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Research 21 (2012) 517–529

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Gondwana Research

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Growth and reworking of the early in the North Craton: Constraints from zircon Hf isotopes

Yuansheng Geng ⁎, Lilin Du, Liudong Ren

Institute of Geology, Chinese Academy of Geological Sciences, 100037, PR China article info abstract

Article history: We synthesize more than 2600 Hf isotope data on the Archean-Paleoproterozoic zircons from the North China Received 28 September 2010 Craton (NCC). Recalculation of the data based on single stage and two-stage Hf model ages of the Eastern Received in revised form 3 July 2011 Block of the NCC shows peak ages of 3902±13 Ma and 3978 ±18 Ma, respectively, and also small peaks at Accepted 3 July 2011 3.5–4.0 Ga. The majority of zircon ε (t) values are positive, suggesting the possibility of the crust and the Available online 18 July 2011 Hf differentiation at ca. 3.9–4.0 Ga in the Eastern Block of the NCC. Most magmatic zircons from the whole of NCC have their Hf model age range of 2.4–2.9 Ga, and the single stage model ages is cluster at 2698 ±4 Ma, Keywords: Zircon Hf isotope geochemistry whereas the two-stage model ages concentrate at 2714±5 Ma, implying that the protoliths were juvenile Crustal growth crustal rocks. The most prominent peak at 2.7 Ga indicates that this period marks the most important stage of Crustal reworking the crust-mantle differentiation and crust formation of the NCC. The widespread 2.5 Ga rocks in the NCC and Crust–mantle differentiation the absence of the 2.5 Ga peaks in Hf model ages are consistent with the partial melting and reworking of the Tectonics juvenile rocks at 2.5 Ga. Furthermore, the 2.5–1.7 Ga zircon Hf isotope features are also related to the reworking of the crustal rocks. Our results from the integration of a large database suggest that the Eastern Block and the Trans-North China Orogen have undergone similar crust-mantle differentiation and magmatism, leading to the conclusion that the essential cratonization of the North China took place at the end of Neoarchean. © 2011 Published by Elsevier B.V. on behalf of International Association for Gondwana Research.

1. Introduction In the northern hemisphere, the (Beakhouse et al., 1999; Henry et al., 2000; Polat and Kerrich, 2000, 2002; Polat and Early Precambrian was a crucial stage for continental growth in our Münker, 2004; Percival et al., 2006), the western Canadian Shield planet. As the growth rate of the continental crust in the early (Sandeman et al., 2006), the Wyoming Greenstone Belt (Rino et al., Precambrian was significantly higher than that in the late Precam- 2004, 2008), the Baltic Shield (Ohlander et al., 1987; BibiKova et al., brian, 50%–80% (in mass) of the present on the were 2005; Samsonov et al., 2005) and western Greenland Craton (Friend formed during 2800–2500 Ma (Moorbath, 1977; O'Nions et al., 1979). and Nutman, 2005; Steenfelt et al., 2005; Garde, 2007; Polat et al., Updated data show that the proportion of continents grown during 2008, 2011), and in the southern hemisphere the South and the period 3.0–2.5 Ga comprises 36%, and at 2.15–1.65 Ga is 39% of the Zimbabwe Cratons (Kröner et al., 1999; Matthew et al., 1999; Hofmann present crust (Condie, 1998). Since the major continental et al., 2004) and the Pilbara and Yilgarn Cratons in western growth occurred in the early Precambrian, the continent growth (Bateman et al., 2001; Rasmussen et al., 2005), all record a significant styles, stages and interactions between the crust and mantle have influence of the ca 2.7–2.8 Ga event responsible for the rapid formation remained topics of debate (McCulloch and Wasserburg, 1978; of the continent crusts in the Archean. However, in the North China Depaolo et al., 1991; McCulloch and Bennett, 1994; Stein and Craton, this tectonothermal event has only been locally demonstrated Hofmann, 1994; Condie, 1998; 2000; Condie et al., 2009). (Cao, 1996; Zhuang et al., 1997; Jahn et al., 1988; Du et al., 2003; Lu Some workers have suggested that continental growth in the early et al., 2008; Wan et al., 2011; Zhai and Santosh, 2011). Instead, the ca. Precambrian occurred during three periods, 3.6 Ga, 2.7 Ga and 1.8 Ga 2.5 Ga tectonothermal event was demonstrated to be widespread in (McCulloch and Bennett, 1994), whereas some others suggested that the whole craton through zircon U–Pb dating (Kröner et al., 2005a, the principal growth of continental crust occurred at 2.7 Ga, 1.9 Ga and 2005b; Shen et al., 2005; Wilde et al., 2005; Geng et al., 2006a, 2006b, 1.2 Ga (Condie, 1998; 2000). On a global perspective, the 2.7–2.8 Ga 2010; Yang et al., 2008; Grant et al., 2009; Liu et al., 2011a, 2011b; tectonothermal event was indeed important for the continent growth. Wang et al., 2011). The Sm–Nd isotope features of whole rocks from the NCC have revealed that the crust differentiation from the mantle of the NCC occurred prior to the ca 2.5 Ga tectonothermal event. The Nd fi ⁎ Corresponding author. isotope depleted mantle model ages (TDM) of 249 ma c rock samples E-mail address: [email protected] (Y. Geng). show a range from 4.4 Ga to 1.6 with a peak at 2.6–3.0 Ga, suggesting

