Paleoproterozoic Arc Magmatism in the North China Craton: No Siderian Global Plate Tectonic Shutdown

Gondwana Research 28 (2015) 82–105

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Paleoproterozoic arc magmatism in the North China Craton: No Siderian global plate tectonic shutdown

Qiong-Yan Yang a,M.Santosha,b,⁎ a School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China b Faculty of Science, Kochi University, Akebono-cho 2-51, Kochi 780-8520, Japan article info abstract

Article history: Arc magmatism in convergent plate margins has been a major contributor to continental growth. Following arc– Received 20 June 2014 arc and arc–continent collisions in the Archean leading to the amalgamation of micro-blocks, the North China Received in revised form 3 August 2014 Craton (NCC) witnessed major pulses of continental arc magmatism during the Paleoproterozoic. In this study, Accepted 3 August 2014 we present geochemistry, zircon U–Pb geochronology and Lu–Hf isotope data from a suite of magmatic rocks Available online 23 August 2014 sampled from the region of confluence of two major Paleoproterozoic suture zones in the NCC — the Inner – Handling Editor: S. Kwon Mongolia Suture Zone (IMSZ) and the Trans-North China Orogen (TNCO). Our zircon U Pb geochronological data indicate new zircon growth during multiple tectonothermal events as displayed in the 207Pb/206Pb weighted Keywords: mean ages of 2410 ± 41 Ma for metagranite, 2480 ± 12 Ma, 2125 ± 18 Ma, 1946 ± 8 Ma, 1900 ± 15 Ma and Zircon U–Pb geochronology 1879 ± 12 Ma from metagabbros, 2446 ± 11 Ma from charnockite, and 1904 ± 6 Ma and 1901 ± 9 Ma from Geochemistry metatuffs. The 207Pb/206Pb upper intercept age of zircons in the khondalite shows 2102 ± 76 Ma which is iden- Continental arc magmatism tical to the age obtained from the magmatic zircons in one of the metagabbros. The khondalites also carry a group Crustal growth and recycling of concordant metamorphic zircons with 207Pb/206Pb mean age of 1881 ± 20 Ma. Metamorphic zircons in the North China Craton gabbros and charnockites also yield similar ages of 1890 ± 14 Ma and 1852 ± 19 Ma respectively. The age data suggest prolonged arc magmatism in a convergent margin setting during ca. 2.48 to 1.9 Ga, followed by metamorphism at ca. 1.89–1.85 Ga associated with the final collision. Lu–Hf analyses reveal that the dominant populations of zircons from all the rock types are characterized by positive εHf values (−1.9 to 6.8; mean 1.8). C The εHf and TDM data suggest that the magmas were mostly derived from Neoarchean and Paleoproterozoic juvenile components. The salient geochemical features of these rocks attest to magma generation from heterogeneous sources involving subduction-derived arc components with minor input from continental crust. The results presented in this study, together with those from previous investigations in different domains of the IMSZ and TNCO suggest major Paleoproterozoic arc magmatic events in the NCC lasting for nearly 600 million years associated with the final assembly of the crustal blocks into a coherent craton. Construction of the final cratonic architecture of the NCC thus witnessed not only the arc–continent amalgamations at 2.7– 2.5 Ga, but also major crust building events in the Paleoproterozoic through melts generated from juvenile and recycled components in continental magmatic arc systems along an active convergent margin, followed by intense deformation and metamorphism during the final collision at 1.85–1.80 Ga. The prominent Paleoproterozoic magmatic records in the NCC do not support the proposal of global plate tectonic shutdown in the Siderian and confirm vigorous convergent margin magmatism and crust building processes throughout the Paleoproterozoic. © 2014 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

1. Introduction active continental margin setting associated with ocean–continent subduction (e.g., Manikyamba and Kerrich, 2012; Straub and Zellmer, The subduction of oceanic lithosphere in convergent margins 2012; Santosh et al., 2013a). Condie and Kröner (2013) noted that gives rise to arc magmatism (Stern, 2002), with a pronounced composi- with few exceptions, post-Archean accretionary orogens comprise tional link between the trench input and arc output (Straub and b10% of accreted oceanic arcs, whereas continental arcs compose Zellmer, 2012). Arc magmatism in space and time under different 40–80% of these orogens. From Nd and Hf isotopic data, they showed geodynamic settings ranges from intra-oceanic arcs associated with that accretionary orogens on the globe include 40–65% juvenile crustal ocean–ocean convergence, plume–arc interaction, arc–backarc, and components, with more than 50% of these produced in continental arcs. Due to higher degrees of partial melting in the mantle, oceanic arcs in the Archean were thicker as compared to their Proterozoic equivalents. ⁎ Corresponding author at: School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China. Condie and Kröner (2013) suggested that the vigorous onset of plate E-mail address: [email protected] (M. Santosh). tectonics in the late Archean with rapid production of continental

http://dx.doi.org/10.1016/j.gr.2014.08.005 1342-937X/© 2014 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved. Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 83 crust witnessed a major transition in the primary site of production of (TNCO), respectively. Post-collisional magmatism related to slab continental crust from accreted oceanic arcs and oceanic plateaus in break-off has also been recorded from a number of localities along the Archean to dominantly continental arcs thereafter. these suture zones (e.g., Yang et al., 2014a). Convergent plate margins are potential regions of crustal growth In this study, we investigate the geochemistry and zircon U–Pb geo- where magmas derived by melting of mantle wedge fluxed with slab- chronology and Lu–Hf isotopes in a suite of plutonic, volcanic and dehydrated fluids and subducted slab result in vertical growth and metasedimentary rocks from the zone linking the two major thickening of arc crust, whereas the accretion of oceanic and trench ma- Paleoproterozoic subduction systems in the NCC — the IMSZ and the terials onto the active continental margins causes lateral growth TNCO. We report a diverse assemblage of granitoids, charnockites, (Santosh, 2013). Subduction-derived mafic magmas and crust-derived gabbros, felsic volcanic tuffs and khondalites from this region which felsic magmas in arc settings thus contribute to vertical growth of the shows a common link to active convergent margin tectonics and crust (e.g., Foley et al., 2002; Rudnick and Gao, 2003). Tholeiitic to magmatism within continental arc settings. Our results compare with calc-alkaline mafic, intermediate and felsic magmas are generated in the isotopic data of Paleoproterozoic arc magmatic suites reported active margins through a combination of processes including influx of from elsewhere in these zones suggesting an important phase of conti- slab-dehydrated fluids and melts into mantle wedge, wedge melting, nent building in the NCC during the Paleoproterozoic. assimilation of crustal materials by arc magma and magma mixing (Gao et al., 2012; Santosh et al., 2013a; Samuel et al., 2014; 2. Geological setting Manikyamba et al., in press). In a recent model, Castro et al. (2013) proposed relamination from below the lithosphere as an alternate mecha- 2.1. North China Craton nism for new crust generation in magmatic arcs of active continental margins and mature intraoceanic arcs, and explained the dominantly The North China Craton (NCC) (Fig. 1) is a collage of several andesitic composition of the continental crust. micro-continents that preserve the history of Neoarchean crust for- The North China Craton (NCC) (Fig. 1) preserves important rock re- mation, which were subsequently incorporated into two major cords of early Precambrian crustal growth and microcontinent amal- crustal blocks by the late Neoarchean, the Eastern and Western gamation. The Neoarchean greenstone belts that surround the micro- Blocks (e.g., Zhai and Santosh, 2011; Geng et al., 2012; Zhao and blocks in the NCC are considered to represent the vestiges of older Zhai, 2013). The final collision and cratonization of these crustal arc–continent collision (Zhai and Santosh, 2011). Subsequently, the blocks occurred during the late Paleoproterozoic at around 1.85– NCC witnessed a prolonged subduction–accretion history from early 1.80 Ga (e.g., Wilde et al., 2002; Kusky and Li, 2003; Zhao et al., to the late Paleoproterozoic associated with the amalgamation of 2005; Kusky et al., 2007; Santosh et al., 2007; Zhao et al., 2008; major crustal blocks and the final cratonization (Zhai and Santosh, Santosh, 2010; Zhai and Santosh, 2011; Peng et al., 2011; Liu et al., 2011; Santosh et al., 2012, 2013b; Zhao and Zhai, 2013). Two major con- 2012; Santosh et al., 2013b; Zhao and Zhai, 2013). The NCC is bor- vergent margins, one running E–W between the Yinshan and Ordos dered on the south by the Qinling–Dabie Shan orogen, to the north Blocks and the other trending N–S between the Western and Eastern by the Central Asian Orogenic Belt, and to the east by the Su-Lu belt Blocks, possibly in a double-sided subduction realm (Santosh, 2010) (e.g., Zhai and Santosh, 2011; Zhao and Zhai, 2013). generated voluminous arc magmas of diverse composition during the The Western Block formed by amalgamation of the Ordos Block in Paleoproterozoic (e.g., Zhao et al., 2008; Dan et al., 2012; Liu et al., the south and the Yinshan Block in the north along the east–west- 2012; Santosh et al., 2012) which were subsequently incorporated trending IMSZ (incorporating the Khondalite Belt) at 1.90–1.95 Ga. within the two major collisional sutures, termed as the Inner This was followed by the final collision between the Western and East- Mongolia Suture Zone (IMSZ) and the Trans-North China Orogen ern Blocks along the TNCO at ca. 1.85–1.80 Ga (e.g., Zhao et al., 2005;

Fig. 1. Generalized 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 study area in Fig. 2 is shown by box. 84 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

