Ore Geology Reviews - Cugb...Tectonics The link between metallogeny and craton destruction in the North China Craton (NCC) remains poorly under-stood, particularly the mechanisms within

Ore Geology Reviews 56 (2014) 376–414

Contents lists available at ScienceDirect

Ore Geology Reviews

j ourna l homepage: www.e lsev ie r .com/ locate /oregeorev

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, Chinab School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, Chinac Faculty of Science, Kochi University, Kochi 780-8520, Japan

⁎ Corresponding author at: State Key Laboratory of Geol8232 1732; fax: +86 10 8232 2176.

E-mail address: [email protected] (S.-R. Li).

0169-1368/$ – see front matter © 2013 Elsevier B.V. Allhttp://dx.doi.org/10.1016/j.oregeorev.2013.03.002

a b s t r a c t
a r t i c l e i n f o
Article history:Received 26 January 2013Received in revised form 8 March 2013Accepted 11 March 2013Available online 22 March 2013

Keywords:North China CratonLithospheric thinningMetallogenyCraton destructionTectonics

The link between metallogeny and craton destruction in the North China Craton (NCC) remains poorly under-stood, particularly the mechanisms within the interior of the craton. In this overview, we summarize themajor stages in the history of formation and evolution of the NCC, the spatio-temporal distribution and typesofmajor ore species, aswell asmantle contribution to themetallogeny, in an attempt to evaluate the geodynamicsettings of metallogeny and the mechanisms of formation of the ore deposits. The early Precambrian history ofthe NCCwitnessed the amalgamation of micro-blocks and construction of the fundamental tectonic architectureof the craton by 2.5 Ga. The boundaries of these micro-blocks and the margins of the NCC remained as weakzones and were the principal locales along which inhomogeneous destruction of the craton occurred duringlater tectonothermal events. These zones record the formation of orogeny related gold, copper, iron and titaniumduring the early to middle Paleoproterozoic with ages ranging from 2.5 to 1.8 Ma. The Early Ordovician kimber-lite and diamondmineralization at ca. 480 Ma, the Late Carboniferous and Early tomiddle Permian calc-alkaline,I-type granitoids and gold deposits of 324–300 Ma, and the Triassic alkaline rocks and gold–silver-polymetallicdeposits occurring along these zones and the margins of the blocks correlate with rising mantle plume, south-ward 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 arealso localized along theweak zones and blockmargins. The concentration ofmost of these deposits in the easternpart of the NCC invokes correlation with lithosphere thinning associated with the westward subduction of thePacific plate. Although magmatism and mineralization have been recorded along the margins and few placeswithin the interior of the NCC in the Jurassic, their peak occurred in the Cretaceous in the eastern part of theNCC, marking large scale destruction of the craton at this time. The junctions of the boundaries between themicro-continental blocks are characterized by extensive inhomogeneous thinning. We propose that these junc-tions are probably for future mineral exploration targeting in the NCC.

© 2013 Elsevier B.V. All rights reserved.

Contents

1. Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3772. Formation and evolution of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 378

2.1. Amalgamation of microblocks . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3782.2. Two major types of craton destruction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3782.3. The timing of destruction of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3792.4. The heterogeneity of the NCC destruction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 380

3. Metallogeny in the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3813.1. Spatial distribution of ore systems . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 381

3.1.1. Gold . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3813.1.2. Molybdenum . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3813.1.3. Copper, lead and zinc . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 382

3.2. Chronology of metallogeny . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3833.2.1. Gold mineralization . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3833.2.2. Molybdenum mineralization . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 384

ogical Processes andMineral Resources, China University of Geosciences, 29 Xueyuan Road, Beijing 100083, China. Tel.:+86 10

rights reserved.

http://dx.doi.org/10.1016/j.oregeorev.2013.03.002

mailto:[email protected]


http://www.sciencedirect.com/science/journal/01691368

http://crossmark.crossref.org/dialog/?doi=10.1016/j.oregeorev.2013.03.002&domain=pdf

377S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

3.3. Ore deposit types . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3843.3.1. Gold ore systems . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3843.3.2. Molybdenum ore systems . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3893.3.3. Chaijiaying lead–zinc ore systems . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 391

3.4. Mantle contribution . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3913.4.1. Northern margin of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3913.4.2. Eastern margin of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 4063.4.3. Southern margin of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 4083.4.4. Western margin and central NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 408

3.5. Link between metallogeny and the evolution of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 4083.5.1. Metallogeny in response to the formation of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 4083.5.2. Metallogeny in response to the destruction of the NCC . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 4093.5.3. Metallogeny linked with plate motion and mantle plume activity . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 410

4. Ore systems in the NCC: theoretical considerations and prospecting targets . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 4105. Conclusions . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 410Acknowledgments . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 411Appendix A. References for Tables 1 to 6 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 411References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 411

1. Introduction

The construction and destruction of cratons have received muchattention in recent years from geological, geophysical, geochronolog-ical and tectonic perspectives (e.g., Zhang et al., 2013, and referencestherein). In the past, various models including thermo-mechanical(e.g. Davies, 1994; Ruppel, 1995) and chemical (e.g., Bedini et al.,1997) erosion as well as delamination (e.g., Bird, 1978, 1979; Kayand Kay, 1993) have been proposed to explain the process ofdecratonization. The North China Craton (NCC) provides a classic ex-ample of craton destruction where the erosion model (e.g., Griffin etal., 1998; Lu et al., 2000; Menzies and Xu, 1998; Xu et al., 1998;Zhang et al., 2005; Zheng, 1999), and the delamination model(Deng et al., 2004a,b; Gao et al., 2002; Wu and Sun, 1999) havebeen invoked to explain the extensive lithospheric thinning, particu-larly in the eastern and central domains of the craton during the Me-sozoic. Those who favor the thermo-mechanical erosion modelattributed recycling of the asthenosphere and mantle plume upwell-ing as the major cause which resulted in erosion from the bottom ofthe lithosphere. In contrast, those who argue in favor of the lattermodel proposed the delamination of eclogitic material generatedthrough continental collision and crustal thickening as the majorcause for lithospheric thinning beneath the NCC.

Although several studies have addressed the geodynamics associ-ated with metallogeny in the NCC (e.g., Chen et al., 2007, 2009a,b; Liet al., 1996; Li et al., 2012, 2013; Mao et al., 2005a,b; Zhai and Santosh,2013; Zhai et al., 2002), only few have investigated the link betweenmetallogeny and the process of lithospheric destruction in the NCC.The criteria and predictions for the different mechanisms of lithospheretransformation are markedly different (Zhou, 2009), and therefore it isimportant to evaluate the process which is more likely to generatelarge-scale metallic deposits.

The heterogeneity of the lithospheric destruction in the NCC, partic-ularly the inhomogeneous thinning, has been recognized in severalstudies in the past (e.g., Deng et al., 2004a,b; Luo et al., 2006; Menzieset al., 1993) and confirmed in more recent studies (H.F. Zhang et al.,2012; Tang et al., 2013). This heterogeneity has been documented notonly from the marginal domains of the craton both from the Westernand Eastern Blocks of the NCC across the Great Hinggan Range–TaihangMountain gravity lineament (HTGL, e.g., Xu et al., 2009), but also fromthe central part of the NCC, along the Trans-North China Orogen(TNCO) (e.g., Li et al., 2012, 2013; Tang et al., 2013). Integrated studiesof the NCC based on high-resolution seismic images combined with ob-servations on surface geology, regional tectonics and mantle dynamicshave revealed marked variations in crustal and lithospheric structure

and thickness, upper mantle anisotropy, and discontinuity structuresand thickness of themantle transition zone near the boundary betweenthe eastern and central parts of theNCC (Chen, 2009, 2010; Cheng et al.,2013). Preliminary studies have identified a systematic relationship be-tween the inhomogeneous lithosphere thinning and variations in thenature and distribution of ore systems (Li et al., 2012, 2013). However,systematic investigations to evaluate the possible relationship betweenthe heterogeneity of lithosphere structure and metallogeny, which arefundamental to the formulation of exploration strategies for ore de-posits, have not been carried out.

There is amarked distinction in the distribution of the youngermag-matic rocks in the NCC, with Carboniferous to Triassic suites occurringin the craton margin, and Jurassic to Cenozoic suites extending gradu-ally into the interior. This distribution probably suggests that the de-struction of the NCC started from its margins to the interior, reflectingthe vulnerability of plate boundaries and weak zones on cratonic de-struction (Xu et al., 2009). Within the basement of the NCC, at leastsix Precambrian microblocks have been identified such as the Alashan,Jining, Fuping, Qianhuai, Xuchang and Jiaoliao blocks (Zhai et al.,2005), the amalgamation of which occurred during the Neoarchean,and subsequent rifting–subduction–collision in the Paleoproterozoicled to the final stabilization of the craton (e.g., Santosh, 2010; Santoshet al., 2007; Zhai and Santosh, 2011; Zhai et al., 2005). The relationshipbetween these microblocks and their boundaries with the inhomoge-neous lithosphere thinning remain equivocal, although it is generallyagreed that there is a strong link between metallogeny and thegeodynamics of the NCC (e.g., Chen et al., 2007, 2009a,b; Li et al.,2012, 2013;Mao et al., 2005a,b, 2011;Qiu et al., 2002; Yang et al., 2003).

Previous workers have adopted different tectonic classificationschemes for the major mineral deposits in the NCC such as orogenicgold (e.g., Mao et al., 2002, 2005a,b, 2008, 2011; Qiu et al., 2002), andorogenic metals (Chen et al., 2004, 2007, 2009a). Several other classifi-cations have also been proposed such asmesothermal–epithermal type(e.g., Chen et al., 1989; Li et al., 1996; Li et al., 2012, 2013), skarn type(e.g., Li et al., 2013; Shen et al., 2013), porphyry type (e.g., Li et al.,2003), cryptoexplosive breccia type (e.g., Li, 1995), quartz vein type(e.g., Nie et al., 2004; Pirajno et al., 2009), fracture-altered and brecciatype (e.g., Mao et al., 2008; Qiu et al., 2002), etc. Among these classifica-tions, somewere based on the genesis of the ore deposit (genetic type),and the others took into account the ore characteristics (industrialtype). Although the occurrence of major ore deposits in the marginaldomains of the NCC are well established, their geneses remain debated.Most importantly, the ore deposits and prospecting potential within theinterior of the NCC, regardless of the genetic and industrial types, arepoorly understood.

378 S.-R. Li, M. Santosh / Ore Geology Reviews 56 (2014) 376–414

In this overview, we attempt to characterize the ore deposits bothin the interior and marginal domains of the NCC and examine theirprospecting potential. Our work provides new insights on the possi-ble relationship between metallogeny and lithosphere thinning asso-ciated with craton destruction.

2. Formation and evolution of the NCC

2.1. Amalgamation of microblocks

Based on the distribution of early Precambrian rocks, and throughintegrated geological, geochronological and geophysical information,at least six micro-continental blocks have been identified within theNCC (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,Ji'ning, Ordos, Fuping or Xuchang, Qianhuai, Xuhuai and Jiaoliaoblocks (Fig. 1). Rock types and their distribution in these micro-blocks display distinct differences, with Neoarchean volcanism andmagmatism at 2.9–2.7 Ga and 2.6–2.45 Ga, indicating that thesemicro-blocks were not amalgamated into a coherent craton until atleast 2.5 Ga. Several granitic intrusives with ages around 2.5–2.4 Gainvade the basement rocks in all these blocks (e.g., Geng et al.,2012; H.F. Zhang et al., 2012; Wu et al., 1998; Z. Zhang et al., 2012),suggesting that the microblocks were assembled prior to the em-placement of these granitoids, and that these microblocks define theunified tectonic architecture of the NCC at the end of Neoarchean(Li et al., 1997). An alternative framework of the NCC basement wassuggested with two discrete blocks, the Western and Eastern Blocks,developed independently during the Archean and finally collidedalong the central zone (Trans-North China Orogen) to form a coher-ent craton during a global Paleoproterozoic collisional event at1.85 Ga (Zhao et al., 2005, 2007).

The nature of the NCC in the late Neoarchean has been addressedthrough several models. Among these, the vertical accretion withmulti-stage cratonization (Zhao et al., 1993) and marginal accretion-reworking (Jin and Li, 1996) are popular. Arc–continent or continent–continent collision models have also proposed to explain the earlyPrecambrian evolution of this craton (Zhai and Santosh, 2011). A

Fig. 1. Boundaries and locations of the Newarchean micro-continental blocks in the NCCXCH = Xuchang or Fuping block, XH = Xuhuai, and JL = Jiaoliao block.After Zhai and Santosh (2011).

volcanic–plutonic island arc zone characterized by TTG (tonalite–trondhjemite–granodiorite) rocks of 2.56–2.5 Ga along the western/outer side, and calc-alkaline granitic rocks of 2.5–2.45 Ga on theeastern/inner side have been suggested in the western part of theJiaoliao continent block (Wu et al., 1998; Zhao et al., 1993), implyingarc–continent collision between the Jiaoliao block and the Qianhuaiblock. Based on the distribution of high-pressure granulites, Zhai et al.(1992) proposed continent–continent collision between the Qianhuaiand Fuping blocks and between the Qianhuai and Ji'ning blocks at2.5–2.6 Ga. Zhai et al. (2000) and Zhai and Santosh (2011) also pro-posed that between 2.6 and 2.45 Ga, the six microblocks in the NCCwere amalgamated together by continent–continent, continent–arc orarc–arc collision (Fig. 1c).

2.2. Two major types of craton destruction

Thermo-mechanical or chemical erosion and delamination are con-sidered as the two major mechanisms that led to the destruction of theNCC. According to the erosion model, the bottom of the lithosphere issoftened through heating by upwelling asthenosphere, and the shearstress from the horizontal flow of the asthenosphere would transferthe weakened lithospheric bottom to the asthenosphere. This type oferosion could upwell the thermal conduction of the asthenosphereinto the bottom of the lithosphere leading to further erosion and thin-ning (Davies, 1994; Ruppel, 1995). The thermo-mechanical erosionmodel has been developed into a coupled scheme of both thermo-mechanical and chemical erosions (e.g., Ji et al., 2008; Xu, 1999). Theduration of the thinning from the thermo-mechanical erosion dependson the temperature of the convective asthenosphere and the originalthickness of the lithosphere. Based on a numerical simulation, Davies(1994) suggested that the duration for thinning a 200 km thick litho-sphere to 100 km would be about ten million years provided that aplume is present at the bottom. However, in the absence of a plume,this process might take about 50–100 million years.

The delamination model emphasizes the processes of regional tec-tonics. When cratons undergo tectonic convergence, such as platesubduction or collision, the crustal thickness increases leading to highgrade metamorphism and mineralogical phase changes to generate

. ALS = Alashan block, JN = Jining block, OR = Ordos Block, QH = Qianhuai block,


eclogite at the bottom. Eventually, the high density eclogitic materialwould break off and drop down into the mantle, leading to the delami-nation of the lithosphere (Beck and Zandt, 2002; Bird, 1979; Pysklywecet al., 2000). Thus, based on geological and tectonic models, Zhai et al.(2002), Deng et al. (2006) and Gao et al. (2008), among othersdiscussed the thickening of the continental crust of the NCC and delam-ination during the Yanshanian.

Recent studies have emphasized the role of interaction betweenmelt or fluid and mantle peridotite on the micro-mechanics of chem-ical erosion (e.g., Xu et al., 2013). Investigations on mantle xenolithshave led to the identification of lithospheric alteration by melt orfluid. The spatial variation of isotopic characteristics in the source re-gion, low Mg# values, systematic changes in the mineral phases, dis-turbance of the Re/Os isotopic system, mixed tDM ages, chemicalzoning of minerals, among other features, have been documented.These features have been correlated to variations in the nature andcharacteristic of the lithospheric mantle during craton destructionprocess (e.g., Reisberg et al., 2005; Zhang et al., 2004; Zhou, 2006;Zhang et al., 2008; Zhang et al., 2013).

Zhou (2009) summarized the criteria to evaluate the two mecha-nisms of lithospheric thinning. The thermo-mechanical/chemical ero-sion model is related with a prolonged and continuous magmaticactivity, initially sourced from the lithosphere and gradually extendingto asthenosphere. In this case, the resulting features include lithosphereextension, chemically layered lithosphere with different ages, and vol-canic or sub-volcanic activity with different chemistry correlatingwith changes in the source characteristics. The delamination model, incontrast, is reflected in short and episodic magmatism derived fromthe asthenosphere, rapid extension of the lithosphere accompanied bystrong surface erosion, and younger components dominating the litho-sphere with volcanic or sub-volcanic material displaying the signatureof recycled ancient crust.

Apparently, evidence in support of both these phenomena— erosionand delamination— exists in the NCC, and a combined erosion plus de-lamination model is gaining acceptance with the notion that these twomodels are not mutually exclusive (e.g., Wu et al., 2008).

2.3. The timing of destruction of the NCC

Craton destruction is not only related to the thinning of the cratonlithosphere, but also involves changes in composition of the litho-sphere, its thermal state and rheological nature. The loss in the stabil-ity of craton as a whole is recognized as craton destruction ordecratonization by Zhu et al. (2011). Theoretically, the initiation oflithosphere thinning and the variations mentioned above mark thestart of craton destruction. Since not all of these variations can necessar-ily show clear geological records on the earth surface, only magmatism,tectonic evolution, palaeogeography andmetallogeny are taken as indi-cators of the destruction process. Among these, themagmatic signatureis the most commonly employed criterion at present.

Since its final cratonization during Paleoproterozoic, the NCC hasremained largely stable for a long time. Intermittent small scale mag-matic activity has been recorded in the Mesoproterozoic, such as themafic dyke swarms, K-rich volcanics in the Dahongyu Formation, theMiyun rapakivi granite north of Beijing city, and theDamiao anorthositein the northern part of Hebei province (Li et al., 2009; Zhang et al.,2009), which might all correlate with the rifting event of the Columbiasupercontinent of which the NCC was an integral part (e.g., Santosh,2010). Younger magmatic episodes include the Early Ordoviciandiamond-bearing kimberlite of ca. 480 Ma in the Mengyin area,Shandong province, and the Fuxian area, Liaoning province (Chi andLu, 1996; Xu, 2001). The magmatism since Carboniferous is classifiedinto 5 periods (Xu et al., 2009). The earliest phase is recorded fromthe northern margin of the NCC with a series of calc-alkaline, I-typegranitoids of 324–300 Ma, correlated with the southward subductionof the paleo Asian plate (Fig. 2a; Zhang et al., 2007). Relatively weak

magmatism in the Late Triassic characterized mostly by alkaline rockshas been documented from the northern and eastern margins of theNCC (Yang and Wu, 2009; Yang et al., 2007). The magmatism duringthe Jurassic is also mainly distributed in the north and east margins ofthe NCC, with granitoids comprising themajor suite (Fig. 2b). Examplesinclude the Tongshi intrusive complex emplaced at 180.1–184.7 Ma inthe Luxi region (Lan et al., 2012), and the Linglong and Luanjiahe gran-ites emplaced at 157–159 Ma in the northwest Jiaodong region (Yang etal., 2012). The magmatism attained its peak in the Cretaceous and wascharacterized by a wide range of felsic and mafic igneous rocks, distrib-uted mainly in the Yanshan Mountains, Taihang Mountains, Jiaodongand Luxi regions. TheMapeng granitic pluton in the TaihangMountainsand the Sunzhuang dioritic pluton in the Heshan Mountain wereemplaced at ca. 130 Ma (Li et al., 2012, 2013), and the Guojialing grano-diorites in the north-western Jiaodong were also emplaced in the earlyCretaceous (129 Ma, Yang et al., 2012). The magmatism during the endof Cretaceous to the Neogenewas characterized by tholeiitic and alkalinebasalt distributed within extensional basins and along deep-seated frac-tures within the craton.

Although the duration of the magmatism cannot be directly corre-lated with the duration of craton destruction, the ages of thesemagmatic suites provide important constraints on the lithosphericthinning event. Thus, Xu et al. (2009) suggested that the initiationof the NCC lithosphere thinning would not be later than the Carbon-iferous and Triassic, respectively in the northern and eastern margins,and the southward subduction of the Paleo Asian Ocean Plate and thenorthward subduction of the Yangtze Plate as well as the consequentcollision triggered the activity along the northern and southern mar-gins of the NCC. The thinning of the NCC peaked in the late Jurassic toCretaceous and continued even to the early Cenozoic, during aprotracted period of more than 100 Ma (Xu et al., 2009).

Geochemically, the Cenozoic basalts in the NCC show increasingalkalinity with time, suggesting an increase in the depth of themagma source (Xu et al., 2009). Combined with the ca. 100 Ma basaltin the Fuxin region derived from the asthenosphere, Wu et al. (2008)suggested that the destruction of the NCC occurred in the Cretaceousearlier than 100 Ma. Zhu et al. (2011) suggested that the start of de-struction of the NCC should be later than the Late Mesozoic when thePacific plate subducted towards west and the Mongolia–Okhotsk Seaclosed which led to the transition of the tectonic system.

In the central part of the NCC, previous studies on the Shihu golddeposit and the Xishimen iron deposit from the Taihang Mountains,and their genetically related intrusive rocks led to the suggestionthat the Shihu gold deposit witnessed a greater amount of mantleinput as compared to the Xishimen iron deposit during their forma-tion in the Early Cretaceous (ca. 130 Ma); however, the major compo-nents for both were derived from the lower crust (Cao et al., 2011a,b;Li et al., 2012, 2013). Combined with published geophysical data (Weiet al., 2008), Li et al. (2013) suggested that the continental litho-sphere is markedly thinner under the Fuping region than that underthe Wu'an region, and that the inhomogeneous lithosphere thinningin the central NCC occurred at least as early as 130 Ma. Further studieson the major magmatism and metallogenesis in the Hengshan terrainrevealed that these were part of the strong magmatic–metallogenicevent that took place in the Taihang Mountains at ca. 130 Ma ago, andthe lithosphere underneath the Hengshan terrain was strongly thinnedand decoupled during the early Cretaceous, with the state of thedestructed lithosphere largely preserved through the Cenozoic topresent (Li et al., 2012, 2013).

Although different opinions exist concerning the timing of theNCC destruction based mainly on magmatism, all the available evi-dence indicates that the Cretaceous marks the peak for lithospherethinning or destruction in the NCC. The magmatic pulses can be clear-ly divided into several periods or stages, and the duration of eachstage was relatively short, showing a prominent instantaneity. Theo-retically, any magmatic event after final cratonization, regardless of

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,should be taken as a record of the craton destruction. However, theeffect of the destruction would sometimes be local, or can even leadto episodes of lithospheric accretion, such as in the case of the Ceno-zoic pulse in the NCC.

2.4. The heterogeneity of the NCC destruction

As mentioned in a previous section, the magmatism in the NCCsince Carboniferous has been classified into 5 periods with differentcharacteristics for the rock suites formed at different periods (Xu etal., 2009). If magmatism after cratonization is a robust record of thecraton destruction, the magmas with different characteristics mustrepresent different levels or tectonic domains. This would mean thatthe loci of craton destruction shifted vertically with time. Further-more, the magmatism occurred at different locations in the NCC, im-plying that the destruction also shifted laterally.

