Gondwana Research 31 (2016) 96–123

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Gondwana Research

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Microblock amalgamation in the North China Craton: Evidence from Neoarchaean magmatic suite in the western margin of the Jiaoliao Block

Qiong-Yan Yang a,b,M.Santosha,b,c,⁎,AlanS.Collinsb, Xue-Ming Teng a a School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China b Department of Earth Sciences, University of Adelaide, SA 5005, Australia c Faculty of Science, Kochi University, Akebono-cho 2-5-1, Kochi 780-8520, Japan article info abstract

Article history: The Archaean Earth is considered to have been characterized by microcontinents that formed, dominantly, Received 22 February 2015 through the accretion of oceanic arcs and plateaus. The North China Craton (NCC) provides a typical case Received in revised form 17 April 2015 where at least seven ancient microcontinental nuclei with distinct lithological features and independent tectonic Accepted 19 April 2015 histories were amalgamated into the cratonic framework at the end of the Archaean. Here we investigate a suite Available online 24 April 2015 of magmatic rocks developed at the periphery of one of these microblocks, the Jiaoliao Block that forms part of the – Handling Editor: S. Kwon composite Eastern Block of the NCC. We present petrological, geochemical and zircon U Pb geochronological data from the Taipingzhai charnockite suite, and associated amphibolites, metagabbros and orthogneisses from – Keywords: the Qianxi Complex. Geochemically the rocks show a wide range of SiO2 (charnockite suite: 52.57 75.50 wt.%; Geochemistry metagabbro: 43.71 wt.%; amphibolite: 50.24 wt.%; garnet-bearing biotite: 63.73 wt.%), and MgO (charnockite Zircon U–Pb geochronology suite: 0.89–5.01 wt.%; metagabbro: 3.99 wt.%; amphibolite: 6.23 wt.%; garnet-bearing biotite: 2.08 wt.%). The Tectonics composition of the felsic units straddle from diorite through syeno-diorite to granite with both alkalic and Micro-block amalgamation subalkalic affinity, with dominantly magnesian composition and arc-related features. Their immobile trace ele- North China Craton ment relationships suggest calc-alkaline affinity. They show positive Pb, Ba, La, Nd, and Gd and negative Nb, Ta, Sr, Th and Ti anomalies with slightly negative anomalies of Ce and Y, attesting to arc-related features. In tectonic classification diagrams, the rocks plot in the VAG + syn-COLG field or the VAG area suggesting subduction- related origin. The dominant population of zircons in all these rocks displays magmatic crystallization features including high Th/U values with core-rims textures indicating subsequent thermal events. The zircon U–Pb data yield upper intercept ages of 2587 ± 10 Ma to 2543 ± 17 Ma and 207Pb/206Pb mean ages of 2578 ± 7.3 Ma to 2536 ± 8 Ma for the charnockite suite, marking the timing of emplacement of the arc magmas. The overgrowth rims as well as discrete neoformed grains are interpreted as dating subsequent metamorphism and yield 207Pb/206Pb ages between 2533 Ma to 2490 Ma. Zircons in the metagabbro preserve upper intercept ages of 2556 ± 20 Ma representing the crystallization age of this rock. The younger ages of 2449 ± 58 Ma (upper inter- cept age) and 1845 ± 25 Ma (207Pb/206Pb spot age) are interpreted to represent subsequent multiple thermal events in this area. Zircons in the amphibolite preserve the 207Pb/206Pb mean age of 2539 ± 9 Ma, representing the crystallization age of this rock. The garnet-bearing biotite gneiss shows an upper intercept age of 2562 ± 10 Ma (MSWD = 0.66; N = 36) and the 207Pb/206Pb mean age of 2561 ± 9 Ma (MSWD = 0.63; N = 33) which is taken to represent the crystallization age of this rock. Some inherited zircons are also identified with 207Pb/206Pb ages of 2664 ± 26 Ma and 2628 ± 26 Ma. Zircon Lu–Hf data show dominantly positive εHf(t) values and combined with crustal residence ages, the results suggest Mesoarchean to Neoarchean juvenile crust formation in the NCC. We interpret the data presented here to represent a phase of major late Neoarchaean arc magmatism along the western margin of the Jiaoliao Block related to the birth of microcontinental nuclei within the NCC. Our data suggest that the Western and Eastern Blocks might not have existed as discrete crustal blocks, and that the construction of the NCC is a result of the assembly of several microblocks or terranes at the end of Archaean. Similar Archean cratonic nuclei in other regions of the world might have formed part of a primitive supercontinent in the early Earth. © 2015 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

⁎ Corresponding author at: School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China. E-mail address: [email protected] (M. Santosh).

http://dx.doi.org/10.1016/j.gr.2015.04.002 1342-937X/© 2015 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved. Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 97

1. Introduction Cawood, 2012; Zhai, 2014). In addition, various models have been proposed for its Archaean formation from being dominated by plume- The early Earth was characterized by double-layered mantle convec- derived melting (Wilde et al., 2002; Zhai and Santosh, 2011; Zhao and tion with the formation of protocontinental nuclei through both Zhai, 2013) to originating as amalgamated volcanic arcs (Wu et al., magmatic differentiation and remelting of magmatic protoliths (Wood 1998; Martin, 1999; Condie, 2005; Martin et al., 2005; Zhai et al., et al., 1970; Hostetler and Drake, 1980; Zhai and Santosh, 2011; 2005; Li et al., 2010; Zhai and Santosh, 2011; Wang et al., 2012, 2013; Tsuchiya et al., 2013). Although contrasting models have been proposed Zhai, 2014). for the growth and destruction of continental crust through time In this study, we present geochemical and geochronological data (e.g., Rino et al., 2008; Condie et al., 2009; Stern, 2011; Roberts, 2012; from one of the key terrane-bounding regions of the NCC (the Qianxi Spencer et al., 2014), geochronological and isotopic data from various Complex, located in the eastern Hebei Province). We interpret these regions on the globe suggest substantial growth of continental data to support the amalgamation of this region during extensive late crust during 3.5–3.2 Ga and 2.8–2.7 Ga (Hawkesworth and Kemp, Neoarchaean arc magmatism. 2006), resulting in the production of voluminous TTGs (tonalite– trondhjemite–granodiorite) and volcanic rocks (Zhao, 1993; Windley, 2. Geological setting 1995; Goodwin, 1996; Santosh et al., 2010; Polat and Santosh, 2013 and references therein; Zhai and Santosh, 2011). Most of the major 2.1. Tectonic framework of the North China Craton cratons on our planet stabilized by Late Neoarchaean, with only few examples in Paleoproterozoic (ca. 2.0–1.9 Ga) (Rogers and Santosh, The North China Craton (NCC, Fig. 1), considered to be composed of 2003; Zhai and Santosh, 2011, and references therein). Zircon age data the Western and Eastern Blocks in many popular models (e.g., Zhao on early Precambrian magmatic suites around the world also suggest et al., 2005; Santosh, 2010; Zhao and Zhai, 2013), is in fact a collage of voluminous crustal growth around 2.8–2.7 Ga (e.g., Condie et al., several ancient cratonic nuclei, preserving orthogneisses, metavolcanics 2009, and references therein). Since the majority of these rocks are felsic and metamorphosed sedimentary units that date back to the Eoarchaean orthogneisses characterized by high Na content, along with subordinate (Santosh, 2010; Zhao and Cawood, 2012; Zhai, 2014). Zircon U–Pb isoto- volumes of mafic–ultramafic volcanic rocks, mantle plume or super- pic ages of ca. 3.8 Ga have been reported from near Tiejiashan, northeast plume has been invoked by some authors as one of the triggers for the China and near Caozhuang, eastern Hebei (see Zhai and Santosh, 2011 crustal accretion event (e.g., Condie et al., 2001; Condie and Kröner, for a recent review; Liu et al., 1992), demonstrating the antiquity of 2008; Condie et al., 2009). It has also been proposed that the Archaean these cratonic cores. The next major crust building event in the NCC oc- continental crust was built largely through accretion of oceanic arcs curred at ca. 2.7 Ga, which is contemporaneous with a major global and plateaus whereas continental arcs dominated as the building blocks crust-formation event (Condie, 2005; Hawkesworth et al., 2010). In the in the younger Earth (Condie and Kröner, 2013). NCC, rocks of this age make up the core of at least seven granitoid The North China Craton (NCC) is an excellent place to address some terranes (micro-blocks) such as the Jiaoliao Block (JL), the Qianhuai of these controversies due to its good exposure, accessibility, and range Block (QH), the Ordos Block (OR), the Jining Block (JN), the Xuchang of magmatic and metasedimentary rock systems that date from Block (XCH), the Xuhuai Block (XH) and the Alashan Block (ALS) (Shen the Eoarchaean to the Palaeoproterozoic (Santosh, 2010; Zhao and and Qian, 1995; Bai et al., 1996; Wu et al., 1998; Zhai and Bian, 2001;

