Records from the North China Craton

Ore Geology Reviews 56 (2014) 376–414

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Ore Geology Reviews

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Review Metallogeny and craton destruction: Records from the North China Craton

Sheng-Rong Li a,b,⁎, M. Santosh b,c a State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, 29 Xueyuan Road, Beijing 100083, China b School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China c Faculty of Science, Kochi University, Kochi 780-8520, Japan article info abstract

Article history: The link between metallogeny and craton destruction in the North China Craton (NCC) remains poorly under- Received 26 January 2013 stood, particularly the mechanisms within the interior of the craton. In this overview, we summarize the Received in revised form 8 March 2013 major stages in the history of formation and evolution of the NCC, the spatio-temporal distribution and types Accepted 11 March 2013 of major ore species, as well as mantle contribution to the metallogeny, in an attempt to evaluate the geodynamic Available online 22 March 2013 settings of metallogeny and the mechanisms of formation of the ore deposits. The early Precambrian history of the NCC witnessed the amalgamation of micro-blocks and construction of the fundamental tectonic architecture Keywords: North China Craton of the craton by 2.5 Ga. The boundaries of these micro-blocks and the margins of the NCC remained as weak Lithospheric thinning zones and were the principal locales along which inhomogeneous destruction of the craton occurred during Metallogeny later tectonothermal events. These zones record the formation of orogeny related gold, copper, iron and titanium Craton destruction during the early to middle Paleoproterozoic with ages ranging from 2.5 to 1.8 Ma. The Early Ordovician kimber- Tectonics lite and diamond mineralization at ca. 480 Ma, the Late Carboniferous and Early to middle Permian calc-alkaline, I-type granitoids and gold deposits of 324–300 Ma, and the Triassic alkaline rocks and gold–silver-polymetallic deposits occurring along these zones and the margins of the blocks correlate with rising mantle plume, southward subduction of the Siberian plate and northward subduction of the Yangtze plate, respectively. The volumi- nous Jurassic granitoids and Cretaceous intrusives carrying gold, molybdenum, copper, lead and zinc deposits are also localized along the weak zones and block margins. The concentration of most of these deposits in the eastern part of the NCC invokes correlation with lithosphere thinning associated with the westward subduction of the Paciﬁc plate. Although magmatism and mineralization have been recorded along the margins and few places within the interior of the NCC in the Jurassic, their peak occurred in the Cretaceous in the eastern part of the NCC, marking large scale destruction of the craton at this time. The junctions of the boundaries between the micro-continental blocks are characterized by extensive inhomogeneous thinning. We propose that these junctions are probably for future mineral exploration targeting in the NCC. © 2013 Elsevier B.V. All rights reserved.

Contents

1. Introduction ...... 377 2. Formation and evolution of the NCC ...... 378 2.1. Amalgamation of microblocks ...... 378 2.2. Two major types of craton destruction ...... 378 2.3. The timing of destruction of the NCC ...... 379 2.4. The heterogeneity of the NCC destruction ...... 380 3. Metallogeny in the NCC ...... 381 3.1. Spatial distribution of ore systems ...... 381 3.1.1. Gold ...... 381 3.1.2. Molybdenum ...... 381 3.1.3. Copper, lead and zinc ...... 382 3.2. Chronology of metallogeny ...... 383 3.2.1. Gold mineralization ...... 383 3.2.2. Molybdenum mineralization ...... 384

⁎ Corresponding author at: State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, 29 Xueyuan Road, Beijing 100083, China. Tel.: +86 10 8232 1732; fax: +86 10 8232 2176. E-mail address: [email protected] (S.-R. Li).

3.3. Ore deposit types ...... 384 3.3.1. Gold ore systems ...... 384 3.3.2. Molybdenum ore systems ...... 389 3.3.3. Chaijiaying lead–zinc ore systems ...... 391 3.4. Mantle contribution ...... 391 3.4.1. Northern margin of the NCC ...... 391 3.4.2. Eastern margin of the NCC ...... 406 3.4.3. Southern margin of the NCC ...... 408 3.4.4. Western margin and central NCC ...... 408 3.5. Link between metallogeny and the evolution of the NCC ...... 408 3.5.1. Metallogeny in response to the formation of the NCC ...... 408 3.5.2. Metallogeny in response to the destruction of the NCC ...... 409 3.5.3. Metallogeny linked with plate motion and mantle plume activity ...... 410 4. Ore systems in the NCC: theoretical considerations and prospecting targets ...... 410 5. Conclusions ...... 410 Acknowledgments ...... 411 Appendix A. References for Tables 1 to 6 ...... 411 References ...... 411

1. Introduction and thickness, upper mantle anisotropy, and discontinuity structures and thickness of the mantle transition zone near the boundary between The construction and destruction of cratons have received much the eastern and central parts of the NCC (Chen, 2009, 2010; Cheng et al., attention in recent years from geological, geophysical, geochronolog- 2013). Preliminary studies have identified a systematic relationship be- ical and tectonic perspectives (e.g., Zhang et al., 2013, and references tween the inhomogeneous lithosphere thinning and variations in the therein). In the past, various models including thermo-mechanical nature and distribution of ore systems (Li et al., 2012, 2013). However, (e.g. Davies, 1994; Ruppel, 1995) and chemical (e.g., Bedini et al., systematic investigations to evaluate the possible relationship between 1997) erosion as well as delamination (e.g., Bird, 1978, 1979; Kay the heterogeneity of lithosphere structure and metallogeny, which are and Kay, 1993) have been proposed to explain the process of fundamental to the formulation of exploration strategies for ore de- decratonization. The North China Craton (NCC) provides a classic ex- posits, have not been carried out. ample of craton destruction where the erosion model (e.g., Griffinet There is a marked distinction in the distribution of the younger mag- al., 1998; Lu et al., 2000; Menzies and Xu, 1998; Xu et al., 1998; matic rocks in the NCC, with Carboniferous to Triassic suites occurring Zhang et al., 2005; Zheng, 1999), and the delamination model in the craton margin, and Jurassic to Cenozoic suites extending gradu- (Deng et al., 2004a,b; Gao et al., 2002; Wu and Sun, 1999) have ally into the interior. This distribution probably suggests that the de- been invoked to explain the extensive lithospheric thinning, particu- struction of the NCC started from its margins to the interior, reflecting larly in the eastern and central domains of the craton during the Me- the vulnerability of plate boundaries and weak zones on cratonic de- sozoic. Those who favor the thermo-mechanical erosion model struction (Xu et al., 2009). Within the basement of the NCC, at least attributed recycling of the asthenosphere and mantle plume upwell- six Precambrian microblocks have been identified such as the Alashan, ing as the major cause which resulted in erosion from the bottom of Jining, Fuping, Qianhuai, Xuchang and Jiaoliao blocks (Zhai et al., the lithosphere. In contrast, those who argue in favor of the latter 2005), the amalgamation of which occurred during the Neoarchean, model proposed the delamination of eclogitic material generated and subsequent rifting–subduction–collision in the Paleoproterozoic through continental collision and crustal thickening as the major led to the final stabilization of the craton (e.g., Santosh, 2010; Santosh cause for lithospheric thinning beneath the NCC. et al., 2007; Zhai and Santosh, 2011; Zhai et al., 2005). The relationship Although several studies have addressed the geodynamics associ- between these microblocks and their boundaries with the inhomoge- ated with metallogeny in the NCC (e.g., Chen et al., 2007, 2009a,b; Li neous lithosphere thinning remain equivocal, although it is generally et al., 1996; Li et al., 2012, 2013; Mao et al., 2005a,b; Zhai and Santosh, agreed that there is a strong link between metallogeny and the 2013; Zhai et al., 2002), only few have investigated the link between geodynamics of the NCC (e.g., Chen et al., 2007, 2009a,b; Li et al., metallogeny and the process of lithospheric destruction in the NCC. 2012, 2013; Mao et al., 2005a,b, 2011; Qiu et al., 2002; Yang et al., 2003). The criteria and predictions for the different mechanisms of lithosphere Previous workers have adopted different tectonic classification transformation are markedly different (Zhou, 2009), and therefore it is schemes for the major mineral deposits in the NCC such as orogenic important to evaluate the process which is more likely to generate gold (e.g., Mao et al., 2002, 2005a,b, 2008, 2011; Qiu et al., 2002), and large-scale metallic deposits. orogenic metals (Chen et al., 2004, 2007, 2009a). Several other classifi- The heterogeneity of the lithospheric destruction in the NCC, partic- cations have also been proposed such as mesothermal–epithermal type ularly the inhomogeneous thinning, has been recognized in several (e.g., Chen et al., 1989; Li et al., 1996; Li et al., 2012, 2013), skarn type studies in the past (e.g., Deng et al., 2004a,b; Luo et al., 2006; Menzies (e.g., Li et al., 2013; Shen et al., 2013), porphyry type (e.g., Li et al., et al., 1993) and confirmed in more recent studies (H.F. Zhang et al., 2003), cryptoexplosive breccia type (e.g., Li, 1995), quartz vein type 2012; Tang et al., 2013). This heterogeneity has been documented not (e.g., Nie et al., 2004; Pirajno et al., 2009), fracture-altered and breccia only from the marginal domains of the craton both from the Western type (e.g., Mao et al., 2008; Qiu et al., 2002), etc. Among these classifica- and Eastern Blocks of the NCC across the Great Hinggan Range–Taihang tions, some were based on the genesis of the ore deposit (genetic type), Mountain gravity lineament (HTGL, e.g., Xu et al., 2009), but also from and the others took into account the ore characteristics (industrial the central part of the NCC, along the Trans-North China Orogen type). Although the occurrence of major ore deposits in the marginal (TNCO) (e.g., Li et al., 2012, 2013; Tang et al., 2013). Integrated studies domains of the NCC are well established, their geneses remain debated. of the NCC based on high-resolution seismic images combined with ob- Most importantly, the ore deposits and prospecting potential within the servations on surface geology, regional tectonics and mantle dynamics interior of the NCC, regardless of the genetic and industrial types, are have revealed marked variations in crustal and lithospheric structure poorly understood. 378 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

In this overview, we attempt to characterize the ore deposits both volcanic–plutonic island arc zone characterized by TTG (tonalite– in the interior and marginal domains of the NCC and examine their trondhjemite–granodiorite) rocks of 2.56–2.5 Ga along the western/ prospecting potential. Our work provides new insights on the possi- outer side, and calc-alkaline granitic rocks of 2.5–2.45 Ga on the ble relationship between metallogeny and lithosphere thinning asso- eastern/inner side have been suggested in the western part of the ciated with craton destruction. Jiaoliao continent block (Wu et al., 1998; Zhao et al., 1993), implying arc–continent collision between the Jiaoliao block and the Qianhuai block. Based on the distribution of high-pressure granulites, Zhai et al. 2. Formation and evolution of the NCC (1992) proposed continent–continent collision between the Qianhuai and Fuping blocks and between the Qianhuai and Ji'ning blocks at 2.1. Amalgamation of microblocks 2.5–2.6 Ga. Zhai et al. (2000) and Zhai and Santosh (2011) also proposed that between 2.6 and 2.45 Ga, the six microblocks in the NCC Based on the distribution of early Precambrian rocks, and through were amalgamated together by continent–continent, continent–arc or integrated geological, geochronological and geophysical information, arc–arc collision (Fig. 1c). at least six micro-continental blocks have been identified within the NCC (Bai et al., 1993, Wu et al., 1998; Zhai and Santosh, 2011, 2013; Zhai et al., 2000, 2005). From west to east these are the Alashan, 2.2. Two major types of craton destruction Ji'ning, Ordos, Fuping or Xuchang, Qianhuai, Xuhuai and Jiaoliao blocks (Fig. 1). Rock types and their distribution in these micro- Thermo-mechanical or chemical erosion and delamination are con- blocks display distinct differences, with Neoarchean volcanism and sidered as the two major mechanisms that led to the destruction of the magmatism at 2.9–2.7 Ga and 2.6–2.45 Ga, indicating that these NCC. According to the erosion model, the bottom of the lithosphere is micro-blocks were not amalgamated into a coherent craton until at softened through heating by upwelling asthenosphere, and the shear least 2.5 Ga. Several granitic intrusives with ages around 2.5–2.4 Ga stress from the horizontal flow of the asthenosphere would transfer invade the basement rocks in all these blocks (e.g., Geng et al., the weakened lithospheric bottom to the asthenosphere. This type of 2012; H.F. Zhang et al., 2012; Wu et al., 1998; Z. Zhang et al., 2012), erosion could upwell the thermal conduction of the asthenosphere suggesting that the microblocks were assembled prior to the em- into the bottom of the lithosphere leading to further erosion and thin- placement of these granitoids, and that these microblocks define the ning (Davies, 1994; Ruppel, 1995). The thermo-mechanical erosion unified tectonic architecture of the NCC at the end of Neoarchean model has been developed into a coupled scheme of both thermo- (Li et al., 1997). An alternative framework of the NCC basement was mechanical and chemical erosions (e.g., Ji et al., 2008; Xu, 1999). The suggested with two discrete blocks, the Western and Eastern Blocks, duration of the thinning from the thermo-mechanical erosion depends developed independently during the Archean and finally collided on the temperature of the convective asthenosphere and the original along the central zone (Trans-North China Orogen) to form a coher- thickness of the lithosphere. Based on a numerical simulation, Davies ent craton during a global Paleoproterozoic collisional event at (1994) suggested that the duration for thinning a 200 km thick litho- 1.85 Ga (Zhao et al., 2005, 2007). sphere to 100 km would be about ten million years provided that a The nature of the NCC in the late Neoarchean has been addressed plume is present at the bottom. However, in the absence of a plume, through several models. Among these, the vertical accretion with this process might take about 50–100 million years. multi-stage cratonization (Zhao et al., 1993) and marginal accretion- The delamination model emphasizes the processes of regional tec- reworking (Jin and Li, 1996)arepopular.Arc–continent or continent– tonics. When cratons undergo tectonic convergence, such as plate continent collision models have also proposed to explain the early subduction or collision, the crustal thickness increases leading to high Precambrian evolution of this craton (Zhai and Santosh, 2011). A grade metamorphism and mineralogical phase changes to generate

Fig. 1. Boundaries and locations of the Newarchean micro-continental blocks in the NCC. ALS = Alashan block, JN = Jining block, OR = Ordos Block, QH = Qianhuai block, XCH = Xuchang or Fuping block, XH = Xuhuai, and JL = Jiaoliao block. After Zhai and Santosh (2011). S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 379 eclogite at the bottom. Eventually, the high density eclogitic material magmatism in the Late Triassic characterized mostly by alkaline rocks would break off and drop down into the mantle, leading to the delami- has been documented from the northern and eastern margins of the nation of the lithosphere (Beck and Zandt, 2002; Bird, 1979; Pysklywec NCC (Yang and Wu, 2009; Yang et al., 2007). The magmatism during et al., 2000). Thus, based on geological and tectonic models, Zhai et al. the Jurassic is also mainly distributed in the north and east margins of (2002), Deng et al. (2006) and Gao et al. (2008),amongothers the NCC, with granitoids comprising the major suite (Fig. 2b). Examples discussed the thickening of the continental crust of the NCC and delam- include the Tongshi intrusive complex emplaced at 180.1–184.7 Ma in ination during the Yanshanian. the Luxi region (Lan et al., 2012), and the Linglong and Luanjiahe gran- Recent studies have emphasized the role of interaction between ites emplaced at 157–159 Ma in the northwest Jiaodong region (Yang et melt or fluid and mantle peridotite on the micro-mechanics of chem- al., 2012). The magmatism attained its peak in the Cretaceous and was ical erosion (e.g., Xu et al., 2013). Investigations on mantle xenoliths characterized by a wide range of felsic and mafic igneous rocks, distrib- have led to the identification of lithospheric alteration by melt or uted mainly in the Yanshan Mountains, Taihang Mountains, Jiaodong fluid. The spatial variation of isotopic characteristics in the source re- and Luxi regions. The Mapeng granitic pluton in the Taihang Mountains gion, low Mg# values, systematic changes in the mineral phases, dis- and the Sunzhuang dioritic pluton in the Heshan Mountain were turbance of the Re/Os isotopic system, mixed tDM ages, chemical emplaced at ca. 130 Ma (Li et al., 2012, 2013), and the Guojialing grano- zoning of minerals, among other features, have been documented. diorites in the north-western Jiaodong were also emplaced in the early These features have been correlated to variations in the nature and Cretaceous (129 Ma, Yang et al., 2012). The magmatism during the end characteristic of the lithospheric mantle during craton destruction of Cretaceous to the Neogene was characterized by tholeiitic and alkaline process (e.g., Reisberg et al., 2005; Zhang et al., 2004; Zhou, 2006; basalt distributed within extensional basins and along deep-seated frac- Zhang et al., 2008; Zhang et al., 2013). tures within the craton. Zhou (2009) summarized the criteria to evaluate the two mecha- Although the duration of the magmatism cannot be directly corre- nisms of lithospheric thinning. The thermo-mechanical/chemical ero- lated with the duration of craton destruction, the ages of these sion model is related with a prolonged and continuous magmatic magmatic suites provide important constraints on the lithospheric activity, initially sourced from the lithosphere and gradually extending thinning event. Thus, Xu et al. (2009) suggested that the initiation to asthenosphere. In this case, the resulting features include lithosphere of the NCC lithosphere thinning would not be later than the Carbon- extension, chemically layered lithosphere with different ages, and vol- iferous and Triassic, respectively in the northern and eastern margins, canic or sub-volcanic activity with different chemistry correlating and the southward subduction of the Paleo Asian Ocean Plate and the with changes in the source characteristics. The delamination model, in northward subduction of the Yangtze Plate as well as the consequent contrast, is reflected in short and episodic magmatism derived from collision triggered the activity along the northern and southern mar- the asthenosphere, rapid extension of the lithosphere accompanied by gins of the NCC. The thinning of the NCC peaked in the late Jurassic to strong surface erosion, and younger components dominating the litho- Cretaceous and continued even to the early Cenozoic, during a sphere with volcanic or sub-volcanic material displaying the signature protracted period of more than 100 Ma (Xu et al., 2009). of recycled ancient crust. Geochemically, the Cenozoic basalts in the NCC show increasing Apparently, evidence in support of both these phenomena — erosion alkalinity with time, suggesting an increase in the depth of the and delamination — exists in the NCC, and a combined erosion plus de- magma source (Xu et al., 2009). Combined with the ca. 100 Ma basalt lamination model is gaining acceptance with the notion that these two in the Fuxin region derived from the asthenosphere, Wu et al. (2008) models are not mutually exclusive (e.g., Wu et al., 2008). suggested that the destruction of the NCC occurred in the Cretaceous earlier than 100 Ma. Zhu et al. (2011) suggested that the start of de- 2.3. The timing of destruction of the NCC struction of the NCC should be later than the Late Mesozoic when the Pacific plate subducted towards west and the Mongolia–Okhotsk Sea Craton destruction is not only related to the thinning of the craton closed which led to the transition of the tectonic system. lithosphere, but also involves changes in composition of the litho- In the central part of the NCC, previous studies on the Shihu gold sphere, its thermal state and rheological nature. The loss in the stabil- deposit and the Xishimen iron deposit from the Taihang Mountains, ity of craton as a whole is recognized as craton destruction or and their genetically related intrusive rocks led to the suggestion decratonization by Zhu et al. (2011). Theoretically, the initiation of that the Shihu gold deposit witnessed a greater amount of mantle lithosphere thinning and the variations mentioned above mark the input as compared to the Xishimen iron deposit during their forma- start of craton destruction. Since not all of these variations can necessar- tion in the Early Cretaceous (ca. 130 Ma); however, the major compo- ily show clear geological records on the earth surface, only magmatism, nents for both were derived from the lower crust (Cao et al., 2011a,b; tectonic evolution, palaeogeography and metallogeny are taken as indi- Li et al., 2012, 2013). Combined with published geophysical data (Wei cators of the destruction process. Among these, the magmatic signature et al., 2008), Li et al. (2013) suggested that the continental litho- is the most commonly employed criterion at present. sphere is markedly thinner under the Fuping region than that under Since its final cratonization during Paleoproterozoic, the NCC has the Wu'an region, and that the inhomogeneous lithosphere thinning remained largely stable for a long time. Intermittent small scale mag- in the central NCC occurred at least as early as 130 Ma. Further studies matic activity has been recorded in the Mesoproterozoic, such as the on the major magmatism and metallogenesis in the Hengshan terrain mafic dyke swarms, K-rich volcanics in the Dahongyu Formation, the revealed that these were part of the strong magmatic–metallogenic Miyun rapakivi granite north of Beijing city, and the Damiao anorthosite event that took place in the Taihang Mountains at ca. 130 Ma ago, and in the northern part of Hebei province (Li et al., 2009; Zhang et al., the lithosphere underneath the Hengshan terrain was strongly thinned 2009), which might all correlate with the rifting event of the Columbia and decoupled during the early Cretaceous, with the state of the supercontinent of which the NCC was an integral part (e.g., Santosh, destructed lithosphere largely preserved through the Cenozoic to 2010). Younger magmatic episodes include the Early Ordovician present (Li et al., 2012, 2013). diamond-bearing kimberlite of ca. 480 Ma in the Mengyin area, Although different opinions exist concerning the timing of the Shandong province, and the Fuxian area, Liaoning province (Chi and NCC destruction based mainly on magmatism, all the available evi- Lu, 1996; Xu, 2001). The magmatism since Carboniferous is classified dence indicates that the Cretaceous marks the peak for lithosphere into 5 periods (Xu et al., 2009). The earliest phase is recorded from thinning or destruction in the NCC. The magmatic pulses can be clear- the northern margin of the NCC with a series of calc-alkaline, I-type ly divided into several periods or stages, and the duration of each granitoids of 324–300 Ma, correlated with the southward subduction stage was relatively short, showing a prominent instantaneity. Theo- of the paleo Asian plate (Fig. 2a; Zhang et al., 2007). Relatively weak retically, any magmatic event after final cratonization, regardless of 380 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

