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Research 27 (2015) 1270–1282

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The Alashan Terrane was not part of North China by the Late Devonian: Evidence from detrital U–Pb geochronology and Hf isotopes

Wei Yuan a,b, Zhenyu Yang c,d,a,⁎ a School of Sciences and Engineering, Nanjing University, Nanjing 210093, China b Wuxi Research Institute of Petroleum Geology, SINOPEC, Wuxi, Jiangsu 214126, China c Key Laboratory of Paleomagnetism and Tectonic Reconstruction, Ministry of Land and Resource, Beijing 100081, China d Institute of Geomechanics , Chinese Academy of Geological Sciences, Beijing, 100081, China article info abstract

Article history: The relationship between the Alashan Terrane and North China is a contentious issue given the discovery of al- Received 9 July 2013 lochthonous detrital in Middle flysch sandstones from the southwestern Ordos Margin and Received in revised form 8 November 2013 the large differences in palaeolatitudes between the North China and Tarim . We have collected a suite Accepted 8 December 2013 of Middle to Late Devonian sedimentary rocks from the Niushoushan Mountains at the southeastern margin of Available online 28 December 2013 the Alashan Terrane, adjacent to the western margin of the Ordos Basin of the North China (NCC). U–Pb – – Handling Editor: Z.M. Zhang dating and Lu Hf isotopic studies were carried out on detrital zircons from these rocks. The zircon U Pb ages de- fine five age populations: 0.4–0.7 Ga (peak at 488 Ma), 1.0–1.3 Ga (peaks at 1001 and 1152 Ma), 1.5–1.8 Ga, Keywords: 2.4–2.8 Ga (prominent peak at 2506 Ma and secondary peaks at 2668 and 2796 Ma) and N3.0 Ga (peak at Alashan Terrane 3332 Ma). One detrital zircon yielded a Hadean age of 4022 ± 17 Ma. Zircons with U–Pb age spectra of

North China Craton 2.4–2.7 and N3.0 Ga and their corresponding εHf(t) values are significantly different from those in the NCC, indi- East Gondwana cating that these detrital zircons are not from the NCC, which implies that the Alashan Terrane was not part of Middle to Late Devonian North China until the Middle to Late Devonian. U–Pb age spectra of zircons dated at 1.0–1.3 Ga, 2.4–2.7 Ga, – Zircon U Pb dating and Hf isotopes and N3.0 Ga, and their corresponding Hf isotope data, have a strong similarity with zircons from East Gondwana and the . © 2013 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

1. Introduction these have improved our understanding of the regional geology of these areas. Given its different basement The of China is a mosaic of Precambrian cratonic and geological processes, the existence of the Sino– cratons and terranes separated by orogenic belts, in which the Tarim, Korean–Tarim Craton (Li et al., 1982) has been called into question North China, and Yangtze cratons constitute the basic tectonic on the basis of geological and palaeomagnetic results that suggest framework of China (Lu et al., 2009; Zheng et al., 2013,)(Fig. 1A). The the Tarim Craton had collided with Kazakhstan and by the Alashan Terrane that bridged the southern Central Asian end-, whereas the NCC and Mongolian Orogenic Belt were and the Tarim, Qaidam, and (NCC), is considered distant from Siberia during the Permian– (Enkin et al., as the key in understanding the tectonic of Northern 1992; Yang and Besse, 2001; Xiao et al., 2008, 2010). As such, deter- China. In recent decades, numerous geological and palaeomagnetic mining the affinity of the Alashan Terrane with these two cratons studies have been conducted in the Qilian Orogenic Belt, Hexi corridor, during the Early Palaeozoic might shed light on the tectonic evolution Alashan Terrane, and NCC (e.g., Yang et al., 1992, 1996, 1998; Yang of Northern China. For example, supposed the Alashan Terrane was and Besse, 2001; Geng et al., 2002; Yang et al., 2002, 2004; Zhao et al., the westernmost part of NCC during the Early Palaeozoic, Xiao et al. 2004, 2005; Geng et al., 2007; Xiao et al., 2009; Zhao, 2009; Geng and (2009) proposed the multiple systems that the Alashan Zhou, 2010; Liu et al., 2010; Dan et al., 2012; Liu et al., 2013; Song Terrane and its cover sequence were underthrust southward beneath et al., 2013; Tang et al., 2013; Yang et al., 2014; Zhai and Santosh, the coherent Qilian arc at a low angle, which led to final amalgamation 2013; H.F. Zhang et al., 2013; Zhao and Zhai, 2013; Zheng et al., 2013; between the Alashan Terrane (NCC), Qilian Orogenic belt and Qaidam Zhou and Wilde, 2013; Wang et al., 2013; Zheng et al., 2014), and block in the Late Devonian. However, Ge et al. (2009) argued that a tectono-stratigraphic comparison prior to the between the NCC and Alashan Terrane suggests that suturing between these two ⁎ Corresponding author at: Key Laboratory of Paleomagnetism and Tectonic cratons occurred during the Late Hercynian–Indosinian () Reconstruction, Ministry of Land and Resource, Beijing 100081, China. Tel.: +86 10 68422348; fax: +86 1068422326. in a zone buried under the Tengger Desert. The assumed linkage between E-mail address: [email protected] (Z. Yang). the Alashan Terrane and the NCC in the early Palaeozoic has also been

1342-937X/$ – see front matter © 2013 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved. http://dx.doi.org/10.1016/j.gr.2013.12.009 W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282 1271

Fig. 1. (A) Sketch maps of the tectonic elements of Northern China. (B) Simplified geological map of the study area and adjacent in the Niushoushan Mountains at the southeastern margin of the Alashan Terrane. The star symbol denotes the sampled section. questioned on the basis of the detrital zircon geochronology of Ordovi- not connected with the NCC prior to the Middle Ordovician. Based on cian clastic sediments in the Alashan Terrane (J. Zhang et al., 2011; X.J. field observations, Li et al. (2012) also concluded that amalgamation of Zhang et al., 2011). These results suggest that the Alashan Terrane was the NCC with the Alashan Terrane took place between the Late 1272 W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282