Fig. 1. Tectonic framework of the North China Craton showing the major crustal blocks and intervening suture zones (after Zhao et al., 2005; Santosh, 2010). The location of Qianxi Complex is shown by box. 98 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Zhai and Santosh, 2011, and references therein). These ancient tectonic crust–mantle differentiation and crust formation in the NCC. The wide- blocks are bound by granite–greenstone belts that may indicate the spread occurrence of ca. 2.5 Ga rocks in the NCC, but their absence in Hf site of closure of intervening ocean basins (Zhai and Santosh, 2011). Ex- model ages is interpreted to indicate partial melting and extensive amples include the Zunhua greenstone belt located between the JN and crustal reworking at ca. 2.5 Ga. QH Blocks, the Wutaishan greenstone belt between the OR and QH The terrane model of the NCC that we emphasize in this work is in Blocks, the Yanlingguan greenstone belt between the JL and QH Blocks, contrast to the prevailing view over the last decade, where two main the Dongwufenzi greenstone belt between the JN and OR Blocks, the blocks (the Eastern Block and the Western Block) have been thought Xuchang greenstone belt between the XCH and QH Blocks, among others to have collided along the Trans North China Orogen (Zhao et al., (Zhai and Santosh, 2011). The identification of these micro-blocks is also 2005). Subsequent research has revealed two more, broadly linear tec- supported by geochemical variations (Liu et al., 1998), as well as tonic belts, which have been interpreted as suture zones: the Inner geophysical boundaries imaged from the deep crust (Guan et al., 1987). Mongolian Suture Zone and the Jiao-Liao-Ji Belt (Zhai, 2004a,b; Zhai The lithological associations and crustal evolution history within the and Peng, 2007; Santosh, 2010; Zhao and Zhai, 2013). All the three seven NCC terranes are distinct (Zhai and Santosh, 2011; Zhai, 2014,and belts display lithotectonic elements that are diagnostic of subduction references therein). Thus, the QH and JL Blocks contain remnants of ca. and collision tectonics such as: (1) arc-related juvenile crust; (2) linear 3.8 Ga orthogneisses and BIF-bearing supracrustal rocks, with different structural belts defined by strike–slip ductile shear zones, large-scale metamorphic histories. The Archaean rocks in the JL Block experienced thrusting and folding, and sheath folds and mineral lineations; two phases of metamorphism; a granulite to upper amphibolite facies (3) high-pressure (HP) mafic and pelitic granulites, retrograde eclogites event at ca. 2.51–2.52 Ga and an upper to lower amphibolite facies and ultrahigh temperature (UHT) rocks; (4) clockwise metamorphic event at ca. 1.82–1.9 Ga (Zhai, 2014 and references therein). In contrast, P–T paths involving near-isothermal decompression; (5) possible the Archaean rocks of the QH Block experienced three stages of ancient oceanic fragments and mélange; and (6) back-arc or foreland metamorphism: a granulite facies event at ca. 2.56–2.6 Ga, granulite to basins (Zhao and Zhai, 2013). But the age of these belts is still disputed, upper amphibolite facies at ca. 2.51–2.52 Ga and an upper to lower with some suggesting that were amalgamated at the end of the amphibolite facies at ca. 1.82–1.9 Ga (Zhai and Santosh, 2011). The JN Archaean (e.g., Zhai, 2014), while others point out that the protolith Block is characterized by Neoarchaean metamorphic basement, which age and metamorphic history are more consistent with amalgamation is covered by a carbonate–evaporite sequence and Al-rich sedimentary in the late Palaeoproterozoic (Santosh, 2010; Zhao and Cawood, 2012; rocks. The XCH Block is composed of ca. 2.7 Ga and ca. 2.5–2.6 Ga Wilde, 2014). basement complexes. The ca. 2.7 Ga rocks are represented by TTG gneisses of granulite to upper amphibolite facies and the ca. 2.2. Geology of the study area 2.5–2.6 Ga rocks consist of BIF-bearing supracrustal rocks and amphibolite-facies orthogneisses. Orthogneisses and metasedimentary The area studied here lies to the east of the Trans-North China rocks are the major rock types in the ALS Block, and are preserved to- Orogen (Fig. 1), within the Jiaoliao Block, that is sandwiched between gether with a supracrustal sequence composed of metabasic rocks and the Trans-North China Orogen to its west and the Jiao-Liao-Ji Belt to metamorphosed intermediate to acid volcanic rocks. BIFs are not well the east—a region also known as the Longgang Block (Zhao and developed in the ALS Block. Most of the OR and XH Blocks are covered Cawood, 2012) and the Yanliao Block (Santosh, 2010). Controversy by younger sedimentary rocks and Quaternary cover sediments. has surrounded the petrogenesis and tectonic setting of Neoarchaean Neoarchaean orthogneisses and granulites have been reported from rocks in this region, with one school of thought noting the short time some drill cores in these terranes (Zhai, 2014 and references therein). span between the widely developed TTG rocks and mafic volcanics of The lithologic associations and geochemical characters of the green- continental tholeiite affinity, the anticlockwise P/T paths, the presence stone belts and related granitoids that separate the terranes in the NCC of komatiites and bimodal volcanic assemblages and the diapiric struc- suggest that most of the greenstone belts were formed in an island arc tural style to prefer a mantle plume model (Wilde et al., 2002; Zhai and or a back-arc basin setting (Zhai and Santosh, 2011). Kusky et al. Santosh, 2011; Zhao and Zhai, 2013). In contrast, many workers are (2001, 2004) and Li et al. (2002) reported dismembered ophiolitic persuaded by the geochemical similarities of the TTG gneisses with remnants in the Zunhua (Dongwanzi) greenstone belt (between the calc-alkaline magmas in modern continental margin arcs to envisage JN and QH blocks). The Zunhua greenstone belt (Zunhua unit), and a a similar supra-subduction origin for these rocks (Wu et al., 1998; related granulite complex occurring to the south (Taipingzhai unit), Martin, 1999; Martin et al., 2005; Zhai et al., 2005; Li et al., 2010; Zhai are considered to represent a unified Neoarchaean island arc terrane, and Santosh, 2011; Wang et al., 2012, 2013; Zhai, 2014). with the greenstones representing the upper domain and the granulite The study area in the eastern Hebei region incorporates three complex representing the root zone (Zhai and Bian, 2001). Zhai (2004a,b) complexes: the Eo- to Paleoarchaean Caozhuang Complex, the inferred that the Zunhua greenstone belt and late Archaean granites in Mesoarchaean Shuichang (Qianxi) Complex, and the Neoarchaean east Hebei (Geng et al., 2006; Yang et al., 2008) mark the boundary Zunhua Complex. Previous studies have suggested that the rocks of between the QH Block and the JN Block and were amalgamated during the eastern Hebei province may be distinctly older than elsewhere in an arc–continent collision. Some workers consider that the Mengyin the NCC, based on the intensity of deformation and metamorphism greenstone belt and Wutaishan greenstone belt and related granitoids (Huang et al., 1986), although some of the recent geochronological represent the boundary between the JL Block and QH Blocks and studies have revealed multiple ages (Geng et al., 2006; Nutman et al., between the ER and QH Blocks where subduction and collision occurred 2011; Lv et al., 2012). These complexes are composed of banded iron (Wu et al., 1998; Liu et al., 2004; Chen et al., 2006; Liu et al., 2006; Wang, formation (BIF)-bearing supracrustal rocks and TTG gneisses, with 2009). All the micro-blocks in the NCC were welded by greenstone belts minor gabbroic and dioritic sills or plutons, together with younger during the latest Neoarchaean (Zhai and Santosh, 2011; Zhao and Zhai, granitic sheets. The dome-shaped Shuichang Complex and the sill-like 2013; Zhai, 2014). Zunhua Complex share similar isotopic age and geochemical features Geng et al. (2012) traced the Archaean–Palaeoproterozoic history of and are therefore considered to be comagmatic. They have been corre- the eastern and central parts of the NCC by synthesizing more than 2600 lated to Archaean island-arc setting where the Shuichang Complex is Lu–Hf isotopic zircon data. Their results show Hf model peaks at considered to be equivalent to the root of an island arc and the Zunhua 3902 ± 13 Ma and 3978 ± 18 Ma, respectively. Juvenile protoliths Complex representing the upper crust (Li, 1999). and crust–mantle differentiation at 4.0–3.9 Ga are suggested by the The Qianxi Complex (also known as Qian'an Complex or traditional positive εHf(t) values of many of the zircons. A prominent peak at ca. the Qianxi Group), from where our samples were collected, contains 2.7 Ga with dominantly positive zircon εHf(t) values is taken to mark rocks that date back to the Eoarchaean, which makes the area ideal to Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 99 investigate the evolution of this part of the NCC (Liuetal.,1990). Qianxi Group in the “Regional Stratigraphy Tables” of North China The oldest zircon ages date back to 3.67–3.65 Ga and come from a (Editorial Group of the Stratigraphic Tables of Hebei Province and fuchsite-bearing quartzite (Liu et al., 1990). These detrital zircons and Tianjin Municipality, 1979). Sun et al. (1984) reported extensive are considered to mark the beginning of crustal growth in eastern migmatisation with distinct palaeosome and leucosome domains. Hebei. The evolution of Qianxi Complex spanned ca. 1 Ga and culminated Enclaves of supracrustal rocks occur within the orthogneisses, and vary in extensive 2.7–2.5 Ga magmatism followed by ca. 2.5 Ga amphibolite in size from a few centimeters to a few hundred meters. The enclaves to granulite facies metamorphism (Pidgeon, 1980; Compston et al., occur as lenses and bands and in stratiform, rounded or irregular, forms 1983; Jahn and Zhang, 1984a,b). and mostly show sharp contact with their host rocks. Isotopic ages The metamorphic rocks of the Qianxi Complex preserve granulite of the gneisses concentrate around 2.6 to 2.4 Ga (Jahn et al., 1987; facies assemblages (two pyroxene granulite, pyroxene–plagioclase Liu et al., 1990; Wang and Peng, 1994; Lv et al., 2012). granulite). Hypersthene granulites (charnockites) and migmatites are The supracrustal rocks, including banded iron formations (BIF) and also common. Geochronological studies of the hypersthene granulite acid metavolcanics in association with amphibolites, granulites, ultraba- from the Qianxi region have yielded ages of ca. 2.5 Ga based on Rb–Sr sic rocks and charnockites, have been widely reported from the study whole rock, Sm–Nd whole rock, and U–Pb zircon techniques (Pidgeon, area (Wang et al., 1985; Wang and Peng, 1994). The charnockitic 1980; Jahn and Zhang, 1984a,b). Some amphibolite-facies rocks gneisses were previously assigned to the Shangchuan and Santunying preserve older ages up to 3.8 Ga. Huang et al. (1986) dated some Formations in Qianxi Group (EGNCST, 1979; BGMRHP (Bureau of amphibolites as ca. 3.5 Ga from Qianxi Complex using the Sm–Nd Geology and Mineral Resources of Hebei Province), 1989)although whole rock technique. subsequent studies regarding them as tectonic units produced by Samples for this study were collected from the Santunying– ductile deformation of largely igneous rocks (Wang, 1991a). The Taipingzhai area (Fig. 2) in eastern Hebei province. Wang (1992) charnockites display prominent gneissosity and banding, with elongat- reported hypersthene-bearing granite-gneiss outcrops in this area, ed supracrustal enclaves and felsic bands (Wang and Peng, 1994). comprising two-pyroxene–granulite, plagioclase–pyroxenite, pyroxene– Charnockites with magmatic features and discordant relationships itabirite and garnet–(sillimanite) felsic gneisses (Wang et al., 1985; with the associated supracrustal rocks occur in the Qianxi–Qianan Huang et al., 1986; Jahn et al., 1987; Liu et al., 1990; Wang, 1992; Wang area. Charnockites in the Santunying–Taipingzhai basement area and Peng, 1994; Lv et al., 2012). The rock suites have been grouped cover more than 500 km2 (Wang, 1991b) and are dominated by under the Shangchuan and Santunying Formations of the Archaean hypersthene-bearing felsic gneisses with subordinate magnetite

Fig. 2. Geological map of the Qianxi Complex in the North China Craton showing Taipingzhai charnockites and surrounding rocks. The sample locations for this study are also shown. 100 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 quartzites, two-pyroxene granulites (mafic granulite), metagabbros Zhao (1992) proposed that the Taipingzhai charnockite suite formed and pyroxenites (Yang et al., 1991). These rocks are overlain by through anatexis of quartz dioritic–tonalitic protoliths. Mesoproterozoic to Neoproterozoic sedimentary rocks and Phanerozoic strata that were later intruded by Mesozoic plutons. The charnockites show different grain size and geochemically classified as granodiorite, 3. Sampling and petrography quartz diorite and plagioclase granite (Wang, 1992; Wang and Peng, 1994). Earlier models assigned the charnockites as Archaean country Representative samples of the garnet-bearing and garnet-absent rocks (Wang, 1990), formed by the transformation of tonalite– charnockites, garnet- and biotite-bearing felsic gneisses, amphibolites granodiorite under CO2-rich conditions (Geng et al., 1990), or as a and metagabbros were collected for this study (Table 1). A brief summary product of crystallization from newly produced magma (Wang, 1988). of the field occurrence (Fig. 3) and petrography of the samples used for

