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International Geology Review

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Petrogenesis of early Silurian intrusions in theSanchakou area of Eastern Tianshan, NorthwestChina, and tectonic implications: geochronological,geochemical, and Hf isotopic evidence

Yin-Hong Wang & Fang-Fang Zhang

To cite this article: Yin-Hong Wang & Fang-Fang Zhang (2016) Petrogenesis of early Silurianintrusions in the Sanchakou area of Eastern Tianshan, Northwest China, and tectonicimplications: geochronological, geochemical, and Hf isotopic evidence, International GeologyReview, 58:10, 1294-1310, DOI: 10.1080/00206814.2016.1152516

To link to this article: http://dx.doi.org/10.1080/00206814.2016.1152516

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Petrogenesis of early Silurian intrusions in the Sanchakou area of EasternTianshan, Northwest China, and tectonic implications: geochronological,geochemical, and Hf isotopic evidenceYin-Hong Wang and Fang-Fang Zhang

State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Beijing, China

ABSTRACTPalaeozoic intrusions in Eastern Tianshan are important for understanding the evolution of theCentral Asian Orogenic Belt (CAOB). The Sanchakou intrusions situated in Eastern Tianshan(southern CAOB), are mainly quartz diorite and granodiorite. A comprehensive study of zirconU–Pb ages, zircon trace elements, whole-rock geochemistry, and Lu–Hf isotopes were carried outfor the Sanchakou intrusive rocks. LA-ICP-MS zircon U–Pb dating yielded crystallization ages of439.7 ± 2.5 Ma (MSWD = 0.63, n = 21) for the quartz diorite, and 430.9 ± 2.5 Ma (MSWD = 0.21,n = 21) and 425.5 ± 2.7 Ma (MSWD = 0.04; n = 20) for the granodiorites. These data, incombination with other Silurian ages reported for the intrusive suites from Eastern Tianshan,indicate an early Palaeozoic magmatic event in the orogen. In situ zircon Hf isotope data for theSanchakou quartz diorite shows εHf(t) values of +11.2 to +19.6, and the two granodioritic samplesexhibit similar εHf(t) values from +13.0 to +19.5. The Sanchakou plutons show metaluminous toweakly peraluminous, arc-type geochemical and low-K tholeiite affinities, and display traceelement patterns characterized by enrichment in K, Ba, Sr, and Sm, and depletion in Nb, Ta, Pb,and Ti. The geochemical and isotopic signatures indicate that the Sanchakou dioritic and grano-dioritic magmas were sourced from a subducted oceanic slab, and subsequently underwent someinteraction with peridotite in the mantle wedge. Combined with the regional geological history,we suggest the Sanchakou intrusions formed due to the northward subduction of the Palaeo-Tianshan Ocean beneath the Dananhu–Tousuquan arc during early Silurian time.

ARTICLE HISTORYReceived 14 December 2015Accepted 6 February 2016

KEYWORDSearly Silurian intrusions;zircon U–Pb geochronology;geochemistry; zircon Hfisotope; Sanchakou area;Eastern Tianshan

1. Introduction

The Central Asian Orogenic Belt (CAOB), one of the lar-gest Phanerozoic accretionary orogens in the world(Goldfarb et al. 2001, 2014; Windley et al. 2007;Safonova 2009; Xiao et al. 2013; Deng et al. 2014a;Deng and Wang 2015; Wang et al. 2015c, 2015d), formedby multiple accretionary and collisional events thatoccurred from early Neoproterozoic to Permian timeand were driven by the successive closure of thePalaeo-Asian Ocean (Şengör et al. 1993; Jahn 2004; Xiaoet al. 2010; Deng et al. 2014b, 2015; Shen et al. 2014;Zhang et al. 2016b). The Eastern Tianshan orogenic beltin Northwest China lies along the southern margin of theCAOB (Figure 1A and B) and contains widespreadPalaeozoic intermediate-felsic intrusions (Mao et al.2005; Charvet et al. 2007; Zhou et al. 2010; Pirajno2013; Wang et al. 2014, 2016; Xiao et al. 2015). Theseintrusions are of considerable geological interest, notonly because they are spatially and genetically associated

with numerous metal deposits, especially porphyry sys-tems, such as the Tuwu–Yandong Cu deposits (Shen et al.2014; Wang et al. 2015a, 2015b), Chihu Cu deposit(Zhang et al. 2016a), Sanchakou Cu deposit (Qin et al.2009), and Yuhai Cu deposit (Zang 2014), but alsobecause they offer an opportunity to unravel themechanism of magma formation and geodynamic evolu-tion of the Eastern Tianshan orogenic belt.

In the past decades, numerous studies have examinedlate Palaeozoic magmatic rocks in the Eastern Tianshanorogenic belt (Mao et al. 2008; Pirajno et al. 2011; Chenet al. 2012a; Wang et al. 2015c), exemplified by Tuwu,Yandong, Chihu, and Linglong felsic intrusions, andHuangshan and Xiangshan mafic intrusions, which wereinterpreted to have formed in subduction arc and post-collisional settings, respectively (Qin et al. 2009, 2011; Suet al. 2012; Shen et al. 2014; Wang et al. 2015a, 2015b;Zhang et al. 2016a). However, less attention has beenpaid to the early Palaeozoic igneous rocks in this orogenic

CONTACT Yin-Hong Wang wyh@cugb.edu.cn State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences,Beijing 100083, China

Supplemental data for this article can be accessed here.