Ordovician and Early Devonian. Thus, the relationship between the NCC red beds intercalated with sparse and marly sandstones. and Alashan Terrane requires further clarification. Vertebrate fossil assemblages that include Remigolepis microcephala The robustness of the zircon U–Pb dating technique, coupled with Pan (sp. Nov.), R. major Pan (sp. nov.), Remigolepis zhongweiensis Pan (sp. Lu–Hf isotope investigations of zircon (Kinny et al., 1991; Kinny and nov.), Remigolepis xiangshanensis Pan (sp. nov.), and Sublepidodendron Maas, 2003; Yang et al., 2006), has led to many studies using these mirabile (Nath.) Hirmer (Pan et al., 1987) indicate a Middle Devonian methods to study cycles and the growth of continental age. The Shixiagou Formation is unconformably overlain by the Dadaigou crust (e.g., Condie and Aster, 2013). Moreover, combined U–Pb dating Formation. The Upper Devonian Zhongning Formation conformably and Hf isotope analysis of zircons can be used to constrain the prove- overlies the Upper Devonian Dadaigou Formation and is, in turn, nance of clastic sediments that, in turn, may enable the reconstruction disconformably overlain by the Lower Chouniugou of the tectonic evolution of continental cratons (Hoskin and Ireland, Formation. Sediments of the Zhongning Formation comprise grey to 2000; Fedo et al., 2003). grey–yellow, medium-bedded, fine-grained, quartzo-feldspathic sand- We have carried out a zircon U–Pb geochronological and Hf isotope stone with minor glutenite layers, which contain fossil fish such as study of detrital zircons in Middle to Upper Devonian sediments from Bothriolepis niushoushanensis, Quansipetalichthys haikouensis Liu,and the Niushoushan Mountains at the southeastern margin of the Alashan Bothriolepis niushoushanensis (BGMRGS, Bureau of Geology and Mineral Terrane (Fig. 1B), which is located adjacent to the western margin of the Resources of Gansu Province, 1990). Ordos Basin of the NCC. These data are used to constrain the relationship Five sandstone samples were collected for detrital zircon analysis between the Alashan Terrane and the NCC. from the Middle Devonian Shixiagou Formation and Upper Devonian Zhongning Formation in the Niushoushan Mountains of the Ningxia 2. Geological setting and sampling Autonomous Region at the southeastern margin of the Alashan Terrane (Fig. 1B). Sample SX-1 was collected from the Shixiagou Formation, and The Alashan Terrane is a triangle-shaped terrane that has long been the other four samples were taken from the Zhongning Formation (from considered the western part of the NCC, which sutured to the Qilian Oro- lower to upper: SX-3, SX-4, SX-6, and SX-7). These five samples are genic Belt in the Devonian (Li et al., 1982; Xiao et al., 2009; Zhao, 2009; purple red medium-coarse grained sandstones. Based on microscopic Song et al., 2013; Zheng et al., 2013). Xiao et al. (2009) suggested that observations, sample SX-1 is a medium grained sandstone, composing the Qilian Orogenic Belt has recorded multiple subduction–accretion pro- of 76% quartz, 13% feldspar, 9% lithic fragments and 2% dolomite. Sample cesses between the Alashan and Qaidam blocks during the Early to Middle SX-3 has a composition of 78% quartz, 5% feldspar, 10% lithic fragments Palaeozoic. The Alashan Terrane is bounded to the east by the NCC (across and 7% calcite cement (dolomite). Sample SX-4 is lithologically similar the Helanshan Belt; Fig. 1A), to the northwest by the Tarim Craton to sample SX-3, containing 75% quartz, 7% feldspar, 10% lithic fragments (across the Altyn Tagh ), to the north by the Central Asian Orogenic and 8% dolomite. Sample SX-6 is a coarse sandstone with the composi- Belt, and to the southwest by the Qilian Orogenic Belt. tion of 81% quartz, 10% feldspar, 6% lithic fragments and 3% dolomite. The Alashan Terrane has been proposed to be the western extension Sample SX-7 is composed of 85% quartz, 5% feldspar, 7% lithic fragments of the Yinshan Block that collided with the Ordos Block at ca. 1.95 Ga to and 3% dolomite. form the Western Block of North China (e.g., Zhao et al., 2004, 2005; Santosh et al., 2007). However, the Alashan Terrane has a very different 3. Analytical techniques tectonic history to that of the NCC, particularly in the Neoproterozoic and Early Palaeozoic (Song et al., 2013). The contrasting metamorphic Zircons were separated from crushed samples by conventional basements of the Alashan and Helanshan–Qianlishan regions indicate heavy liquid and magnetic techniques, and then handpicked under a that they have different Precambrian metamorphic histories (Wan binocular microscope. The zircon grains were mounted in epoxy resin, et al., 2006; Xia et al., 2006a). Recently, Dan et al. (2012) proposed polished, and coated with . All zircons were photographed in that the Alashan Terrane was not part of the Yinshan Block, which transmitted and reflected light to characterise the analysed grains. was separated from the Western Block of the NCC during the Cathodoluminescence (CL) images of the grains were made using an Palaeoproterozoic. The Alashan Terrane comprises Late electron microscope (Quanta 400 FEG) equipped with Mono CL3+ and Palaeoproterozoic metamorphic basement. U–Pb zircon dating (Gatan, USA), operated at an accelerating voltage of 10 kV and current results indicate that the lower part of the Diebusige Complex formed of 240 μA at the State Key Laboratory of Continental Dynamics in North- at ca. 2.7 Ga and that the age of the Bayanwulashan Complex is ca. west University, Xi'an, China. 2.5–2.26 Ga (Geng et al., 2007; Dan et al., 2012). Geng et al. (2007) Zircon U–Pb isotopic compositions were analysed at the Institute of also reported U–Pb detrital zircon ages of 1367–1617 Ma from the Geology and Geophysics, Chinese Academy of Sciences, Beijing, China Alashan complex. Syn-collisional were dated at 971 and using laser ablation–inductively coupled plasma–mass spectrometry 845 Ma in the northern part of the terrane (Geng et al., 2002), (LA–ICP–MS). These analyses were carried out with a laser spot size of which indicates it was affected by a Neoproterozoic thermo-tectonic 32 μm, repetition rate of 8 Hz, and energy density of 15 J/cm2. Zircon event during the assembly and break-up of . Glacial deposits of ages were calibrated using zircons 91500 (1062.4 ± 0.6 Ma) and GJ-1 the Hanmushan Group are similar to the Luoquan Tillite of the NCC, (608.53 ± 0.37 Ma) as the standard and unknown. Trace element con- and were developed in the Neoproterozoic (Yang et al., 1988). The sed- centrations were corrected using 29Si as an internal standard and imentary cover is the Lower to Middle Haobiru Formation NIST610 as an external standard (Pearce et al., 1997). The zircon 91500 that comprises siliceous rocks intercalated with phosphatic horizons. and glass NIST 610 standards were measured twice at the beginning A continuous Middle–Upper Cambrian to Silurian sedimentary succes- and end of the analyses of zircons from each sample. Zircons GJ-1 and sion was then deposited on the northern part of the terrane, consisting 91500 were measured once each after analysis of 10 unknown zircons of shallow-marine, shelf facies carbonate to hemipelagic sediments and NIST 610 was analysed once after analysis of 20 unknown zircons. (Zheng and Zhu, 1987). However, a Middle Cambrian (Xiangshan The detailed analytical procedures are similar to those described by Xie Group) to Lower Silurian (Mayinggu Group) succession was deposited et al. (2008). Age calculations and plotting of concordia diagrams were in a continental slope environment or as flysch deposits in the southern performed using the Isoplot programme (version 3.0) (Ludwig, 2003). part of the terrane. The Devonian sediments were deposited in a In situ Hf isotope analyses were made with a Neptune LA–MC–ICP– foreland basin in the Niushoushan area. MS coupled to a 193 nm excimer ArF laser ablation system (GeoLas In the Niushoushan area, the Middle Devonian Shixiagou Formation Plus) at the Institute of Geology and Geophysics, Chinese Academy of unconformably overlies the Middle Cambrian Xiangshan Group. The Sciences, Beijing, China. This instrument is a double focusing multiple- Shixiagou Formation is a fluvio-lacustrine facies that consists of collector ICP–MS that can operate at high mass resolution. The Hf W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282 1273

Fig. 2. CL images of representative zircons from five samples of the Alashan Terrane. The large circles indicate the sites of Hf isotope analyses and the small circles indicate the sites of U–Pb age analyses. The scale bar is 100 μm. isotope analyses used a laser spot size of 60 μm at a repetition rate of and Shixiagou Formations are summarized in Tables 1 and 2 (Supple- 4 Hz, which has an energy density of 15 J/cm2 and pulse width of mentary Data). CL images of representative zircons from all samples 15 ns. Helium was used as a carrier gas to enhance transport of the are shown in Fig. 2. A total of 568 U–Pb ages were obtained that were ablated material to the mass spectrometer. Initial 176Hf/177Hf values concordant between 80% and 110% (Fig. 3) (Table 2; Supplementary were calculated with a 176Lu decay constant of 1.865 × 10−11 y−1 Data). For zircons with ages of N1000 Ma, the 207Pb/206Pb age is more (Soderlund et al., 2004). Lu–Hf model ages were calculated using a reliable, whereas forzirconswithagesofb1000 Ma, the 206Pb/238U 176Lu/177Hf ratio for average crust of 0.015, and present-day 176Lu/ age is more reliable. Although Hf and U–Pb isotope analyses were con- 177Hf ratios of chondritic and depleted of 0.0332 and 0.0384, ducted separately, Hf isotope analyses were made at the same site as respectively, and present-day 176Hf/177Hf ratios of chondritic and de- that used for U–Pb dating. A total of 416 zircon Hf isotope measure- pleted mantle of 0.282772 and 0.28325, respectively (Blichert-Toft ments were carried out (Table 2; Supplementary Data). et al., 1997; Griffinetal.,2004). CL images were used to avoid analysis of inclusions and grain–epoxy 4.1. U–Pb ages boundaries. During U–Pb dating analyses, each zircon grain (N32 μm) in a mount was dated from left to right, until either 140 or 150 zircon 4.1.1. Middle Devonian Shixiagou Formation (Sample SX-1) grains had been dated. A total of 150 analyses of 148 zircon grains were made, of which 107 analyses were concordant with ages ranging from 422 ± 9 to 4. Results 3442 ± 19 Ma (Table 1; Supplementary Data). Four age groups were identified: 0.4–0.5 Ga (peak at 490 Ma); 1.0–1.3 Ga (peaks at The zircon grains were colourless and transparent or brown to light 1029 and 1157 Ma); 1.5–2.0 Ga; and 2.4–2.7 Ga (peak at 2432 Ma, brown in colour. The generally euhedral to subhedral nature of the zir- with subordinate peaks at 2672 and 2770 Ma). Three grains yielded cons suggests their was from nearby rocks. However, some 207Pb/206Pb ages of 3054 ± 19, 3102 ± 17, and 3442 ± 19 Ma. The rounded zircons indicate that they have experienced abrasion during dated zircons range in size from 75 to 200 μmandmostzircons long-distance transport or multiphase reworking. In situ U–Pb and Hf exhibit oscillatory zoning and are bright in CL images. Zircon Th/U isotopic data for detrital zircons from the five samples of the Zhongning ratios vary between 0.01 and 1.82 (93% grains have Th/U N 0.1). 1274 W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282

The CL images and Th/U ratios indicate that the majority of the detri- 4.2. Lu–Hf isotopes tal zircons have a magmatic origin. 4.2.1. Middle Devonian Shixiagou Formation (Sample SX-1) In situ Hf isotopic analyses of 87 zircons were undertaken from this 4.1.2. Upper Devonian Zhongning Formation sample (Table 2; Supplementary Data). Zircons with ages of 0.4–0.5 Ga

have both negative and positive εHf(t) values (−26.0 to +9.0) with 4.1.2.1. Sample SX-3. A total of 144 analyses of 140 grains were undertak- model ages of 1422–2880 Ma (most are 1.7–1.9 Ga). Most zircons en on this sample, which yielded 120 concordant analyses with ages have negative εHf(t) values, which suggest that their parent from 450 ± 10 to 3205 ± 17 Ma (Table 1; Supplementary Data). were the result of crustal reworking. However, zircons with ages of

Four age populations are evident: 0.4–0.6 Ga (peak at 496 Ma); 1.0–1.3 Ga have εHf(t) values between −15.5 and +4.9, which corre- 1.0–1.3 Ga (peaks at 975 and 1084 Ma, with two subordinate peaks at spond to model ages from 1593 to 2950 Ma with an age peak at

