The late-Paleoproterozoic I- and A-type granites in Lüliang Complex, North China Craton: New evidence on post-collisional extension of Trans-North China Orogen

Accepted Manuscript The late-Paleoproterozoic I- and A-type granites in Lüliang Complex, North China Craton: new evidence on post-collisional extension of Trans-North China Orogen Jiao Zhao, Chengli Zhang, Xiaojun Guo, Xinyu Liu PII: DOI: Reference:

S0301-9268(18)30077-9 https://doi.org/10.1016/j.precamres.2018.09.007 PRECAM 5179

To appear in:

Precambrian Research

Received Date: Revised Date: Accepted Date:

2 February 2018 13 August 2018 21 September 2018

Please cite this article as: J. Zhao, C. Zhang, X. Guo, X. Liu, The late-Paleoproterozoic I- and A-type granites in Lüliang Complex, North China Craton: new evidence on post-collisional extension of Trans-North China Orogen, Precambrian Research (2018), doi: https://doi.org/10.1016/j.precamres.2018.09.007

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Abstract The late-Paleoproterozoic granitoids from Lüliang Complex can provide pivotal constraints on the amalgamation process between Eastern and Western blocks of North China Craton along the Trans-North China Orogen. LA-ICPMS zircon dating gives emplacement ages of 1854± 20 Ma for the Huijiazhuang granite, 1830±21 Ma for the Xiyupi granite vein and 1760±20 Ma for the Dacaoping porphyritic granite, respectively. The Huijiazhuang granite and Xiyupi granite dyke have variable SiO2 (66.71-74.31 wt.%), high K2O (5.09-6.35 wt.%), low P2O5 (0.020.16 wt.%), Al2O3 (13.92-15.31 wt.%), right inclined REE patterns with medium negative Eu anomalies, enrichment in LILE, depletion in HFSE, especially Nb, Ta, consisting to high-K I-type granite in a post-collisional setting. The Sr/Y (7.36-59.95), εNd(t) (-5.7 to -4.1) with TDM (2381 Ma to 2570 Ma) from whole rock Sm-Nd isotope and εHf(t) (-9.6 to 2.3) with TCDM (2360 Ma to 3070 Ma) from zircon Lu-Hf isotope suggest that they are produced by partial melting of slightly thickened NeoarcheanPaleoproterozoic basement materials (including both meta-sedimentary and metaigneous rocks). The Dacaoping porphyritic granites are characterized by high SiO2 (70.83-74.30 wt.%), K2O (4.84-5.60 wt.%), FeOT/(FeOT+MgO) (0.86-0.92), “seagulltype” REE pattern with strong negative Eu anomaly (δEu=0.16-0.35) and higher 10000*Ga/Al (2.99-3.36), HFSE (Zr+Nb+Ce+Y=378-583 ppm), showing an affinity of A2-type granite. They have low Sr/Y (1.17-8.62), εNd(t) (-6.1 to -6.4) with TDM (2690 Ma to 2776 Ma) from whole rock Sm-Nd isotope and εHf(t) (-7.9 to -5.2) with TCDM (2775-2938 Ma) from zircon Lu-Hf isotope, indicating a result from the melting of thinned Neoarchean calc-alkaline intermediate basement. Taking into account the temporal-spatial distributions of late-Paleoproterozoic rocks in the Trans-North China Orogen, it suggests a post-collisional extension occurred during 1.89-1.76 Ga and the crust is thinned visibly since 1.82 Ga. The late-Paleoproterozoic I- and A-type granites in Lüliang Complex, North China Craton: new evidence on post-collisional extension of Trans-North China Orogen Jiao Zhao a, Chengli Zhang a,*, Xiaojun Guo b, Xinyu Liu a aState

Key Laboratory of Continental Dynamics, Department of Geology, Northwest

University, Xi’an 710069, China bNo.5

Gold Geological Party of Chinese Armed Police Force, Xi’an 710100, China

ABSTRACT The late-Paleoproterozoic granitoids from Lüliang Complex can provide pivotal constraints on the amalgamation process between Eastern and Western blocks of North China Craton along the Trans-North China Orogen. LA-ICP-MS zircon dating gives emplacement ages of 1854± 20 Ma for the Huijiazhuang granite, 1830±21 Ma for the Xiyupi granite vein and 1760± 20 Ma for the Dacaoping porphyritic granite, respectively. The Huijiazhuang granite and Xiyupi granite dyke have variable SiO2 (66.71-74.31 wt.%), high K2O (5.09-6.35 wt.%), low P2O5 (0.02-0.16 wt.%), Al2O3 (13.92-15.31 wt.%), right inclined REE patterns with medium negative Eu anomalies, enrichment in LILE, depletion in HFSE, especially Nb, Ta, consisting to high-K Itype granite in a post-collisional setting. The Sr/Y (7.36-59.95), εNd(t) (-5.7 to -4.1) with TDM (2381 Ma to 2570 Ma) from whole rock Sm-Nd isotope and εHf(t) (-9.6 to 2.3) with TCDM (2360 Ma to 3070 Ma) from zircon Lu-Hf isotope suggest that they are produced by partial melting of slightly thickened Neoarchean-Paleoproterozoic basement materials (including both meta-sedimentary and meta-igneous rocks). The Dacaoping porphyritic granites are characterized by high SiO2 (70.83-74.30 wt.%), K2O (4.84-5.60 wt.%), FeOT/(FeOT+MgO) (0.86-0.92), “seagull-type” REE pattern with strong negative Eu anomaly (δEu=0.16-0.35) and higher 10000*Ga/Al (2.993.36), HFSE (Zr+Nb+Ce+Y=378-583 ppm), showing an affinity of A2-type granite. They have low Sr/Y (1.17-8.62), εNd(t) (-6.1 to -6.4) with TDM (2690 Ma to 2776 Ma) from whole rock Sm-Nd isotope and εHf(t) (-7.9 to -5.2) with TCDM (2775-2938 Ma) from zircon Lu-Hf isotope, indicating a result from the melting of thinned Neoarchean calc-alkaline intermediate basement. Taking into account the temporal-spatial distributions of late-Paleoproterozoic rocks in the Trans-North China Orogen, it suggests a post-collisional extension occurred during 1.89-1.76 Ga and the crust is thinned visibly since 1.82 Ga. Key words: granitoids; late-Paleoproterozoic; post-collision; Lüliang Complex; North China Craton

1. Introduction Orogeny is the natural consequence of plate tectonics and is driven by a variety of forces most notably the descent of oceanic lithosphere at subduction zones (Davies and von Blanckenburg, 1995; Conrad and Lithgow-Bertelloni, 2002). Magmatic records display distinct response to the different stages from subduction to collision: in the initial collisional stage, normal arc-type calc-alkaline magmas mark oceanic plate subduction; in the syn-collisional stage, minor magmatic rocks are mostly peraluminous when the oceanic plate subduction terminates (Harris et al., 1986); in the post-collisional stage, slab breakoff often opens slab window and consequently triggers partial melting of differing magma sources, producing intense magmatism with compositional diversity, including OIB-like basalts, high-K calc-alkaline intermediate-acidic and A2-type rocks (von Blanckenburg and Davies, 1995; Zhu et al., 2015). Therefore, magmatism can provide important time-stamp on the sequence of orogenic events. The 2.0-1.8 Ga collision-type orogenic belts in the Earth recorded a global continental collision event, resulting in the formation of the Meso-Paleoproterozoic supercontinent lately named as Columbia or Nuna (Zhao et al., 2002a; Rogers and Santosh, 2002). Similar to most other cratons (Laurentia, Baltica, Siberia, Amazonia, West African, South Africa, India, Australia, and Antarctica), the discovery of TransNorth China Orogen (TNCO) confirmed that the basement of the North China Craton (NCC) resulted from the amalgamation of two discrete continental blocks of the Western and Eastern Blocks at late-Paleoproterozoic. The late-Paleoproterozoic tectonic framework and geological events documented of TNCO have deepened the understanding on Paleoproterozic amalgamation of NCC. As a key aspect to clearly explore the picture of orogenic process, metamorphic and geochronological investigations on high-pressure granulites with clockwise P-T paths of the metamorphic terranes have led Zhao et al. (2012) to suggest that the TNCO was formed due to the collision process at ~1.85 Ga. Recently, the ~1.95 Ga metamorphic ages are reported and new interpretations have emerged that the age of ~1.95 Ga

records the timing of the main collision and/or crust thickening, and the relatively

younger ages of 1.93-1.80 Ga reflect the timing of uplift and cooling of the thickened crust after the collision (Qian et al., 2013, 2015; Wei et al., 2014; Zhang et al., 2016; Wu et al., 2017; Xiao et al., 2017; Zhao et al., 2017a). Some studies on mafic dykes swarms and Xiong'er volcanic belt have been representative of the ending time of the orogenic process. Wang et al. (2014a) suggests the 1.78-1.75 Ga mafic dykes are emplaced during a post-orogenic extensional event, whereas some researchers believe that they are formed under rifting setting, marking the initiation of the breakup of the Columbia surpercontinent (Peng et al., 2005). The ~1.78 Ga Xiong'er volcanic rocks have been interpreted as the products in an intra-continental rift setting or subduction zone at the southern margin of NCC (Peng et al., 2008; Zhao et al., 2009). For the controversies aforementioned, it is critical to study the magmatism which identifies various stages of orogenic process well. Currently several ~1.8 Ga A2-type granites in the southern margin of the NCC are thought to be emplaced in a postorogenic extensional tectonic settings (Zhao and Zhou, 2009; Gao et al., 2013; Zhang et al., 2013; Deng et al., 2016; Shi et al., 2017). The Lüliang Complex in the central part of TNCO consists of widespread late-Paleoproterozoic granitoids, which is an ideal area to probe the orogenic process. Previous studies on the granitoids focus more attention on the geochronology and field geological investigation, detail researches on petrogenesis are quite few (Geng et al., 2006; Zhao et al., 2008b). Liu et al. (2009) obtained 1.9-1.85 Ga formation age of the Guandishan granitoid intrusions with gneissic to massive structures and suggested they were produced in a syn-collisional to post-collisional setting. Obviously, the clearly division of magmatism stages and genetic types for all granitoids in the Lüliang Complex are weaknesses, which no doubt hinders the understanding of orogenic process. In this paper, we present systematic LA-ICP-MS zircon U-Pb ages, in situ zircon Lu-Hf isotope, whole-rock major, trace elemental compositions and Sm-Nd isotope for the late-Paleoproterozoic granites in Lüliang Complex to conform their ages, petrogenesis, and further to constrain their tectonic process related to amalgamation between Eastern and Western Blocks of the NCC along TNCO.