Santosh et al., 2007; Zhai and Santosh, 2011; Santosh et al., 2013b; Zhao 2001, 2008). The occurrence of high-pressure granulites and and Zhai, 2013) in a double-sided subduction realm, broadly coeval retrograded eclogites in some locations within the TNCO has been with the global assembly of the Columbia supercontinent into which taken to indicate that this zone represents a major continent–continent the NCC was incorporated at this time (Santosh, 2010). The Yinshan collision zone (Zhao et al., 2001; Wilde et al., 2002; Li and Kusky, 2007; Block is composed of low-grade granite–greenstone and high-grade Trap et al., 2007; Zhao et al., 2008, among others). Kröner et al. (2005a, TTG (tonalite–trondhjemite–granodiorite) gneiss and granulite ter- b) proposed that the TNCO represents an Andean-type continental mar- rains, with greenschist to granulite facies metamorphism at ca. 2.5 Ga gin or a Japan-type island arc. The earliest arc magmatic event in the and preserves broad structural style and metamorphic history similar TNCO is recorded by a suite of granitoids emplaced at 2.56–2.52 Ga to that of the Eastern Block (Liu et al., 1993). The Ordos Block is largely (Wilde et al., 2005), with the final collision between the Eastern and covered by Mesozoic to Cenozoic strata of the Ordos Basin (Zhao et al., Western Blocks recorded from the timing of metamorphism at 2005). The Eastern Block preserves some of the oldest rock records in 1880–1820 Ma, a time span of more than 650 Ma (Zhao et al., 2008; the NCC (Zhai and Santosh, 2011) and is considered to have witnessed Zhao and Zhai, 2013). Santosh et al. (2013b) proposed a long lived sub- Paleoproterozoic rifting along its eastern margin during 2.2–1.9 Ga, duction–accretion history prior to the final collisional amalgamation of and subsequent closure along the Jiao-Liao-Ji Belt (Zhao and Zhai, the major crustal blocks in the NCC during the late Paleoproterozoic. 2013, and references therein). The Paleoproterozoic metamorphic complexes in the TNCO include the Lüliang, Zhongtiao, Zanhuang, Taihua and Northern Hebei. Among 2.2. Inner Mongolia Suture Zone these, the Lüliang complex has been well studied and the systematic geochronological data presented by Zhao et al. (2008) from the various The IMSZ, within which the Khondalite Belt is distributed, is consid- rock suites in this complex provide insights into the pre-, syn- and post- ered as the suture zone along which the Yinshan Block in the north and collisional history. The pre-tectonic rocks in the complex are mostly TTG the Ordos Block in the south amalgamated to form the coherent West- gneisses with calc-alkaline chemistry and magmatic arc affinity which ern Block of the NCC during the late Paleoproterozoic (e.g., Zhao et al., were emplaced at ca. 2.5 Ga, representing the earliest arc-related mag- 2005, 2006; Santosh et al., 2007; Zhai and Santosh, 2011; Santosh matic event. This was followed by arc-related magmatic pulses at 2.4 et al., 2012, 2013b; Zhao and Zhai, 2013). The northern margin of the and 2.2 Ga. Metamorphism associated with collision occurred at ca. IMSZ is marked by the E–W trending ductile shear zones between the 1.87 Ga. Subsequently, a series of post collisional granitoids including Paleoproterozoic lithologies within the IMSZ and the Neoarchean TTG porphyritic granite, charnockite, and massive granite were emplaced gneisses and granulites in the Yinshan Block. The northeast-trending during 1.83 to 1.79 Ga. ductile shear zone between the Paleoproterozoic khondalites within Liu et al. (2012) reported geochemical and zircon U–Pb data from the IMSZ and the Paleoproterozoic high-pressure-granulite-bearing metavolcanic units in the Yejishan and Lüliang groups of the Lüliang TTG gneisses within the TNCO represents its eastern margin. The south- Complex in TNCO. Their geochemical modeling shows that the parental ern margin of the IMSZ is covered by Phanerozoic sedimentary strata. magma of these metavolcanics was derived from the partial melting of The Helanshan–Qianlishan, Daqingshan, and Jining–Liangcheng– subduction-enriched spinel lherzolites and spinel–garnet lherzolites, Fengzhen are the major belts occurring within the IMSZ. The rock with subsequent fractional crystallization and assimilation of continental types in these belts have been broadly grouped into accretionary se- material. Their data are consistent with a magmatic arc system in an ac- quence and continental arc components, both of which were subjected tive continental margin, generating widespread arc-related magmatism to granulite-facies metamorphism during the Paleoproterozoic colli- at 2.2 Ga, followed by metamorphism during 1.90–1.83 Ga associated sional event (Santosh, 2010). The varied lithological associations in with the collisional event and post-collisional extension at 1.80 Ga. the IMSZ including amphibolites, metachert, metagabbro, and marble, Late Paleoproterozoic post-collisional magmatic suites also occur in with a vast sequence of quartzite, and metapelitic units have been cor- the central and southern segments of the TNCO represented by related to a long-lived subduction–accretion of both oceanic and conti- charnockites, granites, mafic dykes and volcanic suites (e.g., Geng nental components. The TTG gneisses, charnockites and calc-alkaline et al., 2004; Peng et al., 2005, 2008; Hou et al., 2008; Liu et al., 2009; granites are thought to represent a continental arc. Thus, the Khondalite Zhao et al., 2009; Wang et al., 2010). These rocks range in age from ca. Belt has been redefined as a major Paleoproterozoic collisional suture, as 1.68 Ga to 1.78 Ga and are considered to extend for more than 500 km the Inner Mongolia Suture Zone (Santosh, 2010). across the border between the TNCO and the Eastern Block along the The khondalites in the IMSZ have attracted considerable attention northern margin of the NCC. In a recent study, Yang et al. (2014a) re- in recent studies following the discovery of ca. 1.92 Ga ultrahigh- ported petrological, geochemical and zircon U–Pb geochronological temperature granulites representing extreme metamorphism under and Lu–Hf data from a pyroxenite (websterite)–gabbro–diorite suite temperatures exceeding 1000 °C and pressures around 10 kbar at Xinghe in Inner Mongolia along the northern segment of the TNCO. (Santosh et al., 2006, 2007, 2008, 2009; Liu et al., 2011; Tsunogae The LA-ICPMS U–Pb data show emplacement ages of 1786.1 ± 4.8 Ma, et al., 2011; Guo et al., 2012; Zhang et al., 2012; Jiao et al., 2013; 1783 ± 15 Ma, 1767 ± 13 Ma 1754 ± 16 Ma and 1754 ± 16 Ma, with Santosh et al., 2013b; Yang et al., 2014b). Sapphirine-bearing granulites dominantly positive εHf(t) values (up to 5.8), suggesting magma deri- in Tuguiwula and Daqingshan, and spinel- and cordierite-bearing vation from juvenile sources. Yang et al. (2014a) correlated the khondalites elsewhere in several localities within the IMSZ have provid- magma genesis with post-collisional extension during slab break-off ed insights into the metamorphic and tectonic history associated with following the westward subduction of the Eastern Block and its collision the subduction–collision tectonics along the IMSZ (e.g., Santosh et al., with the Western Block. Asthenospheric upwelling and heat input are 2013b). considered to have triggered the magma generation from a heterogeneous, subduction-modified sub-lithospheric mantle source. 2.3. Trans-North China Orogen 2.4. Study area The 100–300 km wide and ca. 1200 km long and nearly N–Strending TNCO represents the collisional suture between the Eastern and Our present study areas in the Xinghe and Jining regions of Inner Western Blocks of the NCC (Zhao and Zhai, 2013). The TNCO has been Mongolia are located at the junction between the E–W trending IMSZ subdivided into two major domains: (1) high-grade areas (including and the approximately N–S trending TNCO (Figs. 1, 2), and include the Taihua, Fuping, Hengshan, Huai'an, and Xuanhua Complexes) and three distinct terranes, the Huai'an, Fengzhen, and Yinshan, juxtaposed (2) low-grade granite–greenstone terrains (including the Dengfeng, from southeast to northwest. The Huai'an terrane is largely composed of Zhongtiao, Zanhuang, Lüliang and Wutai Complexes) (Zhao et al., ca. 2.5 Ga tonalite–trondhjemite–granodiorite (TTG) gneisses and 2.0 to Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 85

Fig. 2. Geological map of part of the North China Craton showing the study area and locations of samples analyzed in this study.

1.9 Ga potassic granitoids into which are emplaced Paleoproterozoic as that in the Huangtuyao mine, although some of the recent studies mafic dykes that have undergone ca. 1.85 Ga high-pressure granulite fa- suggest that the protoliths of these rocks also involved active margin cies metamorphism (e.g., Zhai et al., 1992; Liu et al., 2009; Peng et al., volcanic input in an arc-related setting (Dan et al., 2012). 2010). The Yinshan terrane comprises the ca. 2.5 Ga late Archean TTG Samples for the present study were collected from several locations gneisses and granulites, along with granite–greenstone belt (e.g., Zhao in the Jining area belonging to the Jining–Liangcheng–Fengzhen com- et al., 2005), and covered by Paleoproterozoic sediments (Wan et al., plex and from the Xinghe are belonging to the Huai'an terrane of the 2009). The Fengzhen terrane incorporates the ‘Khondalite Belt’ com- Northern Hebei complex (Fig. 2). The sample locations, GPS coordinates, prising a vast Paleoproterozoic accretionary sequence of psammopelitic, rock types and summary of mineral assemblages are given in Table 1, pelitic, volcanic and carbonate sediments metamorphosed to high and and representative field photographs are shown in Fig. 3. ultra-high temperature conditions, together with imbricated oceanic fragments (amphibolites, metagabbros, Banded Iron Formations), and 3. Rock types and petrography arc-related continental fragments (charnockites, granitoids) developed during a prolonged subduction–accretion history prior to final collision The rock types analyzed in this study for geochemistry and zircon U– in the late Paleoproterozoic (Santosh et al., 2012, 2013b). The major Pb geochronology and Lu–Hf isotopes include metagranite, charnockite, rock types in this area include charnockites, TTG gneisses, khondalites metagabbro, meta-tuff and khondalite. A brief description of the rock (granulite facies metapelites), and minor Banded Iron Formations. The types and their petrography (as studied from polished thin sections at TTG gneisses locally incorporate lenses and blocks of garnet-bearing the Peking University, China) is given below. Representative photomi- mafic granulites. The khondalites were thought to represent continental crographs showing the mineral assemblages and textures are given in shelf sequences, incorporating abundant graphite mineralization such Figs. 4–5.

Table 1 Details of samples analyzed for whole rock geochemical analysis and zircon U–Pb and Hf isotopes.

No. Sample no. Rock type Locality Mineralogy

1 OY-XH-1A Metagranite Xinghe area (GPS coordinates N40° 43′ 26.23″; E114° 09′ 05.31″; height 1122 m) Kfs+Pl+Qtz+Bt 2 OY-XH-12 Metagranite Longshengzhuang village (GPS coordinates N40° 43′ 08.26″; E113° 25′ 34.65″; height 1363 m) Kfs+Pl+Qtz+Bt+Grt 3 OY-XH-7A Charnockite Zhujiaying village (GPS coordinates N40° 36′ 20.88″; E113° 58′ 50.76″; height 1298 m) Pl+Kfs+Qtz+Cpx+Opx+Hbl 4 IM13-18 Metagabbro Tuguiwula area (GPS coordinates N40° 46′ 42.15″; E113° 15′ 08.43″; height 1305 m) Pl+Cpx+Opx+Hbl+Mt 5 IM13-19 Metagabbro Tuguiwula area (GPS coordinates N40° 45′ 46.35″; E113° 15′ 11.92″; height 1332 m) Pl+Cpx+Opx+Mt 6 IM13-20 Metagabbro Tuguiwula area (GPS coordinates N40° 45′ 46.35″; E113° 15′ 11.92″; height 1332 m) Pl+Cpx+Opx+Bt+Mt+Ap 7 OY-XH-1B Metagabbro Xinghe area (GPS coordinates N40° 43′ 26.23″; E114° 09′ 05.31″; height 1122 m) Pl+Cpx+Opx+Mt+Bt 8 OY-XH-9A Felsic tuffs Longshengzhuang village (GPS coordinates N40° 42′ 01.98″; E113° 26′ 13.68″; height 1373 m) Kfs+Qtz+Pl+Grt+Bt 9 OY-XH-11 Felsic tuffs Longshengzhuang village (GPS coordinates N40° 43′ 06.92″; E113° 25′ 37.40″; height 1371 m) Kfs+Qtz+Pl+Grt+Bt 10 OY-XH-3A Khondalite Xinghuagou village (GPS coordinates N40° 52′ 47.98″; E113° 59′ 05.54″; height 1240 m) Kfs+Qtz+Pl+Grt+ Sil+Bt+Zr+Ap

Mineral abbreviations: Opx — orthopyroxene; Cpx — clinopyroxene; Bt — biotite; Hbl — hornblende; Kfs — K-feldspar; Pl — Plioclase; Qtz — quartz; Mt — magnetite; Ap — apatite; Zr — zircon; Grt — garnet; Sil — sillimanite. 86 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

Fig. 3. Representative ﬁeld photographs. (a) Metagranite exposure with enclaves of metagabbro (location OY-XH-1A and B in Table 1). (b) Porphyritic metagranite (OY-XH-12). (c) Felsic tuff layer (left) in association with garnet-bearing metapelitic rock (right) (OY-XH-9A). (d) Thin intercalation of felsic tuff in metapelite (OY-XH-11). (e) Greasy green charnockite (OY-XH-7A). (f) Coarse porphyroblastic garnet and sillimanite bearing khondalite (OY-XH-3A).

Fig. 4. Representative photomicrographs of thin sections of the analyzed rock samples. (a) and (b): Charnockite. (c) and (d) Metagabbro. Mineral abbreviations: Opx — orthopyroxene; Cpx — clinopyroxene; Hbl — hornblende; Pl — plagioclase; Kfs — K-feldspar. Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 87

Fig. 5. Representative photomicrographs of thin sections of the analyzed rock samples. (a) and (b): Metagranite. (c) Khondalite. (d) Felsic tuff. Mineral abbreviations: Grt — garnet; Sil — sillimanite; Bt — biotite; Pl — plagioclase; Kfs — K-feldspar; Qtz — quartz.