880 and 1314 Ma); 1.5–2.0 Ga; and 2.4–2.7 Ga (peak at 2491 Ma, with 2.3–2.4 Ga. The 1.5–2.0 Ga zircons have εHf(t) values from −7.6 to a subordinate peak at 2629 Ma). One zircon yielded a 207Pb/206Pb age +7.3 with model ages of 1870–3121 Ma. The Archean zircons have of 3205 ± 17 Ma. Zircons in this sample range in size from 60 to εHf(t) values of −23.7 to +7.8 and model ages from 2447 to 4510 Ma, 200 μm, and are euhedral, rounded, or prismatic with rounded edges. which demonstrates that their parent magmas were derived from The majority of grains have oscillatory zoning and are bright in CL images ancient continental crust. (Fig. 2). The zoning and Th/U ratios (98% of grains have Th/U N 0.13) are indicative of a magmatic origin. 4.2.2. Upper Devonian Zhongning Formation

4.2.2.1. Sample SX-3. A total of 82 zircons were analysed for their Hf 4.1.2.2. Sample SX-4. A total of 140 analyses of 140 grains were con- isotope composition (Table 2; Supplementary Data). The 0.4–0.5 Ga zir- ducted on this sample (Table 1; Supplementary Data), which yielded cons have εHf(t) values from −17.6 to +12.2 with a correspondingly 125 concordant ages ranging from 425 ± 10 to 2814 ± 18 Ma. large range in model ages from 720 to 2564 Ma, suggesting the zircons – Five age groupings were obtained: 0.4 0.5 Ga (peak at 474 Ma); have different origins or host magmas if they crystallized at a similar 0.7–0.8 Ga (peak at 725 Ma); 1.0–1.3 Ga (peaks at 999 and time. Zircons with ages of 1.0–1.3 Ga have εHf(t) values of −13.9 to – – 1159 Ma); 1.4 2.1 Ga; and 2.4 2.7 Ga (peak at 2496 Ma). Zircons +12.8 and corresponding model ages from 1110 to 2717 Ma (most in this sample range in size from 50 to 250 μm. Th/U ratios vary are 2.3–2.4 Ga). The 1.5–2.0 Ga zircons have εHf(t) values from −12.6 fi b from 0.04 to 3.16, and only ve zircon grains have Th/U 0.1. Most to +4.5 and model ages from 2153 to 3147 Ma, and the 2.4–2.7 Ga zircon grains exhibit oscillatory zoning and high Th/U values, typical zircons have εHf(t) values of −14.2 to +0.3 with model ages from of a magmatic origin. 3036 to 3863 Ma, indicating that their parent magmas were derived from 3.0–3.8 Ga continental crust.

4.1.2.3. Sample SX-6. A total of 141 analyses of 140 grains were obtained 4.2.2.2. Sample SX-4. Hf isotope analyses of 86 zircons were made for this for this sample (Table 1; Supplementary Data), which produced 100 sample (Table 2; Supplementary Data). The 0.4–0.5 Ga zircons have concordant ages from 457 ± 10 to 3351 ± 18 Ma. Four age popula- ε values from −16.3 to +13.9 and model ages of 616–2531 Ma tions can be identified: 0.4–0.5 Ga (peak at 478 Ma); 1.0–1.3 Ga Hf(t) (most are 1.2–1.5 Ga). However, the 1.0–1.3 Ga zircons have ε (peaks at 1003 and 1144 Ma); 1.5–2.1 Ga; and 2.4–2.8 Ga (peak at Hf(t) values from −14.6 to +9.1 and model ages of 1464–2732 Ma (most 2464 Ma, with a subordinate peak at 2808 Ma). Two zircons yielded are 1.7–1.9 Ga). The 1.6–2.1 Ga zircons have ε values from −7.9 ages older than 3.0 Ga of 3299 ± 17 and 3351 ± 17 Ma. Th/U ratios Hf(t) to +8.2 and a large range of model ages from 1893 to 3219 Ma. The of these zircons range between 0.07 and 2.72, with only one zircon zircons have ε values from −13.3 to +4.4 and model having Th/U b 0.1. Most zircons have oscillatory zoning, and this ob- Hf(t) ages of 2730–3909 Ma. servation, along with their high Th/U ratios, indicates a magmatic origin. 4.2.2.3. Sample SX-6. A total of 86 zircons were analysed for Hf isotopes

(Table 2; Supplementary Data). The 0.4–0.5 Ga zircons have εHf(t) − 4.1.2.4. Sample SX-7. For this sample, 144 analyses of 140 grains (Table 1; values from 11.0 to +1.9 and a large range of model ages from – ε − Supplementary Data) yielded 116 concordant ages that vary from 1332 to 2158 Ma. The 1.0 1.3 Ga zircons have Hf(t) values from 9.9 430 ± 9 to 4022 ± 16 Ma. Five age groups are evident for this sample: to +11.9 and model ages from 1193 to 2468 Ma (most are – – ε − 0.5–0.7 Ga (peak at 580 Ma); 1.0–1.3 Ga (peaks at 999 and 1157 Ma); 2.0 2.2 Ga). The 2.4 2.5 Ga zircons have Hf(t) values from 6.2 to – 1.5–2.1 Ga; 2.4–2.7 Ga (peak at 2441 Ma); and 3.1–3.3 Ga (peak at +4.9 and model ages from 2689 to 3387 Ma (most are 2.9 3.0 Ga), 3267 Ma). One detrital zircon has an age of 4022 ± 16 Ma. This Hadean which is consistent with reworking of Mesoarchean crust. The zircon – zircon grain is colourless, rounded, and has a diameter of 100 μm, with a U Pb age of 3351 ± 17 Ma yielded a model age of 4077 Ma, suggesting that it has experienced long-distance transport, strong which indicates that its host originated from Hadean crust. abrasion, and/or multiphase reworking. The oscillatory zoning, bright CL image, and high Th/U ratio (0.58) of the Hadean zircon 4.2.2.4. Sample SX-7. In total, 75 zircons from this sample were analysed are indicative of a magmatic origin. Several thin overgrowth rims for Hf isotopes (Table 2; Supplementary Data). The 0.5–0.7 Ga zircons are evident in the CL image, suggesting that the Hadean zircon has have εHf(t) values from −10.4 to −8.3 and model ages from 2062 to experienced several metamorphic events (Fig. 2). Th/U ratios in the 2213 Ma, indicating that their parent magmas were produced by other zircons range from 0.07 to 2.72. Most of the zircons display os- reworking of 2.0–2.2 Ga continental crust. The 1.0–1.3 Ga zircons have cillatory zoning and have high Th/U values, indicating a magmatic εHf(t) values from −12.8 to +10.4, and a corresponding large range of origin. model ages from 1276 to 2747 Ma with two groups at 1.4–1.6 and

Fig. 3. Age histogram, εHf(t) versus U–Pb age, and U–Pb concordia diagrams for detrital zircons from Devonian rocks of the Niushoushan Mountains at the southeastern margin of the Alashan Terrane. W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282 1275 1276 W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282

5.2. Relationship between the Alashan Terrane and the NCC

Controversy exists as to the tectonic affinity of the Alashan Terrane (Dan et al., 2012; Zhang et al., 2013b,c). Recent studies have shown that the Alashan Terrane was separated from the NCC in the Palaeoproterozoic based on U–Pb zircon dating results of the lower part of the Diebusige Complex and the Bayanwulashan Complex (Dan et al., 2012). However, on the basis of systematic zircon U–Pb and Hf isotopic investigation of four orthogneiss samples in the Beidashan area of the western Alashan Terrane, Gong et al. (2012) and Zhang et al. (2013a) proposed that the Terrane experienced a ~2.5 Ga magmatic–metamorphic event and subse- quent late Palaeoproterzoic high-grade metamorphism, which were very

Fig. 4. εHf(t) versus U–Pb age for 0.4–0.5 Ga detrital zircons in this study and εNd(t) versus age of Palaeozoic volcanic rocks in the North Qilian Orogenic Belt (Wu et al., 2006; Zhang et al., 2006; He et al., 2007).

2.0–2.3 Ga. The Neoarchean zircons have εHf(t) values from −13.2 to +2.7 and model ages from 2919 to 3809 Ma (most are 3.1–3.3 Ga).

5. Discussion

5.1. Detrital zircon provenance of the Middle to Late Devonian sediments

In this study, zircon U–Pb age spectra obtained from the Devonian sedimentary rocks at the southeastern margin of the Alashan Terrane generally define five age populations at 0.4Ga–0.7Ga, 1.0Ga–1.3Ga, 1.5Ga–1.8Ga, 2.4Ga–2.7Ga, and N3.0 Ga (peak at 3332 Ma) (Fig. 3f). Detrital zircons with U–Pb ages of 0.4–0.5 Ga (peak at 488 Ma) are typically euhedral, suggesting derivation from a nearby source area. Our sampling area is close to the North Qilian Orogenic Belt (Fig. 1). Ordovician island-arc volcanic rocks are abundant in the North Qilian Orogen and have ages that are largely between 424 and 490 Ma (Zhang et al., 1997; Gehrels et al., 2003; Xia et al., 2003; Su et al., 2004; Wang et al., 2005; Chen, 2007; Tseng et al., 2009; J.H. Yu et al.,