Fig. 2. Distribution of the igneous rocks in the NCC. a — Caledonian, Variscanian and Indo-China epoches and b — Yanshanian epoch. 1 — North margin of the NCC fault zone; 2 — South margin of the NCC fault zone; 3 — Tan–Lu fault zone; and 4 — Taihangshan fault zone. After Cheng, 1994.

the source such as asthenosphere, lithosphere mantle, or crust, granodiorites in the northwest Jiaodong peninsula, however, possess should be taken as a record of the craton destruction. However, the high CaO, TFe2O3, MgO, LREEs, LILEs, Sr/Y, εNd(t) and εHf(t) values, effect of the destruction would sometimes be local, or can even lead and are metaluminous, with depletion in HFSEs (Yang et al., 2012), to episodes of lithospheric accretion, such as in the case of the Ceno- suggesting the involvement of mantle components in the magmatic zoic pulse in the NCC. source. Yang et al. (2012) correlated the formation of magma with the processes accompanying the subduction of the Pacific plate be- 2.4. The heterogeneity of the NCC destruction neath the NCC and the associated asthenospheric upwelling. The distribution of the magmatic rocks in the NCC (Fig. 2) shows As mentioned in a previous section, the magmatism in the NCC that the magmatism occurred at the margins of the NCC in the Car- since Carboniferous has been classified into 5 periods with different boniferous to Triassic, extended from the margin to the inner areas characteristics for the rock suites formed at different periods (Xu et of the NCC in the Jurassic, and reached its peak in the Cretaceous al., 2009). If magmatism after cratonization is a robust record of the (Xu et al., 2009). This suggests that the destruction of the NCC started craton destruction, the magmas with different characteristics must at its margins, and extended to the inner domains with time. The NCC represent different levels or tectonic domains. This would mean that is bound by Phanerozoic orogenic belts with the Xing'an–Mongolia the loci of craton destruction shifted vertically with time. Further- orogenic belt in the north, the Qinling–Dabie orogenic belt in the more, the magmatism occurred at different locations in the NCC, im- south, the Sulu orogenic belt and the subduction zone between the plying that the destruction also shifted laterally. Eurasia–Pacific plates in the east, and the Qilian orogenic belt in the Recent studies, such as for example from the Late Jurassic (157– west. The margins of the NCC, therefore, are all weak zones prone to 159 Ma) Linglong and Luanjiahe granites in the northwest Jiaodong be eroded or delaminated leading to the thinning of the lithosphere. peninsula in the eastern NCC, show high Na2O+K2O, Al2O3, Sr/Y ra- The Trans-North China Orogen or the Daxing'an–Taihang Zone in tios, LREEs and LILEs (Rb, Ba, U, and Sr), low MgO, HFSEs (Nb, Ta, P, the central part of the NCC, as a Paleoproterozoic orogenic belt and Ti) and εHf(t) values (Yang et al., 2012). These characteristics (Zhao et al., 2007), or the boundary between the microblocks Fuping are comparable to adakitic rocks, suggesting that the Linglong and and Qianhuai (Zhai and Santosh, 2011), is also a major weak zone (Li Luanjiahe granitoids formed under relatively high pressure condi- et al., 2013; Xu et al., 2009). Magmatism and metallogeny of ca. tions and were likely derived from partial melting of the thickened 130 Ma have led to lithosphere thinning beneath the Taihang Moun- lower crust of the NCC. The early Cretaceous (129 Ma) Guojialing tains (Li et al., 2012, 2013; Shen et al., 2013). If the structure of the S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 381 basement of the NCC is taken into consideration, the weak zones in- hosts the second largest gold cluster. Gold deposits in the NCC clude the boundaries of the micro-blocks beside the Taihang Moun- are dominantly distributed along the central domains of the eastern, tains. The NNE Tan–Lu Fault Zone, the major lithospheric fracture southern and northern margins of the craton. In the Jiaodong region, zone in eastern China, formed during the Mesozoic is a prominent located within the eastern margin of the NCC, several important gold weak zone in the interior of the NCC. During the northward subduc- deposits occur such as the Linglong quartz-vein type and the Jiaojia tion of the Izanagi plate in the early Cretaceous, the Tan–Lu Fault fracture-filling and altered type, both of which are recognized as Zone witnessed counter-clockwise strike-slip activity, and served as super-large gold deposits with gold reserve exceeding 100 t. Several a major channel for the upwelling of asthenosphere materials (Guo fracture-filling and altered type gold deposits, such as those of et al., 2013). Sanshandao, Xincheng, Dayingezhuang, Dongfeng and the Canzhuang Recent geophysical data and their geological interpretations are also among the super-large category. The gold reserves of the (Fig. 3) reveal pronounced variation in the thicknesses of the litho- Jinqingding and Denggezhuang quartz-vein type gold deposits, the sphere beneath the NCC which can be spatially correlated with the two largest gold deposits in the east of the Jiaodong region, exceed boundaries between the micro-blocks, the Trans-North China Craton 100 t. In the Xiaoqinling region in the south-western margin of the or Daxing'an–Taihang Zone, the Tan–Lu Fault Zone and the margins NCC, large scale mining for gold is traced to the Ming Dynasty of the craton, suggesting strong heterogeneity in cratonic architecture (A.D.1368–1644). More than 1200 auriferous quartz veins have been following the destruction. Coupled with the distribution of the explored in the Xiaoqinling region, among which about 400 t of gold magmatism in the NCC, it is obvious that the regions with thin litho- reserve has been proved and more than 10 large and super-large gold sphere show clustered large scale magmatic rocks of Mesozoic age, deposits are exploited. These are represented by the Dongtongyu, implying that the extensive thinning of the lithosphere was coeval Wenyu, Dongchuang, and Yangzhaiyu quartz-vein type gold deposits. with the Mesozoic magmatism. This finding has also been extended Several large crypto-explosive-breccia type gold deposits, such as the to metallogeny in recent studies with evidence from the Taihang Qiyugou gold deposit, and fracture-filling and altered type, such as the Mountains (Li et al., 2013) and the Heshan terrain (Li et al., 2012). Shanggong gold deposit, are found in the Xiong'ershan region in eastern Qinling within the southern margin of the NCC (Chen et al., 2008). In the Jibei region, northern margin of the NCC, the Xiaoyingpan quartz-vein 3. Metallogeny in the NCC gold deposit, the Dongping quartz-vein–altered–fracture transition type gold deposit, and the Jinchangyu quartz-vein gold deposit are 3.1. Spatial distribution of ore systems among the large-super large gold deposits. Apart from the gold deposits located along the margins of the NCC, some large scale gold deposits are During the prolonged tectonic evolution of the NCC, several types also found in the interior of the NCC. These include the Shihu auriferous of economic ore deposits formed at different times. Ore deposits of quartz-vein in the west of Hebei province within the central domain of Precambrian age, particularly nonferrous metallic deposits, are widely the Taihang Mountains (Li et al., 2013) and the Yixingzhai auriferous developed in the northern margin of the craton (Rui et al., 1994). quartz-vein in the northeast of Shanxi province, at the northern domain However, in this paper, we focus mainly on the mineralization that of the Taihang Mountains (Li et al., 2012). In the Luxi area, west of the formed subsequent to the cratonization of the NCC in an attempt to Tan–Lu fault zone, the Guilaizhuang cryptoexplosive breccia type gold evaluate their relationship with the decratonization event. deposit and the Yinan skarn type gold deposit have also been proved to be large scale with gold reserves of more than 20 t (Guo et al., 3.1.1. Gold 2013; Mao et al., 2005a,b). Gold is one of the most important mineral resources in the NCC. The major gold deposits are found in the Jiaodong peninsula (eastern Shandong province), the Xiaoqinling region (south-eastern Shaanxi 3.1.2. Molybdenum province and the west of Henan province) and the Jibei region Seventeen large and medium molybdenum deposits have been (northern Hebei province) (Fig. 4a). The Jiaodong peninsula has long identified in the NCC (Fig. 4b). The southern and northern margins of been known to host the largest cluster of gold deposits in China, and the craton are the main locations of the large ones. The Luanchuan– has been the major production in the country. The Xiaoqingling region Lushi area of Henan province in the central part of the southern margin

Fig. 3. Maps of mantle transition thickness (a) and lithosphere thickness and (b) beneath the NCC. After Zhu et al. (2011) with revisions. 382 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 of the NCC, hosts clusters of several important molybdenum deposits Hebei province within the northern margin of the NCC, is one of the in Asia, such as the Nannihu, Sandaozhuang, Shangfanggou and well-studied representatives. The Mesoproterozoic Dongshengmiao, Yechangping deposits. Recently, the molybdenum deposits of Laiyuan Tanyaokou, Huogeqi and Jiashengpan SEDEX deposits in the Langshan– in Hebei province in northern Taihang Mountains within the central Cha'ertaishan region, northern margin of the NCC, were discovered re- NCC are prospected as large molybdenum reserves (our unpublished cently with overprinting Variscanian mineralization (Zhai et al., 2004). data). The spatial distribution of the metallic deposits shows that not only the margins of the blocks/craton, but also the interior of the 3.1.3. Copper, lead and zinc NCC bear important metallic deposits. Notably, the important ore de- Copper deposits are not well developed in the NCC, with only a posits in the interior of the craton are mostly located in the Taihang few large deposits occurring in the west and northeast margins. How- Mountains (Li et al., 2012, 2013; Shen et al., 2013; Wang et al., ever, small scale copper deposits occur scattered in other margins and 2013), which defines the boundary between the Fuping, Ordos and in the cratonic interior (Fig. 4c, Zhao et al., 2006a). Qianhuai microblocks, as well as the collisional suture between the Until now, no super-large Pb–Zn–(Ag) deposits have been reported Western and Eastern Blocks (Santosh et al., 2012). A similar case in from the NCC. However, a number of large and middle scale Pb– the eastern NCC is the occurrences in the western part of the Tan– Zn–(Ag) deposits have been identified from the northern margin, with- Lu fault zone, which defines the boundary between the Qianhuai in the central segment of the southern margin and the interior region in and Jiaoliao microblocks (Fig. 4a–e). In the other basement bound- the Taihang Mountains (Fig. 4d, Zhao et al., 2006b). The Chaijiaying aries between the microblocks, only a few ore deposits are found. large scale Pb–Zn–Ag deposit located at the northwestern part of the In addition, within the same tectonic region, the ore deposits are

Fig. 4. Locations of ore deposits in the NCC. a — gold, b — molybdenum, c — copper, d — zinc–lead, and e — iron. S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 383

Fig. 4 (continued). scattered heterogeneously, such as for example in the southern mar- porphyry type gold deposits, such as the Zhulazhaga (280 Ma, Li et gin of the NCC, where the ore deposits are mainly clustered in the al., 2010) and the Bilihe (273 Ma, Qing et al., 2012) formed in the middle section. Inner Mongolia region, at the northern margin of the NCC. The third period is the middle Triassic, when the Qingchengzi gold–silver- 3.2. Chronology of metallogeny polymetallic deposits (ca. 239 Ma, Xue et al., 2003) in the Liaoning province formed along the north-eastern margin of the NCC. The 3.2.1. Gold mineralization fourth period is in the early Cretaceous, when a large number of Gold mineralization in the NCC formed mainly during 4 periods gold deposits formed in the northern, southern and eastern margins (Table 1). The ﬁrst phase is during Paleoproterozoic, when typical of the NCC. Most of the super-large gold deposits, such as those of orogenic gold deposits formed such as the Diantou (2416 Ma, Luo et Jiaodong represented by the Linglong quartz vein type (121 Ma, Li al., 2002), Xiaobanyu (2317 Ma, Luo et al., 2002), Dongyaozhuang et al., 2008), and the Jiaojia fracture-altered type (120 Ma, Li et al., (2451 Ma, Chen et al., 2001), Hulishan, Kangjiagou, Daiyinzhang, 2003), formed in the eastern margin of the NCC. Similar deposits in Shangyanghua, and Xiaozhongzhui ductile–brittle shear zone type the southern margin of the NCC include the Xiaoqinling quartz vein gold in the Wutai Mountain, northeast of Shanxi province, central gold deposits (127–129, Wang, 2010), and the Dongping-quartz NCC with ages ranging from 2.3 to 2.5 Ga (Zhang et al., 2003). vein-fracture altered gold deposit (140 Ma, Li et al., 2010) in the These gold deposits are all small scale with gold reserves less than north-western segment of the Hebei province. Notably, some large 10 t. The second period is the early to middle Permian, when some scale gold deposits also formed in the interior of the NCC. The Shihu 384 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

Fig. 4 (continued).

quartz vein gold deposit (130–140 Ma, Cao et al., 2012; Li et al., 2013) ductile–brittle shear zone type (the Dongyaozhuang type); 2) Perm- and the Yixingzhai quartz vein gold deposit (132 Ma, Li et al., 2012; ian porphyry-dominated type (the Bilihe type); 3) Jurassic (?) Ye et al., 1999) are two representatives in the central NCC. cryptoexplosive breccia type (the Guilaizhuang type); 4) Cretaceous quartz vein type (the Linglong type); 5) Cretaceous fracture altered type (the Jiaojia type); 6) Cretaceous strata-bound type (the Dujiaya 3.2.2. Molybdenum mineralization type); 7) Cretaceous skarn type (the Yinan type); 8) Cretaceous The molybdenum deposits in the NCC formed during three periods cryptoexplosive breccia type (the Qiyugou type) and 9) Cretaceous (Table 1). The first is in the early to middle Triassic, when some small quartz vein-fracture altered-type (the Dongping type). to medium scale molybdenum deposits formed in the northern and southern margins (223–258 Ma). There are only a few large scale molybdenum deposits such as the Sadaigoumen porphyry molybdenum 3.3.1.1. The Paleoproterozoic Dongyaozhuang type. This type includes deposit (238 Ma, Shen, 2011) in the north of Hebei province, and the the Dongyaozhuang, Diantou, Xiaobanyu, Hulishan, Kangjiagou, Dasuji porphyry molybdenum deposit (223 Ma, Zhang et al., 2009)in Daiyinzhang, Shangyanghua and Xiaozhongzhui gold deposits in the the Inner Mongolia Autonomous Region, the northern margin of the Wutai Mountain (Fig. 5a) in the central NCC. These deposits occur NCC. The second period is in the early–middle Jurassic when some within Archean greenstones, the protoliths of which are considered large scale molybdenum deposits formed at the north-eastern margin to be a suite of intercalated mafic and intermediate to felsic volcanics. of the NCC and a few small scale deposits developed in the southern Metamorphosed mafic and intermediate dykes also occur in the ore margin. The large molybdenum deposits are represented by the field (Fig. 5b). The greenstones and dykes underwent strong ductile Lanjiagou (187 Ma, Huang et al., 1996) and the Beisongshumao to brittle shearing and metamorphic hydrothermal alteration. From (162 Ma, Li et al., 2009) porphyry type deposits, as well as the the metamorphosed mafic rocks to the orebody, alteration zoning is Yangjiazhangzi (190 Ma, Huang et al., 1996) skarn type deposit in observed with carbonate–quartz–chlorite–albite marginal zone grad- the western part of Liaoning Province. The most important molybdenum ing into quartz–sericite–pyrite intermediate zone, and further to deposits formed in the third period during early Cretaceous in the south- tourmaline–pyrite–quartz core. Most of the orebodies are stratiform ern and northern margins, as well as in the interior of the NCC. The and consist of highly silicified and pyritic schist wall-rocks with fine Luanchuan porphyry type molybdenum deposits in the southern margin grained albite, sericite, quartz, tourmaline, ankerite, dolomite, calcite of the NCC including the Sandaozhuang (145 Ma, Mao et al., 2005a,b), and chlorite as common gangue minerals. Pyrite, chalcopyrite, pyr- Nannihu (142 Ma, Mao et al., 2005a,b, and Shangfanggou (144 Ma, rhotite, magnetite and native gold (occasionally arsenopyrite and Mao et al., 2005a,b) are among the major molybdenum deposits in chalcocite) are the main ore minerals. The ore is dominated by China. The skarn copper–molybdenum deposits, the Shouwangfen veinlet-disseminated style with gold grades ranging from 1 to 10 g/t deposit (148 Ma, Huang et al., 1996) and Xiaosigou deposit (134 Ma, with an average of 3.5 g/t. The fineness of the native gold is greater Huang et al., 1996) at the north-eastern margin of the NCC are also than 905 (Zhang et al., 2003; our unpublished data). well known. Recently, the Laiyuan porphyry–skarn copper–molybdenum deposits in the central NCC has proved to be an important deposit 3.3.1.2. The Permian Bilihe type. The Bilihe porphyry-dominated type based on drill core studies (our unpublished data). gold deposit is a newly found large scale gold deposit in the Sonid Youqi area (Qing et al., 2012). The deposit is located in the Caledonian 3.3. Ore deposit types accretionary orogen along the northern margin of the NCC. The Bainaimiao, Baiyinhe'er, Hedamiao and Baiyinchagan gold deposits 3.3.1. Gold ore systems are clustered nearby. A suite of Permian intermediate-felsic volcano- According to their nature of occurrence, the gold deposits in the sedimentary rocks (dated as 281.1 ± 4.3 Ma by zircon LA-ICP-MS NCC can be divided into the following types: 1) Paleoproterozoic U–Pb method, Qing et al., 2012) are the dominant rocks. I-type S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 385

Table 1 Isotopic ages of the major deposits in the NCC.

No. Deposit Location Species Age/Ma Method Mineral Reference

N. margin W. portion 1 Shalamiao Baiyun'ebo, Au 266.8 ± 3.9 Re–Os Molybdenite Wang et al., 2007 Inner Mongolia 2 Shibaqinghao Inner Mongolia 277 ± 1.73 40Ar–39Ar Biotite Chen et al., 1996 3 Bilihe Inner Mongolia 272.7 ± 1.6 Re–Os Molybdenite Qing et al., 2011 4 Zhulazhaga Alashan, Inner Mongolia 282.3 ± 0.9 40Ar–39Ar Quartz Li et al., 2010 5 Dongping Chongli, Hebei Province 187 ± 0.3 40Ar–39Ar K-feldspar Jiang et al., 2000 188 ± 0.4 177.4 ± 5 140.3 ± 1.4 LA-ICP-MS Zircon Li et al., 2010 6 Hougou Chicheng, Hebei Province 172.9 ± 5 40Ar–40Ar K-feldspar Wang et al., 1992 154.4 ± 1.3 LA-ICP-MS Zircon Li et al., 2012 7 Bieluwutu Sunite, Inner Mongolia Pb–Zn 279–481 Sm–Nd Nie et al., 2008 8 Chaganbulagen Xin Barag Left Banner, 131.6 K–Ar Pan et al., 1990 Inner Mongolia 9 Baiyinnuoer Bairin Left Banner, 170/161 Rb–Sr Zhang et al., 1991 Inner Mongolia 10 Haobugao Bairin Left Banner, Inner Yanshanian Dai et al., 2005 Mongolia 11 Caijiayingzi Zhangbei, Hebei 130 K–Ar Lv et al., 2004 12 Yingfang Fengning, Hebei 120.66 ± 3.16 K–Ar Liu et al., 1997, Duan et al., 2008 13 Sadaigoumen Fengning, Hebei Mo 227.1 ± 2.7 U-Pb Zircon Shen et al., 2011 14 Dacaoping Fengning, Hebei 220.10 ± 117 U–Pb Zircon Duan et al., 2007; ~232.17 ± 115 Hu et al., 2010 15 Yangshugou Fengning, Hebei 220.10 ± 117 U–Pb Zircon Duan.,2007 ~232.17 ± 115 Hu et al., 2010 16 Dasuji Zhuozi, Inner Mongolia 222.5 ± 3.2 Re–Os Molybdenite Zhang et al., 2009; Nie et al., 2012 Li.,2012 17 Caosiyao Xinghe, Inner Mongolia 131–134 U–Pb Granite Zhang et al., 2009; porphyry Nie et al.,2012; Li.,2012 18 Xishadegai Wulateqianqi, 225.4 ± 2.6 LA-ICP-MS Zircon Zhang et al., 2011 Inner Mongolia 19 Jiajiaying Zhangjiakou, Hebei 20 Baiyunebo Baotou, Neimenggu Fe 439 Re–Os Pyrite Zhang et al., 2008 21 Hongzhaoxiang Zhuozi, Neimenggu 1929 U–Pb Zircon Liu et al., 2010 E. portion 22 Niuxinshan Kuancheng, Hebei Province Au 175.8 ± 3.1 40Ar–39Ar Quartz Hu et al., 1996 23 Qingchengzi Fengcheng, Hebei Province 238.8 ± 0.3 40Ar–39Ar Quartz Xue et al., 2003 239.46 ± 1.13 40Ar–39Ar Quartz Xue et al., 2003 24 Bajiazi Fuxin, Hebei Province 204.0 ± 0.5 40Ar–39Ar Sericite Luo et al., 2002 25 Baiyun Fengcheng, Hebei 209 ± 2 40Ar–39Ar Quartz Liu et al., 2000 197 ± 2 26 Erdaogou Chaoyang, Liaoning 140.6 ± 2.8 40Ar–40Ar Sericite Pang et al., 1997 27 Xiaotongjiapuzi Liaoning 167.0 ± 2 40Ar–39Ar Sericite Liu et al., 2002 167.0 ± 4 40Ar–39Ar Sericite Liu et al., 2002 28 Wulong Dandong, Liaoning 120 ± 3 Rb–Sr Quartz Wei et al., 2001 112 ± 1 29 Paishanlou Fuxin, Liaoning 124.2 ± 0.4 40Ar–39Ar Biotite Yu et al., 2002 30 Siping Siping, Liaoning 187 ± 4 Rb–Sr Quartz Liang et al., 2001 31 Guanmenshan Kaiyuan, Liaoning Pb–Zn 467 Pb–Pb Fang et al., 1991 32 Yangjiazhangzi Jianchang, Liaoning 155–170 Pb–Pb Chen et al., 2003; Dai et al., 2005 33 Bajiazi Jianchang, Liaoning 177.4–183.8 Pb–Pb model Chen et al., 2003; age Dai et al., 2005 34 Beichagoumen Longhua, Hebei 138.5 ± 1.3 U–Pb Zircon Mao et al., 2005 35 Qingyanggou Chicheng, Hebei Yanshanian 36 Jiaodingshan Chengde, Hebei Yanshanian 37 Xiaodonggou Keshiketengqi, Mo 135.5 ± 1.5 Re–Os Molybdenite Nie et al., 2007 Inner Mongolia 38 Kulitu Chifeng, Inner Mongolia 210–230 Sr–Nd–Pb monzogranite Wu et al., 2008 39 Chehugou Chifeng, Inner Mongolia 257.5 ± 2.5 Re–Os Molybdenite Zhang etal.,2009 40 Jiguanshan Chifeng, Inner Mongolia 242.9 ± 2–256.9 ± 6.9 U–Pb Zircon Zhang etal.,2009 41 Nianzigou Chifeng, Inner Mongolia 154.3 ± 3.6 Re–Os Molybdenite Zhang etal.,2009 42 Hadamengou Chifeng, Inner Mongolia 239.76 ± 3.04 40Ar–39Ar sericite Nie et al., 2005 43 Xiaojiayingzi Kazuo, Liaoning 177 ± 5 40Ar–39Ar sericite Nie et al., 2005 44 Lanjiagou Liaoning 186.5 Re–Os Molybdenite Huang et al., 1996 45 Gangtun Huludao, Liaoning 46 Yangjiazhangzi West of Liaoning 190 ± 6 ~ 191 ± 6 Re–Os Molybdenite Huang et al., 1996 47 Beisongshumao West of Liaoning 162 Molybdenite Liu et al., 2009 48 Dazhuangke Yanqing, Beijing 146 ± 11 Re–Os Molybdenite Huang et al., 1996 49 Xiaosigou Cu, Mo Pingquan, Hebei 134 ± 3 Re–Os Molybdenite Huang et al., 1996 50 Shouwangfen Cu, Chengde, Hebei 148 ± 4 Re–Os Molybdenite Huang et al., 1996 Mo