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belt. There is no consensus for the regional geologicalhistory, magmatic activities, and associated mineralization(Rui et al. 2002; Gu et al. 2006; Han et al. 2006; Li et al.2006; Chen et al. 2011; Pirajno 2013; Zang 2014), largelyrelated to a lack of geochronological and geochemicaldata on early Palaeozoic igneous rocks. The Sanchakouarea, located within eastern part of the Eastern Tianshan,is an ideal area to investigate the geodynamic processesof early Palaeozoic magmatic activity, because of its link-age to the Dananhu–Tousuquan arc and the Kanggur–Huangshan ductile shear zone (Figure 1C). To date, littleresearch has been undertaken on the Sanchakou area,which precludes a comprehensive understanding of thepetrogenesis and its relationship to Cu mineralization.Here, we present new LA-ICP-MS zircon U–Pb dating,whole-rock geochemical data, and zircon trace elementand Hf isotopic compositions of the Sanchakou quartzdiorite and granodiorite in an attempt to better constrainthe timing of magmatic activities, the petrogenesis ofthese intrusions, and the geodynamic setting of earlySilurian magmatism in Eastern Tianshan orogenic beltand elsewhere in CAOB.

2. Geological setting

The Eastern Tianshan orogenic belt is an approximately300 km wide collage bounded by the Junggar Basin to

the north and the Tarim Basin to the south (Figure 1B;Chen et al. 2012b), and can be divided into the Bogeda–Haerlike belt, the Jueluotage belt, and the CentralTianshan Terrane from north to south (Figure 1C;Pirajno et al. 2011; Chen et al. 2012b; Xiao et al. 2013),with a series of approximately E–W-trending regional-scale faults defining the boundaries, including theDacaotan, Kanggur, Yamansu, and Aqikuduke faults,and some small-scale faults (Figure 1C; Mao et al.2005, 2008; Chen et al. 2012a; Huang et al. 2013).

The Jueluotage belt may be subdivided into theDananhu–Tousuquan arc belt, the Kanggur–Huangshan ductile shear zone, and the Aqishan–Yamansu arc belt, which are separated by the Kanggurand Yamansu faults (Figure 1C). The Dananhu–Tousuquan arc belt is mainly composed of Devonianvolcanic and clastic sedimentary rocks of the DananhuFormation; Carboniferous turbidites of the GandunFormation; Carboniferous basaltic to andesitic volcanicand sedimentary rocks of the Qi’eshan Group; Permiancalc-alkaline volcanic, pyroclastic, and clastic rocks;Jurassic sandstone; and Cenozoic cover (Zhou et al.2008, 2010; Shen et al. 2014; Xiao et al. 2015).Intrusions were widely emplaced in the arc during theDevonian to Carboniferous, associated with severalimportant porphyry Cu deposits of different sizes,including the Tuwu, Yandong, Linglong, Chihu, and

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Figure 1. (A) Location of the study area in the Central Asian Orogenic Belt (modified from Jahn et al. 2000); (B) sketch map showinggeologic units of the Tianshan Belt (modified from Chen et al. 2012b); (C) simplified geological map of the Eastern Tianshan Belt(modified from Huang et al. 2013). Isotopic age data from Shu et al. (1999, 2004), Li and Chen (2004), Wang et al. (2005, 2015a,2015b, 2015c, 2015f, 2016), Zhang et al. (2005), Wu et al. (2006a), Zhou et al. (2010), He et al. (2012), Lei et al. (2014), Zang (2014),and this study.

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Fuxing deposits (Figure 1C). The middle Kanggur–Huangshan ductile shear zone is mainly composed ofDevonian–Carboniferous volcaniclastic rocks, basalt,tuff, limestone, sandstone, and ophiolitic slice (Maoet al. 2008; Zhang et al. 2008; Xiao et al. 2010).Permian mafic and ultramafic intrusions (e.g.Xiangshan, Huangshandong, Huangshan, and Hulu) arecommon within the eastern Kanggur–Huangshan duc-tile shear zone (Han et al. 2006; Qin et al. 2011; Zhanget al. 2015a). The Aqishan–Yamansu arc belt is com-posed of early Carboniferous basalt, andesite, dacite,and tuff of the Yamansu Formation and lateCarboniferous rhyolite of the Tugutubulake Formation(Chen et al. 2012a; Xiao et al. 2013; Hou et al. 2014).Numerous arc-related late Palaeozoic granitoids intrudethis belt (Wang et al. 2005; Wu et al. 2006a; Zhou et al.2010; Zhang et al. 2015a), including the Weiquan gran-odiorite (297 ± 3 Ma), Bailingshan granodiorite(317.7 ± 3.7 Ma), Hongyuntan granodiorite(328.5 ± 9.3 Ma), and Xifengshan granite (349 ± 3.4 Ma).

The Sanchakou pluton is situated in the easternDananhu–Tousuquan arc belt, approximately 120 kmsoutheast of Hami City, Xinjiang (Figure 1C). The mainlithostratigraphic units in the Sanchakou area include:the lower Carboniferous Gandun Formation, consistingof turbidites, argillaceous slate and siltstone intercalatedwith lithic sandstone; lower Carboniferous WutongwoziFormation spilite–keratophyric series; and the overlyingMiocene Taoshuyuan Formation and Quaternary sedi-ments (Qin et al. 2009; Wang et al. 2015f). The majorstructures in the Sanchakou pluton are NE-trendingductile shear faults that are related to the Kanggur–Huangshan ductile shear zone, whereas NW- and NE-trending structures are also present within the area(Figure 2; Li et al. 2004; Lang et al. 1992). These well-developed faults control the distribution of major strata

and intrusive rocks at Sanchakou. The intrusions gener-ally occur as stocks or dikes with an outcrop area ofapproximately 65 km2 (Figure 2; Li et al. 2004; Qin et al.2009), and are mainly composed of diorite and grano-diorite (Figure 3A and B), with minor gabbro, tonalite,muscovite granite, and alkali-feldspar granitic rocks. Thequartz diorite and granodiorite host most of the Cumineralization (Figure 4A–C). The ore minerals atSanchakou are dominated by chalcopyrite and bornite(Figure 4D), accompanied by minor pyrite, molybdenite,and chalcocite. Chalcopyrite generally is disseminated(Figure 4A) or cloddy (Figure 4B and C) structure in theore-hosting intrusive rocks. The main gangue mineralsconsist of quartz, biotite, K-feldspar, sericite, with minorchlorite, epidote, and calcite.

