Journal of Asian Earth Sciences 113 (2015) 544–559

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Journal of Asian Earth Sciences

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Tectonic evolution of a complex orogenic system: Evidence from the northern Qinling belt, Central China ⇑ Li Tang a, M. Santosh a,b,c, , Yunpeng Dong b a School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China b State Key Laboratory of Continental Dynamics, Department of Geology, Northwest University, Xi’an 710069, China c Centre for Tectonics Resources and Exploration, Department of Earth Sciences, University of Adelaide, SA 5005, Australia article info abstract

Article history: The Qinling orogenic belt preserves the records of a long evolution history of convergence between the Received 29 December 2014 North China Craton and the South China Craton. In this study, we present results from new geological, Received in revised form 12 March 2015 geochemical, zircon U–Pb geochronological and Lu–Hf isotopic investigations on a suite of orthogneisses Accepted 13 March 2015 from the Taihua Group (THG) and Tietonggou Group (TGG). We also present geochronological data on Available online 27 March 2015 schist and migmatite from the North Qinling belt (NQB) and metasedimentary rocks from the Wuguan unit (WGU) which is exposed along the southern side of the Shangdan suture zone. Two orthogneisses Keywords: from the THG define several stages of arc magmatism at 2.51 Ga, 2.34 Ga, 2.28 Ga and 2.16 Ga, Geochemistry followed by metamorphism at 1930 ± 31 Ma. Zircons from the TGG trace a tectonothermal event at Zircon U–Pb geochronology Lu–Hf isotopes 1897 ± 15 Ma. Geochemical data on biotite gneiss from the THG and the TTG (tonalite–trondhjemite– Tectonic evolution granodiorite) gneiss from the TGG classify these rocks as dacite and display volcanic arc affinity. Northern Qinling orogenic belt Zircon Lu–Hf isotopic results suggest that the parental magma for the protolith of felsic gneisses were C derived from Mesoarchean crustal components (TDM = 2766–3067 Ma). The amphibole gneiss from the

THG classifies as metabasalt and the zircons from this rock show dominantly negative eHf(t) values vary- C ing from 10.3 to 4.6 and TDM range of 3088–3437 Ma, suggesting magma derivation by melting of Paleoarchean–Mesoarchean subducted oceanic crust. Zircons in the schist from the NQB show a wide age population in the range of 937–1131 Ma (peak at 1035 Ma). Zircons from the melanosomes of the migmatite in the NQB define ages between 405 and 379 Ma, correlating with the melting event in the NQB during 450–380 Ma. The WGU shows age populations of 854–803 Ma (with a peak at 829–824 Ma), 2460 Ma, 1802 Ma and 1180–1000 Ma, which are markedly different from that of the NQB and SQB. The ages obtained in our study correlate with the widely reported Grenvillian-aged magmatism in the NQB, and suggest that the NQB might have been a discrete micro-continent during Paleo- and Mesoproterozoic which has been overprinted by Paleozoic tectonic event. Ó 2015 Elsevier Ltd. All rights reserved.

1. Introduction North China Craton (NCC) and South China Craton (SCC) (Mattauer et al., 1985; Zhang et al., 1995a; Meng and Zhang, 1999, 2000; Tseng Many of the major collisional orogenic belts in the world were et al., 2009; Dong et al., 2011a, 2012, 2013; Wu and Zheng, 2013; constructed through prolonged processes of arc–arc, arc–continent Tang et al., 2014). The QOB has been divided into the Southern mar- and continent–continent collisional events with multiple subduc- gin of the NCC (S-NCC), the North Qinling belt (NQB) and the South tion and accretion regimes (Yin and Harrison, 2000; Brown, 2007, Qinling belt (SQB) (Fig. 1b), and these three terranes are separated 2009; Xiao et al., 2010; Santosh, 2013; Xiao and Santosh, 2014; by the Paleozoic Shangdan suture zone (SSZ) in the north and the Santosh et al., 2010, 2015a, 2015b). The Qinling orogenic belt Mianlue suture zone in the south (Zhang et al., 1995a). The (QOB) in Central China, one of the major collisional orogens in east- Qinling orogenic system is characterized by (1) Archean– ern Asia, resulted from multiple stages of convergence between the Paleoproterozoic basement rocks, (2) Neoproterozoic metasedi- mentary rocks with Grenvillian-aged (Neoproterozoic) magmatic records, (3) Mesoproterozoic–Paleozoic ophiolitic suits, (4) ⇑ Corresponding author at: School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China. Paleozoic metasedimentary rocks, migmatites and HP-UHP E-mail address: [email protected] (M. Santosh). metamorphic rocks and (5) Paleozoic–Mesozoic granitoid plutons http://dx.doi.org/10.1016/j.jseaes.2015.03.033 1367-9120/Ó 2015 Elsevier Ltd. All rights reserved. L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 545

Fig. 1. Geological sketch map of the North Qinling orogenic belt (modified after Dong et al., 2011a), showing the location of QOB, tectonic units and sample locations.

(Zhang et al., 1995a; Yang et al., 2001; Wu et al., 2007; Liu et al., 2. Geological setting 2009a; Dong et al., 2011a, 2014). A number of studies in the past decade have addressed the geo- The nearly east–west trending QOB connects the Dabie–Sulu chemical and geochronological features of the northern part of the orogenic belt to the east and the Qilian–Kunlun orogenic belt to QOB (comprising the S-NCC, NQB and SSZ) (e.g. Dong et al., 2011c, the west (Fig. 1). To the north, the QOB is separated with the 2014; Huang et al., 2013; Shi et al., 2013; Diwu et al., 2014). The NCC by the Lingbao–Lushan–Wuyang intra-continental fault, basement rocks discontinuously exposed in the S-NCC witnessed whereas toward south, the belt is bound by the Mianlue– Neoarchean–Paleoproterozoic magmatism followed by 1.96– Bashan–Xiangguang thrust fault with the SCC (Zhang et al., 1.82 Ga metamorphism (e.g. Huang et al., 2012; Diwu et al., 1995a). Within the Lingbao–Lushan–Wuyang fault, with the 2014; Lu et al., 2014), similar to the records from elsewhere in Luonan–Luanchuan fault, SSZ and Mianlue–Bashan–Xiangguang the NCC (Wan et al., 2014; Yang and Santosh, 2014; Zhai, 2014 thrust fault to the south (Fig. 1), the QOB has been divided into and references therein). Late Paleoproterozoic metamorphism three domains from north to south as S-NCC, NQB and SQB, respec- (1.86–1.80 Ga) has also been recorded from the Trans-North tively (Zhang et al., 1995a). China Orogen (TNCO) associated with the collision between the Western and Eastern Blocks of the NCC (e.g. Guo et al., 2005; 2.1. Southern margin of the North China Craton Zhao et al., 2009; Trap et al., 2009; Zhai and Santosh, 2011; Zhao and Zhai, 2013). Debates surround question whether the NQB The S-NCC is the northernmost zone of the QOB (Fig. 1). The belongs to part of the S-NCC (e.g. Zhang et al., 1995b, 2001), SCC region is mainly composed of amphibolite facies Archean– (e.g. Xue et al., 1996; Shi et al., 2009) or is a discrete micro-conti- Paleoproterozoic basement complexes (e.g. THG, TGG and nent block (e.g. Dong et al., 2003; Yang et al., 2010). The Wuguan Dengfeng Group), weakly metamorphosed Mesoproterozoic vol- unit (WGU) and the migmatites exposed in the Qinling Group pre- canics (Xiong’er Group) and Mesoproterozoic to Mesozoic sedi- serve one of the keys to address this debate, although detailed mentary cover sequences such as Gaoshanhe and Luonan Groups studies have not been carried out as yet from this region. In this (Zhang et al., 1995a, 2001). The THG is mainly scattered along study, we present integrated whole rock geochemistry, in situ zir- the S-NCC in five regions: the Lantian–Xiaoqinling, Xiaoshan, con U–Pb ages and Hf isotopic data for the basement rocks from Xiong’ershan, Lushan, and Wuyang (Fig. 1b) (Xu et al., 2009). The the S-NCC (THG and TGG), schist and migmatite from the NQB THG is traditionally subdivided into the lower and the upper units, and metasedimentary rocks from the WGU. In combination with where the lower unit is mainly composed of amphibolite to gran- previous studies, our data provide important insights to under- ulite facies metamorphosed TTG gneiss and amphibolite, and the stand the complex Qinling orogenic system. upper one includes graphite-bearing gneiss, banded iron formation 546 L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 and amphibolite (Liu et al., 2009a). In the Lantian–Xiaoqinling area, (quartzite, mica schist and marble). The youngest detrital zircons the THG is mainly composed of biotite gneiss and amphibole from mica schist show late Neoproterozoic ages (Diwu et al., gneiss, which are unconformably overlain by the TGG unit, which 2010; Zhu et al., 2011; Shi et al., 2013). is dominated by TTG gneisses, metasedimentary rocks and minor The Erlangping Group comprises ophiolitic suite (comprising amphibolites. massive or pillow basalt, sparse ultramafic rock, sheeted dike, gab- bro and some radiolarian chert), clastic sedimentary succession 2.2. North Qinling belt and carbonate. The ophiolitic units show both MORB affinity and subduction-related magmatic character (Sun et al., 1996; Dong The NQB is bound by the Luonan–Luanchuan fault to the north et al., 2011c). Together with the radiolarians within cherts, a and the SSZ to the south (Fig. 1C). From north to south, the NQB has back-arc basin is suggested during Cambrian and Ordovician been divided into three units: the Kuanping Group (KPG), (Wang et al., 1995; Sun et al., 1996), in which the sedimentary Erlangping Group and Qinling Group (QLG) separated by several assemblages were deposited (Lu et al., 2003). thrust faults or ductile shear zones. The KPG is mainly composed The QLG consists of amphibolite to granulite facies metamor- of ophiolitic unit and meta-clastic unit. The ophiolitic unit (green- phic rocks including gneiss, amphibolite and marbles. The orthog- schist and amphibolite) shows N-MORB and T-MORB affinity neiss of the QLG shows zircon U–Pb ages of 1015–850 Ma (e.g. Shi (Zhang and Zhang, 1995; Dong et al., 2011b, 2014), with Sm–Nd et al., 2009; Yang et al., 2010), and the paragneiss and carbonate whole rock isochron ages ranging from 0.94 to 1.2 Ga (Zhang rocks record Early Paleozoic metamorphism (Shi et al., 2009; et al., 1994, 1996) and LA-ICP-MS zircon U–Pb ages of 943 and Yang et al., 2010; Wan et al., 2011; Diwu et al., 2012). Further stud- 1445 Ma (Diwu et al., 2010; Dong et al., 2014). The meta-clastic ies indicated that some of the gneisses were migmatitized, the tim- unit comprises metamorphosed terrestrial clastic sediments ing of which is constrained as ca. 517–417 Ma (Dong et al., 2011a).