1342-937X/$ – see front matter © 2011 Published by Elsevier B.V. on behalf of International Association for Gondwana Research. doi:10.1016/j.gr.2011.07.006 518 Y. Geng et al. / Gondwana Research 21 (2012) 517–529 that the most important crust-forming stage of the NCC occurred at convenience of discussion, this paper adopts the classification for the 2.6–3.0 Ga. The peak value of the Nd isotopic depleted mantle model NCC of Zhao et al. (2001, 2005) into the eastern and western blocks ages (TDM) for the 91 samples of TTG (tonalite–trondhjemite– dissected by the Trans North China Orogen. However, it must be noted granodiorite) gneisses stands at 2.6–2.8 Ga, reflecting a crustal that the Western Block itself is composed of two distinct crustal units, retention age of the parental rocks for the TTG gneisses (Lu et al., the Yinshan and Ordos Blocks which were sutured along the Inner 1996). More than 500 basic and acid magmatic rocks of the NCC show Mongolia Zone as identified in recent studies (Santosh, 2010;

Nd isotope depleted mantle model ages (TDM) peaking at 2.82 Ga, Santosh et al., 2010). representing the extraction time of the parent from the mantle to form the continental crust (Wu et al., 2005a). 2.1. The Eastern Block The tectonothermal event determined through zircon U–Pb ages is different from the time assigned for the mantle and crust differen- The Eastern Block includes in turn -Jinan, -, tiation of the NCC based on whole rock Sm–Nd method. There are two Jianping-, Jidong-Miyun, Luxi, Yishui and Jiaodong metamorphic possibilities for the discrepancy. One is that there was an actual time terrains from north to south (Fig. 1). The large dataset on zircon U–Pb gap between the tectonothermal and the crust–mantle differentiation ages demonstrates that the metamorphic terrains of the Eastern Block events, and the tectonothermal event is later than the crust–mantle are predominantly composed of the TTG gneisses formed in late differentiation. The other possibility lies in the problems with using Neoarchean (Fig. 2). Minor supracrustal rocks are also present as diverse isotope systems. U–Pb analysis is from zircon, while Sm–Nd bands, pods and enclaves within the TTG gneisses, such as measurement of whole rock in which the Sm–Nd isotope system may metamorphosed mafic volcanics, sediments and banded iron forma- be reset to some extent due to later metamorphic events. With the tions (BIF). In Luxi (western Shandong Province) metamorphic rocks development of the MC-ICP-MS technique (Halliday et al., 1998; are exposed in the early Neoarchean (2.8–2.65 Ga) metamorphic Albarede et al., 2004), we can simultaneously make in-situ measure- volcano-sedimentary formations of the Taishan Complex and are ment of both U–Pb and Lu–Hf isotopes on the same zircon grain. It is strongly deformed together with the TTG gneisses (2.75–2.65 Ga) also possible to measure the U–Pb age of zircon through SHRIMP (Jahn et al., 1988; Polat et al., 2006b; Lu et al., 2008). Some of the technique at first and then analyze the Lu–Hf isotope with MC-ICP-MS metamorphic terrains of the Eastern Block underwent granulite grade method on the same grain (Wu et al., 2007). Since both the U–Pb age metamorphism in late Neoarchean, such as the Jidong-Miyun, Liaoxi and Hf isotope may be obtained simultaneously or successively on the and Yishui, while the other terrains display chiefly amphibolite facies same zircon grain, it is possible to directly and effectively discuss the metamorphism. relationship of the differentiation event and the tectonothermal In the Anshan-Benxi metamorphic terrain of the Eastern Block, event. In addition, due to the rather low Lu/Hf value of zircon some Eoarchean–Paleoarchean supracrustal relicts are exposed, the (176Lu/177Hf usually less than 0.002), the 176Hf formed through decay major outcrops are the banded trondhjemite (3811±4 Ma) at of 176Lu is extremely low. Thus the 176Lu/177Hf ratio of zircon may be Dongshan in Anshan City (Song et al., 1996), mylonitized trondhjemite regarded as the value when zircon initially formed and can provide (3804 Ma) at Baijiafen (Liu et al., 1992), fine-grained trondhjemite important