The samples of mica schists are all plotted in the acidic arc source and those of the feldsparthic gneiss and leptynite are plotted near the acidic arc towards the passive margin source, showing that their protolith materials were sourced from arc setting mixed with some passive margin rocks. The diagrams of La/ Sm vs. TiO2/Yb, Th/Sc vs. TiO2/Yb and Cr/Sc vs. TiO2/Yb (e.g. Kontinen et al., 2007) show that the source rocks were possibly a mixture of granite, TTG and felsic volcanic rocks (Fig. 14b–d). The detrital zircons from the three lithological units of the Delingha paragneiss suite show clear oscillatory zoning with Th/U ratios mostly >0.3, indicating magmatic origin (Vervoort and Patchett, 1996; Belousova et al., 2002; Rubatto, 2002; Wu and Zheng, 2004) and supporting that they were sourced from granitoids and/or felsic volcanic rocks. Trace elements in zircons are closely dependent on their parental magma compositions (Belousova et al., 2002). Based on multivariate statistic study of trace elements in zircons from typical lithologies worldwide, Belousova et al. (2002) proposed classification and regression tree (CART) to discriminate the parental magmas of zircons. When their criteria are applied, our results show that the parental magmas for the detrital zircons from samples CN07-27-1 and CN09-6 are dominantly of

Fig. 14. Discrimination diagrams for tectonic setting affinity (a) (after Floyd and Leveridge, 1987) and compositions (b–d) of the source rocks (after Kontinen et al., 2007) for the protolith deposits of the Delingha khondalite. Symbols are as those in Fig. 11. Data point of sample LZR-3 has TiO2/Yb value of 0.02 and is plotted outside the Fig. 14c–d.

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Fig. 15. Histograms showing abundance of type of the host rocks for the dated detrital zircon grains, based on the short CART (classification and regression trees) by Belousova et al., 2002, for (a) the muscovite-bearing quartzite (sample CN09-4), (b) the K-feldspar leptynite (sample CN07-27-1) and (c) the mica quartz schist (sample CN096) rock abbreviations: K – kimberlite; C – carbonatite; Syn – Syenite; Ne-S – Ne-syenite, SP – syenite pegmatites; B – basalt; S/M – syenite/monzonite; Dor – dolerite; G1 – granitoid (<65% SiO2); G2 – granitoid (70–75% SiO2); G3 – granitoid (>75% SiO2).

doleritic and low-SiO2 granitic rocks (Fig. 15). Most of the detrital zircons from each of the three units have positive eHf(t) values (Supplementary Data Tables 6–8, Fig. 16), suggesting involvement of juvenile materials in the formation of their parental magmas. The age spectra show some differences for the detrital zircons from the North, Middle and South units, indicating compositional changes of the source rocks in the provenances. The zircon age spectrum for the North unit (sample CN09-4) displays a remarkable major peak at 2.38 Ga and two very minor peaks at 2.45 Ga and 2.24 Ga (Fig. 10b), suggesting that the sediments were mainly derived from a provenance dominated by rocks of 2.38 Ga, with minor 2.45 Ga and 2.24 Ga magmatic rocks. However, previous data indicate two age peaks at 2.45 Ga and 2.24 Ga for detrital zircons from a quartzite near the Middle unit (see Fig. 3, sample CN07-1), suggesting that more sediments came from the 2.45 Ga and 2.24 Ga magmatic rocks (Chen et al., 2012). The zircon ages for the Middle unit cluster at 2.07–2.28 Ga, with a mono-peak at 2.17 Ga (Fig. 10d), indicating that most of their sediments were derived from around 2.17 Ga magmatic rocks. The zircon age spectrum for the South unit show a major peak at 2.45 Ga, a minor peak at 2.38 Ga and a very small peak at 2.20 Ga (Fig. 10f), implying that most of their sediments were sourced from major 2.45 Ga with minor 2.38 Ga and 2.20 Ga magmatic