Fig. 2. Representative field photographs from the QOB. (a) Amphibole gneiss from the THG. (b) Biotite plagioclase gneiss from the THG. (c) TTG gneiss interbedded with amphibolite from the TGG. (d) Schist from the KPG. (e) WGU metasediment. (f) Migmatite from the QLG. See text for details. L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 547

2.3. Shangdan suture zone At Lantian–Xiaoqinling, the two types of gneisses belonging to the THG are exposed, a dark gray amphibole gneiss (13QL- The SSZ is mainly represented by a nearly east–west trending 01) composed of hornblende (40%), plagioclase (30%), quartz tectonic mélange which consists of ophiolitic units, arc related vol- (20%) and minor biotite (Fig. 2a), and a light gray biotite plagio- canic suites and accretionary prism. The mafic rocks of this discon- clase gneiss (13QL-02) mainly composed of plagioclase (40%), tinuous tectonic mélange show zircon U–Pb ages of 540–420 Ma quartz (40%), biotite (15%) and minor hornblende (Fig. 2b). (Lu et al., 2003; Yang et al., 2006; Liu et al., 2009b; Li et al., These rocks are highly deformed and show minerals oriented 2008; Dong et al., 2011c; Tang et al., 2014). These ages are consis- domains of plagioclase + hornblende + biotite. The TGG is as tent with the Cambrian–Ordovician age obtained from the volcanic interbedded TTG gneisses and amphibolites (Fig. 2c), which rocks intercalated with radiolarian cherts (Cui et al., 1995). unconformably overlie the THG. The TTG gneiss (sample In the Shangnan–Danfeng area, the WGU is exposed along the 13QL-03) in the studied location occurs as a 1.5 m band and is southern side of the SSZ (Fig. 1C), which mainly comprises mica- mainly composed of quartz (45%), plagioclase (35%) and biotite schist, quartzite, garnet amphibolite and minor lenticular calcite (15%). The amphibolite (sample 13QL-04) is composed of horn- marbles. blende (40%), plagioclase (30%), biotite (15%) and quartz (10%) (Fig. 3). 3. Petrology and sample description The KPG at Hongmenhe is mainly composed of two mica-schist and biotite schist. The biotite schist (13QL-23) is composed of Geological investigations and sampling were carried out in the quartz (40%), biotite (35%) and plagioclase (18%), and show clear S-NCC, NQB and WGU (Fig. 1). interlayered quartz and biotite (Fig. 3).

Fig. 3. Photomicrographs showing mineral assemblages and textures of representative samples. (a) Oriented hornblend, plagioclase and quartz assemblage in orthogneiss 13QL-01. (b) Plagioclase, quartz, oriented biotite and minor hornblend in orthogneiss 13QL-02. (c) Gneiss (13QL-03) showing major mineral assemblages of quartz, biotite and slightly altered plagioclase. (d) Schist (13QL-23) showing oriented biotite + muscovite. (e) Fine-grained and oriented quartz + plagioclase + biotite in metasediment (13QL-36). (f) Oriented biotite in the matrix of quartz in melanosome (13QL-49) of migmatite. Scale bars are 500 lm. 548 L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559

At Weiziping, migmatites of the QLG are exposed, where the Research Center for Geoanalysis, Chinese Academy of Geological melanosomes (13QL-46, 13QL-49) are highly deformed and show Sciences, China. Trace and rare earth elements were analyzed with oriented assemblages of biotite + quartz + plagioclase (Fig. 3). The analytical uncertainties 10% for elements with abundances leucosomes show boudinage structure, and rootless folds. <10 ppm and approximately 5% for those >10 ppm (Zeng et al., At Shangnan, felsic schists belonging to WGU are exposed (sam- 2011). ples 13QL-36, 13QL-37, 13QL-41), together with greenschist (13QL-44), marble and minor garnet bearing amphibolite. 4.2. Zircon U–Pb and Lu–Hf isotopes

Fresh rock samples for zircon separation were crushed and 4. Analytical techniques milled, followed by gravimetric and magmatic separation and hand picking of zircon grains under a binocular microscope at the 4.1. Whole-rock geochemistry Yu’neng Geological and Mineral Separation Survey Center, Langfang, China. Individual zircon grains were mounted in epoxy Representative fresh rock chips were initially reduced to avoid resin disks along with the standard TEMORA1 (417 Ma; Black surface alteration or weathering. These chips were then powered et al., 2004). The mount was polished and cleaned to reveal mid- to 200-mesh for geochemical analyses. Major oxides were analyzed section, and followed by high-purity gold sputter coating. In order by X-ray fluorescence (XRF) spectrometry (PW4400) with analyti- to investigate the internal structures of zircons, cathodolumines- cal uncertainties <5%, and trace elements were measured by induc- cence (CL) images were obtained using scanning electron micro- tive coupled plasma mass spectrometry (ICP-MS) at the National scope (JSM510) equipped with Gantan CL probe at the Beijing Geoanalysis Centre, and transmitted and reflected light images were examined by a petrological microscope. The high spatial resolution zircon U–Pb isotopic analyses were performed on a laser ablation inductively coupled plasma spec- trometry (LA-ICP-MS) housed at the State Key Laboratory of Continental Dynamics of Northwest University, China. The detailed analytical procedures are same with those described in Yuan et al. (2004). On an Agilent 7500a ICP-MS instrument, the laser spot diameter and frequency was set to be 30 lm and 10 Hz, respec- tively. Harvard zircon 91500 was used as external standard with a recommended 206Pb/238U age of 1065.4 ± 0.6 Ma (Wiedenbeck et al., 2004) to correct instrumental mass bias and depth-dependent elemental and isotopic fractionation, the standard silicate glass NIST 610 and GJ-1 were used to optimize the instrument. U–Th– Pb concentrations were calibrated by using NIST 610 as an external standard and 29Si as an internal standard. The isotopic ratios and ages of 207Pb/206Pb, 206Pb/238U, 207Pb/235U were calculated using the GLITTER program, and the concordia diagram and weighted Fig. 4. Total alkalis against silica (TAS) diagram after LeBas et al. (1986). mean calculation were computed using ISOPLOT software.