2010; J.Y. Yu et al., 2010; Wu et al., 2011), and also have εNd(t) values that are consistent with the εHf(t) values obtained from 0.4 to 0.5 Ga detrital zircons in our study (Fig. 4)(Zhang et al., 2006; Tseng et al., 2009; Wu et al., 2011). These observations suggest that Ordovician volcanic rocks in the North Qilian Orogen were the source of detrital zircons with ages of 0.4–0.5 Ga. Moreover, igneous rocks with ages of 724 ± 4 to 776 ± 10 Ma crop out widely in the North Qilian Orogen (Su et al., 2004; Tseng et al., 2006; He et al., 2010), and have a similar age to the ca. 0.7 Ga detrital zircons in our Devonian sediments. Igneous rocks with ages of 790 ± 12 to 943 ± 28 Ma are exposed in the Central Qilian Massif (Guo et al., 2000; Wan et al., 2000, 2003; Tung et al., 2007; Wang et al., 2007; Tung et al., 2012, 2013; Yu et al., 2013), and ages of 807 ± 4 to 833 ± 35 Ma have been obtained from the Jinchuan pluton of the Longshoushan area at the southern margin of the Alashan Terrane (Li et al., 2004; Yang et al., 2005; Tian et al., 2007). Ages of 845 to 971 Ma have also been reported for from the eastern Alashan Terrane (Geng et al., 2002; Geng and Zhou, 2010). These results indicate that the detrital zircons with ages of 0.7–1.0 Ga were probably sourced from igneous rocks in both the Qilian Orogenic Belt and the Alashan Terrane. All of these indicators of sediment provenance demonstrate that the source of Middle to Late Devonian sediments in the Alashan Terrane was the North Qilian Orogenic Belt and the Middle Qilian Massif, which implies that the North Qilian Ocean closed prior to the Fig. 5. Relative age probability plot comparing the ages of detrital zircons from: (a) the Middle to Late Devonian. western part of the NCC (Zheng et al., 2004; Darby and Gehrels, 2006; Xia et al., 2006b; He et al., 2009; Zheng et al., 2009; Jiang et al., 2010; Diwu et al., 2011; Peng et al., 2011; Detrital zircons with ages of 1.0–1.3 Ga originated from igneous Wan et al., 2011a,b; Yin et al., 2011; Ying et al., 2011; J. Zhang et al., 2011; X.J. Zhang rocks of an unknown source, which cannot be clearly traced to a source et al., 2011); (b) the Zhuozishan Mountains adjacent to the western margin of Ordos area at the southeastern margin of the Alashan Terrane. Basin in the NCC (Darby and Gehrels, 2006); and (c) the Alashan Terrane (this study). W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282 1277

Ordovician (J. Zhang et al., 2011; X.J. Zhang et al., 2011), and that amalgamation might have occurred between the Late Ordovician and Early Devonian (Li et al., 2012). Notably, reinterpretation of new palaeomagnetic data suggests that the Alashan Terrane experienced a ca. 26° anticlockwise rotation relative to the NCC in Early to Middle Triassic times (Liu et al., 2010), which implies that these two blocks joined after the Early to Middle Triassic. Detrital zircons from Precambrian to Late Mesozoic strata in the western NCC are characterised by three major U–Pb age groups at 2.4–2.7 Ga, 1.8–2.1 Ga, and during the Late (Fig. 5a), which are distinct from those of the southeastern margin of the Alashan Terrane (Fig. 5c). Furthermore, detrital zircons from Neoproterozoic to Early Palaeozoic sedimentary rocks in the Zhuozishan Mountains (northwestern Ordos Basin of the NCC) have U–Pb age spectra typical of the NCC with two age populations at 2.4–2.6 and 1.85–2.1 Ga (Darby and Gehrels, 2006)(Fig. 5b). These ages are significantly differ- ent from those obtained in our study from the Niushoushan Mountains adjacent to the southwestern Ordos Basin at the southeastern margin of the Alashan Terrane (Fig. 5c). Although these two mountain ranges are in close proximity, different sediment provenances characterised the southeastern margin of the Alashan Terrane and the NCC in the Middle to Late Devonian, implying that these regions were separate at that time. A prominent group of detrital zircons with U–Pb ages of ca. 2.5 Ga has been reported from sedimentary strata in major Gondwana blocks. However, it is unwise to deduce their provenance only on the basis of zircon U–Pb age spectra. Zircon Hf isotopic data can also be used as a provenance tool (Hoskin and Ireland, 2000; Fedo et al., 2003). Our sam- ples have a ca. 2.5 Ga U–Pb age peak with two secondary peaks at 2688

and 2796 Ma (Fig. 3f). The ca. 2.5 Ga zircons have εHf(t) values between +4.9 and −23.7, which correspond to Hf model ages between 2689 and 4501 Ma with a peak at ca. 3.10 Ga (Fig. 6c). These data suggest that the parent magmas of the zircons were generated from ca. 3.10 Ga continental crust. The ca. 2.5 Ga detrital zircons from Palaeozoic strata of the North Qilian Orogenic Belt are thought to have been sourced from the NCC (Yang et al., 2009; Xu et al., 2010a,b). However, detrital zircons with ages of ca. 2.5 Ga from the NCC have Hf isotope model ages that peak at 2.75 Ga, implying an important crustal growth event at 2.75 Ga (Li et al., 2007; Zheng et al., 2009; Jiang et al., 2010; Diwu et al., 2011; Wan et al., 2011a,b; Wang et al., 2011)(Fig. 6). These results indicate that a significantly different crustal growth event affected the southeastern margin of the Alashan Terrane com- pared with the NCC (Figs. 6 and 7). In addition, a population of zircons with U–Pb ages of ca. 3332 Ma is present in our samples, which includes numerous Palaeoarchean zircons. However, their Hf isotope ratios are significantly different from those of the NCC (Fig. 8), suggesting that the ca. 2.5 and 3.3 Ga detrital zircons were not sourced from the NCC Fig. 6. Histogram of Hf isotope model ages of 2.4–2.7 Ga detrital zircons in (a) the NCC and confirming that the Middle to Upper Devonian sediments in the (Li et al., 2007; Zheng et al., 2009; Jiang et al., 2010; Diwu et al., 2011; Wan et al., 2011a, Alashan Terrane did not originate from the NCC. b; Wang et al., 2011; Ying et al., 2011; Zhou et al., 2011), (b) the South China Craton (Yu et al., 2008, 2009; J.H. Yu et al., 2010; J.Y. Yu et al., 2010; Li et al., 2011; Yao et al., 2011; 5.3. Potential origin of the Alashan Terrane Zheng et al., 2011), and (c) the Alashan Terrane (this study).

Our results indicate that detrital zircons with ages of 1.0–1.3 Ga have two prominent peaks at 1001 and 1152 Ma (Fig. 3f), implying that the sediments had a source with characteristics typical of the Grenvillian similar to those events of the NCC. They further argued that the Alashan . Geological studies suggest that the Grenvillian Orogeny Terrane was probably the western extension of the Belt was widespread in South , the Maud–Namaqua–Natal prov- between the Yinshan and Ordos blocks. According to palaeomagnetic ince of East , southwest , Amazonia, and at results, some studies have suggested that the Alashan Terrane formed 1.0–1.3 Ga (Hoffman, 1991; Boger et al., 2000; Jayananda et al., 2000). the western extension of the NCC by Late Cambrian time (Meng et al., Grenvillian ages have been obtained from detrital zircons of Early 1990; Wu et al., 1993; Huang et al., 1999, 2000, 2001). If this is the Palaeozoic sedimentary strata in , southeast China, and yield case, then palaeomagnetic data from the Alashan Terrane can be used two age peaks at 1.0 and 1.15 Ga (Yao et al., 2011)(Fig. 9c). These re- to represent the NCC (Meng et al., 1990; Wu et al., 1993; Huang et al., sults are similar to the age spectra obtained in the present study

1999, 2000, 2001). However, other studies of the detrital zircon geo- (Fig. 9d). Furthermore, the εHf(t) values of 1.0–1.3 Ga zircons of the chronology of Ordovician sedimentary rocks have suggested that the present study are similar to those from Cathaysia (Figs. 7 and 10). In

Alashan Terrane did not connect with the NCC prior to the Middle addition, εHf(t) values of zircons with ages of 2.4–2.7 and N3.0 Ga from 1278 W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282

Fig. 7. εHf(t) versus U–Pb ages of detrital zircons from the NCC, South China Craton, western Australia, Tethyan Himalaya, and the Alashan Terrane. the Alashan Terrane are consistent with those of zircons from the (Wang et al., 1995). These results suggest that the Alashan Terrane and Cathaysian Block (Fig. 8). As such, detrital material in the Middle to South China Belt were located close to each other during the Palaeozoic. Late Devonian sandstones from the southeastern margin of the Alashan In Neoproterozoic to Early Palaeozoic times, the South China Block Terrane have a strong affinity with sediments from the Cathaysian Block was probably connected with the northwestern margin of Australia in southeast China. (Yang et al., 2004)orhadastrongaffinity with East Gondwana (Yu Palaeontological studies have shown that trilobites in Cambrian stra- et al., 2008). Detrital zircon U–Pb geochronology data from the Te- ta from the Qilian Orogen are endemic species of the Tarim–Yangtze thys–Himalaya (northern India) (Gehrels et al., 2006; McQuarrie biogeographic domain (Duan and Ge, 2005), and have a close relation- et al., 2008; Myrow et al., 2010; Zhu et al., 2011), the Albany–Fraser ship with trilobites from western Hunan Province, eastern Guizhou in Belt in southwest Australia (Cawood and Nemchin, 2000; Veevers south China, and northwest Queensland in Australia (Zhou et al., et al., 2005), Cathaysia (southeast China), and the Alashan Terrane 1996). Antiarchian fossils are a type of freshwater fish that are found (this study) all have similar U–Pb age spectra (Fig. 9) and Hf isotope in the Upper Devonian Zhongning Formation in the present study characteristics (Fig. 7). A recent study has shown that crustal gener- area, and have a close affinity with those from south China and New ation in the Gondwana supercontinent had a major pulse at ca. South Wales, Australia (Pan et al., 1987; Jia et al., 2010). In addition, 3.3 Ga (Kemp et al., 2006). The zircon U–Pb age population of ca. Sinoleperditiini (Ostracoda) found in the lower part of the Upper 3332 Ma in the Alashan Terrane highlights its potential relationship Devonian Zhongning Formation have the droop in the “V”-shaped with Gondwana and also with south China, where igneous zircons muscle scars that is indistinguishable from Ostracoda from south China from trondhjemitic in the northern Kongling Terrane have

been dated at 3302 ± 7 Ma (Gao et al., 2011). εHf(t) values of the 3.3 Ga zircons from our samples are similar to those from the Kongling Terrane gneisses (Fig. 8).