2. Geological setting The basement of the NCC was divided into the Eastern and Western Blocks and intervening TNCO. In which, the TNCO is situated in the central NCC and trend in an approximate N-S with a length of ~1200 km and width of 100-300 km (Zhao et al., 2000, 2005). It is bounded by the Xinyang-Kaifeng-Shijiazhuang-Jianping Faults to the east and the Huashan-Lishi-Datong-Duolun Faults to the west (Fig. 1). The TNCO is composed of the Neoarchean to Paleoproterozoic TTG gneisses, metasupracrustal rocks, syn- and post-tectonic granites and mafic dykes. Geochemical and isotopic data suggest that most igneous rocks are dominated by the arc-related juvenile crust with minor rocks formed from Neoarchean to early Paleoproterozoic (Zhao and Kröner, 2007; Huang et al., 2010). Minor ancient oceanic fragments of ultramafic to mafic rocks in the Jingangku Formation were reported in the Wutai Complex (Wang et al., 1997; Polat et al., 2005). In addition, younger sequence-set of low-grade supracrustal successions with syn-tectonic foreland basin characters have been found in the Wutai, Lüliang, Zanhuang and Zhongtiao Complexes, respectively (Liu et al., 2011a, b, 2012a, b; Hu et al., 2017). Furthermore, the classical indicators of collision tectonics, such as linear structures of the strike-slip ductile shear zones, large scale thrust-fold and transcurrent tectonics (Zhang et al., 2007, 2009, 2012; Trap et al., 2009, 2012), high-pressure granulites and retrograde eclogite with a clockwise near-isothermal decompression metamorphic P-T paths, were found in the Hengshan, Huai’an and Chengde Complexes, respectively (Zhai et al., 1996, 1997; Zhao et al., 2000; Qian et al., 2013, 2015; Wei et al., 2014; Zhang et al., 2016). These features contrast with those in the Eastern and Western Blocks and led Zhao et al. (2000) to propose that the TNCO is a continent-continent collisional belt, along which the Eastern and Western Blocks amalgamated to form the coherent basement of the NCC. As one of an important component in the TNCO, the Lüliang Complex is situated at its central section (Fig. 1) and consists of the late-Neoarchean to Paleoproterozoic magmatic rocks and meta-supracrustal rocks of the Jiehekou, Lüliang, Yejishan, Heichashan and Lanhe Groups (Fig. 2; Geng et al., 2006; Zhao et al., 2008b; Liu et al., 2009; Trap et al., 2009; Liu et al., 2011a, 2013, 2014a, 2014b; Du et al., 2012;

Santosh et al., 2015; Yang and Santosh, 2015; Zhao et al., 2015, 2017a, 2017b; Xiao et al., 2017). The Jiehekou Group is composed mainly of meta-argilloarenaceous rocks, marble and minor amphibolite, and underwent to granulite facies metamorphism. They were regarded as deposition on the stable continental margin surrounding the Ordos block during the period of 2.0-1.90 Ga based on their khondalite series feature and the youngest age peak of ~2.0 Ga from detrital zircons and metamorphic ages of 1.911.85 Ga from zircon and monazite within them (Trap et al., 2009; Liu et al., 2013). While, Liu et al. (2012d) suggested they were formed in an active continental margin setting due to some interbedding of metamorphic volcanics and minor igneous plutons related to island-arc. Based on the EPMA Th-U-Pb monazite dating, Liu et al. (2006, 2007a) and Trap et al. (2009) distinguished two age groups of 1.94-1.91 Ga and 1.881.85 Ga. Of which the former is interpreted as the timing of an early magmatic event, and the latter as the age of major metamorphic event. New zircon U-Pb dating from pelitic migmatite and mafic granulite indicated that their main metamorphism occurred at 1.95-1.92 Ga, most likely representative of peak age of a long-lived continent-continent collision between Eastern and Western Blocks from 1.95 Ga to 1.80 Ga (Xiao et al., 2017; Zhao et al., 2017a). The Lüliang Group is exposed in the central part of the complex and consists predominantly of meta-sedimentary rocks in the lower sequence and meta-volcanic rocks in the upper sequence (Liu et al., 2014b). The protoliths of the lower sequence was considered to be deposited around 2.2-2.1 Ga (Liu et al., 2014b). While the zircon crystallization ages of ~2.2 Ga have been obtained from meta-basalt in the upper sequence (Liu et al., 2012d; Liu et al., 2014b; Zhao et al., 2017b), and two contrasting tectonic settings are proposed, including 1) a rift on continent margin and 2) an arc-related basin environment (Geng et al., 2003; Liu et al., 2014b). The Yejishan Group consists of meta-volcanic rocks in the lower sequence and flysch-type meta-sedimentary rocks in the upper sequence (Liu et al., 2011a). The Lanhe Group unconformably overlies the Lüliang Group, and consists of greenschistfacies meta-sedimentary rocks with interbeds of volcanic rocks (Hu et al., 2017). The

Heichashan Group unconformably overlies the Jiehekou Group and mainly consists of meta-conglomerates in the lower part and pebbled feldspar quartzites in the upper part (Liu et al., 2016a). No direct contact relation among the three groups can be found, therefore, their sequence relationship cannot be constrained by the field geology. Liu et al. (2012a) and Liu et al. (2014a) identified a suit of rock association of adakitic rocks, Nb-enriched basalts and andesites in the Yejishan Group, similar to those of arc magmatism in the subduction zone and being interpreted as products formed in active continental margin around 2.2 Ga. However, Wang et al. (2017b) proposed that part of the Yejishan Group was likely formed in an active continental marginal basin at 1.87~1.78 Ga. The Lanhe Group was considered to be formed in back-arc basin in the 2.17-1.81 Ga and the Heichashan Group was deposited in a foreland basin before 1.87-1.81 Ga (Liu et al. 2011a, 2016a). More recently, Hu et al. (2017) compared the Lanhe Group to lower sequence of the Yejishan Group and proposed both were deposited in the arc-related basin of continental margin. While the upper sequence of the Yejishan Group are well comparing to the Heichashan Group with molasse affinity and deposited in a foreland basin during the collision between Eastern and Western Blocks (Hu et al., 2017). Based on geochronologic data, the earliest TTG gneisses, monzogranitic gneisses and meta-high-Mg igneous assemblage were recognized in Yunzhong Mountain area, representing the earliest arc-related magmatic event in the Lüliang Complex (Zhao et al., 2008b; Kang et al., 2017; Wang et al., 2018). Whereas, the Gaijiazhuang syenitegranite with typical features of A2-type granite was formed in a post-orogenic setting during 2.41~2.38 Ga (Geng et al., 2006; Zhao et al., 2015). The following 2.2-2.1 Ga magmatic events are widely recorded by Chijianlin-Guandishan gneiss including gneissic tonalities, granodiorites, monzogranites and granitoids, which were proposed as production of continental arc magmatism (Liu et al., 2009; Santosh et al., 2015). However, Du et al. (2012) defined the Dujiagou porphyrite as A-type granite, and postulates that 2.2-2.1Ga magmatic rocks were formed under the rifting regimes related to island arc. The late-Paleoproterozoic magmatism include granitic intrusions, mafic dykes

and granite dykes. Of which, the granitoids are mainly distributed in the south of Lüliang Complex, the widely area that west to Fangshan County and east to Jiaocheng County, and intruded into Chijianling-Guandishan gneiss. Based on field-based structural and petrological characteristics, previously incorporated Guandishan granitic batholith with surrounding rock xenoliths could be disintegrated into syn- to post-collisional intrusions, such as Huijiazhuang pluton, Shizhuang pluton, Dacaoping pluton (Geng et al., 2006; Zhao et al., 2008b). Geochemically, Liu et al. (2009) revealed that gneissic to massive monzogranite with or without garnet in the Guandishan granitoid intrusions were produced in a syn-collisional to post-collisional setting during 1.9~1.85 Ga. Furthermore, some contemporaneous granitoids, such as Luyashan charnockite, Luchaogou porphyritic granite, Tangershang massive granite also were reported (Liu et al., 2005; Geng et al., 2006; Zhao et al., 2008b; Yang and Santosh, 2015). As excellent time markers, the ~1.94 Ga NW-SE trending meta-mafic dykes in the study area are arc-related and ~1.78 Ga E-W trending mafic dykes are most likely emplaced along extensional fractures in a post-collisional setting (Wang et al., 2014a, b). Moreover, undeformed medium-grained granite dykes crosscut the migmatites characterized by layered structures of garnet-bearing leucosomes and gneisses mesosomes in the Xiyupi area. 3. Sampling and analytical methods 13 representative samples from Huijiazhuang granites, Xiyupi granite dykes and Dacaoping porphyritic granites were collected for zircon U-Pb-Hf isotope and wholerock major, trace elements, Sm-Nd isotope. Of which, sample 12LL-106, 12LL-107, 12LL-108, 12LL-110 and 12LL-111 (located around 37°38′51.1″N/111°47′10.5″E) were collected from Huijiazhuang granite, showing grayish white and massive structure (Fig. 3a). They are characterized by fine grained granitic texture and composed of K-feldspar (40%), plagioclase (25%), quartz (25%), minor biotite (5%) and accessory minerals (5%) including zircon, apatite, allanite, Fe-Ti oxide, etc (Fig. 3d). Most of K-feldspar appears as microcline with intense kaolinitization. Sample 15LL-16, 15LL-16a, 15LL-16b and 15LL-16c were collected from Xiyupi granite dyke (37°29′57.0″N/111°54′13.2″E), displaying grayish white and

massive structure (Fig. 3b). They are medium grained granitic texture with the composition of K-feldspar (45%), plagioclase (20%), quartz (25%), biotite (5%) and accessory minerals (5%) including zircon, apatite, Fe-Ti oxide, etc (Fig. 3e). Some K-feldspar appears also as microcline. Plagioclase shows albite twin and is sericiticized more or less. Sample 12LL-87, 12LL-88, 12LL-89 and 12LL-90 were collected from Dacaoping porphyritic granite (37°52′32.4″N/111°26′34.6″E), brick red with massive structure (Fig. 3c). They are coarse grained porphyraceous structure and composed of Kfeldspar (50%), plagioclase (15%), quartz (25%), biotite (5%) and accessory minerals (5%) including zircon, apatite, Fe-Ti oxide, etc (Fig. 3f). K-feldspar appears zoning structure. Plagioclase is sericiticized and more or less saussuritized with an edulcoration border. Some biotite is slightly altered to chlorite. 3.1 Zircon U-Pb analyses All the sample were analyzed at the State Key Laboratory of Continental Dynamics, Northwest University, China. Zircons were separated by combined heavy-liquid and magnetic techniques, and handpicked under a binocular microscope. The grains selected were mounted in epoxy resin and then polished to near half of their thickness. After being photographed under a microscope with reflected light, the cathodoluminescence (CL) images of zircons were carried out using the Gatan Mono CL 3+ Fluorescence Spectrometer to demonstrate the internal texture of zircons. LA-ICP-MS zircon U-Pb dating was conducted on Agilent 7500a ICP-MS instrument equipped with a 193 nm (wave length) ArF excimer laser ablation system, which can examine the trace element contents simultaneously. The analytical procedures were described by Yuan et al. (2004). Helium was used as the carrier gas to ensure efficient aerosol delivery to the torch and a beam diameter of 32 um with a laser pulse width of 15ns was adopted throughout analysis processes. The