Fig. 5. Discrimination diagrams for basalts and granites. (a) MnO–TiO2–P2O5 diagram (after Mullen, 1983), CAB: calc-alkaline arc basalt, IAT: island arc tholeiite, MORB: mid ocean ridge basalt, OIT: oceanic island tholeiite, OIA: oceanic island arc. (b) Th–Hf–Ta diagram (after Wood, 1980), A: N-MORB, B: R-MORB and within plate tholeiite, C: within plate alkalic basalt, D1: calc-alkaline basalt (Hf/Th < 3), D2: volcanic arc tholeiite (Hf/Th > 3). (c) Nb–Y diagram (after Pearce et al., 1984), VAG: volcanic arc granite, syn-COLG: syn-collisional granite, WPG: within plate granite, ORG: ocean ridge granite. (d) Ta–Yb diagram (after Pearce et al., 1984). L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 549

In situ Lu–Hf isotopic compositions of zircon were obtained (Chu et al., 2002) was used to calculate mean bYb value from using the same instrument at the State Key Laboratory of 172Yb and 173Yb. Zircon 91500 was used as the reference standard, Continental Dynamics of Northwest University, China. The detailed with a weighted mean 176Hf/177Hf ratio of 0.282306 ± 10 analytical procedures were the same as those described by Yuan (Woodhead et al., 2004). Calculation of initial 176Hf/177Hf was based et al. (2008). A stationary spot adjacent to the U–Pb dated domain on the reference to the chondritic reservoir (Blichert-Toft and was used for analysis with a beam diameter of 45 lm. The energy Albarède, 1997). Hf model age (TDM1) was calculated with respect density of laser ablation used was 15–20 J/cm2. Recommended to the depleted mantle with present-day 176Hf/177Hf = 0.28325 176Lu/175Lu ratio of 0.02669 (DeBievre and Taylor, 1993) was used and 176Lu/177Hf = 0.0384 (Griffin et al., 2000), and two-stage Hf 176 177 176 172 to calculate Lu/ Hf ratios, and the Yb/ Yb ratio of 0.5886 model age (TDM2) was calculated with respect to the average continental crust with a 176Lu/177Hf ratio of 0.015 (Griffin et al., 2002), using the 176Lu decay constant of 1.865 1011 year1 (Scherer et al., 2001).

5. Results

5.1. Whole-rock geochemistry

5.1.1. Major elements Whole rock geochemical results from the S-NCC, NQB and WGU are presented in Supplementary Table 1. In the TAS diagram (LeBas et al., 1986), the amphibole gneiss (13QL-01) and amphibolite (13QL-04) fall in the fields of basalt and basaltic andesite, respec- tively (Fig. 4). The two metabasalts display moderate variation in

SiO2 (46.39–52.79 wt.%), Al2O3 (15.24–15.48 wt.%), CaO (9.27– T 10.52 wt.%), Fe2O3 (11.87–12.17 wt.%), MgO (4.69–6.59 wt.%), MnO (0.14–0.20 wt.%), TiO2 (0.94–1.51 wt.%) and P2O5 (0.14– 0.47 wt.%). These rocks fall in the CAB field (13QL-01) or the

MORB field (13QL-04) in the MnO–TiO2–P2O5 (Mullen, 1983) tern- ary discrimination diagram (Fig. 5a). The biotite plagioclase gneiss

(13QL-02) and TTG gneiss (13QL-03) show SiO2,Al2O3, CaO and total alkali (Na2O+K2O) contents of 64.09–68.47 wt.%, 15.38– 15.69 wt.%, 2.55–4.19 wt.% and 6.49–6.52 wt.%, respectively.

The greenschist from the WGU (13QL-44) shows lower SiO2 (48.46 wt.%) and higher CaO (2.86 wt.%) contents as compared with the metasediments (13QL-36, 13QL-37, 13QL-41) which dis-

play SiO2 (50.74–59.60 wt.%) and CaO (7.56–9.81 wt.%). These rocks show similar Na2O+K2O (3.70–4.00 wt.%), although the greenschist (13QL-44) has low K2O content of 0.3 wt.%. Fig. 6. Chondrite-normalized REE plots and Primitive mantle-normalized multi The melanosomes (13QL-46, 13QL-49) of the Qinling migmatite element variation plots for varied rocks from the QOB. Normalizing values are from show moderate variations of SiO2 (55.76–60.41 wt.%), relatively Sun and McDonough (1989). high Al2O3 (15.91–16.35 wt.%) and variable CaO (2.86–6.25 wt.%),

Fig. 7. Cathodoluminescence (CL) images of representative zircons in sample 13QL-01, 13QL-02, 13QL-03 and 13QL-23. Yellow circles for U–Pb analysis and red circles for

Lu–Hf analysis, ages in Ma and eHf(t) values are also shown. Scale bars are in 100 lm. (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.) 550 L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559

T Fe2O3 (7.81–9.79 wt.%), MgO (3.4–3.6 wt.%) and Na2O+K2O (4.52– ((La/Yb)n = 87.16), whereas the amphibolite shows a flat chondrite 6.64 wt.%). normalized REE pattern ((La/Yb)n = 1.02). The three metasedimentary rocks (13QL-36, 13QL-37, 13QL-41) from the WGU share REE patterns (Fig. 6a) similar to those of the 5.1.2. Trace elements orthogneiss from the THG. These schistose rocks display LREE The four samples from the S-NCC show variation in their REE enrichment ((La/Yb)n = 6.83–12.34) and moderate to flat HREE pat- patterns (Fig. 6a). The rocks from the THG show similar REE frac- terns ((Gd/Yb)n = 1.49–1.77). The greenschist (13QL-44) from the tionation with enriched LREE contents ((La/Yb)n = 8.45–13.75) WGU shows nearly parallel and elevated pattern ((La/Yb)n = 1.44, and without Eu anomaly. The orthogneiss from the TGG exhibit a RREE = 87.60 ppm) as compared to the amphibolite (13QL-04) relatively steep distribution pattern (Fig. 6a) with LREE enrichment ((La/Yb)n = 1.02, RREE = 56.56 ppm) from TGG.

Fig. 8. Cathodoluminescence (CL) images of representative zircons in sample 13QL-36, 13QL-37, 13QL-46 and 13QL-49. Yellow circles for U–Pb analysis and red circles for

Lu–Hf analysis, ages in Ma and eHf(t) values are also shown. Scale bars are in 100 lm. (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.)