Fig. 3. Representative field photographs. (a) Panoramic view of the charnockite quarry. (b) and (c) Medium to coarse grained charnockite with typical anhydrous assemblage characterized by the presence of orthopyroxene. (d) and (e) Garnet grains along the compositional bands of charnockite. Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 101 zircon dating is given below. Representative thin section photomicro- 3.2. TP-2 (samples 2/1, 2/3, 2/4) graphs showing the mineral assemblages are shown in Fig. 4. An active open cast mine in Fanjiayu village exposes fresh vertical sections of massive grayish green and medium to coarse grained 3.1. TP-1 (sample TP-1/1) charnockitic rocks. In some domains, the charnockite contains medium- to coarse-grained garnet occurring as aggregates or along compositional Medium to coarse grained greasy green charnockitic rocks in this planes. In the lower levels of the quarry, foliated layers of garnet- and locality are exposed along a road cutting near the Qianxi County. biotite-bearing felsic gneisses are exposed. The gneisses show composi- Although the rock appears homogenous and massive, biotite flakes tional layering with garnet- and biotite-rich layers alternating with define a distinct foliation. Garnet is sporadically present as tiny grains quartzofeldspathic layers. The charnockite is locally traversed by pink along compositional bands. Orthopyroxene grains appear as dark clots K-feldspar bearing veins and tongues. These irregular brick-red veins in association with bluish-green quartz. The surrounding rocks are correspond to K-feldspathization possibly resulting from metasomatic leucocratic quartzo-feldspathic gneisses into which the charnockites alteration. intrude. Under thin section, sample TP-2/1 shows the medium to coarse Under thin section, the major mineral assemblage is defined by grained assemblage with orthopyroxene, K-feldspar, plagioclase, quartz antiperthitic feldspar showing stringers and flames of gray K-feldspar and hornblende with minor biotite. The feldspar is dominantly within light colored sodic plagioclase, together with quartz, and straw antiperthite with stringers, island and flames of gray K-feldspar within yellow to light gray coarse and subhedral orthopyroxene. Discrete light colored matrix of plagioclase. Magnetite, apatite and zircon occur plagioclase laths showing lamellar twinning or sometimes oscillatory as accessories. Sample TP-2/3 is composed of coarse grained antiperthitic zoning also occur. feldspar, minor discrete plagioclase showing lamellar twinning, quartz

Fig. 4. Representative photomicrographs of the Taipingzhai charnockite suite and associated rocks. (a) and (b) Mineral assemblage of charnockite with orthopyroxene, K-feldspar, quartz, plagioclase hornblende and biotite. (c) Coarse grained antiperthite in charnockite. (d) Orthopyroxene + clinopyroxene + magnetite assemblage in metagabbro. (e) Garnet + biotite as- semblage. (f) Orthopyroxene + clinopyroxene + plagioclase + antiperthite assemblage. Mineral abbreviations: Opx—orthopyroxene; Cpx—clinopyroxene; Hbl—hornblende; Bt—biotite; Mt—magnetite; Kfs—K-feldspar; Plg—plagioclase; Aprt—antiperthite. 102 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

and biotite. Myrmekite is developed at the grain margins of antiperthitic was re-dissolved in 2% HNO3 to a sample/solution weight ratio of feldspar. The plagioclase shows alteration along cleavage traces and grain 1:1000. The analytical errors vary from 5 to 10% depending on the margins to sericite. Sample TP-2/4 shows an assemblage of garnet- concentration of any given element. An internal standard was used for biotite–K-feldspar–plagioclase-quartz with altered orthopyroxene. monitoring drift during analysis. Trace and rare earth elements were an- Metasomatic alteration has led to the development of myrmekite at the alyzed with analytical uncertainties 10% for elements with abundances margins of plagioclase grains. b10 ppm and approximately 5% for those N10 ppm (Gao et al., 2008).

3.3. TP-3 4.3. Sample preparation and imaging for U–Pb dating and Hf analyses

This locality, exposed along a road cutting near the Santunying Zircons grains were separated using standard procedures for U–Pb middle school, carries large exposures of altered and pale greenish dating and Hf analyses at the Yu'neng Geological and Mineral amphibolite in association with pink K-feldspar bearing syenitic rock. Separation Survey Centre, Langfang city, Hebei Province, China. Under thin section, the amphibolite is medium grained with domi- Cathodoluminescence (CL) imaging was carried out at the Beijing nant assemblage of chloritized hornblende in association with abundant Geoanalysis Centre using scanning electron microscope (JSM510) magnetite and plagioclase. Minor quartz is also present. Zircon occurs as equipped with Gantan CL probe, and transmitted and reflected light accessory mineral. images were examined by a petrological microscope. Individual grains were mounted along with the standard TEMORA 1, with 206Pb/238U 3.4. TP-4 age of 416.75 ± 0.24 Ma (Black et al., 2003), onto double-sided adhesive tape and enclosed in epoxy resin disks. The disks were The open-cast iron mine in Zhaojiacun village exposes garnet- polished to a certain depth and gold coated for CL imaging and U–Pb bearing metagabbroic rocks that occur as thick layers, blocks and isotope analysis. boudins in within magnetite-rich amphibolite and in association with garnet-bearing charnockitic rocks. 4.4. Zircon U–Pb analysis Sample TP-4/1 is metagabbro that shows an assemblage of garnet, clinopyroxene, plagioclase and magnetite with minor secondary recrys- Zircon U–Pb analysis was performed on laser ablation inductively tallized quartz. Sample TP-4/2 is garnet- and magnetite-rich charnockitic coupled plasma spectrometry (LA-ICP-MS) housed at Tianjin Institute that shows medium grained assemblage of garnet + hornblende + of Geology and Mineral Resources. The zircon U–Pb dating analyses altered orthopyroxene + magnetite + K-feldspar + quartz + plagio- were conducted using a Neptune MC-ICP-MS equipped with a 193 nm clase with minor biotite. Apatite and zircon occur as accessories. Geolas Q Plus ArF exciplex laser ablation, with spot sizes of 35 μm. Zircon GJ-1 was used as an external standard for U–Pb dating analyses 3.5. TP-6 (published thermal ionization mass spectrometry normalizing ages of 207Pb/206Pb = 607.7 ± 4.3 Ma, 206Pb/238U = 600.7 ± 1.1 Ma, and Massive exposures of charnockitic rocks occur along rocky hills in 207Pb/235U = 602.0 ± 1.0 Ma; Jackson et al., 2004). Common-Pb correc- the area of Qiuzhuangzi village. Fresh rocks are exposed in several active tions were made using the method of Anderson (2002).Datawere quarries where medium to coarse grained light greenish gray rocks processed using the GLITTER and ISOPLOT (Ludwig, 2003) programs. carrying sporadic enclaves of diorites occur. Orthopyroxene in some Errors on individual analyses by LA-ICP-MS are quoted at the 95% domains are coarse (7–8 mm) and pristine. (1σ)confidence level. Details of the technique are described by Li Under thin section, charnockite sample 6/1 shows coarse assemblage et al. (2009) and Geng et al. (2011). of orthopyroxene–clinopyroxene–plagioclase, K-feldspar (sometimes up to 3–5 mm in size) and quartz. Some of the feldspar grains show 4.5. Zircon Lu–Hf analysis antiperthitic texture. The rock is mostly anhydrous with only rare biotite in most places. Magnetite, apatite and zircon occur as accessories. In situ zircon Hf isotopic analyses were conducted by using a Neptune MC-ICP-MS equipped with a 193-nm laser at the IGGCAS, 4. Analytical techniques with a spot size of 60 μm and a laser repetition rate of 10 Hz at 100 mJ. The detailed analytical procedure and correction for interferences are 176 177 4.1. Petrography similar to those described by Wu et al. (2006).The Hf/ Hf ratios of the standard zircon (GJ-1) and standard zircon (Mud Tank) during anal- σ Polished thin sections were prepared for petrographic study at Peking ysis were 0.282000 ± 0.000030 (2 , n = 200) and 0.282500 ± 0.000030 176 177 University, China. The petrographic study and thin section micrograph (2σ, n = 200), respectively. The Hf/ Hf ratio of GJ-1 is very similar to were carried out at the China University of Geosciences, Beijing. the commonly accepted 176Hf/177Hf ratio of 0.282015 ± 0.0000019 (2σ, n = 15) reported by Elhlou et al. (2006). While the 176Hf/177Hf ratio of 4.2. Whole rock geochemistry Mud Tank is almost identical to the values based on long-term extensive LA-MC-ICP-MS analyses, which are 0.282523 ± 0.000043 (2σ,n= The least altered and homogeneous portions of 13 whole rock 2190; Griffin et al., 2006) and 0.282504 ± 0.000044 (2σ, n = 158; samples were crushed and powdered to 200 mesh for geochemical Woodhead and Hergt, 2005), respectively. analyses after petrographic observation. Major and trace (including rare earth elements) elements analyses were conducted in the National 5. Results Research Center for Geoanalysis, Beijing. The major elements were determined by X-ray fluorescence (XRF model PW 4400), with an ana- 5.1. Whole-rock geochemistry lytical uncertainties ranging from 1 to 3%. Loss on ignition was obtained using about 1 g of sample powder heated at 980 °C for 30 min. The trace The whole rock geochemical data of the samples analyzed in this elements were analyzed by Agilent 7500ce inductively coupled plasma study are given in Table 2 (Supplementary data) and the salient features mass spectrometry (ICP-MS). About 50 mg of powder was dissolved for are briefly described below. about 7 days at ca. 100 °C using HF–HNO3 (10:1) mixtures in screw-top The charnockite suite shows SiO2 contents varying between 52.57 Teflon beakers, followed by evaporation to dryness. The material was and 75.50 wt.%, moderate TiO2 contents of 0.19–1.16 wt.%, moderate t dissolved in 7 N HNO3 and taken to incipient dryness again, and then to high Al2O3 (9.92–18.36 wt.%), FeO (1.96–17.28 wt.%), MgO (0.89– Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 103

5.01 wt.%) and CaO (1.37–7.18 wt.%) contents. Total alkali contents of charnockites have calc-alkaline affinities (Fig. 6a). The exceptions, the charnockites are high and in the range of 3.53–8.51 wt.%; their samples TP2/1 and TP5, lie along the boundary between tholeiite and Mg# values show a wide range from 27.38–60.14. The metagabbro transitional fields (Fig. 6a, fields after Pearce and Norry, 1979). The and amphibolite samples show low SiO2 contents of 43.71–50.24 wt.% charnockites follow a high to medium-K calc-alkaline trend in a SiO2 and their major element chemistry are marked by high TiO2 (1.17– vs. K2Odiagram(Fig. 6b), with two samples (TP1/3 and TP6/1) plotting t 2.46 wt.%), moderate Al2O3 (12.72–13.62 wt.%), high FeO (17.83– off this trend with higher K2O, which may well be due to potassium 18.46 wt.%), high MgO (3.99–6.23 wt.%) and various CaO values (0.95– mobility during metamorphism. The metagabbro and amphibolite show 10.36 wt.%), whereas the garnet-bearing biotite gneiss shows higher medium-K calc-alkaline affinity, and the garnet-bearing biotite gneiss silica content (63.73 wt.%), lower TiO2 (0.57 wt.%), higher Al2O3 displays high-K calc-alkaline composition on K2O vs. SiO2 plot (Fig. 6b, t (17.28 wt.%), lower FeO (5.30 wt.%), and lower MgO (2.08 wt.%) and rel- Rickwood, 1989). In the SiO2 vs. Fe*/(Fe* + MgO) diagram (Frostetal., atively lower CaO (2.65 wt.%) contents. The amphibolites have lower 2001; Fig. 6c), the charnockites and garnet-bearing biotite gneiss fall in total alkali content (3.69–3.75 wt.%) than the garnet-bearing biotite the magnesian field except two samples (TP4/2 and TP4/3) that show gneiss (7.55 wt.%) and their Mg# values are comparable (30.69–44.58). ferroan affinity, similar to the Neoarchaean charnockites of the Yinshan In the total alkali vs. silica diagram (Le Bas et al., 1986; Fig. 5a), the Block (Ma et al., 2013), the post-collisional charnockites from the charnockite suite of rocks straddle the fields from diorite through Chengde area of TNCO (Yang et al., 2014) and the Paleoproterozoic arc syeno-diorite to granite showing both alkalic and subalkalic composi- magmatic charnockites from the Xinghe area of TNCO (Yang and tion. The metagabbro and amphibolite correspond to the field of Santosh, 2015). However, they are distinct from the Paleoproterozoic alkaline gabbro, and the garnet-bearing biotite gneiss falls in the field transitional magmatic charnockites with ferroan features in the Lüliang of monzodiorite with alkaline affinity (Fig. 5a). In An-Ab-Or diagram complex of TNCO (Yang and Santosh, 2015). The garnet-bearing biotite (Maniar and Piccoli, 1989; Frost et al., 2001), the charnockites gneiss also falls in the magnesian field whereas the two amphibolites show tonalitic through granodiorite to granite composition, and the fall in the ferroan field. In the SiO2 vs. Na2O+K2O–CaO diagram composition of the garnet-bearing biotite gneiss corresponds to that (Fig. 6d, Frost et al., 2001), the charnockites dominantly plot in the region of granodiorite (Fig. 5b). In terms of A/NK vs. A/CNK relationships between the boundaries of calc-alkaline and alkali-calcic except one (Maniar and Piccoli, 1989; Frost et al., 2001), the charnockites sample (sample TP1/2) plots in the alkali field and another one (sample dominantly show metaluminous affinity, whereas the garnet-bearing TP2/3) in the calcic field. The garnet-bearing biotite gneiss falls in the biotite gneiss has peraluminous composition (Fig. 5c). alkali-calcic field whereas the amphibolites show alkali affinity. Immobile trace element relationships suggest that the metagabbro, The charnockites show a wide range in transitional trace element amphibolite, garnet-bearing biotite gneiss and, all but two of, the compositions (Ni: 6.18–81.2 ppm; Cr: 3.26–267 ppm; Co: 4.77–