207Pb/206Pb, 206Pb/238U, 237Pb/235U

and 208Pb/232Th

ratios were calculated using the GLITTER 4.0 program (Macquarie University). The Harvard zircon 91500 was used as an external reference material with a recommended 206Pb/238U

age of 1064.2 ± 1.7 Ma, to correct for both instrumental mass bias and

depth-dependent elemental and isotopic fractionation. The ages were calculated using ISOPLOT 3 (Ludwig, 2003). 3.2 Zircon Lu-Hf isotopic analyses In-situ zircon Lu-Hf isotopic analyses were performed using a Nu Plasma HR MC-ICP-MS (Nu Instrument Ltd., UK) equipped with a GeoLas 193 nm excimer laser-ablation system. Analyses were carried out using a beam size of 44 μm and repetition rate of 10 Hz. Time dependent drifts of Lu-Hf isotopic ratios were corrected using a linear interpolation according to the variations of 91500, Monastery and GJ-1. The analytical procedures are similar to those described by Yuan et al. (2008). The chondritic ratios of

176Hf/177Hf

= 0.282772 and

176Lu/177Hf

= 0.0332 (Blichert-Toft

and Albarède, 1997) were adopted to calculate εHf(t) values at the time of zircon crystallization. Single-stage Hf model ages (TDM) were calculated relative to the depleted mantle with a present-day

176Hf/177Hf

ratio of 0.28325 and

176Lu/177Hf

ratio

of 0.0384 (Griffin et al., 2000). The Hf crustal model ages (TCDM) were calculated by projecting the initial

176Hf/177Hf

of zircon back to the depleted mantle growth curve

using 176Lu/177Hf = 0.015 for the average continental crust (Griffin et al., 2002). 3.3. Whole-rock major and trace elements Fresh chips of whole-rock samples were powdered to 200 mesh using a tungsten carbide ball mill. The 0.7 g sample powders had been dried in an oven at 105 °C for 2 hours were mixed with 5.2 g Li2B4O7, 0.4 g LiF, 0.3 g NH4NO3, minor LiBr in a platinum pot and then fused into glass beads prior to analysis (Wang and Liu, 2016). Major element concentrations were determined on a Rikagu RIX 2100 X-ray fluorescence (XRF) spectrometer, with analytical uncertainties lower than 5 %. H2O was estimated by loss on ignition (LOI). Trace elements were analyzed using an Agilent 7700a inductively coupled plasma mass spectrometer (ICP-MS) employing United States Geological Survey (USGS) and international rock standards (BHVO-2, AGV-2, BCR-2 and GSP-1). For the trace element analysis, sample powders were digested using an HF+HNO3 mixture in high-pressure Teflon bombs at 190 °C for 48 h. For most trace elements, the relative deviation and relative standard deviation are lower than 5 % (Liu et al.,

2007b). 3.4. Whole-rock Sm-Nd isotopic analyses The sample powders were removed with cation AG50W-X8 exchange resin and HDEHP chromatographic column. Whole-rock Sm-Nd isotopic data were obtained using a multicollector inductively coupled plasma mass spectrometry (MC-ICPMS) under static model. NBS981、 NBS987、 La Jolla and JMC475 were used as certified reference standard solutions for

143Nd/144Nd

isotopic ratios. Nd isotopic

fractionation was corrected to 146Nd/144Nd = 0.7219. εNd(t) is calculated using presentday (147Sm/144Nd)CHUR = 0.1967 and (143Nd/144Nd)CHUR = 0.512638 (Hamilton et al., 1983) and TDM,, TDM2 is calculated through present-day (147Sm/144Nd)DM = 0.2137 and (143Nd/144Nd)DM = 0.51315 (Goldstein et al., 1984). 4. Analytical results 4.1 Zircon U-Pb age Representative CL images of the zircons were analyzed together with spot ages and εHf(t) values are shown in Fig. 4. Zircon U-Pb dating results are listed in Table 1 and shown in Fig. 5. Zircons from the Huijiazhuang granite (sample 12LL-111) are transparent and subhedral to euhedral, with lengths and length / width ratios ranging from 100 μm to 150 μm and 3:2 to 2:1, respectively. The CL images show visible oscillatory zonings although low luminescence (Fig. 4). Thirty analyses were conducted on thirty zircons, of which sixteen analyses give discordant age data due to the result of partial Pb-lose reduced by later tectono-thermal event. Another fourteen analyses give variable Th/U of 0.05-1.70, but they all display a typical oscillatory zoning structure with HREErich chondrite-normalized REE patterns, suggesting a typical magmatic origin (Belousova et al., 2002). The fourteen concordant analyses yield a discordant line with an upper intercept at 1849 ± 17 Ma (Fig. 5a) and a weighted mean

207Pb/206Pb

age of 1854 ± 20 Ma (Fig. 5b), interpreted as crystallization age of Huijiazhuang granite. Zircons from the Xiyupi granite dyke (sample 15LL-16) are transparent, euhedral and prismatic morphology, with lengths and length / width ranging from 50 μm to 150

μm and 1:1 to 2:1, respectively (Fig. 4). They show oscillatory zonings. Twenty-five spot analyses are conducted on twenty-five zircons, of which eleven analyses give discordant age data due to later partial Pb-lose. Another fourteen analyses have high Th/U of 0.98-1.77 and chondrite-normalized REE patterns with HREE-rich, indicating a typical magmatic origin (Belousova et al., 2002). They yield an intercept age of 1826 ± 15 Ma (Fig. 5c) and a weighted mean 207Pb/206Pb age of 1830 ± 21 Ma (Fig. 5d), being considered as crystallization age of Xiyupi granite dyke. Zircons from the Dacaoping porphyritic granite (sample 12LL-87) are predominantly transparent, euhedral and prismatic morphology, with lengths and length / width ratios ranging from 200 to 300 μm and 3:2 to 3:1, respectively (Fig. 4). The CL images show week oscillatory zonings. Twenty-two spot analyses are conducted on twenty-two zircons, of which seven analyses give discordant age data due to later partial Pb-lose. Another fifteen analyses have high Th/U of 0.48-0.89 and chondrite-normalized REE patterns with HREE-rich, indicating a typical magmatic origin (Belousova et al., 2002). They yield an intercept age of 1792 ± 13 Ma (Fig. 5c), coincident with the weighted mean 207Pb/206Pb age of 1760 ± 20 Ma in error (Fig. 5d), interpreted as crystallization age of Dacaoping porphyritic granite. 4.2 Zircon Lu-Hf isotopic data The results of zircon Lu-Hf isotopes from 3 samples are listed in Table 2 and shown in Fig. 6a. The zircons from Huijiazhuang granite (sample 12LL-111) show variable initial 176Hf/177Hf

ratios of 0.281452 to 0.281692. Their age-corrected εHf(t) values range

from -5.5 to 2.3 (Fig. 6a), with TDM of 2169-2460 Ma and TCDM of 2360-2842 Ma, respectively. The zircons from Xiyupi granite dyke (sample 15LL-16) show variable initial 176Hf/177Hf

ratios from 0.281359 to 0.281577. Their age-corrected εHf(t) values range

between -3.1 and -9.6 (Fig. 6a), with TDM and TCDM ages ranging from 2310 Ma to 2592 Ma and from 2608 Ma to 3070 Ma, respectively. The zircons from Dacaoping porphyritic granite (sample 12LL-87) have relative homogeneous

176Hf/177Hf

ratios varying from 0.281450 to 0.281520. Their age-

corrected εHf(t) values range between -7.9 and -5.2 (Fig. 6a), with TDM of 2405-2509 Ma and TCDM of 2775-2938 Ma, respectively. 4.3 Whole-rock major and trace element The fresh rocks without deformation have low loss on ignition (LOI) values (mostly lower than 1 wt.%), suggesting that all the samples have rarely been affected by later metamorphism and alteration. Therefore, whole-rock geochemical analyses were carried out to better understand their rock types and magma sources. Major and trace element concentrations are listed in Table 3. 4.3.1 Huijiazhuang grantie The five samples from Huijiazhuang granite have variable SiO2 = 66.7174.31wt.%, FeOT = 1.35-3.98 wt.%, Na2O = 3.13-3.82 wt.%, K2O = 5.09-6.35 wt.%, but contain low MgO = 0.12-0.83 wt.%, Mg# = 14.61-30.42, CaO = 1.01-2.38 wt.%, TiO2 = 0.09-0.79 wt.% and P2O5 =0.02-0.16 wt.%. Their alkali is high with a narrow K2O+Na2O range of 8.56-9.48 wt.%, and high K2O/Na2O ratio of 1.41-2.03, mainly falling in the granite field in the K2O+Na2O vs. SiO2 diagram (Fig. 7a) and showing high potassium characteristics in the K2O vs. SiO2 diagram (Fig. 7b). They are metaluminous to weak peraluminous (Al2O3 = 13.92-15.31 wt.%, A/CNK = 0.921.08) (Fig. 7c) and are ferruginous (Fig. 7d). They show variable REE contents of 174.40-1245.44 ppm and strongly fractionated REE patterns ((La/Yb)N = 59.09-195.02, (Gd/Yb)N = 4.55-11.25), with medium negative Eu anomalies (δEu = 0.31-0.68) (Fig. 8a). In the primitive mantlenormalized spidergram, they are characterized by enrichment in large ion lithophile elements (LILE) such as Rb, Th, U, K, evidently positive Pb anomaly, and depletion in high field strength elements (HFSE), with relatively marked grooves in Ba, Nb, Ta, Sr, P, Ti (Fig. 8b). 4.3.2 Xiyupi granite dyke The four samples from the Xiyupi granite dyke have SiO2 = 70.78-71.42 wt.%, FeOT = 2.19-2.82 wt.%, Na2O = 3.07-3.38 wt.%, K2O = 5.33-5.61 wt.%, but contain low MgO = 0.34-0.40 wt.%, Mg# = 22.92-25.81, CaO = 0.95-1.36 wt.%, TiO2 = 0.190.35 wt.% and P2O5 = 0.06-0.07 wt.%. They are highly alkali with a narrow