(continued on next page) 386 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

Table 1 (continued) No. Deposit Location Species Age/Ma Method Mineral Reference

51 Huashi Chengde, Hebei 52 Huanggang Keerketengqi, Inner Mongolia Fe 135.31 ± 0.85 Re–Os Molybdenite Mao,2011 53 Zhoutaizi Luanping, Hebei 2460 U–Pb Zircon Xiang,2010 54 Damiaoheishan Chengde, Hebei 396 40Ar–39Ar Biotite Zhou et al., 2012 55 Xiaojiayingzi Kazuo, Liaoning 165.5 ± 4.6 Re–Os Molybdenite Dai et al., 2007 56 Zabuqi Ximen, Neimenggu 337 ± 1.5 U–Pb Zircon Deng,2012 57 Tiemahabaxin Chengde, Hebei 371 ± 11 40Ar–39Ar Hornblende Li et al., 2012 E. margin Jiaodong 58 Cangshang Laizhou, Shandong Au 121.3 ± 0.2 40Ar–39Ar Sericite Zhang et al., 2003 59 Jiaojia Laizhou, Shandong 120.5 ± 0.6 40Ar–39Ar Sericite Li et al., 2003 120.1 ± 0.2 120.2 ± 0.2 60 Wangershan Laizhou, Shandong 120.6 ± 0.7 40Ar–39Ar Sericite Mao et al.,2005 61 Xincheng Laizhou, Shandong 120.2 ± 0.3 40Ar–39Ar Sericite Mao et al.,2005 120.9 ± 0.3 62 Linglong Zhaoyuan, Shandong 122 ± 11 Rb–Sr Pyrite Yang and 123 ± 3 Zhou,2001 123 ± 4 63 Denggezhuang Yantai, Shandong 117.5 40Ar–39Ar Quartz Zhao et al., 1993 64 Dongji Shandong 116.1 ± 0.3 40Ar–39Ar K-feldspar Li et al., 2003 115.2 ± 0.2 Quartz 65 Pengjiakuang Rushan, Shandong 118.4 ± 0.3 40Ar–39Ar Quartz Zhang et al., 2002 120.5 ± 0.5 Quartz 117.5 ± 0.3 Biotite 66 Dazhuangzi Longkou, Shandong 117.4 ± 0.6 40Ar–39Ar Quartz Zhang et al., 2002 67 Rushan Rushan, Shandong 118.6 ± 0.6 Rb–Sr Phyllic Zhang et al., 1995 68 Wangjiazhuang Fushan, Shandong Pb–Zn 128–130 K–Ar Zhang et al., 2008 Luxi 69 Xiaoyao Yishui, Shandong Au 116 ± 20 LA-ICP-MS, Zircon Li et al.,2009 U–Pb 70 Guilaizhuang Pingyi, Shandong 188 ~ 178 40Ar–40Ar Hornblende Tan et al., 1993 71 Yinan Yinan, Shandong Fe 133 ± 6.0 Rb–Sr Biotite Hu et al., 2012 Liaodong 72 Qingchegnzi Fengcheng, Liaoning Pb–Zn 1500–1800 Pb–Pb model sulﬁde Lv et al., 2004 age 73 Zhangjiabaozi Fengcheng, Liaoning 1640–1764 Pb–Pb model sulﬁde Qu et al., 1989 age 74 Lvjiabaozi Fengcheng, Liaoning Yanshanian Dai et al., 2005 75 Dongsheng Xiuyan, Liaoning Yanshanian Dai et al., 2005 S. margin Xiaoqinling 76 Xiaoqinling Henan Province Au 128.5 ± 0.2 40Ar–39Ar Biotite Wang et al., 2002 126.7 ± 0.2 128.3 ± 0.3 40Ar–39Ar Biotite Wang et al.,2002 126.9 ± 0.3 77 Dongchuang Lingbao, Henan Pb–Zn 128–143 39Ar–40Ar Li et al., 2002; Li et al., 1997; Nie et al., 2001 78 Xizaogou Ruyang, Henan Yanshanian Yan et al., 2004 79 Shuidongling Nanzhao, Henan 440–646 Pb age pattern ore Wei et al., 2003 80 Banchang Neixiang, Henan 148.1 ± 1.6 39Ar–40Ar K-feldspar Li et al., 2008 81 Dahu Au, Mo Lingbao, Henan Mo 223 ± 2.8–232.9 ± 2.7 Re–Os Molybdenite Huang.2009 82 Quanjiayu Lingbao, Henan 129.1 ± 1.6, Re–Os Molybdenite Li,2007 130.8 ± 1.5 83 Majiawa Henan 232.5 ~ 268.4 Re–Os Molybdenite Wang et al., 2010 84 Yechangping Sanmenxia, Henan 85 Jinduicheng Huaxian, Shanxi 129 ± 7, 131 ± 4, Re–Os Molybdenite Huang,1994 139 ± 3 Xiong'ershan 86 Qiyugou Songxian, Henan Au 122 ± 0.4 40Ar–39Ar K-feldspar Wang et al., 2001 115 ± 2 125 ± 3 40Ar–39Ar K-feldspar Wang et al., 2001 114 ± 4 134.1 ± 2.3 LA-ICP-MS, Zircon Yao et al., 2009 U–Pb 135.6 ± 5.6 Re–Os Molybdenite Yao et al., 2009 87 Miaoling Songxian, Henan 121.6 ± 1.2 40Ar–39Ar K-feldspar Zhai et al., 2012 117.0 ± 1.6 40Ar–39Ar K-feldspar Zhai et al., 2012 88 Xiasongping Songxian, Henan 129 ± 45 Rb–Sr Pyrite Pang et al., 2011 89 Shangzhuangping Songxian, Henan Pb–Zn 508–574 Pb age pattern Ore Chen et al., 2005 90 Nannihu Luanchuan, Henan 141.5 ± 7.8 Re–Os Molybdenite Ye et al., 2006

91 Chitudian Luanchuan, Henan Pt3 Yan et al., 2002; Dai et al., 2005 92 Lengshuibeigou Luanchuan, Henan 136.13 ± 0.44 39Ar–40Ar Quartz isochron 93 Huanglongpu Luonan, Henan Mo 221 Re–Os Molybdenite Huang,1994 94 Sandaozhuang Mo, Luoyang, Henan 144.5 ± 2.2, Re–Os Molybdenite Mao et al., 2005 Wu 145.0 ± 2.2, 145.4 ± 2.0 95 Nannihu Luoyang, Henan 141.8 ± 2.1 Re–Os Molybdenite Mao et al., 2005 96 Shangfanggou Luoyang, Henan 143.8 ± 2.1, Re–Os Molybdenite Mao et al., 2005 145.8 ± 2.1 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 387

Table 1 (continued) No. Deposit Location Species Age/Ma Method Mineral Reference

97 Leimengou Songxian, Henan 131.6 ± 2.0, Re–Os Molybdenite Mao et al., 2005 131.1 ± 1.9 98 Huangshui'an Songxian, Henan 209.5 ± 4.2 Re–Os Molybdenite Huang.,2009 99 Qiushuwan Nanyang, Henan Interior Taihangshan 100 Nanzhaozhuang Laiyuan, Hebei Pb–Zn Yanshanian Dai et al., 2005 101 Lianbaling Laiyuan, Hebei Yanshanian 102 Nanzhaozhuang Laiyuan, Hebei Yanshanian Dai et al., 2005 103 Yintonggou Lingshou, Hebei Mo 104 Dawan Cu, Mo Laiyuan, Hebei 144 ± 7 Re–Os Molybdenite Huang et al. 1996 105 Futuyu Laiyuan, Hebei 106 Mujicun Laiyuan, Hebei Hengshan 107 Puziwan Wutai, Shanxi Au 142.9 ± 0.5 40Ar–39Ar Quartz Luo et al., 1999 142.5 ± 0.5 108 Yixingzhai Fanshi, Shanxi 130 40Ar–39Ar Quartz Ye et al., 109 Shihu Lingshou, Hebei Au 140 40Ar–39Ar Quartz Cao et al., 2012 Wutaishan 110 Dongyaozhuang Wutai, Shanxi 2451 Re–Os Molybdenite 111 Diangou Wutai, Shanxi 2456 ± 14 40Ar–39Ar 2416 ± 64 40Ar–39Ar 112 Xiaobanyu Daixian, Shanxi 2333 ± 10 40Ar–39Ar 2317 ± 63 40Ar–39Ar

Dabieshan 113 Yindongling Tongbo, Henan Pb–Zn Pz2 Yan et al., 2004

monzogranitic porphyry and granodioritic porphyry, dated at one (Qing et al., 2012). The alteration system associated with this de- 279.9 ± 4.2 Ma by zircon LA-ICP-MS U–Pb method (Qing et al., posit is remarkably similar to the classic porphyry deposits. Potassic 2012), are genetically related with the gold mineralization. An and silicic alteration zone is developed at the contact zone between integrated porphyry metallogenic system consisting of porphyry, the porphyry and the volcano-sedimentary rocks, especially in the cryptoexplosive breccia, fracture altered and quartz vein type gold lower part of the inner contact zone, with K-feldspar, quartz, magne- orebodies are recognized with the porphyry type as the dominant tite, rutile, barite and anhydrite as its mineralogical assemblage. A

Fig. 5. Regional geology and ore deposit distribution in the Wutaishan region (a) and the geology of the Dongyaozhuang gold deposit (b). 388 .R i .Snoh/OeGooyRves5 21)376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. – 414

Fig. 6. Regional geology and ore deposit distribution in the Jiaodong region (a), geology of the Linglong gold field (b), vertical profile perpendicular to main gold-veins in the Linglong gold field (c) and vertical profile perpendicular to ore-controlling fault in the Jiaojia gold deposit (d) (modified after Li et al., 2007). S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 389 quartz–sericite zone is mainly developed at the inner and outer con- breccias are present with large gold reserve in the Archean Taihua tact zones of the porphyry and the volcanic–sedimentary rocks and Group of gneiss and the Proterozoic Xiong'er Group of meta-andesite partially overprints the potassic and silica alteration zone, with in the southeast of the Cretaceous Huashan monzogranitic pluton. quartz, sericite, calcite, and pyrite as its typical mineralogical assem- Among these, more than 15 breccia pipes were found in the north- blage. The propylitic zone is broadly distributed in the volcanic westerly extending Qiyugou valley, eight of which are auriferous rocks with quartz, calcite, chlorite, epidote and pyrite as its main min- (Fig. 7b). The lentiform, tube-like or irregular orebodies are con- erals. Kaolinite alteration locally overprints the potassic and silica trolled by cryptoexplosive breccia pipes or belts (Fig. 7c). Within zone and the quartz–sericite zone. The low-S, low-Mo, low-Cu and and surrounding the breccia pipes, the alteration zones are repre- high-Au disseminated-veinlet orebodies are found mainly in the sented by: adularia–biotite–quartz in the core of the ore zone, and neighboring area of the contact zone. The lentiform orebody 1 in silica–chlorite at the margins of the pipe, followed by chlorite–epi- the ore belt II holds 90% of the gold resource with grades averaging dote–actinolite–albite–calcite in the andesitic wall rocks. The 2.73 g/t and bears a bonanza with ca. 10 t of gold reserve with a ore-forming processes can be divided into an early oxide mineral stage gold grade >15 g/t (Qing et al., 2012). The orebodies are dominated represented by quartz, and an iron sulfide stage represented by pyrite, by altered granodioritic porphyry ore, altered tuff and tuffaceous a middle polymetallic sulfide stage represented by chalcopyrite, galena sandstone ore, and altered andesite ore with veinlet-disseminated min- and sphalerite, and a late carbonate stage represented by calcite (Chen eralization style. The timing of the mineralization was constrained by et al., 2009b; Li and Shao, 1991; Shao et al., 1992). molybdenite Re–Os method to be 272.7 ± 1.6 Ma (Qing et al., 2012). 3.3.2. Molybdenum ore systems 3.3.1.3. The Cretaceous Linglong type. The Linglong-type quartz vein Porphyry and skarn types are the two most important molybde- gold deposits are developed in the eastern and southern margins as num deposit types in the NCC, especially in the northern and south- well as the interior of the NCC. In the eastern margin of the NCC, the rep- ern margins of the NCC. In the north-western and northern Hebei resentatives are the Linglong, Jinqingding and Denggezhuang deposits Province within the central section of the northern margin of the in the Jiaodong region (Fig. 6a, b, c). In the southern margin of the NCC, the Cretaceous Jiajiaying deposit and the Triassic Shadaigoumen NCC, the representatives are those in the Xiaoqingling region (Fig. 7a). deposit are well known large-scale porphyry molybdenum deposits. In the interior of the NCC, Shihu and Yixingzhai deposits in the Taihang The Cretaceous Dazhuangke deposit in Yanqing County, Beijing mu- Mountains also belong to this type. All these deposits occur in regions nicipality, is a large scale cryptoexplosive type molybdenum deposit with a Precambrian basement and Cretaceous intermediate-felsic in the central section of the northern margin of the NCC. In the intrusions. Their host rocks are Precambrian TTG rocks like those in south-western Liaoning Province within the north-eastern margin the Taihang Mountains (Li et al., 2012, 2013), Precambrian metamor- of the NCC, are the Jurassic Lianjiagou and Gangtun porphyry molyb- phic supracrustal rocks like those in the Xiaoqinling region (Luan denum deposits. In the southern margin of the NCC, are the Nannihu et al., 1991), or the Cretaceous granitoids like those in the Jiaodong re- large scale skarn-porphyry molybdenum deposits. Quartz vein or car- gion (Chen et al., 1989, 1993, 2012; Li et al., 1996). The orebodies bonate vein type molybdenum deposits were also found in the are prominantly controlled by vertical to sub-vertical faults with dip Luoning–Songxian area of the southern margin of the NCC but with angles greater than 65° and show multiple structural features from small scale resources (Rui et al., 1994). transpression to transtension. Alteration zoning is recognized with a zone of broad K-feldspar (30–50 m) at the margins, followed towards 3.3.2.1. The Triassic Sadaigoumen type. The Sadaigoumen molybdenum the auriferous quartz vein by narrow quartz–sericite–pyrite (QSP) deposit is located in the north of Fengning county, Hebei Province (Luo zone (b2m)(Chen et al., 1989, 2012; Li et al., 1996, 2012, 2013; Luan et al., 2010). It is one of the large scale molybdenum deposits in the et al., 1991). The hydrothermal mineralization phase can be divided Yan–Liao Mo (Cu) metallogenic zone along the northern margin of into four main stages: pyrite–quartz, quartz–pyrite, poly-metallic sul- the NCC. The deposit is closely associated with the Triassic reddish fide and quartz–carbonate. The orebodies are dominated by ores of monzogranite which occur within the Mesozoic grayish monzogranite banded and massive structures with gold grade ranging from 3 to and the Archean TTG gneiss. The outcrop of the reddish monzogranite 20 g/t with an average of about 6–9 g/t. The ore minerals are mainly occupies an area of about 0.9 km2. Geochemical studies revealed pyrite, chalcopyrite, galena, sphalerite, native gold, native silver, and that the monzogranite is metaluminous high-K calc-alkaline I-type, various telluride minerals. LREE-enriched with weak Eu negative anomalies (δEu = 0.78). The monzogranite is depleted with Nb, Ta, P, Zr, and Ti and enriched with 3.3.1.4. The Cretaceous Jiaojia type. The Jiaojia fracture-filling and al- Rb, Th, K, and Ba. The formation pressure of the monzogranite was esti- tered type gold deposits are mostly developed in the north-western mated to be 1.83 kbar, implying an emplacement depth of 6.78 km (Luo Jiaodong region in the eastern margin of the NCC (Fig. 6d). These et al., 2010). Typical hydrothermal alteration zones of porphyry type types of gold deposits are also found in the Xiaoqingling region and occur with a potassic zone in the core, followed outward by quartz– the Luoning–Songxian region in the southern margin of the NCC. Their sericite–pyrite and propylitic alteration zone. The Mo orebody extends geological setting is more or less the same as that of the Linglong for 700 m N–Sand960mE–W, with vertical extension of 275 m and type. The orebodies generally exhibit low dip angles (b45°). Broad showing average Mo grade of 0.059% (Shen, 2011). The ore is character- K-feldspar zone (10–50 m) in the margins followed towards the main ized by veinlets of molybdenite, pyrite and chalcopyrite. The minerali- fault by broad quartz–sericite–pyrite (QSP) zone (2–40 m) (Chen zation process can be divided into an early barren magnetite–quartz et al., 1989). The ore is characterized by highly pyrite–microquartz– stage, a pyrite–molybdenite–quartz stage and a late barren fluorite– sericitized rocks superposed with pyrite–quartz, quartz–pyrite and quartz–calcite stage. Re–Os isotopic dating of the molybdenite yielded polymetallic sulfide veinlets. The ore minerals are similar with those an age of 237 ± 4.1 Ma for the mineralization (Shen, 2011). of the Linglong type gold deposits. 3.3.2.2. The Jurassic Lanjiagou type. The Lanjiagou porphyry type molyb- 3.3.1.5. The Cretaceous Qiyugou type. The Qiyugou cryptoexplosive denum deposits are located in the southwest of Liaoning Province at the breccia gold deposits are developed in the Xiong'ershan region, south- north-eastern margin of the NCC, and are closely associated with ern margin of the NCC, the Wutai–Hengshan region, central NCC and Yanshanian (189 Ma, Dai et al., 2008) magmatic rocks which intruded the Luxi region, eastern margin of the NCC. The deposits in these areas into the Mesoproterozoic dolomitic limestone and the Early Paleozoic occur within Precambrian basement or volcanics, or Paleozoic sediment limestone and shale. The intrusive rocks consist of, according to their rocks. In the Xiong'ershan area, three clusters of auriferous explosive order of formation, coarse grained granite (SiO2 71.89%, Na2O/K2O 390 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 391

0.96, DI 88.5, δEu 0.44, Mo 12.43 ppm), ﬁne grained porphyritic granite porphyry type Mo deposits. The proven metal reserves exceed 2 Mt