information on the origin of zircon grains (Patchett et al., (3800±5 Ma), metamorphosed quartz diorite (3794±4 Ma) at Dong- 1981; Knudsen et al., 2001; Kinny and Mass, 2003; Wu et al., 2007). shan, banded trondhjemite (3791±9 Ma and 3777±13 Ma) and More than 2600 Hf isotope data have been reported in recent studies biotite schist (3723±17 Ma) (Liu et al., 2008) and banded trondhjemite on zircons from the NCC. Combining with the isotope ages of zircons, (3680±19 Ma) (Wan et al., 2005; Liu et al., 2007a, 2008). The we discuss the early Precambrian growth and reworking of the Geochronological data indicate that most of the magmatic activity at continental crust of the NCC in the paper. this stage occurred at 3800 Ma, some continued to ca 3680 Ma. The magmatism was predominated by trondhjemite, with minor quartz 2. Regional geological background diorite, suggesting the Na-rich feature. The Chentaigou supracrustal rocks (3.3–3.4 Ga) were also formed at this period (Song et al., 1996). Together with the Tarim and South China, the North China Craton is In addition to the exposures of the Eo- to Paleoarchean (3.8– among the three major cratons in China and covers an area of 3.2 Ga) rocks in the Anshan-Benxi metamorphic terrain, some spots of 1,500,000 km2 in central and northern China (Wu et al., 2005a). To Eoarchean rocks may be present in the Eastern Block, such as the the north of the craton is the late Paleozoic Tianshan-Mongol-Xing'an enclave of acid granulite in the Mesozoic volcanic breccia in Xinyang orgoen, to the southwest is the early Paleozoic Qilian orogen, to the , Henan Province. Two samples of the enclave yield upper south is the Qingling-Dabie-Sulu orogen (UHP belt), and to the intercept zircon ages of 3670±120 Ma and 3655±100 Ma through southeast is the Yangtze Block of the . The evolution SIMS method (Zheng et al., 2004, 2008; Zheng, 2005). The Hf isotopic of the NCC and its tectonics is still debated. Early researchers proposed ratios of the samples are slightly lower than those of Eastern Hebei that the NCC was formed through successive growth of the continental and Anshan and their model age reaches ca. 4.0 Ga. It can be nuclei in the Archean (Ma et al., 1963; Jiang, 1986; Xie et al., 1986). Other inferred that the regions may host the oldest crustal rocks of the NCC workers advanced the concept of microplate amalgamation (Bai et al., (Wu et al., 2005b). 1993; Wu et al., 1998; Zhai and Bian, 2000; Zhai et al., 2005; Zhai and Peng, 2007). Despite the various controversies, most workers consid- 2.2. The Trans-North China Orogen ered that the NCC was resulted from microplate amalgamation in the Neoarchean. Some of the recent studies stressed the importance of the The Trans-North China Orogen covers, from north to south, the collision between the Eastern and Western blocks along the Trans-North Chengde-Huai'an, Hengshan, Wutai, Fuping, Zanhuang, Lüliang, China Orogen (e.g., Zhao et al., 2001; Santosh, 2010; Zhai and Santosh, Zhongtiao and Dengfeng metamorphic terrains, which consist 2011). The delineation of the Trans-North China Orogen (TNCO) and the predominantly of late Neoarchean TTG gneisses (Fig. 3) and minor polarity and timing of collision are also debated (Santosh, Neoarchean volcano-sedimentary sequence. Paleoproterozoic volca- 2010). Some workers proposed a NEE strike for the TNCO with nic-sediments are exposed in the Zhongtiao, Lüliang, Fuping, subduction from SE to NW and collision at 2.5 Ga (Li et al., 2002; Zanhuang and Wutai metamorphic terrains: the Hutuo Group in the Kusky and Li, 2003; Polat et al., 2005, 2006a; Faure et al., 2007; Kusky et Wutai terrain, the Yejishan and Lanhe Groups in the Lüliang terrain, al., 2007; Trap et al., 2007), whereas others suggested that the TNCO the Wanzi Group in the Fuping and Gantaohe Group in the Zanhuang trends NNE with subduction from NW to SE, and final amalgamation at terrains. Late Paleoproterozoic granites are sporadically distributed ca. 1.85 Ga (Kröner et al., 2005a; Zhao et al., 2005; Trap et al., 2007). For from Chengde-Huai'an terrain in the north to the Dengfeng terrain in Y. Geng et al. / Gondwana Research 21 (2012) 517–529 519