3. Samples and petrology

Eleven least altered samples of quartz diorite and grano-diorite were collected from outcrops or from the open pitmine for LA-ICP-MS zircon U–Pb dating, whole-rock majorand trace element compositions, and in situ Hf isotopicand whole-rock geochemical analyses; sampling locationsare shown in Figure 2. Quartz diorite shows light greycolour and displays medium-grained texture (Figure 3A).It exhibitsmassive structure, consisting of plagioclase (~50vol. %), hornblende (~ 20 vol. %), biotite (~15 vol. %),quartz (~10 vol. %), and K-feldspar (~5 vol. %) (Figure 5),with accessory magnetite, apatite, and zircon. Plagioclaseis characterized by a hypidiomorphic, tabular texture withpolysynthetic twinning (Figure 3C). Hornblende is domi-nated by a xenomorphic tabular texture, and biotiteshows hypidiomorphic–xenomorphic flaky or fragmentaltexture. Granodiorite is light grey to grey-white and showsmedium-coarse grain texture and massive structure(Figure 3B). The rock is primarily composed of plagioclase

Alkali-feldspargranite

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Figure 2. Simplified geological map of the Sanchakou intrusions (modified from Sun et al. 2009).

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(~40 vol. %), quartz (~25 vol. %), K-feldspar (~15 vol. %),hornblende (~10 vol. %), and biotite (~5 vol. %) (Figure 5),with accessory magnetite, apatite, and zircon. Plagioclasegenerally appears as hypidiomorphic–xenomorphic board(Figure 3D). Hornblende is characterized by hypidio-morphic, tabular texture, and quartz is characterized byxenomorphic granular texture with weak silicification.

4. Analytical methods

Zircons were separated from dioritic and granodioriticsamples using conventional heavy liquids, magneticseparation techniques, and handpicking under a bino-cular microscope at the Langfang Regional GeologicalSurvey in Hebei Province, China. The zircons were thenmounted in epoxy before polishing with a diamond

Figure 3. Representative photographs and photomicrographs showing mineral compositions of the Sanchakou intrusions. (A) Handspecimen of quartz diorite; (B) hand specimen of granodiorite; (C) microphotograph of quartz diorite, composed of quartz, biotite,hornblende, and plagioclase, under crossed-polarized light; (D) microphotograph of medium grain granodiorite, mainly composed ofplagioclase, quartz, biotite, and hornblende, under crossed-polarized light. Abbreviations: Q, quartz; Bt, biotite; Pl, plagioclase; Hb,hornblende; Kf, K-feldspar.

Figure 4. Photographs and photomicrographs showing ore fabrics and mineral assemblages of the Sanchakou Cu deposit. (A)Chalcopyrite and bornite assemblages in quartz diorite; (B) cloddy chalcopyrite in granodiorite; (C) cloddy chalcopyrite and bornite inalerted quartz diorite; (D) subhedral chalcopyrite and bornite assemblages, reflected right. Abbreviations: Cp, chalcopyrite; Bn, bornite.

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compound to reveal the internal structures. To charac-terize the internal structures of the zircons and selectpotential sites for U–Pb dating, cathodoluminescence(CL) images were collected using a CL spectrometer(Garton Mono CL3+) attached to a Quanta 200 F ESEMwith a scanning time of 2 min under operating condi-tions of 15 kV and 120 nA. The instruments are housedat Peking University, Beijing, China. Based on the CLimages, we selected zircons that were transparent,unfractured, and inclusion-free for isotopic analyses.

LA-ICP-MS zircon U–Pb dating and trace element ana-lyses were synchronously conducted on an Agilent 7500aICP-MS, equipped with a 193 nm laser ablation system,housed at the State Key Laboratory of Geological Processand Mineral Resources of the China University ofGeosciences, Beijing. During the analyses, the laser spotwas 10 or 23 μm in different samples. The 207Pb/206Pband 206Pb/238U ratios were calculated using the GLITTERprogram, and then corrected using zircon TEMORA-1 asan external standard. The detailed analytical proceduresare similar to those described by Yuan et al. (2004) andWu et al. (2006b). Error on individual analysis by LA-ICP-MS is quoted at the 1σ confidence level. The results wereprocessed using ISOPLOT software (Ludwig 2003).

Major and trace element analyses of the dioritic andgranodioritic samples were conducted at the test centreof the Beijing Research Institute of Uranium Geology.The samples were chipped and powdered to about 200mesh for major and trace element analyses. Major ele-ments were determined by a Philips PW 2404 X-rayfluorescence (XRF) spectrometer with a rhodium X-raysource. The testing precision was better than 1%, and

the detailed analytical procedures were after Norrishand Hutton (1969). Sample powders for trace elementanalyses were accurately weighed (25 mg) into Savillexteflon beakers within a high-pressure bomb, and thendigested using HF + HNO3 + HClO4 acid to assurecomplete dissolution of refractory minerals. Trace ele-ments, including rare earth elements, were determinedusing an Element-I plasma mass spectrometer(Finnigan-MAT Ltd. German), and national geologicalstandard reference samples GSR-3 and GSR-15 wereused for analytical quality control. The analytical preci-sion for trace elements was better than 5%, and theanalytical procedures were described by Qi et al. (2000).