(SiO2 76.09%, Na2O/K2O 0.82, DI 89.3, δEu 0.25, Mo 27.13 ppm) and gra- of Mo, 0.64 Mt of W, and 111 t of Re. The metal grades range from nitic porphyry (SiO2 76.73%, Na2O/K2O0.39,DI94.6,δEu 0.11, Mo 0.06‰ to 0.24‰ for Mo and from 0.09‰ to 0.13‰ for W (Li et al., 56.67 ppm) (Rui et al., 1994). The thick tabular orebodies occur at the 2003). The deposits are closely associated with Yanshanian (Late Cre- top and periphery of the fine grained porphyritic granite and are con- taceous) granitic stocks intruding the Neoproterozoic metamor- trolled by fractures and faults in the intrusive rocks. Ores of quartz vein phosed marine clastic and carbonate rocks of the Luanchuan Group. type, quartz veinlet type, and fracture altered type are common with mo- NNW to NW directed fractures are the major ore-controlling struc- lybdenite and pyrite as the major ore minerals and sphalerite, chalcopy- tures. The intrusive rocks evolved from granodiorite, monzogranite rite, galena, tetrahedrite, magnetite, argentite and native silver as the to granitic porphyry accompanied by mineralization, with Mo and minor minerals. The gangue minerals are mainly K-feldspar, plagioclase, W abundances several hundred times more than those of the average quartz, illite and calcite with minor rhodochrosite, siderite, chlorite and crustal values. The intrusive rocks are of high-K, alkaline-rich and fluorite. K-feldspathization, greisenization (quartz–white mica), silicifi- highly acidic nature. The orebodies occur mostly in the contact zone cation, illitization and Fe–Mn carbonitization and chloritization are com- of the intrusive rocks and in the strata-controlled skarn. Besides monly close to the orebodies. The mineralization period can be divided hornfelsization and skarnification in the contact zone and the weak into an early alteration sub-period, when K-feldspatic and greisen strata of the carbonate rocks, broadly superposed typical porphyry occurred, and a late sulfide sub-period, with three mineralization type alterations are strongly developed in the intrusive rocks. The ore stages: the early stage characterized by quartz (326 °C) + molybdenite types are dominated by skarn (>50%), hornfels (~40%) and granitic (317 °C) association; the middle stage characterized by quartz porphyry (~10%) (Li et al., 2003). The metallogenic process is character- (295 °C) + molybdenite (295 °C) + pyrite (265 °C) + galena associa- ized by an early anhydrous skarn stage, hydrous skarn–magnetite– tion; and the late stage characterized by quartz (235 °C) + molybdenite scheelite–molybdenite stage, middle quartz–molybdenite–pyrite– (212 °C) + illite association (Dai et al., 2007; Rui et al., 1994). chalcopyrite–sphalerite stage, and late quartz–calcite–fluorite stage. Molybdenite Re–Os isotopes yielded model ages of ~142 Ma for the 3.3.2.3. The Cretaceous Dazhuangke type. This deposit type includes the Nannihu Mo deposit, ~145 Ma for the Sandaozhuang Mo deposit and Dazhuangke and Dongjiagou explosive breccia type molybdenum de- ~145 Ma for the Shangfanggou Mo deposit. A Re–Os isochron age of posits located at the junction of the E–WYangyuan–Xifengkou–Jinzhou 142 Ma was obtained from 6 samples in the three deposits (Li et al., deep seated fault and the NNE–SSW Zhenglanqi–Fengning–Jurongguan 2003). deep seated fault at the northern margin of the NCC. Except for a few outcrops of the Mesoproterozoic carbonate rocks in the neighboring 3.3.3. Chaijiaying lead–zinc ore systems area, the deposits areas are mainly occupied by Late-Jurassic to Early The Chaijiaying stringer lode type lead–zinc deposit surrounded by Cretaceous intrusive and extrusive intermediate-felsic rocks. A few gold and molybdenum deposits in the well known Zhang–Xuan region cryptoexplosive breccias of about 1200–1700 m length, 200–700 m (Fig. 8a), is located to the north of a NEE directed fault of about 100 km width and >600 m vertical extension intruded into the quartz– length at the central-northern margin of the NCC. The orebodies are monzonitic porphyry and dioritic porphyrite. The brecciated and hydro- controlled by a series of fractures directed NWW, NNE and SWW. The thermally altered quartz–monzonite porphyry was dated of 147 Ma, and ore-hosting rocks are mainly Paleoproterozoic leptite, granulite and the unaltered porphyritic monzogranite was dated of 139 Ma (K–Ar, Rui gneiss (Fig. 8b). Part of the host rocks includes Late Jurassic volcanic– et al., 1994). The orebodies are tube-like or stratiform and occur within sedimentary rocks. Small scale Yanshanian granitic porphyry and the explosive breccias. Molybdenite is the main ore mineral accompa- quartz porphyry (134 Ma, K–Ar, Rui et al., 1994) dikes and stocks are nied with rare magnetite, chalcopyrite, sphalerite, pyrite, ilmenite, and exposed in the mining area. Two types of ores, early chlorite–sphalerite scheelite. The 2H1 molybdenite occurs as disseminations, fine stockwork, and late sericite–polymetallic, are recognized. The chlorite–sphalerite and as cementing material of the breccias with rhenium ranging from 13 type of ore is clustered and densely disseminated, and partially in vein- to 18.6 ppm. Re–Os isochron dating of the ore constrained the timing of lets, with numerous sphalerite, ferruginous sphalerite and aminor arse- mineralization at 137.6 ± 3.7 Ma (Liu et al., 2012).Thegangueminerals nopyrite and marcasite as well as galena, pyrrhotite and hematite. The consist mainly of the rock-forming minerals of the breccias and the hy- sericite–polymetallic type of ore occurs as clustered, disseminated or drothermal minerals with plagioclase, K-feldspar, quartz, biotite and in veinlets with galena, sphalerite and pyrite. The lead grade of the hornblende as the major ones and zeolite, epidote, apatite, zoisite, fluo- chlorite–sphalerite type of ore ranges from 0.01% to 0.2% with Pb/Zn ra- rite and sericite occurring in subordinate amounts. A zone of potassic tios ranging from 1/18 to 1/100, whereas the lead grade of the sericite– and silica alteration is developed within or nearby the molybdenum polymetallic type of ore ranges from 0.3% to 4% with Pb/Zn ratios from orebodies, bordered by a quartz–sericite–pyrite zone, and propylitization 1/0.5 to 1/4. Apart from lead and zinc, silver of 10 to 100 g/t and gold of in the outermost zone. The ore forming process can be divided into three 0.02 to 1 g/t are also estimated. The hydrothermal alteration is character- stages: molybdenite–magnetite–pyrrhotite–scheelite–K-feldspar–biotite ized by a sericitic zone at the center of the orebody, followed with pene- (460–380 °C); molybdenite–quartz–K-feldspar–biotite (350–280 °C); trative sericitic and chloritic alteration zones outwards. The decrepitation and quartz–pyrite–carbonate–zeolite–molybdenite (250–150 °C). The temperature of fluid inclusions in the metal minerals shows a range of salinities of the fluid inclusions are >20% NaCl equiv. and peak at 62% 200 to 350 °C (Hu et al., 2005; Rui et al., 1994; Wang et al., 2003). NaCl equiv. Daughter minerals in the polyphase fluid inclusions are ha- lite, sylvite and molybdenite (Ma et al., 2008; Rui et al., 1994). 3.4. Mantle contribution

3.3.2.4. The Cretaceous Nannihu type. The Nannihu skarn–porphyry 3.4.1. Northern margin of the NCC type Mo (W) is a super-large Mo (W) ore ﬁeld located in the Luanchuan county, Henan Province at the southern margin of the 3.4.1.1. Northwest of Hebei Province. The Zhang–Xuan (Zhangjiakou– NCC. This ore ﬁeld includes the Nannihu porphyry type Mo (W), Xuanhua) region, northwest of the Hebei Province, is host to a well Sandaozhuang skarn type Mo (W), Shangfanggou porphyry type Mo known ore district with more than 100 deposits and occurrences of (Fe) and Majuan, Shibaogou, Yuku, and Huangbeiling skarn or gold, molybdenum and lead–zinc (Wang et al. 2010). The Dongping,

Fig. 7. Regional geology and ore deposit distribution in the Xiaoqinling–Xiong'ershan region (a), geology of the Qiyugou gold deposit (b) and the vertical alteration–mineralization proﬁle of the No.4 explosive breccia pipe (c). Panel a is modiﬁed after Luo et al. (2000) and panels b and c are after Shao et al. (1992). 392 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

Fig. 8. Regional geology and ore deposit distribution in the northern margin of the NCC (a) and the geology of the Caijiaying lead–zinc deposit (b). Panel a is modiﬁed after Mao et al., 2005a. Panel b is modiﬁed from Wang et al., 2010).

the Xiaoyingpan and the Huangtuliang deposits are among the im- mineral would decrease by 20% (Ohmoto, 1972). Thus, the 32S-rich portant gold resources in this area. The Chaijiaying lead–zinc–silver, characteristics of the sulfide minerals in the northwest of the Hebei the Xiangguang manganese–silver and the Jiajiaying molybdenum Province was interpreted to be the result of alkali metasomatism represent large scale polymetallic deposits. Most of the gold deposits (Wang et al., 1992; Wang et al., 2010). Apart from the alkali metaso- occur within Archean metamorphic rocks and the Variscan alkaline matism and K-feldspathization of the wallrocks of some of the gold complex, whereas most of the polymetallic deposits are found in deposits (the Hougou, Zhongshangou, Huangtuliang, Xiping, Beigou, the Proterozoic cover sequences and the Mesozoic basin. Taogou, Zhaojiagou, Yujiazhuang, Xiashuangtai and Xialiangjiafang The δ34S values for the sulfide minerals from the Jurassic gold de- gold deposits, represented by the Dongping gold deposit) in this posits range from −24 ‰ to +5‰ with most of the values clustering area, the gold mineralization itself is considered to be genetically re- between −16‰ and −6‰ (Table 2; Fig. 9). Gold deposits of Early lated to the syenite. The quartz vein type and fracture-altered type Cretaceous age show δ34S values ranging from −16‰ to +6‰ with gold deposits in the Jiaodong peninsula, are developed with strong most values clustering between −13‰ and −4‰ (Wang et al., K-feldspathization, but the δ34S values of the sulfide minerals from 2010). The δ34S measurement of 49 sulfide mineral separates from the Jiaodong gold deposits range mainly from 5‰ to 10‰ which are the Chaijiaying lead–zinc deposit yield values ranging from 2.2 to predominantly rich in 34S. This implies that the δ34S values of the sul- 7.8‰, with an average of 5.2‰. Most of the sulfides from the silver fide minerals from the northwest of the Hebei Province mainly reflect and molybdenum deposits show δ34S values ranging from −4‰ to the source characteristics which are not in favor of mantle origin. Al- +8‰. The general trend in variation of the δ34S values for the sulfide though there is no marked difference in the sulfur isotopes between minerals is as follows: δ34Spy>δ34S cpy > δ34S sph > δ34Sgn the Jurassic and the Early Cretaceous gold deposits, the δ34S values (Wang et al., 2010), suggesting equilibrium sulfur isotopic fraction- show a slight increase, suggesting that deeper sources might have ation during the ore forming process. The average δ34S value of the been involved in the gold mineralization during Cretaceous. The sul- sulfide minerals is consistent with the total δ34S value of the fur isotope compositions of the sulfide minerals from the Mesozoic ore-forming fluid. In hydrothermal systems at 250 °C, for an increase gold and polymetallic deposits in the northwest Hebei Province are 34 in logarithm unit of fO2 or a unit of pH value, the δ S value of sulfide comparable with those from the Wulashan gold field in the western Table 2 Sulfur isotopic compositions of the ore deposits in the NCC.

No. Deposit Location Age/Ma Type S (‰) Ref.

δ34 S Range

N. margin W portion 1 Jiawula Au Bayannur, 2.6 −2.9–4.0 Guan et al., 2004 Inner Mongolia 2 Houshihua Au Hohhot, Inner Mongolia −3.3 Xu et al., 1998; Xu,1991 3 Songshubei Au Hohhot, Inner Mongolia −3.7 −3.3 to −4.1 Xu et al., 1998 4 Donghuofang Au Hohhot, Inner Mongolia 3.1 2.6–3.7 Xu et al., 1998; Xu et al., 1991 5 Bayinhanggai Au Hohhot, Inner Mongolia −6.1 −8.3 to −0.5 Chen et al., 2001 6 Dayingzi Au Zhangbei, Hebei −0.5 The third geological team of Heibei 7 Jinjiazhuang Au Zhangjiakou, Hebei 181.9 Fracture-altered 1.9 –1.4–5.0 Province (1998), Wang etal, 1992; 8 Dongping Au Zhangjiakou, Hebei 187 ± 0.3, 188 ± 0.4, Fracture-altered −8.1 −5.5 to −13.5 Jin and Dui,1991; Song et al., 1994; 177.4 ± 5, 140.2 ± 1.3 Peng et al., 1992; Wang et al., 2010; 9 Shuijingtun Au Chongli, Hebei −10.4 Bao et al., 1996;Yu et al., 1989 10 Zhongshangou Au Chongli, Hebei 155.47, 115.1 −16.1 −23.8 to −11.1 .R i .Snoh/OeGooyRves5 21)376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. 11 Huangtuliang Au Chicheng, Hebei 120.63 Fracture-altered −5.0 −1.6 to −7.4 12 Hougou Au Chicheng, Hebei 172.9 ± 5, 154.4 ± 1.3 Fracture-altered −10.4 −3.5 to −15.95 E portion 1 Haolaibao Au Chifeng, Inner Mongolia 4.6 4.1–4.8 Wang et al., 2010 2 Wunuketushan Au Hulun Buir, Inner Mongolia 2.8 −0.2–4.2 Guan et al., 2004 3 Badaguan Au Hulun Buir, Inner Mongolia 2.6 0.5–4.8 Guan et al., 2004 4 Huashi Au Chengde, Hebei 3.7 3.0–4.3 Wang et al., 2010; Niu et al., 2001 5 Dongzigou Au Chengde, Hebei 1.3 −0.5–4.9 Wang et al., 2010; Yang et al., 1996; You Se Pu Cha Da Dui,1996 6 Xiajinbao Au Pingquan, Hebei 2.8 0.4–7.4 Shao et al., 1987;Luan et al., 1996 7 Tianjiacun Au Tangshan, Hebei 1.9 Wang et al., 2010 8 Malanguan Au Tangshan, Hebei 3.3 1.1–6.7 Song et al., 1994 9 Jinchangyu Au Qianxi, Hebei 2661, 2391, 2190 ± 58 Quartz vein −1.8 −6.3–3.1 Lin et al., 1985; Yu, 1989; Zhang, 1996 10 Yu'erya Au Kuancheng, Hebei Quartz vein 2.7 1.6–4.5 Chai et al., 1989; Song et al., 1994; Wang et al, 2010; Lin et al,1985; Zhang et al, 1996 11 Tangzhangzi Au Kuancheng, Hebei Breccia 2.9 0.7–5.7 Wang et al., 2010; Song et al., 1994; Niu et al., 2001 12 Huzhangzi Au Kuancheng, Hebei −11.3 −15.3 to −7.3 Wang et al., 2010

13 Shapoyu Au Kuancheng, Hebei 2.6 Wang et al., 2010 – 414 14 Baimiaozi Au Kuancheng, Hebei 3.3 Wang et al., 2010 15 Sajingou Au Kuancheng, Hebei 1.9 Wang et al., 2010 16 Maoshan Au Zunhua, Hebei 6.4 5.2–8.3 Bai et al., 1990; Shao et al., 1987; Luan et al., 1996 17 Niuxinshan Au Qinhuangdao, Hebei 5.5 4.3–6.3 Xu et al., 1987; Song et al., 1994 18 Maojiadian Au Lingyuan, Liaoning −6.2 Wang et al., 2010 19 Wangjiadagou Au Qingyuan, Liaoning 3.6 2.1–6.1 Yu et al., 2005 20 Hongshi Au Yixian, Liaoning 0.6 −32.7–17.4 Yin et al., 1994 21 Erdaogou Au Beipiao, Liaoning 0.8 −2.2–5.1 Xu et al., 2007; Liu et al., 2002 22 Jinchanggouliang Au Beipiao, Liaoning −5.0–1.5 Li et al., 1990; Liu et al, 2002 23 Shuiquan Au Beipiao, Liaoning 0.3 −7.6–1.9 Wang et al., 2009 24 Dongwujiazi Au Chaoyang, Liaoning 1.9–3.1 Xu et al., 2010 25 Qinglonggou Au Huludao, Liaoning 7.7 Yao et al., 2004 E. margin Jiaodong 1 Jiaojia Au Jiaodong, Shandong 120.5 ± 0.6, 120.1 ± 0.2, Fracture altered 10.3 7.8–11.8 Wang et al., 2001; Wang et al., 1991; 120.2 ± 0.2 Ding et al., 1998; Lin et al., 1999; 15.7 7.9–11.8 Wen et al., 1990; Yao et al., 1990 2 Linglong Au Zhaoyuan, Shandong 122 ± 11, 123 ± 3, 123 ± 4 Quartz vein 5.8 2.9–8.2 Cui et al., 2012 6.9 4.5–8.5 Wang et al., 2002; Yang et al., 2000; Yang et al., 1998; Guan et al., 1997; Yao et al,1990; Liu et al,1987; 393 Wen et al, 1990

(continued on next page) 394

Table 2 (continued) No. Deposit Location Age/Ma Type S (‰) Ref.

δ34 S Range

3 Pengjiakuang Au Jiaodong, Shandong 118.4 ± 0.3, 120.5 ± 0.5, Strata-bound 11.2 9.7–11.5 Sun et al., 1995; Zhang et al., 1999; 117.5 ± 0.3 Zhao et al,2000; Zhang et al,2001; Chen et al,1997; 4 Xiadian Au Zhaoyuan, Shandong Fracture-altered 7.8 7.4–8.0 Chen et al., 1989; Deng et al., 2000 5 Dazhuangzi Au Longkou, Shandong 117.4 ± 0.6 Strata-bound 10.6 Zhang et al., 2002; Zhu et al., 1999 6 Dujiaya Au Jiaodong, Shandong Strata-bound 5.5 −14.0–15.1 Yan et al., 2012 7 Denggezhuang Au Jiaodong, Shandong 117.5 Quartz vein 9.7 8.0–10.8 Ying et al., 1994; Yang et al., 2000 8 Fayunkuang Au Yantai, Shandong Strata-bound 13.1 Zhang et al., 2001; .R i .Snoh/OeGooyRves5 21)376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. 9 Penglai–Qixia Au Yantai, Shandong 5.7 −14.2–9.9 Wang et al., 2002 10 Yigezhuang Au Zhaoyuan, Shandong Fracture-altered 7.1 5.9–8.9 Huang et al., 1994; Chen et al., 1989; Deng et al., 2000 12 Majiayao Qixia, Shandong Quartz vein 4.9 1.4–8.6 Chen et al, 1989; Wang et al, 2002; Li et al., 1990 13 Wang'ershan Au Laizhou, Shandong 120.6 ± 0.7 Quartz vein 7.8 6.7–10.0 Wang et al., 2002 14 Lingshangou Au Zhaoyuan, Shandong Quartz vein 7.4 Wang et al., 2002; Lin et al., 1999; Yao et al, 1990 15 Liukou Au Qixia, Shandong Quartz vein 7.4 7.0–7.9 Chen et al., 1989 16 Bailidian Au Qixia, Shandong Quartz vein 5.9 Wang et al., 2002 17 Panzijian Au Qixia, Shandong Quartz vein 6.2 Wang et al., 2002; Yao et al., 1990 18 Fushan Au Zhaoyuan, Shandong Quartz vein 7.0 Wang et al., 2002; Lin et al., 1999; Yao et al,1990 19 Jinchiling Au Zhaoyuan, Shandong Quartz vein 4.0 Wang et al., 2002; Yao et al., 1990 20 Taishang Au Zhaoyuan, Shandong Fracture-altered 8.0 Chen et al., 1989; Deng et al., 2000 21 Qibaoshan Au Wulian, Shandong 2.5 Qiu et al., 1996; Chen et al., 1992; Wang et al., 1991 22 Hexi Au Penglai, Shandong Fracture-altered 8.2 7.4–8.8 Hou et al., 2004 − –