Fig. 1. Schematic map showing the distribution of metamorphic basements and tectonic subdivision of the North China Craton (after Zhao et al., 2005). Abbreviations of metamorphic basements in the figure: CD—Chengde, DF—Dengfeng, EH—Jidong (eastern Hebei Province), ES—Jiaodong(eastern Shandong Province), FP—Fuping, HA—Huai'an, HL— Helanshan Mountains, HS—Hengshan Mts., JN—Jining, LL—Lüliang Mts., MY—Miyun, NH—Jibei (northern Hebei Province), NL—Liaobei (northern Province), SJ—Jinan (southern Province), SL—Liaonan (southern Liaoning Province), TH—Taihua, WD—Wula-Daqing Mts., WL—Liaoxi (western Liaoning Province), WS—Luxi (western Shandong Province), YS—Yishui, WT—Wutai Mts., XH—Xuanhua, ZH—Zanhuang, ZT—Zhongtiao Mts.

the south, and these granites display potassic composition and syn- underwent multiple stages of deformation and metamorphism and is a orogenic tectonic setting (Geng et al., 1997, 2006b; Guo et al., 2002; very complex tectonic zone. Guo et al., 2005; Tian et al., 2006; Liu et al., 2007b; Wan et al., 2008; Zhao et al., 2008a, 2008b). In the Chengde, Huai'an and Hengshan 2.3. The Western Block terrains at the northern section of the Trans-North China Orogen, high pressure basic granulites are sporadically distributed (Zhai et al., This block is composed of the Ordos block, khondalite belt and 1993; Mao et al., 1999; Guo et al., 2001, 2005; O'Brien, et al., 2005). Yinshan block (Zhao et al., 2005; Santosh et al., 2007a,b). Recent Recently, meta-volcanics and dioritic gneisses of 2829–2845 Ma, with studies identify the khondalite belt as a collisional suture between the metamorphic ages of ca.2.77 Ga, were reported at Lushan County in Yinshan and Ordos Block and redefined the belt as the the Dengfeng metamorphic terrain (Liu et al., 2009a). The grade of Suture Zone (Santosh, 2010; Santosh et al., 2010). The Ordos block is metamorphism varies in different terrains. Upper amphibolite– mostly covered by Mesozoic to Cenozoic cover sequence and inferred granulite facies metamorphism occurred in the Chengde-Huai'an, as the metamorphic basement based on geophysical data (Wu et al., Hengshan and Fuping terrains, while greenschist-amphibolie facies 1998; Zhu and Zheng, 2009). The Yinshan block consists of the metamorphism is recorded in the Wutai, Lüliang, Zhongtiao and Neoarchean Wulashan Complex, Sertengshan Group and various Dengfeng terrains. Based on the substantial difference in the orthogneisses which include tonalitic, granodioritic and dioritic metamorphic conditions and rock compositions, some researchers gneisses, charnockites, hornblende adamellites and hornblende called the former as high grade gneiss domain and the latter as the granites. Among these, some diorites and quartz diorites have high granite-greenstone belt (Zhao et al., 2000, 2001). contents of MgO, Cr and Ni, with MgO=2.46–9.11 wt.%, Mg#=0.57– As described above, the components of the Trans-North China Orogen 0.59, and mean abundance of Cr and Ni of 256 ppm and 166 ppm. are rather complex. Minor late Mesoarchean volcanics and dioritic These features suggest enrichment in Mg, Cr and Ni of the Mg-rich gneisses and widespread late Neoarchean TTG gneisses and volcano- diorite and can be compared with sanukite (Jian et al., 2005). The sedimentary formations, and many outcrops of late Paleoproterozoic khondalite belt is sandwiched between the Yinshan block in the north granites are present. As to the grade of metamorphism, some terrains are and the Ordos block in the south and stretches from the Helan Mts- high grade domains, and high pressure basic granulites occur in the Qianli Mts in the west, through the Daqingshan Mts to Jining City in northern segment of the granite-greenstone belt. The central zone the east. The belt is dominated by high grade aluminous gneisses and 520 Y. Geng et al. / Gondwana Research 21 (2012) 517–529

Fig. 2. Diagram showing zircon U–Pb isotopic ages and lithologic features of late Neoarchean to Paleoproterozoic orthogneisses from the Eastern Block (after Geng et al., 2010). a— Liaobei-Jinan metamorphic terrain, b—Liaoxi metamorphic terrain, c—Jidong-Miyun metamorphic terrain, d—Luxi metamorphic terrain, e—Yishui metamorphic terrain.

S-type granites. Geochronological data indicate that both the Al-rich assemblage of kyanite+perthite+garnet are also present (Zhou gneisses and S-type granites were essentially formed in the late et al., 2010). Although earlier studies defined clockwise paths for the Paleoproterozoic (Wan et al., 2006a, 2006b; Xia et al., 2006b; Geng et khondalite belt (Zhao et al., 2005; Zhou et al., 2010), the al., 2009; Zhou and Geng, 2009). A large part of the khondalite recent detailed works on the ultrahigh-temperature granulites belt underwent granulite facies metamorphism up to ultrahigh identify anti-clockwise P-T paths consistent with formation and temperature (UHT) conditions (Guo et al., 2006; Santosh et al., extrusion in a subduction–collision setting using petrologic and 2006, 2007a, b; 2009a,b; Liu et al., 2010; Santosh and Kusky, 2010; pseudosection modeling methods (Santosh et al., 2007a, 2009a, b; Tsunogae et al., 2011). Some high pressure pelitic granulites with the Tsunogae et al., 2011). Y. Geng et al. / Gondwana Research 21 (2012) 517–529 521

Fig. 3. Diagram of zircon U–Pb isotopic ages and lithologic features for late Neoarchean to Paleoproterozoic orthogneisses from the Trans-North China Orogen (after Geng et al., 2010). a—Huai'an-Chengde metamorphic terrains, b—Hengshan metamorphic terrain, c—Wutai metamorphic terrain, d—Fuping metamorphic terrain, e—Dengfeng metamorphic terrain.

3. Data and major parameters and metamoprphic in origin, and I, D, H, and M are used to represent these types (Table 1), respectively. The magmatic zircons commonly Since the application of the LA-ICP-MS technique in zircon Hf isotope come from the TTG and granitic gneisses and show typical oscillatory measurement, abundant Hf isotope data were generated from zircons in zones in CL images (Yang, et al., 2008; Liu et al., 2009b). Some magmatic various rock types of the NCC (Table 1). The rocks hosting the zircon are zircons have developed bright metamorphic rims and will be treated mainly the TTG gneisses of Archean-Paleoproterozoic and metasedi- separately as metamorphic origin in the following discussion. The mentary rocks of Archean-Mesoproterozoic. The zircons derived from detrital zircons from the metasedimentary rocks are generally rounded various source rocks can be classified as magmatic, detrital, inherited in shape, suggesting their fluvial transporation. Most detrital zircons 522 Y. Geng et al. / Gondwana Research 21 (2012) 517–529 have distinct oscillatory zones, such as the zircons of the quartzite in the 176Lu/177Hf ratios higher than 0.003000, with the maximum Songshan Group (DiWu et al., 2008) and zircons of the sandstone in the 0.009182. It should be pointed out that the two samples with higher Zaltay Group (Li et al., 2007). In both these localities, zircons have 176Lu/177Hf have 176Hf/177Hf ratios ranging between 0.281600 and obvious oscillatory zones and fairly uniform ages, implying the 0.281800. Whereas the other samples have 176Hf/177Hf ratios focused homogeneous source of the magmatic gneisses or volcanics. In some in two ranges, one at 0.281000–0.281600 and the other 0.280300– of the metasedimentary rocks, especially in khondalites, zircons with 0.280800 (Fig. 4). obscure textures show substantial age variation (Wan et al., 2006a, Apart from the higher 176Lu/177Hf ratios of specific zircon grains in 2006b; Xia et al., 2006a, b; Yin et al., 2009), suggesting multiple sources. some samples, the majority of the 176Lu/177Hf ratios of the detrital Inherited zircons are few in amount and are mostly preserved as the zircons fall within the range of 0.000007–0.002000, suggesting their cores of magmatic zircons, demonstrating their earlier crystallization rather low Lu contents in spite of their subsequent geologic history from . The metamorphic zircons usually form as overgrowth including transportation, deposition and metamorphism. It is rim on earlier zircons. Some independent grains with obscure internal textures and low Th/U ratio are also present (Yang et al., 2008).