Fig. 5. (a) SiO2 vs. Na2O+K2O diagram. The compositional fields are after Le Bas et al. (1986) (b) An-Ab-Or. (c) A/CNK [Al2O3/(CaO + Na2O+K2O)] vs. A/NK [Al2O3/(Na2O+K2O)] plots. The fields are after Maniar and Piccoli (1989) and Frost et al. (2001). 104 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 6. (a) Zr vs. Y plots (fields after Pearce and Norry, 1979). (b) SiO2 vs. K2Oplots(fields after Rickwood, 1989). (c) Fe*/(Fe* + MgO) vs. SiO2 (fields after Frost et al., 2001). Late Archean charnockites from Ma et al., 2013, post-collisional charnockites from Yang et al., 2014, arc magmatic charnockites from Yang and Santosh, 2014, ridge subduction-related charnockite from

Yang and Santosh, 2015. (d) SiO2 vs. Na2O+K2O–CaO (fields after Frost et al., 2001).

27.5 ppm) whereas the amphibolites and garnet-bearing biotite gneiss et al., 1984). In the Nb/Zr vs. Zr diagram, all the plots fall in the field of have relatively higher concentrations of these elements (Ni: 48.2– rocks generated in subduction-related setting (Fig. 8c; Pearce et al., 121 ppm, 25.3 ppm; Cr: 8.75–311 ppm, 62.1 ppm; Co: 24.1–66.6 ppm, 1984). 14.4 ppm). The rocks are characterized by prominent and variable LREE enrichment on chondrite normalized REE patterns, with relative depletion in HREE (Fig. 7a, c, e and g). Among the ten charnockites 5.2. Geochronology samples, one shows highly depleted REE pattern (sample TP1/3) and clear negative Eu anomaly (δEu = 0.34), whereas another charnockite Representative cathodoluminescence (CL) images of the zircon grains sample TP2/3 shows obviously positive Eu anomaly (δEu = 9.87). The from the different rocks analyzed in this study are given in Figs. 9–16.The remaining eight charnockite samples all show negative Eu anomaly U–Pb analytical data are given in Table 3 (Supplementary data), and the or slightly positive Eu anomaly. The metagabbro and amphibolite data are plotted in concordia diagrams together with age data histo- (samples TP4/1 and TP3) with very flat REE pattern display negative grams and probability curves in Figs. 17–24. A brief description of the Eu anomaly (δEu = 0.82 and 0.89, respectively); a similar trend is also zircon characteristics and age results from individual samples is given shown by the garnet-bearing biotite gneiss (δEu = 0.86). The primitive below. mantle normalized trace element abundances for the charnockites (Fig. 7b) show positive Pb anomaly and negative Nb, Ta, Sr, Th and Ti anomalies. Furthermore, the charnockites exhibit positive anomalies of 5.2.1. Zircon morphology Ba, La, Nd, and Gd and slightly negative anomalies at Ce and Y. The metagabbro and amphibolite exhibit negative anomalies of Th and Sr 5.2.1.1. Charnockite suite. Zircons from the charnockite suite (samples and positive anomalies at Pb and Zr (Fig. 7d and f). The mantle normal- TP1/1, TP 2/1, TP 2/3, TP 4/2 and TP6/1) show prismatic to stumpy mor- ized multi-element patterns (Fig. 7h) of garnet-bearing biotite gneiss phology, and few grains are partly rounded. Most of the zircon grains are similar to those the charnockites with their obviously positive anom- from these samples are colorless and some are light brownish. The alies for Ba, La, Pb and Gd and negative anomalies for U, Nb, Ta and Ti. grains range from 50–300 μm×50–200 μm in size with aspect ratios The salient geochemical features of these rocks suggest subduction- of 4:1 to 1:1. In CL images, all the zircons display clear oscillatory zoning related magmatic settings. In the Y-Nb diagram (Fig. 8a), all these rocks except few zircons with structureless texture, and some of them show are plotted in the VAG + syn-COLG field (Pearce et al., 1984). In the the core–rim textures with thin thick rims where the U–Pb age data Y + Nb vs. Rb diagram, they all fall in the VAG area (Fig. 8b; Pearce are obtained (Figs. 9–13). Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 105

Fig. 7. Chondrite-normalized REE patterns (left side panels) and Primitive mantle-normalized spider diagrams (right side panels). Chondrite normalization values and Primitive mantle values are after Sun and McDonough (1989). 106 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 8. (a) Nb vs. Y diagram, (b) Rb vs. Y + Nb diagram and (c) Nb/Zr vs. Zr diagram. Fields after Pearce et al. (1984).

5.2.1.2. Metagabbro. The zircons from the metagabbro in the study area 5.2.2. U–Pb data (sample TP4/1) display prismatic to stumpy morphology and a few of the grains show partly rounded shapes (Fig. 14). However, only few zir- 5.2.2.1. Charnockite suite cons show clear oscillatory zoning and most of them are structureless. 5.2.2.1.1. TP1/1. Forty two zircon grains from charnockite sample Some of the zircon grains show core–rims textures with thick or thin TP1/1 were analyzed for U–Pb age dating. Among the 42 analyzed rims where the U–Pb dating was done. The zircons are colorless or slight spots, 39 spots are within 5% of discordance, whereas three spots brownish, with a size range of 80–200 μm×50–120 μm and aspect (3, 11 and 12) are discordant resulting from lead loss (see Fig. 17 and ratios of 3:1 to 1:1. Table 3). All the zircon grains define an upper intercept age of 2578 ± 8.4 Ma (MSWD = 0.85; N = 42) and 207Pb/206Pb mean age of 2578 ± 7.3 Ma (MSWD = 0.33, N = 37) (Fig. 17) with relatively high 5.2.1.3. Amphibolite. The zircons from amphibolite in the study area Th/U ratios of 0.20–0.76 except for spot 19 (Th/U = 0.02) and the (samples TP3) display prismatic to stumpy morphology and show three discordant spots (spots of 3, 11 and 12, Th/U = 0.19, 0.06 and clear oscillatory zoning (Fig. 15). A few of the grains show partly round- 0.04, respectively). The two youngest concordant analyses (spots 14 ed shapes and are structureless. All the zircon grains show core–rims and 42) represent zircon overgrowth rims and yield 207Pb/206Pb spot textures with thick or thin rims where the U–Pb dating was done. ages of ca. 2490 Ma and ca. 2506 Ma these are interpreted to represent The zircons are colorless or slight brownish, with a size range of a later thermal event. The 2578 ± 7.3 Ma age is taken to represent the 50–200 μm×50–100 μm and aspect ratios of 2.5:1 to 1:1. best estimate of the crystallization age of this rock.

5.2.2.1.2. TP2/1. Thirty six zircon spots were analyzed from this sam- 5.2.1.4. Garnet-bearing biotite gneiss. All the zircon grains from the ple, and the age data can be divided into two groups (see Fig. 18). Thirty garnet-bearing biotite gneiss (TP2/4) display well-defined crystal two spots define an upper intercept age of 2574 ± 11 Ma (MSWD = morphology with prismatic to stumpy shape and clear oscillatory 0.84; N = 32) and show a 207Pb/206Pb mean age of 2568 ± 9 Ma zoning in the CL images, suggesting typical magmatic origin. The zircon (MSWD = 0.98; N = 27) (Fig. 18). Among the 32 analyzed spots, 27 grains also show core–rim texture with very thin rims suggesting later concordant spots (concordance of 96–100%) possess Th/U values of thermal event, although the rims are too thin to for U–Pb age dating. 0.12 to 1.07. The other five spots in this group (spots 12, 20 21, 27 and Most grains are colorless and some are light brownish, ranging in size 34) show lead loss features and have Th/U ratios of 0.08, 0.56, 1.06, from 100–200 μm×80–120 μm with aspect ratios of 3.5:1 to 1.5:1 0.10 and 0.27, respectively (Table 3). The remaining four zircon spots (Fig. 16). (spots 1, 8, 9 and 11) are concordant and display slightly older ages Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 107

Fig. 9. CL images of zircons from Sample TP1/1 in the charnockite suite. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis. ranging from ca. 2750 to 2600 Ma, with high Th/U ratios of 0.23–0.63. four spots define an upper intercept age of 2544 ± 10 Ma (MSWD = The 2568 ± 9 Ma age is taken as the best estimate of the crystallization 0.93; N = 34) and the concordant plots of this array yield a age of the charnockite, and the minor groups of older zircons are 207Pb/206Pb weighted mean age of 2541 ± 9 Ma (MSWD = 0.74; considered to be inherited grains. N=30)(Fig. 21). Among the 34 analyzed spots, 30 concordant spots 5.2.2.1.3. TP2/3. Forty zircons were analyzed from this sample. (discordance less than 5%) show high Th/U ratios of up to 3.35, the Among the 40 analyzed spots, 38 spots are concordant or near- four discordant analyses (spots 14, 17, 35 and 36) are interpreted to concordant (concordance 92–100%), whereas two spots (6 and 37) have experienced lead loss and display relatively low Th/U ratios of are clearly discordant and suggest lead loss (see Fig. 19 and Table 3). 0.01, 0.43, 0.20 and 0.07, respectively (Table 3). Moreover, two spots The data define an upper intercept age of 2587 ± 10 Ma (MSWD = in this group (spot 12 and 25) are from CL rims and preserve relatively 1.3; N = 40) and yield a 207Pb/206Pb weighted mean age of 2575 ± young 207Pb/206Pb spot ages of ca. 2533 Ma and 2514 Ma, suggesting the 10 Ma (MSWD = 1.5, N = 38) (Fig. 19) with Th/U ratios of 0.25–0.95 possibility of a younger thermal event that may have partially reset except the spot 13 (Th/U = 0.07). This age of 2587 ± 10 Ma is these zircons. One anomalous analysis (spot 22) is also from a zircon interpreted as dating the crystallization age of the rock. rim and yields a 207Pb/206Pb age of 2350 ± 26 Ma with Th/U ratio of 5.2.2.1.4. TP4/2. All the thirty six zircons analyzed from this sample 0.27. The significance of this single analysis is unknown. The 2541 ± are within 5% of discordance and define a discordia line with an upper 9 Ma age is taken as the crystallization age of the charnockite. intercept age of 2543 ± 17 Ma (MSWD = 1.02; N = 36) and a 207Pb/206Pb weighted mean age of 2536 ± 8 Ma (MSWD = 0.9, N = 5.2.2.2. Metagabbro 36) (Fig. 20), with Th/U ratios of 0.25–0.95 except two spots of 1 and 5.2.2.2.1. TP4/1. Thirty of the thirty six zircon analyses obtained from 35 (Th/U = 0.00 and 0.08, respectively; Table 3). Among the 36 this sample (see Fig. 22)define a discordia line with an upper intercept analyzed spots, two spots (spot 25 and 32) are from CL rims with age of 2556 ± 20 Ma (MSWD = 0.33, N = 30). These analyses yield a 207Pb/206Pb spot ages of ca. 2504 Ma and 2514 Ma. These may represent 207Pb/206Pb weighted mean age of 2529 ± 8 Ma (MSWD = 0.92, N = a later thermal event close to the Archaean/Proterozoic boundary, the 30). The Th/U ratios of this zircon group range from 0.23 to 0.65 and resolution of the technique is not precise enough to confirm this. We in- all show higher than 90% concordance. Five younger zircons (spot 1, terpret the 2536 ± 8 Ma age as the crystallization age of the charnockite 13, 18, 32 and 37) have lower Th/U ratios of 0.15–0.57 and are variably magma. discordant. One single analysis (spot. 11) is concordant and preserves a 5.2.2.1.5. TP6/1. Thirty five zircon spots were analyzed from this sam- 207Pb/206Pb age of 1845 ± 25 Ma, which is interpreted to reflect the ca. ple and the age data can be divided into two groups (see Fig. 21). Thirty 1.85 Ga Paleoproterozoic thermal event reported throughout much of 108 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 10. CL images of zircons from Sample TP2/1 in the charnockite suite. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis.