23 Congjia Au Rushan, Shandong 0.3 5.7 6.3 Wen et a,1990 – 24 Daliujia Au Qixia, Shandong −9.5 −9.7–9.3 Yao et al., 1990 414 25 Jiudian Au Pingdu, Shandong Quartz vein 7.6 4.9–9.3 Wang et al., 1982; Lin et al., 1990; Qiu et al., 1988 26 Xincheng Au Laizhou, Shandong 120.2 ± 0.3, 120.9 ± 0.3 Fracture-altered 9.5 7.9–10.7 Wang et al., 2002; Yao et al., 1990 27 Sanshandao Au Jiaodong, Shandong Fracture-altered 11.5 10.0–12.6 Wang et al., 2002 28 Cangshang Au Laizhou, Shandong 121.3 ± 0.2 Fracture-altered 10.8 9.6–12.0 Huang et al., 1994 29 Cangshang Au Laizhou, Shandong 11.6 Wang et al., 2002 30 Dongji Au Laizhou, Shandong 116.1 ± 0.3, 115.2 ± 0.2 Fracture-altered 11.3 Huang et al., 1994 31 Longbu Au Laizhou, Shandong 9.8 Wang et al., 2002 32 Matang Au Laizhou, Shandong Fracture-altered 9.4 5.6–10.7 Huang et al., 1994; Wang et al., 2002 33 Hongbu Au Laizhou, Shandong Fracture-altered 8.9 4.8–10.9 Huang et al., 1994 34 Hexijin Au Zhaoyuan, Shandong Fracture-altered 8.0 Huang et al., 1994; Wang et al., 2002; Hou et al., 2004 35 Jiehe Au Jiaodong, Shandong Fracture-altered 9.4 8.7–10.3 Wang et al., 2002 36 Shangzhuang Au Zhaoyuan, Shandong Fracture-altered 9.9 9.1–10.5 37 Wangjiagou Au Yantai, Shandong Fracture-altered 9.2 38 Hedong Au Zhaoyuan, Shandong Fracture-altered 10.3 9.3–10.8 39 Fujia Au Zhaoyuan, Shandong Fracture-altered 10.1 40 Wasunjia Au Zhaoyuan, Shandong Fracture-altered 4.8 −0.2–6.8 41 Qiansunjia Au Zhaoyuan, Shandong Fracture-altered 5.3 42 Huangbuling Au Zhaoyuan, Shandong Fracture-altered 7.8 7.0–8.8 43 Beijie Au Zhaoyuan, Shandong Fracture-altered 9.1 7.6–9.7 44 Longhudou Au 6.8 45 Luanjiahe Au Zhaoyuan, Shandong 2.4 −1.3–6.0 46 Dongqujia Au 4.9 47 Caogoutou Au Zhaoyuan, Shandong Fracture-altered 6.3 48 Caojiawa Au Zhaoyuan, Shandong Fracture-altered 7.0 49 Jianli Au Pingdu, Shandong Fracture-altered 8.4 50 Chijia Au Yantai, Shandong 3.7 51 Tengjia Au Rongcheng, Shandong 5.8 52 Chengkuo Au 3.7 53 Nanshu Au Laixi, Shandong Fracture-altered 6.7 54 Xilin Au Qixia, Shandong 6.9 55 Lingnan (Taishang) Au Zhaoyuan, Shandong 8.0 Chen et al., 1989 56 Heilangou Au Penglai, Shandong Fracture-altered 6.7 5.8–7.8 Chen et al., 1989 57 Jinqingding Au Jiaodong, Shandong Quartz vein 8.6 6.8–9.7 Chen et al., 2010 58 Dayigezhuang Au Jiaodong, Shandong Fracture-altered 6.4 5.9–7.0 Wang et al., 2012 59 Canzhuang Au Jiaodong, Shandong Fracture-altered 6.8 5.3–7.6 Yan et al., 2012 60 Lingqueshan Au Zhaoyuan, Shandong Quartz vein 7.8 Zhen et al., 2006 Luxi 1 Jinchang Au Yinan, Shandong 2.8 1.9–3.5 Qiu et al., 1996 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. 2 Buwa Au Mengyin, Shandong Fracture-altered 2.1–4.1 Zang et al., 1998 3 Guilaizhuang Au Pingyi, Shandong 188–178 Explosive-breccia 2.4 2.0–3.0 Liu et al., 1994 4 Mofanggou Au Pingyi, Shandong Explosive-breccia −0.7–3.0 Hu et al., 2004 S. margin Xiaoqinling 1 Jinlongshan Au Zhen'an, Shaanxi 9.5 −4.2–19.8 Lv et al., 2012 2 Qiuling Au Zhen'an, Shaanxi 15.3 11.1–19.8 Shen et al., 1996 3 Xiong'ershan Au Shangluo, Shaanxi Quartz vein 2.4 −5.0–5.0 Lu et al., 2003; Chen et al., 1995 4 Dongtongyu Au Tongguan, Shaanxi Province 6.5 3.5–12.9 Lu et al., 2004 5 Xitongyu Au Tongguan, Shaanxi −7.7 −11.4 to −0.2 Lu et al., 2004 6 Chengjiagou Au Tongguan, Shaanxi −6.1 −9.3 to −2.4 Lu et al., 2004 7 Bayuan Au Lam Tin, Shaanxi Quartz vein 3.7 2.3–4.6 Lu et al., 2004 8 Tongyu Au Tongguan, Shaanxi Quartz vein 2.7 −8.7–5.7 Yu et al., 1989 9 Wenyu Au Lingbao, Henan Quartz vein 3.0 5.4–6.6 Xu et al., 1992 10 Dongchuang Au Lingbao, Henan 132.16 ± 2.64, 132.55 ± 2.65 Quartz vein 1.1 −2.8–5.8 Fan et al., 2012 11 Jindongcha Au Lingbao, Henan Quartz vein −0.9 −12.5–8.2 Lu et al., 2004 12 Yangzhaiyu Au Lingbao, Henan 113.72 ± 2.27, 114.26 ± 2.29 Quartz vein 2.4 −14.7–7.1 Lu et al., 2004 13 Lianggancha Au Lingbao, Henan Quartz vein 0.6 −7.6–5.5 Lu et al., 2004 14 Qiangmayu Au Lingbao, Henan Quartz vein 5.7 −0.7–9.2 Lu et al., 2004 15 Linghu Au Lingbao, Henan Quartz vein 1.8 −8.7–15.3 Lu et al., 2004 – 16 Dahu Au Lingbao, Henan Quartz vein −3.3 −8.1–1.3 Lu et al., 2004 414 17 Tonggou Au Lingbao, Henan Quartz vein −4.7 −28.5–3.6 Lu et al., 2004 18 Shenjiayao Au Shanxian, Henan Fracture-altered 3.6 0.4–5.9 Lu et al., 2004 19 Bankuan Au Yingxian, Henan Quartz vein 2.0 −12.1–8.5 Lu et al., 2004 20 Hongtuling Au Lingbao, Henan Quartz vein 0.5 −2.8–2.7 Lu et al., 2004 Xiong'ershan 1 Qianhe Au Songxian, Henan Quartz vein −13.3 −11.9 to −14.6 Li et al., 1999 2 Xiaonangou Au Songxian, Henan Fracture-altered −13.1 −16.6 to −9.5 Zhu et al., 1998 3 Qiyugou Au Songxian, Henan 122 ± 0.4, 115 ± 2, 125 ± 3, Explosive-breccia −0.8 −3.5–1.7 Wang et al., 1996 114 ± 4, 134.1 ± 2.3, 135.6 ± 5.6

(continued on next page) 395 396 Table 2 (continued) No. Deposit Location Age/Ma Type S (‰) Ref.

δ34 S Range

−0.4 −2.0–2.7 Shao et al., 1996 4 Pasigou Au Songxian, Henan 4.9–8.4 Xu et al., 2005 5 Xiaogongyu Au Songxian, Henan −1.0–2.1 Guo et al., 2008 6 Huanxiangwa Au Songxian, Henan −9.1 −16.8–0.6 Gao et al., 2010 7 Dianfang Au Songxian, Henan Explosive-breccia 4.8 −6.4–9.2 Lu et al., 2004 8 Yaogou Au Songxian, Henan Fracture-altered −4.3 −9.7–1.8 Lu et al., 2004 9 Beiling Au Songxian, Henan Fracture-altered −6.8 −10.2 to −0.6 Lu et al., 2004 10 Shagou–Yuelianggou Au Songxian, Henan 0.7 −8.1–6.1 Lu et al., 2004 11 Songpinggou Au Luoning, Henan Quartz vein 1.5 −9.4–9.8 Lu et al., 2004 12 Jinjiawan Au Luoning, Henan Fracture-altered −10.0 −10.9 to −9.1 Lu et al., 2004 13 Qinggangping Au Luoning, Henan −1.1 −8.7–4.2 Lu et al., 2004 14 Hugou Au Luoning, Henan −10.1 −28.2–7.9 Lu et al., 2004 15 Qiliping Au Luoning, Henan 9.4 8.5–10.7 Lu et al., 2004 16 Tieluping Au Luoning, Henan Fracture-altered −5.0 −8.8 to −1.4 Lu et al., 2004 17 Shanggong Au Luoning, Henan Fracture-altered −8.4 −19.2–6.7 Lu et al., 2004 18 Hongzhuang Au Luanchuan, Henan Quartz vein 4.0 −2.2–7.6 Lu et al., 2004 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. 19 Kangshanxingxingyin Au Luanchuan, Henan 4.1 −7.4–7.3 Lu et al., 2004 20 Laowan Au Tongbai, Henan Fracture-altered 4.0 −0.1–5.3 Chen et al., 2009 Other 1 Baguamiao Au Fengxian, Henan Quartz vein 10.7 7.4–15.4 Wu et al., 1999 2 Linxiang Au Xunyang, Henan 16.0 14.0–18.2 Zou et al., 2001 Interior Taihangshan 1 Shihu Au Lingshou, Hebei 132, 121.08, 119.93 Quartz vein 2.4 −0.4–3.0 Ao et al., 2009 2 Qiubudong Au Pingshan, Hebei 4.4 Wang et al., 2010 3 Xishimen Au Lingshou, Hebei 0.6 −0.3–1.4 Wang et al., 2010 4 Jiujizhuang Au North Taihangshan 2.3 1.7–5.0 Geng et al., 1997 5 Luanmuchang Au Yixian, Hebei 0.7 0.3–1.1 Chen et al., 1990 6 Konggezhuang Au Yixian, Hebei 6.1 4.3–7.2 Wang et al., 2010 7 Chounikou Au Lingshou, Hebei 1.6 Wang et al., 2010 8 Beiyingxigou Ag, Pb, Zn Lingshou, Hebei −4.5 −11.4–2.2 Wang et al., 2012 Wutaishan 1 Qitu Au Wutai, Shanxi 2.9 2.3–3.6 Yang et al., 2001 2 Diantou Au Wutai, Shanxi 2456 ± 14, 2416 ± 64 4.2 3.9–4.6 Tian et al., 1991 3 Dongyaozhuang Au Wutai, Shanxi 1.0–2.4 Tian et al., 2000 4 2.7 1.0–5.7 Tian et al., 1998 5 Xiaobanyu Au Wutai, Shanxi 2333 ± 10, 2317 ± 63 −0.1 −0.2–0.1 Wang et al., 1996 6 Yixingzhai Au Fanshi, Shanxi 131.4 ± 1.3 Quartz vein 1.4 −2.1–3.4 Luo et al., 2009 –

−0.9–4.4 Jing et al., 1992 414 3.2 −0.8–5.6 Tian et al., 1991 2.5 2.0–3.0 Zhang et al., 2009 7 Majiacha Au Fanshi, Shanxi 0.5 −8.1–2.4 Tian et al., 1991 Hengshan 1 Gengzhuang Au Fanshi, Shanxi Explosive-breccia 2.5 0.2–3.7 Huang et al., 2004 0.5–3.6 Li et al., 1988 3.9 1.6–4.5 Li et al., 1994 2 Tainashui Au Lingqiu, Shanxi 0.2 Tian et al., 1991 3 Lugou Au Lingqiu, Shanxi Quartz vein −0.1 −4.2–2.7 Tian et al., 1991 4 Hulishan Au Yuanping, Shanxi 0.3 −3.7–5.6 Chang et al., 1998 5 Gaofan Au Daixian, Shanxi 1.5 −3.3–2.7 Tian et al., 1991 0.7 −5.4–3.5 Gao et al., 2004 6 Xishandi Au Yuanping, Shanxi 3.7 Yang et al., 2001 7 Diaoquan Ag, Au, Cu Lingqiu, Shanxi Skarn 3.4 0.5–5.7 Li et al., 1994 Other 1 Puziwan Au Yanggao, Shanxi 142.9 ± 0.5, 142.5 ± 1.5 Explosive-breccia −0.1 −3.2–5.3 Cao et al., 2000 3.9 2.2–5.2 Long et al., 2011 0.0 −3.2–1.5 Zhang et al., 2001 2 Dongfengding Au Xiangfen, Shanxi 4.2 2.7–5.7 Yao et al., 2004 6.9 −1.9–29.4 Wang et al., 2009 −1.0 −9.4–5.7 Zeng et al., 1991 W. margin 1 Niutougou Au Shizhuishan, Ningxia Fracture-altered 4.9–6.8 Li et al., 2010 2 Jinchangzi Au Zhongwei, Ningxia 3.8–6.7 Zhou et al., 1993; Zhong et al., 2012 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 397

Fig. 9. Sulfur isotopic composition histograms of sulﬁde minerals from the ore deposits in the NCC.

18 Baotou area within the Inner Mongolia Autonomous Region along the Hebei Province show a relatively large range with δ Osmow varying 18 north-western margin of the NCC, where the gold deposits yield from 4.9‰ to 18.77‰, δ OH2O from −3.14‰ to 7.31‰, and δDsmow δ34S values ranging from −7.9‰ to −18.4‰ with an average from −109.5‰ to −80.5‰ (Table 5). The oxygen isotopic composi- 18 of −14.98‰ (Wei et al., 1993). tions of the fluid δ OH2O were calculated from that of quartz 18 6 −2 The lead isotopes of the Jurassic to Cretaceous gold, silver and δ OSMOW with the equation 1000lnαQ–W = 3.38 × 10 T − 3.40 lead–zinc deposits in the northwest of Hebei Province show a rela- (Clayton et al., 1972), where T represents the homogenisation tem- 207 204 tively large variation with Pb/ Pb ranging from 15.13 to 15.54. perature of fluid inclusions. It is noted that the δDSMOW values are 206Pb/204Pb and 208Pb/204Pb values show limited ranges of 16.31– markedly lower than that of the typical metamorphic water (−65‰ 17.64 and 36.22–37.72, respectively (Table 3; Fig. 10). Plotting of to −20‰, Hugh and Taylor, 1974). In the δD versus δ18O diagram the data on the Zartman's diagrams suggests that lead of the ores for fluids from various ore deposits in the northwest of Hebei Prov- was derived from multiple sources including mantle and the lower ince (Fig. 11), all the plots fall below the primary magmatic water as well as upper crust, although most of the data plot in the orogenic and shift slightly towards the region for meteoric water, suggesting field. that magmatism played an important role in the mineralization Source tracing with silicon isotope systematics has also been (Hugh and Taylor, 1974). 13 attempted. Molini-Velsko et al. (1986) obtained the isotopic composi- The δ CPDB data of the carbonate minerals from the ore deposits in tion of silicon in meteorites which shows a δ30Si range of −1.8‰ to the northwest of Hebei Province range between −6.0‰ and −2.5‰ 13 0.3‰ with an average of −0.5‰. Ding and Jiang (1994) compared (Table 5). The δ CPDB value of mantle carbon is around −5‰ and the silicon isotopic composition of the granites from China and that of magmatic carbon is within the range of −9‰ to −3‰ (Taylor North America, which show δ30Si values ranging from −0.4‰ to and Bucher-Nurminen, 1986). The carbon from sedimentary carbonate 0.4‰, peaking at −0.1‰, and with an average of −0.12‰. Analyses rocks or from the interaction between brine and argillite is character- 13 of 23 siliceous sediment samples from the black chimney in the ized by heavy carbon isotope with the δ CPDB values in the range of 30 13 Mariana trench yielded δ Si values ranging from −0.4‰ to 3.1‰ av- −2‰ to +3‰;theδ CPDB data of marine carbonate rocks are ca. 0‰ eraging −1.6‰ (Wu, 1995). Analyses of 27 quartz, intrusive rocks (Veizer et al., 1980). Organic carbon is characterized by lighter carbon 13 and gneiss samples from the northwest of Hebei Province yielded enrichment with δ CPDB values varying from −30‰ to −15‰ and 30 13 δ Si values of −0.2‰ to 0.3‰ with an average −0.05‰ for the an average of −22‰ (Ohmoto, 1972). Comparing the δ CPDB data ore-bearing quartz vein (Table 4; Wang et al., 2010; Lu and Wang, from different sources, the carbon isotope values reported from the 1992; Yin, 1995), −0.3‰ to 0.4‰ with an average of 0.05‰ for the in- ore deposits in the northwest of Hebei Province is close to those trusive rocks, and 0.6‰ for an Archean gneiss sample (Lu and Wang, mantle-derived magmatic sources. 1992). The δ30Si data of the quartz and intrusive rocks from the study Wang et al. (2010) measured the helium and argon isotopic com- area are consistent with those of the granitoids in China and else- positions of 23 pyrite, galena, sphalerite, and quartz samples from un- where. The δ30Si data of the quartz from the study area are also with- derground levels of 10 gold, silver, and lead–zinc deposits and 2 in the δ30Si range of the meteorite, implying that at least part of the granite samples from the Dongping gold field in the northwest of silicon was derived from magmas sourced from the mantle. Since Hebei Province (Table 6). The 3He/4He values of the sulfide minerals only one analysis is available for the Archean gneiss, its contribution and quartz are in the range of 0.38 × 10−6 to 9.47 × 10−6 (0.27Ra to the hydrothermal silicon cannot be excluded. to 6.81Ra, where Ra is the 3He/4He ratio of air = 1.39 × 10−6), The mean values of the hydrogen and oxygen isotopes of fluids much higher than those of the granite samples (0.007 × 10−6 to trapped in the quartz from various ore deposits in the northwest of 0.008 × 10−6, 0.005 Ra–0.006 Ra). With the equation formulated by 398

Table 3 Lead isotopic compositions of the ore deposits in the NCC.

No. Deposit Location Age/Ma Type Pb Ref.

206 Pb/204 Pb 207 Pb/204 Pb 208 Pb/204 Pb

N.margin W-M.portion Au 1 Ulantolgoi Bayannao'er, Inner Mongolia Porphyry 18.48 15.66 38.33 Qiu et al., 1994 2 Saiwusu Baotou, Inner Mongolia 16.84 15.39 37.24 Wang et al., 2010 3 Wulashan Baotou, Inner Mongolia 230 17.69 15.59 38.11 Xu et al., 1991 4 Shibaqinghao Guyang, Inner Mongolia 277 ± 1.73 17.93 15.57 38.66 Xu et al., 1991 5 Houshihua Hohhot, Inner Mongolia Ductile shear zone 17.09 15.56 37.58 Shi et al., 1993 6 Donghuofang Hohhot, Inner Mongolia 237 Far contact zone 18.93 16.01 39.73 Xu et al., 1998 7 Bayinhanggai Hohhot, Inner Mongolia 18.11 15.55 38.11 Yang et al., 2001 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. 8 Bainaimiao Hohhot, Inner Mongolia 300 Contact zone 18.72 15.57 38.67 Li et al., 2003 9 Xiaoyingpan Zhangjiakou, Hebei 180 17.39 15.43 37.46 The third Geological Team of Hebei,1998; 10 Dongping Zhangjiakou, Hebei 177.4 ± 5 Fracture-altered 17.64 15.47 37.43 Wang et al., 1992;Song et al., 1994; Peng et al., 1992;Wang et al., 2010 11 Hanjiagou Zhangjiakou, Hebei 17.33 15.35 37.34 12 Shuijingtun Chongli, Hebei 17.18 15.39 37.10 Xu et al., 1998;Xu et al., 1991 13 Zhongshangou Chongli, Hebei 120 17.30 15.46 37.26 The third Geological Team of Hebei,1998; 14 Huangshanliang Chicheng, Hebei 230 Fracture-altered 17.38 15.39 37.19 Wang et al., 1992;Song et al., 1994; 15 Hougou Chicheng, Hebei 172.9 ± 5 Fracture-altered 17.54 15.38 37.39 Peng et al., 1992;Wang et al., 2010 Cu 16 Wunugetushan Xin Barag Yougi, Inner Mongolia 178.1 ± 0.6 18.38 15.53 38.11 Tan et al., 2011 Pb–Zn 17 Caijiaying Caijiaying, Hebei 16.74 15.40 37.52 Huang et al., 1997 18 Yueshanyin Lujiang, anhui 18.20 15.63 38.53 Cha et al., 2002 19 Laochang Laochang, shanxi 17.98 15.54 37.98 Xu et al., 2009 Mo 20 Yangshugou Fengning, Hebei 16.05 15.17 37.03 Wang et al., 2010 E.portion Au 21 Reshui Chifeng, Inner Mongolia 160 Far contact zone 17.59 15.46 37.84 Liu et al., 1991 22 Anjiayingzi Chifeng, Inner Mongolia 120 Contact zone 17.20 15.42 37.44 Ye et al., 1997 23 Xiajinbao Pingquan, Hebei 155.73 16.30 15.14 36.03 Wang et al., 2000 24 Tianjiacun Tangshan, Hebei 16.35 15.27 36.70 Wang et al., 2010 – 25 Jinchangyu Qianxi, Hebei 230 Disseminated quartz-vein 15.88 15.26 35.87 Wang et al., 2010;Zhang et al., 1996; 414 26 Yuerya Kuancheng, Hebei 180 Quartz-vein 15.86 15.16 35.68 Wang et al., 2010;Zhen et al., 1988 27 Tangzhangzi Kuancheng, Hebei 180 Cryptoexplosive breccia 16.16 15.41 36.79 Niu et al., 2001 28 Huzhangzi Kuancheng, Hebei 16.25 15.22 36.23 Wang et al., 2010 29 Shapoyu Kuancheng, Hebei 14.99 14.96 34.83 Wang et al., 2011 30 Baimiaozi Kuancheng, Hebei 16.30 15.30 36.49 Wang et al., 2012 31 Maoshan Zunhua, Hebei 16.13 15.23 36.13 Bai et al., 1990;Shao et al., 1987; Luan et al., 1996 32 Qingheyan Chinhuangtao, Hebei 179.5 16.17 15.06 35.95 Li et al., 1997 33 Xiazhangzi Chinhuangtao, Hebei 105.4 16.50 15.24 36.30 Yao et al., 2004 34 Niuxinshan Chinhuangtao, Hebei 175.8 ± 3.1 16.06 15.26 36.15 Wang et al., 2010;Yang et al., 1996 35 Erdaogou Chinhuangtao, Hebei 140.6 ± 2.8 17.58 15.76 38.91 36 Jinchanggouliang Chinhuangtao, Hebei 125.5 17.04 15.46 36.93 Mo 37 Hadamengou Chifeng, Inner Mongolia 239.76 ± 3.04 17.08 15.38 37.06 Hou et al., 2011 38 Huashi Chengde, Hebei 15.83 15.19 35.92 Wang et al., 2010 E. margin Jiaodong Au 39 Jiaojia Northern Shandong, Shandong 120.1 ± 0.2 Fracture-altered 17.25 15.43 37.82 Wang et al., 2001; Wang et al., 1991; Ding et al., 1998;Lin et al., 1999; Wen et al., 1990;Yao et al., 1990 40 Linglong Zhaoyuan, Shandong 123 ± 3 Quartz-vein 17.31 15.49 37.95 Wang et al., 2002; Yang et al., 2000; Yang et al., 1998; Guan et al., 1997; Yao et al., 1990;Liu et al., 1987; Wen et al., 1990 41 Dujiaya Northern Shandong, Shandong 129 Strata-bound 19.95 15.85 43.04 Sun et al., 1995; Wang et al., 1999; Zhao et al., 2000; Wang et al., 2001; Chen et al., 1997; 42 Hexi Penglai, Shandong 120 Fracture-altered 17.42 15.54 38.26 Ying et al., 1994;Yang et al., 2000 43 Fayunkuang Yantai, Shandong 120 Strata-bound 17.16 15.42 37.65 Wen et al., 1990 44 Denggezhuang Northern Shandong, Shandong 117.5 Quartz-vein 17.16 15.46 35.03 Wang et al., 2002 45 Xiadian Zhaoyuan, Shandong 120 Fracture-altered 16.79 15.31 37.08 Chen et al., 1989; Wang et al., 2002; Li et al., 1990 46 Yigezhuang Zhaoyuan, Shandong 120 Fracture-altered 16.95 15.52 38.39 Zhang et al., 2002;Zhu et al., 1999 47 Lingshangou Zhaoyuan, Shandong 120 Quartz-vein 17.33 15.47 37.88 Lin et al., 1990 48 Fushan Zhaoyuan, Shandong Quartz-vein 17.50 15.52 38.08 Chen et al., 1989 49 Jinchiling Zhaoyuan, Shandong 120–80 Quartz-vein 17.13 15.35 37.54 Wang et al., 2002;Yao et al., 1990 50 Taishang Zhaoyuan, Shandong 120 Fracture-altered 17.70 15.80 38.94 Chen et al., 1989;Deng et al., 2000 51 Dayingezhuang Northern Shandong, Shandong 118.5 Fracture-altered 17.33 15.52 38.13 Qiu et al., 1996;Chen et al., 1992; Wang et al., 1991 52 Canzhuang Northern Shandong, Shandong Fracture-altered 17.29 15.48 37.92 53 Xincheng Laizhou, Shandong 120 Fracture-altered 17.75 15.37 37.58 Zhen et al., 2006 54 Majiayao Qixia County, Shandong 120 Quartz-vein 16.56 15.24 37.07 Wang et al., 2002 55 Liukou Qixia County, Shandong 125 Quartz-vein 16.55 15.33 37.66 Wang et al., 2002 56 Panzijian Qixia County, Shandong 71.86 Quartz-vein 16.17 15.16 36.82 Wang et al., 2002 57 Jinguanding Qixia County, Shandong 120 Quartz-vein 16.92 15.31 37.28 Wang et al., 2002; Lin et al., 1999; 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. Yao et al., 1990 58 Daliujia Qixia County, Shandong 120 16.75 15.32 37.30 Yao et al., 1990; 59 Jiudian Pingdu, Shandong 120 Quartz-vein 17.59 15.74 38.57 Wang et al., 1982; Lin et al., 1990; Yuan et al., 1988 60 Pengjiakuang Northern Shandong, Shandong 120.5 ± 0.5 Strata-bound 17.11 15.42 37.63 Wang et al., 2002; Yao et al., 1990 61 Congjia Rushan, Shandong 120 17.21 15.41 37.92 Chen et al., 1989; Deng et al., 2000 62 Dazhuangzi Longkou, Shandong 120 Fracture-altered 17.28 15.52 37.95 Yao et al., 1990; Li et al., 1990 63 Qibaoshan Wulian, Shandong 120 Explosive-breccia 16.97 15.37 37.16 Ying et al., 1994 64 Jinqingding Northern Shandong, Shandong 120 Quartz-vein 17.02 15.48 37.55 Hou et al., 2004 Luxi Au 65 Xinanyu Taian, Shandong Fracture-altered 18.88 15.54 39.02 Zhang et al., 1999 66 Yuejiazhuang Xintai, Shandong Fracture-altered 21.63 16.08 47.52 Zhang et al., 1999 67 Yinan Yinan, Shandong 120 Skarn 18.84 15.56 42.59 Hu et al., 2004 68 Tongjing Yinan, Shandong 120 Skarn 17.44 15.50 37.52 Li et al., 2010 Fe 69 Yinan Yinan, Shandong 133 ± 6.0 Skarn 19.25 15.69 39.13 Hu et al., 2010;Qiu et al., 1996 S. margin Xiaoqinling Au 70 Jinlongshan Zhenan county, Shanglou, Shaanxi 230 Fracture-altered 18.35 15.68 38.44 Lv et al., 2012 71 Qiuling Zhenan county, Shanglou, Shaanxi Fracture-altered 18.27 15.68 38.44 Shen et al., 1996 72 Xiongershan Shanglou, Shaanxi 120 Quartz-vein 17.57 15.50 37.94 Lu et al., 2003:Chen et al., 1995 73 Xiajiadian Shanyang county, Shanglou, Shaanxi Carlin 18.41 15.58 38.29 Zhou et al., 2004 – 74 Tongyu Tongguan County, Weinan, Shaanxi Quartz-vein 17.25 15.57 38.02 Yu et al., 1989 414 75 Wenyu Lingbao County, Henan 120 Quartz-vein 17.18 15.58 38.33 Xu et al., 1992 76 Dongchuang Lingbao County, Henan 120 Quartz-vein 17.02 15.36 37.41 Fan et al., 2012 Mo 77 Jingduicheng Huaxian, Shaanxi 131 ± 4 17.13 15.35 38.36 Taylor et al., 1986; Li et al., 1984; Guo et al., 2009 Xiong'ershan Au 78 Qianhe Songxian, Henan 127 Fracture-altered 17.94 15.56 37.84 Zhang et al., 2003 79 Xiaonangou Songxian, Henan Fracture-altered 17.08 15.44 37.67 Shao et al., 1996