Based on the available data, we have re-calculated the εHf(t), TDM and crust residence ages TDMC, applying the following equations: ε 176 = 177 − 176 = 177 λt− Hf ðÞt = Hf Hf Lu Hf ×e 1 S S λ = 176Hf = 177Hf − 176Lu= 177Hf ×et−1 −1 ×10; 000; CHUR; 0 CHUR

n hi = λ 176 = 177 – 176 = 177 TDM =l ln 1+ Hf Hf Hf Hf S DM hio = 176Lu= 177Hf – 176Lu= 177Hf ; S DM hi = λ 176 = 177 – 176 = 177 Crust residence ages TDMC =1 ln 1+ Hf Hf Hf Hf f DM S h λ + 176Lu= 177Hf – 176Lu= 177Hf ccÞ ×et–1 S i = 176Lu= 177Hf – 176Lu= 177Hf cc DM g

The parameters used in the calculations are: mean continent crust (176Lu/177Hf)cc=0.015; Chondrite Uniform Reservoir 176 177 176 177 ( Lu/ Hf) CHUR=0.0332, ( Hf/ Hf) CHUR=0.282772 (Blichert- 176 177 Toft and Albarede, 1999), and depleted mantle ( Lu/ Hf) DM= 176 177 0.0384, ( Hf/ Hf) DM =0.28325 (Griffin et al., 2000); λLu = 1.867×10−11/year (Söderlund et al., 2004), and the t represents the crystallization time of zircon. As the techniques adopted vary, the crystallization time (t) of zircon can be measured in the following three cases. (1) If the MC-ICPMS, Q-ICPMS and quasi-molecular laser sampling system are used for U–Pb and Lu–Hf in-situ isotope measurement, the apparent 207Pb/206Pb age of the same spot is taken as the crystallization time of zircon. (2) If the SHRIMP method is adopted firstly for determining zircon U–Pb isotope ages, and measuring Hf isotope through LA-ICPMS in the corresponding spot then the appar- ent 207Pb/206Pb age of the spot is taken as the crystallization time of zircon. (3) Without the corresponding spot analyzed, the concordant (weighted mean) 207Pb/206Pb age of the same type of zircons is taken as the crystallization time of the zircon. If there is no U–Pb data for the corresponding spot available, the concordant (weighted mean) 207Pb/206Pb age of the zircons is taken as the crystallization time according to the zircon type.