sources. In brief, the preservation of minor detrital rock-making minerals, whole-rock trace element geochemistry and isotopic compositions and trace elemental geochemistry of the detrital zircons suggest that the protolith sediments for the Delingha paragneiss suite were derived from sources of acidic arc or continental margin composed of granite, felsic volcanic rocks and TTG which were dominantly formed at 2.20–2.45 Ga. In the study area, the Delingha Complex is composed of metamorphosed 2.37–2.39 Ga and minor 2.2 Ga quartz-diorite, monzonitic granite and alkali-feldspar granite (Lu et al., 2002; Lu et al., 2006a, 2008a; Ba et al., 2012; Gong et al., 2012, 2014). Whole-rock Sm–Nd and zircon Hf isotopes indicate clear involvement of juvenile materials in the granitoid magma source, as evidenced by high positive eNd(t) and eHf(t) values (e.g. Chen et al., 2007b; Gong et al., 2012, 2014). Major inputs of depleted mantle materials into the continental crust and the crustal growth events have been constrained to at 2.5 Ga and 2.7 Ga in the QM (Gong et al., 2012, 2014). In addition, the paragneisses of the LDG contain detrital zircons with ages clustering from 2400 Ma to 2560 Ma, and the relative probability plot of 207Pb/206Pb ages for those with concordance higher than 95% shows a remarkable age peak at 2.47 Ga. On the other hand, most detrital zircons possess positive eHf(t) values with a main peak at  +4.5 and TDM2 peaks at  2.71 Ga and 2.45 Ga, supporting the important crustal growth events at 2.45–2.71 Ga (Chen et al., 2012). The isotopic data from the Delingha paragneiss suite show juvenile crustal input during 2.5–2.9 Ga, covering the crustal growth period suggested by Hf isotopes, but the negative eNd(t) values ( 1.48 to +5.93) suggest metamorphic reworking at 1.92 Ga. Therefore, the timing and nature of both the magmatic and crustal growth events recorded in the granitoids of the DC and the LDG clearly overlap with those of the Delingha paragneiss suite, suggesting that the underlying DC and LDG might be one of the potential provenances for the source materials of the protoliths of the Delingha paragneiss suite. Existence of the detrital feldspars in the different rocks suggests short-distant transportation and thus nearby provenance for the deposits of the protolith of the Dalingha paragneiss suite.

6.3. Tectonic setting for the source rocks

Fig. 16. eHf (t) vs. 207Pb/206Pb age diagram for the detrital zircons from the Delingha khondalite, showing signatures about input of juvenile material. Also shown are those data reported by Chen et al. (2012).

High field strength elements (HFSE) such as Nb, Ta, Zr, Hf, Th, REE and transition elements Ti, V, Cr, Fe, Co and Ni remain largely immobile during closed-system metamorphism and thus provide a useful tool in determining the protoliths of rocks that have undergone metamorphism up to the upper amphibolite facies

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conditions, as well as in evaluating lower crustal anatexis (e.g. Cullers et al., 1974; Muecke et al., 1979). Immobile trace elements such as La, Th, Y, Zr, Ti, Co and Ni and ratios of Zr/Hf, Eu/Eu*, Ta/ Nb, La/Sc and Th/U etc. scarcely change during erosion and transportation, and are therefore useful tracers for unraveling tectonic settings for the sediments (Bhatia, 1985; Bhatia and Crook, 1986; Crichton and Condie, 1993). Systematic study of immobile trace elements in sandstones from sedimentary basins with different tectonic settings provided a set of discrimination schemes to understand tectonic settings such as oceanic arcs, continental arcs, active continental margins and passive continental margins (Bhatia, 1983, 1985; Bhatia and Crook. 1986). In discrimination diagrams of Th–Co–Zr/10 and Th–Sc–Zr/10, most of the feldspar gneiss, leptynite and mica schist samples are plotted within continental arc and active continental margin domains (Fig. 17); a similar result is also shown by La/Th vs. Hf plot (Fig. 14a). However, two essential constraints should be considered when applying trace elements to discriminate tectonic settings of the sedimentary basin with regard to the discrimination diagrams proposed by Bhatia (1983, 1985). The first is that transport of the materials to the sedimentary basins must be straight forward in order to exclude changes in the original compositions due to differentiation and mixing; the second is that the deposits must be generated synchronously or closely with formation and development of the basins. Short-distance transportation of the protolith materials of the Delingha paragneiss suite may help them to preserve original compositions. The younger U–Pb age population of 2.17 Ga for the detrital zircons from sample CN07-27-1 of this study and the metamorphic age of 1.92 Ga for the anatectic zircons reported by Wang et al. (2008) well constrain formation of the sedimentary basin and deposits of part of the sediments occurring at 1.92–2.17 Ga (Fig. 10c and d). However, as mentioned above, the protolith sediments for the Delingha paragneiss suite were dominantly sourced from 2.20 to 2.45 Ga granite and felsic volcanic rocks as well as TTG, which are obviously older and thus cannot represent the tectonic setting of the sedimentary basin. Therefore continental island arc or active continental margin setting would fit well for the generation of the magmas of the granite, felsic volcanic rocks and TTG, which later became the source rocks, rather than the sedimentary basin for the deposition of the protolith materials of the Delingha paragneiss suite. Further investigations are required for understanding the tectonic settings for the sedimentary basin of the protolith of the Delingha paragneiss (khondalite) suite. 6.4. Comparison with the khondalite suite in the Western Block, North Western China The QM is separated from the Ordos Block within the unified Western Block of the NCC (including the Alxa block) by the early