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Table 3 (continued) No. Deposit Location Age/Ma Type Pb Ref.

206 Pb/204 Pb 207 Pb/204 Pb 208 Pb/204 Pb

80 Jinchangzi Songxian Henan 180 18.20 15.55 38.04 81 Huachanggou 230 18.20 15.50 38.20 82 Ganshuao Songxian, Henan 17.14 15.40 37.72 Chen et al., 1992 83 Hugou Songxian, Henan 17.23 15.47 37.63 Chen et al., 1996 84 Yaogou Songxian, Henan 17.26 15.40 37.55 Fan et al., 1994 85 Dianfang Songxian, Henan 17.06 15.37 37.50 Ren et al., 1993 86 Hongzhuang Songxian, Henan 17.28 15.38 37.77 Yan et al., 2005 87 Pasigou Songxian, Henan 17.13 15.44 38.06 Xu et al., 2005 88 Xiasongping 129 ± 45 17.47 15.51 38.21 Pang et al., 2011 89 Shanggong Luoning, Henan 242 Fracture-altered 17.12 15.41 37.63 90 Kangshan Luanchuan, Henan 17.77 15.51 38.19 Chen et al., 1996 91 Laowan Tongbai, Henan 120 Fracture-altered 18.05 15.50 38.55 Zhu et al., 1998 Pb–Zn 92 Yangshuao Luanchuan, Henan 17.58 15.49 38.38 Lu et al., 2002

93 Lengshuibeigou Luanchuan, Henan 17.69 15.55 38.57 Lu et al., 2002 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. 94 Xigou Luanchuan, Henan 17.29 15.35 38.74 Wen et al., 1996 Mo 95 Sandaozhuang Luanchuan, Henan 145.0 ± 2.2 Porphyry 17.53 15.48 38.36 Luo et al., 1991 96 Nannihu Luanchuan, Henan 141.8 ± 2.1 Porphyry 17.57 15.48 38.22 Xu et al., 1999;Zhou et al., 1993; Zhang et al., 1987;Li et al., 1994; Luo et al., 1991 97 Shangfanggou Luanchuan, Henan 145.8 ± 2.1 Porphyry 17.12 15.23 37.57 Luo et al., 1991 98 Qiushuwan Nanyang, Henan 17.78 15.45 37.64 Zhu et al., 1998 Others Au 99 Linxiang Xunyang, Shaanxi 18.33 15.75 38.70 Zou et al., 2001 Interior Taihangshan Au 100 Konggezhuang North of Yi County, Hebei 121 17.05 15.24 37.26 The Taihang research team,1994 101 Jiujizhuang North of Yi County, Hebei 122 16.73 15.31 37.42 Geng et al., 1997 102 Shihu Lingshou County, Hebei 140 Quartz-vein 16.34 15.33 37.44 Wang et al., 2010;Yang et al., 1991 103 Xishimen Middle of Taihang Mountains 135.1 16.30 15.23 37.26 The Taihang research team,1994 104 Chounizhuang Middle of Taihang Mountains 120 16.02 15.17 36.88 Cu 105 Mujicun Laiyuan, Hebei 142.5 ± 1.4 16.51 15.26 36.60 Gao et al., 2011 Fe 106 Fushan Wuan, Hebei 128.8 ± 1.9 Skarn 17.25 15.39 37.34 Wang et al., 2012;Zhang et al., 1996; Cai et al., 2004;Zhang et al., 2007 107 Jiazhuang Shahe, Hebei Skarn 17.80 15.42 37.92 Zhang et al., 1995 108 Baishabei Wuan, Hebei Skarn 17.77 15.48 38.02 –

109 Beiandong Wuan, Hebei Skarn 17.71 15.46 28.05 414 110 Hongshan Wuan, Hebei Skarn 17.71 15.45 37.76 Yan et al., 2000 111 Pingshun Changzhi, Shanxi Skarn 18.30 15.55 37.94 Zhang et al., 200 112 Jiulongshan Shunping, Hebei Skarn 17.85 15.40 37.76 Mo 113 Dawan Laiyuan, Hebei 144 ± 7 Porphyry–Skarn 16.63 15.26 36.87 Tu et al., 1985;Wang et al., 2010 114 Yindonggou Lingshou County, Hebei 18.32 15.65 38.74 Wang et al., 2010;Wang et al., 2007 115 Futuyu Laiyuan, Hebei Skarn 15.92 15.31 37.01 Wang et al., 2010 116 Mujicun Laiyuan, Hebei Porphyry 36.29 15.20 36.29 Wang et al., 2010 Wutaishan Au 117 Qitu Wutai County, Shanxi 182.9 Strata-bound 19.31 15.57 37.68 Yang et al., 2001 118 Yixingzhai Fanshi, Shanxi 130 Quartz-vein 16.72 15.31 36.83 Jing et al., 1992 119 Shangyanghua Fanshi, Shanxi 19.15 15.71 39.34 Tian et al., 1991 120 Majiacha Fanshi, Shanxi 16.71 15.25 36.77 Tian et al., 1992 Hengshan Au 121 Chakou Fanshi, Shanxi 16.56 15.28 36.66 Tian et al., 1993 122 Xiaozhongzui 15.09 15.07 34.99 Li et al., 1994 123 Gengzhuang Fanshi, Shanxi 180 Explosive breccia 17.34 15.35 37.88 Luo et al., 2009 124 Tainashui Lingqiu, Shanxi 16.73 15.33 36.82 Tian et al., 1998 125 Diaoquan Lingqiu, Shanxi 120 Skarn 17.11 15.36 37.28 Li et al., 1994 Others Au 126 Puziwan Yanggao, Shanxi 120 Explosive breccia 16.92 15.41 36.96 Long et al., 2011 127 Dongfengding Xiangfen, Shanxi 120 18.33 15.58 38.85 Wang et al., 2009 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 401

Fig. 10. Lead isotopic composition diagrams of sulﬁde minerals from the ore deposits in the NCC.

Tolstikhin (1978) and Kendrick et al. (2001), the mantle helium in the characteristics of the intrusive rocks suggest that the magmas were ore-forming fluid was calculated to be in the range of 3.3% to 86.1% derived from the lower crust with some contribution of mantle with an average of 31.5%, and mostly in the range of 13% to 26%. materials. Combining all the data from the S, Pb, Si, H, O, C, and He isotopic The large sulfur isotopic data base (>260 samples from 19 deposits) analyses, it can be concluded that materials and fluid derived from from previous studies display δ34S values of the sulfide minerals from the mantle cannot be excluded as an important contribution to the −6.3‰ to 8.3‰ with most of the values falling within the range of formation of the gold, silver, lead and zinc as well as the molybdenum −1‰ to 3‰ and an average of −1.9‰ with a few exceptions (Table 2). deposits in the northwest of Hebei Province. The sulfur isotopes of the sulfide minerals from most of these deposits show equilibrium fractionation trend. These sulfur isotopic composi- 3.4.1.2. Eastern Hebei Province. The eastern part of Hebei Province is tions are comparable with those from the Jinchanggouliang gold depos- located within the north-eastern margin of the NCC. More than 100 it in Chifeng City of Inner Mongolia (δ34S=−5.0 to 1.1 average −0.1; Mesozoic gold deposits and occurrences and 40 copper (gold), silver– Wei et al., 1993), the Lanjiagou molybdenum deposit in Jinxi County lead–zinc polymetallic deposits occurrences were reported from this (δ34S=−0.3 to 7.9 average −3.3 for 11 samples; Rui et al., 1994) area. Most of the gold deposits are located in the Archean metamorphic and the Xiadabao gold deposit in Qingyuan County (δ34S=−2.0 to rocks whereas the majority of the polymetallic deposits are hosted 1.9 average −0.4; Wei et al., 1993) of Liaoning Province. in the Jurassic strata. Almost all the deposits are associated spatially The lead isotopic compositions of 67 samples from 13 deposits in and temporally with the Yanshanian granitic intrusions (Wang et al., east Hebei Province vary within narrow ranges with 206Pb/204Pb 2010). values varying from 14.986 to 16.304, 207Pb/204Pb from 14.961 to The emplacement of the Yanshanian granitic intrusions was coe- 15.408, and 208Pb/204Pb from 34.834 to 36.787 (Table 3). In Zartman's val with the formation of the deposits. The REE patterns of the intru- diagrams, most of the data cluster around the mantle line, suggesting sive rocks are characterized by negative Eu anomaly (ΣREE varies that the lead of the ores were mainly derived from the mantle and the 66.75 ppb to 317.55 ppb; δEu varies from 0.12 to 0.85; LREE/HREE lower crust (Fig. 10). These data are remarkably consistent with those 87 86 varies from 1.66 to 24.04). ( Sr/ Sr)i values for the intrusive rocks from the Xiadabao gold deposit of Qingyuan County, Liaoning Prov- vary from 0.704 to 0.708 (Zhang and Chen, 1996). Trace element ince where the 206Pb/204Pb vary from 15.912 to 16.177, 207Pb/204Pb analyses of the small stocks (with an outcrop area of b2km2) yielded vary from 15.154 to 15.373, and 208Pb/204Pb vary from 36.107 to high gold contents ranging from 11 ppb to 92 ppb. These 36.671 (Wei et al., 1993). The lead isotopic systematics of the ore 402

Table 4 Silicon isotopic compositions of the ore deposits in the NCC.

No. Deposit Location Mineralization type Age/Ma Type δ30 Si_NBS-28 Reference

N. margin W–M portion 1 Dongping Zhangjiakou, Hebei Au 140.2 ± 1.3 Fracture-altered −0.3–0.4 Wang et al., 2010;Lu et al., 1992 2 Xiaoyingpan Xuanhua, Hebei Au 171.45 Quartz-vein −0.3–0.1 Wanget al., 2010; Yin et al., 1995 3 Wanquansi Wuanquan, Hebei Au, Ag −0.2 to −0.1 Wanget al., 2010 4 Shuijingtun Chongli, Hebei Au Fracture-altered −0.2–0.3 Wanget al., 2010 .R i .Snoh/OeGooyRves5 21)376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. 5 Zhongshangou Chongli, Hebei Au 115.1 Far contact −0.2–0.2 Wanget al., 2010 6 Huangtuliang Chicheng, Hebei Au 120.63 Fracture-altered −0.3–0.0 Wanget al., 2010 7 Hougou Chicheng, Hebei Au 154.4 ± 1.3 Fracture-altered −0.2 Wanget al., 2010 8 Yangshugou Fengning, Hebei Mo, Ag 140.10 ± 213 Porphyry −0.3 Wanget al., 2010 9 Dacaoping Fengning, Hebei Mo 220.10 ± 117 Porphyry 0.07 Guo et al., 2011 10 Fengning Fengning, Hebei Au Fracture-altered −0.2 Wang et al., 2010 E. portion 11 Huashi Chengde, Hebei Au, Mo Quartz-vein 0.92 Xiao et al., 1994 12 Dongzigou Chengde, Hebei Ag, Au Quartz-vein 1.31 Wang et al., 2010 13 Xiajinbao Pingquan, Hebei Au 2.66 Wang et al., 2000 14 Malanguan Tangshan, Hebei Au 3.0 Song et al., 1994 15 Jinchangyu Qianxi, Hebei Au 2190 ± 58 Fracture-altered Quartz-vein −0.3 Wang et al., 2010; Zhang et al., 1996 16 Yuerya Kuancheng, Hebei Au 175 ± 1 Quartz-vein −0.2 Wang et al., 2010; Zheng et al., 1988 17 Tangzhangzi Kuancheng, Hebei Au 172 ± 2 Explosive-breccia 1.45 Wang et al., 2010 18 Jianbaoshan Kuancheng, Hebei Au Stata-bound −0.3 to −0.1 Wang et al., 2010 19 Maoshan Zunhua, Hebei Au Quartz-vein 1.03 Bo et al., 1990; Shao et al., 1987; Luan et al., 1996 20 Sanjia Qinhuangdao, Hebei Au Contact −0.1 Wang et al., 2010 21 Huajian Qinhuangdao, Hebei Au −0.3 Wang et al., 2010

22 Niuxinshan Qinhuangdao, Hebei Au 172 ± 2 Contact 0.46 Wang et al., 2010; Yang et al. 1996; – Luo et al., 2001 414 E.margin Luxi 23 Jinchangyu Yinan, Shandong Au 133 ± 6 Skarn 1.9–3.5 Zang et al., 1998; Hu et al., 2010 24 Buwa Mengyin, Shandong Au Fracture-altered 2.05–4.06 Liu et al., 1994 25 Guilaizhuang Pingyi, Shandong Au 188–178 Explosive-breccia 2.000–2.990 Zhang et al., 1999; Tan et al., 1993 S.margin 26 Baguamiao Baoji, Shaanxi Au 131.91 ± 0.89 Quartz-vein −0.33 Chen et al,2009; Shao et al,2001 Interior Taihang 27 Lianbaling Laiyuan, Hebei Au, Pb, Zn 0.1 Wang et al., 2010 28 Beiyingxigou Lingshou, Hebei Ag, Pb, Zn 153 ± 1 Fracture-altered 0.0 Wang et al., 2010;Ke et al., 2012 29 Qiubudong Pingshan, Hebei Ag, Au 0.0–0.1 Wang et al., 2010 30 Xishimen Lingshou, Hebei Au −0.2 Wang et al., 2010 31 Chounikou Lingshou, Hebei Au 0.0 Wang et al., 2010 32 Shanggang Laishui, Hebei Au 0.1 Wang et al., 2010 Table 5 Hydrogen, oxygen and carbon isotopic compositions of the ore deposits in the NCC.