6. Conclusions

In situ U–Pb age and Hf isotopic data for detrital zircons from Middle to Late Devonian sedimentary rocks in the southeastern Alashan Terrane, northwest China, largely define four age populations (0.4Ga– 0.7Ga, 1.0Ga–1.3Ga, 1.5Ga–1.8Ga, and 2.4Ga–2.7 Ga) along with a few Palaeoarchean and one Hadean ages (4022 ± 17 Ma). The population of zircons with ages of 0.4–0.5 Ga and their Hf isotopic data indicate that the North Qilian Orogenic Belt was the source of Middle to Late De- vonian sediments from the southeastern margin of the Alashan Terrane. However, other zircon populations (1.0Ga–1.3Ga, 1.5Ga–1.8Ga, 2.4Ga–

2.7Ga, and ca. 3.3 Ga) and their corresponding εHf(t) values indicate that the detrital sediments of the Alashan Terrane were not sourced from the NCC, implying that a connection between the Alashan Terrane and the NCC did not exist prior to the Late Devonian. In contrast, zircon U–Pb age spectra and Hf isotope data show a strong affinity between the Alashan Terrane and East Gondwana and the South China Block in the Fig. 8. εHf(t) versus U–Pb ages of N3.0 Ga zircons in the Alashan Terrane, the NCC (Zheng et al., 2004; Wu et al., 2005), and the South China Craton (Gao et al., 2011). Late Devonian. W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282 1279

Fig. 10. Histogram of Hf isotope model ages for ca. 0.9–1.3 Ga detrital zircons in (a) the Alashan Terrane and (b) Cathaysia (southeastern part of the South China Craton) (Yu et al., 2008, 2009; Li et al., 2011; Yao et al., 2011).

Supplementary data to this article can be found online at http:// dx.doi.org/10.1016/j.gr.2013.12.009.

Acknowledgements

This work has been supported by the SinoProbe (08-01-01). Prof. Xiaohong Ge is thanked for the useful warm discussions. The constructive reviews by Drs. J. X. Zhang W. J. Xiao were also greatly appreciated.

References

BGMRGS (Bureau of Geology and Mineral Resources of Gansu Province), 1990. Regional Geology of the Gansu Province. Geological Publishing House Beijing (In Chinese). Blichert-Toft, J., Chauvel, C., Albarede, F., 1997. Separation of Hf and Lu for high-precision isotope analysis of rock samples by magnetic sector-multiple collector ICP–MS. Contributions to Mineralogy and Petrology 127, 248–260. Boger, S.D., Carson, C.J., Wilson, C.J.L., Fanning, C.M., 2000. Neoproterozoic deformation in the Radok region of the northern Prince Charles Mountains, east Antarctica: evidence for a single protracted orogenic event. Precambrian Research 104, 1–24. Cawood, P.A., Nemchin, A.A., 2000. Provenance record of a basin: U/Pb ages of detrital zircons from the Perth Basin, Western Australia. Sedimentary Geology 134, 209–234. Chen, H.Q., 2007. Geochemical features of ningchanhe body and its' tectonic sig- nificance in lenglongling of north Qilian. Gansu Geology 16 (4), 37–42 (In Chinese with English abstract). Condie, K.C., Aster, R.C., 2013. Refinement of the with Hf, Nd and Sr isotopes. Geoscience Frontiers. http://dx.doi.org/10.1016/j.gsf.2013.06.001. Dan, W., Li, X.H., Guo, J.H., Liu, Y., Wang, X.C., 2012. evolution of the east- ern Alxa Block, westernmost North China: evidence from in situ zircon U–Pb dating and Hf–O isotopes. Gondwana Research 21, 838–864. Darby, B.J., Gehrels, G., 2006. Detrital zircon reference for the North China block. Journal of Fig. 9. Relative age probability plot comparing detrital zircon ages from the Alashan Asian Earth Sciences 26, 637–648. Terrane, the Southwestern Australia (Cawood and Nemchin, 2000; Veevers et al., 2005), Diwu, C.R., Sun, Y., Guo, A.L., Wang, H.L., Liu, X.M., 2011. Crustal growth in the North China the Tethyan Himalaya (McQuarrie et al., 2008; Myrow et al., 2010), and the South China Craton at 2.5 Ga: evidence from in situ zircon U–Pb ages, Hf isotopes and whole-rock Craton (Yao et al., 2011). geochemistry of the Dengfeng complex. Gondwana Research 20, 149–170. 1280 W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282