K2O+Na2O range of 8.40-8.89 wt.%, and high K2O/Na2O ratio of 1.63-1.79, falling in granite field in the K2O+Na2O vs. SiO2 diagram (Fig. 7a) and showing high potassium characteristics in the K2O vs. SiO2 diagram (Fig. 7b). They are weak peraluminous (Al2O3 = 14.31-14.43 wt.%, A/CNK = 1.08-1.09) (Fig. 7c) and are ferruginous (Fig. 7d). They have REE contents of 358.97-503.59 ppm and strongly fractionated REE patterns ((La/Yb)N = 55.33-174.80, (Gd/Yb)N = 3.94-8.01), with medium negative Eu anomalies (δEu = 0.38-0.55) (Fig. 8c). They show enrichment in LILE such as Rb, Th, U, K, especially positive Pb anomaly, and depletion in HFSE, with relatively marked depletions of Nb, Ta, Sr, P, Ti (Fig. 8d). 4.3.3 Dacaoping porphyritic granite The four samples selected from the Dacaoping porphyritic granite show high SiO2 = 70.83-74.30 wt.%, FeOT = 1.92-2.85 wt.%, Na2O = 3.17-3.51 wt.%, K2O = 4.84-5.60 wt.%, MgO = 0.20-0.47 wt.%, Mg# = 17.33-25.69 and CaO = 0.67-1.48 wt.%, TiO2 = 0.15-0.33 wt.% and P2O5 =0.02-0.08 wt.%. These granites are alkalienriched (K2O+Na2O = 8.27-8.77 wt.%, K2O/Na2O = 1.43-1.77), plotting in the granite field in the K2O+Na2O vs. SiO2 diagram (Fig. 7a) and displaying high potassium characteristics (Fig. 7b). They display weak peraluminous features (Al2O3 = 13.26-14.71 wt.%, A/CNK = 1.04-1.10) (Fig. 7c), and exhibit ferruginous compositions (Fig. 7d). They show REE contents of 330.71-490.87 ppm and relative flat REE patterns ((La/Yb)N = 7.50-55.17, (Gd/Yb)N = 1.12-4.22), with significantly negative Eu anomalies (δEu = 0.16-0.35) (Fig. 8e). They display enrichment in Rb, Th, U, K, positive Pb anomaly, and depletion in Ba, Nb, Ta, Sr, P, Ti (Fig. 8f). 4.4 Whole-rock Sm-Nd isotope Whole-rock Sm-Nd isotope data for the late-Paleoproterozoic granites are listed in Table 4 and shown in Fig. 6b. The εNd(t) values are calculated according to DePaolo (1981) at the time of magma crystallization. The Huijiazhuang granites have 143Nd/144Nd ranging from 0.510843 to 0.511276. The age-corrected εNd(t) values vary from -4.1 to -5.7. Their TDM and TDM2 ages are

from 2381 Ma to 2570 Ma and from 2664 Ma to 2793 Ma, respectively (Fig. 6b). The Dacaoping porphyritic granites have

143Nd/144Nd

= 0.511288-0.511360,

εNd(t) = -6.1--6.4, TDM = 2690-2776 Ma and TDM2 = 2777-2797 Ma, respectively (Fig. 6b). 5. Discussion 5.1. Petrogenesis Generally, granitoids can be divided into I- and S- type granite in terms of their differences in petrography and geochemical composition (Chappell and White, 1974; Collins et al. 1982). The late-Paleoproterozoic granites in Lüliang Complex are metaluminous to weak peraluminous and show obvious P2O5 decreases with increasing SiO2 (Fig. 9a). No aluminium-rich minerals such as garnet or cordierite are observed and their CIPW normative corundum are low (0.4-1.2%), in contrast to strongly peraluminous S-type granite generated by partial melting of metapelitic protolith (Clemens, 2003), excluding S-type granitoid. Based on their geochemistry, two types of granitoids could be distinguished from late-Paleoproterozoic granites in the Lüliang Complex. Of which, the Huijiazhuang granite and Xiyupi granite dyke have variable SiO2, high K2O, alkali, highly fractionated REE patterns with medium negative Eu anomalies, enrichment in LILE (K, Rb, Sr, Ba), depletion in HFSE and HREE (Y, Yb), similar to those of high-K Itype granite. Whereas, the Dacaoping granites have “seagull-type” REE pattern with strong negative Eu anomaly and higher SiO2, Na2O+K2O, FeOT/MgO, Ga/Al, HFSE, lower CaO, Sr, Eu, being consistent with typical A-type granite (Loiselle and Wones, 1979; Whalen et al., 1987; Bonin, 2007). Moreover, the calculated zircon saturation temperatures (TZr) for Dacaoping porphyritic granite using the equation of Watson and Harrison (1983) are 790-845 °C, suggesting a relatively high temperature origin (Miller et al., 2003). Their higher 10000*Ga/Al (2.99-3.36) and Zr+Nb+Ce+Y (378583 ppm) also support that they belong to A-type granite (Fig. 10a, b). Eby (1992) identifies two sub-groups of A-type granite with different origins. The A1-type granite represents differentiates of magmas derived from OIB-like sources but emplaced in continental rifts or during intraplate magmatism, whereas the A2-type granite is

derived from melting of continental crust or underplated mafic crust that has been through a cycle of continent-continent collision or island-arc magmatism (Eby, 1992). The Dacaoping porphyritic granites yield A2-type granites except minor cross the boundary of A2- and A1-types (Fig. 10c, d). This is confirmed by their low Nb/Ta (7.66-12.19, averaging 9.39), consisting with continental crust (~11, Taylor and McLennan, 1985). 5.2 Magma sources As mentioned above, the Huijiazhuang granite and Xiyupi granite dyke belong to high-K I-type granite. The high-K I-type granitic magma is commonly thought to form via AFC process of basaltic magmas generated in enriched mantle wedges (Chappell, 1999), through the reaction of basaltic melts with metamorphic rocks of supracrustal origin, re-melting of older calc-alkaline rocks which themselves were the products of assimilation of meta-sediments by basaltic melts (Patiño Douce, 1999), derived only from the partial melting of moderately hydrous medium-to-high K basaltic compositions or hydrous calc-alkaline to high-K calc-alkaline mafic to intermediate metamorphic rocks in the crust (Roberts and Clemens, 1993; Sisson et al., 2005). The low Mg# (14.61-30.42) suggests that they are produced by partial melting of crustal rocks and no significant mantle-derived magmas are mixed into the crustal melts. Additionally, the low volume ratios of intermediate and acidic rocks in Lüliang area, absence of cumulate rocks and obvious partial melting trends on LaLa/Sm diagram (Fig. 9b) collectively suggest the significant role of partial melting instead of fractionated crystallization, excluding the AFC of basaltic magmas model. They have higher K character than experimental partial melts derived from various high-K calc-alkaline mafic to intermediate metamorphic rocks in the crust (Fig. 7b). In the CaO/(FeOT + MgO + TiO2) versus CaO + FeOT + MgO + TiO2 diagram, they plot in the field of partial melting of metamorphic greywackes and amphibolites (Fig. 9c; Patiño Douce, 1999), which both hint that the input of K from metamorphic rocks of supracrustal origin is needed. Single-stage Nd model ages (TDM) are typically used for revealing the age of the source rocks. The εNd(t) (-5.7 to -4.1) and TDM (2381 Ma to 2570 Ma) of Huijiazhuang granites suggest that the source rocks have ages similar to

those of the Neoarchean-Paleoproterozoic crustal materials. In addition, the zircon from Huijiazhuang granites and Xiyupi granite dykes have εHf(t) (-9.6 to 2.3) and TCDM ages ranging from 2360 Ma to 3070 Ma, which also support they are generated by partial melting of Neoarchean-Paleoproterozoic basement rocks that fractionated from depleted mantle between 2360 Ma to 3070 Ma. The highly fractionated REE patterns, medium negative Eu anomalies and Sr/Y imply that the source melting occurred at pressures between the garnet and plagioclase stability field, which show a negative correlation among samples on Sr/Y-Y diagram (Fig. 9d) and corresponding to a slightly thickened crust of 0.8-1.4 Gpa (Zhang et al., 2011). Obviously, elemental and isotope data suggest that the Huijazhuang granite and Xiyupi granite dyke with features of high-K I-type granitoids are most likely formed by partial melting of Neoarchean-Paleoproterozoic basement including both meta-sedimentary and metaigneous rocks in a slightly thickened lower crust. The Dacaoping porphyritic granite belongs to typical A-type granite. Generally speaking, two petrogenetic schemes have been proposed for the origin of A-type magmatism: (1) low degree melting of granulitic igneous sources previously depleted in hydrous felsic melt (Collins et al., 1982, Whalen et al., 1987); (2) partial melting of crustal igneous rocks of tonalitic to granodioritic composition (Creaser et al., 1991; Patiño Douce, 1997). For the former scheme, the Dacaoping A-type porphyritic granites have higher K2O (average 5.60 wt.%) and lower Zr/Hf (31.6) than the Gabo A-type granite suites with K2O (4.11 wt.%), Zr/Hf (42.0) in the Lachlan Fold Belt formed by the “residual-source modal” (Collins et al., 1982). Furthermore, the granulitic residue will be enriched in Al, Ca and depleted K, Si due to the melt extraction to form I-type granites. Therefore, low degree melting of granulitic igneous could not account for the low Al, Ca and high K, Si contents of A-type granites in principle, excluding from first genesis model (Creaser et al., 1991). Consequently, the second model is reasonable candidate and calc-alkaline intermediate basement are likely to be source material for the similar characteristics of Dacaoping A-type porphyritic granites (average K2O = 5.60 wt.%) to melt (such as average K2O = 5.50 wt.%) obtained from petrological experiments at 0.4-0.8 Gpa, which tonalitic to