Recent studies, such as for example from the Late Jurassic (157–159 Ma) Linglong and Luanjiahe granites in the northwest Jiaodongpeninsula in the eastern NCC, show high Na2O + K2O, Al2O3, Sr/Y ra-tios, LREEs and LILEs (Rb, Ba, U, and Sr), low MgO, HFSEs (Nb, Ta, P,and Ti) and εHf(t) values (Yang et al., 2012). These characteristicsare comparable to adakitic rocks, suggesting that the Linglong andLuanjiahe granitoids formed under relatively high pressure condi-tions and were likely derived from partial melting of the thickenedlower crust of the NCC. The early Cretaceous (129 Ma) Guojialing

granodiorites in the northwest Jiaodong peninsula, however, possesshigh CaO, TFe2O3, MgO, LREEs, LILEs, Sr/Y, εNd(t) and εHf(t) values,and are metaluminous, with depletion in HFSEs (Yang et al., 2012),suggesting the involvement of mantle components in the magmaticsource. Yang et al. (2012) correlated the formation of magma withthe processes accompanying the subduction of the Pacific plate be-neath the NCC and the associated asthenospheric upwelling.

The distribution of the magmatic rocks in the NCC (Fig. 2) showsthat the magmatism occurred at the margins of the NCC in the Car-boniferous to Triassic, extended from the margin to the inner areasof the NCC in the Jurassic, and reached its peak in the Cretaceous(Xu et al., 2009). This suggests that the destruction of the NCC startedat its margins, and extended to the inner domains with time. The NCCis bound by Phanerozoic orogenic belts with the Xing'an–Mongoliaorogenic belt in the north, the Qinling–Dabie orogenic belt in thesouth, the Sulu orogenic belt and the subduction zone between theEurasia–Pacific plates in the east, and the Qilian orogenic belt in thewest. The margins of the NCC, therefore, are all weak zones prone tobe eroded or delaminated leading to the thinning of the lithosphere.The Trans-North China Orogen or the Daxing'an–Taihang Zone inthe central part of the NCC, as a Paleoproterozoic orogenic belt(Zhao et al., 2007), or the boundary between the microblocks Fupingand Qianhuai (Zhai and Santosh, 2011), is also a major weak zone (Liet al., 2013; Xu et al., 2009). Magmatism and metallogeny of ca.130 Ma have led to lithosphere thinning beneath the Taihang Moun-tains (Li et al., 2012, 2013; Shen et al., 2013). If the structure of the

image of Fig.�2


basement of the NCC is taken into consideration, the weak zones in-clude the boundaries of the micro-blocks beside the Taihang Moun-tains. The NNE Tan–Lu Fault Zone, the major lithospheric fracturezone in eastern China, formed during the Mesozoic is a prominentweak zone in the interior of the NCC. During the northward subduc-tion of the Izanagi plate in the early Cretaceous, the Tan–Lu FaultZone witnessed counter-clockwise strike-slip activity, and served asa major channel for the upwelling of asthenosphere materials (Guoet al., 2013).

Recent geophysical data and their geological interpretations(Fig. 3) reveal pronounced variation in the thicknesses of the litho-sphere beneath the NCC which can be spatially correlated with theboundaries between the micro-blocks, the Trans-North China Cratonor Daxing'an–Taihang Zone, the Tan–Lu Fault Zone and the marginsof the craton, suggesting strong heterogeneity in cratonic architecturefollowing the destruction. Coupled with the distribution of themagmatism in the NCC, it is obvious that the regions with thin litho-sphere show clustered large scale magmatic rocks of Mesozoic age,implying that the extensive thinning of the lithosphere was coevalwith the Mesozoic magmatism. This finding has also been extendedto metallogeny in recent studies with evidence from the TaihangMountains (Li et al., 2013) and the Heshan terrain (Li et al., 2012).

3. Metallogeny in the NCC

3.1. Spatial distribution of ore systems

During the prolonged tectonic evolution of the NCC, several typesof economic ore deposits formed at different times. Ore deposits ofPrecambrian age, particularly nonferrous metallic deposits, are widelydeveloped in the northern margin of the craton (Rui et al., 1994).However, in this paper, we focus mainly on the mineralization thatformed subsequent to the cratonization of the NCC in an attempt toevaluate their relationship with the decratonization event.

3.1.1. GoldGold is one of the most important mineral resources in the NCC.

The major gold deposits are found in the Jiaodong peninsula (easternShandong province), the Xiaoqinling region (south-eastern Shaanxiprovince and the west of Henan province) and the Jibei region(northern Hebei province) (Fig. 4a). The Jiaodong peninsula has longbeen known to host the largest cluster of gold deposits in China, andhas been the major production in the country. The Xiaoqingling region

Fig. 3. Maps of mantle transition thickness (a) and lAfter Zhu et al. (2011) with revisions.

hosts the second largest gold cluster. Gold deposits in the NCCare dominantly distributed along the central domains of the eastern,southern and northern margins of the craton. In the Jiaodong region,located within the eastern margin of the NCC, several important golddeposits occur such as the Linglong quartz-vein type and the Jiaojiafracture-filling and altered type, both of which are recognized assuper-large gold deposits with gold reserve exceeding 100 t. Severalfracture-filling and altered type gold deposits, such as those ofSanshandao, Xincheng, Dayingezhuang, Dongfeng and the Canzhuangare also among the super-large category. The gold reserves of theJinqingding and Denggezhuang quartz-vein type gold deposits, thetwo largest gold deposits in the east of the Jiaodong region, exceed100 t. In the Xiaoqinling region in the south-western margin of theNCC, large scale mining for gold is traced to the Ming Dynasty(A.D.1368–1644). More than 1200 auriferous quartz veins have beenexplored in the Xiaoqinling region, among which about 400 t of goldreserve has been proved and more than 10 large and super-large golddeposits are exploited. These are represented by the Dongtongyu,Wenyu, Dongchuang, and Yangzhaiyu quartz-vein type gold deposits.Several large crypto-explosive-breccia type gold deposits, such as theQiyugou gold deposit, and fracture-filling and altered type, such as theShanggong gold deposit, are found in the Xiong'ershan region in easternQinlingwithin the southernmargin of theNCC (Chen et al., 2008). In theJibei region, northern margin of the NCC, the Xiaoyingpan quartz-veingold deposit, the Dongping quartz-vein–altered–fracture transitiontype gold deposit, and the Jinchangyu quartz-vein gold deposit areamong the large-super large gold deposits. Apart from the gold depositslocated along themargins of theNCC, some large scale gold deposits arealso found in the interior of the NCC. These include the Shihu auriferousquartz-vein in the west of Hebei province within the central domain ofthe Taihang Mountains (Li et al., 2013) and the Yixingzhai auriferousquartz-vein in the northeast of Shanxi province, at the northern domainof the Taihang Mountains (Li et al., 2012). In the Luxi area, west of theTan–Lu fault zone, the Guilaizhuang cryptoexplosive breccia type golddeposit and the Yinan skarn type gold deposit have also been provedto be large scale with gold reserves of more than 20 t (Guo et al.,2013; Mao et al., 2005a,b).

3.1.2. MolybdenumSeventeen large and medium molybdenum deposits have been

identified in the NCC (Fig. 4b). The southern and northern margins ofthe craton are the main locations of the large ones. The Luanchuan–Lushi area of Henan province in the central part of the southern margin

ithosphere thickness and (b) beneath the NCC.

image of Fig.�3


of the NCC, hosts clusters of several important molybdenum depositsin Asia, such as the Nannihu, Sandaozhuang, Shangfanggou andYechangping deposits. Recently, the molybdenum deposits of Laiyuanin Hebei province in northern Taihang Mountains within the centralNCC are prospected as large molybdenum reserves (our unpublisheddata).

3.1.3. Copper, lead and zincCopper deposits are not well developed in the NCC, with only a

few large deposits occurring in the west and northeast margins. How-ever, small scale copper deposits occur scattered in other margins andin the cratonic interior (Fig. 4c, Zhao et al., 2006a).

Until now, no super-large Pb–Zn–(Ag) deposits have been reportedfrom the NCC. However, a number of large and middle scale Pb–Zn–(Ag) deposits have been identified from the northernmargin, with-in the central segment of the southernmargin and the interior region inthe Taihang Mountains (Fig. 4d, Zhao et al., 2006b). The Chaijiayinglarge scale Pb–Zn–Ag deposit located at the northwestern part of the

Fig. 4. Locations of ore deposits in the NCC. a — gold, b — m

Hebei province within the northern margin of the NCC, is one of thewell-studied representatives. The Mesoproterozoic Dongshengmiao,Tanyaokou, Huogeqi and Jiashengpan SEDEX deposits in the Langshan–Cha'ertaishan region, northern margin of the NCC, were discovered re-cently with overprinting Variscanian mineralization (Zhai et al., 2004).

The spatial distribution of the metallic deposits shows that notonly the margins of the blocks/craton, but also the interior of theNCC bear important metallic deposits. Notably, the important ore de-posits in the interior of the craton are mostly located in the TaihangMountains (Li et al., 2012, 2013; Shen et al., 2013; Wang et al.,2013), which defines the boundary between the Fuping, Ordos andQianhuai microblocks, as well as the collisional suture between theWestern and Eastern Blocks (Santosh et al., 2012). A similar case inthe eastern NCC is the occurrences in the western part of the Tan–Lu fault zone, which defines the boundary between the Qianhuaiand Jiaoliao microblocks (Fig. 4a–e). In the other basement bound-aries between the microblocks, only a few ore deposits are found.In addition, within the same tectonic region, the ore deposits are

olybdenum, c — copper, d — zinc–lead, and e — iron.

image of Fig.�4

Fig. 4 (continued).


scattered heterogeneously, such as for example in the southern mar-gin of the NCC, where the ore deposits are mainly clustered in themiddle section.

3.2. Chronology of metallogeny

3.2.1. Gold mineralizationGold mineralization in the NCC formed mainly during 4 periods

(Table 1). The first phase is during Paleoproterozoic, when typicalorogenic gold deposits formed such as the Diantou (2416 Ma, Luo etal., 2002), Xiaobanyu (2317 Ma, Luo et al., 2002), Dongyaozhuang(2451 Ma, Chen et al., 2001), Hulishan, Kangjiagou, Daiyinzhang,Shangyanghua, and Xiaozhongzhui ductile–brittle shear zone typegold in the Wutai Mountain, northeast of Shanxi province, centralNCC with ages ranging from 2.3 to 2.5 Ga (Zhang et al., 2003).These gold deposits are all small scale with gold reserves less than10 t. The second period is the early to middle Permian, when some

porphyry type gold deposits, such as the Zhulazhaga (280 Ma, Li etal., 2010) and the Bilihe (273 Ma, Qing et al., 2012) formed in theInner Mongolia region, at the northern margin of the NCC. The thirdperiod is the middle Triassic, when the Qingchengzi gold–silver-polymetallic deposits (ca. 239 Ma, Xue et al., 2003) in the Liaoningprovince formed along the north-eastern margin of the NCC. Thefourth period is in the early Cretaceous, when a large number ofgold deposits formed in the northern, southern and eastern marginsof the NCC. Most of the super-large gold deposits, such as those ofJiaodong represented by the Linglong quartz vein type (121 Ma, Liet al., 2008), and the Jiaojia fracture-altered type (120 Ma, Li et al.,2003), formed in the eastern margin of the NCC. Similar deposits inthe southern margin of the NCC include the Xiaoqinling quartz veingold deposits (127–129, Wang, 2010), and the Dongping-quartzvein-fracture altered gold deposit (140 Ma, Li et al., 2010) in thenorth-western segment of the Hebei province. Notably, some largescale gold deposits also formed in the interior of the NCC. The Shihu

image of Fig.�4

Fig. 4 (continued).


quartz vein gold deposit (130–140 Ma, Cao et al., 2012; Li et al., 2013)and the Yixingzhai quartz vein gold deposit (132 Ma, Li et al., 2012;Ye et al., 1999) are two representatives in the central NCC.

3.2.2. Molybdenum mineralizationThemolybdenum deposits in the NCC formed during three periods

(Table 1). The first is in the early to middle Triassic, when some smallto medium scale molybdenum deposits formed in the northern andsouthernmargins (223–258 Ma). There are only a few large scale mo-lybdenum deposits such as the Sadaigoumen porphyry molybdenumdeposit (238 Ma, Shen, 2011) in the north of Hebei province, and theDasuji porphyry molybdenum deposit (223 Ma, Zhang et al., 2009) inthe Inner Mongolia Autonomous Region, the northern margin of theNCC. The second period is in the early–middle Jurassic when somelarge scale molybdenum deposits formed at the north-eastern marginof the NCC and a few small scale deposits developed in the southernmargin. The large molybdenum deposits are represented by theLanjiagou (187 Ma, Huang et al., 1996) and the Beisongshumao(162 Ma, Li et al., 2009) porphyry type deposits, as well as theYangjiazhangzi (190 Ma, Huang et al., 1996) skarn type deposit inthewestern part of Liaoning Province. Themost importantmolybdenumdeposits formed in the third period during early Cretaceous in the south-ern and northern margins, as well as in the interior of the NCC. TheLuanchuan porphyry typemolybdenumdeposits in the southernmarginof the NCC including the Sandaozhuang (145 Ma, Mao et al., 2005a,b),Nannihu (142 Ma, Mao et al., 2005a,b, and Shangfanggou (144 Ma,Mao et al., 2005a,b) are among the major molybdenum deposits inChina. The skarn copper–molybdenum deposits, the Shouwangfendeposit (148 Ma, Huang et al., 1996) and Xiaosigou deposit (134 Ma,Huang et al., 1996) at the north-eastern margin of the NCC are alsowell known. Recently, the Laiyuan porphyry–skarn copper–molybde-num deposits in the central NCC has proved to be an important depositbased on drill core studies (our unpublished data).

3.3. Ore deposit types

3.3.1. Gold ore systemsAccording to their nature of occurrence, the gold deposits in the

NCC can be divided into the following types: 1) Paleoproterozoic

ductile–brittle shear zone type (the Dongyaozhuang type); 2) Perm-ian porphyry-dominated type (the Bilihe type); 3) Jurassic (?)cryptoexplosive breccia type (the Guilaizhuang type); 4) Cretaceousquartz vein type (the Linglong type); 5) Cretaceous fracture alteredtype (the Jiaojia type); 6) Cretaceous strata-bound type (the Dujiayatype); 7) Cretaceous skarn type (the Yinan type); 8) Cretaceouscryptoexplosive breccia type (the Qiyugou type) and 9) Cretaceousquartz vein-fracture altered-type (the Dongping type).

3.3.1.1. The Paleoproterozoic Dongyaozhuang type. This type includesthe Dongyaozhuang, Diantou, Xiaobanyu, Hulishan, Kangjiagou,Daiyinzhang, Shangyanghua and Xiaozhongzhui gold deposits in theWutai Mountain (Fig. 5a) in the central NCC. These deposits occurwithin Archean greenstones, the protoliths of which are consideredto be a suite of intercalated mafic and intermediate to felsic volcanics.Metamorphosed mafic and intermediate dykes also occur in the orefield (Fig. 5b). The greenstones and dykes underwent strong ductileto brittle shearing and metamorphic hydrothermal alteration. Fromthe metamorphosed mafic rocks to the orebody, alteration zoning isobserved with carbonate–quartz–chlorite–albite marginal zone grad-ing into quartz–sericite–pyrite intermediate zone, and further totourmaline–pyrite–quartz core. Most of the orebodies are stratiformand consist of highly silicified and pyritic schist wall-rocks with finegrained albite, sericite, quartz, tourmaline, ankerite, dolomite, calciteand chlorite as common gangue minerals. Pyrite, chalcopyrite, pyr-rhotite, magnetite and native gold (occasionally arsenopyrite andchalcocite) are the main ore minerals. The ore is dominated byveinlet-disseminated style with gold grades ranging from 1 to 10 g/twith an average of 3.5 g/t. The fineness of the native gold is greaterthan 905 (Zhang et al., 2003; our unpublished data).

3.3.1.2. The Permian Bilihe type. The Bilihe porphyry-dominated typegold deposit is a newly found large scale gold deposit in the SonidYouqi area (Qing et al., 2012). The deposit is located in the Caledonianaccretionary orogen along the northern margin of the NCC. TheBainaimiao, Baiyinhe'er, Hedamiao and Baiyinchagan gold depositsare clustered nearby. A suite of Permian intermediate-felsic volcano-sedimentary rocks (dated as 281.1 ± 4.3 Ma by zircon LA-ICP-MSU–Pb method, Qing et al., 2012) are the dominant rocks. I-type

image of Fig.�4

Table 1Isotopic 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,Inner Mongolia

Au 266.8 ± 3.9 Re–Os Molybdenite Wang et al., 2007

2 Shibaqinghao Inner Mongolia 277 ± 1.73 40Ar–39Ar Biotite Chen et al., 19963 Bilihe Inner Mongolia 272.7 ± 1.6 Re–Os Molybdenite Qing et al., 20114 Zhulazhaga Alashan, Inner Mongolia 282.3 ± 0.9 40Ar–39Ar Quartz Li et al., 20105 Dongping Chongli, Hebei Province 187 ± 0.3

188 ± 0.4177.4 ± 5

40Ar–39Ar K-feldspar Jiang et al., 2000

140.3 ± 1.4 LA-ICP-MS Zircon Li et al., 20106 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., 20127 Bieluwutu Sunite, Inner Mongolia Pb–Zn 279–481 Sm–Nd Nie et al., 20088 Chaganbulagen Xin Barag Left Banner,

Inner Mongolia131.6 K–Ar Pan et al., 1990

9 Baiyinnuoer Bairin Left Banner,Inner Mongolia

170/161 Rb–Sr Zhang et al., 1991

10 Haobugao Bairin Left Banner, InnerMongolia

Yanshanian Dai et al., 2005

11 Caijiayingzi Zhangbei, Hebei 130 K–Ar Lv et al., 200412 Yingfang Fengning, Hebei 120.66 ± 3.16 K–Ar Liu et al., 1997,

Duan et al., 200813 Sadaigoumen Fengning, Hebei Mo 227.1 ± 2.7 U-Pb Zircon Shen et al., 201114 Dacaoping Fengning, Hebei 220.10 ± 117

~232.17 ± 115U–Pb Zircon Duan et al., 2007;

Hu et al., 201015 Yangshugou Fengning, Hebei 220.10 ± 117

~232.17 ± 115U–Pb Zircon Duan.,2007

Hu et al., 201016 Dasuji Zhuozi, Inner Mongolia 222.5 ± 3.2 Re–Os Molybdenite Zhang et al., 2009;

Nie et al., 2012Li.,2012

17 Caosiyao Xinghe, Inner Mongolia 131–134 U–Pb Graniteporphyry

Zhang et al., 2009;Nie et al.,2012;Li.,2012

18 Xishadegai Wulateqianqi,Inner Mongolia

225.4 ± 2.6 LA-ICP-MS Zircon Zhang et al., 2011

19 Jiajiaying Zhangjiakou, Hebei20 Baiyunebo Baotou, Neimenggu Fe 439 Re–Os Pyrite Zhang et al., 200821 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., 199623 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., 200324 Bajiazi Fuxin, Hebei Province 204.0 ± 0.5 40Ar–39Ar Sericite Luo et al., 200225 Baiyun Fengcheng, Hebei 209 ± 2

197 ± 2

40Ar–39Ar Quartz Liu et al., 2000

26 Erdaogou Chaoyang, Liaoning 140.6 ± 2.8 40Ar–40Ar Sericite Pang et al., 199727 Xiaotongjiapuzi Liaoning 167.0 ± 2 40Ar–39Ar Sericite Liu et al., 2002

167.0 ± 4 40Ar–39Ar Sericite Liu et al., 200228 Wulong Dandong, Liaoning 120 ± 3

112 ± 1Rb–Sr Quartz Wei et al., 2001

29 Paishanlou Fuxin, Liaoning 124.2 ± 0.4 40Ar–39Ar Biotite Yu et al., 200230 Siping Siping, Liaoning 187 ± 4 Rb–Sr Quartz Liang et al., 200131 Guanmenshan Kaiyuan, Liaoning Pb–Zn 467 Pb–Pb Fang et al., 199132 Yangjiazhangzi Jianchang, Liaoning 155–170 Pb–Pb Chen et al., 2003;

Dai et al., 200533 Bajiazi Jianchang, Liaoning 177.4–183.8 Pb–Pb model

ageChen et al., 2003;Dai et al., 2005

34 Beichagoumen Longhua, Hebei 138.5 ± 1.3 U–Pb Zircon Mao et al., 200535 Qingyanggou Chicheng, Hebei Yanshanian36 Jiaodingshan Chengde, Hebei Yanshanian37 Xiaodonggou Keshiketengqi,

Inner MongoliaMo 135.5 ± 1.5 Re–Os Molybdenite Nie et al., 2007

38 Kulitu Chifeng, Inner Mongolia 210–230 Sr–Nd–Pb monzogranite Wu et al., 200839 Chehugou Chifeng, Inner Mongolia 257.5 ± 2.5 Re–Os Molybdenite Zhang etal.,200940 Jiguanshan Chifeng, Inner Mongolia 242.9 ± 2–256.9 ± 6.9 U–Pb Zircon Zhang etal.,200941 Nianzigou Chifeng, Inner Mongolia 154.3 ± 3.6 Re–Os Molybdenite Zhang etal.,200942 Hadamengou Chifeng, Inner Mongolia 239.76 ± 3.04 40Ar–39Ar sericite Nie et al., 200543 Xiaojiayingzi Kazuo, Liaoning 177 ± 5 40Ar–39Ar sericite Nie et al., 200544 Lanjiagou Liaoning 186.5 Re–Os Molybdenite Huang et al., 199645 Gangtun Huludao, Liaoning46 Yangjiazhangzi West of Liaoning 190 ± 6 ~ 191 ± 6 Re–Os Molybdenite Huang et al., 199647 Beisongshumao West of Liaoning 162 Molybdenite Liu et al., 200948 Dazhuangke Yanqing, Beijing 146 ± 11 Re–Os Molybdenite Huang et al., 199649 Xiaosigou Cu, Mo Pingquan, Hebei 134 ± 3 Re–Os Molybdenite Huang et al., 199650 Shouwangfen Cu,

MoChengde, Hebei 148 ± 4 Re–Os Molybdenite Huang et al., 1996

(continued on next page)


Table 1 (continued)


51 Huashi Chengde, Hebei52 Huanggang Keerketengqi, Inner Mongolia Fe 135.31 ± 0.85 Re–Os Molybdenite Mao,201153 Zhoutaizi Luanping, Hebei 2460 U–Pb Zircon Xiang,201054 Damiaoheishan Chengde, Hebei 396 40Ar–39Ar Biotite Zhou et al., 201255 Xiaojiayingzi Kazuo, Liaoning 165.5 ± 4.6 Re–Os Molybdenite Dai et al., 200756 Zabuqi Ximen, Neimenggu 337 ± 1.5 U–Pb Zircon Deng,201257 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., 200359 Jiaojia Laizhou, Shandong 120.5 ± 0.6