4. Basic Hf isotope feature of zircons in the NCC

The Hf isotopes of zircons from different rocks and regions show distinct features. The 176Lu/177Hf ratios of magmatic zircons range between 0.000013 and 0.009182, most between 0.000013 and 0.002500. Except for some spots, relatively high 176Lu/177Hf ratios are displayed in two samples. One of these was collected from the Tangjiashan granite, Eastern Block, and 16 analyses for 17 zircons show their 176Lu/177Hf ratios higher than 0.003000, with a maximum of 0.007638. The other sample with high 176Lu/177Hf ratio is a Fig. 4. Zircon 176Lu/177Hf vs 176Hf/177Hf diagram. a— zircons of the Eastern Block, b— Paleoproterozoic dolerite dyke collected from Fengzhen County in the zircons of the Trans-North China Orogen, c— zircons of the Western block; D— detrital Trans-NorthChinaOrogen.80%ofthe10zirconspotshave zircons, H— inherited zircons, I— magmatic zircons, M— metamorphic zircons. Y. Geng et al. / Gondwana Research 21 (2012) 517–529 523 apparent that no detectable radiogenic Hf was added after the zircon results were dominantly reported from the basic rocks which were formation, and that the measured 176Hf/177Hf ratios basically extracted from the depleted mantle through partial melting. The represent the Hf composition of the system when zircon was initially intermediate-acidic rocks, especially the TTG, are mainly the result of formed (Wu et al., 2007). In the zircon 176Lu/177Hf vs 176Hf/177Hf the partial melting of the middle-lower continental crust (or oceanic diagram (Fig. 4), the detrital zircons are distributed in two fields, one crust) and are hardly derived from a depleted mantle. Most of the in the upper part of the diagram with 176Hf/177Hf ratios of 0.281000– samples that we chose are from the intermediate-acidic rocks where 0.281800, and the other with ratios of 0.280200–0.280800. The the zircon U–Pb ages represent the time of magma crystallization samples of detrital zircons in the latter field are much fewer than the (formation time of the rock) and the zircon Hf model ages imply the samples of magmatic zircons. residence time of the melted parent rocks in the crust. If the Hf model The inherited zircons are small in amount and can be grouped into two fields in the zircon 176Lu/177Hf vs 176Hf/177Hf diagram (Fig. 4), one in the upper part of the diagram with 176Hf/177Hf ratios of 0.281200–0.281500, and the other at the lower left with ratios of 0.280400–0.280800. The metamorphic zircons fall in a single field on the top left part of the diagram (Fig. 4) with 176Hf/177Hf in the range of 0.281000–0.281800. Most of the metamorphic zircons have 176Lu/177Hf ratios in the range of 0.000006–0.003000, a few spots show high values up to 0.004974. As for the spatial distribution, the zircon 176Hf/177 Hf ratios of the Eastern Block are obviously clustered in two fields (Fig. 4a), one with 176Hf/177 Hf ratios of 0.281100–0.281700 and the other with 176Hf/177Hf ratios 0.280200–0.280800. The 176Hf/177Hf ratios of magmatic, detrital and inherited zircons appear in all the domains, whereas the metamorphic zircons are clustered mainly in the zone with higher 176Hf/177Hf ratios (Fig.4a). The Western Block and the Trans-North China Orogen have relatively high zircon 176Hf/177Hf ratios, and most of the 176Hf/177Hf ratios plot in the upper left region of the diagram (Figs. 4b,c). Only a minor population of the detrital zircons show lower 176Hf/177Hf ratios and are distributed in the lower part of the diagram. The wide variation in the 176Hf/177Hf ratios of zircons even without substantial change in the 176Lu/177Hf ratios in the Eastern Block can be attributed to the negative correlation 176 177 between the Hf/ Hf ratios and the TDM values while the 176Lu/177Hf ratios are constant from the model age formula. The 176Hf/177Hf ratios show negative correlation with the model ages, and linear negative correlation with U–Pb ages if there is no Pb loss in zircons (Fig. 5). In the Eastern Block of the NCC, 3.6–3.8 Ga magmatic zircons occur in the Anshan metamorphic terrain (Liu et al., 1992, 2008; Song et al., 1996; Wan et al., 2005), detrital zircons with ages of N3.5 Ga are reported from Caozhuang Village, Jidong terrain (Liu et al., 1992) and inherited zircons with N3.6 Ga occur in volcanics at Xinyang City (Zheng et al., 2004). Recently, Hf isotope studies have been carried out on these old zircons (Zheng et al., 2004; Wu et al., 2005a, 2008; Wan et al., 2007; Liu et al., 2008). Apart from the relicts of the old crustal rocks, the Eastern Block is dominated by Neoarchean magmatic rocks (Fig. 2). The 176Hf/177Hf ratios are distributed as two zones (Fig.4a) reflecting the existence of Eo-to Paleoarchean (4.0– 3.2 Ga) crustal remnant and abundant Neoarchean rocks. However, there are no such relcits of the Eo-Paleoarchean crusts in the Western Block or the Trans-North China Orogen, and they show uniformly higher 176Hf/177Hf ratios of zircons (Fig. 4b,c). The lower 176Hf/177Hf ratios of the detrital zircons suggest their derivation from ancient crust in the Trans-North China Orogen, even within the Western Block.

5. Implication of the zircon Hf isotope results

5.1. The crustal growth of the NCC

Similar to the whole rock Nd isotope model ages, the zircon Hf model ages are often used to constrain the time when the isotope system differentiated from the mantle (Wu et al., 2007). However, the two isotope systems are different. As basic rocks are usually silica unsaturated with only rare formation of magmatic zircons, most of the Fig. 5. Zircon U–Pb ages vs 176Hf/177Hf diagram. A— Eastern Block, b— Trans-North zircons analyzed in the various studies synthesized here were taken China Orogen, c— Western Block; D— detrital zircons, H— inherited zircons, I— from intermediate-acidic rocks. On the other hand, the Nd isotope magmatic zircons, M— metamorphic zircons. 524 Y. Geng et al. / Gondwana Research 21 (2012) 517–529 age greatly exceeds the formation age, the parent rocks must have model age, both showing a small peak at 3.5–4.0 Ga and an obvious remained settled in the crust for a long time. If the model ages peak at 2.4–2.8 Ga. The former peak is similar to the earlier peak of approximate the formation age, the source of the parent rocks are 3.2–3.6 Ga from whole rock Nd model ages of the Eastern Block juvenile and the residence time is very short (Wu et al., 2007). The whereas the latter peak shows some difference from the peak longer residence time of the parent rocks of the intermediate-acidic obtained from the NCC rocks (Wu et al., 2005a, 2005b). We attribute magmas in the crust, the larger derivation of the single stage model this difference to the two different methods employed. For the ca. age, and the model age must be calibrated through the Lu/Hf 3.8 Ga trondhjemite at Anshan from the Eastern Block of the NCC, the differentiation index (fLu/Hf) of the crust, and we can obtain the zircon Hf model age is older than 3.8 Ga; only minor amphibolites of two-stage Hf model age which may reflect the separation time of the 3.0–3.5 Ga occur in this block, and the whole rock Nd model ages may parent rocks from the depleted mantle. be rather old, but not older than 3.8 Ga. For comparison, we have separately calculated the single stage The 3.5–4.0 Ga single stage zircon Hf model ages have a peak at model and two-stage model ages of the magmatic zircons from the 3902±13 Ma, and the two-stage model ages show peak at 3978± NCC. As shown in the histogram of Hf depleted mantle model ages 18 Ma, with a small difference of 76 Ma, suggesting the short (Fig. 6a and b), the distribution pattern of the single-stage zircon Hf residence time of the parent rocks in the crust through zircon Hf model age is basically identical to that of the two-stage zircon Hf isotope features and the differentiation of the crust and the mantle at