Duan, J.Y., Ge, X.H., 2005. Stratigraphic and paleobiogeographic affinities between differ- Li, L.M., Sun, M., Wang, Y.J., Xing, G.F., Zhao, G.C., He, Y.H., He, K.J., Zhang, A.M., 2011. U–Pb ent tectonic units in northwestern China—with a discussion of the tectonic frame- and Hf isotopic study of detrital zircons from the meta-sedimentary rocks in central work of northwestern China. Geological Bulletin of China 24 (6), 558–563 (In Jiangxi Province, South China: implications for the Neoproterozoic tectonic evolution Chinese with English abstract). of South China Block. Journal of Asian Earth Sciences 41, 44–55. Enkin, R.J., Yang, Z.Y., Courtillot, V., 1992. Paleomagnetic constraints on the geodynamic Li, J.Y., Zhang, J., Qu, J.F., 2012. Amalgamation of North China Craton with Alxa Block in the history of the major blocks of China from the Permian to the present. Journal of late of Early : evidence from sedimentary sequences in the Niushou Moun- Geophysical Research 97, 13953–13989. tain, Ningxia Hui Autonomous Region, NW China. Geological Review 58 (2), 208–214 Fedo, C.M., Sircombe, K.N., Rainbird, R.H., 2003. Detrital zircon analysis of the sedimentary (In Chinese with English abstract). record. In: Hanchar, J.M., Hoskin, P.W.O. (Eds.), Zircon. Reviews in Mineralogy and Liu, J., Yang, Z.Y., Tong, Y.B., Yuan, W., 2010. Tectonic implications of early-middle Triassic Geochemistry, 53, pp. 277–303. palaeomagnetic results from Hexi Corridor, North China. Geophysical Journal Interna- Gao, S., Yang, J., Zhou, L., Li, M., Hu, Z.C., Guo, J.L., Yuan, H.L., Gong, H.J., Xiao, G.Q., Wei, J.Q., tional 182 (3), 1216–1228. 2011. Age and growth of the Archean Kongling terrain, South China, with emphasis Liu, Y.C., Wang, A.D., Li, S.G., Rolfo, F., Li, Y., Groppo, C., Gu, X.F., Hou, Z.H., 2013. Composi- on 3.3 Ga granitoid gneisses. American Journal of Science 311 (2), 153–182. tion and geochronology of the deep-seated from the southeastern margin Ge, X.H., Ma, W.P., Liu, J.L., Ren, S.M., Liu, Y.J., Yuan, S.H., Wang, M.P., 2009. A discussion on of the North China Craton. Gondwana Research 23, 1021–1039. the tectonic framework of Chinese mainland. Geology in China 36 (5), 949–965 (In Lu, S.N., Yu, H.F., Li, H.K., Chen, Z.H., Wang, H.C., Zhang, C.L., 2009. Precambrian geology of Chinese with English abstract). the Central Orogenic Belt (Central–Western). Geological Publishing House, Beijing 1 Gehrels, G.E., Yin, A., Wang, X.F., 2003. Detrital-zircon geochronology of the northeastern (In Chinese with English abstract). Tibetan . Geology Science of American Bulletin 115 (7), 881–896. Ludwig, K.R., 2003. Mathematical-statistical treatment of data and errors for 230Th/U geo- Gehrels, G.E., DeCelles, P.G., Ojha, T.P., Upreti, B.N., 2006. Geologic and U-Pb geochrono- chronology. Uranium-Series Geochemistry 52, 631–656. logic evidence for early Paleozoic tectonism in the Dadeldhura thrust sheet, far- McQuarrie, N., Robinson, D., Long, S., Tobgay, T., Grujic, D., Gehrels, G., Duce, M., 2008. Pre- west Nepal Himalaya. Journal of Asian Earth Sciences 28, 385–408. liminary stratigraphic and structural architecture of Bhutan: implications for the Geng, Y.S., Zhou, X.W., 2010. Early Neoproterozoic granite events in Alax area of Inner along strike architecture of the Himalayan system. Earth and Planetary Science Letters Mongolia and their geological significance: evidence from geochronology. Acta 272, 105–117. Petrologica et Mineralogica 29 (6), 779–795 (In Chinese with English abstract). Meng, Z.F., Huang, H.F., Chen, Y.Z., 1990. The late Permian pole of the western Jiuquan Geng, Y.S., Wang, X.S., Shen, Q.H., 2002. The discovery of Neoproterozoic Jinningian de- basin (NW China) and its tectonic implication. Acta Sedimentologica Sinica 8 (3), formed granites in Alax area and its significance. Acta Petrologica et Mineralogica 58–65 (in Chinese with English abstract). 21 (4), 412–420 (In Chinese with English abstract). Myrow, P.M., Hughes, N.C., Goodge, J.W., Fanning, C.M., Williams, I.S., Peng, S.C., Bhargava, Geng, Y.S., Wang, X.S., Shen, Q.H., Wu, C.M., 2007. Chronology of the Precambrian meta- O.N., Parcha, S.K., Pogue, K.R., 2010. Extraordinary transport and mixing of sediment morphic series in the Alxa area, . 34, 251–261. across Himalayan central Gondwana during the Cambrian–Ordovician. Geological Gong, J.H., Zhang, J.X., Yu, S.Y., Li, H.K., Hou, K.J., 2012. 2.5 Ga TTG gneiss and its geological Society of America Bulletin 122, 1660–1670. implications in the western Alxa block, North China Craton. Chinese Science Bulletin Pan, J., Huo, F.C., Cao, J.X., Gu, Q.C., Liu, S.Y., Wang, J.Q., Gao, L.D., Liu, C., 1987. Continental 57, 4064–4076. Devonian System of Ningxia and its biotas. Geological Publishing House 1–315 (In Griffin, W.L., Belousova, E.A., Shee, S.R., Pearson, N.J., O'Reilly, S.Y., 2004. Archean crustal Chinese with English abstract). evolution in the northern Yilgarn Craton: U–Pb and Hf-isotope evidence from detrital Pearce, N.J.G., Perkins, W.T., Westgate, J.A., 1997. A compilation of new and published zircons. Precambrian Research 131, 231–282. major and trace element data f or NIST SRM 610 and NIST SRM 612 glass reference Guo, J.J., Zhao, F.Q., Li, H.K., Li, H.M., Zou, Y.C., 2000. New chronological evidence of the age materials. Geostandards Newsletter 21 (115), 144. of Huangyuan Group in the eastern segment of Mid-Qilian massif and its geological Peng, P., Guo, J.H., Windley, B.F., Li, X.H., 2011. Halaqin volcano-sedimentary succession significance. Regional Geology of China 19 (1), 26–31 (In Chinese with English in the central-northern margin of the North China Craton: products of Late abstract). Paleoproterozoic ridge subduction. Precambrian Research 187, 165–180. He, S.P., Wang, H.L., Xu, X.Y., Zhang, H.F., Ren, G.M., 2007. Geochemical characteristics and Santosh, M., Wilde, S.A., Li, J.H., 2007. Timing of Paleoproterozoic ultrahigh temperature tectonic environment of Hongtubu basalts and Chenjiahe intermediate-acid volcanic metamorphism in the North China Craton: evidence from SHRIMP U–Pb zircon geo- rocks in the eastern segment of North Qilian orogenic belt. Acta Petrologica et chronology. Precambrian Research 159, 178–196. Mineralogica 26 (4), 296–309 (In Chinese with English abstract). Soderlund, U., Patchett, J.P., Vervoort, J.D., Isachaen, C.E., 2004. The 176Lu decay constant He, Y.H., Zhao, G.C., Sun, M., Xia, X.P., 2009. SHRIMP and LA–ICP–MS zircon geochronology of determined by Lu–Hf and U–Pb isotope systematics of Precambrian mafic intrusions. the Xiong'er volcanic rocks: implications for the Paleo-Mesoproterozoic evolution of the Earth and Planetary Science Letters 219, 311–324. southern margin of the North China Craton. Precambrian Research 168, 213–222. Song, S.G., Niu, Y.L., Su, L., Xia, X.H., 2013. Tectonics of the North Qilian orogen, NW China. He,S.P.,Li,R.S.,Wang,C.,Yu,P.S.,Gu,P.Y.,Shi,C.,2010.Geochronology of gneissic Gondwana Research 23, 1378–1401. plagioclase-amphibolite from Beidahe Group-complex in western segment of Qilian Su, J.P., Hu, N.G., Zhang, H.F., Fu, G.M., 2004. Single-zircon U–Pb dating and geological sig- Mountains, China. Geological Bulletin of China 29 (9), 1275–1280 (In Chinese with nificance of the Diaodaban granitic gneiss in the western segment of north Qilian English abstract). Mountains. Geological Science and Technology Information 23 (3), 11–14 (In Chinese Hoffman, P.F., 1991. Did the breakout of Laurentia turn Gondwanaland inside out. Science with English abstract). 252, 1409–1412. Tang, Y.J., Zhang, H.F., Ying, J.F., Su, B.X., Chu, Z.Y., Xiao, Y., Zhao, X.M., 2013. Highly hetero- Hoskin, P.W.O., Ireland, T.R., 2000. Rare earth element chemistry of zircon and its use as a geneous lithospheric mantle beneath the Central Zone of the North China Craton provenance indicator. Geology 28 (7), 627–630. evolved from Archean mantle through diverse melt refertilization. Gondwana Re- Huang, B.C., Otofuji, Y.I., Yang, Z.Y., Zhu, R.X., 1999. Preliminary result and its tectonic search 23, 130–140. implications of middle Cambrian paleomagnetism in the Alax and Hexi corridor Tian, Y.L., Wu, S.J., Memng, R., Wang, Y.S., Lin, C.L., Xiao, L.Z., 2007. LA–ICP–MS zircon U–Pb terrane. Chinese Journal of Geophysics 43 (3), 393–401 (in Chinese with English age of the Jinchuan ultramafic intrusion. Acta Mineralogica Sinica 27 (2), 211–217 (In abstract). Chinese with English abstract). Huang, B.C., Otofuji, Y.I., Yang, Z.Y., Zhu, R.X., 2000. New Silurian and Devonian paleomag- Tseng, C.Y., Yang, H.Y., Wan, Y.S., Liu, D.Y., Wen, D.J., Lin, T.C., Tung, K.A., 2006. Finding of netic results from the Hexi Corridor terrane, Northwest China, and their tectonic Neoproterozoic (∼775 Ma) magmatism recorded in metamorphic complexes from implications. Geophysical Journal International 140, 132–146. the North Qilian orogen: Evidence from SHRIMP zircon U–Pb dating. Chinese Science Huang, B.C., Otofuji, Y.I., Zhu, R.X., Shi, R.P., Wang, Y.C., 2001. Paleomagnetism of Carbon- Bulletin 51 (8), 963–970. iferous sediments in the Hexi corridor: its origin and tectonic implication. Earth and Tseng, C.Y., Yang, H.J., Yang, H.Y., Liu, D.Y., Wu, C.L., Cheng, C.K., Chen, C.H., Ker, C.M., 2009. Planetary Science Letters 194, 135–149. Continuity of the North Qilian and North Qinling orogenic belts, Central Orogenic Sys- Jayananda, M., Moyen, J.F., Martin, H., Peucat, J.J., Auvray, B., Mahabaleswar, B., 2000. Late tem of China: evidence from newly discovered Paleozoic adakitic rocks. Gondwana Archaean (2550–2520 Ma) juvenile magmatism in the Eastern Dharwarcraton, Research 16, 285–293. southern India: constraints from geochronology, Nd–Sr isotopes and whole rock geo- Tung, K.A., Yang, H.J., Yang, H.Y., Liu, D.Y., Zhang, J.X., Wan, Y.S., Tseng, C.Y., 2007. SHRIMP chemistry. Precambrian Research 99, 225–254. U–Pb geochronology of the zircons from the Precambrian basement of the Qilian Jia, L.T., Zhu, M., Zhao, W.J., 2010. A new antiarch fish from the Upper Devonian Block and its geological significances. Chinese Science Bulletin 52, 2687–2701. Zhongning Formation of Ningxia, China. Palaeoworld 19, 136–145. Tung, K.A., Yang, H.Y., Liu, D.Y., Zhang, J.X., Yang, H.J., Shau, Y.H., Tseng, C.Y., 2012. The Jiang, N., Guo, J.H., Zhai, M.G., Zhang, S.Q., 2010. −2.7 Ga crust growth in the North China amphibolite-facies metamorphosed mafic rocks from the Maxianshan area, Qilian Craton. Precambrian Research 179, 37–49. block, NW China: a record of early Neoproterozoic arc magmatism. Journal of Asian Kemp, A.I.S., Hawkesworth, C.J., Paterson, B.A., Kinny, P.D., 2006. Episodic growth of the Earth Sciences 46, 177–189. Gondwana supercontinent from and oxygen isotopes in zircon. Nature Tung, K.A., Yang, H.Y., Liu, D.Y., Zhang, J.X., Yang, H.J., Shau, Y.H., Tseng, C.Y., 2013. The 439, 580–583. Neoproterozoic granitoids from the Qilian block, NW China: evidence for a link be- Kinny, P.D., Maas, R., 2003. Lu–Hf and Sm–Nd isotope systems in zircon. In: Hanchar, J.M., tween the Qilian and South China blocks. Precambrian Research 235, 163–189. Hoskin, P.W.O. (Eds.), Zircon. Reviews in Mineralogy and Geochemistry, 53, pp. 327–341. Veevers, J.J., Saeed, A., Belousova, E.A., Griffin, W.L., 2005. U–Pb ages and source composi- Kinny, P.D., Compston, W., Williams, I.S., 1991. A reconnaissance ionprobe study of hafni- tion by Hf-isotope and trace-element analysis of detrital zircons in Permian sandstone um isotopes in zircons. Geochimica et Cosmochimica Acta 55, 849–859. and modern sand from southwestern Australia and a review of the paleogeographical Li, C.Y., Wang, Q., Liu, X.Y., Tang, Y.Q., 1982. Tectonic Map of (scale 1:8,000,000). and denudational history of the Yilgarn Craton. Earth Science Reviews 68, 245–279. Cartographic Publishing House, Beijing, 49 (In Chinese). Wan, Y.S., Yang, J.S., Xu, Z.Q., Wu, C.L., 2000. Geochemical characteristics of rocks from the Li, X.H., Su, Li, Song, B., Liu, D.Y., 2004. SHRIMP U–Pb zircon age of the Jinchuan ultramafic Maxianshan complex and Xinglongshan group in the eastern segment of Qilian oro- intrusion and its geological significance. Chinese Science Bulletin 49 (4), 401–402. genic Belt. Journal of the Geological Society of China 43, 52–68. Li,Q.L.,Chen,F.K.,Guo,J.H.,Li,X.H.,Yang,Y.H.,Siebel,W.,2007.Zircon ages and Nd–Hf isotopic Wan, Y.S., Xu, Z.Q., Yang, J.S., Zhang, J.X., 2003. The Precambrian high-grade basement of composition of the Zhaertai Group (Inner Mongolia): evidence for early Proterozoic evolu- the Qilian Terrane and neighboring areas: its ages and compositions. Acta Geoscientia tion of the northern North China Craton. Journal of Asian Earth Sciences 30, 573–590. Sinica 24 (4), 319–324 (In Chinese with English abstract). W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282 1281