Paleozoic Qilian Orogenic belt (e.g. Lu et al., 2009; Zhang et al., 2013) (Fig. 1). A khondalite belt is exposed on the northwestern margin of the Ordos Block (e.g. Qian et al., 1985; Condie et al., 1992; Lu et al., 1992; Zhao et al., 2005; Yin et al., 2009, 2011; Zhai and Santosh, 2011; Santosh et al., 2012). The protolith of this khondalite suite has been previously considered to be deposited in passive continental margins (e.g. Qian et al., 1985; Lu et al., 1992) and broadly considered to be formed at 2.3–1.95 Ga (Wan et al., 2006b; Xia et al., 2006a,b; Dong et al., 2007; Xia et al., 2008, 2009; Yin et al., 2009, 2011; Li et al., 2011; Zhao and Zhai, 2013). However, a recent study of the khondalite suggested that part of their protolith was derived from 2.18 to 2.0 Ga continental arc based on their eHf(t) values (+8.9 to 2.9) (Dan et al., 2012). The khondalite suite was subjected to strong regional metamorphism during the collision of the Ordos Block with the Yinshan Block along the Inner Mongolia Suture Zone to form the Western Block of NCC at 2.0–1.9 Ga and 1.85–1.80 Ga (e.g. Geng et al., 2006, 2007, 2010; Wan et al., 2006b; Xia et al., 2006a,b; Zhai et al., 2005; Zhai and Peng, 2007; Zhai and Santosh, 2011; Dong et al., 2007; Xia et al., 2008, 2009; Yin et al., 2009; Li et al., 2011; Yin et al., 2011; Dan et al., 2012; Santosh et al., 2012), indicating that the khondalites underwent the same metamorphic processes with those within the Trans-North China Orogen (Guo et al., 1993; Mao et al., 1999; Zhao et al., 1999a,b,c, 2001, 2002, 2005, 2010; Guo and Zhai, 2001; Wang et al., 2001; Zhao, 2001; Wilde et al., 2002; Guo et al., 2005; Kröner et al., 2005, 2006; O’Brien et al., 2005; Liu et al., 2006; Faure et al., 2007; Xiao et al., 2011; Zhai and Santosh, 2011; Wan et al., 2013; Dan et al., 2012; Lu et al., 2013; Zhao and Zhai, 2013). The protolith sediments of the Delingha paragneiss suite were sourced from 2.20 to 2.45 Ga arc- or active margin-related magmatic rocks and deposited at 1.92–2.17 Ga (Fig. 10d), with subsequent regional metamorphic events at 1.90–1.92 Ga and 1.80–1.85 Ga (e.g. Wang et al., 2008; Lu et al., 2008b; Zhang et al., 2011; Chen et al., 2009, 2013). There is a broad similarity in the nature of the source rocks, formation and tectonothermal history of the Delingha paragneiss suite to those of the khondalite suite along the northern margin of the Ordos Block mentioned above, suggesting that the QM probably shared a similar tectonic history to the Western Block of the NCC in period of 2.4–1.8 Ga. 6.5. Tectonic implications Recent studies on supercontinents proposed that the first coherent supercontinent on the globe, termed Columbia, was assembled during 2.2–1.8 Ga (Rogers, 1996; Hoffman, 1997; Meert, 2002, 2012; Rogers and Santosh, 2002, 2003, 2009; Bleeker, 2003; Zhao et al., 2002, 2004; Roberts, 2013; Nancea et al., 2014). The North China and Tarim Cratons are considered

Fig. 17. Th–Co–Zr/10 and Th–Sc–Zr/10 plots for discriminating tectonic setting for deposit basin of the Delingha khondalite protolith (after Bhatia and Crook, 1986). Tectonic settings: A – oceanic island arc, B – continental island arc, C – active continental margin, D – passive continental margin. Symbols are as those in Fig. 11.