120.1 ± 0.2120.2 ± 0.2

40Ar–39Ar Sericite Li et al., 2003

60 Wangershan Laizhou, Shandong 120.6 ± 0.7 40Ar–39Ar Sericite Mao et al.,200561 Xincheng Laizhou, Shandong 120.2 ± 0.3

120.9 ± 0.3

40Ar–39Ar Sericite Mao et al.,2005

62 Linglong Zhaoyuan, Shandong 122 ± 11123 ± 3123 ± 4

Rb–Sr Pyrite Yang andZhou,2001

63 Denggezhuang Yantai, Shandong 117.5 40Ar–39Ar Quartz Zhao et al., 199364 Dongji Shandong 116.1 ± 0.3

115.2 ± 0.2

40Ar–39Ar K-feldsparQuartz

Li et al., 2003

65 Pengjiakuang Rushan, Shandong 118.4 ± 0.3120.5 ± 0.5117.5 ± 0.3

40Ar–39Ar QuartzQuartzBiotite

Zhang et al., 2002

66 Dazhuangzi Longkou, Shandong 117.4 ± 0.6 40Ar–39Ar Quartz Zhang et al., 200267 Rushan Rushan, Shandong 118.6 ± 0.6 Rb–Sr Phyllic Zhang et al., 199568 Wangjiazhuang Fushan, Shandong Pb–Zn 128–130 K–Ar Zhang et al., 2008

Luxi 69 Xiaoyao Yishui, Shandong Au 116 ± 20 LA-ICP-MS,U–Pb

Zircon Li et al.,2009

70 Guilaizhuang Pingyi, Shandong 188 ~ 178 40Ar–40Ar Hornblende Tan et al., 199371 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 modelage

sulfide Lv et al., 2004

73 Zhangjiabaozi Fengcheng, Liaoning 1640–1764 Pb–Pb modelage

sulfide Qu et al., 1989

74 Lvjiabaozi Fengcheng, Liaoning Yanshanian Dai et al., 200575 Dongsheng Xiuyan, Liaoning Yanshanian Dai et al., 2005

S. margin Xiaoqinling 76 Xiaoqinling Henan Province Au 128.5 ± 0.2126.7 ± 0.2

40Ar–39Ar Biotite Wang et al., 2002

128.3 ± 0.3126.9 ± 0.3

40Ar–39Ar Biotite Wang et al.,2002

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., 200479 Shuidongling Nanzhao, Henan 440–646 Pb age pattern ore Wei et al., 200380 Banchang Neixiang, Henan 148.1 ± 1.6 39Ar–40Ar K-feldspar Li et al., 200881 Dahu Au, Mo Lingbao, Henan Mo 223 ± 2.8–232.9 ± 2.7 Re–Os Molybdenite Huang.200982 Quanjiayu Lingbao, Henan 129.1 ± 1.6,

130.8 ± 1.5Re–Os Molybdenite Li,2007

83 Majiawa Henan 232.5 ~ 268.4 Re–Os Molybdenite Wang et al., 201084 Yechangping Sanmenxia, Henan85 Jinduicheng Huaxian, Shanxi 129 ± 7, 131 ± 4,

139 ± 3Re–Os Molybdenite Huang,1994

Xiong'ershan 86 Qiyugou Songxian, Henan Au 122 ± 0.4115 ± 2

40Ar–39Ar K-feldspar Wang et al., 2001

125 ± 3114 ± 4

40Ar–39Ar K-feldspar Wang et al., 2001

134.1 ± 2.3 LA-ICP-MS,U–Pb

Zircon Yao et al., 2009

135.6 ± 5.6 Re–Os Molybdenite Yao et al., 200987 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., 201288 Xiasongping Songxian, Henan 129 ± 45 Rb–Sr Pyrite Pang et al., 201189 Shangzhuangping Songxian, Henan Pb–Zn 508–574 Pb age pattern Ore Chen et al., 200590 Nannihu Luanchuan, Henan 141.5 ± 7.8 Re–Os Molybdenite Ye et al., 200691 Chitudian Luanchuan, Henan Pt3 Yan et al., 2002;

Dai et al., 200592 Lengshuibeigou Luanchuan, Henan 136.13 ± 0.44 39Ar–40Ar

isochronQuartz

93 Huanglongpu Luonan, Henan Mo 221 Re–Os Molybdenite Huang,199494 Sandaozhuang Mo,

WuLuoyang, Henan 144.5 ± 2.2,

145.0 ± 2.2,145.4 ± 2.0

Re–Os Molybdenite Mao et al., 2005

95 Nannihu Luoyang, Henan 141.8 ± 2.1 Re–Os Molybdenite Mao et al., 200596 Shangfanggou Luoyang, Henan 143.8 ± 2.1,

145.8 ± 2.1Re–Os Molybdenite Mao et al., 2005


able 1 (continued)


T

97 Leimengou Songxian, Henan 131.6 ± 2.0,131.1 ± 1.9

Re–Os Molybdenite Mao et al., 2005

98 Huangshui'an Songxian, Henan 209.5 ± 4.2 Re–Os Molybdenite Huang.,200999 Qiushuwan Nanyang, Henan

Interior Taihangshan 100 Nanzhaozhuang Laiyuan, Hebei Pb–Zn Yanshanian Dai et al., 2005101 Lianbaling Laiyuan, Hebei Yanshanian102 Nanzhaozhuang Laiyuan, Hebei Yanshanian Dai et al., 2005103 Yintonggou Lingshou, Hebei Mo104 Dawan Cu, Mo Laiyuan, Hebei 144 ± 7 Re–Os Molybdenite Huang et al. 1996105 Futuyu Laiyuan, Hebei106 Mujicun Laiyuan, Hebei

Hengshan 107 Puziwan Wutai, Shanxi Au 142.9 ± 0.5142.5 ± 0.5

40Ar–39Ar Quartz Luo et al., 1999

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 Molybdenite111 Diangou Wutai, Shanxi 2456 ± 14 40Ar–39Ar

2416 ± 64 40Ar–39Ar112 Xiaobanyu Daixian, Shanxi 2333 ± 10 40Ar–39Ar

2317 ± 63 40Ar–39ArDabieshan 113 Yindongling Tongbo, Henan Pb–Zn Pz2 Yan et al., 2004


monzogranitic porphyry and granodioritic porphyry, dated at279.9 ± 4.2 Ma by zircon LA-ICP-MS U–Pb method (Qing et al.,2012), are genetically related with the gold mineralization. Anintegrated porphyry metallogenic system consisting of porphyry,cryptoexplosive breccia, fracture altered and quartz vein type goldorebodies are recognized with the porphyry type as the dominant

Fig. 5. Regional geology and ore deposit distribution in the Wutaishan r

one (Qing et al., 2012). The alteration system associated with this de-posit is remarkably similar to the classic porphyry deposits. Potassicand silicic alteration zone is developed at the contact zone betweenthe porphyry and the volcano-sedimentary rocks, especially in thelower part of the inner contact zone, with K-feldspar, quartz, magne-tite, rutile, barite and anhydrite as its mineralogical assemblage. A

egion (a) and the geology of the Dongyaozhuang gold deposit (b).

image of Fig.�5

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 toore-controlling fault in the Jiaojia gold deposit (d) (modified after Li et al., 2007).

388S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

image of Fig.�6


quartz–sericite zone is mainly developed at the inner and outer con-tact zones of the porphyry and the volcanic–sedimentary rocks andpartially overprints the potassic and silica alteration zone, withquartz, sericite, calcite, and pyrite as its typical mineralogical assem-blage. The propylitic zone is broadly distributed in the volcanicrocks with quartz, calcite, chlorite, epidote and pyrite as its main min-erals. Kaolinite alteration locally overprints the potassic and silicazone and the quartz–sericite zone. The low-S, low-Mo, low-Cu andhigh-Au disseminated-veinlet orebodies are found mainly in theneighboring area of the contact zone. The lentiform orebody 1 inthe ore belt II holds 90% of the gold resource with grades averaging2.73 g/t and bears a bonanza with ca. 10 t of gold reserve with agold grade >15 g/t (Qing et al., 2012). The orebodies are dominatedby altered granodioritic porphyry ore, altered tuff and tuffaceoussandstone ore, and altered andesite orewith veinlet-disseminatedmin-eralization style. The timing of the mineralization was constrained bymolybdenite Re–Os method to be 272.7 ± 1.6 Ma (Qing et al., 2012).

3.3.1.3. The Cretaceous Linglong type. The Linglong-type quartz veingold deposits are developed in the eastern and southern margins aswell as the interior of theNCC. In the easternmargin of theNCC, the rep-resentatives are the Linglong, Jinqingding and Denggezhuang depositsin the Jiaodong region (Fig. 6a, b, c). In the southern margin of theNCC, the representatives are those in the Xiaoqingling region (Fig. 7a).In the interior of the NCC, Shihu and Yixingzhai deposits in the TaihangMountains also belong to this type. All these deposits occur in regionswith a Precambrian basement and Cretaceous intermediate-felsicintrusions. Their host rocks are Precambrian TTG rocks like those inthe Taihang Mountains (Li et al., 2012, 2013), Precambrian metamor-phic supracrustal rocks like those in the Xiaoqinling region (Luanet al., 1991), or the Cretaceous granitoids like those in the Jiaodong re-gion (Chen et al., 1989, 1993, 2012; Li et al., 1996). The orebodiesare prominantly controlled by vertical to sub-vertical faults with dipangles greater than 65° and show multiple structural features fromtranspression to transtension. Alteration zoning is recognized with azone of broad K-feldspar (30–50 m) at the margins, followed towardsthe auriferous quartz vein by narrow quartz–sericite–pyrite (QSP)zone (b2 m) (Chen et al., 1989, 2012; Li et al., 1996, 2012, 2013; Luanet al., 1991). The hydrothermal mineralization phase can be dividedinto four main stages: pyrite–quartz, quartz–pyrite, poly-metallic sul-fide and quartz–carbonate. The orebodies are dominated by ores ofbanded and massive structures with gold grade ranging from 3 to20 g/t with an average of about 6–9 g/t. The ore minerals are mainlypyrite, chalcopyrite, galena, sphalerite, native gold, native silver, andvarious telluride minerals.

3.3.1.4. The Cretaceous Jiaojia type. The Jiaojia fracture-filling and al-tered type gold deposits are mostly developed in the north-westernJiaodong region in the eastern margin of the NCC (Fig. 6d). Thesetypes of gold deposits are also found in the Xiaoqingling region andthe Luoning–Songxian region in the southern margin of the NCC. Theirgeological setting is more or less the same as that of the Linglongtype. The orebodies generally exhibit low dip angles (b45°). BroadK-feldspar zone (10–50 m) in the margins followed towards the mainfault by broad quartz–sericite–pyrite (QSP) zone (2–40 m) (Chenet al., 1989). The ore is characterized by highly pyrite–microquartz–sericitized rocks superposed with pyrite–quartz, quartz–pyrite andpolymetallic sulfide veinlets. The ore minerals are similar with thoseof the Linglong type gold deposits.

3.3.1.5. The Cretaceous Qiyugou type. The Qiyugou cryptoexplosivebreccia gold deposits are developed in the Xiong'ershan region, south-ern margin of the NCC, the Wutai–Hengshan region, central NCC andthe Luxi region, eastern margin of the NCC. The deposits in these areasoccurwithin Precambrian basement or volcanics, or Paleozoic sedimentrocks. In the Xiong'ershan area, three clusters of auriferous explosive

breccias are present with large gold reserve in the Archean TaihuaGroup of gneiss and the Proterozoic Xiong'er Group of meta-andesitein the southeast of the Cretaceous Huashan monzogranitic pluton.Among these, more than 15 breccia pipes were found in the north-westerly extending Qiyugou valley, eight of which are auriferous(Fig. 7b). The lentiform, tube-like or irregular orebodies are con-trolled by cryptoexplosive breccia pipes or belts (Fig. 7c). Withinand surrounding the breccia pipes, the alteration zones are repre-sented by: adularia–biotite–quartz in the core of the ore zone, andsilica–chlorite at the margins of the pipe, followed by chlorite–epi-dote–actinolite–albite–calcite in the andesitic wall rocks. Theore-forming processes can be divided into an early oxide mineral stagerepresented by quartz, and an iron sulfide stage represented by pyrite,a middle polymetallic sulfide stage represented by chalcopyrite, galenaand sphalerite, and a late carbonate stage represented by calcite (Chenet al., 2009b; Li and Shao, 1991; Shao et al., 1992).

3.3.2. Molybdenum ore systemsPorphyry and skarn types are the two most important molybde-

num deposit types in the NCC, especially in the northern and south-ern margins of the NCC. In the north-western and northern HebeiProvince within the central section of the northern margin of theNCC, the Cretaceous Jiajiaying deposit and the Triassic Shadaigoumendeposit are well known large-scale porphyry molybdenum deposits.The Cretaceous Dazhuangke deposit in Yanqing County, Beijing mu-nicipality, is a large scale cryptoexplosive type molybdenum depositin the central section of the northern margin of the NCC. In thesouth-western Liaoning Province within the north-eastern marginof the NCC, are the Jurassic Lianjiagou and Gangtun porphyry molyb-denum deposits. In the southern margin of the NCC, are the Nannihularge scale skarn-porphyry molybdenum deposits. Quartz vein or car-bonate vein type molybdenum deposits were also found in theLuoning–Songxian area of the southern margin of the NCC but withsmall scale resources (Rui et al., 1994).

3.3.2.1. The Triassic Sadaigoumen type. The Sadaigoumen molybdenumdeposit is located in the north of Fengning county, Hebei Province (Luoet al., 2010). It is one of the large scale molybdenum deposits in theYan–Liao Mo (Cu) metallogenic zone along the northern margin ofthe NCC. The deposit is closely associated with the Triassic reddishmonzogranite which occur within the Mesozoic grayish monzograniteand the Archean TTG gneiss. The outcrop of the reddish monzograniteoccupies an area of about 0.9 km2. Geochemical studies revealedthat the monzogranite is metaluminous high-K calc-alkaline I-type,LREE-enriched with weak Eu negative anomalies (δEu = 0.78). Themonzogranite is depleted with Nb, Ta, P, Zr, and Ti and enriched withRb, Th, K, and Ba. The formation pressure of themonzogranite was esti-mated to be 1.83 kbar, implying an emplacement depth of 6.78 km(Luoet al., 2010). Typical hydrothermal alteration zones of porphyry typeoccur with a potassic zone in the core, followed outward by quartz–sericite–pyrite and propylitic alteration zone. The Mo orebody extendsfor 700 m N–S and 960 m E–W, with vertical extension of 275 m andshowing averageMo grade of 0.059% (Shen, 2011). The ore is character-ized by veinlets of molybdenite, pyrite and chalcopyrite. The minerali-zation process can be divided into an early barren magnetite–quartzstage, a pyrite–molybdenite–quartz stage and a late barren fluorite–quartz–calcite stage. Re–Os isotopic dating of the molybdenite yieldedan age of 237 ± 4.1 Ma for the mineralization (Shen, 2011).

3.3.2.2. The Jurassic Lanjiagou type. The Lanjiagou porphyry typemolyb-denumdeposits are located in the southwest of Liaoning Province at thenorth-eastern margin of the NCC, and are closely associated withYanshanian (189 Ma, Dai et al., 2008) magmatic rocks which intrudedinto the Mesoproterozoic dolomitic limestone and the Early Paleozoiclimestone and shale. The intrusive rocks consist of, according to theirorder of formation, coarse grained granite (SiO2 71.89%, Na2O/K2O


image of Fig.�7


0.96, DI 88.5, δEu 0.44, Mo 12.43 ppm), fine grained porphyritic granite(SiO2 76.09%, Na2O/K2O 0.82, DI 89.3, δEu 0.25,Mo 27.13 ppm) and gra-nitic porphyry (SiO2 76.73%, Na2O/K2O 0.39, DI 94.6, δEu 0.11, Mo56.67 ppm) (Rui et al., 1994). The thick tabular orebodies occur at thetop and periphery of the fine grained porphyritic granite and are con-trolled by fractures and faults in the intrusive rocks. Ores of quartz veintype, quartz veinlet type, and fracture altered type are commonwithmo-lybdenite and pyrite as the major ore minerals and sphalerite, chalcopy-rite, galena, tetrahedrite, magnetite, argentite and native silver as theminor minerals. The gangue minerals are mainly K-feldspar, plagioclase,quartz, illite and calcite with minor rhodochrosite, siderite, chlorite andfluorite. K-feldspathization, greisenization (quartz–white mica), silicifi-cation, illitization and Fe–Mn carbonitization and chloritization are com-monly close to the orebodies. The mineralization period can be dividedinto an early alteration sub-period, when K-feldspatic and greisenoccurred, and a late sulfide sub-period, with three mineralizationstages: the early stage characterized by quartz (326 °C) + molybdenite(317 °C) association; the middle stage characterized by quartz(295 °C) + molybdenite (295 °C) + pyrite (265 °C) + galena associa-tion; and the late stage characterized by quartz (235 °C) + molybdenite(212 °C) + illite association (Dai et al., 2007; Rui et al., 1994).

3.3.2.3. The Cretaceous Dazhuangke type. This deposit type includes theDazhuangke and Dongjiagou explosive breccia type molybdenum de-posits located at the junction of the E–W Yangyuan–Xifengkou–Jinzhoudeep seated fault and the NNE–SSW Zhenglanqi–Fengning–Jurongguandeep seated fault at the northern margin of the NCC. Except for a fewoutcrops of the Mesoproterozoic carbonate rocks in the neighboringarea, the deposits areas are mainly occupied by Late-Jurassic to EarlyCretaceous intrusive and extrusive intermediate-felsic rocks. A fewcryptoexplosive breccias of about 1200–1700 m length, 200–700 mwidth and >600 m vertical extension intruded into the quartz–monzonitic porphyry and dioritic porphyrite. The brecciated and hydro-thermally altered quartz–monzonite porphyrywas dated of 147 Ma, andthe unaltered porphyritic monzogranite was dated of 139 Ma (K–Ar, Ruiet al., 1994). The orebodies are tube-like or stratiform and occur withinthe explosive breccias. Molybdenite is the main ore mineral accompa-nied with rare magnetite, chalcopyrite, sphalerite, pyrite, ilmenite, andscheelite. The 2H1molybdenite occurs as disseminations,fine stockwork,and as cementingmaterial of the breccias with rhenium ranging from 13to 18.6 ppm. Re–Os isochron dating of the ore constrained the timing ofmineralization at 137.6 ± 3.7 Ma (Liu et al., 2012). The ganguemineralsconsist mainly of the rock-forming minerals of the breccias and the hy-drothermal minerals with plagioclase, K-feldspar, quartz, biotite andhornblende as the major ones and zeolite, epidote, apatite, zoisite, fluo-rite and sericite occurring in subordinate amounts. A zone of potassicand silica alteration is developed within or nearby the molybdenumorebodies, bordered by a quartz–sericite–pyrite zone, and propylitizationin the outermost zone. The ore forming process can be divided into threestages:molybdenite–magnetite–pyrrhotite–scheelite–K-feldspar–biotite(460–380 °C); molybdenite–quartz–K-feldspar–biotite (350–280 °C);and quartz–pyrite–carbonate–zeolite–molybdenite (250–150 °C). Thesalinities of the fluid inclusions are >20% NaCl equiv. and peak at 62%NaCl equiv. Daughter minerals in the polyphase fluid inclusions are ha-lite, sylvite and molybdenite (Ma et al., 2008; Rui et al., 1994).

3.3.2.4. The Cretaceous Nannihu type. The Nannihu skarn–porphyrytype Mo (W) is a super-large Mo (W) ore field located in theLuanchuan county, Henan Province at the southern margin of theNCC. This ore field includes the Nannihu porphyry type Mo (W),Sandaozhuang skarn type Mo (W), Shangfanggou porphyry type Mo(Fe) and Majuan, Shibaogou, Yuku, and Huangbeiling skarn or

Fig. 7. Regional geology and ore deposit distribution in the Xiaoqinling–Xiong'ershan regionprofile 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).

porphyry type Mo deposits. The proven metal reserves exceed 2 Mtof Mo, 0.64 Mt of W, and 111 t of Re. The metal grades range from0.06‰ to 0.24‰ for Mo and from 0.09‰ to 0.13‰ for W (Li et al.,2003). The deposits are closely associated with Yanshanian (Late Cre-taceous) granitic stocks intruding the Neoproterozoic metamor-phosed marine clastic and carbonate rocks of the Luanchuan Group.NNW to NW directed fractures are the major ore-controlling struc-tures. The intrusive rocks evolved from granodiorite, monzograniteto granitic porphyry accompanied by mineralization, with Mo andW abundances several hundred times more than those of the averagecrustal values. The intrusive rocks are of high-K, alkaline-rich andhighly acidic nature. The orebodies occur mostly in the contact zoneof the intrusive rocks and in the strata-controlled skarn. Besideshornfelsization and skarnification in the contact zone and the weakstrata of the carbonate rocks, broadly superposed typical porphyrytype alterations are strongly developed in the intrusive rocks. The oretypes are dominated by skarn (>50%), hornfels (~40%) and graniticporphyry (~10%) (Li et al., 2003). Themetallogenic process is character-ized by an early anhydrous skarn stage, hydrous skarn–magnetite–scheelite–molybdenite stage, middle quartz–molybdenite–pyrite–chalcopyrite–sphalerite stage, and late quartz–calcite–fluorite stage.Molybdenite Re–Os isotopes yielded model ages of ~142 Ma for theNannihu Mo deposit, ~145 Ma for the Sandaozhuang Mo deposit and~145 Ma for the Shangfanggou Mo deposit. A Re–Os isochron age of142 Ma was obtained from 6 samples in the three deposits (Li et al.,2003).

3.3.3. Chaijiaying lead–zinc ore systemsThe Chaijiaying stringer lode type lead–zinc deposit surrounded by

gold and molybdenum deposits in the well known Zhang–Xuan region(Fig. 8a), is located to the north of a NEE directed fault of about 100 kmlength at the central-northern margin of the NCC. The orebodies arecontrolled by a series of fractures directed NWW, NNE and SWW. Theore-hosting rocks are mainly Paleoproterozoic leptite, granulite andgneiss (Fig. 8b). Part of the host rocks includes Late Jurassic volcanic–sedimentary rocks. Small scale Yanshanian granitic porphyry andquartz porphyry (134 Ma, K–Ar, Rui et al., 1994) dikes and stocks areexposed in the mining area. Two types of ores, early chlorite–sphaleriteand late sericite–polymetallic, are recognized. The chlorite–sphaleritetype of ore is clustered and densely disseminated, and partially in vein-lets, with numerous sphalerite, ferruginous sphalerite and aminor arse-nopyrite and marcasite as well as galena, pyrrhotite and hematite. Thesericite–polymetallic type of ore occurs as clustered, disseminated orin veinlets with galena, sphalerite and pyrite. The lead grade of thechlorite–sphalerite type of ore ranges from 0.01% to 0.2%with Pb/Zn ra-tios ranging from 1/18 to 1/100, whereas the lead grade of the sericite–polymetallic type of ore ranges from 0.3% to 4% with Pb/Zn ratios from1/0.5 to 1/4. Apart from lead and zinc, silver of 10 to 100 g/t and gold of0.02 to 1 g/t are also estimated. The hydrothermal alteration is character-ized by a sericitic zone at the center of the orebody, followed with pene-trative sericitic and chloritic alteration zones outwards. The decrepitationtemperature of fluid inclusions in the metal minerals shows a range of200 to 350 °C (Hu et al., 2005; Rui et al., 1994; Wang et al., 2003).