granodioritic composition are the starting materials (Patiño Douce, 1997). The consistent negative εNd(t) (-6.1 to -6.4) with TDM (2690 Ma to 2776 Ma) from whole rock Sm-Nd isotope and εHf(t) (-7.9 to -5.2) with TCDM (2775-2938 Ma) from zircon Lu-Hf isotope hint that they are formed by partial melting of Neoarchean crustal materials that extracted from depleted mantle between 2775 Ma to 2938 Ma. The strong negative Eu anomaly, high Y content, low Sr and lower Sr/Y suggest that the residue of plagioclase and none garnet in their sources, in favor of the parting melting in a shallow level less than 8 kbar (Zhang et al., 2011). Therefore, the A-type Dacaoping porphyritic granite is formed by melting of Neoarchean calc-alkaline intermediate basement rocks in the thinned lower crust. 5.3 Tectonic setting and implications 5.3.1 Tectonic setting There are two possibilities for tectonic scenarios in which high-K I-type magmas may be generated: (1) in a continental arc setting similar to that of the Andes (Pitcher, 1987), (2) in a post-collisional setting similar to that of Caledonian, where melting of the source rocks is caused by decompression following crustal thickening (Pitcher, 1987). Within marginal-arcs, the rock type is represented by the voluminous, gabbroquartz

diorite-tonalite-granodiorite

association

with

tonalite

dominated,

compositionally the end-member of a less calcic, metaluminous and also mantlederived material involved. Certain discrete, high-K rock suites that sporadically accompany the more usual calc-alkaline granitoids for the primitive magmas are variously contaminated. The late-Paleoproterozoic high-K I-type Huijiazhuang granite and Xiyupi granite dyke share a common feature of massive in structure, suggesting that they are formed in a non-compressional tectonic setting and have not undergone any strong deformation or metamorphism. Furthermore, they are mainly crustal originated and show high K with enrichment of LILE, LREE and depletion of HFSE, especially the striking Nb, Ta anomalies, which are consistent with post-collision magmatic rocks produced in post-collisional setting (Bonin, 2004). Accordingly, in the Nb vs. Y (Fig. 11a) and Rb vs. Y+Nb diagram (Fig. 11b), the 1.85-1.83 Ga high-K I-type Huijiazhuang granite and Xiyupi granite dyke straddle the boundary between

syn-collision to post-collision field. In addition, the 1.76 Ga A2-type Dacaoping porphyritic granite without strong deformation plots in the boundary between postcollision to within-plate granite field, indicating a continental crust origin in the postcollisional setting. Consequently,, the transition from high-K I-type granitoids of Huijiazhuang and Xiyupi intrusions to A2-type granite of Dacaoping intrusion during late-Paleoproterozoic are representative of the post-collisional setting. 5.3.2. Protracted post-collision process Comprehensive geochronology investigations on aspects like metamorphism, magmatism, sedimentation and the structural details can provide framework to evaluate

continent-continent

collision.

Based

on

the

newly-reported

late-

Paleoproterozoic metamorphic ages, two peak metamorphic ages of ~1.95 and ~1.85 Ga are widely occurred in TNCO (Fig. 12a; Supplementary Table 1). Taking Lüliang Complex as an example, the EPMA Th-U-Pb monazite dating from gneisses suggested

that the major metamorphic event occurred during 1.89-1.85 Ga (Liu et al., 2006, 2007a; Trap et al., 2009). New zircon U-Pb dating on pelitic migmatite and mafic granulite had advanced the peak metamorphism to 1.95-1.92 Ga, much earlier than the previous major ~1.85 Ga event (Xiao et al., 2017; Zhao et al., 2017a). Combined with granulites in other areas of the TNCO, the older ~1.95 Ga metamorphism corresponds to the main collision by lines of evidence (e.g. mineral inclusions; REE patterns; the close age got in migmatite) and the younger ~1.85 Ga metamorphism is considered as a result of the uplifting and cooling of high-grade terranes during latePaleoproterozoic (Qian et al., 2013, 2015; Wei et al., 2014; Zhang et al., 2016; Wu et al., 2017; Xiao et al., 2017; Zhao et al., 2017a). The lack of metamorphic age less than ~1.82 Ga also suggested that no strong regional metamorphism resulted from compressional collision after that. In comparison, three igneous age groups of 1.971.90 Ga, 1.89-1.82 Ga, 1.82-1.76 Ga can be recognized (Fig. 12b; Supplementary Table 1). Some 1.97-1.90 Ga ages are obtained in S-type granite and gneissic syenogranite, which correspond to high-pressure granulite metamorphism and are formed during the syn-collision process (Huang et al., 2016; Liu et al., 2016b; Wang et al., 2016). While, the youngest detrital zircon age peaks of 1.82 Ga, 1.88 Ga, 1.84

Ga and 1.85 Ga place maximum depositional ages of the Heichashan group and upper parts of the Hutuo, Yejishan and Zhongtiao groups, consisting only of metaconglomerates and metasandstones, which were interpreted as a deposition of the foreland basin due to rapid exhumation/uplift and unroofing after crustal thickening, hinting that the syn-collision stage before ~1.88 Ga (Liu et al., 2012e and references cited therein). Therefore, all the evidences suggest that it has entered a post-collisional setting at ~1.89 Ga and may last to 1.76Ga. The late-Paleoproterozoic granitoids with ages of 1.89-1.76 Ga is widespread developed throughout TNCO and their geochemical composition changes obviously around 1.82 Ga. Before 1.82 Ga, the high-K granitoids were produced by partial melting of the slightly thickened lower crust during the early period of post-collision, represented by high-K I-type Huijiazhuang granite and Xiyupi granite dyke, Shizhuang granodiorite in the Lüliang Complex, anatexis pegmatite in the Pingshan region and K-feldspar granite in the Taihua Complex (Li et al., 2004; Geng et al., 2006; Zhao et al., 2008b; Wang et al., 2017). We proposed the early stage of high-K granitoids were most likely resulted from slab breakoff before 1.82 Ga, evidently supported by: (1) oceanic subduction zone revealed by previous magnetotelluric data and geochemical studies on Luyashan charnockite (Yang and Santosh , 2015; Yin et al., 2017), (2) the linear distribution of magmatism in thermal weakened crust straddling the TNCO initiated by rapid lateral migration of slab breakoff; (3) the ~1.94 Ga meta-mafic dykes to ~1.78 Ga mafic dykes geochemically resembling oceanic island basalt to within-plate basalts, and continuous intermediate-silicic magmatism related to an extensional setting due to partial melting of different source regions (including upwelling asthenospheric mantle, enriched lithospheric mantle and even overlying crust) according to petrological association diagnostic of slab breakoff (Wang et al., 2014a, 2014b); (4) the return of high-pressure rocks to the surface and short time interval between their uplift and the onset of magmatism (Geng et al., 2006; Liu et al., 2009; Xiao et al., 2017; Zhao et al., 2017a) and (5) no adakitic rock has been founded yet, distinguishing from intensive delamination of thickened lower crust in the southern Tibet (Chung et al., 2009). Therefore, the slab breakoff appears

to be the most probable driving force for the early stages of post-collisional magmatism. While after 1.82 Ga, numerous granites with A-type geochemical features were produced by the partial melting of the thinned lower crust, characterized by the gradually decrease of δEu and Sr/Yb (Fig. 13), such as the Dacaoping porphyritic granite, Tangershang massive granite, Tangershang massive granite, Yunzhongshan granite in the Lüliang Complex, Motianzhai granite, Guijiayu granite, Shangdian granite, Dengfeng granite, Shizuizi granite, Songshan granite in the southern segment of TNCO and pegmatite dike in the Huai’an Complex to the north of TNCO (Geng et al., 2006; Zhao et al., 2008b; Trap et al., 2009; Wan et al., 2009; Zhao and Zhou, 2009; Qu et al., 2012b; Gao et al., 2013; Zhang et al., 2013; Deng et al., 2016; Shi et al., 2017; Wang et al., 2017a). Hence, the evolutionary trend of latePaleoproterozoic high-K I- to A- type granites in the TNCO reveals that it is a protracted post-collision extensional regime during 1.89-1.76 Ga and the continental crust uplifted and thinned intensively after 1.82 Ga. Then the most robust evidence in the NCC for the Mesoproterozoic fragmentation of Columbia comes from the 1.6-1.2 Ga Zhaertai-Bayan Obo-Huade-Weichange rift zone along the northern margin of the craton (Zhao et al., 2003). 6. Conclusions Based on the field investigations, geochemical analyses of the latePaleoproterozoic granites in Lüliang Complex and combined with previous researches of magmatism and metamorphism in TNCO of NCC, the following conclusions are drawn: (1) The Huijiazhuang granite, Xiyupi granite dyke and Dacaoping porphyritic granite yield zircon U-Pb ages of 1854±20 Ma, 1830 ± 21 Ma, 1760±20 Ma, respectively, representative of an important granitic magmatism during late-Paleoproterozoic. (2) The Huijiazhuang granite and Xiyupi granite dyke have variable SiO2, high K2O, alkali, highly fractionated REE patterns with medium negative Eu anomalies, enrichment in LILE, depletion in HFSE, suggesting high-K I-type granite produced by partial melting of slightly thickened Neoarchean-Paleoproterozoic basement (including both meta-sedimentary and meta-igneous rocks). While the

Dacaoping porphyritic granites are characterized by high 10000*Ga/Al, Zr+Nb+Ce+Y and “seagull-type” REE pattern with strong negative Eu anomaly, being A2-type granite formed by partial melting of thinned Neoarchean calcalkaline intermediate basement. (3) The widespread 1.89-1.76 Ga I-type to A2-type granitoids in the TNCO suggest a post-collisional setting and the occurrence of numerous A2-type granites mark evidently crust thinning after 1.82 Ga. Acknowledgements This research was jointly supported by the Natural National Science Foundation of China (Grant: 41772189) National Key Basic Research Program of China (Grant: 2012CB416606) and MOST Special Funds from the State Key Laboratory of Continental Dynamics, Northwest University, Xi’an, China. We would like to thank two anonymous reviewers for their detailed and constructive comments. References Belousova, E., Griffin, W.L., O'Reilly, S.Y., Fisher, N.L., 2002. Igneous zircon: trace element composition as an indicator of source rock type. Contrib. Mineral. Petr. 143, 602-622. Blichert-Toft, J., Albarède, F., 1997. The Lu-Hf isotope geochemistry of chondrites and the evolution of the mantle-crust system. Earth Planet. Sc. Lett. 148, 243258. Bonin, B., 2004. Do coeval mafic and felsic magmas in post-collisional to withinplate regimes necessarily imply two contrasting, mantle and crustal, sources? A review. Lithos 78, 1-24. Bonin, B., 2007. A-type granites and related rocks: evolution of a concept, problems and prospects. Lithos 97, 1-29. Chappell, B.W. and White, A.J.R., 1974. Two contrasting granite types. Pac. Geol. 8， 173-174. Chappell, B.W., 1999. Aluminium saturation in I- and S-type granites and the characterization of fractionated haplogranites. Lithos 46, 535-551. Chen, B., Liu, S.W., Geng, Y.S., Liu, C.Q., 2006. Zircon U-Pb ages, Hf isotopes and