Fig. 9. Zircon U–Pb concordia plots for sample 13QL-01, 13QL-02, 13QL-03 and 13QL-23 from the QOB. L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 551

The melanosomes (13QL-46, 13QL-49) of the QLG migmatite age of 2163 ± 26 Ma (MSWD = 0.13) and have Th/U ratios of display moderate fractionation ((La/Yb)n = 6.60–8.38, (Gd/ 0.49–1.28, suggesting a magmatic population. The remaining one 207 206 Yb)n = 1.36–1.66) and weak Eu anomaly (dEu = 0.63–0.82). spot display Pb/ Pb age of 1957 ± 44 Ma. In the primitive-mantle normalized (Sun and McDonough, Zircons in sample 13QL-02 are euhedral to subhedral, with 1989) trace element plot, all samples are enriched in large ion length varying from 40 to 200 lm and aspect ratio of 2.5:1–1:1. lithophile elements (LILE) like K, Rb and Ba, except for the green- Most of the zircons show clear oscillatory zoning or heterogeneous schist from the WGU that displays nearly flat pattern (Fig. 6b). fractured domains in CL images (Fig. 7a). A total of 30 spots from All the samples exhibit negative Ta, Nb and Ti anomaly. In the Y– 30 zircons were analyzed from this rock. The age results can be Nb diagram and Yb–Ta diagram (Pearce et al., 1984), the orthog- divided into four groups in the concordia (Fig. 9b), yielding neisses (13QL-02, 13QL-03) fall in the field of volcanic-arc granite weighted mean 207Pb/206Pb age of 2510 ± 22 Ma (MSWD = 0.62), (VAG) or syn-collisional granite. 2342 ± 26 Ma (MSWD = 1.17), 2155 ± 70 Ma (MSWD = 1.3) and 1930 ± 31 Ma (MSWD = 0.19), respectively. The six spots which yielded the youngest age group were analyzed at the rim domains 5.2. Zircon U–Pb geochronology or the homogeneous gray color zircons without texture, and shows Th/U = 0.02–0.29, suggesting metamorphic origin. We present zircon U–Pb ages for one amphibole gneiss (13QL- Zircons in sample 13QL-03 are euhedral to subhedral, with 01), one biotite plagioclase gneiss (13QL-02) and one TTG gneiss length varying from 50 to 200 lm and length to width ratio of (13QL-03) from the S-NCC, one meta-sedimentary rock (13QL-23) 2:1–1:1. Most of the zircons show clear oscillatory zoning in CL and two migmatites (13QL-46, 13QL-49) from the NQB, and two images (Fig. 7a), suggesting a magmatic origin. A total of 29 spots meta-sedimentary rocks (13QL-36, 13QL-37) from the WGU. The from 29 zircons were analyzed from this rock. All of the spots form age results are given in Supplementary Table 2. a coherent tight group on the concordia (Fig. 9c) and display weighted mean 207Pb/206Pb age of 1897 ± 15 Ma (MSWD = 1.2) 5.2.1. S-NCC with Th/U = 0.05–0.58. Zircons in sample 13QL-01 are euhedral to subhedral, with length varying from 50 to 400 lm and aspect ratio of 4:1–1:1. Most of the zircons show clear oscillatory zoning in CL images 5.2.2. NQB (Fig. 7a). A total of 29 spots were analyzed from this rock. Zircons in sample 13QL-23 (schist) from the KPG are anhedral Nineteen spots cluster as a coherent tight group on the concordia to subhedral and show subrounded to well-rounded shapes, dis- (Fig. 9a), yielding a weight mean 207Pb/206Pb age of 2285 ± 17 Ma playing detrital zircon characters. These zircons are colorless or (MSWD = 0.44), with Th/U ratios of 0.41–1.58 except one zircon light brown with small size (40–150 lm) and aspect ratio of 2:1– grain (Th/U = 0.06). Nine spots yield a weight mean 207Pb/206Pb 1:1. In CL images, most zircons show clear oscillatory zoning or

Fig. 10. Zircon U–Pb concordia plots for sample 13QL-36, 13QL-37, 13QL-46 and 13QL-49 from the QOB. 552 L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 heterogeneous fractured domains (Fig. 7d). A total of 30 spots from display detrital rounded feature. The zircons show clear oscillatory 30 zircons were analyzed from this rock. Twenty-one zircons zoning or heterogeneous domains in CL images (Fig. 8a and b). In define dominant 937–1131 Ma ages with peak at 1035 Ma. This sample 13QL-36, the dominant population shows an age range of rock also contains five older zircons (2463 Ma, 1668–1311 Ma) 887–805 Ma with peak at 824 Ma (Fig. 10c). In sample 13QL-37, fif- and four Neoproterozoic zircons (601–865 Ma) which are concor- teen zircons define dominant 854–803 Ma ages with peak at dant (Fig. 9d). The youngest detrital zircon age of 601 ± 3 Ma con- 829 Ma (Fig. 10d). The remaining concordant zircons of these strain the maximum depositional time. two samples define two age populations at 2460–1802 Ma and Zircons in the melanosomes (13QL-46, 13QL-49) show similar 1180–1000 Ma, suggesting Paleoproterozoic and Mesoproterozoic features, colorless or light brown, anhedral to subhedral, with a sources. size range of 50–200 lm and aspect ratio of 2:1–1:1. In CL images, most zircons show core-rim texture, with the cores showing clear 5.3. Zircon Hf isotopes oscillatory zoning or dark heterogeneous domains and the rims display light color without zoning. Several zircons show homoge- In situ Hf isotopic analyses were carried out in the adjacent neous gray color which is similar to the rims. In sample 13QL-46, domains of the same zircons where the U–Pb dating had done. twenty-seven of the 29 analyses cluster as a coherent tight group The results are given in Supplementary Table 3 and plotted in 206 238 and yield weighted mean Pb/ U age of 391.0 ± 2.3 Ma Fig. 11. All samples show fLu/Hf values vary from 0.88 to 1.00, (MSWD = 2.6) (Fig. 10a) with Th/U = 0.01–0.80. The remaining which are obviously lower than the mafic crust (fLu/Hf = 0.34, two zircons exhibit concordant age at 478 Ma and 614 Ma. In sam- Amelin et al., 2000) and sialic crust (fLu/Hf = 0.72, Vervoort and ple 13QL-49, a total of 22 spots were analyzed from 22 zircons. The Jonathan Patchett, 1996). Therefore, the two-stage model age is age result can be divided into two groups except for one inherited applied to evaluate the time of source material extraction from 206 238 zircon (804 Ma), yielding weighted mean Pb/ U ages of the depleted mantle or the residence time of the source material 405.0 ± 3.7 Ma (MSWD = 1.7) and 378.5 ± 4.8 Ma (MSWD = 2.3), in the crust (Blichert-Toft and Albarède, 1997). respectively (Fig. 10b). 5.3.1. S-NCC Ten zircons of sample 13QL-01 show moderate initial 5.2.3. WGU 176Hf/177Hf ratios of 0.281060–0.281221, with e (t) values varying Zircon grains in the WGU metasediments (13QL-36, 13QL-37) Hf from 10.3 to 4.6 with an average of 7.0. The Hf crustal model are relatively small (30–150 lm) with length to width ratio of ages (TC ) show a range of 3088–3437 Ma, implying that the par- 2:1–1:1. These zircons are colorless or light brown, transparent DM ental magma was probably derived from the reworked Archean to translucent and anhedral to subhedral. Most of the grains crust. Eight zircons were analyzed from sample 13QL-02 for Lu–Hf isotopes. Three spots at the age of 2510 Ma are dominated by posi- 176 177 tive eHf(t) values (1.2–4.0) with initial Hf/ Hf ratios ranging from 0.281244 to 0.281309, and show Hf crustal model ages C (TDM) of 2766–2937 Ma (mean 2858 Ma), suggesting Archean juve- nile crustal source. The remaining five spots show eHf(t) ranging from 12.3 to 1.1 with initial 176Hf/177Hf ratios (0.281236–

0.281357). The Hf depleted model ages (TDM) are between C 2634 Ma and 2819 Ma, and Hf crustal model ages (TDM) varies from 2811 Ma to 3316 Ma. The results suggest a mixed source from both juvenile and Archean crust. Nine zircons from sample 13QL-03 show moderate initial 176Hf/177Hf ratios of 0.281345–0.281421 which are dominated by

negative eHf(t) values (8.6 to 5.9). The Hf crustal model ages C (TDM) range from 2889 Ma to 3057 Ma, suggesting that the source material was evolved from Mesoarchean crust.

5.3.2. NQB 207 206 Fig. 11. eHf(t) versus Pb/ Pb age diagram of zircons in varied rocks from the Ten zircons were analyzed from sample 13QL-23 for Lu–Hf iso- QOB. topes. Eight zircons show initial 176Hf/177Hf ratios of 0.281543–

Table 1 Details of samples from the QOB used for this study.