3.4. Mantle contribution

3.4.1. Northern margin of the NCC

3.4.1.1. Northwest of Hebei Province. The Zhang–Xuan (Zhangjiakou–Xuanhua) region, northwest of the Hebei Province, is host to a wellknown ore district with more than 100 deposits and occurrences ofgold, molybdenum and lead–zinc (Wang et al. 2010). The Dongping,

(a), geology of the Qiyugou gold deposit (b) and the vertical alteration–mineralization

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-portant gold resources in this area. The Chaijiaying lead–zinc–silver,the Xiangguang manganese–silver and the Jiajiaying molybdenumrepresent large scale polymetallic deposits. Most of the gold depositsoccur within Archean metamorphic rocks and the Variscan alkalinecomplex, whereas most of the polymetallic deposits are found inthe Proterozoic cover sequences and the Mesozoic basin.

The δ34S values for the sulfide minerals from the Jurassic gold de-posits range from −24 ‰ to +5‰ with most of the values clusteringbetween −16‰ and −6‰ (Table 2; Fig. 9). Gold deposits of EarlyCretaceous age show δ34S values ranging from −16‰ to +6‰ withmost values clustering between −13‰ and −4‰ (Wang et al.,2010). The δ34S measurement of 49 sulfide mineral separates fromthe Chaijiaying lead–zinc deposit yield values ranging from 2.2 to7.8‰, with an average of 5.2‰. Most of the sulfides from the silverand molybdenum deposits show δ34S values ranging from −4‰ to+8‰. The general trend in variation of the δ34S values for the sulfideminerals is as follows: δ34S py > δ34S cpy > δ34S sph > δ34S gn(Wang et al., 2010), suggesting equilibrium sulfur isotopic fraction-ation during the ore forming process. The average δ34S value of thesulfide minerals is consistent with the total δ34S value of theore-forming fluid. In hydrothermal systems at 250 °C, for an increasein logarithm unit of fO2 or a unit of pH value, the δ34S value of sulfide

mineral would decrease by 20% (Ohmoto, 1972). Thus, the 32S-richcharacteristics of the sulfide minerals in the northwest of the HebeiProvince was interpreted to be the result of alkali metasomatism(Wang et al., 1992; Wang et al., 2010). Apart from the alkali metaso-matism and K-feldspathization of the wallrocks of some of the golddeposits (the Hougou, Zhongshangou, Huangtuliang, Xiping, Beigou,Taogou, Zhaojiagou, Yujiazhuang, Xiashuangtai and Xialiangjiafanggold deposits, represented by the Dongping gold deposit) in thisarea, the gold mineralization itself is considered to be genetically re-lated to the syenite. The quartz vein type and fracture-altered typegold deposits in the Jiaodong peninsula, are developed with strongK-feldspathization, but the δ34S values of the sulfide minerals fromthe Jiaodong gold deposits range mainly from 5‰ to 10‰ which arepredominantly rich in 34S. This implies that the δ34S values of the sul-fide minerals from the northwest of the Hebei Province mainly reflectthe source characteristics which are not in favor of mantle origin. Al-though there is no marked difference in the sulfur isotopes betweenthe Jurassic and the Early Cretaceous gold deposits, the δ34S valuesshow a slight increase, suggesting that deeper sources might havebeen involved in the gold mineralization during Cretaceous. The sul-fur isotope compositions of the sulfide minerals from the Mesozoicgold and polymetallic deposits in the northwest Hebei Province arecomparable with those from the Wulashan gold field in the western

image of Fig.�8

Table 2Sulfur isotopic compositions of the ore deposits in the NCC.

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

δ34S Range

N. margin W portion 1 Jiawula Au Bayannur,Inner Mongolia

2.6 −2.9–4.0 Guan et al., 2004

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., 19984 Donghuofang Au Hohhot, Inner Mongolia 3.1 2.6–3.7 Xu et al., 1998;

Xu et al., 19915 Bayinhanggai Au Hohhot, Inner Mongolia −6.1 −8.3 to −0.5 Chen et al., 20016 Dayingzi Au Zhangbei, Hebei −0.5 The third geological team of Heibei

Province (1998), Wang etal, 1992;Jin and Dui,1991; Song et al., 1994;Peng et al., 1992; Wang et al., 2010;Bao et al., 1996;Yu et al., 1989

7 Jinjiazhuang Au Zhangjiakou, Hebei 181.9 Fracture-altered 1.9 –1.4–5.08 Dongping Au Zhangjiakou, Hebei 187 ± 0.3, 188 ± 0.4,

177.4 ± 5, 140.2 ± 1.3Fracture-altered −8.1 −5.5 to −13.5

9 Shuijingtun Au Chongli, Hebei −10.410 Zhongshangou Au Chongli, Hebei 155.47, 115.1 −16.1 −23.8 to −11.111 Huangtuliang Au Chicheng, Hebei 120.63 Fracture-altered −5.0 −1.6 to −7.412 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., 20102 Wunuketushan Au Hulun Buir, Inner Mongolia 2.8 −0.2–4.2 Guan et al., 20043 Badaguan Au Hulun Buir, Inner Mongolia 2.6 0.5–4.8 Guan et al., 20044 Huashi Au Chengde, Hebei 3.7 3.0–4.3 Wang et al., 2010; Niu et al., 20015 Dongzigou Au Chengde, Hebei 1.3 −0.5–4.9 Wang et al., 2010; Yang et al., 1996;

You Se Pu Cha Da Dui,19966 Xiajinbao Au Pingquan, Hebei 2.8 0.4–7.4 Shao et al., 1987;Luan et al., 19967 Tianjiacun Au Tangshan, Hebei 1.9 Wang et al., 20108 Malanguan Au Tangshan, Hebei 3.3 1.1–6.7 Song et al., 19949 Jinchangyu Au Qianxi, Hebei 2661, 2391, 2190 ± 58 Quartz vein −1.8 −6.3–3.1 Lin et al., 1985; Yu, 1989; Zhang, 199610 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., 201013 Shapoyu Au Kuancheng, Hebei 2.6 Wang et al., 201014 Baimiaozi Au Kuancheng, Hebei 3.3 Wang et al., 201015 Sajingou Au Kuancheng, Hebei 1.9 Wang et al., 201016 Maoshan Au Zunhua, Hebei 6.4 5.2–8.3 Bai et al., 1990; Shao et al., 1987;

Luan et al., 199617 Niuxinshan Au Qinhuangdao, Hebei 5.5 4.3–6.3 Xu et al., 1987; Song et al., 199418 Maojiadian Au Lingyuan, Liaoning −6.2 Wang et al., 201019 Wangjiadagou Au Qingyuan, Liaoning 3.6 2.1–6.1 Yu et al., 200520 Hongshi Au Yixian, Liaoning 0.6 −32.7–17.4 Yin et al., 199421 Erdaogou Au Beipiao, Liaoning 0.8 −2.2–5.1 Xu et al., 2007; Liu et al., 200222 Jinchanggouliang Au Beipiao, Liaoning −5.0–1.5 Li et al., 1990; Liu et al, 200223 Shuiquan Au Beipiao, Liaoning 0.3 −7.6–1.9 Wang et al., 200924 Dongwujiazi Au Chaoyang, Liaoning 1.9–3.1 Xu et al., 201025 Qinglonggou Au Huludao, Liaoning 7.7 Yao et al., 2004

E. margin Jiaodong 1 Jiaojia Au Jiaodong, Shandong 120.5 ± 0.6, 120.1 ± 0.2,120.2 ± 0.2

Fracture altered 10.3 7.8–11.8 Wang et al., 2001; Wang et al., 1991;Ding et al., 1998; Lin et al., 1999;Wen et al., 1990; Yao et al., 199015.7 7.9–11.8

2 Linglong Au Zhaoyuan, Shandong 122 ± 11, 123 ± 3, 123 ± 4 Quartz vein 5.8 2.9–8.2 Cui et al., 20126.9 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;Wen et al, 1990


393S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

Table 2 (continued)


δ34S Range

3 Pengjiakuang Au Jiaodong, Shandong 118.4 ± 0.3, 120.5 ± 0.5,117.5 ± 0.3

Strata-bound 11.2 9.7–11.5 Sun et al., 1995; Zhang et al., 1999;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., 20005 Dazhuangzi Au Longkou, Shandong 117.4 ± 0.6 Strata-bound 10.6 Zhang et al., 2002; Zhu et al., 19996 Dujiaya Au Jiaodong, Shandong Strata-bound 5.5 −14.0–15.1 Yan et al., 20127 Denggezhuang Au Jiaodong, Shandong 117.5 Quartz vein 9.7 8.0–10.8 Ying et al., 1994; Yang et al., 20008 Fayunkuang Au Yantai, Shandong Strata-bound 13.1 Zhang et al., 2001;9 Penglai–Qixia Au Yantai, Shandong 5.7 −14.2–9.9 Wang et al., 200210 Yigezhuang Au Zhaoyuan, Shandong Fracture-altered 7.1 5.9–8.9 Huang et al., 1994; Chen et al., 1989;

Deng et al., 200012 Majiayao Qixia, Shandong Quartz vein 4.9 1.4–8.6 Chen et al, 1989; Wang et al, 2002;

Li et al., 199013 Wang'ershan Au Laizhou, Shandong 120.6 ± 0.7 Quartz vein 7.8 6.7–10.0 Wang et al., 200214 Lingshangou Au Zhaoyuan, Shandong Quartz vein 7.4 Wang et al., 2002; Lin et al., 1999;

Yao et al, 199015 Liukou Au Qixia, Shandong Quartz vein 7.4 7.0–7.9 Chen et al., 198916 Bailidian Au Qixia, Shandong Quartz vein 5.9 Wang et al., 200217 Panzijian Au Qixia, Shandong Quartz vein 6.2 Wang et al., 2002; Yao et al., 199018 Fushan Au Zhaoyuan, Shandong Quartz vein 7.0 Wang et al., 2002; Lin et al., 1999;

Yao et al,199019 Jinchiling Au Zhaoyuan, Shandong Quartz vein 4.0 Wang et al., 2002; Yao et al., 199020 Taishang Au Zhaoyuan, Shandong Fracture-altered 8.0 Chen et al., 1989; Deng et al., 200021 Qibaoshan Au Wulian, Shandong 2.5 Qiu et al., 1996; Chen et al., 1992;

Wang et al., 199122 Hexi Au Penglai, Shandong Fracture-altered 8.2 7.4–8.8 Hou et al., 200423 Congjia Au Rushan, Shandong 0.3 −5.7–6.3 Wen et a,199024 Daliujia Au Qixia, Shandong −9.5 −9.7–9.3 Yao et al., 199025 Jiudian Au Pingdu, Shandong Quartz vein 7.6 4.9–9.3 Wang et al., 1982; Lin et al., 1990;

Qiu et al., 198826 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., 199027 Sanshandao Au Jiaodong, Shandong Fracture-altered 11.5 10.0–12.6 Wang et al., 200228 Cangshang Au Laizhou, Shandong 121.3 ± 0.2 Fracture-altered 10.8 9.6–12.0 Huang et al., 199429 Cangshang Au Laizhou, Shandong 11.6 Wang et al., 200230 Dongji Au Laizhou, Shandong 116.1 ± 0.3, 115.2 ± 0.2 Fracture-altered 11.3 Huang et al., 199431 Longbu Au Laizhou, Shandong 9.8 Wang et al., 200232 Matang Au Laizhou, Shandong Fracture-altered 9.4 5.6–10.7 Huang et al., 1994;

Wang et al., 200233 Hongbu Au Laizhou, Shandong Fracture-altered 8.9 4.8–10.9 Huang et al., 199434 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., 200236 Shangzhuang Au Zhaoyuan, Shandong Fracture-altered 9.9 9.1–10.537 Wangjiagou Au Yantai, Shandong Fracture-altered 9.238 Hedong Au Zhaoyuan, Shandong Fracture-altered 10.3 9.3–10.839 Fujia Au Zhaoyuan, Shandong Fracture-altered 10.140 Wasunjia Au Zhaoyuan, Shandong Fracture-altered 4.8 −0.2–6.8

394S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

41 Qiansunjia Au Zhaoyuan, Shandong Fracture-altered 5.342 Huangbuling Au Zhaoyuan, Shandong Fracture-altered 7.8 7.0–8.843 Beijie Au Zhaoyuan, Shandong Fracture-altered 9.1 7.6–9.744 Longhudou Au 6.845 Luanjiahe Au Zhaoyuan, Shandong 2.4 −1.3–6.046 Dongqujia Au 4.947 Caogoutou Au Zhaoyuan, Shandong Fracture-altered 6.348 Caojiawa Au Zhaoyuan, Shandong Fracture-altered 7.049 Jianli Au Pingdu, Shandong Fracture-altered 8.450 Chijia Au Yantai, Shandong 3.751 Tengjia Au Rongcheng, Shandong 5.852 Chengkuo Au 3.753 Nanshu Au Laixi, Shandong Fracture-altered 6.754 Xilin Au Qixia, Shandong 6.955 Lingnan (Taishang) Au Zhaoyuan, Shandong 8.0 Chen et al., 198956 Heilangou Au Penglai, Shandong Fracture-altered 6.7 5.8–7.8 Chen et al., 198957 Jinqingding Au Jiaodong, Shandong Quartz vein 8.6 6.8–9.7 Chen et al., 201058 Dayigezhuang Au Jiaodong, Shandong Fracture-altered 6.4 5.9–7.0 Wang et al., 201259 Canzhuang Au Jiaodong, Shandong Fracture-altered 6.8 5.3–7.6 Yan et al., 201260 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., 19962 Buwa Au Mengyin, Shandong Fracture-altered 2.1–4.1 Zang et al., 19983 Guilaizhuang Au Pingyi, Shandong 188–178 Explosive-breccia 2.4 2.0–3.0 Liu et al., 19944 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., 20122 Qiuling Au Zhen'an, Shaanxi 15.3 11.1–19.8 Shen et al., 19963 Xiong'ershan Au Shangluo, Shaanxi Quartz vein 2.4 −5.0–5.0 Lu et al., 2003; Chen et al., 19954 Dongtongyu Au Tongguan, Shaanxi Province 6.5 3.5–12.9 Lu et al., 20045 Xitongyu Au Tongguan, Shaanxi −7.7 −11.4 to −0.2 Lu et al., 20046 Chengjiagou Au Tongguan, Shaanxi −6.1 −9.3 to −2.4 Lu et al., 20047 Bayuan Au Lam Tin, Shaanxi Quartz vein 3.7 2.3–4.6 Lu et al., 20048 Tongyu Au Tongguan, Shaanxi Quartz vein 2.7 −8.7–5.7 Yu et al., 19899 Wenyu Au Lingbao, Henan Quartz vein 3.0 5.4–6.6 Xu et al., 199210 Dongchuang Au Lingbao, Henan 132.16 ± 2.64, 132.55 ± 2.65 Quartz vein 1.1 −2.8–5.8 Fan et al., 201211 Jindongcha Au Lingbao, Henan Quartz vein −0.9 −12.5–8.2 Lu et al., 200412 Yangzhaiyu Au Lingbao, Henan 113.72 ± 2.27, 114.26 ± 2.29 Quartz vein 2.4 −14.7–7.1 Lu et al., 200413 Lianggancha Au Lingbao, Henan Quartz vein 0.6 −7.6–5.5 Lu et al., 200414 Qiangmayu Au Lingbao, Henan Quartz vein 5.7 −0.7–9.2 Lu et al., 200415 Linghu Au Lingbao, Henan Quartz vein 1.8 −8.7–15.3 Lu et al., 200416 Dahu Au Lingbao, Henan Quartz vein −3.3 −8.1–1.3 Lu et al., 200417 Tonggou Au Lingbao, Henan Quartz vein −4.7 −28.5–3.6 Lu et al., 200418 Shenjiayao Au Shanxian, Henan Fracture-altered 3.6 0.4–5.9 Lu et al., 200419 Bankuan Au Yingxian, Henan Quartz vein 2.0 −12.1–8.5 Lu et al., 200420 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., 19992 Xiaonangou Au Songxian, Henan Fracture-altered −13.1 −16.6 to −9.5 Zhu et al., 19983 Qiyugou Au Songxian, Henan 122 ± 0.4, 115 ± 2, 125 ± 3,

114 ± 4, 134.1 ± 2.3, 135.6 ± 5.6Explosive-breccia −0.8 −3.5–1.7 Wang et al., 1996


395S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

Table 2 (continued)


δ34S Range

−0.4 −2.0–2.7 Shao et al., 19964 Pasigou Au Songxian, Henan 4.9–8.4 Xu et al., 20055 Xiaogongyu Au Songxian, Henan −1.0–2.1 Guo et al., 20086 Huanxiangwa Au Songxian, Henan −9.1 −16.8–0.6 Gao et al., 20107 Dianfang Au Songxian, Henan Explosive-breccia 4.8 −6.4–9.2 Lu et al., 20048 Yaogou Au Songxian, Henan Fracture-altered −4.3 −9.7–1.8 Lu et al., 20049 Beiling Au Songxian, Henan Fracture-altered −6.8 −10.2 to −0.6 Lu et al., 200410 Shagou–Yuelianggou Au Songxian, Henan 0.7 −8.1–6.1 Lu et al., 200411 Songpinggou Au Luoning, Henan Quartz vein 1.5 −9.4–9.8 Lu et al., 200412 Jinjiawan Au Luoning, Henan Fracture-altered −10.0 −10.9 to −9.1 Lu et al., 200413 Qinggangping Au Luoning, Henan −1.1 −8.7–4.2 Lu et al., 200414 Hugou Au Luoning, Henan −10.1 −28.2–7.9 Lu et al., 200415 Qiliping Au Luoning, Henan 9.4 8.5–10.7 Lu et al., 200416 Tieluping Au Luoning, Henan Fracture-altered −5.0 −8.8 to −1.4 Lu et al., 200417 Shanggong Au Luoning, Henan Fracture-altered −8.4 −19.2–6.7 Lu et al., 200418 Hongzhuang Au Luanchuan, Henan Quartz vein 4.0 −2.2–7.6 Lu et al., 200419 Kangshanxingxingyin Au Luanchuan, Henan 4.1 −7.4–7.3 Lu et al., 200420 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., 19992 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., 20092 Qiubudong Au Pingshan, Hebei 4.4 Wang et al., 20103 Xishimen Au Lingshou, Hebei 0.6 −0.3–1.4 Wang et al., 20104 Jiujizhuang Au North Taihangshan 2.3 1.7–5.0 Geng et al., 19975 Luanmuchang Au Yixian, Hebei 0.7 0.3–1.1 Chen et al., 19906 Konggezhuang Au Yixian, Hebei 6.1 4.3–7.2 Wang et al., 20107 Chounikou Au Lingshou, Hebei 1.6 Wang et al., 20108 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., 20012 Diantou Au Wutai, Shanxi 2456 ± 14, 2416 ± 64 4.2 3.9–4.6 Tian et al., 19913 Dongyaozhuang Au Wutai, Shanxi 1.0–2.4 Tian et al., 20004 2.7 1.0–5.7 Tian et al., 19985 Xiaobanyu Au Wutai, Shanxi 2333 ± 10, 2317 ± 63 −0.1 −0.2–0.1 Wang et al., 19966 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., 19923.2 −0.8–5.6 Tian et al., 19912.5 2.0–3.0 Zhang et al., 2009

7 Majiacha Au Fanshi, Shanxi 0.5 −8.1–2.4 Tian et al., 1991Hengshan 1 Gengzhuang Au Fanshi, Shanxi Explosive-breccia 2.5 0.2–3.7 Huang et al., 2004

0.5–3.6 Li et al., 19883.9 1.6–4.5 Li et al., 1994

2 Tainashui Au Lingqiu, Shanxi 0.2 Tian et al., 19913 Lugou Au Lingqiu, Shanxi Quartz vein −0.1 −4.2–2.7 Tian et al., 19914 Hulishan Au Yuanping, Shanxi 0.3 −3.7–5.6 Chang et al., 19985 Gaofan Au Daixian, Shanxi 1.5 −3.3–2.7 Tian et al., 1991

0.7 −5.4–3.5 Gao et al., 20046 Xishandi Au Yuanping, Shanxi 3.7 Yang et al., 20017 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., 20003.9 2.2–5.2 Long et al., 20110.0 −3.2–1.5 Zhang et al., 2001

2 Dongfengding Au Xiangfen, Shanxi 4.2 2.7–5.7 Yao et al., 20046.9 −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., 20102 Jinchangzi Au Zhongwei, Ningxia 3.8–6.7 Zhou et al., 1993; Zhong et al., 2012

396S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

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


Baotou area within the Inner Mongolia Autonomous Region along thenorth-western margin of the NCC, where the gold deposits yieldδ34S values ranging from −7.9‰ to −18.4‰ with an averageof −14.98‰ (Wei et al., 1993).

The lead isotopes of the Jurassic to Cretaceous gold, silver andlead–zinc deposits in the northwest of Hebei Province show a rela-tively large variation with 207Pb/204Pb ranging from 15.13 to 15.54.206Pb/204Pb and 208Pb/204Pb values show limited ranges of 16.31–17.64 and 36.22–37.72, respectively (Table 3; Fig. 10). Plotting ofthe data on the Zartman's diagrams suggests that lead of the oreswas derived from multiple sources including mantle and the loweras well as upper crust, although most of the data plot in the orogenicfield.

Source tracing with silicon isotope systematics has also beenattempted. Molini-Velsko et al. (1986) obtained the isotopic composi-tion of silicon in meteorites which shows a δ30Si range of −1.8‰ to0.3‰ with an average of −0.5‰. Ding and Jiang (1994) comparedthe silicon isotopic composition of the granites from China andNorth America, which show δ30Si values ranging from −0.4‰ to0.4‰, peaking at −0.1‰, and with an average of −0.12‰. Analysesof 23 siliceous sediment samples from the black chimney in theMariana trench yielded δ30Si values ranging from−0.4‰ to 3.1‰ av-eraging −1.6‰ (Wu, 1995). Analyses of 27 quartz, intrusive rocksand gneiss samples from the northwest of Hebei Province yieldedδ30Si values of −0.2‰ to 0.3‰ with an average −0.05‰ for theore-bearing quartz vein (Table 4; Wang et al., 2010; Lu and Wang,1992; Yin, 1995),−0.3‰ to 0.4‰with an average of 0.05‰ for the in-trusive rocks, and 0.6‰ for an Archean gneiss sample (Lu and Wang,1992). The δ30Si data of the quartz and intrusive rocks from the studyarea are consistent with those of the granitoids in China and else-where. The δ30Si data of the quartz from the study area are also with-in the δ30Si range of the meteorite, implying that at least part of thesilicon was derived from magmas sourced from the mantle. Sinceonly one analysis is available for the Archean gneiss, its contributionto the hydrothermal silicon cannot be excluded.