Fig. 6. Histograms of the Hf model ages of magmatic zircon. a— single stage model age, b— two-stage model age. Y. Geng et al. / Gondwana Research 21 (2012) 517–529 525 ca. 3.9 Ga in the Eastern Block of the NCC. The 3.6–3.8 Ga old TTG ation in the Eastern Block of the NCC started as early as 3.9 Ga, and the gneisses are the partial melting products of the lower crust partial melting of the ca. 3.9 Ga accreted crustal materials produced differentiated at 3.9–4.0 Ga. In the formation age vs εHf(t) diagram 3.6–3.8 Ga trondhjemite-dominated Baijiafen and Dongshan granit- (Fig. 7), the εHf(t) of the 3.6-3.8 Ga old TTG gneisses ranges between oid complexes in Anshan area. −8 and +10, suggesting that the parent rocks of the TTG were partly In the histograms, the most prominent peak is at 2.4–2.9 Ga. The derived from the depleted mantle and partly from the addition of the maximum peak of the single stage model ages is 2698±4 Ma, and the older crustal rocks (N3.8 Ga). However, the mixing mechanism of the maximum peak is at 2714±5 Ma for the two-stage model ages, with a crust and mantle magmas in early earth history is uncertain. The difference of less than 20 Ma, implying a short crustal residence time of previous investigations suggest that the crust and mantle differenti- the parent rocks of the intermediate-acidic magmatic rocks. The 2.7 Ga peak marks the major crustal growth stage in the NCC and the whole rock Nd isotope results (Wu et al., 2005a) are also consistent with this. In

the formation age vs εHf(t)diagrams(Fig. 7), the TTG gneisses formed at 2.7–2.8 Ga in the Eastern Block and the Trans-North China Orogen, with

most zircons in the rocks showing positive εHf(t) values situated between the evolutionary trends of the depleted mantle and chondrite, suggesting that the parent rocks of the TTG at this stage were mainly

derived from the depleted mantle. A minor group of samples have εHf(t) values between −4 and 0, implying the reworking of a small volume of older crustal rocks. Zircon Hf isotope model ages indicate that the crust of the NCC mostly grew at 2.7–2.8 Ga, when the widespread volcano- sedimentary sequences and TTG gneisses were formed in the Eastern Block and the Trans-North China Orogen, such as the basic volcanics and widespread TTG gneisses in the Luxi metamorphic terrain of the Eastern Block (Jahn et al., 1988; Du et al., 2003, 2010; Polat et al., 2006b; Lu et al., 2008; Wang et al., 2009), as well as the presence of the contempora- neous gneisses in the Jiaodong terrain (Jahn et al., 2008). The Lushan terrain of the Trans-North China Orogen shows 2838–2845 Ma basic volcanics and the 2829–2832 Ma TTG gneisses, both of which have undergone the 2.77 Ga metamorphism (Liu et al., 2009a). The Fuping and Hengshan terrains of the Trans-North China Orogen expose the 2.7– 2.8 Ga TTG gneisses (Guan et al., 2002; Kröner et al., 2005a, b). The above data show that both the Eastern Block and the Trans- North China Orogen of the NCC witnessed the 2.7–2.8 Ga magmatic events. Though their exposure areas are much less than that of the 2.5 Ga rocks, both the zircon Hf model ages and Nd model ages of the basic rocks reveal that 2.7–2.8 Ga is the most important crustal growth stage in the NCC. The 2.7–2.8 Ga volcanics and TTG gneisses were less preserved because of the strong alteration from widespread magmatism and metamorphism at the end of Archean and in Paleoproterozoic. Some researchers have suggested that the crustal growth at 2.7–2.8 Ga in the NCC may be related to the major activity (Yang et al., 2008; Liu et al., 2009b).

5.2. The reworking of the NCC crustal rocks

The ca. 2.5 Ga magmatic event was widespread in the NCC (Figs. 2, 3). Statistical data from more than 600 zircon U–Pb ages indicate that 2.5 Ga was the most predominant stage of rock-formation in early Precambrian in the NCC (Shen et al., 2005). However, the zircon Hf model ages do not show the obvious ca. 2.5 Ga peak, suggesting that the rocks were not directly derived from the differentiation of the

depleted mantle. In the formation age vs εHf(t) diagram (Fig. 7), the magmatic zircons in the ca. 2.5 Ga rocks and the detrital zircons in the Eastern Block and the Trans-North China Orogen mostly show positive