Wan, Y.S., Song, B., Liu, D.Y., Wilde, S.A., Wu, J.S., Shi, Y.R., Yin, X.Y., Zhou, H.Y., 2006. Yang, Z.Y., Otofuji, Y.I., Sun, Z.M., Huang, B.C., 2002. Magnetostratigraphic constraints on SHRIMP U–Pb zircon geochronology of Palaeoproterozoic metasedimentary rocks in the Gondwanan origin of North China: Cambrian/Ordovician boundary results. Geo- the North China Craton: evidence for a major Late Palaeoproterozoic tectonothermal physical Journal International 151 (1), 1–10. event. Precambrian Research 149 (3–4), 249–271. Yang, Z.Y., Sun, Z.M., Yang, T.S., Pei, J.L., 2004. A long connection (750–380 Ma) between Wan, Y.S., Liu, D.Y., Wang, S.J., Yang, E.X., Wang, W., Dong, C.Y., Zhou, H.Y., Du, L.L., Yang, South China and Australia: paleomagnetic constraints. Earth and Planetary Science Y.H., Diwu, C.R., 2011a. ∼2.7 Ga juvenile crust formation in the North China Craton Letters 220, 423–434. (Taishan–Xintai area, western Province): further evidence of an understated Yang, G., Du, A.D., Lu, J.R., Qu, W.J., Chen, J.F., 2005. Re–Os (ICP–MS) dating of the massive sul- event from U–Pb dating and Hf isotopic composition of zircon. Precambrian Research fide from the Jinchuan Ni–Cu–PGE deposit. Science in China Series D 35 (3), 241–245. 186, 169–180. Yang, J.H., Wu, F.Y., Wilde, S.A., Xie, L.W., Yang, Y.H., Liu, X.M., 2006. Constains on the Wan, Y.S., Liu, D.Y., Wang, W., Song, T.R., Kroner, A., Dong, C.Y., Zhou, H.Y., Yin, X.Y., 2011b. timing of uplift of the Yanshan Fold and Thrust Belt, North China. Earth and Planetary U–Pb and Hf isotopic study of detrital zircons from the Wulashan : con- Science Letters 246, 336–352. straints on the evolution of the Ordos Terrane, Western Block of the North China Cra- Yang, J.H., Du, Y.S., Cawood, P.A., Xu, Y.J., 2009. Silurian collisional suturing onto the south- ton. Gondwana Research 20, 219–242. ern margin of the North China craton: detrital zircon geochronology constraints from Wang, S.Q., Yu, Z.Z., Wang, C., 1995. Discovery of Late Devonian Sinoleperditiini the Qilian Orogen. Sedimentary Geology 220, 95–104. (Ostracoda) in Zhongwei-Zhongning Basin of Ningxia. Journal of Stratigraphy 19 Yang, Q.Y., Santosh, M., Shen, J.F., Li, S.R., 2014. Juvenile vs. recycled crust in NE (3), 204–207 (In Chinese with English abstract). China: zircon U–Pb geochronology, Hf isotopes and an integrated model for Me- Wang, Y.C., Zhang, Q., Qian, Q., Zhou, M.F., 2005. Geochemistry of the Early Paleozoic sozoic gold mineralization in the Jiaodong Peninsula. Gondwana Research 25 (4), Baiyin Volcanic Rocks (NW China): implications for the Tectonic Evolution of the 1445–1468. North Qilian Orogenic Belt. The Journal of Geology 113 (1), 83–94. Yao, J.L., Shu, L.S., Santosh, M., 2011. Detrital zircon U–Pb geochronology, Hf-isotopes and Wang, H.L., He, S.P., Chen, J.L., Xu, X.Y., Song, Y., Diwu, C.R., 2007. LA–ICPMS dating of zir- geochemistry—new clues for the Precambrian crustal evolution of Cathaysia Block, con U–Pb and its tectonic significance of Maxianshan granitoid intrusive complex, South China. Gondwana Research 20, 553–567. Gansu province. Acta Geologica Sinica 81 (1), 72–78 (In Chinese with English Yin, C.Q., Zhao, G.C., Guo, J.H., Sun, M., Xia, X.P., Zhou, X.W., Liu, C.H., 2011. U–Pb and Hf abstract). isotopic study of zircons of the Helanshan complex: constrains on the evolution of Wang, W., Liu, S.W., Bai, X., Yang, P.T., Li, Q.G., Zhang, L.F., 2011. Geochemistry and zircon the Khondalite Belt in the Western Block of the North China Craton. Lithos 122, U–Pb–Hf isotopic systematics of the Neoarchean Yixian–Fuxin , 25–38. northern margin of the North China Craton: implications for petrogenesis and tecton- Ying, J.F., Zhang, H.F., Tang, Y.J., 2011. Crust–mantle interaction in the central North China ic setting. Gondwana Research 20, 64–81. Craton during the Mesozoic: evidence from zircon U–Pb chronology, Hf isotope and Wang, Y., Zhou, L.Y., Zhao, L.J., 2013. Cratonic reactivation and orogeny: an example from geochemistry of syenitic–monzonitic intrusions from province. Lithos 125, the northern margin of the North China Craton. Gondwana Research 24 (3-4), 449–462. 1203–1222. Yu, J.H., O'Reilly, S.Y., Wang, L.J., Griffin, W.L., Zhang, M., 2008. Where was South China in Wu, H.N., Zhou, L.F., Zhao, Z.Y., 1993. Tectonic implication of the paleomagnetic result of the Rodinia supercontinent? Evidence from U–Pb geochronology and Hf isotopes of the later Paleozoic and Mesozoic rocks from the Alax area of the western North China detrital zircons. Precambrian Research 164, 1–15. block. Science Geology Sinica 2 (1), 19–46 (In Chinese with English abstract). Yu, J.H., Wang, L.J., O'Reilly, S.Y., Griffin, W.L., Zhang, M., Li, C.Z., Shu, L.S., 2009. A Wu, F.Y., Yang, J.H., Liu, X.M., Li, T.S., Xie, L.W., Yang, Y.H., 2005. Hf isotopes of the 3.8 Ga Paleoproterozoic orogeny recorded in a long-lived cratonic remnant (Wuyishan ter- zircons in eastern Province, China: implications for early crustal evolution of rane), eastern Cathaysia Block, China. Precambrian Research 174, 347–363. the North China Craton. Chinese Science Bulletin 50 (21), 2473–2480. Yu, J.Y., Li, X.M., Ma, Z.P., Wang, G.Q., Wu, P., 2010. Geochemical characters and LA–ICP– Wu, C.L., Yao, S.Z., Yang, J.S., Zeng, L.S., Chen, S.Y., Wooden, J.L., Mazda, F., 2006. Double MS Zircon U–Pb dating of the lenglongling volcanic rocks, Tectonic Belt of the subduction of the Early Paleozoic North Qilian oceanic Plate: evidence from gran- North Qilian. Geological Science and Technology Information 29 (4), 6–13. ites in the central segment of North Qilian, NWChina. Geology in China 33 (6), Yu, J.H., O'Reilly, S.Y., Wang, L.J., Griffin, W.L., Zhou, M.F., Zhang, M., Shu, L.S., 2010. 1197–1208 (In Chinese with English abstract). Components and episodic growth of Precambrian crust in the Cathaysia Block, Wu, C.L., Gao, Y.H., Frost, B.R., Robinson, P.T., Wooden, J.L., Wu, S.P., Chen, Q.L., Lei, M., South China: evidence from U–Pb ages and Hf isotopes of zircons in Neoproterozoic 2011. An early Palaeozoic double-subduction model for the North Qilian oceanic sediments. Precambrian Research 181 (1), 97–114. plate: evidence from zircon SHRIMP dating of granites. International Geology Review Yu, S.Y., Zhang, J.X., Real, P.G.D., Zhao, X.L., Hou, K.J., Gong, J.H., Li, Y.S., 2013. The 53 (2), 157–181. Grenvillian orogeny in the Altun–Qilian–North Qaidam mountain belts of northern Xia, L.Q., Xia, Z.C., Xu, X.Y., 2003. Magmagenesis in the Ordovician backarc basins of the Tibet Plateau: constraints from geochemical and zircon U–Pb age and Hf isotopic northern Qilian Mountains, China. Geological Society of America Bulletin 115, study of magmatic rocks. Journal of Asian Earth Sciences 73, 372–395. 1510–1522. Zhai, M.G., Santosh, M., 2013. Metallogeny of the North China Craton: link with secular Xia, X.P., Sun, M., Zhao, G.C., Luo, Y., 2006a. LA–ICP–MS U–Pb geochronology of detrital changes in the evolving Earth. Gondwana Research 24, 275–297. zircons from the Jining Complex, North China Craton and its tectonic significance. Zhang, J.X., Xu, Z.Q., Chen, W., Xu, H.F., 1997. A tentative discussion on the ages of the sub- Precambrian Research 144, 199–212. duction–accretionary complex/volcanic arcs in the middle sector of North Qilian Xia, X.P., Sun, M., Zhao, G.C., Wu, F.Y., Xu, P., Zhang, J.H., Luo, Y., 2006b. U–Pb and Hf iso- Mountain. Acta Petrologica et Mineralogica 16 (2), 112–119 (In Chinese with English topic study of detrital zircons from the Wulashan khondalites: constraints on the abstract). evolution of the Ordos Terrane, Western Block of the North China Craton. Earth and Zhang, H.F., Jin, L.L., Zhang, L., Yuan, H.L., Zhou, L., Zhang, B.R., 2006. Pb and Nd Isotopic Planetary Science Letters 241, 581–593. compositions of basement and granitoid in the Qilianshan: constraints on tectonic Xiao, W.J., Han, C.M., Yuan, C., Sun, M., Lin, S.F., Chen, H.L., Li, J.L., Sun, S., 2008. Middle affinity. Earth Science-Journal of China University of Geosciences 31 (1), 57–65. Cambrian to Permian subduction-related accretionary orogenesis of Northern Zhang,J.,Li,J.Y.,Liu,J.F.,Feng,Q.W.,2011.Detrital zircon U–Pb ages of Middle Ordo- , NW China: implications for the tectonic evolution of central Asia. Journal vician flysch sandstones in the western ordos margin: new constraints on their of Asian Earth Sciences 32 (2), 102–117. provenances, and tectonic implications. Journal of Asian Earth Sciences 42 (5), Xiao, W.J., Windley, B.F., Yong, Y., Yong, Y., Yan, Z., Yuan, C., Liu, C.Z., Li, J.L., 2009. Early 1030–1047. Paleozoic to Devonian multiple-accretionary model for the Qilian Shan, NW China. Zhang, X.J., Zhang, L.C., Xiang, P., Wan, B., Pirajno, F., 2011. Zircon U–Pb age, Hf isotopes Journal of Asian Earth Sciences 35, 323–333. and geochemistry of Shuichang Algoma-type banded iron-formation, North China Xiao, W.J., Huang, B.C., Han, C.M., Sun, S., Li, J.L., 2010. A review of the western part of the Craton: constraints on the -forming age and tectonic setting. Gondwana Research Altaids: a key to understanding the architecture of accretionary orogens. Gondwana 20, 137–148. Research 18 (2), 253–273. Zhang, H.F., Zhu, R.X., Santosh, M., Ying, J.F., Su, B.X., Hu, Y., 2013a. Episodic widespread Xie, L.W., Zhang, Y.B., Zhang, H.H., Sun, J.F., Wu, F.Y., 2008. In situ simultaneous determi- magma underplating beneath the North China Craton in the Phanerozoic: implica- nation of trace elements, U–Pb and Lu–Hf isotopes in zircon and baddeleyite. Chinese tions for craton destruction. Gondwana Research 23, 95–107. Science Bulletin 53, 1565–1573. Zhang, J.X., Yu, S.Y., Gong, J.H., Li, H.K., Hou, K.J., 2013b. The latest Neoarchean– Xu, Y.J., Du, Y.S., Cawood, P.A., Guo, H., Huang, F.H., An, Z.H., 2010a. Detrital zircon record Paleoproterozoic evolution of the Dunhuang block, the eastern Tarim craton of north- of continental collision: assembly of the Qilian Orogen, China. Sedimentary 230, western China: evidence from zircon U–Pb datings and Hf isotopic analyses. Precam- 35–45. brian Research 226, 21–42. Xu, Y.J., Du, Y.S., Cawood, P.A., Yang, J.H., 2010b. Provenance record of a foreland basin: Zhang, J.X., Gong, J.H., Yu, S.Y., Li, H.K., Hou, K.J., 2013c. Neoarchean–Paleoproterozoic detrital zircon U–Pb ages from Devonianstrata in the North Qilian OrogenicOrogen, multiple tectonothermal events in the western Alxa block, North China Craton and China. Tectonophysic 495, 337–347. their geological implication: evidence from zircon U–Pb ages and Hf isotopic compo- Yang, Z.Y., Besse, J., 2001. New Mesozoic apparent polar wander path for south China: sition. Precambrian Research 235, 36–57. tectonic consequences. Journal of Geophysical Research 106 (B5), 8493–8520. Zhao, G.C., 2009. Metamorphic evolution of major tectonic units in the basement of Yang, Z.D., Pan, X.S., Yang, Y.F., 1988. Geological Struture Characteristics and Deposites of the North China Craton: key issues and discussion. Acta Petrologica Sinica 25, Alax Block and adjacent region. Science Press, Beijing 1–254 (In Chinese). 1772–1792. Yang, Z.Y., Courtillot, V., Besse, J., Ma, X.H., Xing, L.S., Xu, S.J., Zhang, J.X., 1992. pa- Zhao, G.C., Zhai, M.G., 2013. Lithotectonic elements of Precambrian basement in the North leomagnetic constraints on the relative motions and collision of the North and South China Craton: review and tectonic implications. Gondwana Research 23, 1207–1240. China blocks. Geophysical Research Letters 19 (6), 577–580. Zhao, G.C., Sun, M., Wilde, S.A., Li, S.Z., 2004. A Paleo-Mesoproterozoic supercontinent: Yang, Z.Y., Sun, Z.M., Ma, X.M., Huang, B.C., Dong, J.M., Zhou, Y.X., Zhu, H., 1996. Preliminary assembly, growth, and breakup. Earth-Science Reviews 67, 91–123. palaeomagnetic results from the Lower Palaeozoic of North China ( Province) Zhao,G.C.,Sun,M.,Wilde,S.A.,Li,S.Z.,2005.Late Archean to Paleoproterozoic evolu- and its implications. Chinese Science Bulletin 42, 401–405. tion of the North China Craton: key issues revisited. Precambrian Research 136, Yang, Z.Y., Ma, X.H., Huang, B.C., Sun, Z.M., Zhou, Y.X., 1998. Apparent polar wander path 177–202. and tectonic movement of the North China Block in Phanerozoic. Science in China Se- Zheng, S.C., Zhu, H., 1987. Stratigraphy development and tectonic evolution of Paleozoic ries D 41, 51–64 (Suppl.). in the margin of the Alax massif. In: Zhu, H., Zheng, S.C., He, X.Y. (Eds.), Paleozoic 1282 W. Yuan, Z. Yang / Gondwana Research 27 (2015) 1270–1282