the NCC. The upper intercept age of 2556 ± 20 Ma age is considered to 5.3.1. Charnockite suite represent the crystallization age of this rock. 5.3.1.1. TP1/1. Twenty zircons from this rock were analyzed for Lu–Hf 5.2.2.3. Amphibolite isotopes (Table 7). Among these, nineteen grains show initial 5.2.2.3.1. TP3. Thirty seven zircon spots were selected for U–Pb age 176Hf/177Hf values between 0.281259 and 0.281348 (Fig. 25a) and dating from this sample. All the analyzed spots define an upper inter- positive εHf(t) values ranging from 4.3 to 7.5 with an average of 5.7 cept age of 2540 ± 11 Ma (MSWD = 1.2; N = 37) and yield a (Fig. 25b), when calculated based on the upper intercept age of 207 206 C Pb/ Pb weighted mean age of 2539 ± 9 Ma (MSWD = 1.00; 2578 Ma. They show crustal residence ages (TDM) ranging from 2602 N=28)(Fig. 23). Among the 37 analyzed spots, 28 spots show higher to 2795 Ma (Fig. 25c). However, one zircon grain (spot 29) shows than 95% concordance with high Th/U ratios of up to 2.18. The 9 analy- negative εHf(t) value of —4.6 with lower initial 176Hf/177Hf value of ses (spots 1, 2, 7, 25, 27, 31, 32, 33 and 35) are discordant and preserve 0.281007, when calculated by the same upper intercept age C very low Th/U ratios of 0.01-0.04 (Table 3) similar to those found (2578 Ma). The crustal residence age (TDM) of this zircon grain is in metamorphic zircon. The 2539 ± 9 Ma age is interpreted as the 3343 Ma, much older than the other 19 zircons. The data indicate that crystallization age of this rock. the zircons in the rock were derived from the Meso-Neoarchean juve- nile components with possible reworking of minor Paleoarchean 5.2.2.4. Garnet-bearing biotite gneiss components. 5.2.2.4.1. TP2/4. Thirty eight zircon grains from sample TP2/4 were analyzed for U–Pb age dating. Most of the analyses (36) define an upper intercept age of 2562 ± 10 Ma (MSWD = 0.66; N = 36) and 5.3.1.2. TP2/1. Eight zircons from this sample show initial 176Hf/177Hf show a 207Pb/206Pb weighted mean age of 2561 ± 9 Ma (MSWD = values between 0.281166 and 0.281263 (Table 7, Fig. 25a). Seven zir- 0.63; N = 33; Fig. 24). Among the 36 analyzed spots, 33 analyses display cons show the positive εHf(t) values between 1.0 and 4.4 (Fig. 25b) more than 95% of concordance and preserve Th/U ratios of 0.13–0.94 with an average of 3.0, when calculated by the upper intercept age of C (except the spot of 4, with Th/U = 0.09). Two older analyses (spots 15 2574 Ma. Their crustal residence ages (TDM) range from 2789 to and 34) yield 207Pb/206Pb ages of 2664 ± 26 Ma and 2628 ± 26 Ma, 3000 Ma (Fig. 25c). One zircon grain (spot 29) from xenocrysts shows with Th/U ratios of 0.44 and 0.32, respectively. The 207Pb/206Pb weight- positive εHf(t) value of 6.2, when calculated by the 207Pb/206Pb mean C ed mean age of 2561 ± 9 Ma is taken to represent the crystallization age age of 2686 Ma, with the crustal residence age (TDM) of 2767 Ma, The of this rock, which is similar to the ages from the charnockite suite. The data indicate that the magma was sourced from Mesoarchean juvenile older group of ca. 2.63–2.66 Ga is identical to those from the inherited components. zircons.

5.3. Lu–Hf isotopes 5.3.1.3. TP2/3. In this rock, six zircons were analyzed for Lu–Hf isotopes and the results show initial 176Hf/177Hf values of 0.281168 and Lu–Hf isotope analyses were performed in the same magmatic 0.281244 (Table 7; Fig. 25a). They yield positive εHf(t) values ranging domains from where U–Pb age data were obtained (Fig. 25, Table 7- from 1.3 to 4.0 with an average of 2.8 (Fig. 25b), when calculated by Supplementary Data). The results are briefly discussed below. the upper intercept age of 2587 Ma. The data indicate crustal residence Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 109

Fig. 11. CL images of zircons from Sample TP2/3 in the charnockite suite. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis.

C C ages (TDM) in the range of 2823 to 2988 Ma (Fig. 25c), suggesting residence ages (TDM) range from 2752 to 2906 Ma (Fig. 25c). The data magma sources from Mesoarchean juvenile components. indicate that the magma source came from Mesoarchean juvenile mantle. 5.3.1.4. TP4/2. Sixteen zircons from this rock show initial 176Hf/177Hf values between 0.281229 and 0.281291 (Table 7; Fig. 25a) and positive 5.3.3. Amphibolite εHf(t) values between 2.5 and 4.7 (Fig. 25b) with an average of 3.7, when calculated by the upper intercept age of 2543 Ma. The data 5.3.3.1. TP3. Five zircons from the amphibolite show initial 176Hf/177Hf show crustal residence ages (TC ) in the range of 2748 to 2882 Ma DM values between 0.281227 and 0.281262 (Table 7; Fig. 25a). They show (Fig. 25c) with the average of 2810 Ma, suggesting the magma sources positive εHf(t) values of 2.3 to 3.6 (Fig. 25b) with an average of 3.1, from Mesoarchean juvenile components. when calculated by the upper intercept age of 2540 Ma. All the 5 zircon grains show the crustal residence ages (TC ) ranging from 2813 to 5.3.1.5. TP6/1. In this sample, twelve zircons were analyzed for Lu–Hf DM 2889 Ma (Fig. 25c) with an average of 2845 Ma. The data indicate that isotopes, and the results show initial 176Hf/177Hf values of 0.281142 to the magma source was derived from the Mesoarchean juvenile mantle. 0.281287 (Table 7; Fig. 25a). They display positive εHf(t) values in the range of 0.6 to 4.6 (Fig. 25b) with an average of 3.0 (except one spot shows the slightly negative εHf(t) value of —0.6), when calculated by 5.3.4. Garnet-bearing biotite gneiss the crystallization age of 2544 Ma (the upper intercept age). Their C 176 177 crustal residence ages (TDM) range from 2756 to 3071 Ma (Fig. 25c). 5.3.4.1. TP2/4. In this sample, fourteen zircons show initial Hf/ Hf The data indicate that the magma sources are derived from Mesoarchean values between 0.280966 and 0.281271. Twelve zircons show positive juvenile components with limited reworked crustal materials. εHf(t) values between 0.0 and 4.4 with an average of 2.2, when calculat- ed by the upper intercept age of 2562 Ma. Their crustal residence ages C 5.3.2. Metagabbro (TDM) range from 2779 to 3047 Ma (Fig. 25). However, one zircon grain (spot 19) in this group shows negative εHf(t) value of —5.7, when calcu- 5.3.2.1. TP4/1. Five zircon spots from this rock were analyzed for Lu –Hf lated by the same upper intercept age (2562 Ma). The crustal residence 176 177 C isotopes and the results show initial Hf/ Hf values between age (TDM) of this zircon grain is 3395 Ma, older than the other 12 zircons 0.281215 and 0.281285 (Table 7; Fig. 25a). They show positive in this group. The remaining one grain (spot 34) yielding the individual εHf(t) values between 1.2 and 4.8 (Fig. 25b) with an average of 3.4, 207Pb/206Pb age of 2628 Ma, show the negative εHf(t) values of —4.9 C when calculated by the upper intercept age of 2556 Ma. Their crustal with the crustal residence ages (TDM) of 3399 Ma (Fig. 25). The data 110 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 12. CL images of zircons from Sample TP4/2 in the charnockite suite. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis.

indicate that the magma was sourced from both Mesoarchean– metagabbro shows an assemblage of garnet, clinopyroxene, plagioclase Paleoarchean juvenile components and Paleoarchean reworked crustal and magnetite with minor secondary recrystallized quartz. The amphib- materials. olite has dominant assemblage of chloritized hornblende in association with abundant magnetite and plagioclase. Minor quartz is also present. 6. Discussion Overall the rock types correspond to metamorphosed mafic, intermedi- ate and felsic magmatic protoliths.

6.1. Petrogenesis and formation of Qianxi charnockite suite The rocks analyzed in our study show a wide range of SiO2 (charnockite suite: 52.57–75.50 wt.%; amphibolites: 43.71–50.24 wt.%; The magmatic suite reported in this study is composed of garnet-bearing biotite: 63.73 wt.%), and MgO (charnockite suite: charnockites, metagabbros and amphibolites, metamorphosed under 0.89–5.01 wt.%; metagabbro and amphibolite: 3.99–6.23 wt.%; garnet- amphibolite to granulite faces conditions. The similarity of their crystal- bearing biotite: 2.08 wt.%). In the classification diagrams (Le Bas et al., lization age suggests a prominent phase of magmatism and subsequent 1986; Fig. 5a), the charnockite suite of rocks define a compositional metamorphism in one of the major terranes that makes up the NCC. range from diorite through syeno-diorite to granite showing both The charnockite suite represents massive exposures of medium to alkalic and subalkalic composition. The metagabbro and amphibolite coarse grained rocks with garnet occurring along compositional bands correspond to the field of alkaline gabbro, and the garnet-bearing and representing the product of metamorphism. The feldspar is domi- biotite gneiss falls in the field of monzodiorite with alkaline affinity. In nantly antiperthite with stringers, island and flames of gray K-feldspar An-Ab-Or diagram (Maniar and Piccoli, 1989; Frost et al., 2001), the within light colored matrix of plagioclase formed through high temper- charnockites show tonalitic through granodiorite to granitic composi- ature exsolution. The major mineral assemblage is typically anhydrous tion, whereas the garnet-bearing biotite gneiss is of granodiorite and defined by Opx + Apth + Plg + Qtz ± Hbl + Bt + Grt with apatite composition (Fig. 5b). and zircon occurring as accessories. The garnet bearing biotite gneiss The dominant calc-alkaline affinity (Fig. 6a, b) and the broadly mag- shows an assemblage of garnet–biotite–K-feldspar–plagioclase-quartz nesian composition (Fig. 6c) of the rocks in present study are similar to with altered orthopyroxene. Metasomatic alteration has led to the those of charnockites in subduction–collision settings reported from the development of myrmekite at the margins of plagioclase grains. The other terranes of the NCC (e.g., Ma et al., 2013; Yang and Santosh, 2015; Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 111

Fig. 13. CL images of zircons from Sample TP6/1 in the charnockite suite. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis.