In situ zircon Hf isotopic analyses were measured usinga Neptune MC-ICP-MS, equipped with a Geolas 193 nmlaser-ablation system at the Institute of Geology andGeophysics, Chinese Academy of Sciences, in Beijing. Lu–Hf isotope of zircons were acquired on the same spot as U−Pb ages with spot size of 60 μm and a 6 Hz pulsefrequency, and the international standard zircon sampleGJ-1 was used as a reference. Details on the instrumentalconditions and data acquisition were comprehensivelydescribed by Wu et al. (2006b). In order to correct theisobaric interferences of 176Lu and 176Yb on 176Hf,176Lu/175Lu = 0.02658 and 176Yb/173Yb = 0.796218 (Chuet al. 2002) ratios were assumed. Zircon GJ-1 was used asthe reference standard and yielded a weighted average176Hf/177Hf ratio of 0.282006 ± 0.000006 and 176Lu/177Hfratio 0.00024 (2σ, n = 71). The initial 176Lu/177Hf ratios werecalculated by using a decay constant of 1.867 × 10−11

year−1 for 176Lu (Söderlund et al. 2004). The chondriticvalues of the 176Lu/177Hf ratio of 0.0332 and 176Hf/177Hfratio of 0.282772 (Blichert-Toft and Albarède 1997) wereadopted to calculate the εHf(t) values. The TDM (depletedmantle model age) was measured in reference to thedepleted mantle at a present-day 176Lu/177Hf ratio of0.0384 and 176Hf/177Hf ratio of 0.28325 (Griffin et al.2002). The TDM

c (crustal model age) was calculated usingan average continental crustal 176Lu/177Hf ratio of 0.015(Griffin et al. 2002).

5. Result

5.1. Zircon U–Pb ages

The analytical results of three samples from theSanchakou quartz diorites and granodiorites are listedin Supplementary Table 1 (see http://dx.doi.org/10.1080/00206814.2016.1152516 for supplementarytables), and representative zircon CL images are shownin Figure 6.

One sample SCK-3 of the Sanchakou quartz dioriteswas chosen for LA-ICP-MS zircon U–Pb dating and 25

Figure 5. QAP modal diagram showing the classification of theSanchakou intrusions (after Le Maitre 2002). Q, quartz; A, alkali-feldspar; P, plagioclase.

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zircon rims were dated. The zircon grains are euhedral-subhedral and show prismatic forms (150–230 μm long),with aspect ratios of 1:1 to 2:1, and exhibit well-devel-oped oscillatory zoning in CL images (Figure 6A). Exceptfor four discordant spots (05, 06, 22, and 23), theremaining 21 analyses from the quartz diorite sample(SCK-3) give concordant 206Pb/238U ages ranging from428 to 447 Ma, with a weighted mean age of439.7 ± 2.5 Ma (MSWD = 0.63; Figure 7A). The low U(37–506 ppm) and Th (10–228 ppm) contents, inte-grated with the internal structure and morphology ofthe zircons, suggest that the weighted mean age can beinterpreted as the magma emplacement age of thequartz diorite at Sanchakou.

Two samples of Sanchakou granodiorites, SCK-4 andSCK-2, were selected for LA-ICP-MS zircon U–Pb dating.Zircons from both samples are prismatic, euhedral, rangein length from 150 to 350 μm, with an aspect ratio of 2:1 to3:1, and display clear oscillatory zoning in CL images(Figure 6B and C). The U (29–452 ppm) and Th (7–448 ppm) contents, combined with the structural featuresin CL images, suggest these are typical magmatically crys-tallized zircon (Hoskin and Schaltegger 2003). Twenty-fivezircon grains from sample SCK-4 were analysed. Amongthese, 21 spot analyses show concordant ages from 426to 439 Ma with a weighted mean 206Pb/238U age of430.9 ± 2.5 Ma (MSWD = 0.21; Figure 7B), which is consid-ered to represent the crystallization age of the rock.Twenty-five zircons from the sample SCK-2 were also ana-lysed. Among these, 20 spot analyses are clustered around206Pb/238U ages in the range of 424–429 Ma, with an errorweighted mean age of 425.5 ± 2.7 Ma (MSWD = 0.04;Figure 7C), which also represents the crystallization age ofthe intrusion. Therefore, we suggest that the magmaemplacement of the Sanchakou granodiorites occurred atca. 431–426 Ma.