Sample no. Group Coordinate Rock type Mineral assemblage 13QL-01 THG N34°37.000; E109°59.810 Amphibole gneiss Hbl + Pl + Qtz + Bt 13QL-02 THG N34°37.050; E109°59.880 Biotite plagioclase gneiss Qtz + Pl + Bt + Hbl 13QL-03 TGG N34°30.410; E109°57.710 TTG gneiss Qtz + Pl + Bt 13QL-04 TGG N34°30.380; E109°57.630 Amphibolite Qtz + Pl + Hbl + Bt 13QL-23 KPG N34°00.100 E109°49.070 Schist Qtz + Pl + Bt 13QL-36 WGU N33°34.420; E110°40.010 Schist Qtz + Pl + Bt 13QL-37 WGU N33°34.470; E110°40.050 Schist Qtz + Pl + Bt + Chl + Grt 13QL-41 WGU N33°34.480; E110°40.070 Schist Qtz + Pl + Bt + Hbl 13QL-44 WGU N33°34.530; E110°40.110 Greenschist Chl + Ep + Hbl + Pl 13QL-46 Migmatite N33°57.770; E108°50.650 Melanosome Qtz + Pl + Bt + Grt 13QL-49 Migmatite N33°57.750; E108°50.590 Melanosome Qtz + Pl + Bt

Mineral abbreviations: Hbl – hornblende; Pl – plagioclase; Qtz – quartz; Bt – biotite; Chl – chlorite; Grt – garnet. L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 553

Table 2 Compilation of age data (Taihua Group) from the study area.

Sample no. Position Rock Method Age (Ma) Interpretation References 13QL-01 Xiaoqinling Amphibole gneiss U–Pb zircon LA-ICPMS 2285 ± 17, 2163 ± 26 Formation This study 13QL-02 Xiaoqinling Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 2510 ± 22, 2342 ± 24 Formation This study xql0909-1 Xiaoqinling Granitic gneiss U–Pb zircon LA-ICPMS 2346 ± 28 Formation Yu et al. (2013) QL0703-1 Xiaoqinling Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 1912 ± 13 Metamorphism Shi et al. (2011) QL0703-2 Xiaoqinling Two-fieldspar gneiss U–Pb zircon LA-ICPMS 2469 ± 12 Formation Shi et al. (2014) S2 Xiaoqinling Plagioclase amphibole gneiss U–Pb zircon SIMS 1823 ± 4 Metamorphism Wang et al. (2012) S3 Xiaoqinling Plagioclase amphibole gneiss U–Pb zircon SIMS 2293 ± 7 Formation Wang et al. (2012) S33 Xiaoqinling Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 1941 ± 13 Metamorphism Wang et al. (2012) S51 Xiaoqinling Plagioclase amphibole gneiss U–Pb zircon LA-ICPMS 1852 ± 23 Metamorphism Wang et al. (2012) S24a Xiaoqinling Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 2367 ± 31 Formation Wang et al. (2013) 1869 ± 39 Metamorphism Wang et al. (2013) S25 Xiaoqinling Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 2497 ± 32, 2297 ± 44 Formation Wang et al. (2013) 1848 ± 20 Metamorphism Wang et al. (2013) S31 Xiaoqinling Biotite two-feldspar gneiss U–Pb zircon LA-ICPMS 2333 ± 24 Formation Wang et al. (2013) S34 Xiaoqinling Biotite two-feldspar gneiss U–Pb zircon LA-ICPMS 2307 ± 14 Formation Wang et al. (2013) QL0701 Xiaoqinling Biotite gneiss U–Pb zircon LA-ICPMS 2300–2500 Formation Xu et al. (2009) 08LF2 Xiaoqinling Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 1928–2128 Deposition Diwu et al. (2014) 04TY09 Xiaoqinling Granitic gneiss U–Pb zircon LA-ICPMS 2428 ± 24 Formation Diwu et al. (2014) 01TH10 Xiaoqinling Granitic gneiss U–Pb zircon LA-ICPMS 2362 ± 27 Formation Diwu et al. (2014) 01TH17 Xiaoqinling Dioritic gneiss U–Pb zircon LA-ICPMS 2467 ± 19 Emplacement Diwu et al. (2014) THB05-103 Xiaoqinling Tonalitic gneiss U–Pb zircon SHRIMP 2164 ± 16 Formation Huang et al. (2013) THH05-97 Xiaoqinling Tonalitic gneiss U–Pb zircon SHRIMP 2477 ± 8 Formation Huang et al. (2013) THH08-62 Xiaoqinling Granitic gneiss U–Pb zircon SIMS 2277 ± 28 Formation Huang et al. (2013) 1918 ± 17 Metamorphism Huang et al. (2013) THQ08-76 Xiaoqinling Tonalitic gneiss U–Pb zircon SIMS 2311 ± 3 Formation Huang et al. (2013) THQ08-82 Xiaoqinling Granitic gneiss U–Pb zircon SIMS 2307 ± 5 Formation Huang et al. (2013) 01LSTH39 Lingtong Granitic gneiss U–Pb zircon LA-ICPMS 2321 ± 9 Formation Diwu et al. (2014) 01LSTH40 Lingtong Trondhjemitic gneiss U–Pb zircon LA-ICPMS 2316 ± 14 Emplacement Diwu et al. (2014) 01TH04 Lantian Granodiorite gneiss U–Pb zircon LA-ICPMS 2313 ± 13 Emplacement Diwu et al. (2014) 04MC10 Xiong’ershan Dioritic gneiss U–Pb zircon LA-ICPMS 2315 ± 17 Formation Diwu et al. (2014) 04MC14 Xiong’ershan Amphibolitic gneiss U–Pb zircon LA-ICPMS 2313 ± 11 Formation Diwu et al. (2014) 04MC14 Xiong’ershan Amphibolitic gneiss U–Pb zircon LA-ICPMS 1950 ± 20 Metamorphism Diwu et al. (2014) THX05-41 Xiong’ershan Tonalite gneiss U–Pb zircon SHRIMP 2065 ± 23 Formation Huang et al. (2012) THX05-45 Xiong’ershan K-feldspar granite gneiss U–Pb zircon SHRIMP 2188 ± 26 Formation Huang et al. (2012) THX08-57 Xiong’ershan Granodiorite gneiss U–Pb zircon SIMS 2318 ± 8 Formation Huang et al. (2012) THX08-54 Xiong’ershan Diorite gneiss U–Pb zircon SIMS 2305 ± 23 Formation Huang et al. (2012) THX08-54 Xiong’ershan Diorite gneiss U–Pb zircon SIMS 2169 ± 6 Metamorphism Huang et al. (2012) Q1 Xiong’ershan Amphibolite U–Pb zircon LA-ICPMS 2100–2400 Formation Xu et al. (2009) HN804 Xiong’ershan Plagioclase amphibole gneiss U–Pb zircon SIMS 2304 ± 12 Formation Jiang et al. (2011) 1939 ± 19 Metamorphism Jiang et al. (2011) Yu21 Xiong’ershan Plagioclase amphibole gneiss U–Pb zircon SIMS 2321 ± 8 Formation Jiang et al. (2011) 1958 ± 32 Metamorphism Jiang et al. (2011) Yu19 Xiong’ershan Plagioclase amphibole gneiss U–Pb zircon SIMS 2336 ± 10 Formation Jiang et al. (2011) 1967 ± 32 Metamorphism Jiang et al. (2011) Yu23 Xiong’ershan Plagioclase amphibole gneiss U–Pb zircon SIMS 2305 ± 4 Formation Jiang et al. (2011) 1938 ± 9 Metamorphism Jiang et al. (2011) MC-12 Xiong’ershan Tonalitic gneiss U–Pb zircon LA-ICPMS 2336 ± 13 Formation Diwu et al. (2007) MC-13 Xiong’ershan Tonalitic gneiss U–Pb zircon LA-ICPMS 2316 ± 16 Formation Diwu et al. (2007) L51 Lushan TTG gneiss U–Pb zircon SIMS 2828 ± 14 Formation Lu et al. (2014) 1934 ± 7 Metamorphism Lu et al. (2014) L54 Lushan TTG gneiss U–Pb zircon SIMS 2897 ± 28 Formation Lu et al. (2014) 1915 ± 14 Metamorphism Lu et al. (2014) L55 Lushan TTG gneiss U–Pb zircon SIMS 2778 ± 3 Formation Lu et al. (2014) 1940 ± 15 Metamorphism Lu et al. (2014) L10 Lushan Amphibolite U–Pb zircon SIMS 1927 ± 7 Metamorphism Lu et al. (2014) L56 Lushan Amphibolite U–Pb zircon SIMS 1918 ± 5 Metamorphism Lu et al. (2014) L50 Lushan Gneissic granite U–Pb zircon SIMS 1928 ± 5 Metamorphism Lu et al. (2014) LS0417-1 Lushan Amphibolite U–Pb zircon SHRIMP 2838 ± 35, 2792 ± 11 Formation Liu et al. (2009a) LS0417-2 Lushan Gneissic biotite tonalite U–Pb zircon SHRIMP 2845 ± 23, 2776 ± 20 Formation Liu et al. (2009a) LS0417-3 Lushan Gneissic amphibolite U–Pb zircon SHRIMP 2829 ± 18, 2772 ± 22 Formation Liu et al. (2009a) LS0417-4 Lushan Gneissic hornblend–biotite tonalite U–Pb zircon SHRIMP 2832 ± 11, 2772 ± 17 Formation Liu et al. (2009a) TW006/1 Lushan Graphite garnet sillimanit gneiss U–Pb zircon SHRIMP 2010–2730 Formation Wan et al. (2006) 1844 ± 66 Metamorphism Wan et al. (2006) Lushan Tonalitic gneiss U–Pb zircon SHRIMP 2841 ± 6, 2806 ± 7 Formation Kröner et al. (1988) LSP01 Lushan Amphibolite U–Pb zircon LA-ICPMS 2755 ± 8 Formation Lin (2006) LSX04 Lushan Amphibolite U–Pb zircon LA-ICPMS 2763 ± 13, Formation Lin (2006) LSX05 Lushan Amphibolite U–Pb zircon LA-ICPMS 2812 ± 27 Formation Lin (2006) LSP07 Lushan Trondhjemitic gneiss U–Pb zircon LA-ICPMS 2761 ± 11 Formation Lin (2006) LSP08 Lushan Trondhjemitic gneiss U–Pb zircon LA-ICPMS 2757 ± 59 Formation Lin (2006) LSP13 Lushan Tonalitic gneiss U–Pb zircon LA-ICPMS 2766 ± 14 Formation Lin (2006) LSP24 Lushan Amphibolite U–Pb zircon LA-ICPMS 1932 ± 48 Formation Lin (2006) LSP26 Lushan Amphibole anorthosite U–Pb zircon LA-ICPMS 2759 ± 52 Formation Lin (2006) TH-05 Lushan Amphibolite U–Pb zircon LA-ICPMS 2794 ± 5 Formation Diwu et al. (2010) TH-07 Lushan Trondhjemitic gneiss U–Pb zircon LA-ICPMS 2763 ± 4 Formation Diwu et al. (2010)