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Structural pattern of the Wutai Complex and its constraints on the tectonic framework of the Trans-North China Orogen. Precam. Res. 222-223, 212-229. Zhang, J., Zhao, G.C., Li, S.Z., Sun, M., Liu, S.W., Wilde, S.A., Kröner, A., Yin, C.Q., 2007. Deformation history of the Hengshan Complex: implications for the tectonic evolution of the Trans-North China Orogen. J. Struct. Geol. 29, 933-949. Zhang, J., Zhao, G.C., Li, S.Z., Sun, M., Liu, S.W., Yin, C.Q., 2009. Deformational history of the Fuping Complex and new U-Th-Pb geochronological constraints: implications for the tectonic evolution of the Trans-North China Orogen. J. Struct. Geol. 31, 177-193. Zhang, Q., Jin, W.J., Li, C.D., Wang, Y., Wang, Y.L., 2011. Granitic rocks and their formation depth in the crust. Geotect. Metal. 35, 259-269 (in Chinese with English abstract). Zhao, G.C., Cawood, P.A., Wilde, S.A., Sun, M., 2002a. A review of the global 2.11.8 Ga orogens: Implications for a pre-Rodinian supercontinent. Earth. Sci. Rev. 59, 125-162. Zhao, G.C., Wilde, S.A., Cawood, P.A., Sun, M., 2002b. SHRIMP U-Pb zircon ages of the Fuping Complex: implications for Late-Archean to Paleoproterozoic accretion and assembly of the North China Craton. Am. J. Sci. 302, 191-226. Zhao, G.C., Cawood, P.A., Li, S.Z., Wilde, S.A., Sun, M., Zhang, J., He, Y.H., Yin, C.Q., 2012. Amalgamation of the North China Craton: Key issues and discussion. Precam. Res. 222-223, 55-76. Zhao, G.C., Cawood, P.A., Wilde, S.A., Sun, M., Lu, L.Z., 2000. Metamorphism of basement rocks in the Central Zone of the North China Craton: implications for Paleoproterozoic tectonic evolution. Precam. Res. 103, 55-88. Zhao, G.C., He, Y., Sun, M., 2009. The Xiong'er volcanic belt at the southern margin of the North China Craton: Petrographic and geochemical evidence for its outboard position in the Paleo-Mesoproterozoic Columbia Supercontinent. Gondwana Res. 16,170-181. Zhao, G.C., Kröner, A., 2007. Geochemistry of Neoarchean (ca. 2.55-2.50 Ga) volcanic and ophiolitic rocks in the Wutaishan greenstone belt, central orogenic

belt, North China Craton: implications for geodynamic setting and continental growth: discussion. Geol. Soc. Amer. Bul. 199, 487-489. Zhao, G.C., Sun, M., Wilde S.A., Li, S.Z., 2003. Assembly, accretion and breakup of the Paleo-Mesoproterozoic Columbia Supercontinent: Records in the North China Craton. Gondwana Res. 6, 417-434. Zhao, G.C., Sun, M., Wilde, S.A., Li, S.Z., 2005. Late Archean to Paleoproterozoic evolution of the North China Craton: key issues revisited. Precam. Res. 136, 177202. Zhao, G.C., Wilde, S.A., Sun, M., Guo, J.H., Kroner, A., Li, S.Z., Li, X.P., Zhang, J., 2008a. SHRIMP U-Pb zircon geochronology of the Huai'an Complex: Constraints on Late Archean to Paleoproterozoic magmatic and metamorphic events in the Trans-North China Orogen. Am. J. Sci. 308, 270-303. Zhao, G.C., Wilde, S.A., Sun, M., Li, S.Z., Li, X.P., Zhang, J., 2008b. SHRIMP U-Pb zircon ages of granitoid rocks in the Lüliang Complex: Implications for the accretion and evolution of the Trans-North China Orogen. Precam. Res. 160, 213226. Zhao, G.C., Wilde, S.A., Guo, J.H., Cawood, P.A., Sun, M., Li, X.P., 2010. Single zircon grains record two Paleoproterozoic collisional events in the North China Craton. Precam. Res. 177, 266-276. Zhao, J., Gou, L.L., Zhang, C.L., Guo, A.L., Guo, X.J., Liu, X.Y., 2017a. P-T-t path and tectonic significance of pelitic migmatites from the Lüliang Complex in Xiyupi area of Trans-North China Orogen, North China Craton. Precam. Res. 303, 573-589. Zhao, J., Zhang, C.L., Guo, X.J., Liu, X.Y., Wang, Q., 2015. Determination of the 2.4Ga A-type granite in Lüliang area of the North China Craton and its geological significance. Acta Petrol. Sin. 31, 1606-1620 (in Chinese with English abstract). Zhao, J., Zhang, C.L., Liu, X.Y., Guo, X.J., 2017b. Protolith age and geochemical characteristics of meta⁃ basic volcanic rocks from Lüliang Group in the Lüliang complex and its tectonic setting. Chin. J. Geol. 52, 1220-1240 (in Chinese with English abstract).

Zhao, T.P., Chen, W., Zhou, M.F., 2009. Geochemical and Nd-Hf isotopic constraints on the origin of the ~1.74-Ga Damiao anorthosite complex, North China Craton. Lithos 113, 673-690. Zhao, T.P., Zhou, M.F., 2009. Geochemical constraints on the tectonic setting of Paleoproterozoic A-type granites in the southern margin of the North China Craton. J. Asian Earth Sci. 36, 183-195. Zhu, D.C., Wang, Q., Zhao, Z.D., Chung, S.L., Cawood, P.A., Niu, Y.L., Liu, S., Wu, F.Y., Mo, X.X., 2015. Magmatic record of India-Asia collision. Sci. Rep. 5, 14289. Figure captions Fig. 1. Tectonic subdivisions of the North China Craton (after Zhao et al., 2005). Abbreviations of metamorphic complexes: JN, Jining; DU, Daqingshan-Ulashan; HL, Helashan; CD, Chengde; NH, Northern Hebei; XH, Xuanhua; HA, Huai’an; HS, Hengshan; WT, Wutai; FP, Fuping; LL, Lüliang; ZT, Zhongtiao; DF, Dengfeng; TH, Taihua; TNCO, Trans-North China Orogen. Fig. 2. Geological sketch map of the Lüliang Complex (revised after Zhao et al., 2008b). Fig. 3. Photographs of the outcrops and photomicrographs of the latePaleoproterozoic granites in Lüliang Complex: (a) Huijiazhuang granite; (b) Xiyupi granite dyke; (c) Dacaoping porphyritic granite; (d) fine-grained and granitic texture; (e) medium-grained and granitic texture; (f) coarse-grained and porphyraceous structure. Fig. 4. Representative CL images of zircons from the late-Paleoproterozoic granites in Lüliang Complex. Fig. 5. Zircon U-Pb concordia and weighted average diagrams of the latePaleoproterozoic granites in Lüliang Complex. Fig. 6. (a) εHf(t) vs. zircon

207Pb/206Pb

age and (b) εNd(t) vs. zircon

207Pb/206Pb

age

diagram of the late-Paleoproterozoic granites in Lüliang Complex. The isotopic characteristics of granitoids in other complexes are from Liu et al. (2005), Chen et al. (2006), Zhao and Zhou. (2009), Yang and Santosh, (2015), Deng et al. (2016) and Shi

et al. (2017). Symbols in Fig. 6b as in Fig. 6a. Fig. 7. (a) K2O+Na2O vs. SiO2 (Middlemost, 1994); (b) K2O vs. SiO2 (Roberts and Clemens, 1993); (c) A/NK vs. A/CNK (Shand, 1927); (d) FeOT/( FeOT+MgO) vs. SiO2 diagram (Frost et al., 2001) of the late-Paleoproterozoic granites in Lüliang Complex. Symbols in Fig. 9, 10, 11, 13 as in Fig. 7. Fig. 8. Chondrite-normalized REE patterns and primitive mantle-normalized spidergrams of the late-Paleoproterozoic granites in Lüliang Complex. The primitive mantle and chondrite values are from Sun and McDonough (1989). Fig. 9. (a) P2O5 vs. SiO2; (b)La/Sm vs. La; (c) CaO/(FeOT+MgO+TiO2) vs. CaO+ FeOT+MgO+TiO2; (d) Sr/Y vs. Y diagram of the late-Paleoproterozoic granites in Lüliang Complex. Fig. 10. (a) FeOT/MgO vs. 10000*Ga/Al (Whalen et al., 1987); (b) (Na2O+K2O)/CaO vs. Zr+Nb+Ce+Y (Whalen et al., 1987); (c) Zr/4-Nb-Y (Eby, 1992); (d) 3*Ga-Nb-Y diagram (Eby, 1992) of the late-Paleoproterozoic granites in Lüliang Complex. Fig. 11 (a) Nb vs. Y (Pearce., 1984) and (b) Rb vs. Y+Nb (Pearce., 1984) diagram of the late-Paleoproterozoic granites in Lüliang Complex. Fig. 12. (a) Histogram of late-Paleoproterozoic metamorphic zircon U-Pb

207Pb/206Pb

ages and (b) histogram of late-Paleoproterozoic igneous zircon U-Pb 207Pb/206Pb ages in the TNCO. Fig. 13 (a) Sr/Yb vs.