The mean values of the hydrogen and oxygen isotopes of fluidstrapped in the quartz from various ore deposits in the northwest of

Hebei Province show a relatively large range with δ18Osmow varyingfrom 4.9‰ to 18.77‰, δ18OH2O from −3.14‰ to 7.31‰, and δDsmow

from −109.5‰ to −80.5‰ (Table 5). The oxygen isotopic composi-tions of the fluid δ18OH2O were calculated from that of quartzδ18OSMOW with the equation 1000lnαQ–W = 3.38 × 106T−2 − 3.40(Clayton et al., 1972), where T represents the homogenisation tem-perature of fluid inclusions. It is noted that the δDSMOW values aremarkedly lower than that of the typical metamorphic water (−65‰to −20‰, Hugh and Taylor, 1974). In the δD versus δ18O diagramfor fluids from various ore deposits in the northwest of Hebei Prov-ince (Fig. 11), all the plots fall below the primary magmatic waterand shift slightly towards the region for meteoric water, suggestingthat magmatism played an important role in the mineralization(Hugh and Taylor, 1974).

The δ13CPDB data of the carbonate minerals from the ore deposits inthe northwest of Hebei Province range between −6.0‰ and −2.5‰(Table 5). The δ13CPDB value of mantle carbon is around −5‰ andthat of magmatic carbon is within the range of −9‰ to −3‰ (Taylorand Bucher-Nurminen, 1986). The carbon from sedimentary carbonaterocks or from the interaction between brine and argillite is character-ized by heavy carbon isotope with the δ13CPDB values in the range of−2‰ to +3‰; the δ13CPDB data of marine carbonate rocks are ca. 0‰(Veizer et al., 1980). Organic carbon is characterized by lighter carbonenrichment with δ13CPDB values varying from −30‰ to −15‰ andan average of −22‰ (Ohmoto, 1972). Comparing the δ13CPDB datafrom different sources, the carbon isotope values reported from theore deposits in the northwest of Hebei Province is close to thosemantle-derived magmatic sources.

Wang et al. (2010) measured the helium and argon isotopic com-positions of 23 pyrite, galena, sphalerite, and quartz samples from un-derground levels of 10 gold, silver, and lead–zinc deposits and 2granite samples from the Dongping gold field in the northwest ofHebei Province (Table 6). The 3He/4He values of the sulfide mineralsand quartz are in the range of 0.38 × 10−6 to 9.47 × 10−6 (0.27Rato 6.81Ra, where Ra is the 3He/4He ratio of air = 1.39 × 10−6),much higher than those of the granite samples (0.007 × 10−6 to0.008 × 10−6, 0.005 Ra–0.006 Ra). With the equation formulated by

image of Fig.�9

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

No. Deposit Location Age/Ma Type Pb Ref.

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

N.margin W-M.portion Au 1 Ulantolgoi Bayannao'er, Inner Mongolia Porphyry 18.48 15.66 38.33 Qiu et al., 19942 Saiwusu Baotou, Inner Mongolia 16.84 15.39 37.24 Wang et al., 20103 Wulashan Baotou, Inner Mongolia 230 17.69 15.59 38.11 Xu et al., 19914 Shibaqinghao Guyang, Inner Mongolia 277 ± 1.73 17.93 15.57 38.66 Xu et al., 19915 Houshihua Hohhot, Inner Mongolia Ductile shear zone 17.09 15.56 37.58 Shi et al., 19936 Donghuofang Hohhot, Inner Mongolia 237 Far contact zone 18.93 16.01 39.73 Xu et al., 19987 Bayinhanggai Hohhot, Inner Mongolia 18.11 15.55 38.11 Yang et al., 20018 Bainaimiao Hohhot, Inner Mongolia 300 Contact zone 18.72 15.57 38.67 Li et al., 20039 Xiaoyingpan Zhangjiakou, Hebei 180 17.39 15.43 37.46 The third Geological Team of Hebei,1998;

Wang et al., 1992;Song et al., 1994;Peng et al., 1992;Wang et al., 2010

10 Dongping Zhangjiakou, Hebei 177.4 ± 5 Fracture-altered 17.64 15.47 37.43

11 Hanjiagou Zhangjiakou, Hebei 17.33 15.35 37.3412 Shuijingtun Chongli, Hebei 17.18 15.39 37.10 Xu et al., 1998;Xu et al., 199113 Zhongshangou Chongli, Hebei 120 17.30 15.46 37.26 The third Geological Team of Hebei,1998;

Wang et al., 1992;Song et al., 1994;Peng et al., 1992;Wang et al., 2010

14 Huangshanliang Chicheng, Hebei 230 Fracture-altered 17.38 15.39 37.1915 Hougou Chicheng, Hebei 172.9 ± 5 Fracture-altered 17.54 15.38 37.39

Cu 16 Wunugetushan Xin Barag Yougi, Inner Mongolia 178.1 ± 0.6 18.38 15.53 38.11 Tan et al., 2011Pb–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., 200219 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., 2010E.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., 199723 Xiajinbao Pingquan, Hebei 155.73 16.30 15.14 36.03 Wang et al., 200024 Tianjiacun Tangshan, Hebei 16.35 15.27 36.70 Wang et al., 201025 Jinchangyu Qianxi, Hebei 230 Disseminated quartz-vein 15.88 15.26 35.87 Wang et al., 2010;Zhang et al., 1996;26 Yuerya Kuancheng, Hebei 180 Quartz-vein 15.86 15.16 35.68 Wang et al., 2010;Zhen et al., 198827 Tangzhangzi Kuancheng, Hebei 180 Cryptoexplosive breccia 16.16 15.41 36.79 Niu et al., 200128 Huzhangzi Kuancheng, Hebei 16.25 15.22 36.23 Wang et al., 201029 Shapoyu Kuancheng, Hebei 14.99 14.96 34.83 Wang et al., 201130 Baimiaozi Kuancheng, Hebei 16.30 15.30 36.49 Wang et al., 201231 Maoshan Zunhua, Hebei 16.13 15.23 36.13 Bai et al., 1990;Shao et al., 1987;

Luan et al., 199632 Qingheyan Chinhuangtao, Hebei 179.5 16.17 15.06 35.95 Li et al., 199733 Xiazhangzi Chinhuangtao, Hebei 105.4 16.50 15.24 36.30 Yao et al., 200434 Niuxinshan Chinhuangtao, Hebei 175.8 ± 3.1 16.06 15.26 36.15 Wang et al., 2010;Yang et al., 199635 Erdaogou Chinhuangtao, Hebei 140.6 ± 2.8 17.58 15.76 38.9136 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., 201138 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

398S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

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., 200043 Fayunkuang Yantai, Shandong 120 Strata-bound 17.16 15.42 37.65 Wen et al., 199044 Denggezhuang Northern Shandong, Shandong 117.5 Quartz-vein 17.16 15.46 35.03 Wang et al., 200245 Xiadian Zhaoyuan, Shandong 120 Fracture-altered 16.79 15.31 37.08 Chen et al., 1989; Wang et al., 2002;

Li et al., 199046 Yigezhuang Zhaoyuan, Shandong 120 Fracture-altered 16.95 15.52 38.39 Zhang et al., 2002;Zhu et al., 199947 Lingshangou Zhaoyuan, Shandong 120 Quartz-vein 17.33 15.47 37.88 Lin et al., 199048 Fushan Zhaoyuan, Shandong Quartz-vein 17.50 15.52 38.08 Chen et al., 198949 Jinchiling Zhaoyuan, Shandong 120–80 Quartz-vein 17.13 15.35 37.54 Wang et al., 2002;Yao et al., 199050 Taishang Zhaoyuan, Shandong 120 Fracture-altered 17.70 15.80 38.94 Chen et al., 1989;Deng et al., 200051 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., 199152 Canzhuang Northern Shandong, Shandong Fracture-altered 17.29 15.48 37.9253 Xincheng Laizhou, Shandong 120 Fracture-altered 17.75 15.37 37.58 Zhen et al., 200654 Majiayao Qixia County, Shandong 120 Quartz-vein 16.56 15.24 37.07 Wang et al., 200255 Liukou Qixia County, Shandong 125 Quartz-vein 16.55 15.33 37.66 Wang et al., 200256 Panzijian Qixia County, Shandong 71.86 Quartz-vein 16.17 15.16 36.82 Wang et al., 200257 Jinguanding Qixia County, Shandong 120 Quartz-vein 16.92 15.31 37.28 Wang et al., 2002; Lin et al., 1999;

Yao et al., 199058 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., 198860 Pengjiakuang Northern Shandong, Shandong 120.5 ± 0.5 Strata-bound 17.11 15.42 37.63 Wang et al., 2002; Yao et al., 199061 Congjia Rushan, Shandong 120 17.21 15.41 37.92 Chen et al., 1989; Deng et al., 200062 Dazhuangzi Longkou, Shandong 120 Fracture-altered 17.28 15.52 37.95 Yao et al., 1990; Li et al., 199063 Qibaoshan Wulian, Shandong 120 Explosive-breccia 16.97 15.37 37.16 Ying et al., 199464 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., 199966 Yuejiazhuang Xintai, Shandong Fracture-altered 21.63 16.08 47.52 Zhang et al., 199967 Yinan Yinan, Shandong 120 Skarn 18.84 15.56 42.59 Hu et al., 200468 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., 1996S. 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., 199672 Xiongershan Shanglou, Shaanxi 120 Quartz-vein 17.57 15.50 37.94 Lu et al., 2003:Chen et al., 199573 Xiajiadian Shanyang county, Shanglou, Shaanxi Carlin 18.41 15.58 38.29 Zhou et al., 200474 Tongyu Tongguan County, Weinan, Shaanxi Quartz-vein 17.25 15.57 38.02 Yu et al., 198975 Wenyu Lingbao County, Henan 120 Quartz-vein 17.18 15.58 38.33 Xu et al., 199276 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., 200379 Xiaonangou Songxian, Henan Fracture-altered 17.08 15.44 37.67 Shao et al., 1996


399S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

Table 3 (continued)

No. Deposit Location Age/Ma Type Pb Ref.

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

80 Jinchangzi Songxian Henan 180 18.20 15.55 38.0481 Huachanggou 230 18.20 15.50 38.2082 Ganshuao Songxian, Henan 17.14 15.40 37.72 Chen et al., 199283 Hugou Songxian, Henan 17.23 15.47 37.63 Chen et al., 199684 Yaogou Songxian, Henan 17.26 15.40 37.55 Fan et al., 199485 Dianfang Songxian, Henan 17.06 15.37 37.50 Ren et al., 199386 Hongzhuang Songxian, Henan 17.28 15.38 37.77 Yan et al., 200587 Pasigou Songxian, Henan 17.13 15.44 38.06 Xu et al., 200588 Xiasongping 129 ± 45 17.47 15.51 38.21 Pang et al., 201189 Shanggong Luoning, Henan 242 Fracture-altered 17.12 15.41 37.6390 Kangshan Luanchuan, Henan 17.77 15.51 38.19 Chen et al., 199691 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., 200293 Lengshuibeigou Luanchuan, Henan 17.69 15.55 38.57 Lu et al., 200294 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., 199196 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., 199198 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., 2001Interior 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., 1997102 Shihu Lingshou County, Hebei 140 Quartz-vein 16.34 15.33 37.44 Wang et al., 2010;Yang et al., 1991103 Xishimen Middle of Taihang Mountains 135.1 16.30 15.23 37.26 The Taihang research team,1994104 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., 2011Fe 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., 2007107 Jiazhuang Shahe, Hebei Skarn 17.80 15.42 37.92 Zhang et al., 1995108 Baishabei Wuan, Hebei Skarn 17.77 15.48 38.02109 Beiandong Wuan, Hebei Skarn 17.71 15.46 28.05110 Hongshan Wuan, Hebei Skarn 17.71 15.45 37.76 Yan et al., 2000111 Pingshun Changzhi, Shanxi Skarn 18.30 15.55 37.94 Zhang et al., 200112 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., 2010114 Yindonggou Lingshou County, Hebei 18.32 15.65 38.74 Wang et al., 2010;Wang et al., 2007115 Futuyu Laiyuan, Hebei Skarn 15.92 15.31 37.01 Wang et al., 2010116 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., 2001118 Yixingzhai Fanshi, Shanxi 130 Quartz-vein 16.72 15.31 36.83 Jing et al., 1992119 Shangyanghua Fanshi, Shanxi 19.15 15.71 39.34 Tian et al., 1991120 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., 1993122 Xiaozhongzui 15.09 15.07 34.99 Li et al., 1994123 Gengzhuang Fanshi, Shanxi 180 Explosive breccia 17.34 15.35 37.88 Luo et al., 2009124 Tainashui Lingqiu, Shanxi 16.73 15.33 36.82 Tian et al., 1998125 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., 2011127 Dongfengding Xiangfen, Shanxi 120 18.33 15.58 38.85 Wang et al., 2009

400S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

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 theore-forming fluid was calculated to be in the range of 3.3% to 86.1%with an average of 31.5%, and mostly in the range of 13% to 26%.

Combining all the data from the S, Pb, Si, H, O, C, and He isotopicanalyses, it can be concluded that materials and fluid derived fromthe mantle cannot be excluded as an important contribution to theformation of the gold, silver, lead and zinc as well as the molybdenumdeposits in the northwest of Hebei Province.

3.4.1.2. Eastern Hebei Province. The eastern part of Hebei Province islocated within the north-eastern margin of the NCC. More than 100Mesozoic gold deposits and occurrences and 40 copper (gold), silver–lead–zinc polymetallic deposits occurrences were reported from thisarea. Most of the gold deposits are located in the Archeanmetamorphicrocks whereas the majority of the polymetallic deposits are hostedin the Jurassic strata. Almost all the deposits are associated spatiallyand temporally with the Yanshanian granitic intrusions (Wang et al.,2010).

The emplacement of the Yanshanian granitic intrusions was coe-val with the formation of the deposits. The REE patterns of the intru-sive rocks are characterized by negative Eu anomaly (ΣREE varies66.75 ppb to 317.55 ppb; δEu varies from 0.12 to 0.85; LREE/HREEvaries from 1.66 to 24.04). (87Sr/86Sr)i values for the intrusive rocksvary from 0.704 to 0.708 (Zhang and Chen, 1996). Trace elementanalyses of the small stocks (with an outcrop area of b2 km2) yieldedhigh gold contents ranging from 11 ppb to 92 ppb. These

characteristics of the intrusive rocks suggest that the magmas werederived from the lower crust with some contribution of mantlematerials.

The large sulfur isotopic data base (>260 samples from 19 deposits)from previous studies display δ34S values of the sulfide minerals from−6.3‰ to 8.3‰ with most of the values falling within the range of−1‰ to 3‰ and an average of−1.9‰with a few exceptions (Table 2).The sulfur isotopes of the sulfide minerals from most of these depositsshow equilibrium fractionation trend. These sulfur isotopic composi-tions are comparable with those from the Jinchanggouliang gold depos-it in Chifeng City of Inner Mongolia (δ34S = −5.0 to 1.1 average−0.1;Wei et al., 1993), the Lanjiagou molybdenum deposit in Jinxi County(δ34S = −0.3 to 7.9 average −3.3 for 11 samples; Rui et al., 1994)and the Xiadabao gold deposit in Qingyuan County (δ34S = −2.0 to1.9 average −0.4; Wei et al., 1993) of Liaoning Province.

The lead isotopic compositions of 67 samples from 13 deposits ineast Hebei Province vary within narrow ranges with 206Pb/204Pbvalues varying from 14.986 to 16.304, 207Pb/204Pb from 14.961 to15.408, and 208Pb/204Pb from 34.834 to 36.787 (Table 3). In Zartman'sdiagrams, most of the data cluster around the mantle line, suggestingthat the lead of the ores were mainly derived from the mantle and thelower crust (Fig. 10). These data are remarkably consistent with thosefrom the Xiadabao gold deposit of Qingyuan County, Liaoning Prov-ince where the 206Pb/204Pb vary from 15.912 to 16.177, 207Pb/204Pbvary from 15.154 to 15.373, and 208Pb/204Pb vary from 36.107 to36.671 (Wei et al., 1993). The lead isotopic systematics of the ore

image of Fig.�10

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

No. Deposit Location Mineralization type Age/Ma Type δ30Si_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., 19922 Xiaoyingpan Xuanhua, Hebei Au 171.45 Quartz-vein −0.3–0.1 Wanget al., 2010;

Yin et al., 19953 Wanquansi Wuanquan, Hebei Au, Ag −0.2 to −0.1 Wanget al., 20104 Shuijingtun Chongli, Hebei Au Fracture-altered −0.2–0.3 Wanget al., 20105 Zhongshangou Chongli, Hebei Au 115.1 Far contact −0.2–0.2 Wanget al., 20106 Huangtuliang Chicheng, Hebei Au 120.63 Fracture-altered −0.3–0.0 Wanget al., 20107 Hougou Chicheng, Hebei Au 154.4 ± 1.3 Fracture-altered −0.2 Wanget al., 20108 Yangshugou Fengning, Hebei Mo, Ag 140.10 ± 213 Porphyry −0.3 Wanget al., 20109 Dacaoping Fengning, Hebei Mo 220.10 ± 117 Porphyry 0.07 Guo et al., 201110 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., 199412 Dongzigou Chengde, Hebei Ag, Au Quartz-vein 1.31 Wang et al., 201013 Xiajinbao Pingquan, Hebei Au 2.66 Wang et al., 200014 Malanguan Tangshan, Hebei Au 3.0 Song et al., 199415 Jinchangyu Qianxi, Hebei Au 2190 ± 58 Fracture-altered Quartz-vein −0.3 Wang et al., 2010; Zhang et al., 199616 Yuerya Kuancheng, Hebei Au 175 ± 1 Quartz-vein −0.2 Wang et al., 2010; Zheng et al., 198817 Tangzhangzi Kuancheng, Hebei Au 172 ± 2 Explosive-breccia 1.45 Wang et al., 201018 Jianbaoshan Kuancheng, Hebei Au Stata-bound −0.3 to −0.1 Wang et al., 201019 Maoshan Zunhua, Hebei Au Quartz-vein 1.03 Bo et al., 1990; Shao et al., 1987;

Luan et al., 199620 Sanjia Qinhuangdao, Hebei Au Contact −0.1 Wang et al., 201021 Huajian Qinhuangdao, Hebei Au −0.3 Wang et al., 201022 Niuxinshan Qinhuangdao, Hebei Au 172 ± 2 Contact 0.46 Wang et al., 2010; Yang et al. 1996;

Luo et al., 2001E.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., 199425 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,2001Interior 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., 201229 Qiubudong Pingshan, Hebei Ag, Au 0.0–0.1 Wang et al., 201030 Xishimen Lingshou, Hebei Au −0.2 Wang et al., 201031 Chounikou Lingshou, Hebei Au 0.0 Wang et al., 201032 Shanggang Laishui, Hebei Au 0.1 Wang et al., 2010

402S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

Table 5Hydrogen, oxygen and carbon isotopic compositions of the ore deposits in the NCC.

Type Deposit Location Age/Ma Type OSMOW (‰) D (‰) 13C (‰) 18OH2O (‰) Ref.

N.margin W-Mportion Au Wanquansi Wanquan, Hebei 13.3 −109.5 −3.9 2.57 Wang et al., 1992Zhongshan'gou Zhangjiakou, Hebei 120± 12.67 −87.33 −3.77 0.81 Wang et al., 1992Shuijingtun Zhangjiakou, Hebei 12.3 −70.5 3.47 Shi et al., 1993Huangtuliang Chicheng, Hebei 230 Fracture-altered 10.02 −83.75 −4.1 0.38 Song et al., 1994Fengning Fengning, Hebei 4.9 −98 −6 −3.14 Wang et al., 2010Dongping Zhangjiakou, Hebei 180± Fracture-altered 8.76 −91.2 −2.49 1.49 Fan et al., 2001Xiaoyingpan Xuanhua, Hebei 180± 13.17 −93.17 7.31 Mao et al., 2001Hougou Chicheng, Hebei 180± Fracture-altered 11.24 −96.58 3.87 Wang et al., 2010Zhangquanzhuang Xuanhua, Hebei 13.01 −109.1 5.99 Mao et al., 2001Hanjiagou 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, 2000Bainaimiao Wulanchabu, Inner Mongolia 300 3.69 −85 3.98 Ye, 1997Bayinhanggai Bayannaoer, Inner Mongolia 13.6 −79 5.79 Chen et al., 2001Liangqian Guyang, Inner Mongolia 10.7 −80 6 Xu et al., 1998Donghuofang Hohhot, Inner Mongolia 12.7 −96 4.635 Shi et al., 1993Houshihua Hohhot, Inner Mongolia Ductile shear zone 12.9 −83.33 6.18 Wang et al., 2010Jinchanggouliang Chifeng, Inner Mongolia 13.22 −82.92 −7.87 6.07 Zhang et al., 2002Wulashan Baotou, Inner Mongolia 230 12.91 −77.16 4.58 Lang, 1997Dongkalaqin 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., 2004Zhaojiagou 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, 2001Dacaoping Fengning, Hebei 220.10 ± 117

224.10 ± 115232.17 ± 115

Porphyry Guo et al., 2011

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., 1994Shapoyu Xinglong, Hebei 12.6 −61 Wang et al., 2010Malanguan Tangshan, Hebei 12.78 −72.5 −5.25 3.42 Wang et al., 2010Tianjiacun Zunhua 11.24 −73 Wang et al., 2010Yuerya Kuancheng, Hebei 175 Quartz vein 13.112 −88.45 −4.18 7.029 Chai et al., 1989Huzhangzi Qingyuan, Liaoning 14.1 −76 Wang et al., 2010Sajingou Kuancheng, Hebei 12.2 −79 Wang et al., 2010Banbishan Qinglong, Hebei 10.36 −78.8 Wang et al., 2010Maojidian Qingyuan, Liaoning 13.9 −87 Wang et al., 2010Huashi Xinglong, Hebei −84.67 Wang et al., 2010Tangzhangzi Kuancheng, Hebei 12.4 −56 Wang et al., 2010Xiacaonian Qinglong, Hebei −63 −5.1 Wang et al., 2010Xiaojinggou Zhangjiakou, Hebei 24.05 −71.07 −2.36 12.15 Wang et al., 2010Xiajinbao Pingquan, Hebei 13.53 −70.15 4.63 Shao et al., 1987Honghuagou Chifeng, Inner Mongolia 1700 −88 5.8 Wang et al., 1993Erdaogou Beipiao, Hebei 900 −92 6.1 Wang et al., 1992Anjiayingzi Chifeng, Inner Mongolia 800 −109 5.2 Wang et al., 1993Zhaojiagou Chicheng, Hebei −96 0.3 Wang et al., 2010Reshui Chifeng, Inner Mongolia −88 9.2 Wang et al., 2010Hongshi Yixian, Liaoning −116 1.1 Wang et al., 2010Xiazhangzi Qinglong, Hebei 18 −85.1 −2.07 6.01 Wang et al., 2010Sanjia 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, 2007Nianzigou Chifeng, Inner Mongolia 154.3 ± 3.6 −128.8 to −109.2 Zhang, 2010


403S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

Table 5 (continued)

Type Deposit Location Age/Ma Type OSMOW (‰) D (‰) 13C (‰) 18OH2O (‰) Ref.