3.1. Metagranite charnockite is plagioclase (50%), K-feldspar (20%), quartz (15%) orthopyroxene (5%), hornblende (7%) and minor clinopyroxene (3%). The metagranites in the study area occur either as large plutons ex- Biotite is nearly absent. The pyroxene and plagioclase grains show posed in massive hillocks, or as sheet-like intrusions ranging in thick- subhedral morphology and typical magmatic fabric. ness from several tens to few hundreds of meters emplaced within TTG gneisses. At some places, the metagranites carry enclaves of 3.3. Metagabbro metagabbros or meta-dioritic gabbros ranging up to a few meters in size such as in the Xinghe area (Fig. 3a). The metagranite in this study Metagabbros occur as massive exposures or as enclaves within the is medium grained and shows prominent foliation defined by the align- granitoids (Fig. 3a), and are dark grayish and medium grained with pla- ment of biotite flakes. Compositional banding is also displayed at some gioclase, clinopyroxene, orthopyroxene and biotite. The metagabbros places, suggesting partial melting. In sample OY-XH-1A from Xinghe, collected from the Xinghe (samples OY-XH-1B) and Jining (IM13-18, the dominant minerals are pink K-feldspar, quartz, plagioclase and bio- IM13-19, IM13-20) areas for this study are melanocratic and medium tite. In the second location near Longshengzhuang (sample OY-XH-12), grained. In thin section, the rocks are composed of plagioclase (40– the metagranite shows prominent porphyritic texture (Fig. 3b) with 45%), clinopyroxene (30–40%), orthopyroxene (10–15 vol.%), and coarse grained pink K-feldspar (up to 5 cm in length) set in a medium minor hornblende, biotite and apatite (together 2–5%). The metagabbros grained matrix comprising plagioclase, quartz and biotite. The rock from the Jining area show higher modal content of hornblende (up to has been deformed with the feldspar crystals showing a preferred orien- 10%, sample IM13-18) and biotite (up to 8%, sample IM13-19) together tation along the foliation. The quartz is grayish and shows stretching with minor recrystallized quartz. Opaque minerals are ilmenite and mag- and elongation. Clots of porphyroblastic garnet are distributed along netite (3–8%). the foliation planes. In thin section perthitic K-feldspar (40%), quartz (40%), plagioclase (10%), garnet (5%) and biotite (2%) are the dominant 3.4. Felsic tuff minerals. Metamorphosed felsic volcanic tuffs occur as dismembered sequences intercalated with garnet- and biotite-bearing leptynitic rocks 3.2. Charnockite as in Longshengzhuang village (sample OY-XH-9A, Fig. 3c), or as thick meter-sized layers in surrounding regions (sample OY-XH-11, Fig. 3d). Charnockite is one of the dominant rock types in the Xinghe area and These rocks are light gray colored, fine grained and show fine lamina- constitute massive exposures extending from a few tens of meters to tion with sporadic subhedral and undeformed garnet grains. Despite several kilometers (Fig. 3e). Locally veins and patches of incipient metamorphism and deformation, the rocks preserve relict primary tex- charnockite also occur in some localities, developed through high tem- tures such as depositional lamina and clastic nature. The absence of any perature metamorphism during carbonic fluid influx from massive metamorphic aluminosilicate minerals (such as sillimanite in the asso- charnockite into the adjacent TTG gneisses as reported in a recent ciated khondalite) other than the rare millimeter-sized porphyroblastic study (Yang et al., 2014c). The charnockite analyzed in this study (OY- garnets precludes a pelitic sedimentary source and suggests a volcanic XH-7A) was collected from the Zhujiaying village, where the rock is origin, similar to those reported from the Neoarchean convergent mar- emplaced within TTG gneisses. The charnockite is garnet-absent and gin sequences of Attappadi in southern India (Praveen et al., 2013). The carries bands and enclaves of mafic granulites ranging in size from a volcanic origin is also confirmed from their rhyolite to rhyodacite com- few decimeters up to 10 m. The dominant mineral assemblage of the position (see section on geochemistry). The thin laminations (b1to 88 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

5 mm) in the rock defined by alternate mafic-rich and felsic-rich layers silicate glass NIST was used to optimize the instrument. Raw data suggest fluctuations in the debris input (Stix and Gorton, 1991). These were processed using the GLITTER program to calculate isotopic ratios laminations suggest deposition in moderate to deep-water conditions. and ages of 207Pb/206Pb, 206Pb/238U, and 207Pb/235U, respectively. Data In thin section, the rock shows sub-angular to sub-rounded grains of were corrected for common lead, according to the method of quartz (35–45%), occurring in a groundmass of K-feldspar (50–55%), Anderson (2002), and calculated the ages by ISOPLOT 4.15 software plagioclase (8–15%), biotite and minor garnet (together 2–3%). The feld- (Yuan et al., 2004). spars show variable degrees of alteration. The quartz grains are moder- At the Tianjin Institute of Geology and Mineral Resources, zircon U– ately to well-sorted and fine grained (b0.2 mm). Pb dating and in-situ Hf isotopic analyses were conducted using a Nep- tune MC-ICP-MS equipped with a 193 nm Geolas Q Plus ArF exciplex 3.5. Khondalite laser ablation, with spot sizes of 35 μmand50μm, respectively. Zircon GJ-1 was used as an external standard for U–Pb dating and in-situ zircon The khondalite sample OY-XH-3A is from a stream section in the Hf isotopic analyses. Common-Pb corrections were made using the Xinghuagou village of the Xinghe area and the region forms part of method of Anderson (2002). Data were processed using the GLITTER the Jining–Liangcheng–Fengzhen sector of the Khondalite Belt in the and ISOPLOT (Ludwig, 2003) programs. Errors on individual analyses NCC. The rock is medium grained and foliated with garnet–sillimanite- by LA-ICP-MS are quoted at the 95% (1σ) confidence level. Details of rich bands alternating with quartzofeldspathic layers (Fig. 3f). The the technique are described by Li et al. (2009) and Geng et al. (2011). khondalite in the present study does not contain graphite, as against The analytical procedures using SHRIMP II followed those of the various types of graphite-bearing metapelites reported from Williams (1998). Data were processed and assessed using the software adjacent regions (e.g., Yang et al., 2014d). The rock also does not show programs Squid (Ludwig, 2001) and ISOPLOT (Ludwig, 2003). Common typical UHT minerals like sapphirine in association with quartz, Pb correction was made using the measured 204Pb and applying the orthopyroxene + sillimanite and low-Zn spinel + quartz reported values of Stacey and Kramers (1975). Uncertainties for each analysis from adjacent regions (e.g., Santosh et al., 2012; Yang et al., 2014b), sug- are at 1σ, whereas the weighted mean age is quoted at 2σ. gesting a relatively low-Mg–K bulk composition. The major minerals in this rock are feldspar (50% including K-feldspar (40%) and plagioclase 4.3. Whole rock major and trace element analyses (10%)), quartz (30%), garnet (10%) and sillimanite (8%), with minor biotite, zircon and apatite (together 2%). Although previous studies con- Major elements were analyzed on glass discs fused with Li-borate sidered the protoliths of the khondalites as passive margin sediments flux by X-ray fluorescence spectrometry (XRF) at the China University (e.g., Condie et al., 1992), recent works suggest that these rocks might of Geosciences Beijing, following the method of Harvey (1989).Traceel- have formed within an active margin in an arc-related setting (Dan ements (including REE) were analyzed by a Finnigan MAT Element 2, et al., 2012), which is consistent with our finding of felsic tuffs interca- high resolution ICP-MS at the State Key Laboratory of Geological Pro- lated with this rock suite in several localities as described below. cesses and Mineral Resources (GPMR), following procedures described by Qi et al. (2000). The Chinese national standard GSR-1 (Xie et al., 4. Analytical techniques 1989) was used as standard. Major and trace elements of a few samples (IM13-18, 19 and 20) 4.1. Zircon separation and CL imaging were determined by XRF (Phillips MAGIX PRO Model 2440) at the Na- tional Geophysical Research Institute (NGRI), India, on pressed pellets Zircons grains were separated using standard procedures for U–Pb prepared from powdered whole-rock samples. Volatiles were deter- dating and Hf analyses at the Yu'neng Geological and Mineral Separa- mined by loss on ignition. The analytical technique is described in detail tion Survey Centre, Langfang City, Hebei Province, China. The CL imag- in Manikyamba et al. (2012). Trace and REEs were performed using HR ing was carried out at the Beijing Geoanalysis Centre. Individual grains ICP-MS (Nu Attom) at NGRI. Precision and reproducibility obtained for were mounted along with the standard TEMORA 1, with a 206Pb/238U international reference materials JG-2 and JGB-1 are 2–5% (1σ)for age of 417 Ma (Black et al., 2003), onto double-sided adhesive tape most elements. and enclosed in epoxy resin discs. The discs were polished to expose the central part of the grains and gold coated for cathodoluminescence 5. Results (CL) imaging and U–Pb isotope analysis. Zircon morphology and internal structure were examined using a JSM-6510 Scanning Electron Mi- 5.1. Whole-rock geochemistry croscope (SEM) equipped with a backscatter probe and a Chroma CL probe. The zircon grains were also examined under transmitted and Whole rock geochemical data, including major, minor, trace and rare reflected light using a petrological microscope. earth elements, on the metagranites, metagabbros, charnockites, felsic volcanic tuff and khondalites are given in Table 2. The salient geochem- 4.2. Zircon U–Pb and Hf isotopic analysis ical features of the various rock types are summarized below.

Zircon U–Pb analysis was performed on laser ablation inductively 5.1.1. Major elements coupled plasma spectrometry (LA-ICP-MS) housed at the Peking Uni- The metagabbros show a restricted range in SiO2 varying between versity (Beijing) (samples OY-XH-1A, OY-XH-1B, OY-XH-3A, OY-XH- 48.75 and 49.48 wt.%, whereas one sample shows a dioritic composition

7A, OY-XH-9A and OY-XH-11), and the Tianjin Institute of Geology with 54.23 wt.% SiO2.TheserockshavemoderateTiO2 contents ranging and Mineral Resources (Tianjin) (samples IM13-19 and IM13-20). The from 1.4–2.2 wt.%, moderate to high Al2O3 (12.5–16.2 wt.%), Fe2O3 IM13-18 sample was analyzed by using SHRIMP II at the Beijing (9.6–18.4 wt.%), MgO (5.5–9.9 wt.%) and CaO (6.3–9.6 wt.%) contents. SHRIMP Centre. All the in situ zircon Hf isotopic analyses were per- Total alkali contents of these metagabbros are high in the range of formed at the Tianjin Institute of Geology and Mineral Resources. The 3.42–6.5 wt.%. Mg# ranging from 38.1–66.4 indicates a progressive dif- analyses were conducted on the same spots or in adjacent domains ferentiation trend in the metagabbros. The major element chemistry of where U–Pb dating was done. the khondalite is marked by 71. 23 wt.% SiO2, 0.71 wt.% TiO2,15.1wt.% Zircon U–Pb analysis at Peking University followed the analytical Al2O3, 4.04 wt.% Fe2O3, 1.52 wt.% MgO and 1.4 wt.% CaO, whereas the procedures reported in Yuan et al. (2004). In the LA-ICP-MS method, charnockite shows a relatively lower SiO2 content (56.31 wt.%), compa- the laser spot diameter and frequency were 30 μm and 10 Hz, respec- rable TiO2 (0.76 wt.%), higher Al2O3 (17.25 wt.%), Fe2O3 (7.42 wt.%), tively. Zircon 91500 was employed as a standard and the standard MgO (4.57 wt.%) and CaO (7.12 wt.%). The charnockite shows relatively Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 89

Table 2 Whole rock geochemical data from Xinghe and Jining, North China Craton.