207Pb/206Pb

age and (b) δEu vs. 207Pb/206Pb age diagram of the

late-Paleoproterozoic granitoids in TNCO. Black regular triangle and brown inverted triangle are the referenced data of late-Paleoproterozoic granitoids in TNCO before and after 1.82 Ga, respectively (Zhao and Zhou et al., 2009; Gao et al., 2013; Yang et al., 2015; Deng et al., 2016; Shi et al., 2017; Wang et al., 2017). Tables Table 1. LA-ICP-MS zircon U-Pb dating results of the late-Paleoproterozoic granites in Lüliang Complex. Table 2. Zircon in situ Lu-Hf isotope data of the late-Paleoproterozoic granites in Lüliang Complex. Table 3. Whole-rock major (wt.%) and trace (ppm) element concentrations of the late-

Paleoproterozoic granites in Lüliang Complex. Table 4. Whole-rock Sm-Nd isotope data of the late-Paleoproterozoic granites in Lüliang Complex. Supplementary Table 1. Summary of late-Paleoproterozoic igneous and metamorphic ages in the TNCO. Research Highlights:

The late-Paleoproterozoic granites in Lüliang Complex show a transition from high-K I-type to A-type granites. The 1.89-1.76 Ga granites were formed under a post-collisional setting. The occurrence of A2-type granites indicate a crustal thinning in the extensional setting after 1.82 Ga. Table 1. LA-ICP-MS zircon U-Pb dating results of the late-Paleoproterozoic granites in Lüliang Comple Spot No. 12LL-111 12LL-111-01 12LL-111-02 12LL-111-03 12LL-111-04 12LL-111-05 12LL-111-06 12LL-111-07 12LL-111-08 12LL-111-09 12LL-111-10 12LL-111-11 12LL-111-12 12LL-111-13 12LL-111-14 12LL-111-15 12LL-111-16 12LL-111-17 12LL-111-18 12LL-111-19 12LL-111-20 12LL-111-21 12LL-111-22 12LL-111-23 12LL-111-24 12LL-111-25

Contents (× 10-6) Th U

Th/U

395 963 53 188 242 799 424 109 511 41 1200 44 833 605 1694 61 602 83 628 227 1858 85 111 50 1005

0.57 1.66 0.07 0.24 1.17 1.38 0.96 0.25 1.11 0.05 1.47 0.07 1.33 1.43 1.98 0.08 1.31 0.16 0.41 0.92 1.86 0.15 0.28 0.06 1.43

688 579 797 798 206 581 439 429 460 805 815 634 628 422 854 775 458 515 1526 247 997 564 390 840 704

Ratios

Ages (Ma

207Pb/206Pb

1σ

207Pb/235U

1σ

206Pb/238U

1σ

207Pb/206Pb

0.1069 0.1095 0.1054 0.1110 0.1120 0.1150 0.1126 0.1123 0.1132 0.1114 0.1026 0.1119 0.1091 0.1055 0.1053 0.1104 0.1123 0.1133 0.1028 0.1136 0.1068 0.1145 0.1152 0.1155 0.1087

0.0022 0.0025 0.0022 0.0023 0.0025 0.0025 0.0024 0.0024 0.0025 0.0023 0.0022 0.0024 0.0023 0.0023 0.0022 0.0024 0.0025 0.0024 0.0022 0.0027 0.0023 0.0025 0.0025 0.0024 0.0025

4.0946 4.4450 3.8630 4.7022 5.2656 5.3334 4.8252 5.2846 5.2837 5.2628 3.1440 5.2536 4.3525 3.5885 3.4724 4.1705 5.2969 4.8533 2.5639 4.3091 3.0473 5.3273 5.3191 5.3643 3.5812

0.0516 0.0695 0.0496 0.0589 0.0774 0.0710 0.0633 0.0691 0.0735 0.0652 0.0420 0.0667 0.0567 0.0507 0.0450 0.0542 0.0778 0.0648 0.0326 0.0711 0.0417 0.0723 0.0744 0.0684 0.0547

0.2776 0.2941 0.2658 0.3071 0.3407 0.3363 0.3106 0.3412 0.3383 0.3425 0.2222 0.3403 0.2894 0.2467 0.2392 0.2741 0.3420 0.3108 0.1808 0.2751 0.2070 0.3375 0.3349 0.3368 0.2389

0.0032 0.0036 0.0030 0.0035 0.0041 0.0039 0.0036 0.0040 0.0040 0.0039 0.0026 0.0039 0.0034 0.0029 0.0028 0.0032 0.0041 0.0036 0.0021 0.0034 0.0024 0.0040 0.0040 0.0039 0.0029

1748 1792 1720 1816 1833 1880 1842 1837 1852 1823 1672 1831 1784 1723 1719 1805 1838 1852 1676 1858 1745 1872 1884 1888 1778

12LL-111-26 12LL-111-27 12LL-111-28 12LL-111-29 12LL-111-30 15LL-16 15LL-16-01 15LL-16-02 15LL-16-03

534 202 1539 955 702

457 454 907 602 418

1.17 0.44 1.70 1.58 1.68

0.1163 0.1130 0.1137 0.1109 0.1136

0.0025 0.0025 0.0026 0.0024 0.0025

5.3742 5.2937 5.3455 4.5748 4.7930

0.0744 0.0728 0.0831 0.0607 0.0665

0.3354 0.3398 0.3409 0.2992 0.3061

0.0040 0.0040 0.0042 0.0035 0.0036

1899 1848 1860 1815 1858

111 262 240

106 155 183

1.05 1.69 1.31

0.1083 0.1102 0.1141

0.0024 0.0025 0.0025

5.0764 5.0004 5.1013

0.0692 0.0731 0.0662

0.3400 0.3292 0.3243

0.0037 0.0036 0.0034

1771 1802 1865

15LL-16-04 15LL-16-05 15LL-16-06

217 190 980

141 131 744

1.54 1.45 1.32

0.1091 0.1129 0.1114

0.0026 0.0025 0.0023

5.0363 4.9665 4.5242

0.0805 0.0677 0.0475

0.3347 0.3191 0.2944

0.0038 0.0034 0.0029

1785 1846 1823

15LL-16-07 15LL-16-08 15LL-16-09 15LL-16-10 15LL-16-11 15LL-16-12 15LL-16-13 15LL-16-14 15LL-16-15 15LL-16-16 15LL-16-17 15LL-16-18 15LL-16-19 15LL-16-20 15LL-16-21 15LL-16-22 15LL-16-23 15LL-16-24 15LL-16-25 12LL-87

187 444 208 539 72 263 599 2816 268 166 596 463 76 524 374 407 526 285 229

140 311 678 467 81 237 569 2729 257 120 463 261 70 474 237 242 435 176 234

1.33 1.43 0.31 1.15 0.89 1.11 1.05 1.03 1.04 1.39 1.29 1.77 1.08 1.11 1.58 1.68 1.21 1.62 0.98

0.1109 0.1164 0.1060 0.1165 0.1138 0.1101 0.1068 0.1190 0.1136 0.1150 0.1127 0.1134 0.1116 0.1143 0.1119 0.1134 0.1270 0.1121 0.1137

0.0024 0.0025 0.0022 0.0027 0.0032 0.0023 0.0023 0.0024 0.0026 0.0027 0.0025 0.0025 0.0029 0.0026 0.0027 0.0026 0.0027 0.0027 0.0025

5.3012 4.8609 3.0622 3.6728 4.6380 5.0668 3.5100 2.5421 5.1047 4.9768 3.4886 4.7229 4.8732 3.4276 4.3282 4.3902 5.1674 5.0384 5.0086

0.0718 0.0620 0.0332 0.0547 0.1010 0.0606 0.0426 0.0256 0.0733 0.0786 0.0456 0.0609 0.0910 0.0471 0.0684 0.0640 0.0618 0.0809 0.0660

0.3466 0.3030 0.2094 0.2286 0.2956 0.3337 0.2384 0.1549 0.3257 0.3138 0.2245 0.3020 0.3166 0.2174 0.2805 0.2807 0.2950 0.3259 0.3195

0.0037 0.0032 0.0021 0.0025 0.0039 0.0034 0.0024 0.0015 0.0036 0.0036 0.0023 0.0032 0.0039 0.0023 0.0031 0.0030 0.0030 0.0037 0.0033

1815 1901 1732 1903 1861 1801 1745 1941 1858 1880 1843 1855 1826 1869 1830 1855 2057 1834 1859

12LL-87-01 12LL-87-02 12LL-87-03 12LL-87-04 12LL-87-05 12LL-87-06 12LL-87-07 12LL-87-08 12LL-87-09 12LL-87-10 12LL-87-11 12LL-87-12

261 296 835 201 450 184 504 205 158 367 768 707

400 419 703 416 503 296 607 340 208 557 795 839

0.65 0.71 1.19 0.48 0.89 0.62 0.83 0.60 0.76 0.66 0.97 0.84

0.1062 0.1057 0.1000 0.1090 0.1087 0.1074 0.1037 0.1078 0.1075 0.1059 0.1003 0.0976

0.0025 0.0022 0.0020 0.0023 0.0023 0.0023 0.0021 0.0023 0.0023 0.0022 0.0021 0.0020

4.6659 4.6892 3.4262 4.8148 4.7452 4.7625 3.9265 4.8085 4.8271 4.7470 3.2067 3.1574

0.0703 0.0467 0.0323 0.0532 0.0539 0.0556 0.0378 0.0521 0.0591 0.0462 0.0316 0.0307

0.3186 0.3217 0.2483 0.3205 0.3167 0.3216 0.2747 0.3235 0.3258 0.3252 0.2318 0.2346

0.0032 0.0028 0.0021 0.0029 0.0029 0.0029 0.0023 0.0029 0.0030 0.0028 0.0020 0.0020

1735 1726 1625 1783 1778 1755 1691 1763 1757 1730 1630 1579

12LL-87-13 12LL-87-14 12LL-87-15 12LL-87-16 12LL-87-17 12LL-87-18 12LL-87-19 12LL-87-20 12LL-87-21 12LL-87-22

169 485 260 261 457 115 187 313 217 335

298 842 440 422 834 138 241 380 445 407

0.57 0.58 0.59 0.62 0.55 0.83 0.78 0.82 0.49 0.82

0.1050 0.0998 0.1057 0.1089 0.0998 0.1099 0.1091 0.1073 0.1083 0.1085

0.0023 0.0021 0.0022 0.0023 0.0021 0.0025 0.0025 0.0023 0.0023 0.0023

4.0980 2.9943 4.7000 4.8167 3.3669 4.8486 4.8285 4.7594 4.7970 4.8363

0.0525 0.0306 0.0500 0.0485 0.0325 0.0692 0.0661 0.0503 0.0489 0.0524

0.2832 0.2177 0.3225 0.3210 0.2447 0.3202 0.3212 0.3219 0.3215 0.3234

0.0027 0.0019 0.0029 0.0028 0.0021 0.0032 0.0032 0.0029 0.0028 0.0029

1714 1620 1727 1780 1621 1797 1784 1754 1770 1774

Table 2. Zircon in situ Lu-Hf isotope data of the late-Paleoproterozoic granites in Lüliang Complex 176Yb/177Hf 2σ 176Lu/177Hf 2σ 176Hf/177Hf 2σ Spot No. εHf(t) TDM 12LL-111 12LL-111-04 12LL-111-05 12LL-111-06 12LL-111-08 12LL-111-09 12LL-111-10 12LL-111-12 12LL-111-17 12LL-111-22 12LL-111-23 12LL-111-24 12LL-111-26 12LL-111-27 12LL-111-28 15LL-16 15LL-16-01 15LL-16-02 15LL-16-03 15LL-16-04 15LL-16-05 15LL-16-06 15LL-16-07 15LL-16-12 15LL-16-15 15LL-16-16 15LL-16-18 15LL-16-19 15LL-16-24 15LL-16-25 12LL-87