Biostratigraphy and Tectonic Evolution of the Alax Massif Margin. Wuhan College of Zheng, Y.F., Xiao, W.J., Zhao, G.C., 2013b. Introduction to tectonics of China. Gondwana Geology Press, pp. 1–19. Research 23, 1189–1206. Zheng, J.P., Griffin, W.L., O'Reilly, S.Y.O., Lu, F.X., Wang, C.Y., Zhang, M., Wang, F.Z., Li, H.M., Zhou, J.B., Wilde, S.M., 2013. The crustal accretion history and tectonic evolution of the NE 2004. 3.6Ga lower crust in central China: new evidence on the assembly of the North China segment of the Central Asian Orogenic Belt. Gondwana Research 23, China craton. Geology 32 (3), 229–232. 1365–1377. Zheng, J.P., Griffin, W.L., O'Reilly, S.Y.O., Zhao, J.H., Wu, Y.B., Liu, G.L., Pearson, N., Zhang, M., Zhou, Z.Q., Cao, X.D., Hu, Y.X., Zhao, J.T., 1996. Early Paleozoic stratigraphy and sedimen- Ma,C.Q.,Zhang,Z.H.,Yu,C.M.,Su,Y.P.,Tang,H.Y.,2009.Neoarchean (2.7–2.8 Ga) ac- tary tectonic evolution in eastern Qilian Mountains, China. Northwestern Geoscience cretion beneath the North China Craton: U–Pb age, trace elements and Hf isotopes of 17 (1), 1–53 (In Chinese with English abstract). zircons in diamondiferous . Lithos 112, 188–202. Zhou, Y.Y., Zhao, T.P., Wang, Y.C., Hu, G.H., 2011. Geochronology and geochemistry of 2.5 Zheng, J.P., Griffin, W.L., Li, L.S., O'Reilly, S.Y.O., Pearson, N.J., Tang, H.Y., Liu, G.L., Zhao, J.H., to 2.4 Ga granitic plutons from the southern margin of the North China Craton: Yu, C.M., Su, Y.P., 2011. Highly evolved Archean basement beneath the western implications for a tectonic transition from arc to post-collisional setting. Gondwana Cathaysia Block, South China. Geochimica et Cosmochimica Acta 75, 242–255. Research 20, 171–183. Zheng, R.G., Wu, T.R., Zhang, W., Xu, C., Meng, Q.P., Zhang, Z.Y., 2014a. Late Paleozoic Zhu, D.C., Zhao, Z.D., Niu, Y.L., Dilek, Y., Mo, X.X., 2011. Lhasa terrane in southern Tibet subduction system in the northern margin of the Alxa block, Altaids: geochrono- came from Australia. Geology 39, 727–730. logical and geochemical evidences from . Gondwana Research 25 (2), 842–858.