Rock type Metagranites Charnockite Metagabbros Tuffs Khondalite

OY-XH-1A OY-XH-12 OY-XH-7a IM13-18 IM13-19 IM13-20 OY-XH-1B OY-XH-9A OY-XH-11 OY-XH-3A

SiO2 71.55 72.1 56.31 54.23 49.48 49.39 48.75 76.51 78.09 71.23

TiO2 0.29 0.31 0.76 2.21 2.06 1.36 1.97 0.05 0.06 0.71

Al2O3 14.86 13.89 17.25 13.99 15.36 16.1 12.53 13.54 12.01 15.1 (T) Fe2O3 1.65 2.52 7.42 9.64 10.27 10.06 18.38 0.14 0.72 4.04 MnO 0.01 0.03 0.11 0.11 0.14 0.13 0.27 0 0.02 0.05 MgO 0.47 0.91 4.57 5.73 9.92 8.82 5.51 0.07 0.3 1.52 CaO 1.45 1.59 7.12 6.27 8.38 9.2 9.59 1.82 1.07 1.4

Na2O 3.66 2.31 5.13 3.04 3.13 2.1 2.65 3.65 3.79 1.81

K2O 4.77 4.87 1.27 3.62 1.18 2.61 0.75 2.27 2.04 2.74

P2O5 0.17 0.24 0.25 0.82 0.72 0.63 0.33 0.17 0.05 0.07 LOI 0.61 0.39 0.23 0.94 0.77 0.56 −0.18 0.84 0.93 0.82 Total 99.5 99.14 100.42 99.66 100.64 100.4 100.55 99.06 99.09 99.49 Mg# 37.0 42.5 55.8 54.9 66.4 64.2 38.1 50.2 46.1 43.6 Cr 3.7 24.5 102.7 4.6 5.3 5.6 70.4 1.2 3.3 77.6 Co 3.1 3.9 25.5 23.9 30.9 41.5 60.9 0.5 1.1 8.2 Ni 6.4 3.9 50.9 15.6 18 22.2 63.9 1.5 1.8 17.7 Rb 95 244.7 7.1 65.5 10.9 77.2 11.1 46.5 59 89.3 Sr 421.1 200.6 661.4 912.6 1447.6 966.5 126.2 126.1 302.9 168.8 Li 12.5 32 11.1 8.8 25.4 36 14 Cs 0.1 0.9 0 0 0 0.2 0 0.4 0.6 0.5 Be 0.6 4.1 1.3 1.1 1 3.4 0.4 Ba 1261 514 558 2224 613 2227 277 175 565 571 Sc 1.8 7.3 19.3 12 16.3 21.8 47.6 0.6 1.8 9.2 V 22.2 26.4 144.6 7.3 9.8 14.1 406.5 2.5 4.5 74.6 Ta 0 0.6 0.3 2.9 2 1.1 0.6 0 0.1 0.2 Nb 2.5 8.8 7.8 46.5 23.8 15.2 10.2 0.2 0.4 8 Zr 157 145 160 517 71 293 162 129 51 304 Hf 3.9 4 3.7 8.7 1.7 6.1 4.3 3.4 1.3 8 Th 1.1 18.8 0.3 0.7 1.3 0.6 0.3 0.4 0.4 1.4 U 0.2 2.3 0.1 0.4 0.3 0.4 0.2 0.2 0.3 0.5 Y 2.4 22.4 15.4 40.8 19.8 30.6 51.4 3.9 4.5 20.3 Cu 3.2 1.5 33.2 1.5 1.7 1.8 81.8 1.9 1.3 2 Zn 29.1 31.8 89.5 83.2 40.9 57.3 144 7.4 13.3 68.5 Pb 10.6 27.4 3.8 9.2 9.4 9.4 1.3 14.2 10 13.7 Ga 18.8 18.4 21.6 26.9 28 26.7 19.7 14.8 13.6 22.6 La 20.40 46.20 25.30 70.60 57.40 49.80 15.10 68.40 22.20 36.70 Ce 32.90 99.40 58.80 151.80 128.10 111.10 38.50 112.00 34.10 71.20 Pr 3.20 11.60 7.60 23.60 20.10 17.80 5.40 10.50 3.20 7.80 Nd 10.70 42.90 31.30 89.30 76.10 70.60 25.40 32.30 9.60 27.50 Sm 1.50 7.90 5.70 16.60 14.10 14.00 6.60 3.70 1.20 4.50 Eu 0.90 1.00 1.50 3.30 2.20 3.60 2.00 1.10 0.40 1.20 Gd 1.00 5.60 4.30 10.10 7.60 8.40 7.70 2.20 0.90 3.90 Tb 0.10 0.80 0.60 1.50 1.00 1.20 1.30 0.20 0.10 0.60 Dy 0.50 4.20 3.00 6.50 3.90 5.40 8.70 0.80 0.80 3.40 Ho 0.10 0.80 0.60 1.00 0.50 0.80 1.80 0.10 0.20 0.70 Er 0.20 0.10 1.50 2.70 1.40 2.20 5.20 0.30 0.40 2.10 Tm 0.00 0.30 0.20 0.40 0.20 0.30 0.80 0.00 0.10 0.30 Yb 0.10 2.00 1.30 2.30 1.10 2.10 5.00 0.30 0.50 2.20 Lu 0.00 0.30 0.20 0.30 0.20 0.30 0.80 0.10 0.10 0.30 Fe/Fe + Mg 0.8 0.7 0.6 0.6 0.5 0.5 0.8 0.7 0.7 0.7 Na + K − Ca 7 5.6 −0.7 0.4 −4.1 −4.5 −6.2 4.1 4.8 3.2 A/CNK 1.1 1.2 0.8 0.7 0.7 0.7 0.6 1.2 1.2 1.8 A/NK 1.3 1.5 1.8 1.6 2.4 2.6 2.4 1.6 1.4 2.5 Na + K 8.4 7.2 6.4 6.7 4.3 4.7 3.4 5.9 5.8 4.6 Sr/Y 173.5 8.9 42.9 22.4 73 31.5 2.5 32.4 66.8 8.3 Nb/Zr 0 0.1 0 0.1 0.3 0.1 0.1 0 0 0 K/Rb 416.6 164.9 1487.5 458.4 900.2 280.2 555.5 404.7 286.5 254.4 Zr/TiO2 546.4 476 210.6 233.8 34.3 215.8 82.2 2571.2 810.2 427.5 Y + Nb 5 31.3 23.2 87.3 43.7 45.8 61.6 4.1 4.9 28.3 La/Yb 153.3 23.4 20.1 30.4 53.1 23.3 3 201.1 46.8 16.4 Th/Yb 8.6 9.5 0.2 0.3 1.2 0.3 1.1 0.9 0.6 Q 27.5 34.1 0 0 0 0 0 43.3 45.9 43 An 7.3 8 20.2 13.9 24.2 26.7 19.9 9.2 5.4 7 Ab 31.3 19.8 43.3 25.8 26.3 10.9 22.2 31.4 32.7 15.5 Or 28.5 29.1 7.5 21.4 6.9 15.4 4.4 13.7 12.3 16.4 K 39,552 40,349 10,539 30,013 9783 21,639 6187 18,820 16,891 22,719

higher total alkali content (6.4 wt.%) and Mg# (56) than those of the contents ranging from 5.83–5.92 wt.%. Mg# varying between 46 and khondalite (4.55 wt.%; 44). The tuffs are characterized by high SiO2 50 suggests an evolved character. The metagranites characteristically contents in the range of 76.5–78.1 wt.%, extremely low TiO2 (0.05– show high SiO2 (71.55–72.10 wt.%), moderate Al2O3 (13.9–14.9 wt.%), 0.06 wt.%), MgO (0.07–0.03 wt.%), low CaO (1.1–1.8 wt.%) and moder- low Fe2O3 (1.65–2.52 wt.%), CaO (1.45–1.6 wt.%), extremely low TiO2 ate Al2O3 (12–13.5 wt.%). These samples exhibit high total alkali (0.29–0.31 wt.%) and MgO (0.01–0.03 wt.%) contents. Total alkali 90 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 contents are high in the range of 7.18–8.43 wt.%. These metagranites tholeiitic to feeble calc-alkaline affinity and straddle the ferroan and display an evolved character with Mg# varying between 37 and 43. In magnesian fields (Fig. 7c). the total alkali vs. silica diagram (Le Bas et al., 1986; Fig. 6a) the metagabbros occupy the field of gabbro and monzodiorite showing a 5.1.2. Trace and rare earth elements subalkaline to alkaline composition, and the charnockite falls in the The metagabbros show a wide range in transitional trace element field of monzodiorite with a sub-alkaline affinity and the metagranites compositions (Ni: 15.6–63.9 ppm; Cr: 4.6–70.4 ppm; Co: 23.9– correspond to the field of sub-alkaline granite (Fig. 6a). The tuffs and 60.9 ppm) whereas the tuffs and metagranites have relatively lower con- khondalite distinctively show rhyolite–dacite and rhyodacite–dacite centrations of these elements (Ni: 1.5–1.8 ppm, 3.9–6.4 ppm; Cr: 1.2– compositions respectively in Zr/TiO2 vs. SiO2 plot (Fig. 6b), similar to 3.3 ppm, 3.7–24.5 ppm; Co: 0.5–1.1 ppm, 3.1–3.9 ppm). Charnockite magmatic rocks of active continental margin settings. In the An–Ab– shows relatively higher concentrations of Ni, Cr and Co than the Or diagram (Maniar and Piccoli, 1989), the charnockite shows tonalitic khondalite (Ni: 50.9 and 17.7 ppm, Cr: 102.7 and 77.6 ppm and Co: composition, the tuffs fall in the trondhjemite field, and the 25.5 and 8.2 ppm respectively). The studied samples are characterized metagranites and khondalite fall in the granite field (Fig. 6c). In terms by distinct enrichment in large ion lithophile elements (LILE; Table 2). of A/NK vs. A/CNK relationships, the charnockite shows metaluminous They exhibit prominent and variable LREE enrichment on chondrite nor- affinity, whereas the granites, tuffs and khondalite have peraluminous malized REE patterns [metagabbros (La/Sm)N =~1.5–2.8; charnockite composition (Fig. 6d). Immobile trace element relationships suggest a (La/Sm)N =2.9;khondalite(La/Sm)N = 5.2; tuffs (La/Sm)N = ~11.7– tholeiitic to transitional trend for the metagabbros and calc-alkaline af- 12.0; metagranites (La/Sm)N = ~9.0–3.8], with relative depletion in finity for tuffs, khondalite and one sample of metagabbro (Fig. 7a). The HREE (especially in the metagranite OY-XH-1A and the two samples of metagranites exhibit high-K calc-alkaline composition, while the tuffs OY-XH-9A and OY-XH-11) (Fig. 9a, c, e, g and i). Out of four charnockite, khondalite and tuffs reflect medium-K calc-alkaline fea- metagabbro samples one shows a relatively flat REE pattern (Fig. 9e). tures on K2Ovs.SiO2 plot (Fig. 7b). In the SiO2 vs. Fe*/(Fe* + MgO) dia- One metagranite sample displays a positive Eu anomaly whereas the gram (Fig. 7c), the charnockite falls in the magnesian field, consistent other shows a negative Eu anomaly suggesting plagioclase accumula- with the Neoarchean charnockites of the Yinshan Block (Ma et al., tion and fractionation respectively (Fig. 9a). The primitive mantle nor- 2013) and the post-collisional charnockites from the Chengde area of malized trace element abundances for the metagranites (Fig. 9b) TNCO (Yang et al., under review). The metagabbros show a prominent display positive Rb anomalies and negative anomalies at Nb and Ta.

Fig. 6. (a) SiO2 vs. Na2O+K2O diagram. The compositional ﬁelds are after Le Bas et al. (1986).(b)SiO2 vs. Zr/TiO2 diagram. (c) An–Ab–Or. (d) A/CNK [Al2O3/(CaO + Na2O+K2O)] vs. A/NK

[Al2O3/(Na2O+K2O)] plots. The ﬁelds are after Maniar and Piccoli (1989). Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 91

Fig. 7. (a) Zr vs. Y plots (fields after Pearce and Norry, 1979). (b) SiO2 vs. K2O plots (fields after Rickwood, 1989). (c) Fe*/(Fe* + MgO) vs. SiO2 (fields after Frost et al., 2001). Late Archean charnockites from Ma et al., 2013 and post-collisional charnockites from Yang et al., under review.