5.2. Zircon geochemistry and Ti-thermometry

Zircon grains from ca. 440 Ma quartz diorites displaypronounced light rare earth element (LREE) depletionwith LaN/YbN = 0.00003–0.00185, positive Ce anomalieswith Ce/Ce* = 3.70–93.31, but negative Eu anomalieswith Eu/Eu* = 0.52–0.80 (Figure 8A). They show variableSmN/LaN ratios ranging from 3 to 191, with La contents of0.03–1.84 and Th/U ratios of 0.22 to 0.45 (SupplementaryTables 2 and 1; see http://dx.doi.org/10.1080/00206814.2016.1152516 for supplementary tables). The Ti contentsin zircon grains are similar and vary from 3.78 to10.99 ppm (average 6.91 ppm). Zircon grains from ca.431–426 Ma granodiorites have similar chondrite normal-ized rare earth element (REE) patterns with significantheavy rare earth element (HREE) enrichments (LaN/YbN = 0.00001–0.00209), and show strong positive Ceanomalies (Ce/Ce* = 3.82–318.14) and negative Euanomalies (Eu/Eu* = 0.44–0.72) (Figure 8B and C), exceptfor one outlier of 1.10. The grains show highly variableSmN/LaN ratios of 10–2906, with La contents of 0.02–1.65and Th/U ratios of 0.22–1.10 (Supplementary Table 2).They exhibit relatively variable Ti contents ranging from3.96 to 77.35 ppm (average 9.74 ppm). The calculatedresults of Ti-in-zircon thermometer can be used to deter-mine the genetic setting of zircons (Fu et al. 2009;Watson et al. 2006). Calculated Ti-in-zircon thermometertemperatures vary from 662°C to 749°C (average 707°C,n = 25) in the quartz diorite, and 680–815°C (average730°C, n = 25) and 665°C to 959°C (average 720°C, n = 25)in the granodiorites (Supplementary Table 2). Magmaticzircons crystallize from ore-forming fluids at tempera-tures higher than 600°C (Fu et al. 2009; Wan et al.2012). Therefore, the high formation temperatures andTh/U ratios of zircons from the Sanchakou area can betaken as evidence for their crystallization from magmas.

Figure 6. Cathodoluminescence (CL) image of representative zircons from the Sanchakou quartz diorite and granodiorite intrusions.The circles indicate zircon U–Pb and Lu–Hf isotopic analyses. Apparent ages and εHf(t) values are also shown.

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5.3. Whole-rock major and trace elements

Whole-rock major-trace elements and rare earth ele-ments in eight representative samples, which includethree quartz diorites (SCK-5, SCK-8, and SCK-3) and fivegranodiorites (SCK-2, SCK-4, SCK-6, SCK-7, and SCK-9)are presented in Supplementary Table 3. These samplesplot in the diorite and granodiorite fields, respectively,on the Na2O + K2O vs. SiO2 diagram (Figure 9A; LeMaitre 2002).

Quartz diorite samples are characterized by inter-mediate SiO2 (61.57–63.50 wt.%), high MgO (1.93–1.98 wt.%), low K2O contents (0.20–0.56 wt.%)(Figure 9A), and A/CNK ratios (Al2O3/(CaO+Na2O+K2O),mole ratio) of 0.93–1.12. They also show low-K tholeiitecharacteristics with K2O/Na2O ratios ranging from 0.06to 0.15. The Mg# values [100 × molecular Mg2+/(Mg2+ +Fe2+)] of the quartz diorite samples vary from 36 to 44(Supplementary Table 3). Granodioritic samples displayslightly higher SiO2 (63.81–66.41 wt.%), MgO (1.30–2.03 wt.%), and low K2O contents (0.17–0.50 wt.%). Ona K2O vs. SiO2 diagram (Figure 9B; Rollinson 1993), allgranodioritic samples plot in the low-K tholeiite field.They have low A/CNK values in the range of 0.99–1.10,

Figure 8. Chondrite-normalized REE patterns for zircon grainsfrom the Sanchakou intrusions. Chondrite values are from Sunand McDonough (1989).

21Spots:Mean=439.7±2.5MaMSWD=0.63

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Figure 7. Concordia diagrams of zircon U–Pb ages for samplesSCK-3, SCK-4, and SCK-2 from the Sanchakou Cu deposit.

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indicating metaluminous to weakly peraluminous series(Maniar and Piccoli 1989).

The samples from the dioritic and granodioritic intru-sions have similar REE and trace element patterns(Figure 10A and B). In the chondrite-normalized REE dia-gram (Boynton 1984), the intrusive samples are character-ized by high concentrations of LREEs and low contents ofHREEs, with a clear LREE/HREE fractionation ((La/Yb)

N = 7.12–48.43), prominent LREE fractionation, and posi-tive Eu anomaly (Eu/Eu* = 0.98–1.61) (Figure 10A). In theN-MORB-normalized trace element spider diagram (Bevinset al. 1984), these rocks are characterized by distinctlynegative Nb, Ta, Th, Pb, and Ti anomalies, with positiveK, Ba, Sr, U, and Sm anomalies (Figure 10B).

5.4. Zircon Hf isotope

In situ Hf isotopic data for zircons from three samples ofSCK-3 (quartz diorite), SCK-4, and SCK-2 (granodiorite)are shown in Figure 11, and the zircon Hf isotopic dataand calculation results are listed in SupplementaryTable 4. Twenty-one zircon grains from sample SCK-3

(439.7 ± 2.5 Ma) were analysed for Hf isotopic composi-tions, and the results show 176Hf/177Hf ratios rangingfrom 0.282821 to 0.283068, 176Yb/176Hf ratios from0.017831 to 0.065735, and 176Lu/176Hf ratios from0.000849 to 0.002941. They have fLu/Hf in the range of

0

2

4

6

8

10

12

14

7540 45 50 55 60 65 70 80

)%(

OK

+O

aN

22

SiO (%)2

Quartzmonzonite

Gabbro Granodiorite

Monzonite Granite

Diorite

Gabbroicdiorite

Monzo-diorite

A

Syenite

Foidsyenite

Foidmonzosyenite

Foidmonzodiorite

Foidgabbro

Sub-alkalic

Alkalic

0

1

2

3

4

5

6

45 50 55 60 65 70 75 80

SiO2(%)

OK

2)

%(

Shoshoniticseries

Calc-alkaline seriesHigh-K calc alkaline series

-

B

Low-K tholeiite series

GranodioriteQuartz diorite

Figure 9. Classification of the Sanchakou intrusions. (A) Na2O+K2O vs. SiO2 diagram (Le Maitre 2002); (B) K2O vs. SiO2 diagram(Rollinson 1993).