Yang et al., 2014), although they are distinct from the Paleoproterozoic The age data from all the samples of present study are compiled transitional magmatic charnockites in the Lüliang complex of TNCO in Fig. 26, where a peak 207Pb/206Pb mean age of 2554 ± 3.2 Ma (Yang and Santosh, 2015). Their prominent and variable LREE enrich- (N = 257; MSWD = 1.13; Fig. 26a) is displayed. The majority of Th/U ment with relative depletion in HREE, positive Pb, Ba, La, Nd, and Gd values is higher than 0.1, and even range to 3.35 (Fig. 26b), suggesting anomalies and negative Nb, Ta, Sr, Th and Ti anomalies are consistent a magmatic origin for most zircons. The data indicate a major late with arc derivation. Trace element discrimination diagrams also suggest Neoarchean magmatic event at ca. 2.55 Ga. that the rock's protoliths formed in a subduction-related setting. The Lu–Hf data from zircon grains in the various samples of the A summary of the age data obtained in this study (Table 4) shows charnockite suite show dominantly positive εHf(t) values ranging C that the magmatic zircons in the charnockite suite possess upper inter- from 1.0 to 7.5 with crustal residence ages (TDM) of up to 3343 Ma. cept ages of 2587 ± 10 Ma to 2543 ± 17 Ma and 207Pb/206Pb mean ages Zircons in the metagabbro display positive εHf(t) values between 1.2 C of 2578 ± 7.3 Ma to 2536 ± 8 Ma, corresponding to the timing of and 4.8 with TDM of up to 2906 Ma whereas those in the amphibolite emplacement of charnockitic rocks at ca. 2.59–2.54 Ga and marking show 2.3 to 3.6 and 2889 Ma respectively. Zircons from the garnet- major late Neoarchaean magmatism. Some slightly younger zircon rims bearing biotite gneiss also show positive εHf(t) values (up to 4.4) with C might suggest ~2.5 Ga metamorphism, and the few Palaeoproterozoic TDM of 3399 Ma. The data indicate a major juvenile crust formation data suggest tectonothermal events at this time which compare closely event in the Mesoarchean and the reworking in the Neoarchean. A with similar events reported from elsewhere in the NCC (Zhai and previous compilation of data from the NCC (Geng et al., 2012,shadedre- Santosh, 2011; Zhao and Zhai, 2013; Wilde, 2014; Yang and Santosh, gions in Fig. 25) has also recorded crustal addition from juvenile sources 2015, 2015). The amphibolite shows an upper intercept age of 2540 ± during Meso- to Neoarchean. 11 Ma representing the crystallization age of this rock. The garnet- Based on the new geochemical and geochronological data presented bearing biotite gneiss shows upper intercept age of 2562 ± 10 Ma and in this study, we suggest that the formation of the Taipingzhai 207Pb/206Pb mean age of 2561 ± 9 Ma comparable to the ages obtained charnockite suite and associated rocks during a major phase of late from the charnockites. Some inherited zircons in these rocks Neoarchaean magmatism in an arc-related subduction tectonic setting show slightly older 207Pb/206Pb ages of 2664 ± 26 Ma and 2628 ± and was shortly followed by metamorphism at ca. 2.53–2.45 Ga, 26 Ma. possibly marking the assembly of the microblocks within the cratonic 112 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 14. CL images of zircons from Sample TP4/1 of metagabbro. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis.

Fig. 15. CL images of zircons from Sample TP3 of amphibolite. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis. Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 113

Fig. 16. CL images of zircons from Sample 2/4 of garnet-bearing biotite gneiss. Age in Ma (numerator), εHf(t) value (denominator) and spot number (parentheses) are shown against each spot. The large blue circle indicates the spot of Lu–Hf analysis and the smaller pink circle represents the spot of U–Pb analysis.

domain. The ca. 1.85 Ga metamorphic age corresponds with the thermal mantle plumes, we consider the mixed tholeiitic and calc-alkaline affin- event associated with the collision between the Eastern and Western ity as the heterogeneous imprint of subduction-related magmatism. Blocks in the NCC (Zhai and Santosh, 2011; Zhao and Zhai, 2013; Yang and Santosh, 2015, 2015). 6.2.2. Meta-volcanics Lv et al. (2012) reported volcanic rocks that formed at ca. 2.5 Ga 6.2. Neoarchaean arc magmatism in Eastern Block of the North China with bimodal composition of both felsic and maficcomponents. Craton The meta-felsic volcanic rocks display low MgO (0.96–2.67 wt.%), Cr (50.90–87.10 ppm), and Ni (2.78–6.18 ppm) contents, and low The salient geochemical features of the widely distributed late Nb/Ta ratios (13.56–14.54), and high light rare earth elements Neoarchaean magmatic suites in the Eastern Block of the NCC including (LREEs) ((La/Yb)n = 14.75–22.04), which are interpreted to have those of the eastern Hebei area are summarized in Table 5 together with been produced by the partial melting of the lower crust. The meta- the related tectonic setting proposed in previous studies. We briefly basic volcanic rocks (which have been subjected to low-grade amphib- discuss below the salient aspects from the different models proposed olite facies metamorphism) have high MgO and SiO2 and are enriched in previous studies on the various types with a view to evaluate the in LREEs and depleted in high field strength elements (HFSEs) with protolith history and tectonic milieu. positive εNd(t) values (+2.6 to +2.9). Lv et al. (2012) proposed an intra-continent rift setting at 2.5 Ga. 6.2.1. Maficgranulites In another study, Guo et al. (2013) proposed that the Neoarchaean The available geochemical data summarized in Zhao et al., (2001) metavolcanic rocks of the Saheqiao region in eastern Hebei, mainly com- show that the mafic granulites in Eastern Block of the NCC possess posed of garnet two-pyroxene granulites, clinopyroxene amphibolites, tholeiitic or calc-alkali basalt affinity and are characterized by LREE- amphibole plagioclase gneisses and biotite plagioclase gneisses formed enrichment. They also show TiO2, FeO + Fe2O3 and K2O contents and in a subduction-related setting within a convergent plate margin on the REE distribution patterns similar to those observed in continental tho- basis of geochemical features. A previous study by Zhang et al. (2012) leiitic basalts (Cui et al., 1991; Zhai, 1997; Zhao et al., 2001). Although on Neoarchaean metamorphic rocks (hornblende plagiogneiss, plagio- some of the previous studies invoked the interplay of asthenospheric clase amphibolite and magnetite quartzite) in the Shirengou iron deposit 114 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 17. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the sample TP1/1 in charnockite suite. Fig. 18. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the sample TP2/1 in charnockite suite. of eastern Hebei brought out the imprints of submarine volcanic activity related to oceanic slab subduction where Algoma-type BIFs were deposited an arc-related basin during Neoarchaean. volcanics of the Taishan association are the products of partial melting of a subducted oceanic crust. 6.2.3. Felsic volcano-sedimentary rocks The felsic volcano-sedimentary sequence in the western Shandong 6.2.4. Ultramafic–mafic and syenitic dykes Province of the eastern NCC is composed of hornblende gneiss, volumi- A suite of extremely rare coeval ultramafic–mafic and syenitic dykes nous fine-grained biotite gneiss and biotite plagioclase gneiss. Wang was discovered in the Eastern Hebei region of the North China Craton by et al. (2013) constrained the time of formation of the sequence in the Li et al. (2010) with magmatic crystallization ages of 2516 ± 26 Ma and Taishan area as 2.53–2.52 Ga. The majority of zircons from these felsic 2504 ± 11 Ma and single-stage Hf model ages of 2677 Ma and 2705 Ma. rocks have intermediate εHf(t) values (—1.2 to +2.1). Their whole The ultramafic–mafic rocks (olivine gabbros) show high-Mg tholeiitic rock εNd(t = 2522 Ma) values range from +2.6 to —1.8 and TDM2 basalt composition and display LREE-enriched patterns in the absence ages are in the range of 3.03–2.68 Ga. These values suggest reworking of Eu anomalies and enrichment in LILEs and depletion in HFSEs. The sy- or older crust at the end of the Neoarchaean (~2.5 Ga). The Taishan enites are alkaline in composition and show high total REE contents and felsic volcano-sedimentary rocks are rhyodacite–dacite and andesite strong LREE-enriched patterns with minor negative Eu negative as well in composition. These rocks and the associated tonalite display similar as strong LILE-enrichment. The petrological and geochemical features of high SiO2 and low MgO content. The felsic volcanics are characterized these dykes were correlated to magma derivation from a deep subcon- by enrichment in large ion lithophile elements (Rb, Ba, Th and Sr), de- tinental lithospheric mantle source. Combined with evidence for ca. pletion in high field strength elements (Nb, Ta and Ti), moderate to 2.5 Ga granitoid intrusion and metamorphism in the eastern Hebei strong fractionation in REE and Zr–Y systematics and a significant region and adjacent areas, Li et al. (2010) proposed that the NCC has range in whole rock εNd(t = 2522 Ma) values, which are comparable been a stable craton at the end of Archaean. The olivine gabbros in with those of arc-subduction system. The Mg-rich andesites show REE this suite have high εNd(t) values that correlate with the relatively and multi-element patterns similar to those of the rhyodacite–dacites. less enrichment in LILEs and LREEs, whereas the syenites have lower Thus, Wang et al. (2013) suggested that the 2.53–2.52 Ga felsic εNd(t) values that correlate with relative enrichment in LILEs and Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 115

Fig. 20. Zircon U–Pb concordia plots (a) and age data histograms with probability curves Fig. 19. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the sample TP4/2 in charnockite suite. (b) for the sample TP2/3 in charnockite suite.