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). 92 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

Besides, sample OY-XH-1A exhibits positive anomalies for Ba, Sr, Zr, and depletion relative to OY-XH-12 (Fig. 9b). The charnockite (OY-XH-7A) Hf and negative anomalies for Th, Nd and Sm whereas OY-XH-12 con- shows similar mantle normalized multi-element patterns (Fig. 9d) to trastingly exhibits negative anomalies for Ba, Sr, Zr, and Hf and positive the metagranites except negative anomalies at Rb. The metagabbros anomalies for Th, Sm and Nd. Sample OY-XH-1A displays greater HREE show enrichment in LILE (Rb and Ba) and depletion in HFSE (Th)

Fig. 9. Chondrite-normalized REE patterns for (a) metagranites, (c) charnockite, (e) metagabbros, (g) tuffs and (i) khondalite. Chondrite normalization values are after Sun and McDonough (1989). Primitive mantle-normalized spider diagrams for (b) metagranites, (d) charnockite, (f) metagabbros, (h) tuffs and (j) khondalite. Primitive mantle values are after Sun and McDonough (1989). Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 93

Fig. 9 (continued). reflected in terms of negative Nb–Ta and Zr–Hf anomalies. These sam- ratios of 3:1 to 1.2:1. In CL images, the zircons display clear oscillatory ples show distinct negative Sr and Th anomalies (Fig. 9f). Sample OY- zoning, with core–rim textures, suggesting magmatic origin followed XH-1B displays diminished LREE and elevated HREE relative to the by metamorphic overgrowth (Fig. 10a). The rims are too thin for U–Pb other metagabbro samples (Fig. 9f). The mantle normalized trace ele- dating. ment abundance patterns for the tuffs are marked by positive anomalies Sixteen spots were analyzed on 16 zircon grains (Table 3) and the re- for Rb and K with negative anomalies at Ba, Th, Nb, Ta, Zr and Hf sults show Pb contents of 31–616 ppm, U contents of 54–912 ppm and (Fig. 9h). Distinct negative anomalies are observed at Ce, sample OY- Th contents of 40–126 ppm (with spot 14 showing exceptionally high XH-11 exhibits positive anomalies for Ba and Sr whereas OY-XH-9A values of 2152 ppm of Pb, 1149 ppm of U and 534 ppm of Th) and shows negative Ba and Sr anomalies (Fig. 9h). The multi-element pat- high Th/U ratios of 0.14 to 4.39. The data define an intercept age of terns of khondalite exhibit positive Rb, K, Zr and Hf anomalies with neg- 2410 ± 41 Ma (MSWD = 2.1, N = 16) (Fig. 13 a, b), and display ative anomalies at Th, Nb and Ta (Fig. 9j). 207Pb/206Pb weight mean age of 2390 ± 20 Ma (MSWD = 1.4, N = 5) when calculated by using data with concordance higher than 95%. 5.2. Geochronology Based on the high Th/U ratios and clear oscillatory zoning of the zircon grains, the 2.4 Ga age is taken to represent the timing of emplacement of Cathodoluminescence (CL) images of representative zircon grains the granitoid magma. from the various rock types analyzed in this study are shown in Figs. 10–12 with the spot 207Pb/206Pb ages and εHf(t) values. The U– 5.2.2. Charnockite Pb analytical data from LA-ICPMS and SHRIMP dating are given in Sup- Most of the zircon grains from the charnockite (sample OY-XH-7A) plementary Tables 3 and 4. The zircon U–Pb concordia plots and histo- show prismatic to stumpy morphology, and few grains are partly round- grams with probability curves are show in Figs. 13–17. ed. Most grains are colorless and some are light brownish, ranging in size from 80–200 to 50–120 μm with aspect ratios of 3:1 to 1:1 (with a few up 5.2.1. Metagranite to 5:1). In CL images (Fig. 10b), all the zircon grains display clear oscilla- Zircons from the metagranite (sample OY-XH-1A) show prismatic to tory zoning and core–rim textures and carry low luminescence rims stumpy morphology, and few grains are partly rounded. Most of the zir- which are too thin for LA-ICPMS U–Pb analysis. They show complex con grains from these samples are colorless and some are light brown- structures, corresponding to magmatic origin and later metamorphic ish. The grains range from 100–200 × 30–80 μm in size with aspect overprint, with a possible fluid-assisted late magmatic alteration. 94 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

Fig. 10. Cathodoluminescence (CL) images of representative zircon grains from metagranite OY-XH-1A (a), charnockite OY-XH-7A (b) and metagabbro IM13-18 (c). The values written against each grain represent the spot age in Ma (top) and the εHf(t) calculated for the 207Pb/206Pb mean age (bottom).

A total of 32 spots were analyzed on 32 zircon grains (Table 3) and weighted mean age of 2446 ± 11 Ma (MSWD = 0.50, N = 17). The sec- the results are divided into 3 groups: the first group contains 29 spots ond group including the two spots (Nos. 10 and 11) shows Pb contents which show Pb content in the large range of 0.5 to 245 ppm, U content of 88 ppm and 124 ppm, U contents of 70 ppm and 93 ppm, and Th con- in the range of 30 to 460 ppm and Th content in the range of 48 to tents of 154 ppm and 215 ppm, respectively, with Th/U ratios of 0.43 1034 ppm, respectively, with high Th/U ratios of 1.40 to 3.04 (spot 37 and 0.46. They show high concordance of 99%–100% and 207Pb/206Pb with Th/U ratio of 61.76 has been rejected). From the concordia dia- spot ages of 2389 ± 10 Ma and 2370 ± 10 Ma with the mean age of grams (Fig. 13 c, d), 28 of the 29 zircons (except spot 37) define an 2381 Ma. The third group is defined by a single zircon (spot 13) with upper intercept age of 2.47 Ga which is identical to their 207Pb/206Pb concordance of 100%. The grain shows Pb content of 199 ppm, U content

Fig. 11. Cathodoluminescence (CL) images of representative zircon grains from gabbros (a) IM13-19, (b) IM13-20 and (c) OY-XH-1B. The values written against each grain represent the spot age in Ma (top) and the εHf(t) calculated for the 207Pb/206Pb mean age (bottom). Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 95

Fig. 12. Cathodoluminescence (CL) images of representative zircon grains from tuffs (a) OY-XH-9A and (b) OY-XH-11 and khondalite (c) OY-XH-3A. The values written against each grain represent the spot age in Ma (top) and the εHf(t) calculated for the 207Pb/206Pb mean age (bottom).

Fig. 13. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the meta-granite sample OY-XH-1A. Zircon U–Pb concordia plots (c) and age data histograms with probability curves (d) for the charnockite sample OY-XH-7A. 96 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

Fig. 14. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the metagabbro sample IM13-18. Zircon U–Pb concordia plots (c) and age data histograms with probability curves (d) for the metagabbro sample IM13-19. of 205 ppm, and Th content of 372 ppm, with a Th/U ratio of 0.55 and a Twenty five zircon grains were analyzed from sample IM13-19 for 207Pb/206Pb age of 2208 ± 10 Ma. The high Th/U ratios and clear oscilla- U–Pb age dating (Table 3) and the results are plotted in Fig. 14 c, d. tory zoning of the older concordant group of zircons, suggest that the The Pb, U and Th ranges of the zircons are 14–68 ppm, 37–167 ppm 207Pb/206Pb weighted mean age of ca. 2.45 Ga represents the timing of and 5–222 ppm, respectively, with high Th/U ratios of 0.93 to 1.60 emplacement of the protolith magma. The 207Pb/206Pb weighted mean (with the exception of spot 22 showing low Th/U ratios of 0.06). All age of ca. 1.89 Ga suggests new zircon growth at this time from a the spots cluster as a coherent group on the concordia (concordance major thermal event, followed by recrystallization at ca. 1.85 Ga and of 95%–100%, except spot 22 with a concordance of 92) with 207Pb/ 1.75 Ga. The 2.45 Ga and 2.2 Ga ages mark magmatism and thermal 206Pb ages ranging from 1807 to 1935 Ma. The data yield 207Pb/206Pb events. weighted mean age of 1879 ± 12 Ma (MSWD = 0.59, N = 25) (Fig. 14c, d). 5.2.3. Metagabbros Thirty five zircon grains were analyzed from sample IM13-20 In the cathodoluminescence (CL) images, the zircons from the (Table 3) and the results are plotted in Fig. 15 a, b. The Pb, U and Th metagabbros (samples IM13-18, Fig. 10c; IM13-19, IM13-20 and OY- ranges of the zircons are 11–276 ppm, 31–676 ppm and 9–420 ppm, re- XH-1B, Fig. 11 a, b, c) display well-defined crystal morphology with spectively, with high Th/U ratios of 0.27 to 1.02 (except spot 19 with prismatic shape and/or clear oscillatory zoning, suggesting a magmatic low Th/U ratios of 0.06). Twenty-nine spots cluster as a coherent origin. Most of them are colorless and some are light brownish, with a group on the concordia (concordance of 92%–100%) with 207Pb/206Pb size range of 100–500 × 50–300 μm and aspect ratios of 3:1 to 1:1 ages ranging from 1913 to 1976 Ma. The data yield 207Pb/206Pb weight- (some grains show up to 5:1 and 7:1). Many grains possess clear ed mean age of 1944.3 ± 6.6 Ma (MSWD = 0.88, N = 35), and an upper core–rim textures with low luminescence rims of variable size ranges intercept age of 1946.2 ± 8.4 Ma (MSWD = 0.51, N = 35), which are suggesting metamorphic overgrowth. Some of these show rounded very close to the 207Pb/206Pb weighted mean age of 1947 ± 7 Ma shapes and complex structure or lacking any obvious internal features. (MSWD = 0.94, N = 29) from the concordia plots (Fig. 15a, b). Twenty six zircon grains were analyzed from sample IM13-18. The Thirty-seven zircon grains were analyzed from sample OY-XH-1B analytical results are listed in Table 4 and plotted in the concordia dia- (Table 3) and the results are plotted in Fig. 15 c, d. The Pb, U and Th gram (Fig. 14a, b). The analytical data show a wide range of Pb (0.00– ranges of the zircons are 8–207 ppm, 15–863 ppm and 2–96 ppm, re- 79%), U (6–88 ppm) and Th (3–72 ppm) with Th/U ratios of 0.37– spectively, with high Th/U ratios of up to 6.77. The data can be divided 1.05. The 207Pb/206Pb spot ages range from 1834 to 1962 Ma and yield into 3 groups: one with an upper intercept age of 2476 ± 31 Ma and 207Pb/206Pb weighted mean age of 1900 ± 15 Ma (MSWD = 0.52, lower intercept age of 1752 ± 61 Ma (MSWD = 0.80, N = 32); the N = 26), close to the upper intercept age of 1909 ± 24 Ma second with 207Pb/206Pb weighted mean age of 2125 ± 18 Ma (MSWD = 0.52, N = 26) (Fig. 14a, b). (MSWD = 1.12, N = 3); the third showing the 207Pb/206Pb weighted Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 97

Fig. 15. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the metagabbro sample IM13-20. Zircon U–Pb concordia plots (c) and age data histograms with probability curves (d) for the metagabbro sample OY-XH-1B. mean age of 1852 ± 19 Ma (MSWD = 0.112, N = 4). These results sug- (OY-XH-11; Table 3) and the results show high Pb content of 162– gest that the metagabbro was emplaced at ca. 2.5 Ga, followed by new 501 ppm (even up to 1305 ppm), U content of 81 to 809 ppm and Th zircon growth (as well as Pb loss in older zircons) during the thermal content of 41 to 180 ppm with high Th/U ratios of 0.62 to 7.63. All the event at 2.1 Ga, and recrystallization during the later thermal events spots define an intercept age of 1902 ± 17 Ma (MSWD = 1.8, N = at ca. 1.85 Ga and ca. 1.75 Ga. 30) which is identical to their 207Pb/206Pb weighted mean age of The prismatic euhedral to subhedral grain morphology, well-defined 1904.4 ± 6.1 Ma (MSWD = 1.6, N = 20) (Fig. 16c, d). Based on the oscillatory zoning, and high Th/U ratios indicate that the zircon grains high Th/U ratios and clear oscillatory zoning of the zircon grains, the from the metagabbros are of magmatic origin. Therefore, their 207Pb/ 207Pb/206Pb weighted mean age of 1.90 Ga is taken to present the timing 206Pb weighted mean ages ranging from 2.5 to 1.9 Ga are interpreted of eruption of the felsic magma. as the emplacement ages followed by metamorphism at ca. 1.85 Ga. The youngest age of 1.75 Ga correlates with the post-collisional thermal event recorded from this region (Yang et al., 2014a). 5.2.5. Khondalite Zircons from the khondalite sample (OY-XH-3A) are markedly 5.2.4. Felsic tuffs smaller in size than those in the charnockite and metagabbros The zircons from felsic volcanic tuffs in the study area (samples OY- (Fig. 12c). Most of them are smaller than 100 μm in length and 50 μm XH-9A and OY-XH-11) are markedly smaller in size (Fig. 12 a, b). Most in width with aspect ratios of 2.5:1 to 1:1, with a few exceptions that of them are smaller than 100 μm in length and 50 μm in width with show length of 100–120 μm, width of 50–80 μm and aspect ratios of aspect ratios of 2:1 to 1:1, with a few exceptions that show length of 2:1 to 1.5:1. The zircon grains show prismatic to stumpy morphology, 100–120 μm, width of 50–80 μm and aspect ratios of 4:1 to 1.5:1. In and some grains are anhedral. In CL images, some of the zircons display CL images, the zircons display very clear oscillatory zoning; some clear oscillatory zoning, and the others are structureless or show core– show rounded shapes, whereas others display prismatic to stumpy rim textures with very thin rims. Twenty spots were analyzed on 20 zir- morphology. con grains (Table 3) and the results show Pb content of 45–395 ppm, U Twenty-eight spots were analyzed on 28 zircon grains (Table 3) and content of 104–435 ppm and Th content of 38–609 ppm and Th/U ratios the results show Pb, U and Th contents in the range of 252 to 441 ppm, of 0.15 to 4.78. From their concordia plots (Fig. 16c, d), the 20 zircons 151 to 259 ppm and 58 to 139 ppm, respectively, with high Th/U ratios can be divided into two groups: the first set including 17 spots defines of 1.58 to 2.98. The data define an intercept age of 1907 ± 17 Ma an intercept age of 2102 ± 76 Ma (MSWD = 3.3, N = 17); the other (MSWD = 1.12, N = 28) which is identical to their 207Pb/206Pb weight- group shows the 207Pb/206Pb weighted mean age of 1881 ± 20 Ma ed mean age of 1901.2 ± 9.6 Ma (MSWD = 2.7, N = 28) (Fig. 16a, b). (MSWD = 1.02, N = 3) (Fig. 17a, b). The ca. 2.1 Ga zircons were evi- Thirty spots were analyzed on 30 zircon grains from the second sample dently derived from magmatic sources and were incorporated into the 98 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