A

100

101

102

103

La Ce Pr NdSmEu Gd Tb Dy Ho Er TmYb Lu

etirdnohC/elp

maS

B

BR

OM-

N/elpma

S

Rb Th K Ta Ce Sr P Hf Eu Gd Dy Ho

Ba U Nb La Pb Nd Zr Sm Ti Tb Y Er Yb

Lu

100

101

102

10-1

GranodioriteQuartz diorite

Tm

GranodioriteQuartz diorite

Figure 10. Chondrite-normalized REE (A) and N-MORB-normalized trace element abundance spider diagram (B) for the Sanchakouintrusions. Chondrite normalizing values are taken from Boynton (1984); N-MORB normalizing values are taken from Bevins et al.(1984).

Figure 11. Correlation diagrams of zircon Hf isotopes versus U−Pb ages of the Tianshan intrusions. Data for the Tianshanintrusions are from Wang et al. (2015a, 2015b), and Zhaoet al. (2015).

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−0.97 to −0.91, with an average of −0.95. The positiveεHf(t) values of zircons and Hf isotopic crustal modelages (TDM

C) vary from +11.2 to +19.6, and from 173 to709 Ma, respectively (Supplementary Table 4; Figure 11).

Twenty-one zircons analyses were obtained forgrandiorite sample SCK-4 (430.9 ± 2.5 Ma), yielding176Hf/177Hf ratios from 0.282888 to 0.283036,176Yb/176Hf ratios from 0.012865 to 0.121129, and176Lu/176Hf ratios from 0.000691 to 0.005704. Theyhave positive εHf(t) values and Hf isotopic crustalmodel ages (TDM

C) ranging from +13.0 to +7.8, andfrom 279 to 587 Ma, respectively (SupplementaryTable 4). Twenty zircons from granodiorite sampleSCK-2 (425.5 ± 2.7 Ma) were analysed, yielding176Hf/177Hf ratios from 0.282891 to 0.283073,176Yb/176Hf ratios from 0.018600 to 0.063993, and176Lu/176Hf ratios from 0.001024 to 0.003224. The posi-tive εHf(t) values of zircons and Hf isotopic crustal modelages (TDM

C) vary from +13.2 to +19.5, and from 167 to568 Ma, respectively (Supplementary Table 4).

6. Discussion

6.1. Ages of the magmatic events in EasternTianshan

The available geochronological data clearly show threemain magmatic episodes for the Eastern Tianshan oro-genic belt (Wang et al. 2006a, 2015e, 2016; Mao et al.2008, 2014; Zhang et al. 2008; Zhou et al. 2010; Chenet al. 2014). The youngest magmatism occurred in theTriassic and includes: (1) the ~227 Ma Baishan graniteporphyry plutons associated with Mo deposit (Wanget al. 2015e); (2) the 234–232 Ma Donggebi porphyriticgranite and granite porphyry plutons associated withMo deposit (Zhang et al. 2015b); (3) the ~237 Ma fine-grained granite located in the Weiya area (Zhang et al.2005); and (4) the ~210 Ma Tianhu monzonitic granite(Li and Chen 2004), which were formed in an intracon-tinental setting. The second episode of magmatismoccurred during the late Palaeozoic (369–286 Ma).Representative examples include: (1) the 288–286 MaHuangshan and Xiangshan mafic rocks formed in apost-collisional setting (Zhou et al. 2010; Qin et al.2011); and (2) the 332–369 Ma Tuwu and Yandongore-forming porphyries that formed in an arc settingassociated with the northward subduction of thePalaeo-Tianshan ocean (Rui et al. 2002; Shen et al.2014; Wang et al. 2015a, 2015b). The earliest magmaticepisode occurred during the early Palaeozoic, and israrely recognized in the Eastern Tianshan orogenicbelt. However, recent studies reveal some earlyPalaeozoic magmatic events in the orogen (Shu et al.

2004; Zhang et al. 2008; Lei et al. 2011; Wang et al.2015f). Typical examples include the Dananhu monzo-granite (383 ± 9 Ma, Song et al. 2002), the Xingxingxiagranodiorite (425 ± 4 Ma; He et al. 2012), the Yuhaigranodiorite (422.3 ± 4 Ma; Zang 2014), the Weiyagranulite (434.7 ± 2.5 Ma; Shu et al. 2004), andMishigou gabbro (468 Ma; Shu et al. 1999), which repre-sent a significant early Palaeozoic magmatic hydrother-mal event.

In this study, we present new zircon LA-ICP-MSzircon U–Pb data for three representative intrusivesamples collected from the Sanchakou area located inthe interior of the Dananhu–Tousuquan arc belt(Figure 1C). The zircon U–Pb dating results indicatethat the Sanchakou quartz diorite was emplaced at439.7 ± 2.5 Ma (Figure 7A), whereas the granodioriteformed at 430.9 ± 2.5 to 425.5 ± 2.7 Ma (Figure 7Band C). This result is inconsistent with most previousstudies that proposed an early Permian age for theintrusive rocks (278–276 Ma; Lang et al. 1992; Li et al.2004), but comparable to the zircon U–Pb age(443 ± 2.9 Ma) for the granodiorite recently reportedby Wang et al. (2015f). It is increasingly clear that theSanchakou area experienced multi-stage magmatism,and that the earliest stage of magmatism might haveoccurred during the early Silurian (443–426 Ma). Thesegeochronological data, as well as the previous agesmentioned above, demonstrate that the earlyPalaeozoic magmatic activity was also developed inEastern Tianshan orogenic belt.