Hadamengou Chifeng, Inner Mongolia 239.76 ± 3.04 11.6 Hou, 2011Xiaojiayinzi Kezuo, Liaoning 177 ± 5 Skarn 10.1 102 6.5 Tang, 1979Lanjiagou Gongchangling, Liaoning 186.5 Quartz vein −87.7 1.9 Dai, 2008Dazhuagke Yanqing, Beijing 146 ± 11 10.42 Dong et al., 1992Xiaoshigou Pingquan, Hebei 134 ± 3 Porphyry-Skarn −91.93 7.03 Zhang et al., 1994; Quan et al., 1992Huashi Chengde, Hebei −84.67 Wang et al., 2010

Fe Zhangjiagou Dandong, Liaoning Province −2.19–3.09 Xia, 1997Huanggang kesheketengqi, Inner Mongolia 135.31 ± 0.85 Skarn 6.2 −83 7.4 Mao, 2011Zhoutaizi Kuanping, Hebei Province 2460 Xiang et al., 2010Damiaoheishan Chengdeshi, Hebei Province 39 7.98 Zhao et al.,2012; Sun et al., 2009Xiaojiayinzi 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., 1991Jiaodong 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., 1994Xincheng Laizhou, Shandong 120± Fracture-altered 14.17 −85 5.41 Zhang et al., 1994Jiaojia Laizhou, Shandong 120± Fracture-altered 13.15 −84.26 −5.3 3.02 Ding et al., 1998Changshang Laizhou, Shandong 120± Fracture-altered 13.17 −78.67 5.1 Zhang et al., 1994Lingshan'gou Zhaoyuan, Shandong 120± Quartz vein −79.79 2.44 Yang et al., 1996Shilipu Zhaoyuan, Shandong 120± 9.25 −89.67 −4.2 Yang et al., 1996Linglong Zhaoyuan, Shandong 120± Quartz vein 12.99 −69.34 −5.44 4.66 Yang et al., 1996Taishang Zhaoyuan, Shandong 120± Fracture-altered 13.23 −84.67 4 Yang et al., 1996Dayin'gezhuang Zhaoyuan, Shandong 120± Fracture-altered 9.07 −78 2.7 Yang et al., 1996Rushan Rushan, Shandong 120± Quartz vein 10.23 −82.8 3.36 Yang et al., 1996Denggezhuang Yantai, Shandong 120± Quartz vein 12.4 −77.78 −2.37 4.95 An et al., 1988Yuan'gezhuang Yantai, Shandong 120± Quartz vein 7.64 −73.5 2.88 An et al., 1988Dongdaokou Yantai, Shandong 120± 11.66 −82.13 2.71 An et al., 1988Dazhuangzi Pingdu, Shandong 120± Fracture-altered 11.45 −64.93 −1.5 3.11 Mao et al., 2002Qixia Qixia, Shandong 120± Quartz vein 12.39 −77.85 0.87 Zhai et al., 1996Qibaoshan Wulian, Shandong 120± Explosive-breccia 11.54 −68.76 4.21 Qiu et al., 1996Pengjiakuang 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., 2004Jinchang 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., 2010S. 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., 1992Chucha-luanshigou Lingbao, Henan 10.25 −62.7 2.52 Xu et al., 1992Yangzhaiyu-S60 Lingbao, Henan 11.1 −47.62 5.2 Yu et al., 1997Zhuyu Lingbao, Henan 10.8 −47.62 5.16 Li et al., 1998Xichang'an-dongman Lingbao, Henan 11.48 −57.73 4.89 Wang , 1987Dongtongyu-Q8 Tongguan, Shaanxi 12.37 −48.63 6.31 Zhou et al., 1993

404S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

Gongyu Songxian, Henan 10.5 −74 0.1 Li et al., 2004Laowan Tongbo, Henan Fracture-altered 11.95 −70 1.78 Xie et al., 2001Taoyuan Weinan, Shaanxi 10.45 −59.5 7.62 Wang et al., 2010

Mo Yechangping Sanmenxia, Henan 9.12–9.59Jinduicheng 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., 2009Xiong'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., 1998Kangshan Luanchuan, Henan 14.94 −80.5 −1.09 4.82 Wang et al., 2001Qinggangping Luanchuan, Henan 10.14 −83.3 5.35 Chen et al., 1996Putang Nanyang, Henan 5.2 −50.3 −3.12 −6.85 1995Qiyugou 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, 20062006 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., 1991Nannihu 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., 2010Yangshugou Lingshou, Hebei 16 −66 −3.5 2.76 Wang et al., 2010Xishimen Lingshou, Hebei 13.1 −83 5.4 Wang et al., 2010Beiyingxigou Lingshou, Hebei 14.3 −87 4.56 Wang et al., 2010Chounikou 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., 2010Yindong 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., 2010Au–Mo Dawan Laiyuan, Hebei 2.86 −101.72 −5.6 Tu, 1995Au–Mo Futuyu Laiyuan, Hebei 6.77 −115 0.74 Wang et al., 2010Au 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., 1999Lianbaling Laiyuan, Hebei 5 −90 1.2 Wang et al., 2010Luanmuchang Yixian, Hebei −74 12.25 Wang et al., 2010Dashiyu Tangxian, Hebei −72.69 −1.5 Wang et al., 2010Xiaolinggen Yixian, Hebei −56.09 −5.99 Wang et al., 2010

Pb–Zn Lianbaling Laiyuan, Hebei Yanshanian −90 1.2 Wang et al., 2007Fe 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

405S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(2014)376

–414

Fig. 11. D–O isotopic composition diagrams of fluid inclusions in quartz from the oredeposits in the NCC.


and associated granitoids show consistence from both regions(Table 3; Wei et al., 1993) suggesting a close genetic link betweenthe granitic magmatism and the gold and polymetallic mineralization.

Data from 49 samples representing 10 gold and copper–molybdenumdeposits show that in each deposit, the average δ18OH2O values vary from3.4‰ to 7.5‰ with one exception (Table 5). Thus, the Jinchanggoulianggold deposit in Chifeng area (δ18OH2O = 5.6‰ to 7.03‰; Wei et al.,1993), the Nanlongwangmiao gold deposit (δ18OH2O = 4.26‰ to6.69‰; Wei et al., 1993) and the Xiadabao gold deposit (δ18OH2O =4.03‰; Wei et al., 1993) in Qingyuan County, Liaoning Province, showvalues close to that of primary magmatic water (5‰ to 10‰,Sheppard, 1977). The average δDsmow values for each of the 19 de-posits range from −88‰ to −56‰, close to the −80‰ to −40‰value for primary water (Sheppard, 1977; Fig. 11). The averageδ13CPDB for each of the 7 deposits ranges from −5.25‰ to −2.07‰within the range for mantle carbon (−2‰ to −5‰; Taylor andBucher-Nurminen, 1986) and close to the range for magmatic car-bon (−9‰ to −3‰; Taylor and Bucher-Nurminen, 1986).

Wang et al. (2010) measured the helium and argon isotopes of 14pyrite, 1 galena, 1 gneiss and 2 granite samples from the gold and sil-ver deposits in the East Hebei Province (Table 6). The result showsthat the 3He/4He values vary in the range of 2.5 × 10−6 to9.39 × 10−6 with an average at 5.43 × 10−6, much higher thanthose of the granite and gneiss. Calculation with a mantle–crust bina-ry model shows that the mantle helium varies from 23% to 85% withan average at 53% (Wang et al., 2010). The measured 40Ar/36Ar variesfrom 308 to 1304 with a mean at 742, prominently higher than the295.5 value of air saturated water (ASW). The 3He/4He vs. 40Ar/36Ardiagram suggests marked contribution of mantle gas to the minerali-zation (Fig. 12).

3.4.2. Eastern margin of the NCCThere are three ore cluster regions in the eastern margin of the

NCC: the Jiaodong peninsula, the Liaodong peninsula and the Luxiarea (west of Shandong Province). Among these, the Jiaodong penin-sula is the most important gold district in China.

Sulfur isotope data on 68 pyrite samples from 13 quartz vein-typeand fracture alteration-type gold deposits in the Jiaodong peninsulashow δ34S values ranging from 2.4‰ to 12.6‰ with an average of7.6‰ andmost of the values lying in the range of 6‰ to 9‰. The resultsare consistent with those from the Cretaceous Gujialing granodioriteand the Archean Jiaodong Group of rocks (Table 2), as well as those ofthe Miaoling gold deposit in Gaizhou City, Liaodong peninsula (from6.2‰ to 10.9‰ averaging 8.9‰, Wei et al., 1993). Although a few δ34Sdata from the strata-bound gold deposits show marked difference

from those mentioned above, most of the values are broadly similar.These data suggest that the sulfur in the gold deposits in the Jiaodongpeninsula was mainly derived from the Cretaceous igneous intrusionswhich probably scavenged the sulfur from Archean basement.

Table 3 shows the 206Pb/204Pb data of 72 samples of sulfide min-erals from the quartz vein type and fracture-alteration type gold de-posits where the values range from 16.40 to 17.92 with an averageof 17.13. Those of 7 pyrite samples from the strata-bound gold de-posits vary from 16.92 to 22.15 with an average of 18.78 (Table 3),distinctly different from those mentioned above. The 206Pb/204Pbdata of 13 K-feldspar, 2 whole-rock and 1 galena from the Cretaceousand Jurassic intrusive rocks and the Archean Jiaodong Group of rocksvary from 16.4 to 17.87 with an average at 17.17, consistent withthose of the quartz vein type and fracture altered type gold deposits.The 207Pb/204Pb data of 72 samples of sulfide minerals from thequartz vein type and fracture altered type gold deposits range from15.20 to 15.72 with a mean at 15.45, which are different from thoseof 7 pyrite samples from the strata-bound gold deposits (from 15.35to 16.15; average 15.74) and consistent with those of 13 K-feldspar,2 whole-rock and 1 galena from the Cretaceous and Jurassic intrusiverocks and the Archean Jiaodong Group of rocks (from 15.35 to 15.83,average 15.47). The 208Pb/204Pb data for the quartz vein-type andfracture-alteration type gold deposits range from 37.26 to 38.60with an average at 37.70, distinct from those of the strata-boundgold deposits (from 37.08 to 49.05; average 39.81) and consistentwith those of the Cretaceous and Jurassic intrusive rocks and the Ar-chean Jiaodong Group of rocks (from 36.96 to 37.92; average 37.51).The consistence in the lead isotopic composition of the quartzvein-type and fracture alteration-type gold deposits with the Meso-zoic intrusions and the Jiaodong Group of rocks imply a close geneticlinkage among these. On Zartman's diagrams, the data show that thelead of the gold ores was derived from different sources includingmantle and the basement (Fig. 10).

A group of 47 δ18OH2O and δDSMOW data on quartz from 8 quartzvein type and fracture altered type gold deposits show a range ofvalues from −8‰ to 9.69‰ with an average of 3.91‰ and −95.8‰to −33.0‰ with an average of −77.3‰ respectively (Table 5). Agroup of 9 δ18OH2O and δDSMOW data on quartz from 2 altered gold de-posits show values from 0.59‰ to 4.03‰ with an average1.81‰ and−97.9‰ to −79.0‰ with an average −89.3‰, respectively(Table 5). Except for a few data, all the δDSMOW values are lower thanthat of the typical metamorphic water (−65‰ to −20‰, Hugh andTaylor, 1974) and close to the primary magmatic water (−80‰ to−40‰, Hugh and Taylor, 1974). Most of the δ18OH2O data are closeto the primary magmatic water (5‰ to 10‰, Hugh and Taylor,1974; Fig. 11), suggesting that the water associated with mineraliza-tion was closely related with the magmatism.

Fifty three δ13CPDB data of the calcite and siderite from 6 quartz veintype and fracture altered type gold deposits show values from −6.5‰to−0.6‰with an average of−4.6‰, well within the range ofmagmat-ic carbon (from −9‰ to −3‰; Table 5). The majority of the data fallwithin the range of mantle carbon (from −5‰ to −2‰, Taylor andBucher-Nurminen, 1986). Nineteen δ13CPDB data on the calcite and do-lomite from 2 strata-bound gold deposits show variation from −4.8‰to 1.6‰ with an average −2.0‰ and the majority of the values corre-sponds with mantle carbon whereas a few fall in the range of sedimen-tary carbonate rocks (from−2‰ to+3‰, Veizer et al., 1980). The dataclearly reflect the involvement of the wall rocks of the ProterozoicJingshan Group of dolomite, especially in the Dujiaya gold deposit.

Helium and argon isotopic data on 25 fresh pyrite samples fromunderground levels of 5 quartz vein type gold deposits in the Jiaodongpeninsula (Table 6; Fig. 12) show that the mantle helium involved inthe quartz vein gold mineralization vary from 0 to 42% with an aver-age of 6% (the negative values are taken as 0). The mantle helium in-volved in the strata-bound type of gold mineralization varies from 0to 12% with an average value of 4% (8 samples from 3 deposits),

image of Fig.�11

Table 6Helium and argon isotopic compositions of the ore deposits in the NCC.

No. Deposit Location Age/Ma Type 3He 4He 3He/4He (Rc/Ra) 40Ar/36Ar 40Ar/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;Cai et al., 2004; Zheng et al., 20072 Huangtuliang Au Chicheng, Hebei 230 Fracture-altered 0.93 1238 5000

3 Xiaoyingpan Au Xuanhua, Hebei 180 2.2 2073 714.28574 Dongping Au Zhangjiakou, Hebei 180 Fracture-altered 4.05 464 5.62755 Zhongshangou Au Chongli, Hebei 120 0.38 430 1.88116 Yangshugou Mo Fengnin, Hebei 952.15 68.94 1.77 797 0.06

E. portion 7 Jinchangyu Au Qianxi, Hebei 132 Quartz vein 532 106.4 5 653 0.15048 Huzhangzi Au Kuancheng, Hebei 399.25 159.7 2.5 817 0.07649 Huashi Au Chengde, Hebei 62.4 9.6 6.5 308 0.052510 Shapoyu Au Kuancheng, Hebei 265.35 91.5 2.9 1304 0.156711 Yuerya Au Kuancheng, Hebei 175 Quartz vein 156.87 58.1 2.7 575 0.023312 Tanjiacun Au Tangshan, Hebei 1264.56 287.4 4.4 886 0.043613 Huajia Au Qinhuangdao, Hebei 14.08 3.06 4.6 1007 7.142914 Tangzhangzi Au Kuancheng, Hebei 173 Explosive-breccia 91.72 14.11 6.5 365 1015 Malanguan Au Tangshan, Hebei 7553.32 804.4 9.39 1166 0.016316 Xiaoyingzi granite Au Qinhuangdao, Hebei 179.5 0.44 441.617 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 0.177919 Canzhuang Au Zhaoyuan, Shandong Fracture-altered 2.842 20.3 0.1 1636.520 Denggezhuang Au Yantai, Shandong 120 Quartz vein 63.71 2.2921 Jinchiling Au Zhaoyuan, Shandong Quartz vein 4.13 3.69 0.8 383.7 0.481522 Linglong Au Zhaoyuan, Shandong 120 Quartz vein 2.045 3.29 0.4428 590523 Jinqingding Au Rushan, Shandong Quartz vein 2.257 3.43 0.47 474.624 Zhaodaoshan Au Jiaodong, Shandong Quartz vein 2.066 36.9 0.04 428.925 Pengjiakuang Au Rushan, Shandong 120 Strata-bound 92.87 8.98 1.05 380.5 1.28226 Dujiaya Au Yantai, Shandong Strata-bound 8.209 47.4 0.1237 509.527 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 871Interior 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 0.149731 Chounikou Au Lingshou, Hebei 307.8 9.16 3.36 511 0.421932 Shanggang Au Laishui, Hebei 1108 460 2.41 2361 0.028533 Shangmingyu Au Taihang Mountain 2782 231.9 1.2 365 0.012234 Mujicun Cu Au Laiyuan, Hebei 140 0.1089 Gao et al., 201135 Yintonggou Mo Au Lingshou, Hebei 2405.7 235.85 1.02 468 0.58 Wang et al., 2010

407S.-R.Li,M

.Santosh/Ore

Geology

Reviews56

(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 variesfrom 26% to 100% with an average of 63% (8 samples from 2 deposits).

All the above data show substantial input of mantle materials in thegold mineralization in Jiaodong peninsula during the Early Cretaceous.

3.4.3. Southern margin of the NCCThe Xiaoqinling and the Xiong'ershan areas are the two most im-

portant ore cluster regions characterized by predominantly Early Cre-taceous gold and few silver–lead–zinc deposits related with coevalmagmatic rocks in the southern margin of the NCC. The Xiaoqinlingregion is recognized as the second largest gold district in China afterthe Jiaodong peninsula.

Wang et al. (2010) collected 261 δ34S data from 17 deposits ofthe Xiaoqinling and Xiong'ershan areas (Table 2) which show arange of −19.2‰ to 7.2‰ with the average for each deposit rangingfrom −13.1‰ to 6.22‰. Most of the values are concentrated in therange of −4‰ to 6‰, comparable with those of the northwest ofHebei Province.

The average 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb data from265 samples of sulfide minerals from 27 deposits in the southernmargin and the nearby areas vary from 16.92 to 18.32, 15.31 to15.65 and 37.26 to 39.00 (Wang et al., 2010). Plots of the data onthe lead isotope evolution diagrams (Zartman and Doe, 1981;Fig. 10) show that most of the values fall in the orogenic line/region.This feature suggests that the lead was mainly derived from an envi-ronment similar to the orogenic belt, comparable with that in thenorthwest of Hebei Province.

A group of 138 H–O isotopic data from 17 deposits in theXiaoqinling and Xiong'ershan regions shows that, except the Putanggold deposit, the average δ18OH2O and δDSMOW values for each depositvary from 0.10‰ to 6.42‰ and from −87.41‰ to −52.58‰ for thetwo regions respectively, consistent with the role of primary mag-matic water (Table 5; Fig. 11).

Thirty δ13CPDB data on the carbonate minerals from 9 depositsin the southern margin of the NCC show variation from −4.41‰ to−0.80‰ with most of the values clustering in the range of −4‰ to−2‰ (Table 5). The data suggest that the carbonmight have been de-rived from the mantle (δ13CPDB from −5‰ to −2‰; Taylor andBucher-Nurminen, 1986).

3.4.4. Western margin and central NCCWhereas only few data are available for the western margin of the

NCC, there is adequate data from the central NCC, particularly fromthe Taihang Mountain region for a statistical evaluation. The northernTaihang Mountains host numerous gold, molybdenum, lead–zinc andsilver deposits. The southern Taihang Mountain region is character-ized by skarn type iron deposits. A comparison of the chronology

and geochemical characteristics of the two areas (Li et al., 2012; Liet al., 2013) has brought out prominent differences between thetwo areas.

The δ34S data on 169 sulfide samples from 17 gold, silver, molyb-denum, and lead–zinc deposits in the northern Taihang Mountainsshow variation from −3‰ to 5‰ with a few exceptions (Table 2;Fig. 9), whereas 23 δ34S data on pyrite from 13 iron deposits in thesouthern Taihang Mountains vary from 11.6‰ to 18.7‰ with amean at 15.2%.

The lead isotopic compositions of 76 sulfide minerals from 17 de-posits in the northern Taihang Mountains show the following varia-tion in the average value for each deposit: 206Pb/204Pb from 15.77 to17.42, 207Pb/204Pb from 15.09 to 15.45 and 208Pb/204Pb from 36.29to 38.74 (Table 3). Five pyrite samples from the Beiminghe iron de-posit in the southern Taihang Mountains (Shen et al., 2013) show206Pb/204Pb values of 17.84–18.79 (average 18.42); 207Pb/204Pbvalues of 15.46–15.62 (average 15.56) and 208Pb/204Pb values of37.93–39.75 (average 38.73). In the lead isotope evolution models(Fig. 10), most of the data from the northern Taihang plot on thearea between the lower crust line and the mantle line, and the fiveanalyses of the iron deposit from the southern Taihang Mountainsfall between the orogen and the mantle lines, mainly clustering nearthe orogen line.

A set of 48 data on H–O isotopes from 17 deposits in the northernTaihang Mountains (Table 5) shows that, except in the case of threedeposits, the average δ18OH2O and δDSMOW values for each depositrange from−1.50‰ to 7.62‰ and from−101.72‰ to−56.09‰, fairlyclose to that of the primary magmatic water (Fig. 11). Another groupof 13 samples from 9 deposits in the northern Taihang Mountainsshows δ30SiNBS-28 values in the range of −0.3‰ to 0.5‰ with a meanat 0.08‰ (Table 4), consistent with the δ30SiNBS-28 values of granite(−0.4‰ to 0.4‰, Ding and Jiang, 1994).

Thirty oneheliumand argon isotopic data (Table 6) from11depositsshow mantle helium ranging from 0 to 38.52% with a mean of 15%suggesting the involvement of mantle helium in the mineralization ofthe northern Taihang Mountains during the early Cretaceous (Li et al.,2013; Wang et al., 2010). Helium and argon isotope data on the pyritefrom the iron deposit in the southern Taihang Mountains indicate thatmost of the ore-forming fluid was derived from the crust, with nomore than 3% of helium (0.17% to 2.98%, average 1.43%) contributionfrom the mantle (Li et al., 2013; Shen et al., 2013).