13 18 Type Deposit Location Age/Ma Type OSMOW (‰)D(‰) C(‰) OH2O (‰) Ref. N.margin W-Mportion Au Wanquansi Wanquan, Hebei 13.3 −109.5 −3.9 2.57 Wang et al., 1992 Zhongshan'gou Zhangjiakou, Hebei 120± 12.67 −87.33 −3.77 0.81 Wang et al., 1992 Shuijingtun Zhangjiakou, Hebei 12.3 −70.5 3.47 Shi et al., 1993 Huangtuliang Chicheng, Hebei 230 Fracture-altered 10.02 −83.75 −4.1 0.38 Song et al., 1994 Fengning Fengning, Hebei 4.9 −98 −6 −3.14 Wang et al., 2010 Dongping Zhangjiakou, Hebei 180± Fracture-altered 8.76 −91.2 −2.49 1.49 Fan et al., 2001 Xiaoyingpan Xuanhua, Hebei 180± 13.17 −93.17 7.31 Mao et al., 2001 Hougou Chicheng, Hebei 180± Fracture-altered 11.24 −96.58 3.87 Wang et al., 2010 Zhangquanzhuang Xuanhua, Hebei 13.01 −109.1 5.99 Mao et al., 2001 Hanjiagou Zhangjiakou, Hebei 11.74 −115 5.71 Song et al., 1994; Jinjiazhuang Zhangxuan, Hebei 180± Fracture-altered 11.75 −92.9 2.87 Peng et al., 1992; Dayingzi Chengde, Hebei 11.73 −80.5 3.76 Yao, 2000 Bainaimiao Wulanchabu, Inner Mongolia 300 3.69 −85 3.98 Ye, 1997 Bayinhanggai Bayannaoer, Inner Mongolia 13.6 −79 5.79 Chen et al., 2001 Liangqian Guyang, Inner Mongolia 10.7 −80 6 Xu et al., 1998

Donghuofang Hohhot, Inner Mongolia 12.7 −96 4.635 Shi et al., 1993 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. Houshihua Hohhot, Inner Mongolia Ductile shear zone 12.9 −83.33 6.18 Wang et al., 2010 Jinchanggouliang Chifeng, Inner Mongolia 13.22 −82.92 −7.87 6.07 Zhang et al., 2002 Wulashan Baotou, Inner Mongolia 230 12.91 −77.16 4.58 Lang, 1997 Dongkalaqin Chifeng, Inner Mongolia 9.38 −1.16 Wang et al., 2010 Pb–Zn Caijiayingzi Zhangbei, Hebei 130 13.76 −94 −3.67 5.23 Lv et al., 2004 Zhaojiagou Chicheng, Hebei 198.7 12.4 −94 5.43 Song et al., 1994; Wang et al., 2010 Mo Sadaigoumen Fengning, Hebei 227.1 ± 2.7 Porphyry 10 −89.8 0.1–6.2 Shen, 2001 Dacaoping Fengning, Hebei 220.10 ± 117 Porphyry Guo et al., 2011 224.10 ± 115 232.17 ± 115 Yangshugou Fengning, Hebei 16 −66 2.76 Wang et al., 2010; Fe Baiyun'ebo Baotou, Inner Mongolia 439 13.2 Zhang et al.,2008; Wei et al., 1994 E. portion Au Jingchangyu Qianxi, Hebei 132 Quartz vein 12.36 −79.71 −4.75 6.03 Song et al., 1994 Shapoyu Xinglong, Hebei 12.6 −61 Wang et al., 2010 Malanguan Tangshan, Hebei 12.78 −72.5 −5.25 3.42 Wang et al., 2010 Tianjiacun Zunhua 11.24 −73 Wang et al., 2010 Yuerya Kuancheng, Hebei 175 Quartz vein 13.112 −88.45 −4.18 7.029 Chai et al., 1989 Huzhangzi Qingyuan, Liaoning 14.1 −76 Wang et al., 2010 –

Sajingou Kuancheng, Hebei 12.2 −79 Wang et al., 2010 414 Banbishan Qinglong, Hebei 10.36 −78.8 Wang et al., 2010 Maojidian Qingyuan, Liaoning 13.9 −87 Wang et al., 2010 Huashi Xinglong, Hebei −84.67 Wang et al., 2010 Tangzhangzi Kuancheng, Hebei 12.4 −56 Wang et al., 2010 Xiacaonian Qinglong, Hebei −63 −5.1 Wang et al., 2010 Xiaojinggou Zhangjiakou, Hebei 24.05 −71.07 −2.36 12.15 Wang et al., 2010 Xiajinbao Pingquan, Hebei 13.53 −70.15 4.63 Shao et al., 1987 Honghuagou Chifeng, Inner Mongolia 1700 −88 5.8 Wang et al., 1993 Erdaogou Beipiao, Hebei 900 −92 6.1 Wang et al., 1992 Anjiayingzi Chifeng, Inner Mongolia 800 −109 5.2 Wang et al., 1993 Zhaojiagou Chicheng, Hebei −96 0.3 Wang et al., 2010 Reshui Chifeng, Inner Mongolia −88 9.2 Wang et al., 2010 Hongshi Yixian, Liaoning −116 1.1 Wang et al., 2010 Xiazhangzi Qinglong, Hebei 18 −85.1 −2.07 6.01 Wang et al., 2010 Sanjia Qinhuangdao, Hebei 12.8 −48.9 5.11 Song et al., 1994 Pb–Zn Bajiazi Jianchang, Liaoning 177.4–183.8 −74.3 3.27–7.85 Bi et al., 1989, Yang et al., 1990, Chen et al., 2003 Mo Xiaodonggou Keshetengqi, Inner Mongolia 135.5 ± 1.5 −5.6–6.8 Nie, 2007, 2007 Nianzigou Chifeng, Inner Mongolia 154.3 ± 3.6 −128.8 to −109.2 Zhang, 2010

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Table 5 (continued) 13 18 Type Deposit Location Age/Ma Type OSMOW (‰)D(‰) C(‰) OH2O (‰) Ref. .R i .Snoh/OeGooyRves5 21)376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. Hadamengou Chifeng, Inner Mongolia 239.76 ± 3.04 11.6 Hou, 2011 Xiaojiayinzi Kezuo, Liaoning 177 ± 5 Skarn 10.1 102 6.5 Tang, 1979 Lanjiagou Gongchangling, Liaoning 186.5 Quartz vein −87.7 1.9 Dai, 2008 Dazhuagke Yanqing, Beijing 146 ± 11 10.42 Dong et al., 1992 Xiaoshigou Pingquan, Hebei 134 ± 3 Porphyry-Skarn −91.93 7.03 Zhang et al., 1994; Quan et al., 1992 Huashi Chengde, Hebei −84.67 Wang et al., 2010 Fe Zhangjiagou Dandong, Liaoning Province −2.19–3.09 Xia, 1997 Huanggang kesheketengqi, Inner Mongolia 135.31 ± 0.85 Skarn 6.2 −83 7.4 Mao, 2011 Zhoutaizi Kuanping, Hebei Province 2460 Xiang et al., 2010 Damiaoheishan Chengdeshi, Hebei Province 39 7.98 Zhao et al.,2012; Sun et al., 2009 Xiaojiayinzi Kezuo, Liaoning Province 165.5 ± 4.6 Skarn Dai, 2007 E. margin Liaodong Pb–Zn Dongsheng Xiuyan, Liaoning Yanshanian −76 to −83 −2.1–4.3 Jiang et al., 1991 Jiaodong Au Majiayao Qixia, Shandong 120± Quartz vein 13.2 −64.6 4.14 Yang et al., 1991 Sanshandao Laizhou, Shandong 120± Frature-altered 12.44 −76.54 4.16 Zhang et al., 1994 Xincheng Laizhou, Shandong 120± Fracture-altered 14.17 −85 5.41 Zhang et al., 1994 Jiaojia Laizhou, Shandong 120± Fracture-altered 13.15 −84.26 −5.3 3.02 Ding et al., 1998 Changshang Laizhou, Shandong 120± Fracture-altered 13.17 −78.67 5.1 Zhang et al., 1994 Lingshan'gou Zhaoyuan, Shandong 120± Quartz vein −79.79 2.44 Yang et al., 1996 –

Shilipu Zhaoyuan, Shandong 120± 9.25 −89.67 −4.2 Yang et al., 1996 414 Linglong Zhaoyuan, Shandong 120± Quartz vein 12.99 −69.34 −5.44 4.66 Yang et al., 1996 Taishang Zhaoyuan, Shandong 120± Fracture-altered 13.23 −84.67 4 Yang et al., 1996 Dayin'gezhuang Zhaoyuan, Shandong 120± Fracture-altered 9.07 −78 2.7 Yang et al., 1996 Rushan Rushan, Shandong 120± Quartz vein 10.23 −82.8 3.36 Yang et al., 1996 Denggezhuang Yantai, Shandong 120± Quartz vein 12.4 −77.78 −2.37 4.95 An et al., 1988 Yuan'gezhuang Yantai, Shandong 120± Quartz vein 7.64 −73.5 2.88 An et al., 1988 Dongdaokou Yantai, Shandong 120± 11.66 −82.13 2.71 An et al., 1988 Dazhuangzi Pingdu, Shandong 120± Fracture-altered 11.45 −64.93 −1.5 3.11 Mao et al., 2002 Qixia Qixia, Shandong 120± Quartz vein 12.39 −77.85 0.87 Zhai et al., 1996 Qibaoshan Wulian, Shandong 120± Explosive-breccia 11.54 −68.76 4.21 Qiu et al., 1996 Pengjiakuang Rushan, Shandong 120± Strata-bound 7.4 −93.59 −4.27 1.3 Sun et al., 1995 Luxi Au Lifanggou Pingyi, Shandong 19.94 −66.25 9.34 Hu et al., 2004 Jinchang Yinan, Shandong 4.1 −87 7.78 Qiu et al., 1996 Au–Cu–Fe Yinan Yinan, Shandong 133 ± 6.0 Skarn 4.3 10.8 Wang et al., 2010 S. margin Xiaoqinling Au Dongchuang Lingbao, Henan Quartz vein 10.81 −52.58 −4.41 6.42 Li et al., 1998 Wenyu Lingbao, Henan Quartz vein 9.5 −87.41 −3.45 2.43 Xu et al., 1992 Chucha-luanshigou Lingbao, Henan 10.25 −62.7 2.52 Xu et al., 1992 Yangzhaiyu-S60 Lingbao, Henan 11.1 −47.62 5.2 Yu et al., 1997 Zhuyu Lingbao, Henan 10.8 −47.62 5.16 Li et al., 1998 Xichang'an-dongman Lingbao, Henan 11.48 −57.73 4.89 Wang , 1987 Dongtongyu-Q8 Tongguan, Shaanxi 12.37 −48.63 6.31 Zhou et al., 1993 Gongyu Songxian, Henan 10.5 −74 0.1 Li et al., 2004 Laowan Tongbo, Henan Fracture-altered 11.95 −70 1.78 Xie et al., 2001 Taoyuan Weinan, Shaanxi 10.45 −59.5 7.62 Wang et al., 2010 Mo Yechangping Sanmenxia, Henan 9.12–9.59 Jinduicheng Huaxian, Shaanxi 129 ± 7, 131 ± 4 2.86 −76.11 to −100.20 −5 −4.14–7.29 Taylor et al., 1986; Li et al., 1984; Guo et al., 2009 Xiong'ershan Au Shanggong Luoning, Henan 12.98 −81.77 −0.8 6.1 Chen et al., 1992 Funiushan Luanchuan, Henan 12.42 −82 1.34 Zhang et al., 1998 Kangshan Luanchuan, Henan 14.94 −80.5 −1.09 4.82 Wang et al., 2001 Qinggangping Luanchuan, Henan 10.14 −83.3 5.35 Chen et al., 1996 Putang Nanyang, Henan 5.2 −50.3 −3.12 −6.85 1995 Qiyugou Songxian, Henan 120± Explosive breccia 10.27 −73.99 −3.5 2.87 Xie et al., 1991 Pb–Zn Bailugou Lunachuan, Henan −90 Yan et al., 2002, Ye, 2006 2006 Lengshuibeigou Luanchuan, Henan 136.13 ± 0.44 −81 0.81 Wang et al., 2007 Mo Sandaozhuang Luanchuan, Henan 145.0 ± 2.2 9.96 Luo et al., 1991 Nannihu Luanchuan, Henan 141.8 ± 2.1 −74.5 5.09 Xu et al., 1999; Zhou et al., 1993; Zhang et al., 1987; Li et al., 1994; Luo et al., 1991 Interior Taihang Au Qiubodong Pingshan, Hebei 9.7 −64 −4.2 1.49 Wang et al., 2010 − −

Yangshugou Lingshou, Hebei 16 66 3.5 2.76 Wang et al., 2010 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. Xishimen Lingshou, Hebei 13.1 −83 5.4 Wang et al., 2010 Beiyingxigou Lingshou, Hebei 14.3 −87 4.56 Wang et al., 2010 Chounikou Lingshou, Hebei 12.2 −77 −4.9 1.24 Wang et al., 2010 Au–Mo Yingdonggou Lingshou, Hebei 10.2 −87 −3.5 5.13 Wang et al., 2010 Yindong Lingshou, Hebei 14.38 −71.5 1.19 Geng et al., 1999 Au Shihu Au Lingshou, Hebei 120± Quartz vein 12.45 −89 −4.47 3.11 Wang et al., 2010 Au–Mo Dawan Laiyuan, Hebei 2.86 −101.72 −5.6 Tu, 1995 Au–Mo Futuyu Laiyuan, Hebei 6.77 −115 0.74 Wang et al., 2010 Au Konggezhuang Yixian, Hebei 11.65 −93.28 4.6 Wang et al., 2010 Shangmingyu Laiyuan, Hebei 9.3 −80.33 1.7 Zhu et al., 1999 Lianbaling Laiyuan, Hebei 5 −90 1.2 Wang et al., 2010 Luanmuchang Yixian, Hebei −74 12.25 Wang et al., 2010 Dashiyu Tangxian, Hebei −72.69 −1.5 Wang et al., 2010 Xiaolinggen Yixian, Hebei −56.09 −5.99 Wang et al., 2010 Pb–Zn Lianbaling Laiyuan, Hebei Yanshanian −90 1.2 Wang et al., 2007 Fe Beiluohe Wuan, Hebei 137 Skarn 8.4 −100.1 6.7 Ying, 2012 Fuzhan Wuan, Hebei 128.8 ± 1.9 Skarn 6 −100 2.78 Wang, 2012; Zhang et al., 1996; Cai et al., 2004; Zheng, 2007 – 414 405 406 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

from those mentioned above, most of the values are broadly similar. These data suggest that the sulfur in the gold deposits in the Jiaodong peninsula was mainly derived from the Cretaceous igneous intrusions which probably scavenged the sulfur from Archean basement. Table 3 shows the 206Pb/204Pb data of 72 samples of sulfide minerals from the quartz vein type and fracture-alteration type gold deposits where the values range from 16.40 to 17.92 with an average of 17.13. Those of 7 pyrite samples from the strata-bound gold deposits vary from 16.92 to 22.15 with an average of 18.78 (Table 3), distinctly different from those mentioned above. The 206Pb/204Pb data of 13 K-feldspar, 2 whole-rock and 1 galena from the Cretaceous and Jurassic intrusive rocks and the Archean Jiaodong Group of rocks vary from 16.4 to 17.87 with an average at 17.17, consistent with those of the quartz vein type and fracture altered type gold deposits. The 207Pb/204Pb data of 72 samples of sulfide minerals from the Fig. 11. D–O isotopic composition diagrams of fluid inclusions in quartz from the ore quartz vein type and fracture altered type gold deposits range from deposits in the NCC. 15.20 to 15.72 with a mean at 15.45, which are different from those of 7 pyrite samples from the strata-bound gold deposits (from 15.35 to 16.15; average 15.74) and consistent with those of 13 K-feldspar, 2 whole-rock and 1 galena from the Cretaceous and Jurassic intrusive and associated granitoids show consistence from both regions rocks and the Archean Jiaodong Group of rocks (from 15.35 to 15.83, 208 204 (Table 3; Wei et al., 1993) suggesting a close genetic link between average 15.47). The Pb/ Pb data for the quartz vein-type and the granitic magmatism and the gold and polymetallic mineralization. fracture-alteration type gold deposits range from 37.26 to 38.60 Data from 49 samples representing 10 gold and copper–molybdenum with an average at 37.70, distinct from those of the strata-bound 18 gold deposits (from 37.08 to 49.05; average 39.81) and consistent deposits show that in each deposit, the average δ OH2O values vary from 3.4‰ to 7.5‰ with one exception (Table 5). Thus, the Jinchanggouliang with those of the Cretaceous and Jurassic intrusive rocks and the Ar- 18 chean Jiaodong Group of rocks (from 36.96 to 37.92; average 37.51). gold deposit in Chifeng area (δ OH2O =5.6‰ to 7.03‰; Wei et al., 18 The consistence in the lead isotopic composition of the quartz 1993), the Nanlongwangmiao gold deposit (δ OH2O =4.26‰ to 18 vein-type and fracture alteration-type gold deposits with the Meso- 6.69‰; Wei et al., 1993) and the Xiadabao gold deposit (δ OH2O = 4.03‰; Wei et al., 1993) in Qingyuan County, Liaoning Province, show zoic intrusions and the Jiaodong Group of rocks imply a close genetic values close to that of primary magmatic water (5‰ to 10‰, linkage among these. On Zartman's diagrams, the data show that the lead of the gold ores was derived from different sources including Sheppard, 1977). The average δDsmow values for each of the 19 deposits range from −88‰ to −56‰, close to the −80‰ to −40‰ mantle and the basement (Fig. 10). δ18 δ value for primary water (Sheppard, 1977; Fig. 11). The average A group of 47 OH2O and DSMOW data on quartz from 8 quartz 13 vein type and fracture altered type gold deposits show a range of δ CPDB for each of the 7 deposits ranges from −5.25‰ to −2.07‰ within the range for mantle carbon (−2‰ to −5‰; Taylor and values from −8‰ to 9.69‰ with an average of 3.91‰ and −95.8‰ Bucher-Nurminen, 1986) and close to the range for magmatic car- to −33.0‰ with an average of −77.3‰ respectively (Table 5). A δ18 δ bon (−9‰ to −3‰; Taylor and Bucher-Nurminen, 1986). group of 9 OH2O and DSMOW data on quartz from 2 altered gold de- Wang et al. (2010) measured the helium and argon isotopes of 14 posits show values from 0.59‰ to 4.03‰ with an average1.81‰ and pyrite, 1 galena, 1 gneiss and 2 granite samples from the gold and sil- −97.9‰ to −79.0‰ with an average −89.3‰, respectively δ ver deposits in the East Hebei Province (Table 6). The result shows (Table 5). Except for a few data, all the DSMOW values are lower than that the 3He/4He values vary in the range of 2.5 × 10−6 to that of the typical metamorphic water (−65‰ to −20‰, Hugh and 9.39 × 10−6 with an average at 5.43 × 10−6, much higher than Taylor, 1974) and close to the primary magmatic water (−80‰ to − ‰ δ18 those of the granite and gneiss. Calculation with a mantle–crust bina- 40 , Hugh and Taylor, 1974). Most of the OH2O data are close ry model shows that the mantle helium varies from 23% to 85% with to the primary magmatic water (5‰ to 10‰, Hugh and Taylor, an average at 53% (Wang et al., 2010). The measured 40Ar/36Ar varies 1974; Fig. 11), suggesting that the water associated with mineraliza- from 308 to 1304 with a mean at 742, prominently higher than the tion was closely related with the magmatism. 3 4 40 36 δ13 295.5 value of air saturated water (ASW). The He/ He vs. Ar/ Ar Fifty three CPDB data of the calcite and siderite from 6 quartz vein diagram suggests marked contribution of mantle gas to the minerali- type and fracture altered type gold deposits show values from −6.5‰ zation (Fig. 12). to −0.6‰ with an average of −4.6‰, well within the range of magmatic carbon (from −9‰ to −3‰; Table 5). The majority of the data fall within the range of mantle carbon (from −5‰ to −2‰, Taylor and 13 3.4.2. Eastern margin of the NCC Bucher-Nurminen, 1986). Nineteen δ CPDB data on the calcite and do- There are three ore cluster regions in the eastern margin of the lomite from 2 strata-bound gold deposits show variation from −4.8‰ NCC: the Jiaodong peninsula, the Liaodong peninsula and the Luxi to 1.6‰ with an average −2.0‰ and the majority of the values corre- area (west of Shandong Province). Among these, the Jiaodong penin- sponds with mantle carbon whereas a few fall in the range of sedimen- sula is the most important gold district in China. tary carbonate rocks (from −2‰ to +3‰, Veizer et al., 1980). The data Sulfur isotope data on 68 pyrite samples from 13 quartz vein-type clearly reflect the involvement of the wall rocks of the Proterozoic and fracture alteration-type gold deposits in the Jiaodong peninsula Jingshan Group of dolomite, especially in the Dujiaya gold deposit. show δ34S values ranging from 2.4‰ to 12.6‰ with an average of Helium and argon isotopic data on 25 fresh pyrite samples from 7.6‰ and most of the values lying in the range of 6‰ to 9‰.Theresults underground levels of 5 quartz vein type gold deposits in the Jiaodong are consistent with those from the Cretaceous Gujialing granodiorite peninsula (Table 6; Fig. 12) show that the mantle helium involved in and the Archean Jiaodong Group of rocks (Table 2), as well as those of the quartz vein gold mineralization vary from 0 to 42% with an aver- the Miaoling gold deposit in Gaizhou City, Liaodong peninsula (from age of 6% (the negative values are taken as 0). The mantle helium in- 6.2‰ to 10.9‰ averaging 8.9‰, Wei et al., 1993). Although a few δ34S volved in the strata-bound type of gold mineralization varies from 0 data from the strata-bound gold deposits show marked difference to 12% with an average value of 4% (8 samples from 3 deposits), Table 6 Helium and argon isotopic compositions of the ore deposits in the NCC.

No. Deposit Location Age/Ma Type 3He 4He 3He/4He (Rc/Ra) 40 Ar/36 Ar 40 Ar/4He Ref.