(continued on next page) 554 L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559

Table 2 (continued)

Sample no. Position Rock Method Age (Ma) Interpretation References TH-13 Lushan Tonalitic gneiss U–Pb zircon LA-ICPMS 2791 ± 7 Formation Diwu et al. (2010) TH-29 Lushan Amphibolite U–Pb zircon LA-ICPMS 2752 ± 5 Formation Diwu et al. (2010) THL05-2 Lushan Tonalitic gneiss U–Pb zircon SHRIMP 2765 ± 13 Formation Huang et al. (2010) THL05-21 Lushan Tonalitic gneiss U–Pb zircon SHRIMP 2723 ± 9 Formation Huang et al. (2010)

207 206 0.282003, eHf(t) values of 18.3 to 4.9 and Hf crustal model ages groups with weighted mean Pb/ Pb age of 2285 ± 17 Ma and of 2184–2810 Ma, whereas two zircons show values of 0.282148– 2163 ± 26 Ma. The biotite plagioclase gneiss (13QL-02) yielded 0.282173, 0.8–1.7 and 1772–1830 Ma, respectively. The results three groups of ages at 2510 ± 22 Ma, 2342 ± 24 Ma and suggest that the source material was mainly derived from 2155 ± 70 Ma, respectively, interpreted as reflecting the time of Paleoproterozoic juvenile crust with minor mixed Archean– arc magmatism in the southern segment of the TNCO. Paleoproterozoic components. Furthermore, available zircon U–Pb ages from the THG in the Nine zircons from the ten analyses of sample 13QL-46 show ini- Lantian–Xiaoqinling, Xiong’ershan and Lingtong areas revealed tial 176Hf/177Hf ratios varying from 0.282777 to 0.282869. The prolonged magmatism during 2477 Ma and 2065 Ma (Table 2) eHf(t) values are in the range of 8.6–16.7 and Hf crustal model ages with a peak at 2320 Ma (Fig. 12a) (e.g. Yu et al., 2013; Huang C (TDM) vary from 532 Ma to 833 Ma. One zircon has a negative eHf(t) et al., 2013; Diwu et al., 2014). C value (9.9) with TDM of 2012 Ma. The results suggest a mixed The results of zircon analysis from sample 13QL-02 on rim source from major Neoproterozoic juvenile crust with minor domains or on the structureless light gray zircons (Fig. 7b) yielded reworked Paleoproterozoic components. weighted mean 207Pb/206Pb age of 1930 ± 31 Ma with Th/U = 0.02– Five zircons in sample 13QL-49 show broad initial 176Hf/177Hf 0.29, interpreted as the metamorphic age of the THG. The results ratios of 0.282011–0.282606, the eHf(t) values are varying from are in accordance with the previous study on different rock types C 18.1 to 3.0 (mean 4.3). The Hf crustal model ages (TDM) show of the THG, showing metamorphic ages from 1967 Ma to a range of 2541–1207 Ma, suggesting that the parental magma 1823 Ma (Table 2) (e.g. Jiang et al., 2011; Wang et al., 2012; Lu was probably derived from Mesoproterozoic juvenile crust with et al., 2014). Compared to the widespread metamorphism of minor reworked Paleoproterozoic–Mesoproterozoic components. 1.89–1.80 Ga in TNCO (e.g. Guo et al., 2005; Zhao et al., 2008; Trap et al., 2009), the 1.96–1.82 Ga ages from the THG are slightly 5.3.3. WGU older, although these results suggest that the initial collision The zircons grains in sample 13QL-36 are too tiny to do Lu–Hf between the Western and Eastern Block in the southern segment isotopic analyses. of the TNCO is coeval with the 1.96–1.92 Ga amalgamation of the Six zircons in sample 13QL-37 show initial 176Hf/177Hf ratios Yinshan and Ordos Blocks along the Inner Mongolia Suture Zone ranging from 0.281716 to 0.282265. The predominant negative (Santosh et al., 2007; Yin et al., 2011) and the 1.95 Ga collision eHf(t) values (17.2 to 0.1) and wide Hf crustal model ages of the Jiao-Liao-Ji Belt (Luo et al., 2008; Tam et al., 2011). These col- (1727–2796 Ma), indicate that the materials were evolved from lisional events occurred within the period (2.1–1.8 Ga) of the Neoarchean–Paleoproterozoic crust.

6. Discussion

6.1. Archean crustal growth record from the S-NCC

There is a board consensus that the NCC is formed by the amal- gamation of the Eastern and Western Blocks along the TNCO (Zhao et al., 2005, 2012; Santosh, 2010; Zhai and Santosh, 2011). The NCC has been considered to be composed of discrete Archean to Paleoproterozoic basement (Zhao et al., 2005), with the relatively older basement rocks (2.8–2.7 Ga) distributed in the Eastern Block at Taishan (Jahn et al., 1988) and Jiaodong Peninsula (Jahn et al., 2008). As shown in Table 2, the THG in the Lushan area witnessed widespread magmatism at ca. 2.85–2.71 Ga (Fig. 12a). Zhai et al. (2010) proposed two main crustal growth episodes (2.9–2.7 Ga and 2.55–2.50 Ga) in the NCC. Like in other parts of the Eastern Block, the THG in the Lushan area show tectonic affinity with the Eastern Block, and record the history of 2.85–2.71 Ga crustal growth of the NCC (Huang et al., 2013).