6.2. Petrogenesis and magma source

All Sanchakou intrusive samples are characterized byhigh Al2O3 (15.98–17.56 wt.%), Sr (652–773 ppm), andSr/Y ratios (68–120), and low Yb (0.44–1.33 ppm) andY (5.43–11.1 ppm), and obvious positive Eu anomalies(Eu/Eu* = 0.98–1.61), showing geochemical affinitywith adakites (Defant and Drummond 1990). In the(La/Yb)N vs. YbN discrimination diagram, theSanchakou intrusive rocks also plot well within theadakitic field (Figure 12A). We therefore suggest thatthe Sanchakou intrusions can be classified as adakiticrocks. There are several mechanisms proposed for thegenesis of adakitic magmas, including: (1) partialmelting of delaminated lower crust (Guo et al. 2006;Kadioglu and Dilek 2010); (2) partial melting ofhydrated mafic rocks in a thickened lower crust(Guan et al. 2012; Hou et al. 2013; Sui et al. 2013);(3) partial melting of subducted oceanic crust with orwithout contributions from the mantle wedge (Defantand Drummond 1990; Zhu et al. 2009; Sun et al. 2010,2011); and (4) crustal assimilation and fractional

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crystallization (AFC) processes involving parentalbasaltic magmas (Macpherson et al. 2006; Richardsand Kerrich 2007).

Experimental and geochemical studies indicate thatsubducted slab-derived adakites generally have highMgO, CaO, Cr, and Ni contents and Mg# values (>40),due to interaction with the overlying peridotite in themantle wedge during magma ascent, whereas lowercrust-derived adakites have low compatible trace ele-ments (e.g. Cr and Ni) (Yogodzinski and Kelemen 1998;Rapp et al. 1999; Zhu et al. 2009; Guan et al. 2012).Adakitic intrusions in the Sanchakou area exhibit mod-erate MgO contents and Mg# values, ranging from 1.30to 2.03 wt.% and 36–46, respectively, which are consis-tent with being subducted oceanic slab-derived ada-kites (Figure 12B), such as the Tuwu–Yandongtonalites (Wang et al. 2015a, 2015b) in EasternTianshan. This interpretation is also supported by highCr concentration (69.6–118 ppm) of the Sanchakouintrusions (Supplementary Table 3). Thus, these geo-chemical characteristics indicate that these magmaswere probably derived from partial melting of a sub-ducted slab, which subsequently hybridized by mantlewedge.

In addition, the adakitic intrusions at Sanchakouare unlikely to reflect AFC processes of parental

basaltic magmas (Macpherson et al. 2006; Richardsand Kerrich 2007), because they exhibit no obvioussystematic variations in geochemical compositionsassociated with AFC (Castillo et al. 1999;Macpherson et al. 2006). Furthermore, the trace ele-ment signatures of the these rocks show positivecorrelation between Zr/Nb and Zr values, as well asLa/Yb and La values, indicating that the partial melt-ing process was dominant in their petrogenesis(Figure 12C and D). The pronounced LREE fractiona-tion and weak HREE depletion patterns (Figure 10A)of the Sanchakou intrusions further demonstrate thatthey fit with generation from partial melting of sub-ducted oceanic crust (Defant and Drummond 1990;Sun et al. 2010, 2011).

This interpretation is also supported by the positivezircon εHf(t) values (+11.2 to +19.6) recorded in theSanchakou intrusions. In the εHf(t) vs. U–Pb age diagram(Figure 11), zircons from these samples show a spreadof εHf(t) values near the depleted mantle evolution line,comparable to those of the Silurian intrusions inSouthern Tianshan (e.g. Baicheng) (Zhao et al. 2015)and Carboniferous intrusions (e.g. Tuwu and Yandong)in the Dananhu–Tousuquan arc belt formed by partialmelting of subducted oceanic slab (Zhang et al. 2004,2008; Shen et al. 2014). The zircon Hf isotopic

Figure 12. Discrimination diagrams for genetic type of the Sanchakou intrusions. (A) (La/Yb)N vs. YbN diagram (Defant andDrummond 1990); (B) MgO vs. SiO2 diagram; (C) Zr/Nb vs. Zr diagram; (D) La/Yb vs. La diagram. Data for the Tuwu–Yandongtonalite are from Wang et al. (2015a, 2015b).

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compositions of the adakitic tonalites from the Tuwu–Yandong areas show variable εHf(t) values ranging from6.9 to 17.2 (Wang et al. 2015a, 2015b). In comparison,the relatively inhomogeneous Hf isotopic composition(8.4ε units) recorded in the Sanchakou intrusions sug-gest strong interaction between subducted oceaniccrust and mantle wedge peridotite during the formationof adakitic intrusions.

In summary, the Sanchakou adakitic (quartz dioriteand granodiorite) magmas are interpreted to be derivedfrom the partial melting of subducted oceanic crust, andthese magmas interacted further with peridotite in themantle wedge.