3.5. Link between metallogeny and the evolution of the NCC

3.5.1. Metallogeny in response to the formation of the NCCThe formation of the NCC involved complex andmultistage process-

es during the early Precambrian, amongwhich the twomain events are

image of Fig.�12


the assembly of microblocks to construct the fundamental architectureof the NCC by 2500 Ma and the final cratonization through the collisionof the major crustal blocks by 1850 Ma (Santosh, 2010; Wang and Liu,2012; Zhai and Santosh, 2011; Zhang et al., 2011; Z. Zhang et al.,2012). During Neoarchean collision of the microblocks, around eightDongyaozhuang-type of gold deposits formed in the Wutaishan areain the northern TaihangMountains. At the same time, in theWutaishanarea and Lvliangshan area of the central NCC, more than 21 large- tomedium scale BIF type of iron deposits and meta-ultramafic rock-hosted rutile deposits formed, which include the Shanyangping irondeposit, Jingangku iron deposit and the Nianzigou Ti (rutile) deposit(Jia et al., 2006; Shi et al., 2012) in theWutaishan area, the Yuanjiachuniron deposit in the Lvliangshan area. In the Zhongtiaoshan area, south-ern Shanxi Province, 4 large Paleoproterozoic porphyry type copper de-posits and 50 minor occurrences also formed during the amalgamationstage of the NCC (Zhang et al., 2003). After the Neoarchean amalgam-ation, in the early Paleoproterozoic rifting stage, around 17 VMS typecopper deposits such as those of the Hujiayu and Bizigou formed inthe Zhongtiaoshan area (Zhang et al., 2003). Except for the mineraliza-tion in the central NCC, gold deposits similar to the Dongyaozhuangtype, such as the Shibaqinghao in Inner Mongolia, the Paishanlou andNanlongwangmiao, and the Gongchangling BIF type iron deposits inLiaoning Province, also formed during late Neoarchean at the northernmargin of the NCC. Large scale SEDEX and VMS types copper–(lead–zinc) and gold deposits, the Bayan Obo REE–Nb–Fe deposit, theDongshengmiao, Tanyaokou, Huogeqi polymetallic deposits in theLangshan area and the Jiashengpan polymetallic deposit in theCha'ertaishan area of Inner Mongolia, formed in the Paleoproterozoicto Mesoproterozoic at the northern margin of the NCC (Zhai et al.,2004). Large SEDEX and VMS type deposits were also generated in thenorth-eastern margin of the NCC, including the Qingchengzi Pb–Zn–(Ag–Ag) deposit, the Wengquangou B deposit, two of the wellknown SEDEX type deposits, and the Hongtoushan Cu–Zn depositwhich is a VMS type deposit in Liaoning Province. In addition, BIF typedeposits are also found in the interior of the NCC, such as the ShuichangFe deposit in the eastern Hebei Province (Zhai et al., 1999). In theMesoproterozoic, V–Ti–Fe and Cu–Ni–Pt deposits formed in the north-ernmargin (theDamiao–Heishan Fe–Ti–V–P deposit inHebei Province)and in the western margin (the Jinchuan Cu–Ni–Pt deposit in GansuProvince, 1508–1511 Ma, Tang and Li, 1995) of the NCC.

The amalgamation of the unified Eastern and Western Blockswithin the NCC followed a prolonged subduction–accretion historyprior to the final collision in late Paleoproterozoic (Santosh, 2010;Santosh et al., 2013). A series of BIF, porphyry and Dongyaozhuangtypes of gold and polymetallic deposits were generated during thisperiod (Zhang et al., 2003). During the extension period after thecollision, a number of VMS and SEDEX types of polymetallic depositsformed in the aulacogens. It is interesting to note that such minerali-zation not only occurred in the central zone but also broadly along thenorthern margin of the NCC. More importantly, BIF deposits also de-veloped in the interior of the craton, such as the Shuichang area inHebei Province, but a closer examination shows that this regiondefines the boundary between the Jiaoliao microblock and theQianhuai microblock. Thus, the location of the suturing between themicroblocks, as well as the zones of extension could mark importantsites for economic mineralization. The Mesoproterozoic mineraliza-tion can be correlated to the global rifting stage of the supercontinentColumbia (Deng et al., 2004a; Hou et al., 2008; Rogers and Santosh,2009; Santosh et al., 2009). In a recent work, Zhai and Santosh(2013) correlated the various types of metallogeny in the NCC to sec-ular changes associated with global tectonics in the evolving Earth.

3.5.2. Metallogeny in response to the destruction of the NCCAfter the major mineralization events associated with the

Neoarchean micro-block assembly, Paleoproterozoic cratonizationand Mesoproterozoic rifting, the NCC remained stable for a long

time without any major tectonic events or large scale mineralizationuntil the Jurassic. Nevertheless, some small scale Permian and Triassicmineralization occurred as mentioned in previous sections. TheHongqiling gabbro type Ni–Cu deposit in Jilin Province along thedeep-seated fracture at the northern margin of the NCC is recognizedto be of Triassic age (LÜ et al., 2011; Zhai et al., 1999). Surroundingthe craton, the Paleozoic marked the timing of subduction of thepaleo Asian ocean, and the late Paleozoic was the period of the closureof the paleo-Asian ocean. Both these processes were important formantle input into continental crust and mineralization. Targets forprospecting Paleozoic and early Mesozoic mineralization shouldfocus on the Caledonian and Hercynian accretionary belts surround-ing the northern margin of the NCC.

The Triassic was the period when the NCC amalgamated with theYangtze craton. During this process, the Yangtze plate subducted un-derneath the NCC, and some of the mineral deposits in the southernmargin of the NCC are correlated to this event. However, only weakmineralization occurred during Triassic.

From Jurassic to Cretaceous, the eastern part of the NCC and thewhole of east China witnessed a major tectonic transformation fromN–S compression to NNE–SSW shearing. Accompanying the early trans-formation and the onset of extension, adakitic lower crust-derivedgranitic batholiths were emplaced which uplifted the Precambrianbasement rocks. In the Jiaodong peninsula, for instance, the Linglongand Kunyushan granitic batholiths were emplaced at ca. 150 Mawithinmetamorphic basement represented by the Archean Jiaodong Groupand Proterozoic Jingshan Group (Yang et al., 2011 and our unpublisheddata). A series of intermediate and basic dikes and intermediate-felsicplutons with mixed lower crust–mantle features formed during theearly Cretaceous accompanied by the widespread formation of numer-ous ore deposits. The Jiaodong gold deposits and the coeval Guojialingand Sanfoshan granodioritic plutons and numerous intermediate-mafic and lamprophyre dikes (ca. 120 Ma, Cai et al., 2012; and ourunpublished data) in the eastern margin of the NCC, and the Shihuand Yixingzhai gold deposits and the Mapeng and Sunzhuang plu-tons in the Taihang Mountains in the central NCC (ca. 130 Ma, Li etal., 2012, 2013) are among the products of the early Cretaceousmagmatism-mineralization events. Most of the ore deposits wereformed in a transitional compression to extensional tectonic regime.The NE–SW ore-controlling fractures in Jiaodong peninsula showcomplex sinistral and dextral shearing during the ore-formingevents, with dominant sinistral movement in the early stages anddextral in the later stages (Li et al., 1996). Large scale inhomoge-neous lithosphere thinning beneath the NCC has been regarded asa direct geodynamic consequence of the extensive ore-formingevents (e.g., Li et al., 2012, 2013). Since the magmatism and mineral-ization are mostly concentrated in the early Cretaceous, rapid andlarge scale inhomogeneous delamination would also be a feasiblemodel for the thinning of the NCC.

It is interesting to correlate the isotopic data on the mineral de-posits in different domains within the NCC with the contour map ofthe lithosphere thickness of the NCC (Fig. 3, Zhu et al., 2011). The lith-osphere thickness beneath northwest of Hebei Province in the north-ern margin is >120 km, and the ore deposits here show characters ofa reactivated orogenic belt with broad δ34S variation range, orogeniclead isotopes, low to high mantle helium and carbon contribution,and relatively high meteoric water involvement. There are no precisedata available on the lithosphere thickness beneath the Xiaoqinlingand Xiong'ershan areas in the southern margin of the NCC, but thecontour trend shows similar lithosphere thickness around 120 km,and the characteristics of the ore deposits here are more less thesame as those of the north-western Hebei. Beneath the Jiaodong pen-insula, the lithosphere has been significantly eroded to a thickness ofabout 70–80 km. The geochemical data of the ore deposits here aresimilar with those in the southern margin and suggest reactivatedorogenic belt characteristics, suggesting a relation with the features


of deposits in the south-eastern margin. Although the northernTaihang Mountain region is located within the Trans-North ChinaOrogen in the central domain of the NCC, the ore geochemistry alsoshows reactivated orogenic features. Most of the deposits showclear meteoritic sulfur isotopic character. Compared with those inthe north-western Hebei and the southern margin, this might be re-lated with a relatively thinner lithosphere (b110 km). The litho-sphere thickness beneath the eastern Hebei and Luxi areas of thecentral NCC is about 75 to 80 km, and the deposits here showreactivated craton characters with meteoritic-like sulfur isotopes,more mantle lead, helium and carbon, and less meteoric water.

3.5.3. Metallogeny linked with plate motion and mantle plume activityEastern China became part of the Pacific margin tectonic domain

during Jurassic to Cretaceous when the tectonic system transformationwas gradually completed. This region was recognized as a continentalmargin orogenic belt by Deng et al. (2004a,b) and Goldfarb et al.(2007). Its landward boundary was the 100-km-wide, NNE-trendingN–S Gravity Lineament (NSGL, e.g., Griffin et al., 1998). The TaihangMountains are part of the cryptic NSGL in the central NCC. Althoughthe Cretaceous mineralization in the NCC was considered as a productof post-collisional orogeny from north by the Siberian block and thesouth by the Yangtze block (Chen et al., 2009b), nearly all the depositsof the early Cretaceous age are distributed on the eastern side of theNSGL, and almost all the N–S or NNE–SSW ore-controlling fracturesare characterized by early sinistral and late dextral shearing (Li et al.,1996 and authors' unpublished research reports), which is consistentwith the cessation of Jurassic shortening and onset of continent-scalenorthwest–southeast extension at ca. 130 to 120 Ma (Davis, 2003;Webb et al., 1999). A geophysical study of the E–W δvp section alongthe 37°N (Zhu et al., 2011) showed that the crust–mantle δvp structureon the east side of the NSGL was strongly disturbed with a seismicallyanomalous zone (δvp = 1%–2%), suggesting steep subduction underthe eastern part of the Japanese arc, that changed to largely horizontalbeneath the Japanese trough and terminated beneath the NSGL(Fig. 13). The highly disturbed present day crust–mantle structure canbe traced to the late Jurassic–early Cretaceous. The lithosphere thinningof the NCC is closely related with the Pacific plate subduction under theAsian plate, and the ‘staggered’ subduction is considered to have trig-gered the drastic thinning and a surge in mineralization events in theeastern NCC.

Previous studies documented changes in relative plate motionwhich suggest that prior to ca. 135 Ma, the now-extinct Izanagiplate was undergoing orthogonal convergence with the Asian conti-nental margin, whereas by ca. 115 Ma, its motion was parallel tothe margin (Maruyama et al., 1997). The rapid change in the directionof plate motion is correlated with the upwelling of the large Ontong–Java plume beneath the Pacific plate at ca. 124 Ma, causing a far-fieldinstantaneous reorganization of the plates, such that the Izanagi plate

Fig. 13. E–W δVp profile along the 37°N showing the natu

could spread to the north and was no longer pulled southwest by the“captured” Phoenix plate (Goldfarb et al., 2007).

4. Ore systems in the NCC: theoretical considerations andprospecting targets

The distribution of the major ore deposits in the NCC after the for-mation of the craton shows that the margins of the craton are themost potential domains, as these regions are more prone to be in-volved in tectonic regimes of subduction and collision and to channel-ing of ore fluids. However, before the destruction, the rigidity andlarge thickness of the NCC's lithosphere could resist relatively weakcollisions from smaller plates, and thus until the end of Paleozoic,no large scale mineralization appeared.

Theoretically, regions that are involved in multiple tectonomagmaticevents are themost potential sites forwidespreadmetallogeny. Themar-gins both in the north and south (as well as the west) of the NCC havewitnessed subduction and collision (the Siberian Plate in the north andthe Yangtze Plate in the south) from the Caledonian to Variscanian andeven to the Indosinian (Zhai et al., 1999). These major tectonic activitieswould have destabilized the craton margins, allowing deep sourcedfluids to migrate upward forming important ore deposits. Since theNCC had a thick keel with its lithosphere extending downwards formore than 200 km, the formation of ore deposits during the periodwhen the craton was stable should be confined to the accretionarybelts along the craton margins. When the east side of the NSGL becametectonically active in the Yanshanian, parts of the craton including theeastern NCC were transformed into orogenic belts (Goldfarb et al.,2007). The margins of the eastern NCC, where the Caledonian andVariscan mineralization are represented, would be areas superposed bythe Yanshanian mineral events. In addition, in the interior of the NCC,the boundaries between the basement microblocks served as weakzones along which lithospheric thinning might have occurred duringthe Yanshanian. Furthermore, trans-lithospheric faults developed alongthese boundaries and served major pathways for ore fluid migration.Thus, in addition to the margins of the craton, the regions marking theboundaries between the basement microblocks and the domains sur-rounding fault zones that mark major fluid pathways should also betargeted for future ore-prospecting.

5. Conclusions

Based on an overview of the geological, tectonic and metallogenicevents in the North China Craton, we come to the following generalconclusions.

1. At least six microblocks were amalgamated by 2.5 Ga, defining thefundamental Precambrian architecture of the North China Craton.The boundaries between the micro-blocks and the margins of theNCC remained as weak zones, which were prone for destruction

re of crust–mantle structure (after Zhu et al., 2011).

image of Fig.�13


since then. Almost all these zones record the major tectonic, mag-matic and metallogenic events, such as the mafic, alkaline andrapakivi magmatism and orogeny related gold, copper, iron andTi (rutile) metallogeny during the early to middle Proterozoic withages ranging from 2.5 to 1.8 Ma. The Early Ordovician kimberliteand diamond mineralization of ca. 480 Ma, the Late Carboniferousand Early to middle Permian calc-alkaline, I-type granitoids andgold deposits of 324–300 Ma, and the Triassic alkaline rocks andgold–silver–polymetallic deposits occur in these boundaries andmargins, correlatedwith the rise of a small mantle plume (?), south-ward subduction of the paleo Asian plate and the northward subduc-tion of the Yangtze plate, respectively. The large volume of Jurassicgranitoids and Cretaceous felsic and mafic igneous rocks and gold,molybdenum, copper, lead and zinc deposits occur in these bound-aries and margins, although most of these are concentrated in theeastern part of the NCC, related with the westward subduction ofthe Pacific Ocean plate.

2. The geodynamics of the Ordovician kimberlite and diamond miner-alization was dominated by a few rapidly rising small plumes de-rived from the deep mantle which had no effect on the basicarchitecture of the NCC. The magmatism and mineralization duringCarboniferous to Triassic were prominently caused by the subduc-tion of the Siberian plate and the Yangtze plate which led to both de-struction and accretion along the northern and southern margins ofthe NCC. Nomagmatism andmineralizationwere recorded in the in-terior of the NCC during this period, implying that the subductionfrom both the north and south might have been at high angles, andhencemost part of the NCCwas not destructed or affected. Althoughmagmatism and mineralization were recorded in the Jurassic alongthe margin and few places in the interior of the NCC, their peak oc-curred in the Cretaceous in the eastern part of the NCC, with largescale destruction of the craton. After the Cretaceous, no prominentevent occurred that affected the tectonic framework of the NCC.

3. The metallogeny of the NCC during its decratonization is character-ized by a few large and super large gold and molybdenum deposits,and minor copper, lead–zinc deposits. Although the subduction ofthe peripheral plateswas themain geodynamicmechanism, theman-tle contribution to the Cretaceous peak metallogeny, especially in theinterior of the NCC, was directly related with lithosphere thinning.Although a gradual variation in the present lithosphere thickness ofthe eastern NCC is observed from west to east, inhomogeneous thin-ning is also noticed at the junction of two or three boundaries of thebasement microblocks where cratonic thinning is most extensive.We emphasize that, in addition to the margins of the NCC, suchboundaries, especially their junction, should be focused in futureprospecting activities for ores in the NCC.

Acknowledgments

We are grateful to Prof. Franco Pirajno, Editor-in-Chief and twoanonymous referees for constructive comments and correctionswhich greatly helped in improving our paper. This work is supportedby the Key Program of National Natural Science Foundation of China(grant no. 90914002), Scheduled Program of China Geological Survey(grant no. 1212011220926), the China State Administrative Office ofOre-Prospecting Project for Critical Mines (grant nos. 200714009,20089937) and the 111 Project under the China Ministry of Education(B07011). This is a contribution to the 1000 Talent Award to M.Santosh from the Chinese Government. Our special thanks are dueto Academicians Peng-Da Zhao, Yu-Sheng Zhai and Xuan-Xue Mofor their constructive comments.

Appendix A. References for Tables 1 to 6

Supplementary data to this article can be found online at http://dx.doi.org/10.1016/j.oregeorev.2013.03.002.

References

Bai, J., Huang, X.G., Dai, F.Y., Wu, C.H., 1993. The Precambrian Evolution ofChina.Geological Publishing House, Beijing 199–203 (in Chinese with Englishabstract).

Beck, S.L., Zandt, G., 2002. The nature of orogenic crust in central Andes. J. Geophys. Res.107. http://dx.doi.org/10.1029/2000JB00012.

Bedini, R.M., Bodinier, J.L., Dautria, J.M., Morten, L., 1997. Evolution of LILE enrichedsmall melt fractions in the lithospheric mantle: a case study from the East Africarift. Earth Planet. Sci. Lett. 153, 67–83.

Bird, P., 1978. Initiation of intercontinental subduction in the Himalaya. J. Geophys. Res.83, 4975–4987.

Bird, P., 1979. Continental delamination and the Colorado Plateau. J. Geophys. Res. 84,7561–7571.

Cai, Y.C., Fan, H.R., Santosh, M., Liu, X., Hu, F.F., Yang, K.F., Lan, T.G., Yang, Y.H., Li, Y.,2012. Evolution of the lithospheric mantle beneath the southeastern North ChinaCraton: constraints from mafic dikes in the Jiaobei terrain. Gondwana Res. http://dx.doi.org/10.1016/j.gr.2012.11.013.

Chen, L., 2009. Lithospheric structure variations between the eastern and central NorthChina Craton from S- and P-receiver function migration. Phys. Earth Planet. Inter.173, 216–227.

Chen, L., 2010. Concordant structural variations from the surface to the base of theupper mantle in the North China Craton and its tectonic implications. Lithos 120,96–115.

Chen, G.Y., Shao, W., Sun, D.S., 1989. Genetic Mineralogy and Prospecting of JiaodongGold Deposits.Chongqing Publishing House, Chongqing 125–234 (in Chinese withEnglish abstract).

Chen, G.Y., Sun, D.S., Zhou, X.R., 1993. Genetic Mineralogy of the Guojialing Granodio-rite in Jiaodong and Gold Mineralization.China University of Geoscience Press,Wuhan 155–164 (in Chinese with English abstract).

Chen, Z.H., Luo, H., Mao, D.B., Shen, B.F., Lin, Y.X., 2001. The types and their geologicalcharacteristics of Early Precambrian gold deposits in Wutai Area, China. Prog.Precambrian Res. 24, 184–191 (in Chinese with English abstract).

Chen, Y.J., Pirajno, F., Sui, Y.H., 2004. Isotope geochemistry of the Tieluping silver–leaddeposit, Henan, China: a case study of orogenic silver-dominated deposits and re-lated tectonic setting. Miner. Deposita 39, 560–575.

Chen, Y.J., Chen, H.Y., Zaw, K., Pirajno, F., Zhang, Z.J., 2007. Geodynamic settings andtectonic model of skarn gold deposits in China: an overview. Ore Geol. Rev. 31,139–169.

Chen, Y.J., Pirajno, F., Qi, J.P., 2008. The Shanggong gold deposit, Eastern Qinling Orogen,China: isotope geochemistry and implications for ore genesis. J. Asian Earth Sci. 33,252–266.

Chen, Y.J., Pirajno, F., Li, N., Qi, J.P., Guo, D.S., Lai, Y., Zhang, Y.H., 2009a. Isotope system-atics and fluid inclusion studies of the Qiyugou breccia pipe-hosted gold deposit,Qinling Orogen, Henan Province, China: implications for ore genesis. Ore Geol.Rev. 35, 245–261.

Chen, Y.J., Zhai, M.G., Jiang, S.Y., 2009b. Significant achievements and open issues instudy of orogenesis and metallogenesis surrounding the North China continent.Acta Petrol. Sin. 25, 2695–2726 (in Chinese with English abstract).

Chen, H.Y., Li, S.R., Zhang, X.B., Zhang, Y.Q., Zhou, Q.F., Cui, J.C., Liu, Z.H., Song, Y.B., 2012.Wall-rock alteration and gold mineralization in the Jinqingding gold deposit,Jiaodong peninsula. Bull. Mineral. Petrol. Geochem. 31, 5–13 (in Chinese with Englishabstract).

Cheng, Y.Q., 1994. Outline of Regional Geology in China.Geological Publishing House,Beijing 1–517 (in Chinese with English abstract).

Cheng, C., Chen, L., Yao, H., Jiang, M., Wang, B., 2013. Distinct variations of crustal shearvelocity structure and radial anisotropy beneath the North China Craton and tec-tonic implications. Gondwana Res. 23, 25–38.

Chi, J.S., Lu, F.X., 1996. The Kimberlite and Paleozoic Lithospheric Mantle in theNorth China Plateform.Science Press, Beijing 1–292 (in Chinese with Englishabstract).

Dai, J.Z., Mao, J.W., Xie, G.Q., Yang, F.Q., Zhao, C.S., 2007. Ore-foming fluid characteristicsand genesis of Lajiagou moIybdenmn deposit in westem Liaoning Province. Miner.Depos. 26, 443–454 (in Chinese with English abstract).

Dai, J.Z., Mao, J.W., Zhao, C.S., Li, F.R., Wang, R.T., Xie, G.Q., Yang, F.Q., 2008. ZirconSHRIMP U–Pb age and petrogeochemical features of the Lanjiagou granite inWestern Liaoning province. Acta Geol. Sin. 82, 1555–1564 (in Chinese with En-glish abstract).

Davies, G.F., 1994. Thermomechamical erosion of the lithosphere by mantle plumes.J. Geophys. Res. 99, 15709–15722.

Davis, G.A., 2003. The Yanshan belt of North China: Tectonics, adakitic magmatism, andcrustal evolution. Earth Sci. Front. 10, 373–384.

Deng, J.F., Luo, Z.H., Su, S.G., Mo, X.X., Yu, B.S., Lai, X.Y., Zhan, H.W., 2004a. PetrologicalGenesis, Tectonic Environment andMetallogeny.Geological Publishing House, Beijing1–381 (in Chinese with English abstract).

Deng, J.F., Mo, X.X., Zhao, H.L., Wu, Z.X., Luo, Z.H., Su, S.G., 2004b. A new model for thedynamic evolution of Chinese lithosphere: continental roots plume tectonics. EarthSci. Rev. 65, 223–275.

Deng, J.F., Su, S.G., Liu, C., 2006. Discussion on the lithospheric mantle of the NorthChina craton: delamination or thermal erosion and chemical metasomatism?Earth Sci. Front. 13, 105–119 (in Chinese with English abstract).

Ding, T.P., Jiang, S.Y., 1994. Geochemistry of Silicon Isotopes.Geological PublishingHouse, Beijing 51–56 (in Chinese with English abstract).