6.2. Neoarchean–Paleoproterozoic arc magmatic and collisional metamorphic record from the S-NCC

The available zircon U–Pb ages record major pulses of arc mag- matism within the TNCO during 2.55–1.92 Ga (e.g. Zhao et al., 2005, 2008; Trap et al., 2012; Santosh et al., 2014, in preparation; Yang and Santosh, 2014). In the THG from the Fig. 12. Zircon U–Pb age spectra and relative probability plots of the THG (a), KPG Xiaoqinling area, the amphibole gneiss (13QL-01) show two age (b), QLG (c) and migmatite from the NQB (d). Data from Tables 2–4. L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 555 global scale assembly of the Columbia supercontinent (Rogers and 2010; Bader et al., 2013a). The large scale late Mesoproterozoic Santosh, 2002, 2009; Zhao et al., 2005, 2009; Nance et al., 2014). to early Neoproterozoic 1100–950 Ma magmatic activities The zircon U–Pb age data on the TTG gneiss (13QL-03) show an recorded by the QLG and KPG (Fig. 12b) are absent in the NCC additional tectonothermal event associated with the integrated and SCC, whereas abundant early Neoproterozoic (980–930 Ma) TGG during Paleoproterozoic (1897 ± 15 Ma). From zircon Lu–Hf syn-collisional or post-collisional granitoid rocks are exposed in isotopic results, the biotite plagioclase gneiss (13QL-02) from the the QLG (Zhang et al., 2004; Wang et al., 2005; Lu et al., 2005; THG and the TTG gneiss (13QL-03) from the TGG show coherent Chen et al., 2006, 2007). Dong et al. (2014) presented a new tec- C TDM range from 2766 Ma to 3067 Ma (Supplementary Table 3, tonic model which proposed that the southward subduction of Fig. 11), suggesting similar felsic parental magma sources from the Kuanping Ocean led to the amalgamation of the NQB with the reworked Mesoarchean crustal components. The amphibole the NCC at ca. 900 Ma. Thus, it is reasonable to suggest that the gneiss (13QL-01) show dominant negative eHf(t) values varying 1100–950 Ma magmatic activity recorded by the QLG and KPG, C from 10.3 to 4.6 and TDM range of 3088–3437 Ma, suggesting together with the early Neoproterozoic granitoid rocks were magma derivation from Paleoarchean–Mesoarchean components. formed by the southward subduction and collision related arc magmatic system. These arc magmatic events are coeval with the 6.3. Mesoproterozoic tectono-thermal event and Neoproterozoic tectonics associated with the timing of assembly of the Rodinia depositional record from the NQB supercontinent (Li et al., 2008). The tectonic affinity of the NQB is controversial. Some workers The KPG mainly comprises ophiolitic suites and metasedimen- suggested that the NQB is a part of the S-NCC, largely based on the tary rocks. Dong et al. (2014) reported zircon U–Pb age of evidence of island arc related metavolcanic–metasedimentary 1445 ± 60 Ma from the Kuanping ophiolite and considered it to rocks and ophiolitic suites preserved in NQB (Zhang et al., 2001). represent the formation time of the Kuanping Ocean. For the There are also marked similarities between the THG and QLG (Xu metasedimentary rocks, previous studies suggested depositional and Wang, 1990), with similar Nd model ages for the rocks from ages of 690–600 Ma (Diwu et al., 2010; Zhu et al., 2011) or 500– the S-NCC and the NQB (Zhang et al., 1995b). Some studies consid- 400 Ma (Lu et al., 2009). Thus, the KPG shows a complex collage ered the NQB as derived from the SCC based on the evidence of of different rock types. Zircon U–Pb ages of a biotite schist high radioactive Pb isotope content of the NQB (Zhu, 1993), ages (13QL-23) show the largest range in ages of 937–1131 Ma, with (Xue et al., 1996; Shi et al., 2009), occurrence of rock types below peak at 1035 Ma, and the youngest detrital zircon age the QLG (Huang and Wu, 1992) and crust–mantle evolution fea- (601 ± 3 Ma) constrains the maximum depositional time. tures (Zhang et al., 1998). On the other hand, some others sug- The zircon U–Pb age results in previous studies (Table 3) show gested that the NQB was a micro-continent based on the that the QLG was formed in late Mesoproterozoic to early evidence of high initial eNd(t) and Pb isotopic ratio of the NQB Neoproterozoic (1015–850 Ma) (Shi et al., 2009; Yang et al., (Dong et al., 2003) and existence of the Kuanping ophiolite (Dong

Table 3 Compilation of age data (Kuanping Group and Qinling Group) from the study area.

Sample no. Position Rock Method Age (Ma) Interpretation References Kuanping Group 027NB-10 Xieyuguan Amphibolite U–Pb zircon LA-ICPMS 1445 ± 60 Formation Dong et al. (2014) QL0708-1 Lushi Two-mica schist U–Pb zircon LA-ICPMS 552 ± 8 Deposition Shi et al. (2013) QL0708-2 Lushi Biotite schist U–Pb zircon LA-ICPMS 570 Deposition Shi et al. (2013) QL0710 Lushi Meta-sandstone U–Pb zircon LA-ICPMS 450 ± 6 Deposition Shi et al. (2013) D129-1TW Tianshui Plagioclase amphibolite U–Pb zircon LA-ICPMS 1753 ± 14 Formation He et al. (2007) 415–383 Metamorphism He et al. (2007) QD04-58 Shangluo Metabasic volcanic rock U–Pb zircon SHRIMP 611 ± 13 Formation Yan et al. (2008) Metasedimentary rock U–Pb zircon LA-ICPMS 500–400 Deposition Lu et al. (2009) Meta-basalt U–Pb zircon LA-ICPMS 500 Metamorphism Lu et al. (2009) KP-05 Luonan Quartz-mica schist U–Pb zircon LA-ICPMS 600 ± 68 Deposition Diwu et al. (2010) KP-06 Luonan Quartz-mica schist U–Pb zircon LA-ICPMS 689 ± 59 Deposition Diwu et al. (2010) KP-08 Ganyuwan Quartz-mica schist U–Pb zircon LA-ICPMS 632 ± 57 Deposition Diwu et al. (2010) 09LY Huxian Greenschist U–Pb zircon LA-ICPMS 943 ± 6 Formation Diwu et al. (2010) 08HN46, 49, 60 Luanchuan Quartz-mica schist U–Pb zircon LA-ICPMS 640 Deposition Zhu et al. (2011) Q12 Lushi Gneissic quartzite U–Pb zircon LA-ICPMS 950 ± 58 Formation Bader et al. (2013a) Q34 Baoji Orthogneiss U–Pb zircon LA-ICPMS 216 ± 6 Formation Bader et al. (2013a) Qinling Group QL0738 Shangnan Gneiss U–Pb zircon LA-ICPMS 971 ± 21 Formation Shi et al. (2009) QL0752 Ningshan Gneiss U–Pb zircon LA-ICPMS 843 ± 37 Formation Shi et al. (2009) QL0715-2 Yichuan Biotite plagioclase amphibolite U–Pb zircon LA-ICPMS 907 ± 63 Formation Shi et al. (2009) QL0754-1 Weiziping Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 426 ± 6 Metamorphism Shi et al. (2009) 08HN18 Neixiang Migmatite U–Pb zircon LA-ICPMS 975 ± 10 Formation Yang et al. (2010) 08HN31 Neixiang Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 1637 ± 54, 1350 ± 92 Formation Yang et al. (2010) 08HN62 Lushi Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 960 ± 4 Formation Yang et al. (2010) 08HN77 Danfeng Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 1414 ± 73 Formation Yang et al. (2010) 08HN79 Danfeng Biotite plagioclase gneiss U–Pb zircon LA-ICPMS 951 ± 5, 855 ± 11 Formation Yang et al. (2010) U–Pb zircon LA-ICPMS 473 ± 10 Metamorphism Yang et al. (2010) Q124 Tianshui K-feldspar orthogneiss U–Pb zircon LA-ICPMS 853 ± 17 Formation Bader et al. (2013a) D415 Nanyang Granodioritic gneiss U–Pb zircon LA-ICPMS 776 ± 15 Formation Bader et al. (2013a) U–Pb zircon LA-ICPMS 452 ± 8 Metamorphism Bader et al. (2013a) Shangnan Retrograde eclogite U–Pb zircon LA-ICPMS 480 ± 6 Metamorphism Cheng et al. (2011) Q123 Granodiorite U–Pb zircon SIMS 473 ± 7 Crystallization Bader et al. (2013b) YLG0807 Xixia Amphibolite U–Pb zircon SIMS 954 ± 98 Formation Liu et al. (2013) YLG0812 Xixia Amphibolite U–Pb zircon SIMS 845 ± 69 Formation Liu et al. (2013) 556 L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559

Table 4 Compilation of age data (migmatization) from the study area.