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L. Zhang et al. / Journal of Asian Earth Sciences xxx (2014) xxx–xxx

to have been part of the Columbia supercontinent (Zhao et al., 2004; Santosh, 2010). However, the tectonic evolution of the NW China before final amalgamation of the NCC and assembly of the TC with its surrounding micro-blocks or micro-massifs are still debated. Zhao and Zhai (2013, and the references therein) suggested that the unified NCC was formed through amalgamation of the Yinshan Block with Ordos Block to form the Western Block at 1.95 Ga, then final assembly of the Western Block with the Eastern Block (including the Langlin Block) occurred at 1.85 Ga, of which the assembly of the Western and Eastern Blocks is considered to have witnessed prolonged subduction and accretion prior to the final collision at ca. 1.85 Ga (Zhao et al., 2005; Santosh et al., 2012). However, Kusky and Li (2003) considered that the NCC was initially formed by the collision of the Eastern Block with the Western Block (i.e. the Ordos Block) along the Archean Central China Orogen at the end of the Neoarchean, and then collided with the Yinshan Block to form the coherent NCC along the Inner Mongolia–North Hebei Orogen at 1.9–1.80 Ga. Another model also considered that the coherent NCC was formed at 2.5 Ga ago, and then broke up into several micro-blocks during continental rifting along the Fengzhen belt, Jin-Ji-Yu belt and Liao-Ji belt (Zhai and Santosh, 2011 and references therein). Since 2.2 Ga, subduction and accretion along these belts resulted in collision of these rifted microblocks, forming the coherent NCC at 1.85–1.80 Ga (Zhai and Santosh, 2011). A newly proposed model suggests that the NCC was formed via double-side subduction-accretion-collision with welding of the Yinshan and Ordos Blocks along the Inner Mongolia Suture Zone (incorporating the Khondalite belt) and the unified Western and Eastern Blocks along the Trans-North China Orogen through a prolonged subduction-accretion process from ca. 2.5 Ga to 1.80 Ga (Zhao, 2001; Santosh, 2010; Santosh et al., 2010, 2013, and the references therein). Recent studies also suggested a prolonged subduction, accretion and collision history for the assembly of TC and its surrounding micro-blocks or micro-massifs along with incorporation into the Columbia supercontinent, based on the various tectonothermal events (Fig. 1; Chen et al., 2013; Ge et al., 2013; Ma et al., 2013). Subduction of oceanic crust southwards beneath the TC through a long time span of 2.5–1.90 Ga defines the first stage, and collision of the TC with an unknown continent at 1.83–1.80 Ga marks the second stage as suggested by Ma et al. (2013). Along the southeastern margin of the TC, Xin et al. (2011, 2012) reported arc-related 2.14–2.05 Ga magmatism and 2.02–1.92 Ga collisional metamorphism in the Aktasgitag region, and Zhang et al. (2013) reported 1.82–1.85 Ga high-pressure granulite-facies metamorphism, and a 2.5 Ga metamorphic in the Dunhuang region. These results suggest that a long-lived subduction, accretion and collision history at 2.5–1.8 Ga might have also prevailed along the southeastern margin (probably including the southwestern margin). Amalgamation of the QM with other continental blocks in the Paleoproterozoic was recognized to mark a complex history of subduction, accretion and collision as evidenced by the tectonothermal events (e.g. Lu, 2002; Wang et al., 2008; Chen et al., 2009; Zhang et al., 2011). Based on new age data from metamorphic zircons, Chen et al. (2013) identified two metamorphic events and mafic magmatism which can be linked to the subduction-accretioncollision process, with the first stage at 1.95–1.90 Ga and the second at 1.82–1.80 Ga along the southeast margin of the TC. Liao et al. (2014) provided new information further supporting oceanic crust subduction during 1.85–1.83 Ga through study of whole-rock geochemistry and zircon U–Pb age and Lu–Hf isotopes on mafic dykes. Our present study indicates that the protolith materials of the Delingha paragneiss suite were sourced mostly from 2.2 to 2.45 Ga magmatic rocks, including granites, felsic volcanic rocks and TTG. These source rocks were generated in an island arc or