LREEs. The identical Sr and Nd isotopic compositions of the olivine and 2.77–2.71 Ga (Type 2) and —2.35 to 1.23 and 2.93–2.66 Ga (Type gabbros and syenites have been interpreted to indicate a common origin 3), respectively. Hf isotopic compositions of zircons from three samples for these rocks. A mantle source that was metasomatically enriched in a have εHf(t) values and TDM1(Hf) ages of 0.7–7.2 and 2.84–2.56 Ga subduction-related setting has been invoked to explain the geochemical (Type 1), 2.6–7.4 and 2.74–2.56 Ga (Type 2) and 2.1–6.3 and and isotopic features of these rocks. 2.76–2.60 Ga (Type 3). The authors concluded that the syenogranites were generated by melting of continental crust with different mean 6.2.5. Syenogranites crustal residence ages, and that most of them were emplaced during Toward the waning phase of the Neoarchaean continental evolution the second phase (2.52–2.50 Ga) in an extensional tectonic regime. in the NCC, voluminous syenogranites were emplaced together with The formation of these voluminous syenogranites has been correlated other magmatic suites (trondhjemite–tonalite–granodiorite (TTG), with tectono-magmatic events associated with the stabilization of the monzogranite, diorite, gabbro) (Wan et al., 2012). Syenogranites are NCC at the end of the Neoarchaean. widely distributed in Anshan-Benxi, Qinhuangdao and western In areas where syenogranites occur widely, there are also crustally- Shandong, as well as in southern Jilin, northern Liaoning, northwestern derived monzogranites which formed broadly coevally and show Hebei and central Henan. All these rocks share similar major element geochemical features similar to those of the syenogranites but with compositions, with high in SiO2 and low in CaO, total FeO, MgO, TiO2 lower K2O contents and K2O/Na2O ratios (Yang et al., 2008, 2009; and P2O5. However, their trace and REE compositions are different Wan et al., 2012; and references therein). Both rock types are consid- have been subdivided into three types. (1) Type 1 with a large variation ered to be similar in origin, with the crustally-derived monzogranites in total REE contents, low (La/Yb)n ratios, strong negative Eu*/Eu anom- more widespread than the syenogranites. alies and Ba depletion; (2) Type 2 is similar to Type 1 but has higher Large volumes of Neoarchaean hornblendites, and tonalitic, dioritic, (La/Yb)n ratios. (3) Type 3 shows a large variation in total REE and granodioritic and granitic rocks are exposed in the eastern part of the (La/Yb)n ratios and significantly do not show strongly negative Eu*/Eu NCC (Yang et al., 2008; and references therein). The hornblendites show anomalies and Ba depletion. The whole-rock Sm–Nd isotopic composi- high MgO (8.6–10.6 wt.%), Cr (674–1126 ppm), Ni (125–159 ppm) and tions show large variations in εNd(t) values and TDM(Nd) modal ages, V(224–315 ppm) at low silica contents (SiO2 =45.7–49.0 wt.%). They ranging from —9.49 to —4.72 and 3.70 to 3.25 Ga (Type 1), 0.55 1.03 are enriched in LREE and LILE and show depletion in HFSE. They also 116 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 22. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the Sample TP4/1 metagabbro. Fig. 21. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the sample TP6/1 in charnockite suite. Benxi, Qinhuangdao and western Shandong, southern Jilin, northern show positive εNd(t)values(+1.2to+2.0),suggestingderivationfrom Liaoning, northwestern Hebei and central Henan, with dominant ages an enriched mantle source. The monzogranites have high Sr and Ba con- in the range of ca. 2.6 and 2.5 Ga. The metamorphic rocks are mainly tents and Sr/Y and La/Yb ratios, low Y and HREEs abundances, and posi- exposed in the eastern Hebei, western Liaoning, eastern and western tive εNd(t) and zircon εHf(t) values with Nd and Hf model ages Shandong, southern Jilin and Anshan area of Eastern Block of the NCC younger than 3.0 Ga, indicating partial melting of a juvenile lower crust. (Table 6). Their protolith formation ages are between ca. 2.6 and The K-feldspar granites, with low Sr and Ba concentrations and high 2.5 Ga, followed by metamorphism during 2.54 Ga–2.45 Ga. The mag- HREE and Y contents, are considered to have originated from partial melt- matic zircons from these rocks have heterogeneous εHf(t) composition ing of juvenile crustal materials at shallow crustal levels. The diorites and but dominantly positive εHf(t) values. granodiorites have variable major and trace element concentrations. Magmatic zircons from these rocks show heterogeneous εHf(t) values 6.3. Tectonic implications although with uniform U–Pb ages, suggesting mixing of mafic and felsic magmas, coupled with fractional crystallization. The widespread distribu- Contrasting tectonic models have been proposed for the origin of the tion of Late Archaean magmatism and evidence for magma mixing, possi- Neoarchaean magmatic suites in the Eastern Block of the NCC, with one bly related to mafic magma underplating, correlates well with similar school of thought arguing for a continental magmatic arc environment, features described from Neoarchaean convergent margins (e.g., Santosh whereas the other invoking mantle plume connection that resulted in et al., 2015). However, some of the Chinese authors have attempted significant growth of continental crust at this time (Zhao et al., 2001; to Neoarchaean magmatism in the eastern NCC, particularly the rocks Wilde et al., 2002; Geng et al., 2006; Yang et al., 2008; Zhai and in eastern Hebei with mantle plume activity, although this remains Santosh, 2011; Zhao and Zhai, 2013). speculative. In Table 6, we summarize the geochronological data from previous 6.3.1. Mantle plume studies in this region. At the terminal stage of the Neoarchaean, the The mantle plume origin is inferred on the basis of the short time span NCC witnessed voluminous magmatism, closely followed by metamor- between the widely emplaced TTG rocks and mafic volcanics of continen- phism. The magmatic suites (granitoids, TTG, monzogranite, diorite, tal tholeiite affinity, occurrence of minor komatiitic rocks and bimodal gabbro, among other rocks) are widely distributed in the Anshan- volcanic assemblages, and the diapiric structural style (Zhao et al., 1998, Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 117

Fig. 23. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the Sample TP3 amphibolite. Fig. 24. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the Sample 2/4 garnet-bearing biotite gneiss.

1999a,b, 2001; Wilde et al., 2002; Geng et al., 2006; Yang et al., 2008; These rocks show major Nd model age peak at 3.0–2.6 Ga (Wu et al., Geng et al., 2010; Zhao and Zhai, 2013). 2005). Yang et al. (2008) reported zircon U–Pb ages from diorite, On the other hand, the heat source for metamorphism with an anti- granodiorite, biotite monzogranite and K-feldspar granite from the clockwise P–T path involving isothermal decompression is considered eastern part of the NCC with emplacement ages in the range of to be related to the intrusion and underplating of large amounts of 2526–2515 Ma, and metamorphism at 2500–2440 Ma. These authors mantle-derived magmas (Wells, 1980; Bohlen, 1991; Zhao et al., also speculated that the Neoarchaean magmatism in eastern Hebei 2001). Emplacement of large volumes of mantle-derived magma was the result of mantle plume activity, although no convincing through underplating and leading to regional metamorphism is evidence for plume activity exists. common in continental magmatic arc regions (Wells, 1980; Bohlen, 1991; Condie, 1997; Zhao et al., 2001), above hot spots driven by mantle 6.3.2. Arc-related subduction plumes (Bohlen, 1991; Zhao et al., 1999a, 2001), as well as in continen- Zhao et al. (2005) summarized the different tectonic models for the tal rift environments (Sandiford and Powell, 1986). Therefore, Zhao late Archaean NCC including vertical accretion and multi-stage et al. (2001) suggested a mantle plume model for the formation of the cratonization, as well as marginal accretion-reworking. Some models basement rocks in the Eastern and Western Blocks of the NCC. propose arc–continent collision or continent–continent collision similar Based on SHRIMP U–Pb and single zircon stepwise evaporation to those in Phanerozoic orogenic belts. methods on the granitoids from eastern Hebei Province, Geng et al. The major argument for the continental magmatic arc model is that (2006) suggest that, though diverse in composition, type and origin, TTG gneisses in the Eastern Block have geochemical affinities with calc- these rocks were emplaced and crystallized during a rather short period alkaline plutons in modern continental margin arcs (Wu et al., 1998; of magmatic activity (2536–2492 Ma). They proposed a critical crust Zhai et al., 2005; Li et al., 2010; Zhai and Santosh, 2011; Wang et al., accretion stage at the end of Neoarchaean, and the large scale magmatic 2012, 2013; Zhai, 2014). Among the high Mg and low Mg groups of underplating was correlated to mantle plume activity. TTGs identified by Wang et al. (2012) in western Liaoning, partial melt- The eastern NCC is dominated by Archaean TTG plutons (more than ing of a subducted oceanic slab contaminated by mantle peridotites was 80% of the total exposure) and mafic (volcanic or intrusive) rocks, with envisaged for the former, and partial melting of lower continental crust minor supracrustal rocks (Kröner et al., 1998; Zhao et al., 2001, 2005). composed of juvenile basaltic and pelitic components for the latter. 118 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

176 177 C Fig. 25. Zircon Lu–Hf isotope plots for charnockite suite, metagabbro, amphibolite and garnet-bearing biotite gneiss. (a) Hf/ Hfi vs. age (Ma), (b) εHf(t) vs. age (Ma) and (c) TDM (Ma) vs. age (Ma). The shaded regions are data for Archean to Paleoproterozoic rocks from various regions of the North China Craton as compiled by Geng et al. (2012).

Thus, an Andean-type continental margin arc setting was proposed. (outer side) and calc-alkaline granitic rocks occur on the eastern Some workers suggested that the TTG rocks were formed in a subduc- (inner side). The former were emplaced at 2.55–2.5 Ga and the latter tion setting and are the result of interaction between felsic melts formed at 2.5–2.45 Ga (Zhao et al., 1998; Li, 1999). Thus, Wu et al. derived from partial melting of subducted oceanic crust and (1998) visualized an oceanic realm to the west of the continental metasomatized mantle wedge peridotites during the Archaean (Zhai block, with eastward subduction beneath the block, in a typical island et al., 2005; Li et al., 2010; Wang et al., 2013). setting, followed by final arc–continent collision. Zhang et al. (2000) Wu et al. (1998) suggested an ancient volcanic–magmatic arc zone suggested that the greenstone belts occurring between old continental extending from Hongtoushan in NE China, via Qinglong, through blocks represent orogenic zones. The 2.5 Ga greenstone belts mainly Eastern Hebei to western Shandong, where the arc curves westward. occur between the Qianhuai, Xuchang and Fuping blocks, possibly An old continental block is presently located east of the arc zone. The representing continental amalgamation 2.7–2.6 Ga greenstone belts meta-volcano-sedimentary rocks with isotopic ages of 2.56–2.53 Ga in also underwent strong reworking during the 2.5 Ga event. Zhai et al. the Hongtoushan area in NE China and the Qinglongshan area in Eastern (1992, 1995) proposed continent–continent collision between the Hebei were also considered to have formed in an island arc setting (Zhai Qianhuai and Fuping blocks and between the Qianhuai and Ji'ning et al., 1985; Wu et al., 1998). Several granitoid intrusives occur in this blocks at 2.5–2.6 Ga, based on the distribution of high-pressure granu- arc zone. The TTG rocks are mostly distributed along the western side lites. Zhai et al. (2000) also proposed that between 2.6 and 2.45 Ga,

Table 1 Details of samples analyzed for mineral and whole-rock geochemical analysis and zircon U–Pb and Hf isotopes from Luyashan area, Lüliang complex, North China Craton.