εHf(t) values and are situated between the evolutionary trends of the depleted mantle and chondrite. Simultaneously, the zircon U–Pb ages

are close to the TDM of zircons with high εHf(t) values, suggesting that the source rocks of the zircons were produced by the partial melting of the juvenile crustal rocks. The Hf isotope feature indicates that the source materials of the orthogneisses of late Neoarchean–early Paleoproterozoic in the NCC were juvenile crust which was reworked in a very short period. A substantial crustal growth in the NCC mainly in the early Neoarchean (2.7–2.8 Ga) is deduced from the following reasons. The Fig. 7. Zircon formation age vs zirconεHf (t) diagrams. a— Eastern Block, b— Trans-North China Orogen, c— Western Block; D— detrital zircons, H— inherited zircons, I— zircon Hf model ages at the maximum peak ca. 2.7 Ga (Fig. 6) show a magmatic zircons, M— metamorphic zircons. general discrepancy of 100–200 Ma between the formation time of 526 Y. Geng et al. / Gondwana Research 21 (2012) 517–529 the rocks generated at ca. 2.5 Ga and the two-stage model ages (Table in the Neoarchean and had diverging evolution during the

1). Most of the εHf(t) values of zircons formed at ca. 2.5 Ga are situated Paleoproterozoic. between the evolutionary trends of the depleted mantle and the chondrite (Fig. 7). These juvenile lower crustal materials were 6. Conclusion retained for a short time and then strongly reworked in the ca. 2.5 Ga anatexis, resulting in the widespread rocks of late Neoarchean The large amount of zircon Hf isotope data and U–Pb formation in the NCC. Minor zircons of ca. 2.5 Ga yield rather lower (negative) ages synthesized in this study demonstrates that the earliest crustal

εHf(t) values, suggesting the involvement of some older crustal rocks growth event in the NCC occurred at 3.9–4.0 Ga, generating the lower (Liu et al., 2009b). crust dominated by basic rocks. After short residence in the crust, the In the Eastern Block of the NCC, a widespread ca. 2.5 Ga regional basic rocks in the lower crust experienced partial melting and gave metamorphism was responsible for the growth of metamorphic zircons rise to the ancient crust typified by the 3.6–3.8 Ga trondhjemite at which mostly show positive εHf(t) values, nearly the same as that of the Anshan area, Liaoning Province. The strongest crust–mantle differen- synchronous magmatic zircons, and are located between the evolutionary tiation event at ca. 2.7 Ga in the NCC was responsible for of the trends of Hf isotope of the depleted mantle and the chondrite (Fig. 7). As voluminous newly grown crustal rocks and the volcanics and TTG compared to the magmatic zircons, the metamorphic zircons do not gneisses distributed in the Eastern Block and the Trans-North China display depressed trend of their 176Lu/177Hf ratios in this region (Fig. 4), Orogen. At ca. 2.5 Ga, the juvenile crust that formed at ca. 2.7 Ga indicating that the zircon Hf isotope system was essentially not reset underwent extensive partial melting, which resulted in a wide during their metamorphic recrystallization; that is, the Hf isotopic ratios distribution of the late Neoarchean magmatic rocks in the NCC, were not obviously affected by the metamorphic fluids (Du et al., 2010). which define the essential tectonic framework of the NCC. After The Trans-North China Orogen also preserves records of 2.5–2.0 Ga 2.5 Ga, the crustal rocks of the Trans-North China Orogen were magmatic rocks. The age vs εHf(t) diagram of the magmatic rocks reactivated and the 2.4–2.0 Ga magmatic complexes formed. The ca. from TNCO shows that the εHf(t) values change gradually from 1.8 Ga magmatic and metamorphic events were obviously the result positive to negative as age decreases, displaying a reverse relationship of reworking of the pre-existing crustal rocks. The consistency of (Fig. 7b). This tendency implies that the crust was intensely reworked Neoarchean magmatic evolution and zircon Hf isotope compositions and the 2.5–2.0 Ga magmatic rocks are the products of melting of the of the Eastern Block and the Trans-North China Orogen imply that ca. 2.5 Ga crustal rocks. they were once part of an integrated tectonic unit in the Neoarchean. Most zircons from the 1.7–1.9 Ga magmatic rocks from various parts of Supplementary materials related to this article can be found online the NCC have negative εHf(t)values(Fig. 7), suggesting substantial at doi:10.1016/j.gr.2011.07.006 involvement of the crustal rocks and implying a large amount of crustal reworking. A correlation of the Eastern Block and the Trans-North China Acknowledgments Orogen reveals that the Eastern Block has preserved the records of earlier crustal growth and reworking. Both the Eastern Block and the The paper has been granted by the National Natural Science Trans North China Orogen share similar evolutionary history of the Foundation of China (40672126), the Chinese Geological Survey early Neoarchean (2.8–2.65 Ga) crust–mantle differentiation event, (1212010611702 and 1212010811048). Professor Wan Yusheng has and the late Neoarchean (2.6–2.5 Ga) large scale magmatic activity; provided some unpublished data and discussed some questions with their zircon Hf isotopic features display high consistency with their U– the authors. Professors Shen Qihan and Wang Tao have made many Pb ages. Thus we deduce that the Eastern Block and the Trans-North comments and suggestions on the evolution of the North China Craton China Orogen were probably a unified continent block in the and greatly improved the paper. Neoarchean. Due to the scarcity of the zircon Hf isotope data in the Western Block, it is hard to judge the relation between the Western Block and the Eastern Block as well as the Trans-North China Orogen. References Albarede, F., Telouk, P., Blichert-Toft, J., Boyet, M., Agranier, A., Nelson, B., 2004. Precise 5.3. The relationship between the Eastern Block and the Trans-North and accurate isotopic measuments using multipe-collector ICPMS. 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