6.3. Geodynamic implications

Previous studies infer for the Eastern Tianshan the simul-taneous southward and northward subduction of thePalaeo-Tianshan oceanic plate during the Carboniferousformed the Aqishan–Yamansu and the Dananhu–Tousuquan arcs, respectively (Han et al. 2006; Wanget al. 2006b, 2015a; Zhang et al. 2008). In the Dananhu–Tousuquan arc belt, Late Devonian to early Carboniferousvolcanic and plutonic rocks, including the Tuwu,Yandong, and Chihu intrusive rocks, display an obvioussubduction-related component as evidenced by positivebulk εNd(t) and zircon εHf(t) values (Tang et al. 2010; Suet al. 2012; Wang et al. 2014, 2015a), formed in a sub-duction-related setting. Since the early Permian, theEastern Tianshan is considered to have entered thepost-collisional stage, based on the presence of theyoungest ophiolite of ~310 Ma along with widespreadbimodal volcanic rocks of ~290 Ma (Chen et al. 2011; Qinet al. 2011; Su et al. 2012; Xiao et al. 2013).

LA-ICP-MS zircon dating and geochemical data pre-sented in this study provide solid evidence for the

existence of subduction-related adakitic rocks inEastern Tianshan during early Silurian time. This arcmagmatism significantly predates the opening of thePalaeo-Tianshan ocean and suggests the northwardsubduction of oceanic crust prior to ~440 Ma. Thegeochemical characteristics of the ca. 440 Ma quartzdiorite and ca. 431–426 Ma granodiorite in theSanchakou area of the Eastern Tianshan, such as posi-tive Eu anomalies, significant LREE enrichment, andlow HREE abundances, are comparable with those ofTuwu–Yandong arc magmatic rocks (Zhang et al.2008; Xiao et al. 2015; Wang et al. 2015a, 2015b).Moreover, they are also similar to those of modernarc-type volcanics and arc-related plutons, i.e. nega-tive anomalies of Nb, Ta, Zr, Hf, and Ti and positive Pbanomalies (Figure 10A; Briqueu et al. 1984; Pearceet al. 1984; Sun and McDonough 1989; Altherr et al.2008; Boari et al. 2009). In the Th/Yb vs. Ta/Yb and Th/Yb vs. Nb/Yb discrimination diagrams (Figure 13A andB), all samples fall within the oceanic arc field(Whattam and Hewins 2009), and close to E-MORBarea (Pearce and Peate 1995; Sayıt and Göncüoglu2009), which are characteristics of island arc igneousrocks emplaced during Silurian subduction of anoceanic slab. Therefore, the Sanchakou quartz dioriteand granodiorites most likely formed in the Dananhu–Tousuquan island arc.

Taking all of the above into account, we suggestthat the initiation of northward subduction of thePalaeo-Tianshan ocean beneath the Dananhu–Tousuquan arc occurred as early as early Siluriantime, and that arc magmatism in the Sanchakou areabegan ca. 440–426 Ma (Figure 14). The interactionbetween subducted oceanic slab and mantle wedgeperidotite could have formed the Sanchakou adakiticmagmas.

B

10-2

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100

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10-1 100 101 102

bY/h

T

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Subduction zoneenrichment

With

in-p

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enric

hmen

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N-MORB

E-MORB

OIB

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10-2 100 10110-1

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GranodioriteQuartz diorite

E-MORB&OIB

N-MORB

Oceanic

arcsContin

ental a

rcs

bY/h

T

10 -2

10 -1

10 0

10 1

Ta/Yb

Figure 13. (A) Th/Yb vs. Ta/Yb diagram (Whattam and Hewins 2009). (b) Th/Yb vs. Nb/Yb diagram (Pearce and Peate 1995; Sayıt andGöncüoglu 2009).

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7. Conclusions

(1) LA-ICP-MS zircon U–Pb dating indicates that theSanchakou quartz diorite was emplaced at ca.440 Ma, and the granodiorite was emplaced atca. 431–426 Ma, which represents a prominentearly Palaeozoic magmatic event in EasternTianshan orogenic belt.

(2) Petrographic and geochemical data suggest thatthe Sanchakou dioritic and granodioritic plutonsis low-K tholeiite; enriched in K, Ba, Sr, U, and Sm;markedly depleted in Nb, Ta, Pb, and Ti; andshows geochemical affinities similar to those ofadakites. These characteristics and zircon Hf iso-topic data indicate that the Sanchakou intrusionscan be attributed to the partial melting of sub-ducted oceanic crust and that these magmassubsequently interacted with mantle wedge.

(3) Our new data combined with regional geologicalhistory suggest that the Sanchakou intrusionswere generated in an arc setting during theearly Silurian. This implies that the initiation ofnorthward subduction of the Palaeo-Tianshanocean beneath the Dananhu–Tousuquan arcwas present as early as ca. 440 Ma in EasternTianshan.

Acknowledgements

We are very grateful to the Editor-in-Chief Robert J. Stern andtwo anonymous reviewers for constructive comments andassistance in improving the manuscript. We thank Jing Fengof the Xinjiang Bureau of Geology and Mineral Explorationalong with Jinzhu San and Shoubo Chen of No. 704Geological Team of the Xinjiang Nonferrous GeoexplorationBureau, for their great support and assistance in our fieldwork.We also appreciate the kind help of Li Su from the China

University of Geosciences (Beijing) on LA-ICP-MS zircon U–Pbdating. We thank Chinese Academician Yusheng Zhai of theChina University of Geosciences (Beijing) for a helpful scientificreview of an earlier version of the manuscript.

Disclosure statement

No potential conflict of interest was reported by the authors.

Funding

This research was jointly funded by the Fundamental ResearchFunds for the National Natural Science Foundation of China[grant numbers 41572066 and 41030423]; the FundamentalResearch Funds for the Central Universities of China [grantnumbers 2652015019 and 2652015032]; the Open ResearchFunds for the State Key Laboratory of Geological Processesand Mineral Resources [grant number GPMR201512]; and theGeological Survey Project of China [grant numbers1212011085471 and 1212011220923].

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