0.007208 0.001922 0.005147 0.002229 0.039454 0.008960 0.002158 0.018601 0.002485 0.005040 0.005439 0.019972 0.022141 0.007498

0.000093 0.000013 0.000021 0.000014 0.000140 0.000160 0.000034 0.000079 0.000010 0.000051 0.000075 0.000336 0.000111 0.000019

0.000245 0.000083 0.000191 0.000104 0.001187 0.000283 0.000090 0.000601 0.000102 0.000165 0.000182 0.000601 0.000653 0.000232

0.000002 0.000001 0.000001 0.000001 0.000004 0.000005 0.000002 0.000004 0.000001 0.000001 0.000003 0.000010 0.000003 0.000001

0.281495 0.281511 0.281489 0.281532 0.281677 0.281590 0.281558 0.281642 0.281452 0.281503 0.281552 0.281644 0.281692 0.281541

0.000016 0.000017 0.000042 0.000015 0.000016 0.000015 0.000014 0.000016 0.000018 0.000016 0.000017 0.000023 0.000020 0.000014

-4.2 -3.4 -4.4 -2.7 1.1 -0.9 -1.8 0.6 -5.5 -3.8 -2.1 0.6 2.3 -2.6

2411 2380 2417 2353 2219 2286 2317 2233 2460 2396 2331 2231 2169 2349

0.006398 0.005727 0.006651 0.007731 0.007887 0.027769 0.008180 0.011664 0.010893 0.008166 0.012917 0.004686 0.009770 0.019821

0.000042 0.000027 0.000050 0.000054 0.000064 0.000142 0.000064 0.000012 0.000057 0.000036 0.000056 0.000027 0.000069 0.000114

0.000233 0.000209 0.000230 0.000277 0.000287 0.000996 0.000277 0.000412 0.000385 0.000316 0.000456 0.000169 0.000345 0.000706

0.000002 0.000001 0.000002 0.000002 0.000002 0.000005 0.000002 0.000000 0.000002 0.000002 0.000002 0.000001 0.000002 0.000004

0.281359 0.281391 0.281498 0.281469 0.281502 0.281421 0.281479 0.281550 0.281577 0.281459 0.281468 0.281401 0.281472 0.281489

0.000013 0.000011 0.000013 0.000014 0.000012 0.000016 0.000012 0.000013 0.000018 0.000010 0.000012 0.000011 0.000010 0.000013

-9.6 -8.4 -4.7 -5.8 -4.6 -8.4 -5.4 -3.1 -2.1 -6.2 -6.0 -8.0 -5.8 -5.6

2592 2548 2407 2448 2404 2560 2435 2347 2310 2464 2460 2532 2449 2448

12LL-87-01 0.018167 0.000281 0.000691 0.000007 0.281520 0.000013 -5.2 2405 12LL-87-02 0.019599 0.000178 0.000718 0.000007 0.281499 0.000011 -6.0 2436 12LL-87-04 0.032859 0.000377 0.001249 0.000014 0.281534 0.000013 -5.4 2421 12LL-87-05 0.021994 0.001201 0.000805 0.000040 0.281495 0.000011 -6.2 2446 12LL-87-06 0.018671 0.000259 0.000706 0.000007 0.281476 0.000013 -6.8 2466 12LL-87-08 0.032832 0.000425 0.001198 0.000011 0.281485 0.000015 -7.1 2485 12LL-87-09 0.016312 0.000169 0.000608 0.000008 0.281472 0.000011 -6.8 2465 12LL-87-10 0.022161 0.000376 0.000827 0.000008 0.281450 0.000012 -7.9 2509 12LL-87-15 0.017329 0.000079 0.000671 0.000003 0.281485 0.000010 -6.4 2451 12LL-87-16 0.017648 0.000113 0.000663 0.000002 0.281490 0.000012 -6.3 2444 12LL-87-18 0.011041 0.000276 0.000430 0.000009 0.281490 0.000012 -6.0 2429 12LL-87-19 0.023321 0.000837 0.000828 0.000023 0.281464 0.000011 -7.4 2490 12LL-87-20 0.020747 0.000322 0.000793 0.000013 0.281465 0.000016 -7.3 2487 12LL-87-21 0.015171 0.000214 0.000583 0.000005 0.281475 0.000011 -6.7 2460 12LL-87-22 0.017272 0.000755 0.000652 0.000026 0.281494 0.000013 -6.1 2438 Table 3. Whole-rock major (wt.%) and trace (ppm) element concentrations of the latePaleoproterozoic granites in Lüliang Complex Huijiazhuang granite Rock Xiyupi granite dyke 12LL- 12LL12LL- 12LL- 12LL15LL 15LL15LL15LLNo. 106 107 108 110 111 -16 16a 16b 16c SiO2

70.64

74.31

72.85

72.32

66.71

70.78 71.42

71.38

71.08

TiO2

0.22

0.09

0.12

0.15

0.79

0.35

0.19

0.2

Al2O3

15.31

13.92

14.69

14.21

14.9

14.43 14.31

14.37

14.33

FeOT FeO MnO MgO CaO

2.37 2.01 0.04 0.29 1.12

1.47 1.25 0.02 0.12 1.01

1.35 1.15 0.02 0.18 1.15

1.8 1.53 0.03 0.19 1.19

3.98 3.38 0.04 0.83 2.38

2.82 2.54 0.04 0.4 1.36

2.19 1.97 0.04 0.34 0.95

2.38 2.14 0.04 0.37 0.97

2.29 2.06 0.02 0.38 1.17

Na2O

3.82

3.47

3.13

3.26

3.61

3.07

3.38

3.22

3.12

K2O

5.4

5.09

6.35

5.75

5.44

5.33

5.51

5.61

5.59

P2O5 LOI Total σ A/CNK ANK

0.05 0.96 100.22 3.08 1.08 1.26

0.02 0.71 100.23 2.34 1.07 1.24

0.03 0.15 100.02 3.01 1.04 1.22

0.03 0.62 99.55 2.77 1.03 1.23

0.16 1.03 99.87 3.45 0.92 1.26

0.07 0.93 99.58 2.54 1.09 1.33

0.06 1.17 99.57 2.78 1.08 1.24

Mg# Sc V Cr Co Ni

20.41 4.18 8.73 4.16 136 2

14.61 2.11 1.79 4.09 196 2.19

21.84 1.68 4.31 2.63 124 1.4

18.12 2.36 4.22 4.92 187 2.27

30.42 4.62 30.3 7.7 125 5.46

22.92 3.06 15.6 3.83 52.6 3.38

24.55 3.1 10.2 3.33 51.5 3.04

0.06 1.13 99.72 2.75 1.09 1.26 25.5 3.15 10.9 10.7 44.7 7.55

0.06 1.27 99.51 2.7 1.08 1.28 26.75 3.35 10.8 3.49 52.1 4.16

0.2

Cu Zn Ga Ge Rb Sr Ba Y Zr Nb Cs La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Hf Ta Pb Th U Nb/Ta (La/Yb)N (Gd/Yb)N

δEu

2.4 34.9 25.4 1.27 377 156 685 21.1 236 26.9 2.21 137 225 25 79.2 11.2 1.06 8.95 1.03 4.77 0.74 1.86 0.22 1.35 0.2 6.36 1.32 44.3 66.5 3.67 20.38 68.18 5.33 0.31

0.83 23.1 20.6 0.93 261 86.5 313 6.94 132 9.52 1.48 45.2 79.2 8.58 28.9 4.9 0.57 3.59 0.39 1.7 0.25 0.63 0.08 0.52 0.08 4.32 0.46 42.5 47.6 6.56 20.74 59.09 5.62 0.4

0.89 24.1 20.7 0.98 306 137 780 6.76 118 9.81 1.96 50.2 87.9 8.78 28.7 4.54 0.77 3.46 0.37 1.61 0.24 0.62 0.08 0.5 0.08 3.39 0.71 38.9 50.6 3.78 13.83 67.31 5.56 0.58

1.85 30.7 21.9 1.11 305 172 689 12.1 171 14.5 2.18 76.4 133 13.1 41.5 6.03 0.81 4.68 0.53 2.58 0.42 1.08 0.14 0.83 0.13 5.07 0.61 36 52.2 4.65 23.97 62.09 4.55 0.45

20.6 56.3 28.2 1.51 253 1082 3574 18.1 715 17.6 1.21 363 599 59 177 19.4 3.84 14.2 1.15 4.61 0.59 1.65 0.18 1.02 0.14 14.5 1.01 39.7 81.2 9.12 17.42 195.02 11.25 0.68

3.74 35.8 27.4 1.09 242 249 1232 8.13 356 14.5 1.9 156 280 28.1 81.2 8.78 1.38 5.98 0.47 1.99 0.29 0.8 0.1 0.6 0.09 9.19 0.63 43 84.9 4.07 22.95 174.8 8.01 0.55

6.3 29.9 17.7 0.98 190 169 978 11.6 252 16.5 0.81 89.6 174 18 57.8 7.78 0.93 5.33 0.52 2.42 0.4 1.15 0.16 1.09 0.18 6.9 1.13 31.9 76.8 7.1 14.62 55.33 3.94 0.42

4.25 33.2 18.8 1.05 193 187 970 11.7 270 16.5 0.98 107 203 21.5 67 8.75 0.96 6.11 0.57 2.59 0.41 1.18 0.16 1.07 0.18 7.35 0.97 34.9 82.2 7.46 16.92 67.29 4.59 0.38

Mg#=100*(MgO/40.3)/(MgO/40.3+ FeOT*0.85/71.8) Table 4. Whole-rock Sm-Nd isotope data of the late-Paleoproterozoic granites in

Lüliang Complex No. 12LL106 12LL107

Sm(ppm )

Nd(ppm )

147Sm/144N

143Nd/144N

d

d

11.2

79.2

0.0856

0.511000

4.90

28.9

0.1023

0.511276

2σ 0.00000 5 0.00000 7

εNd(t ) -5.7 -4.3

TDM

TDM2

256 0 257 0

279 3 268 1

3.16 22.5 20.3 1.08 220 182 889 12.5 253 16.8 1.2 98.7 185 19 60.4 7.97 0.98 5.68 0.55 2.6 0.43 1.19 0.17 1.08 0.17 6.88 1.35 41.5 78 6.96 12.43 61.48 4.23 0.42

12LL111

19.4

177

0.0661

0.510843

12LL-87

10.2

53.8

0.1079

0.511360

12LL-88

10.4

58.0

0.1151

0.511288

0.00000 6 0.00000 5 0.00000 5

-4.1 -6.4 -6.1

238 1 277 6 269 0

266 4 279 7 277 7