Sample no. Position Rock Method Age (Ma) Interpretation References 10QL07 Danfeng Leucosome U–Pb zircon LA-ICPMS 438 ± 2 Migmatization Liu et al. (2014) 10QL24 Danfeng Leucosome U–Pb zircon LA-ICPMS 436 ± 6 Migmatization Liu et al. (2014) 10QL35 Danfeng Leucosome U–Pb zircon LA-ICPMS 443 ± 2 Migmatization Liu et al. (2014) 10QL91 Danfeng Leucosome U–Pb zircon LA-ICPMS 440 ± 2 Migmatization Liu et al. (2014) 10QL101 Danfeng Leucosome U–Pb zircon LA-ICPMS 431 ± 3 Migmatization Liu et al. (2014) QL53 Danfeng Migmatitic granite U–Pb zircon LA-ICPMS 402 ± 6 Migmatization Faure et al. (2008) QL123 Shangnan Leucosome U–Pb zircon LA-ICPMS 414 ± 20 Migmatization Faure et al. (2008) Qy-04 Qingyouhe Migmatitic granite U–Pb zircon LA-ICPMS 455 ± 5 Migmatization Dong et al. (2011a) ZZ04-3 Dahe Melanosome U–Pb zircon SHRIMP 428 ± 3 Migmatization Liu et al. (2011) 08TB01 Zhouzhuang Leucosome U–Pb zircon LA-ICPMS 428 ± 4 Migmatization Wang et al. (2011) Q33 Danfeng Garnet-sillimanite gneiss melanosome U–Pb zircon LA-ICPMS 502 ± 6 Crystallization Bader et al. (2013b) 76162H Qingyouhe Leucogranite Th–Pb monazite SIMS 397 ± 5 Migmatization Bader et al. (2013b) 76163B Qingyouhe Garnet-gneiss melanosome Th–Pb monazite SIMS 381 ± 7 Migmatization Bader et al. (2013b) 76163F Qingyouhe Garnet schist leucosome U–Pb zircon LA-ICPMS 464 ± 3 Migmatization Bader et al. (2013b) 75244C Danfeng Postmigmatitic granite Th–Pb monazite SIMS 395 ± 3 Migmatization Bader et al. (2013b)

et al., 2014), metasediment geochemistry (Ouyang and Zhang, and migmatization in the QLG, and fall within the broad range of 1996) and zircon U–Pb geochronology (Yang et al., 2010; Diwu 500–380 Ma recognized for migmatization event in the NQB. et al., 2012; Shi et al., 2013). The prominent Grenvillian (early 7. Conclusions Neoproterozoic) magmatic event as recorded by the KPG and QLG (Fig. 12b and c) suggest that the NQB was a discrete micro- (1) The oldest ages from the THG correspond with the Archean continent during this time. (2.85–2.71 Ga) crustal growth within the S-NCC. Neoarchean–Paleoproterozoic (2.51–2.06 Ga) arc magmatic and 1.96–1.82 Ga metamorphic events recorded in this 6.4. Tectonic affinity of the WGU study also correspond well with similar ages reported from the NCC. The felsic gneiss and mafic gneiss show different The WGU occurring along the southern side of the SSZ has parental magma derived from the reworked Mesoarchean undergone lower amphibolite facies metamorphism. A previous crustal components and Paleoarchean–Mesoarchean crust, study reported Sm–Nd age of 1382 Ma from the South Qinling respectively. Belt (Pei et al., 1998). New zircon U–Pb age data on two represen- (2) The QLG and KPG from the NQB record widespread tative metasedimentary rocks in this study show age range of 854– Grenvillian-aged magmatism, implying that the NQB might 803 Ma (peaks at 829–824 Ma), and also define age populations of have been a micro-continent during the Mesoproterozoic 2460 Ma, 1802 Ma and 1180–1000 Ma. Widespread and early Neoproterozoic. Neoproterozoic magmatic events (peaking at 825 Ma), as well (3) The melanosomes of the migmatite from the QLG exhibit zir- as Neoarchean and Paleoproterozoic events (2.5 and 1.8 Ga) have con U–Pb ages of 405–379 Ma, coinciding with the been recorded from the Northern South Qinling Belt and SCC (e.g. migmatization in the NQB during 500–380 Ma. Liu et al., 2008; Wang et al., 2010). Although the North Qinling belt (4) The WGU exposed at the southern side of the SSZ show mul- is dominated by Grenvillian-aged magmatism (1100–950 Ma) (e.g. tiple age groups, especially of 854–803 Ma (peaks at 829– Shi et al., 2009; Yang et al., 2010), without Early Paleozoic age pop- 824 Ma), suggesting SCC as the potential provenance. ulation which is typical of the NQB, the WGU is exceptional, and was not derived from the NQB. Therefore, the sedimentary units in the WGU might have tectonic affinity with the SCC. Acknowledgements

6.5. Late Paleozoic migmatization record from the NQB We thank Guest Editor Prof. Sanghoon Kwon and two referees for constructive comments. We thank Dengfeng He, Bo Zhou, Migmatites with melanosome and leucosome have been widely Qing Li and Xueming Teng for their kindly help in the field and reported in the NQB. Zircon U–Pb dating method has been reliably U–Pb dating analysis. This study was jointly supported through applied to constrain the age of migmatization and partial melting the Project to M. Santosh from Open Fund of SKLCD of the (Foster et al., 2001; Wu et al., 2007). The available zircon U–Pb ages Northwest University, China, and the Talent Award to M. Santosh of migmatites from the NQB range from 520 Ma to 380 Ma under the 1000 Talents Plan of the Chinese Government, and (Table 4; Fig. 12d) (Faure et al., 2008; Dong et al., 2011a; Liu NSFC Fund to Y.P. Dong (Nos. 41225008, 41190074 and 41421002). et al., 2011, 2014; Wang et al., 2011; Bader et al., 2013b). However, migmatization in orogenic belt are frequently associated Appendix A. Supplementary material with granulite metamorphism (Wu and Zheng, 2013 and refer- ences therein). Liu et al. (2014) suggested that the 515–480 Ma Supplementary data associated with this article can be found, in age group is associated with the (ultra)-high pressure metamor- the online version, at http://dx.doi.org/10.1016/j.jseaes.2015.03. phism of the NQB. Wu and Zheng (2013) summarized the ages of 033. migmatization in the NQB to be in the range of ca. 400–450 Ma. Zircon LA-ICPMS U–Pb dating in this study on two typical mel- References anosomes (13QL-46, 13QL-49) from the migmatite of the QLG shows consistent ages. Zircons in sample 13QL-46 yield a weighted Amelin, Y., Lee, D.C., Halliday, A.N., 2000. Early-Middle Archaean crustal evolution mean 206Pb/238U age of 391.0 ± 2.3 Ma whereas those in sample deduced from Lu–Hf and U–Pb isotopic studies of single zircon grains. Geochim. Cosmochim. Acta 64, 4205–4225. 13QL-49 show ages varying from 405.0 Ma to 378.5 Ma. The age Bader, T., Franz, L., Ratschbacher, L., Capitani, C., Webb, A., Yang, Z., Pfänder, J., data (405–379 Ma) are interpreted to record the partial melting Hofmann, M., Linnemann, U., 2013a. The Heart of China revisited: II Early L. Tang et al. / Journal of Asian Earth Sciences 113 (2015) 544–559 557

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