N. margin W. portion 1 Hougou Au Chicheng, Hebei 180 Fracture-altered 2.1 678 2500 Wang et al., 2012; Zhang et al., 1996; 2 Huangtuliang Au Chicheng, Hebei 230 Fracture-altered 0.93 1238 5000 Cai et al., 2004; Zheng et al., 2007 3 Xiaoyingpan Au Xuanhua, Hebei 180 2.2 2073 714.2857 4 Dongping Au Zhangjiakou, Hebei 180 Fracture-altered 4.05 464 5.6275 5 Zhongshangou Au Chongli, Hebei 120 0.38 430 1.8811

6 Yangshugou Mo Fengnin, Hebei 952.15 68.94 1.77 797 0.06 376 (2014) 56 Reviews Geology Ore / Santosh M. Li, S.-R. E. portion 7 Jinchangyu Au Qianxi, Hebei 132 Quartz vein 532 106.4 5 653 0.1504 8 Huzhangzi Au Kuancheng, Hebei 399.25 159.7 2.5 817 0.0764 9 Huashi Au Chengde, Hebei 62.4 9.6 6.5 308 0.0525 10 Shapoyu Au Kuancheng, Hebei 265.35 91.5 2.9 1304 0.1567 11 Yuerya Au Kuancheng, Hebei 175 Quartz vein 156.87 58.1 2.7 575 0.0233 12 Tanjiacun Au Tangshan, Hebei 1264.56 287.4 4.4 886 0.0436 13 Huajia Au Qinhuangdao, Hebei 14.08 3.06 4.6 1007 7.1429 14 Tangzhangzi Au Kuancheng, Hebei 173 Explosive-breccia 91.72 14.11 6.5 365 10 15 Malanguan Au Tangshan, Hebei 7553.32 804.4 9.39 1166 0.0163 16 Xiaoyingzi granite Au Qinhuangdao, Hebei 179.5 0.44 441.6 17 Huashi Mo Chengde, Hebei 62.4 0.96 6.5 308 0.05 E. margin Jiaodong 18 Jiaojia Au Laizhou, Shandong 120 Fracture-altered 222.66 7.37 2.87 775.67 0.1779 19 Canzhuang Au Zhaoyuan, Shandong Fracture-altered 2.842 20.3 0.1 1636.5 20 Denggezhuang Au Yantai, Shandong 120 Quartz vein 63.71 2.29 21 Jinchiling Au Zhaoyuan, Shandong Quartz vein 4.13 3.69 0.8 383.7 0.4815 22 Linglong Au Zhaoyuan, Shandong 120 Quartz vein 2.045 3.29 0.4428 5905 23 Jinqingding Au Rushan, Shandong Quartz vein 2.257 3.43 0.47 474.6 24 Zhaodaoshan Au Jiaodong, Shandong Quartz vein 2.066 36.9 0.04 428.9 –

25 Pengjiakuang Au Rushan, Shandong 120 Strata-bound 92.87 8.98 1.05 380.5 1.282 414 26 Dujiaya Au Yantai, Shandong Strata-bound 8.209 47.4 0.1237 509.5 27 Fangyunkuang Au Yantai, Shandong Strata-bound 8.196 13.66 0.4286 314 Luxi 28 Fushan Fe Wu'an, Hebei 120 skarn 1.6 26.4 8.504 871 Interior Taihengshan 29 Xishimen Au Lingshou, Hebei 4419.2 283.28 1.56 920 0.0461 30 Shihu Au Lingshou, Hebei 140 Quartz vein 193.3 32.21 0.6 879 0.1497 31 Chounikou Au Lingshou, Hebei 307.8 9.16 3.36 511 0.4219 32 Shanggang Au Laishui, Hebei 1108 460 2.41 2361 0.0285 33 Shangmingyu Au Taihang Mountain 2782 231.9 1.2 365 0.0122 34 Mujicun Cu Au Laiyuan, Hebei 140 0.1089 Gao et al., 2011 35 Yintonggou Mo Au Lingshou, Hebei 2405.7 235.85 1.02 468 0.58 Wang et al., 2010 407 408 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

Fig. 12. He and Ar isotopic composition diagrams of the fluids trapped in sulfide minerals from the ore deposits in the NCC. whereas those from the fracture altered gold mineralization varies and geochemical characteristics of the two areas (Li et al., 2012; Li from 26% to 100% with an average of 63% (8 samples from 2 deposits). et al., 2013) has brought out prominent differences between the All the above data show substantial input of mantle materials in the two areas. gold mineralization in Jiaodong peninsula during the Early Cretaceous. The δ34S data on 169 sulfide samples from 17 gold, silver, molybdenum, and lead–zinc deposits in the northern Taihang Mountains 3.4.3. Southern margin of the NCC show variation from −3‰ to 5‰ with a few exceptions (Table 2; The Xiaoqinling and the Xiong'ershan areas are the two most im- Fig. 9), whereas 23 δ34S data on pyrite from 13 iron deposits in the portant ore cluster regions characterized by predominantly Early Cre- southern Taihang Mountains vary from 11.6‰ to 18.7‰ with a taceous gold and few silver–lead–zinc deposits related with coeval mean at 15.2%. magmatic rocks in the southern margin of the NCC. The Xiaoqinling The lead isotopic compositions of 76 sulfide minerals from 17 de- region is recognized as the second largest gold district in China after posits in the northern Taihang Mountains show the following varia- the Jiaodong peninsula. tion in the average value for each deposit: 206Pb/204Pb from 15.77 to Wang et al. (2010) collected 261 δ34S data from 17 deposits of 17.42, 207Pb/204Pb from 15.09 to 15.45 and 208Pb/204Pb from 36.29 the Xiaoqinling and Xiong'ershan areas (Table 2) which show a to 38.74 (Table 3). Five pyrite samples from the Beiminghe iron de- range of −19.2‰ to 7.2‰ with the average for each deposit ranging posit in the southern Taihang Mountains (Shen et al., 2013) show from −13.1‰ to 6.22‰. Most of the values are concentrated in the 206Pb/204Pb values of 17.84–18.79 (average 18.42); 207Pb/204Pb range of −4‰ to 6‰, comparable with those of the northwest of values of 15.46–15.62 (average 15.56) and 208Pb/204Pb values of Hebei Province. 37.93–39.75 (average 38.73). In the lead isotope evolution models The average 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb data from (Fig. 10), most of the data from the northern Taihang plot on the 265 samples of sulfide minerals from 27 deposits in the southern area between the lower crust line and the mantle line, and the five margin and the nearby areas vary from 16.92 to 18.32, 15.31 to analyses of the iron deposit from the southern Taihang Mountains 15.65 and 37.26 to 39.00 (Wang et al., 2010). Plots of the data on fall between the orogen and the mantle lines, mainly clustering near the lead isotope evolution diagrams (Zartman and Doe, 1981; the orogen line. Fig. 10) show that most of the values fall in the orogenic line/region. A set of 48 data on H–O isotopes from 17 deposits in the northern This feature suggests that the lead was mainly derived from an envi- Taihang Mountains (Table 5) shows that, except in the case of three 18 ronment similar to the orogenic belt, comparable with that in the deposits, the average δ OH2O and δDSMOW values for each deposit northwest of Hebei Province. range from −1.50‰ to 7.62‰ and from −101.72‰ to −56.09‰, fairly A group of 138 H–O isotopic data from 17 deposits in the close to that of the primary magmatic water (Fig. 11). Another group Xiaoqinling and Xiong'ershan regions shows that, except the Putang of 13 samples from 9 deposits in the northern Taihang Mountains 18 30 gold deposit, the average δ OH2O and δDSMOW values for each deposit shows δ SiNBS-28 values in the range of −0.3‰ to 0.5‰ with a mean 30 vary from 0.10‰ to 6.42‰ and from −87.41‰ to −52.58‰ for the at 0.08‰ (Table 4), consistent with the δ SiNBS-28 values of granite two regions respectively, consistent with the role of primary mag- (−0.4‰ to 0.4‰, Ding and Jiang, 1994). matic water (Table 5; Fig. 11). Thirty one helium and argon isotopic data (Table 6) from 11 deposits 13 Thirty δ CPDB data on the carbonate minerals from 9 deposits show mantle helium ranging from 0 to 38.52% with a mean of 15% in the southern margin of the NCC show variation from −4.41‰ to suggesting the involvement of mantle helium in the mineralization of −0.80‰ with most of the values clustering in the range of −4‰ to the northern Taihang Mountains during the early Cretaceous (Li et al., −2‰ (Table 5). The data suggest that the carbon might have been de- 2013; Wang et al., 2010). Helium and argon isotope data on the pyrite 13 rived from the mantle (δ CPDB from −5‰ to −2‰; Taylor and from the iron deposit in the southern Taihang Mountains indicate that Bucher-Nurminen, 1986). most of the ore-forming fluid was derived from the crust, with no more than 3% of helium (0.17% to 2.98%, average 1.43%) contribution 3.4.4. Western margin and central NCC from the mantle (Li et al., 2013; Shen et al., 2013). Whereas only few data are available for the western margin of the NCC, there is adequate data from the central NCC, particularly from 3.5. Link between metallogeny and the evolution of the NCC the Taihang Mountain region for a statistical evaluation. The northern Taihang Mountains host numerous gold, molybdenum, lead–zinc and 3.5.1. Metallogeny in response to the formation of the NCC silver deposits. The southern Taihang Mountain region is character- The formation of the NCC involved complex and multistage process- ized by skarn type iron deposits. A comparison of the chronology es during the early Precambrian, among which the two main events are S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 409 the assembly of microblocks to construct the fundamental architecture time without any major tectonic events or large scale mineralization of the NCC by 2500 Ma and the final cratonization through the collision until the Jurassic. Nevertheless, some small scale Permian and Triassic of the major crustal blocks by 1850 Ma (Santosh, 2010; Wang and Liu, mineralization occurred as mentioned in previous sections. The 2012; Zhai and Santosh, 2011; Zhang et al., 2011; Z. Zhang et al., Hongqiling gabbro type Ni–Cu deposit in Jilin Province along the 2012). During Neoarchean collision of the microblocks, around eight deep-seated fracture at the northern margin of the NCC is recognized Dongyaozhuang-type of gold deposits formed in the Wutaishan area to be of Triassic age (LÜ et al., 2011; Zhai et al., 1999). Surrounding in the northern Taihang Mountains. At the same time, in the Wutaishan the craton, the Paleozoic marked the timing of subduction of the area and Lvliangshan area of the central NCC, more than 21 large- to paleo Asian ocean, and the late Paleozoic was the period of the closure medium scale BIF type of iron deposits and meta-ultramaficrock- of the paleo-Asian ocean. Both these processes were important for hosted rutile deposits formed, which include the Shanyangping iron mantle input into continental crust and mineralization. Targets for deposit, Jingangku iron deposit and the Nianzigou Ti (rutile) deposit prospecting Paleozoic and early Mesozoic mineralization should (Jia et al., 2006; Shi et al., 2012) in the Wutaishan area, the Yuanjiachun focus on the Caledonian and Hercynian accretionary belts surround- iron deposit in the Lvliangshan area. In the Zhongtiaoshan area, south- ing the northern margin of the NCC. ern Shanxi Province, 4 large Paleoproterozoic porphyry type copper de- The Triassic was the period when the NCC amalgamated with the posits and 50 minor occurrences also formed during the amalgamation Yangtze craton. During this process, the Yangtze plate subducted un- stage of the NCC (Zhang et al., 2003). After the Neoarchean amalgam- derneath the NCC, and some of the mineral deposits in the southern ation, in the early Paleoproterozoic rifting stage, around 17 VMS type margin of the NCC are correlated to this event. However, only weak copper deposits such as those of the Hujiayu and Bizigou formed in mineralization occurred during Triassic. the Zhongtiaoshan area (Zhang et al., 2003). Except for the mineraliza- From Jurassic to Cretaceous, the eastern part of the NCC and the tion in the central NCC, gold deposits similar to the Dongyaozhuang whole of east China witnessed a major tectonic transformation from type, such as the Shibaqinghao in Inner Mongolia, the Paishanlou and N–S compression to NNE–SSW shearing. Accompanying the early trans- Nanlongwangmiao, and the Gongchangling BIF type iron deposits in formation and the onset of extension, adakitic lower crust-derived Liaoning Province, also formed during late Neoarchean at the northern granitic batholiths were emplaced which uplifted the Precambrian margin of the NCC. Large scale SEDEX and VMS types copper–(lead– basement rocks. In the Jiaodong peninsula, for instance, the Linglong zinc) and gold deposits, the Bayan Obo REE–Nb–Fe deposit, the and Kunyushan granitic batholiths were emplaced at ca. 150 Ma within Dongshengmiao, Tanyaokou, Huogeqi polymetallic deposits in the metamorphic basement represented by the Archean Jiaodong Group Langshan area and the Jiashengpan polymetallic deposit in the and Proterozoic Jingshan Group (Yang et al., 2011 and our unpublished Cha'ertaishan area of Inner Mongolia, formed in the Paleoproterozoic data). A series of intermediate and basic dikes and intermediate-felsic to Mesoproterozoic at the northern margin of the NCC (Zhai et al., plutons with mixed lower crust–mantle features formed during the 2004). Large SEDEX and VMS type deposits were also generated in the early Cretaceous accompanied by the widespread formation of numer- north-eastern margin of the NCC, including the Qingchengzi Pb– ous ore deposits. The Jiaodong gold deposits and the coeval Guojialing Zn–(Ag–Ag) deposit, the Wengquangou B deposit, two of the well and Sanfoshan granodioritic plutons and numerous intermediate- known SEDEX type deposits, and the Hongtoushan Cu–Zn deposit mafic and lamprophyre dikes (ca. 120 Ma, Cai et al., 2012; and our which is a VMS type deposit in Liaoning Province. In addition, BIF type unpublished data) in the eastern margin of the NCC, and the Shihu deposits are also found in the interior of the NCC, such as the Shuichang and Yixingzhai gold deposits and the Mapeng and Sunzhuang plu- Fe deposit in the eastern Hebei Province (Zhai et al., 1999). In the tons in the Taihang Mountains in the central NCC (ca. 130 Ma, Li et Mesoproterozoic, V–Ti–Fe and Cu–Ni–Pt deposits formed in the north- al., 2012, 2013) are among the products of the early Cretaceous ern margin (the Damiao–Heishan Fe–Ti–V–P deposit in Hebei Province) magmatism-mineralization events. Most of the ore deposits were and in the western margin (the Jinchuan Cu–Ni–Pt deposit in Gansu formed in a transitional compression to extensional tectonic regime. Province, 1508–1511 Ma, Tang and Li, 1995) of the NCC. The NE–SW ore-controlling fractures in Jiaodong peninsula show The amalgamation of the unified Eastern and Western Blocks complex sinistral and dextral shearing during the ore-forming within the NCC followed a prolonged subduction–accretion history events, with dominant sinistral movement in the early stages and prior to the final collision in late Paleoproterozoic (Santosh, 2010; dextral in the later stages (Li et al., 1996). Large scale inhomoge- Santosh et al., 2013). A series of BIF, porphyry and Dongyaozhuang neous lithosphere thinning beneath the NCC has been regarded as types of gold and polymetallic deposits were generated during this a direct geodynamic consequence of the extensive ore-forming period (Zhang et al., 2003). During the extension period after the events (e.g., Li et al., 2012, 2013). Since the magmatism and mineral- collision, a number of VMS and SEDEX types of polymetallic deposits ization are mostly concentrated in the early Cretaceous, rapid and formed in the aulacogens. It is interesting to note that such minerali- large scale inhomogeneous delamination would also be a feasible zation not only occurred in the central zone but also broadly along the model for the thinning of the NCC. northern margin of the NCC. More importantly, BIF deposits also de- It is interesting to correlate the isotopic data on the mineral developed in the interior of the craton, such as the Shuichang area in posits in different domains within the NCC with the contour map of Hebei Province, but a closer examination shows that this region the lithosphere thickness of the NCC (Fig. 3, Zhu et al., 2011). The lith- defines the boundary between the Jiaoliao microblock and the osphere thickness beneath northwest of Hebei Province in the north- Qianhuai microblock. Thus, the location of the suturing between the ern margin is >120 km, and the ore deposits here show characters of microblocks, as well as the zones of extension could mark important a reactivated orogenic belt with broad δ34S variation range, orogenic sites for economic mineralization. The Mesoproterozoic mineraliza- lead isotopes, low to high mantle helium and carbon contribution, tion can be correlated to the global rifting stage of the supercontinent and relatively high meteoric water involvement. There are no precise Columbia (Deng et al., 2004a; Hou et al., 2008; Rogers and Santosh, data available on the lithosphere thickness beneath the Xiaoqinling 2009; Santosh et al., 2009). In a recent work, Zhai and Santosh and Xiong'ershan areas in the southern margin of the NCC, but the (2013) correlated the various types of metallogeny in the NCC to sec- contour trend shows similar lithosphere thickness around 120 km, ular changes associated with global tectonics in the evolving Earth. and the characteristics of the ore deposits here are more less the same as those of the north-western Hebei. Beneath the Jiaodong pen- 3.5.2. Metallogeny in response to the destruction of the NCC insula, the lithosphere has been significantly eroded to a thickness of After the major mineralization events associated with the about 70–80 km. The geochemical data of the ore deposits here are Neoarchean micro-block assembly, Paleoproterozoic cratonization similar with those in the southern margin and suggest reactivated and Mesoproterozoic rifting, the NCC remained stable for a long orogenic belt characteristics, suggesting a relation with the features 410 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 of deposits in the south-eastern margin. Although the northern could spread to the north and was no longer pulled southwest by the Taihang Mountain region is located within the Trans-North China “captured” Phoenix plate (Goldfarb et al., 2007). Orogen in the central domain of the NCC, the ore geochemistry also shows reactivated orogenic features. Most of the deposits show 4. Ore systems in the NCC: theoretical considerations and clear meteoritic sulfur isotopic character. Compared with those in prospecting targets the north-western Hebei and the southern margin, this might be related with a relatively thinner lithosphere (b110 km). The litho- The distribution of the major ore deposits in the NCC after the for- sphere thickness beneath the eastern Hebei and Luxi areas of the mation of the craton shows that the margins of the craton are the central NCC is about 75 to 80 km, and the deposits here show most potential domains, as these regions are more prone to be in- reactivated craton characters with meteoritic-like sulfur isotopes, volved in tectonic regimes of subduction and collision and to channel- more mantle lead, helium and carbon, and less meteoric water. ing of ore fluids. However, before the destruction, the rigidity and large thickness of the NCC's lithosphere could resist relatively weak collisions from smaller plates, and thus until the end of Paleozoic, 3.5.3. Metallogeny linked with plate motion and mantle plume activity no large scale mineralization appeared. Eastern China became part of the Pacificmargintectonicdomain Theoretically, regions that are involved in multiple tectonomagmatic during Jurassic to Cretaceous when the tectonic system transformation events are the most potential sites for widespread metallogeny. The mar- was gradually completed. This region was recognized as a continental gins both in the north and south (as well as the west) of the NCC have margin orogenic belt by Deng et al. (2004a,b) and Goldfarb et al. witnessed subduction and collision (the Siberian Plate in the north and (2007). Its landward boundary was the 100-km-wide, NNE-trending the Yangtze Plate in the south) from the Caledonian to Variscanian and N–S Gravity Lineament (NSGL, e.g., Griffinetal.,1998). The Taihang even to the Indosinian (Zhai et al., 1999). These major tectonic activities Mountains are part of the cryptic NSGL in the central NCC. Although would have destabilized the craton margins, allowing deep sourced the Cretaceous mineralization in the NCC was considered as a product fluids to migrate upward forming important ore deposits. Since the of post-collisional orogeny from north by the Siberian block and the NCC had a thick keel with its lithosphere extending downwards for south by the Yangtze block (Chen et al., 2009b), nearly all the deposits more than 200 km, the formation of ore deposits during the period of the early Cretaceous age are distributed on the eastern side of the when the craton was stable should be confined to the accretionary NSGL, and almost all the N–SorNNE–SSW ore-controlling fractures belts along the craton margins. When the east side of the NSGL became are characterized by early sinistral and late dextral shearing (Li et al., tectonically active in the Yanshanian, parts of the craton including the 1996 and authors' unpublished research reports), which is consistent eastern NCC were transformed into orogenic belts (Goldfarb et al., with the cessation of Jurassic shortening and onset of continent-scale 2007). The margins of the eastern NCC, where the Caledonian and northwest–southeast extension at ca. 130 to 120 Ma (Davis, 2003; Variscan mineralization are represented, would be areas superposed by

Webb et al., 1999). A geophysical study of the E–W δvp section along the Yanshanian mineral events. In addition, in the interior of the NCC, the 37°N (Zhu et al., 2011) showed that the crust–mantle δvp structure the boundaries between the basement microblocks served as weak on the east side of the NSGL was strongly disturbed with a seismically zones along which lithospheric thinning might have occurred during anomalous zone (δvp =1%–2%), suggesting steep subduction under the Yanshanian. Furthermore, trans-lithospheric faults developed along the eastern part of the Japanese arc, that changed to largely horizontal these boundaries and served major pathways for ore fluid migration. beneath the Japanese trough and terminated beneath the NSGL Thus, in addition to the margins of the craton, the regions marking the (Fig. 13). The highly disturbed present day crust–mantle structure can boundaries between the basement microblocks and the domains sur- be traced to the late Jurassic–early Cretaceous. The lithosphere thinning rounding fault zones that mark major fluid pathways should also be of the NCC is closely related with the Pacific plate subduction under the targeted for future ore-prospecting. Asian plate, and the ‘staggered’ subduction is considered to have triggered the drastic thinning and a surge in mineralization events in the 5. Conclusions eastern NCC. Previous studies documented changes in relative plate motion Based on an overview of the geological, tectonic and metallogenic which suggest that prior to ca. 135 Ma, the now-extinct Izanagi events in the North China Craton, we come to the following general plate was undergoing orthogonal convergence with the Asian conti- conclusions. nental margin, whereas by ca. 115 Ma, its motion was parallel to the margin (Maruyama et al., 1997). The rapid change in the direction 1. At least six microblocks were amalgamated by 2.5 Ga, defining the of plate motion is correlated with the upwelling of the large Ontong– fundamental Precambrian architecture of the North China Craton. Java plume beneath the Pacific plate at ca. 124 Ma, causing a far-field The boundaries between the micro-blocks and the margins of the instantaneous reorganization of the plates, such that the Izanagi plate NCC remained as weak zones, which were prone for destruction

Fig. 13. E–W δVp proﬁle along the 37°N showing the nature of crust–mantle structure (after Zhu et al., 2011). S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414 411

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Zhou, X.H., 2009. Major transformation of subcontinental lithosphere beneath North M. Santosh is Professor at the China University of China in Cenozoic–Mesozoic: revisited. Geol. J. China Univ. 15, 1–18 (in Chinese Geosciences Beijing (China) and Emeritus Professor at with English abstract). the Faculty of Science, Kochi University, Japan. B.Sc. Zhu, R.X., Chen, L., Wu, F.Y., Liu, J.L., 2011. Timing, scale and mechanism of the destruc- (1978) from Kerala University, M.Sc. (1981) from Uni- tion of the North China Craton. Sci. China Earth Sci. 54, 789–797. versity of Roorkee, Ph.D. (1986) from Cochin University of Science and Technology, D.Sc. (1990) from Osaka City University and D.Sc. (2012) from University of Pretoria. Sheng-Rong Li is Professor at the China University of Founding Editor of Gondwana Research as well as the Geosciences Beijing (China). B.Sc. (1981) from Hebei Insti- founding Secretary General of the International Associa- tute of Geology, Visiting scholar (1986) from Geological tion for Gondwana Research. Research fields include pe- Survey of India Traning Institute, D.Sc. (1992) from China trology, fluid inclusions, geochemistry, geochronology University of Geosciences Beijing, and Postdoctorial fellow and supercontinent tectonics. Published over 350 re- (1994) from Institute of Geochemistry, Chinese Academy search papers, edited several memoir volumes and jour- fi of Sciences. Research elds include genetic mineralogy, nal special issues, and co-author of the book ‘Continents petrology, geochemistry and ecomomic geology. Published and Supercontinents’ (Oxford University Press, 2004). Recipient of National Miner- over 200 research papers and several monographs and al Award, Outstanding Geologist Award, Thomson Reuters 2012 Research Front textbook. Recipient of Beijing Municipality Outstanding Award, Global Talent Award. Teacher Award.