Fig. 16. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the meta-tuff sample OY-XH-9A. Zircon U–Pb concordia plots (c) and age data histograms with probability curves (d) for the meta-tuff sample OY-XH-11. protolith sediments of these rocks, followed by metamorphism as ca. 5.3.1. Metagranite 1.88 Ga. Six zircon grains from sample OY-XH-1A were selected for Lu–Hf isotopic analysis (Table 5). Calibrated to the crystallization age of 5.3. Lu–Hf isotopes 2410 Ma (upper intercept age), the data show low initial 176Hf/177Hf values of 0.281239 to 0. and εHf(t) values of −0.2 to 2.6 (average of

A total of 81 zircon grains were analyzed for Lu–Hf isotopes on the 1.74), Hf depleted mantle model ages (TDM) of 2635 to 2744 Ma and C same domains from where the U–Pb age data were gathered. The results Hf crustal model ages (TDM) of 2774 to 2947 Ma. These results suggest are presented in Table 5 and plotted in Fig. 18. The Lu–Hf data on zircons that the magma source involved Neoarchean juvenile mantle plus limit- from the individual rock types are brieﬂydiscussedbelow. ed reworked older crustal components.

Fig. 17. Zircon U–Pb concordia plots (a) and age data histograms with probability curves (b) for the khondalite sample OY-XH-3A. Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 99

Table 5 In situ Lu–Hf isotopic data of zircons from Xinghe and Jining, North China Craton.

176 177 176 177 176 177 176 177 C No. Age (Ma) Yb/ Hf Lu/ Hf Hf/ Hf 2σ Hf/ Hfi εHf(0) εHf(t) TDM (Ma) TDM (Ma) fLu/Hf OY-XH-1A.4 2410 0.018476 0.0006 0.281346 0.000017 0.281318 −50.4 2.6 2635 2774 −0.98 OY-XH-1A.12 2410 0.025644 0.000800 0.281276 0.000015 0.281239 −52.9 −0.2 2744 2947 −0.98 OY-XH-1A.15 2410 0.019829 0.000635 0.281320 0.000014 0.281291 −51.4 1.6 2673 2834 −0.98 OY-XH-1A.31 2410 0.023801 0.000592 0.281336 0.000017 0.281309 −50.8 2.3 2648 2794 −0.98 OY-XH-1A.35 2410 0.026329 0.000658 0.281330 0.000017 0.281300 −51.0 1.9 2661 2814 −0.98 OY-XH-1A.33 2410 0.023710 0.000585 0.281338 0.000018 0.281311 −50.7 2.3 2645 2790 −0.98 OY-XH-1B.1 2480 0.013095 0.000340 0.281303 0.000018 0.281287 −51.9 3.1 2675 2797 −0.99 OY-XH-1B.2 2480 0.007843 0.000215 0.281304 0.000021 0.281294 −51.9 3.3 2665 2782 −0.99 OY-XH-1B.4 2480 0.011869 0.000310 0.281236 0.000018 0.281222 −54.3 0.8 2762 2939 −0.99 OY-XH-1B.5 2480 0.011696 0.000299 0.281296 0.000021 0.281282 −52.2 2.9 2682 2809 −0.99 OY-XH-1B.8 2480 0.015423 0.000377 0.281269 0.000017 0.281252 −53.1 1.8 2723 2874 −0.99 OY-XH-1B.9 2480 0.011870 0.000295 0.281324 0.000017 0.281310 −51.2 3.9 2643 2746 −0.99 OY-XH-1B.10 2480 0.011761 0.000291 0.281264 0.000021 0.281250 −53.3 1.8 2724 2877 −0.99 OY-XH-1B.11 2480 0.015125 0.000371 0.281247 0.000017 0.281230 −53.9 1.0 2752 2922 −0.99 OY-XH-1B.12 2480 0.020841 0.000473 0.281290 0.000020 0.281267 −52.4 2.4 2702 2840 −0.99 OY-XH-1B.14 2480 0.022316 0.000520 0.281268 0.000020 0.281243 −53.2 1.5 2735 2892 −0.98 OY-XH-1B.15 2125 0.001328 0.000032 0.281555 0.000019 0.281553 −43.1 4.4 2319 2442 −1.00 OY-XH-1B.16 2480 0.009225 0.000230 0.281265 0.000020 0.281255 −53.3 1.9 2718 2868 −0.99 OY-XH-1B.18 2480 0.022825 0.000598 0.281270 0.000020 0.281242 −53.1 1.5 2737 2895 −0.98 OY-XH-1B.19 2480 0.021596 0.000558 0.281287 0.000020 0.281260 −52.5 2.1 2712 2855 −0.98 OY-XH-1B.21 2480 0.019700 0.000524 0.281371 0.000019 0.281346 −49.5 5.2 2596 2668 −0.98 OY-XH-1B.22 2480 0.006377 0.000191 0.281275 0.000018 0.281266 −53.0 2.3 2703 2844 −0.99 OY-XH-1B.23 2480 0.015320 0.000467 0.281276 0.000014 0.281254 −52.9 1.9 2720 2870 −0.99 OY-XH-1B.24 2480 0.017766 0.000571 0.281297 0.000015 0.281270 −52.1 2.5 2699 2833 −0.98 OY-XH-1B.25 2480 0.009365 0.000292 0.281282 0.000015 0.281268 −52.7 2.4 2701 2839 −0.99 OY-XH-1B.26 2480 0.012387 0.000369 0.281319 0.000016 0.281302 −51.4 3.6 2655 2765 −0.99 OY-XH-1B.27 2480 0.015452 0.000492 0.281284 0.000014 0.281260 −52.6 2.1 2712 2855 −0.99 OY-XH-1B.28 2480 0.014839 0.000444 0.281299 0.000015 0.281278 −52.1 2.8 2688 2817 −0.99 OY-XH-1B.31 2480 0.018195 0.000512 0.281326 0.000019 0.281302 −51.1 3.6 2656 2765 −0.98 OY-XH-1B.32 1852 0.009426 0.000251 0.281262 0.000019 0.281253 −53.4 −12.5 2724 3273 −0.99 OY-XH-1B.33 2480 0.011327 0.000300 0.281286 0.000016 0.281272 −52.5 2.6 2695 2830 −0.99 OY-XH-1B.39 2480 0.012231 0.000311 0.281319 0.000023 0.281304 −51.4 3.7 2652 2760 −0.99 OY-XH-1B.40 2480 0.006121 0.000180 0.281290 0.000020 0.281282 −52.4 2.9 2681 2809 −0.99 OY-XH-3A.6 2102 0.021591 0.000703 0.281617 0.000015 0.281589 −40.8 5.1 2274 2378 −0.98 OY-XH-3A.13 2102 0.009722 0.000236 0.281477 0.000016 0.281468 −45.8 0.8 2434 2644 −0.99 OY-XH-3A.30 2102 0.001551 0.000036 0.281540 0.000015 0.281538 −43.6 3.3 2338 2490 −1.00 OY-XH-3A.38 1881 0.001375 0.000024 0.281534 0.000015 0.281534 −43.8 −1.9 2345 2642 −1.00 OY-XH-7A.1 2446 0.032251 0.000951 0.281307 0.000023 0.281263 −51.8 1.4 2712 2871 −0.97 OY-XH-7A.2 2446 0.025880 0.000760 0.281337 0.000024 0.281302 −50.7 2.8 2658 2787 −0.98 OY-XH-7A.3 2446 0.026702 0.000755 0.281302 0.000026 0.281267 −52.0 1.6 2705 2863 −0.98 OY-XH-7A.4 2446 0.012390 0.000363 0.281328 0.000022 0.281311 −51.1 3.2 2643 2766 −0.99 OY-XH-7A.6 2446 0.019596 0.000567 0.281327 0.000024 0.281300 −51.1 2.8 2659 2790 −0.98 OY-XH-7A.8 2446 0.028082 0.000816 0.281379 0.000024 0.281341 −49.3 4.2 2605 2701 −0.98 OY-XH-7A.14 2446 0.019236 0.000689 0.281302 0.000017 0.281269 −52.0 1.7 2701 2857 −0.98 OY-XH-7A.19 2446 0.024234 0.000826 0.281340 0.000020 0.281301 −50.7 2.8 2659 2788 −0.98 OY-XH-7A.21 2446 0.025487 0.000837 0.281313 0.000018 0.281274 −51.6 1.8 2695 2846 −0.97 OY-XH-7A.23 2446 0.021334 0.000637 0.281281 0.000019 0.281251 −52.7 1.0 2726 2897 −0.98 OY-XH-7A.25 2446 0.007606 0.000247 0.281312 0.000019 0.281301 −51.6 2.8 2656 2789 −0.99 OY-XH-7A.26 2446 0.028934 0.000829 0.281310 0.000020 0.281271 −51.7 1.7 2699 2853 −0.98 OY-XH-7A.33 2446 0.030142 0.000888 0.281286 0.000025 0.281244 −52.6 0.8 2737 2912 −0.97 OY-XH-7A.37 2446 0.001409 0.000040 0.281415 0.000015 0.281413 −48.0 6.8 2505 2543 −1.00 OY-XH-7A.46 2446 0.016060 0.000502 0.281244 0.000022 0.281220 −54.1 −0.1 2766 2965 −0.98 OY-XH-7A.47 2446 0.017401 0.000548 0.281372 0.000021 0.281346 −49.5 4.4 2597 2690 −0.98 OY-XH-9A.1 1901.2 0.021225 0.000633 0.281570 0.000015 0.281547 −42.5 −1.0 2334 2600 −0.98 OY-XH-9A.3 1901.2 0.032499 0.000921 0.281558 0.000013 0.281524 −42.9 −1.8 2368 2649 −0.97 OY-XH-9A.15 1901.2 0.018381 0.000541 0.281568 0.000013 0.281549 −42.6 −0.9 2331 2596 −0.98 OY-XH-9A.25 1901.2 0.016691 0.000428 0.281631 0.000016 0.281616 −40.3 1.5 2238 2449 −0.99 OY-XH-9A.34 1901.2 0.026991 0.000626 0.281626 0.000018 0.281603 −40.5 1.0 2257 2476 −0.98 OY-XH-9A.37 1901.2 0.012520 0.000287 0.281589 0.000016 0.281579 −41.8 0.2 2287 2530 −0.99 OY-XH-9A.39 1901.2 0.015761 0.000362 0.281554 0.000016 0.281541 −43.1 −1.2 2339 2613 −0.99 OY-XH-9A.40 1901.2 0.054309 0.001225 0.281628 0.000018 0.281584 −40.5 0.4 2290 2518 −0.96 OY-XH-9A.42 1901.2 0.020438 0.000493 0.281545 0.000016 0.281528 −43.4 −1.6 2359 2642 −0.99 OY-XH-11.1 1904.4 0.016968 0.000439 0.281676 0.000020 0.281660 −38.8 3.1 2178 2349 −0.99 OY-XH-11.21 1904.4 0.008809 0.000222 0.281571 0.000015 0.281563 −42.5 −0.3 2308 2563 −0.99 OY-XH-11.23 1904.4 0.006585 0.000169 0.281569 0.000015 0.281563 −42.5 −0.3 2307 2562 −0.99 OY-XH-11.26 1904.4 0.015831 0.000417 0.281615 0.000015 0.281599 −40.9 1.0 2260 2482 −0.99 OY-XH-11.35 1904.4 0.005974 0.000151 0.281574 0.000014 0.281568 −42.4 −0.1 2300 2550 −1.00 IM13.20.9 1944.3 0.012845 0.000309 0.281562 0.000025 0.281551 −42.8 0.2 2325 2563 −0.99 IM13.20.18 1944.3 0.012276 0.000387 0.281563 0.000017 0.281548 −42.8 0.1 2329 2569 −0.99 IM13.20.19 1944.3 0.019633 0.000613 0.281575 0.000015 0.281553 −42.3 0.2 2325 2559 −0.98 IM13.20.20 1944.3 0.031798 0.000954 0.281567 0.000014 0.281532 −42.6 −0.5 2357 2604 −0.97 IM13.20.23 1944.3 0.023910 0.000707 0.281612 0.000015 0.281586 −41.0 1.4 2281 2486 −0.98 IM13.20.24 1944.3 0.032903 0.000986 0.281593 0.000018 0.281557 −41.7 0.4 2323 2550 −0.97 IM13.20.25 1944.3 0.015838 0.000480 0.281614 0.000016 0.281597 −40.9 1.8 2264 2463 −0.99 IM13.20.29 1944.3 0.013406 0.000394 0.281600 0.000015 0.281585 −41.5 1.4 2279 2488 −0.99