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active continental margin, thus suggesting subduction of oceanic lithosphere beneath the QM during the early Paleoproterozoic. Global magmatic activity is characterized by episodic pulses of enhanced activity (Kemp et al., 2006; Campbell and Allen, 2008; Condie et al., 2009a). However, statistical calculations from orogenic granite and detrital zircons from ancient and modern sediments reveals an early Proterozoic global age trough between 2450 and 2200 Ma (Rino et al., 2004, 2008; Condie et al., 2005, 2009a; Condie et al., 2009b; Campbell and Allen, 2008; Belousova et al., 2010; Condie and Aster, 2010; Safonova et al., 2010; Wang et al., 2010), during which activity of magmatism was low. Condie and Aster (2010) use a plate subduction shutdown or slowdown theory (O’Neill et al., 2007; Silver and Behn, 2008) to interpret this global trend, considering that it is probably related to the rifting events of the Kenorland supercontinent at the end of the Neoarchean (Williams et al., 1991; Bleeker, 2003; Rogers and Santosh, 2004). Previous studies revealed that a prolonged subduction-accretion-collision process occurred during assembly of the NCC during 2.5–1.80 Ga (Santosh, 2010; Santosh et al., 2010, 2013, and the references therein). A similar prolonged history is also documented along the northern and southern margins of the TC (Chen et al., 2013; Ge et al., 2013; Ma et al., 2013; Liao et al., 2014). The TTG, granites and felsic volcanic rocks formed at 2.2–2.45 Ga are suggested as the source rocks for the protolith of the Delingha paragneiss suite in our study. These rocks are also widely exposed in the Trans-North China Orogen and in the Western Block of the NCC as well as in the TC. This might suggest that an active subduction-accretion-collision tectonics prevailed in the North China Craton when there was global shutdown or slowdown of magmatism during the early Paleoproterozoic. 7. Conclusions Comprehensive studies on lithological association, petrography and geochemistry of a typical paragneiss suite from Delingha in the Quanji Massif, constrain the nature of the protoliths, source rocks, provenances and tectonic settings, and thus offer a better understanding of the Precambrian evolution of the Quanji Massif and NW China. The Delingha paragneisses represent a khondalite suite. Their protolith materials came from an interior basement provenance, mainly sourced from 2.37 to 2.39 Ga and 2.2 Ga granitoids of the Delingha Complex and the lower Dakendaban sub-Group. The magmas of these source rocks were generated in a continental island arc or active continental margin setting. The protolith materials of the Delingha paragneiss suite were deposited at 2.17–1.92 Ga. The Delingha paragneiss suite is comparable to the khondalites along Inner Mongolia Suture zone, which welded the Ordos and Yinshan Blocks to form a unified Western Block of the NCC. The Quanji Massif probably shared a similar history with the Tarim Craton and the North China Craton during the Early Paleoproterozoic, and together underwent subduction-accretion tectonics at 2.2–2.45 Ga in NW China, indicating an active tectonic evolution as against the plate subduction shutdown or slowdown worldwide during the early Paleoproterozoic period. Acknowledgements We thank the Guest Editor and two anonymous referees for their helpful comments and suggestions. This study was supported by the National Science Foundation of China, NSFC Grants (Nos. 41172069, 41372075, 40972042 and 41273048) and a HKU CRCG Grant. This study is a contribution to the 1000 Talents Award to M. Santosh from the Chinese Government and to the Joint Laboratory of Chemical Geodynamics between HKU and CAS (Guangzhou Institute of Geochemistry).

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Please cite this article in press as: Zhang, L., et al. Geochemistry and detrital zircon U–Pb and Hf isotopes of the paragneiss suite from the Quanji massif, SE Tarim Craton: Implications for Paleoproterozoic tectonics in NW China. Journal of Asian Earth Sciences (2014), http://dx.doi.org/10.1016/ j.jseaes.2014.05.014