No Sample no. Rock type GPS co-ordinates Mineralogy

1 TP-1/1 Charnockite N40°10′19.71″; E118°20′ 43.76″ Opx + Apth + Plg + Qtz + Bt + Ap + Zr 2 TP-1/2 Charnockite N40°10′19.71″; E118°20′ 43.76″ Opx + Apth + Plg + Qtz + Bt + Grt + Ap + Zr 3 TP-1/3 Charnockite N40°10′19.71″; E118°20′ 43.76″ Opx + Apth + Plg + Qtz + Bt + Grt + Ap + Zr 4 TP-2/1 Charnockite N40°12′ 10.48″; E118°26′ 47.90″ Opx + Kfs + Plg + Qtz + Hbl + Bt + Ap + Zr 5 TP-2/3 Charnockite N40°12′ 10.48″; E118°26′ 47.90″ Opx + Apth + Plg + Qtz + Bt + Ap + Zr 6 TP-2/4 Grt-Bt gneiss N40°12′ 10.48″; E118°26′ 47.90″ Opx + Kfs + Plg + Qtz + Bt + Grt + Ap + Zr 7 TP-3 Amphibolite N40°13′ 14.60″; E118°11′ 27.55″ Hbl + Pl + Mt + Chl + Qtz + Zr 8 TP-4/1 Metagabbro N40°13′ 33.78″; E118°11′ 06.71″ Grt + Cpx + Pl + Mt + Zr 9 TP-4/2 Charnockite N40°13′ 33.78″; E118°11′ 06.71″ Grt + Cpx + Opx + Mt + Hbl + Kfs + Bt + Qtz + Zr 10 TP-4/3 Charnockite N40°13′ 33.78″; E118°11′ 06.71″ Grt + Opx + Kfs + Plg + Qtz + Hbl + Bt + Ap + Zr 11 TP-5 Charnockite N40°12′ 39.32″; E118°32′ 11.40″ Opx + Kfs + Qtz + Pl + Bt + Ap + Zr 12 TP-6/1 Charnockite N40°14′ 10.60″; E118°29′ 24.51″ Opx + Cpx + Plg + Kfs + Qtz + Bt + Ap + Zr 13 TP-6/2 Charnockite N40°14′ 10.60″; E118°29′ 24.51″ Opx + Cpx + Plg + Kfs + Qtz + Bt + Grt + Ap + Zr

Mineral abbreviations: Opx—orthopyroxene; Cpx—clinopyroxene; Grt—garnet; Bt—biotite; Hbl—hornblende; Kfs—K-feldspar; Pl—Plagioclase; Apth—antiperthite; Qtz—quartz; Mt— magnetite; Ap—apatite; Zr—zircon; Chl—chlorite. Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 119

Table 4 Summary of the LA-ICP-MS U–Pb zircon ages in this study for Charnockitic rocks, metagabbro, amphibolite and gneiss from Qianxi complex in Eastern Block, North China Craton.

Sample no. Rock type Magmatic crystallization age Metamorphic age Ages of inherited or xenocryst zircons

TP1/1 Charnockite Upper intercept age: 2578 ± 8.4 Ma (MSWD = 0.85; N = 42) 2490 Ma and 2506 Ma 207Pb/206Pb mean age: 2578 ± 7.3 Ma (MSWD = 0.33, N = 37) TP2/1 Charnockite Upper intercept age: 2574 ± 11 Ma (MSWD = 0.84; N = 32) 207Pb/206Pb mean age: 2686 ± 74 Ma 207Pb/206Pb mean age: 2568 ± 9 Ma (MSWD = 0.98; N = 27) TP2/3 Charnockite Upper intercept age: 2587 ± 10 Ma (MSWD = 1.3; N = 40) 207Pb/206Pb mean age: 2575 ± 10 Ma (MSWD = 1.5, N = 38) TP4/2 Charnockite Upper intercept age: 2543 ± 17 Ma (MSWD = 1.02; N = 36) 2504 Ma and 2514 Ma 207Pb/206Pb mean age: 2536 ± 8 Ma (MSWD = 0.9, N = 36) TP6/1 Charnockite Upper intercept age: 2544 ± 10 Ma (MSWD = 0.93; N = 34) 2533 Ma and 2514 Ma 207Pb/206Pb mean age: 2541 ± 9 Ma (MSWD = 0.74; N = 30) 2350 ± 26 Ma TP3 Amphibolite Upper intercept age: 2540 ± 11 Ma (MSWD = 1.2; N = 37) 207Pb/206Pb mean age: 2539 ± 9 Ma (MSWD = 1.00; N = 28) TP4/1 Amphibolite Upper intercept age: 2556 ± 20 Ma (MSWD = 0.33, N = 30) upper intercept age: 2449 ± 58 Ma 207Pb/206Pb mean age: 2529 ± 8 Ma (MSWD = 0.92, N = 30) (MSWD = 0.59, N = 5) 1845 ± 25 Ma TP2/4 Garnet-bearing Upper intercept age: 2562 ± 10 Ma (MSWD = 0.66; N = 36) 2664 ± 26 Ma and 2628 ± 26 Ma biotite gneiss 207Pb/206Pb mean age: 2561 ± 9 Ma (MSWD = 0.63; N = 33)

the six microblocks in the NCC were amalgamated together by In the eastern part of the NCC, two contrasting models have been continent–continent, continent–arc or arc–arc collision. In a recent proposed for the tectonic setting and evolution of the Jiao-Liao-Ji Belt, study, Wang et al. (2013) suggested an arc-subduction system at with one invoking arc–continent collision (Bai, 1993; Faure et al., ~2.52 Ga in the WPS greenstone belt. 2004; Lu et al., 2006; Wang et al., 2013; and references therein) and the other involving the opening and closing of an intracontinental rift (Zhang and Yang, 1988; Peng and Palmer, 1995a,b; Li et al., 2004a,b; Luo et al., 2004; Li et al., 2005, 2006; Li and Zhao, 2007; Luo et al., 2008; Zhao and Zhai, 2013). Bai (1993) proposed an arc–continent collision model for the belt, with the North and South Liaohe groups considered as N–S-trending back-arc basin, which was subsequently deformed and metamorphosed to form the Jiao-Liao-Ji Belt during arc–continent collision. Faure et al. (2004) considered that the mafic rocks and marine sedimentary units of the North Liaohe Group to represent an active continental arc magmatic belt that developed above a southward subduction zone lying between a northern Archaean Longgang Block and a southern block that incorporated the South Liaohe Group and Neoarchaean basement. This magmatic arc belt was subsequently thrust over the northern Archaean basement during the arc–continent collision. The rift closure model suggests that the Longgang and Langrim blocks originally belonged to the same continen- tal block that underwent early Paleoproterozoic rifting, and closed upon itself in the late Paleoproterozoic to form the Jiao-Liao-Ji Belt (Zhang and Yang, 1988; Li et al., 2004a,b, 2005). The occurrence of Paleoproterozoic high-pressure pelitic granulites in the southern segment of the belt (Zhou et al., 2008; Tam et al., 2011; Li et al., 2012; Tam et al., 2012a,b,c) provides convincing evidence for tectonic processes involving subduction and collision. The close temporal relationship between the emplacement of mafic and TTG magmas and subsequent regional metamorphism, and the major lithologies and their extent of exposure in the unified crustal blocks of the NCC can be accounted for by both mantle plume and con- tinental magmatic arc models (Zhao et al., 2001). The new geochemical and geochronological data presented in our study indicate that late Neoarchaean magmatism occurred in dominantly in an arc-related sub- duction tectonic setting, and was shortly followed by metamorphism during Archaean–Proterozoic transition possibly associated with the collisional assembly of the microcontinents. The Archaean–Proterozoic boundary witnessed global cratonization and formation of large continents, and some workers have even specu- lated a Neoarchaean supercontinent (Windley, 1995; Condie et al., 2001; Rogers and Santosh, 2004). Zhai and Santosh (2011) identified several distinct Archaean continental nuclei in the NCC, termed as microcontinental blocks including the Jiaoliao (JL), Qianhuai (QH), Fig. 26. (a) Combined age data histogram with probability curve and (b) Th/U ratios vs. Ordos Block (OR), Ji'ning (JN), Xuchang (XCH), Xuhuai (XH) and Age (Ma) for all the zircons analyzed in this study. Alashan (ALS) blocks (Fig. 27). Major Neoarchaean magmatic events 120 Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123

Fig. 27. (a) Archean tectonic framework of the North China Craton showing the major microcontinental blocks and intervening greenstone belts (after Zhai and Santosh, 2011). (b) Schematic illustration of the multiple subduction and assembly of the microcontinental blocks; inset shows the QH Block subducting beneath the JL block generating the arc magmatic suite investigated in this study. (c) Archean plate tectonics with multiple subduction realms and magmatism through hotspot (mantle plume) and arc (after Santosh et al., 2010). Abbreviations of the microblocks in (a) and (b): Jiaoliao Block (JL), Qianhuai Block (QH), Ordos Block (OR), Jining Block (JN), Xuchang Block (XCH), Xuhuai Block (XH) Alashan Block (ALS) See text for discussion. at 2.9–2.7 Ga and 2.6–2.45 Ga are recorded in all these blocks albeit with therein). Although a tentative model can be considered where the NCC, different intensity. Other distinctions in rock record have also been Dharwar, Yilgarn and other cratonic nuclei were part of a primitive super- noted among the different microblocks leading to the conclusion that continent, drawing analogy with the model of the earliest supercontinent these microblocks evolved independently before they were amalgamat- Ur as proposed by Rogers and Santosh (2003, 2004) or Kenorland. How- ed into a coherent craton at ca. 2.5 Ga (Zhai and Santosh, 2011). ever, this hypothesis remains speculative until more detailed studies are Our present study area falls along the Jiaoliao microblock adjacent to carried out to better understand the evolution of continental masses in a major Archaean greenstone belt (Fig. 27a, b). Furnes et al. (2014, the early Earth and their correlations and connections. 2015) based on a comprehensive compilation of geochemical and tectonic data on Precambrian greenstone belts from various parts of 7. Conclusions the globe illustrated that the majority of these belts are subduction- related oceanic fragments generated in backarc to forearc tectonic Our investigations on the magmatic suite from the western margin settings. Thus the magmatic suite of present study might have been of the Jialiao microblock in the North China Craton lead to the following generated in an active convergent margin with oceanic lithosphere sub- conclusions. duction beneath the western margin of the Jialiao block. It is believed that Archaean lithosphere was relatively thin (ca. 40 km) which includ- (1) The charnockite suite, metagabbro, amphibolite and gneiss show ed a thick (ca. 20 km) basaltic crust (Komiya et al., 2002; Santosh et al., compositional variation from diorite through syeno-diorite to 2010 and references therein). Therefore, slab melting might have been a granite with dominant calc-alkaline affinity and dominantly dominant process during Archaean subduction. The early Archaean magnesian feature comparable with arc-related magmatic suites. geodynamics was characterized by double layered mantle convection Their positive Pb, Ba, La, Nd, and Gd and negative Nb, Ta, Sr, Th due to higher mantle potential temperatures (e.g., Komiya et al., and Ti anomalies with minor negative anomalies at Ce and Y, 2002). Because of the large number of lithospheric plates, but of smaller are consistent with the geochemical features of arc magmatism. size, multiple subduction zones might have operated resulting in exten- Their compositional plots clustering in the VAG + syn-COLG or sive arc magmatism (Fig. 27c), with an additional minor component of the VAG fields also confirm subduction-related origin. plume-related magmatism (Fig. 27c). Collision of these arcs led to the (2) The morphology, internal structure and high Th/U values of zir- growth of microblocks or primitive continents. The distinct lithological con grains from these rocks suggest magmatic crystallization, features attesting to independent evolution of the six microblocks in closely followed by metamorphism. The zircon U–Pb data from the NCC (Zhai and Santosh, 2011) correspond well with the Archaean the charnockite suite yield upper intercept ages of 2587 ± geodynamic scenario of the growth of microcontinents and their 10 Ma to 2543 ± 17 Ma and 207Pb/206Pb mean ages of 2578 ± subsequent amalgamation to form larger continental masses. 7.3 Ma to 2536 ± 8 Ma, attesting to a major phase of late The early crustal evolution history that we traced from the NCC in the Neoarchaean magmatism, together followed by metamorphism present study is broadly similar to those reported from some of the other during 2533 Ma to 2490 Ma. Zircons in the metagabbro show Archean cratons such as the eastern block of the Dharwar Craton in an upper intercept ages of 2556 ± 20 Ma representing the crys- southern India (2587–2540 Ma accretion followed by 2.53–2.45 Ga ther- tallization age of this rock. The younger ages of 2449 ± 58 Ma mal event; Peucat et al., 2013; Jayananda et al., 2013, and references (upper intercept age) and 1845 ± 25 Ma (207Pb/206Pb spot age) Q.-Y. Yang et al. / Gondwana Research 31 (2016) 96–123 121

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