(continued on next page) 100 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105

Table 5 (continued)

176 177 176 177 176 177 176 177 C No. Age (Ma) Yb/ Hf Lu/ Hf Hf/ Hf 2σ Hf/ Hfi εHf(0) εHf(t) TDM (Ma) TDM (Ma) fLu/Hf IM13.20.30 1944.3 0.031810 0.000891 0.281627 0.000018 0.281594 −40.5 1.7 2272 2469 −0.97 IM13.20.31 1944.3 0.028176 0.000781 0.281608 0.000018 0.281580 −41.1 1.2 2290 2500 −0.98 IM13.20.33 1944.3 0.037364 0.000978 0.281691 0.000021 0.281655 −38.2 3.9 2188 2334 −0.97 IM13.20.35 1944.3 0.025671 0.000638 0.281644 0.000018 0.281620 −39.9 2.6 2234 2412 −0.98 IM13.20.36 1944.3 0.012301 0.000291 0.281543 0.000020 0.281532 −43.5 −0.5 2350 2605 −0.99 IM13.20.42 1944.3 0.035306 0.000822 0.281618 0.000019 0.281588 −40.8 1.5 2279 2482 −0.98

5.3.2. Charnockite 5.3.5. Khondalite Sixteen zircon domains were analyzed for Lu–Hf isotopes from sam- Only four zircon domains were analyzed for Lu–Hf isotopes from ple OY-XH-7A (Table 5) where U–Pb age dating was done. Twenty-five sample OY-XH-3A (Table 5) on domains where U–Pb age dating was spots show initial 176Hf/177Hf values of 0.281220 to 0. 281413 and pos- done, due to the small size of the zircon grains. Three spots, calculated itive εHf(t) values of 0.8 to 6.8 (except spot 46 with an εHf(t) value of for the crystallization age of 2102 Ma (upper intercept age), show initial −0.1, mean 2.48), respectively, with Hf depleted mantle model ages 176Hf/177Hf and εHf(t) values of 0.281468 to 0. 281589 and 0.8 to 5.1 C (TDM) of 2505 to 2766 Ma and Hf crustal model ages (TDM)of2543to (mean 3.10), respectively, with Hf depleted mantle model ages (TDM) C 2965 Ma when computed for the upper intercept age of 2446 Ma. The of 2274 to 2434 Ma and Hf crustal model ages (TDM) of 2378 to data from the charnockite suggest that the magma source mainly in- 2644 Ma. The remaining one zircon grain shows initial 176Hf/177Hf and volved juvenile mantle components and limited reworked ancient εHf(t) values of 0.281534 and −1.9, respectively, with Hf depleted C crustal components (Fig. 18). mantle model ages (TDM) of 2345 Ma and Hf crustal model ages (TDM) of 2642 Ma, when calculated for the crystallization age of 1881 Ma. The data from the khondalite suggest that zircons in the sedimentary 5.3.3. Metagabbros protolith were derived from magmas generated through the reworking Fourteen zircon grains were chosen for Lu–Hf isotopes from of older crustal basement, together with the input of juvenile mantle metagabbro sample IM13-20 (Table 5). Corrected to the crystallization components, as in the case of the other magmatic units described ages of 1944.3 Ma, the data show tight range initial 176Hf/177Hf values above (Fig. 18). of 0.281532 to 281655 and dominantly positive εHf(t) values of −0.5 to 3.9 (average of 1.10), respectively, with Hf depleted mantle model C ages (TDM) of 2188 to 2357 Ma and Hf crustal model ages (TDM)of 6. Discussion 2334 to 2605 Ma. Twenty-seven zircon domains were analyzed for Lu–Hf isotopes 6.1. Evidence for Paleoproterozoic arc magmatism in the NCC from sample OY-XH-1B (Table 5). Twenty-five zircon domains were calculated for the crystallization ages of 2480 Ma (upper intercept age), Previous studies have indicated that the earliest arc-related mag- and show initial 176Hf/177Hf and εHf(t) values of 0.281222 to 0. matic event in the TNCO took place at ca. 2.5 Ga ago (e.g., Zhao et al., 281346 and 0.8 to 5.2 (mean 2.54), respectively, with Hf depleted man- 2008; Wilde et al., 2005; and references therein). The magmatism gen- tle model ages (TDM) of 2596 to 2762 Ma and Hf crustal model ages erated both intrusive and extrusive suites that are now distributed C (TDM) of 2668 to 2939 Ma. One zircon domain computed for its crystal- within the low-grade granite–greenstone terranes such as those in the lization age of 2125 Ma, shows an initial 176Hf/177Hf value of 0.281553 Wutai granite–greenstone belt. According to Wang et al. (2004) the ma- and εHf(t) value of 4.4 with Hf depleted mantle model ages (TDM)of jority of 2530–2515 Ma mafic volcanic rocks in the Wutai Group were C 2319 Ma and Hf crustal model ages (TDM) of 2442 Ma. The other zircon derived from arc-type basalts. Kröner et al. (2005a,b) suggested that domain yields an initial 176Hf/177Hf value of 0.281253 and εHf(t) value the 2520–2445 Ma TTG gneiss in the Hengshan and Fuping terranes of −12.5 with Hf depleted mantle model ages (TDM) of 2724 Ma and were modified by subduction components, and that the wide range in C Hf crustal model ages (TDM) of 3273 Ma, when calculated for its crystal- SiO2 content, high Na2O, Ba, and Sr and low Y and HREE, and the selec- lization age of 1852 Ma. tive enrichment in LILE and depletion in Nb, Ta and Ti correlate with The data from the metagabbros suggest that the magma source in- mantle-derived magmatic precursors. Wan et al. (2000) and Geng volved a mixture of juvenile mantle input and reworked ancient crustal et al. (2000) showed that the 2199–2173 Ma Chijianling–Guandishan components (Fig. 18), typical of continental arc magmatism. gneisses are characterized by calc-alkaline signature and have arc affinities. The Paleoproterozoic magmatic event is also widely represented in

5.3.4. Felsic tuff A total of nine zircons were analyzed for Lu–Hf isotopes from sample OY-XH-9A (Table 5). The data show initial 176Hf/177Hf and εHf(t) values of 0.281524 to 0. 281616 and −1.8 to 1.5 (mean −0.37), respectively, and Hf depleted mantle model ages (TDM) of 2238 to 2368 Ma and Hf C crustal model ages (TDM) of 2449 to 2649 Ma, when calculated at the crystallization age of 1901 Ma. Five zircon domains were analyzed for Lu–Hf isotopes from sample OY-XH-11 (Table 5). When calculated at the crystallization age of 1904 Ma, the data yield initial 176Hf/177Hf and εHf(t) values of 0.281563 to 0. 281660 and −0.3 to 3.1 (average of 0.7), respectively, with Hf depleted mantle model ages (TDM)of C 2178 to 2308 Ma and Hf crustal model ages (TDM) of 2349 to 2563 Ma. The data from felsic tuffs suggest that the magma source involved mainly juvenile mantle and reworked ancient crustal Fig. 18. εHf(t) versus 207Pb/206Pb mean age diagram of zircons from the metagranite, components (Fig. 18). charnockite, gabbros, meta-tuffs and khondalite. Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 101 other complexes in the TNCO including the Zhongtiao Complex from subducted oceanic lithosphere and influx of fluid mobile elements into where Sun et al. (1992) reported a single-grain zircon age of 2321 ± the mantle wedge through metasomatic processes (Manikyamba 2 Ma in granitoid gneiss, and from the Hengshan Complex from where et al., in press). The moderate REE fractionation trends might suggest Kröner et al. (2005a,b) identified granitoid emplacement between a heterogeneous source marked by subduction-derived arc components 2360 Ma and 2330 Ma. Zhao et al. (2008) reported SHRIMP zircon U– with minor input from continental crust. The geochemical features of Pb ages from tonalitic, granodioritic and monzogranitic plutons from the magmatic suite are consistent with their derivation in a continental the Chijianling–Guandishan gneisses which show emplacement ages arc related to an active continental margin, similar to the features of 2199 ± 11 Ma, 2180 ± 7 Ma and 2173 ± 7 Ma, respectively. Granitoid displayed by the arc magmatic suite in the Paleoproterozoic Lüliang gneisses of similar ages have also been reported from other complexes Complex within the TNCO (Liu et al., 2010; Liu et al., 2012). in the TNCO such as the Hengshan Complex with magmatic pulses at Among the two compositional varieties of charnockites as ferroan 2200–2100 Ma (Kröner et al., 2005a), and the Nanying granitoids of and magnesian (Frost and Frost, 2008; Rajesh and Santosh, 2012), the the Fuping Complex with ages of 2109 ± 5 Ma, 2097 ± 6 Ma and charnockite of the present study classifies as magnesian variety. Magne- 2097 ± 46 Ma (Guan et al., 2002; Zhao et al., 2002). Paleoproterozoic sian charnockites are in general considered to have formed in a granitoids in the low-grade Wutai Complex represented by the subduction setting (e.g. Rajesh, 2012; Santosh et al., 2013a). In Fig. 7c, Dawaliang pluton (2176 ± 12 Ma) and the Wangji-ahui pluton the charnockites from the NCC including the present study and those re- (2117 ± 17 Ma, 2116 ± 16 Ma and 2084 ± 20 Ma) are other examples ported in previous works (Ma et al., 2013; Yang et al., under review)are (Wilde et al., 2005). Zhao et al. (2008) and Liu et al. (2012) presented U– characterized by medium-K content, and calc-alkaline, metaluminous Pb zircon data from various units in the Lüliang Complex at the western affinities. The compositional characteristics of the magnesian margin of the TNCO. The TTG gneisses with calc-alkaline chemistry and charnockite including the medium K contents and positive zircon εHf magmatic arc affinity in this complex were emplaced at ca. 2.5 Ga, values (0.8 to 6.8, average 2.48, except one plot with an εHf value of representing the earliest arc-related magmatic event, followed by arc- −0.1) are consistent with magma generation from juvenile sources in related magmatic pulses as 2.4 and 2.2 Ga. Metamorphism associated arc setting. The presence of Neoarchean and Paleoproterozoic arc com- with collision occurred at ca. 1.87 Ga. Subsequently, a series of post col- ponents associated with the subduction–accretion history has been lisional granitoids including porphyritic granite, charnockite, and mas- widely identified in the NCC (e.g., Zhai and Santosh, 2011; Santosh sive granite were emplaced during 1.83 to 1.79 Ga. Liuetal.(2012) et al., 2013a; Yang et al., 2014a). The geochemical features of the mag- reported geochemical and zircon U–Pb data from metavolcanic units nesian charnockites including their immobile trace element-based tec- in the Yejishan and Lüliang groups of the Lüliang Complex which illus- tonic discrimination plots (Fig. 8) are also consistent with subduction- trate active continental margin arc magmatism at 2.2 Ga, followed by related arc signature. metamorphism during 1.90–1.83 Ga associated with the collisional The volcanic tuffs in our study are compositionally similar to event, and post-collisional extension at 1.80 Ga. rhyodacites and dacites. The formation of rhyolitic rocks in an active Paleoproterozoic magmatism has also been reported from the continental margin can occur through: (i) direct melting of basalt pro- southern margin of the NCC. Zhou et al. (2014) investigated potassic ducing extremely fractionated REE patterns and high Al2O3;(ii)a granites from the Lushan area and reported zircon U–Pb ages of 2.2 Ga single-stage melting of a sialic source resulting in an LREE-enriched liq- C and zircon εHf(t) values of −2.4 to +7.3 with TDM varying between uid; and (iii) fractional crystallization of a basaltic magma giving rise to 2848 and 2306 Ma. Although these authors favored intra-continental alowK2O rhyolitic melt (Edwards and Hodder, 1991; Manikyamba rifting for the magma genesis, when we replotted their geochemical et al., 2012). The medium to low K2O contents (2.04–2.27 wt.%), and data in relevant discrimination diagrams, a distinct volcanic arc granite moderate Al2O3 (12.01–13.54 wt.%) contents, and limited fraction of affinity is revealed, suggesting arc magmatic affinity and subduction- LREE/HREE suggest that these rocks might have been derived by the related setting at ca. 2.2 Ga. fractional crystallization of basaltic magma. The majority of zircons in The suite of granitoids, charnockites, gabbros, felsic volcanic tuffs these rocks display positive εHf(t) values (up to 3.1), suggesting domi- and khondalites reported in our study from the Xinghe and Jining nantly juvenile source, with limited input from reworked crustal areas along the junction between the IMSZ and the TNCO, two of the sources. Their petrogenetic features are consistent with formation in major subduction–collision zones in the NCC, suggest prominent an active continental margin arc environment. In a recent study, Dan arc magmatic and related felsic volcanic episodes associated with et al. (2012) reported the results of SIMS U–Pb age and Hf–O isotopes Paleoproterozoic convergent margin tectonics in the NCC. Similar arc in detrital zircons from khondalites and associated granitoid suite of magmatic suites of charnockite–granite–gabbro–felsic tuff association the Helanshan Complex in the westernmost part of the Khondalite have been reported from several regions elsewhere on the globe includ- Belt within the IMSZ. Their study suggested that the protoliths of the ing the Mesoarchean Coorg Block (Santosh et al., 2013a) and the Helanshan khondalites were sourced from a provenance that witnessed Neoarchean Nilgiri Block (Praveen et al., 2013; Samuel et al., 2014)in prolonged, episodic magmatism of ca. 2.18 Ga, 2.14 Ga, 2.09 Ga, 2.06 Ga, southern India, formed in subduction-related active continental margin 2.03 Ga and 2.00 Ga. The εHf(t) values show a range of +8.9 to −2.9 C settings. and Hf TDM model ages between 2.8 and 2.1 Ga. The zircon Hf–O isotopic The salient geochemical features of these rocks are also suggestive of data (with δ18O peaks at 6.6‰ and 8.2‰) indicate that both juvenile and subduction-related arc magmatic settings. In the Zr/TiO2 verse SiO2 dia- ancient crustal components were involved in their source rocks. Dan gram (Fig. 6b), the khondalites and felsic tuffs show rhyodacite to dacite et al. (2012) therefore concluded that the protoliths of the Helanshan compositions, similar to felsic volcanic rocks in active continental mar- khondalite were sourced from a ca. 2.18–2.00 Ga continental arc within gins. In the Zr–Y diagram, all the rocks are plotted in the area of calc- an active continental margin. The volcanic tuffs reported in our study alkaline to tholeiitic affinities (Fig. 7a), typical of rock suites formed in with ca. 1.9 Ga magmatic zircons characterized by dominantly positive continental arcs in other Precambrian terranes (e.g., Santosh et al., εHf(t) values compare with the data from Helanshan khondalites re- 2013b). In the Y–Nb diagram (Fig. 8a), the majority of these rocks are ported by Dan et al. (2012), and might define the latest phase of conti- plotted in the VAG + syn-COLG, and in the Y + Nb vs. Rb diagram, nental arc volcanism prior to the cessation of subduction and final they fall in the VAG area (Fig. 8b). In the Nb/Zr vs. Zr diagram, all the collision in the NCC. plots fall in the field of rocks generated in subduction setting (except one metagabbroic rock IM13-18; Fig. 8c). The trace element distribution 6.2. Tectonic implications patterns (Fig. 9) are broadly consistent with magma processes and in convergent settings. The LILE and LREE enrichment in the majority Our zircon U–Pb geochronological data show new zircon growth samples and relative HFSE depletion might suggest dehydration of during multiple tectonothermal events as inferred from 207Pb/206Pb 102 Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 weighted mean ages of 2410 ± 41 Ma for the metagranite, 2480 ± 1.85–1.80 Ga. The magmatic pulses continued during the post- 12 Ma and 2125 ± 18 Ma from metagabbro sample OY-XH-1B, collision extension at 1.78 to 1.68 Ga. 1946 ± 8 Ma, 1900 ± 15 Ma and 1879 ± 12 Ma from metagabbro sam- In Fig. 19, we compile the major Paleoproterozoic magmatic record ples IM13-20, IM13-18 and IM13-19 respectively, 2446 ± 11 Ma from in the IMSZ and the TNCO. In the Helanshan area of IMSZ, the continen- the charnockite, and 1904 ± 6 Ma and 1901 ± 9 Ma for metatuffs. tal arc volcanics (khondalites) show magmatic ages of 2.18–2.00 Ga The 207Pb/206Pb upper intercept age of zircons in the khondalite (Dan et al., 2012). In the Halaqin area, the volcanic rocks yield magmatic shows 2102 ± 76 Ma which is identical to the age obtained from the ages of 1.90 Ga (Peng et al., 2011). In the Wulashan–Daqingshan area, magmatic zircons in one of the metagabbros (OY-XH-1B). The the meta-mafic rocks show multiple magmatic ages of 2.50–2.45 Ga, khondalites also carry a group of concordant metamorphic zircons 2.30–2.10 Ga and 1.97–1.93 Ga (Wan et al., 2013; Liu et al., 2014). In with 207Pb/206Pb mean age of 1881 ± 20 Ma. Metamorphic zircons in the Tuguiwula area, the timing of mafic magmatism age is constrained the gabbros and charnockites also yield similar metamorphic ages of as 1.96–1.92 Ga (Peng et al., 2010). In the present study, our data from 1890 ± 14 Ma and 1852 ± 19 Ma, respectively. The age data suggest granitoids, charnockite, gabbro, felsic volcanic tuffs and khondalite prolonged arc magmatism in a convergent margin setting during ca. show magmatism between 2.48 and 1.9 Ga in the Jining and Xinghe 2.48 to 1.9 Ga, followed by metamorphism at ca. 1.89–1.85 Ga associat- areas. In the Xuanhua and Huai'an complexes, the TTG gneisses show ed with the final collision. Lu–Hf analyses reveal that the dominant pop- the magmatism ages of 2.52–2.47 Ga (Guan et al., 2002; Kröner et al., ulations of zircons from all the rock types are characterized by positive 2005a,b). In the Hengshan complex, the various rock types show multiple εHf values (−1.9 to 6.8; mean 1.8; except one spot with the εHf value magmatic ages of 2.52–2.44 Ga, 2.36–2.33 Ga, 2.2–2.1 Ga (Kröner et al., C of −12.5) (Fig. 19,Table3).TheεHf and TDM data suggest that the 2005a,b). In the Wutai complex, major magmatic pulses occurred at magmas were mostly derived from Neoarchean and Paleoproterozoic 2.53–2.51 Ga and 2.35–2.08 Ga (Wang et al., 2004; Wilde et al., 2005; juvenile components. Wei et al., 2014), similar to the ages (2.52–2.44 Ga, 2.35–2.00 Ga) in the Based on a global evaluation of Paleo-Mesoproterozoic magmatic Fuping and Zanhuang complexes (Guan et al., 2002; Zhao et al., 2002; arcs, Zhao et al. (2008) identified a major arc magmatic zone extending Deng et al., 2013; Wei et al., 2014). In the Lüliang Complex, the granitoids from Arizona, through Colorado, Michigan, southern Greenland, Scot- were emplaced at 2.50 Ga, 2.37 Ga and 2.20–2.17 Ga (Zhao et al., 2008). land, Sweden and Finland, to western Russia, bordering the present The early Proterozoic Era, termed as the Siderian interval (2.5 to southern margin of North America, Greenland and Baltica (e.g., Gower 2.3 Ga, Plumb, 1991) has been considered as a relatively quiescent peri- et al., 1990; Karlstrom et al., 2001; Zhao et al., 2008). This zone was cor- od of juvenile magmatism as tracked from detrital zircon record (Condie related to subduction-related episodic outgrowth along the continental et al., 2009). The magmatic quiescence has been correlated to plate tec- margin of the supercontinent Columbia (Zhao et al., 2008; and refer- tonic shutdown following widespread lithospheric stagnation and man- ences therein). tle overturn (Condie, 1998; Condie et al., 2009). However, recent studies The results presented in this study, together with those from previ- (Pehrsson et al., 2013, 2014) have revealed prominent record of orogen- ous investigations in different domains of the IMSZ and TNCO suggest esis in cratons and cratonic fragments from various parts of the world major Paleoproterozoic arc magmatic events in the NCC lasting for near- during the Siderian quiet interval. Examples include the 2.5–2.43 Ga ly 600 million years associated with the final assembly of the crustal Sleafordian of South Australia, the 2.49–2.43 Ga subduction–accretion blocks into a coherent craton. Similar age spans have been observed in orogens along the southern margin of the Dharwar craton in India, the some of the major orogenic belts that went through prolonged 2.45–2.4 Ga Selway terrane in NW Wyoming, the 2.45–2.35 Ga subduction–accretion–collision history, such as the Central Asian Arrowsmith of Arctic Canada, and the 2.35–2.30 Ga Borborema province Orogenic Belt (e.g., Xiao and Santosh, 2014). The final cratonic archi- of Brazil, among other examples (Pehrsson et al., 2014). As discussed tecture of the NCC thus witnessed not only the arc–continent amal- above, the North China Craton preserves excellent records of early gamations at 2.7–2.5 Ga (e.g., Zhai and Santosh, 2011; Geng et al., Paleoproterozoic arc magmatic events in several locations along the 2012), but also major crust building events in the Paleoproterozoic IMSZ and the TNCO suggesting vigorous plate tectonic processes along through juvenile and recycled components in continental magmatic active convergent margins. Our results thus confirm the view of arc systems along active convergent margin, followed by intense Pehrsson et al. (2014) and suggest that there was no global plate tecton- deformation and metamorphism during the final collision stage at ic shutdown during the Siderian quiet interval.

Fig. 19. Tectonic framework of the central and northern parts of the North China Craton showing a compilation of the Paleoproterozoic ages from magmatic suites in the Inner Mongolia Suture Zone and the Trans-North China Orogen. See text for discussion and related references. Q.-Y. Yang, M. Santosh / Gondwana Research 28 (2015) 82–105 103

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It also contributes to the Talent grade rocks: implications for Palaeoproterozoic tectonothermal evolution of the – Award to M. Santosh under the 1000 Plan from the Chinese Govern- Khondalite Belt, North China Craton. Precambrian Research 237, 78 100. Karlstrom, K.E., AHall, K.I'., Harlan, S.S., Williams, M.L., McLelland, J., Geissman, J.W., 2001. ment. We thank Xueming Teng for his help during field work and anal- Long-lived (1.8–1.0 Ga) convergent orogen in southern Laurentia, its extensions to yses. We also thank Jianzhen Geng (Tianjin Institute of Geology and Australia and Baltica, and implications for refining Rodinia. Precambrian Research – Mineral Resources), Hangqiang Xie and Prof. Alfred Kröner (Beijing 111, 5 30. Kröner, A., Wilde, S.A., Li, J.H., Wang, K.Y., 2005a. 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