Gao, S., Rudnick, R.L., Carlson, R.W., McDonough, W.F., Liu, Y.S., 2002. Re–Os evidencefor replacement of ancient mantle lithosphere beneath the Norh China Craton.Earth Planet. Sci. Lett. 198, 307–322.



http://dx.doi.org/10.1029/2000JB00012

http://dx.doi.org/10.1016/j.gr.2012.11.013


Gao, S., Rudnick, R.L., Xu, W.L., Yuan, H.L., Liu, Y.S., Walker, R.J., Puchtel, I.S., Liu, X.M.,Huang, H., Wang, X.R., Yang, J., 2008. Recycling deep cratonic lithosphere and gen-eration of intraplate magmatism in the North China Craton. Earth Planet. Sci. Lett.207, 41–53.

Geng, Y.S., Du, L.L., Ren, L.D., 2012. Growth and reworking of the early Precambriancontinental crust in the North China Craton: constraints from zircon Hf isotopes.Gondwana Res. 21, 517–529.

Goldfarb, R.J., Hart, C., Davis, G., Groves, D., 2007. East Asian gold: decipheringthe anomaly of Phanerozoic gold in Precambrian cratons. Econ. Geol. 102,341–345.

Griffin, W.L., Zhang, A., O'Reilly, S.Y., Ryan, C.G., 1998. Phanerozoic evolution of thelithosphere beneath the North China Craton. In: Flower, M.F.J., Chung, S.L., Lo,C.H., et al. (Eds.), Mantle Dynamics and Plate Interactions in East Asia.Geodynamics Series, 27. Am. Geophys. Union, Washington D C, pp. 107–126.

Guo, P., Santosh, M., Li, S.R., 2013. Geodynamics of gold metallogeny in the ShandongProvince, NE China: a geological and geophysical perspective. Gondwana Res.http://dx.doi.org/10.1016/j.gr.2013.02.004.

Hou, G., Santosh, M., Qian, X., Lister, G.S., Li, J.H., 2008. Tectonic constraint on the 1.3–1.2 Ga final breakup of Columbia supercontinent from a giant radiating dykeswarm. Gondwana Res. 14, 561–566.

Hu, X.D., Shen, B.F., Mao, D.B., Zhong, C.T., 2005. On metallogeny of the Caijiaying Pb–Zndeposit. Geol. Surv. Res. 28, 222–227 (in Chinese with English abstract).

Hugh, P., Taylor, J.R., 1974. The application of oxygen and hydrogen isotope studiesto problems of hydrothermal alteration and ore deposition. Econ. Geol. 69,843–883.

Ji, S.C., Wang, Q., Xu, Z.Q., 2008. Break-up of the North China Craton through litho-sphere thinning. Acta Geol. Sin. 82, 174–193 (in Chinese with English abstract).

Jia, X.M., Li, S.R., Yue, L.Q., Zhang, B., 2006. Geological features and economic signifi-cance of rutile deposit in Nianzigou, Shanxi. Geol. Prospect. 42, 42–46.

Jin, W., Li, S.X., 1996. PTt path and crustal thermodynamic model of late Archean–EarlyProterozoic high grade metamorphic terrain in North China. Acta Petrol. Sin. 12,261–275 (in Chinese with English abstract).

Kay, R.W., Kay, S.M., 1993. Delamination and delamination magmatism. Tectonophysics219, 177–189.

Kendrick, M.A., Burgess, R., Pattrick, R.A.D., Turner, G., 2001. Fluid inclusion noble gasand halogen evidence on the origin of Cu-porphyry mineralizing fluids. Geochim.Cosmochim. Acta 65, 2651–2668.

Lan, T.G., Fan, H.R., Santosh, M., Hu, F.F., Yang, K.F., Yang, Y.H., Liu, Y.S., 2012. EarlyJurassic high-K calc-alkaline and shoshonitic rocks from the Tongshi intrusivecomplex, eastern North China Craton: implication for crust–mantle interactionand post-collisional magmatism. Lithos 140–141, 183–199.

Li, S.R., 1995. A metallogenic series of crypto-explosive breccia type-dominated golddeposit. Geol. Explor. Nonferrous Met. 4, 272–277 (in Chinese with Englishabstract).

Li, S.R., Shao, K.Z., 1991. Fluid inclusion typomorphism of the Qiyugou gold deposit,Songxian county, Henan province. Geologica 5, 415–422 (in Chinese with Englishabstract).

Li, S.R., Chen, G.Y., Shao, W., Sun, D.S., 1996. Genetic Mineralogy of the Rushan GoldField, Jiaodong Peninsular.Geological Publishing House, Beijing 1–116 (in Chinesewith English abstract).

Li, J.H., He, W.Y., Qian, X.L., 1997. Genetic mechanism and tectonic setting of Proterozo-ic mafic dyke swarm: its implication to palaeo-plate reconstruction. Geol. J. ChinaUniv. 3, 2–8 (in Chinese with English abstract).

Li, Y.F., Mao, J.W., Bai, F.J., Li, J.P., He, Z.J., 2003. Re–Os isotopic dating of molybde-nites in the Nannihu molybdenum (tungsten) ore field in the eastern Qinlingand its geological significance. Geol. Rev. 49, 652–659 (in Chinese with Englishabstract).

Li, S.X., Liu, C.C., An, Y.H., Wang, W.C., Huang, T.L., Yang, C.H., 2007. Geology of Gold De-posits in Jiaodong.Geological Publishing House, Beijing 1–423 (in Chinese).

Li, H.K., Lu, S.N., Li, H.M., Sun, L.X., Xiang, Z.Q., Geng, J.Z., Zhou, H.Y., 2009. Zircon andbeddeleyite U–Pb precision dating of basic. Geol. Bull. China 28, 1396–1404 (inChinese with English abstract).

Li, C.M., Deng, J.F., Chen, L.H., Su, S.G., Li, H.M., Hu, S.L., Liu, X.M., 2010. Two periods ofzircon from Dongping gold deposit in Zhangjiakou–Xuanhua area, northern mar-gin of North China: constraints on metallogenic chronology. Miner. Depos. 29,265–275 (in Chinese with English abstract).

Li, S.R., Santosh, M., Zhang, H.F., Luo, J.Y., Zhang, J.Q., Li, C.L., Song, J.Y., Zhang, X.B., 2012.Metallogeny in response to lithospheric thinning and craton destruction: geochemis-try and U–Pb zircon chronology of the Yixingzhai gold deposit, central North ChinaCraton. Ore Geol. Rev. http://dx.doi.org/10.1016/j.oregeorev.2012.10.008.

Li, S.R., Santosh, M., Zhang, H.F., Shen, J.F., Dong, G.C., Wang, J.Z., Zhang, J.Q., 2013.Inhomogeneous lithospheric thinning in the central North China Craton: zirconU–Pb and S–He–Ar isotopic record from magmatism and metallogeny in theTaihang Mountains. Gondwana Res. 23, 141–160. http://dx.doi.org/10.1016/j.gr.2012.02.006.

Li, Q.L., Chen, F.K., Yang, J.H., Fan, H.R., 2008. Single grain pyrite Rb–Sr dating of theLinglong gold deposit, eastern China. Ore Geol. Rev. 34, 263–270.

Liu, S.B., Li, C., Cen, K., Qu, W.J., 2012. Re–Os dating for molybdenite-bearing rock samples:application in Dazhuangke molybdenum deposit in Beijing. Geoscience 26, 254–260(in Chinese with English abstract).

Lu, F.X., Zheng, J.P., Li, W.P., Zheng, Z.M., 2000. The main evolution pattern of Phanero-zoic mantle in the eastern China: the “mushroom cloud” model. Earth Sci. Front. 7,97–117 (in Chinese with English abstract).

LÜ, L.S., Mao, J.W., Li, H.B., Pirajno, F., Zhang, Z.H., Zhou, Z.H., 2011. Pyrrhotite Re–Osand SHRIMP zircon U–Pb dating of the Hongqiling Ni–Cu sulphide deposits inNortheast China. Ore Geol. Rev. 43, 106–119.

Luan, S.W., Chen, S.D., Cao, D.C., Fang, Y.K., 1991. Characteristics of the Deepseated GoldMineralization and Its Evaluational Criteria in Xiaoqingling Area.Press of ChengduUniversity of Science and Technology, Chengdu 1–180 (in Chinese with Englishabstract).

Luo, M.J., Li, S.M., Lu, X.X., Zheng, D.Q., Su, Z.B., 2000. Metallogenesis and Deposit Seriesof Main Mineral Resources of Henan Province.Geological Publishing House, Beijing1–355 (in Chinese).

Luo, H., Yu, K.R., Chen, Z.H., Tian, Y.Q., Shen, B.F., 2002. The Geology and MetallogenicPrognosis of BIF-hosted Gold Deposits in Wutaishan Area.Geological PublishingHouse, Beijing 1–147 (in Chinese with English abstract).

Luo, Z.H., Wei, Y., Xin, H.T., Ke, S., Li, W.T., Li, D.D., Huang, J.X., 2006. The Mesozoic in-traplate orogeny of the Taihang Mountains and the thinning of the continentallithosphere in North China. Earth Sci. Front. 13, 52–63 (in Chinese with Englishabstract).

Luo, W.J., Zhang, D.H., Sun, J., 2010. Geochemical charaters of mineralization rock of theSadaigoumen molybdenum deposit and their constrains on the deposit genesis inFengning, Hebei Province. Geol. Explor. 46, 491–505 (in Chinese with Englishabstract).

Ma, G.X., Chen, Z.K., Chen, L.J., 2008. Geological characteristics of the Dazhuangke mo-lybdenum deposit in Yanqing County, Beijing Municipality and further evaluationsuggestion. Hebei Geol. 1, 3–9 (in Chinese).

Mao, J.W., Goldfarb, R.J., Zhang, Z.W., Xu, W.Y., Qiu, Y.M., Deng, J., 2002. Gold deposits inthe Xiaoqinling–Xiong'ershan region, Qinling Mountains, central China. Miner.Deposita 37, 306–325.

Mao, J.W., Li, X.F., Zhang, R.H., Wang, Y.T., He, Y., Zhang, Z.H., 2005a. Mantle-derivedFluid-related Ore-forming System.China Land Publishing House, Beijing 1–365.

Mao, J.W., Xie, G.Q., Zhang, Z.H., Li, X.F., Wang, Y.T., Zhang, C.Q., Li, Y.F., 2005b. Mesozoiclarge-scale metallogenic pulses in North China and corresponding geodynamic set-tings. Acta Petrol. Sin. 21, 169–188 (in Chinese with English abstract).

Mao, J.W., Wang, Y.T., Li, H.M., Pirajno, F., Zhang, C.Q., Wang, R.T., 2008. The relation-ship of mantle-derived fluids to gold metallogenesis in the Jiaodong Peninsula:evidence from D–O–C–S isotope systematics. Ore Geol. Rev. 33, 361–381.

Mao, J.W., Pirajno, F., Cook, N., 2011. Mesozoic metallogeny in East China and corre-sponding geodynamic settings — an introduction to the special issue. Ore Geol.Rev. 43, 1–7.

Maruyama, S., Isozaki, Y., Kimura, G., Terabayashi, M., 1997. Paleogeographic maps ofthe Japanese Islands: plate tectonic synthesis from 750 Ma to the present. IslandArc 6, 121–142.

Menzies, M.A., Xu, Y.G., 1998. Geodynamics of the North China Craton in mantle dy-namics and plate interactions in East Asia. Monograph, 27. Am. Geophys Union,Washington DC, pp. 155–166.

Menzies, M.A., Fan, W.M., Zhang, M., 1993. Palaeozoic and Cenozoic lithoprobes andthe loss of >120 km of Archean lithosphere, Sino-Korean craton, China. Geol.Soc. Lond. Spec. Publ. 76, 71–81.

Molini-Velsko, C., Mayeda, T.K., Clayton, R.N., 1986. Isotopic composition of silicon inmeteorites. Geochim. Cosmochim. Acta 50, 2719–2726.

Nie, F.J., Jiang, S.H., Liu, Y., 2004. Intrusion-related gold deposits of North China craton,People's Republic of China. Resour. Geol. 54, 299–324.

Ohmoto, H., 1972. Systematics of sulfur and carbon isotopes in hydromhermal ore de-posits. Econ. Geol. 67, 551–579.

Pirajno, F., Ernst, R.E., Borisenko, A.S., Fedoseev, G., Naumov, E.A., 2009. Intraplatemagmatismin Central Asia and China and associated metallogeny. Ore Geol. Rev.35, 114–136.

Pysklywec, R.N., Beaumont, C., Fullsack, P., 2000. Modeling the behaviour of the conti-nental mantle lithosphere during plate convergence. Geology 28, 655–659.

Qing,M., Tang, M.G., Ge, L.S., Xiao, L., Han, X.J., Niu, C.W., Xia, R., 2012. Research of the Bilihegold deposit, Inner Mogolia. A Scientific Report, 1–268 (in Chinese, unpublished).

Qiu, Y.M., Groves, D.I., McNaughton, R.J., Phillips, G.N., 2002. Nature, age, and tectonicsetting of granitoid-hosted, orogenic gold deposits of the Jiaodong Peninsula, east-ern North China craton, China. Miner. Deposita 37, 283–305.

Reisberg, L., Zhi, X.C., Lorand, J.P., Wanger, C., Peng, Z.C., Zimmermann, C., 2005. Re–Osand S systematics of spinel peridotite xenoliths from east China: evidence for con-trasting effects of melt percolation. Earth Planet. Sci. Lett. 239, 286–308.

Rogers, J.J.W., Santosh, M., 2009. Tectonics and surface effects of the supercontinentColumbia. Gondwana Res. 15, 373–380.

Ruppel, C., 1995. Extensional processes in continental lithosphere. J. Geophys. Res. 100,24187–24215.

Santosh, M., 2010. Assembling North China Craton within the Columbia superconti-nent: the role of double-sided subduction. Precambrian Res. 178, 149–167.

Santosh, M., Wilde, S.A., Li, J.H., 2007. Timing of Paleoproterozoic ultrahigh tempera-ture metamorphism in the North China Craton: evidence from SHRIMP U–Pb zir-con geochronology. Precambrian Res. 159, 178–196.

Santosh, M., Maruyama, S., Yamamoto, S., 2009. The making and breaking of supercon-tinents: some speculations based on superplume, superdownwelling and the roleof tectosphere. Gondwana Res. 15, 324–341.

Santosh, M., Liu, S.J., Tsunogae, T., Li, J.H., 2012. Paleoproterozoic ultrahigh-temperature granulites in the North China Craton: implications for tectonicmodels on extreme crustal metamorphism. Precambrian Res. 222–223,77–106.

Santosh, M., Liu, D., Shi, Y., Liu, S.J., 2013. Paleoproterozoic accretionary orogenesis inthe North China Craton: a SHRIMP zircon study. Precambrian Res. 227, 29–54.http://dx.doi.org/10.1016/j.precamres.2011.11.004.

Shao, K.Z., Wang, B.D., Wu, X.G., Li, S.R., Luan, W.L., Yang, Z.S., 1992. Study ofmetallogenic condition and prospecting orientation of the explosive breccia typegold deposits in the Qiyugou region, Henan province. J. Hebei Coll. Geol. 15, 1–94(in Chinese with English abstract).





http://dx.doi.org/10.1016/j.precamres.2011.11.004


Shen, G.Y., 2011. Geological features and prospect of exploration in Sadaigoumen mo-lybdenum deposit, Hebei. Miner. Explor. 2, 493–500 (in Chinese with Englishabstract).

Shen, J.F., Santosh, M., Li, S.R., Zhang, H.F., Yin, N., Dong, G.C., Wang, Y.J., Ma, G.G., Yu,H.J., 2013. The Beiminghe skarn iron deposit, eastern China: geochronology, iso-tope geochemistry and implications for the destruction of the North China Craton.Lithos 156–159, 218–229.

Sheppard, S.M.F., 1977. The Cirnubian batholith, SW England: D/H and 18O/16O studiesof kaolinite and other alteration minerals. Geol. Soc. Lond. 133, 573–591.

Shi, G.H., Li, X.H., Li, Q.L., Chen, Z.Y., Deng, J., Liu, Y.X., Kang, Z.J., Pang, E.C., Xu, Y.J., Jia,X.M., 2012. Ion microprobe U–Pb age and Zr-in-rutile thermometry of rutilesfrom the Daixian rutile deposit in the Hengshan Mountains, Shanxi Province,China. Econ. Geol. 107, 525–535.

Tang, Z.L., Li, W.Y., 1995. Metallogenic Model and Geological Correlation of theJinchuang Copper Nickel Sulphide (with Platinum) Deposit.Geological PublishingHouse, Beijing (in Chinese with English abstract).

Tang, Y.J., Zhang, H.F., Ying, J.F., Su, B.X., Chu, Z.Y., Xiao, Y., Zhao, X.M., 2013. Highly het-erogeneous lithospheric mantle beneath the Central Zone of the North ChinaCraton evolved from Archean mantle through diverse melt fertilization. GondwanaRes. 23, 130–140.

Taylor, B.E., Bucher-Nurminen, K., 1986. Oxygen and carbon isotope and cation geo-chemistry of metasomatic carbonates and fluids—Bergell aureole, Northern Italy.Geochim. Cosmochim. Acta 50, 1267–1279.

Tolstikhin, I.N., 1978. A review: some recent advances in isotope geochemistry of lightrare gases. In: Alexander, E.C., Ozima,M. (Eds.), Terrestrial Rare Gases. Japan ScientificSociety Press, Tokyo, pp. 27–62.

Veizer, J., William, T., Holser, W.T., Wilgus, C.K., 1980. Correlation of 13C/12C and 34S/32Ssecular variations. Geochim. Cosmochim. Acta 44, 579–587.

Wang, A., Liu, Y., 2012. Neoarchean (2.5–2.8 Ga) crustal growth in the North ChinaCraton revealed by zircon Hf isotope: a synthesis. Geosci. Front. 3, 147–173.

Wang, Z.K., Jiang, X.M., Wang, Y., Shang, M.Y., 1992. A comparative analysis on geolog-ical—geochemical features of the Xiaoyingpan and Dongping gold deposits, Hebei.Geol. Explor. 28, 14–20 (in Chinese with English abstract).

Wang, L.J., Wang, J.B., Wang, Y.W., Zhu, H.P., 2003. Ore-forming fluid and metallogenyof the Caijiaying–Dajing polymetalic deposit. Sci. China D 33, 941–950 (inChinese).

Wang, B.D., Niu, S.Y., Sun, A.Q., Zhang, J.Z., 2010. Deep Sources of Ore-forming Materialsand the Metallogenesis of Mantle Branch Structure.Beijing, Geological PublishingHouse 1–256 (in Chinese with English abstract).

Wang, X., Li, S.R., Santosh, M., Gan, H.N., Sun, W.Y., 2013. Source characteristics andfluid evolution of the Beiyingxigou Pb–Ag deposit, central North China Craton: anintegrated stable isotope investigation. Ore Geol. Rev. http://dx.doi.org/10.1016/j.oregeorev.2013.02.003.

Webb, L.E., Graham, S.A., Johnson, C.L., Badarch, G., Hendrix, M.S., 1999. Occurrence,age, and implications of the Yagan–Onch Hayrhan metamorphic core complex,southern Mongolia. Geology 27, 143–146.

Wei, Y.F., Qiu, Y.S., Yu, C.T., Zheng, R.L., Li, W.K., 1993. Reseach on Gold Deposit Geologyof Eastern China.Geological Publishing House, Beijing 1–148 (in Chinese withEnglish abstract).

Wei, W.B., Ye, G.F., Jin, S., Deng, M., Jin, J.E., Peng, Z.Q., Lin, X., Song, S.L., Tang, B.S.,Qu, S.Z., Chen, K., Yang, H.W., Li, G.Q., 2008. Geoelectric structure of lithospherebeneath eastern North China: features of a thinned lithosphere frommagnetotelluric soundings. Earth Sci. Front. 15, 204–216 (in Chinese withEnglish abstract).

Wu, S.Y., 1995. Study of the Hydrothermal Chimney Materials from the Seafloor atthe Mariama Trench. Ocean Press, Beijing 1–129 (in Chinese with Englishabstract).

Wu, F.Y., Sun, D.Y., 1999. The Mesozoic magmatism and lithosphere thinning in easternChina. J. Changchun Univ. Sci. Technol. 29, 313–318 (in Chinese with Englishabstract).

Wu, J.S., Geng, Y.S., Shen, Q.H., 1998. Archaean Geology Characteristics and TectonicEvolution of Sino-Korea Paleo-continent.Geological Publishing House, Beijing192–211 (in Chinese).

Wu, F.Y., Xu, Y.G., Gao, S., Zheng, J.P., 2008. Lithospheric thinning and destruction of theNorth China Craton. Acta Petrol. Sin. 24, 1145–1174 (in Chinese).

Xu, Y.G., 1999. Roles of thermo-mechanic and chemical erosion in continental litho-spheric thinning. Bull. Mineral. Petrol. Geochem. 18, 1–5 (in Chinese with Englishabstract).

Xu, Y.G., 2001. Thermo-tectonic destruction of the Archean lithospheric keel beneaththe Sino-Korean Craton in China: evidence, timing and mechanism. Phys. Chem.Earth. 26, 747–757.

Xu, Y.G., Menzies, M.A., Vroon, P., Mercier, J.C., Lin, G.Y., 1998. Texture–temperaturegeochemistry relationships in the upper manltle as revealed from spinel peridotitexenoliths from Wangqing. J. Petrol. 39, 469–493.

Xu, Y.G., Li, H.Y., Pang, C.J., He, B., 2009. On the timing and duration of the destruction ofthe North China Craton. Chin. Sci. Bull. 54, 1974–1989 (in Chinese).

Xu, W.L., Zhou, Q.J., Pei, F.P., Yang, D.B., Gao, S., Li, Q.L., Yang, Y.H., 2013. Destruction ofthe North China Craton: delamination or thermal/chemical erosion? Mineralchemistry and oxygen isotope insights from websterite xenoliths. Gondwana Res.23, 119–129.

Yang, J.H., Wu, F.Y., 2009. Triassic magmatism and its relation to decratonization in theeastern North China Craton. Sci. China Ser. D Earth Sci. 52. http://dx.doi.org/10.1007/s11430-009-0137-5.

Yang, J.H., Wu, F.Y., Wilde, S.A., 2003. A review of geodynamic setting of large-scaleLate Mesozoic gold mineralization in the North China Craton: an association withlithospheric thinning. Ore Geol. Rev. 23, 125–152.

Yang, J.H., Sun, J.F., Chen, F.K., Wilde, S.A., Wu, F.Y., 2007. Sources and petrogenesis oflate Triassic dolerite dikes in the Liaodong Peninsula: implications for post-collisional lithosphere thinning of eastern North China Craton. J. Petrol. 48,1973–1997.

Yang, K.F., Fan, H.R., Santosh, M., Hu, F.F., Wilde, S.W., Lan, T.G., Lu, L.N., Liu, Y.S.,2012. Reactivation of the Archean lower crust: Implications for zircon geochro-nology, elemental and Sr–Nd–Hf isotopic geochemistry of late Mesozoic granit-oids from northwestern Jiaodong Terrane, the North China Craton. Lithos112–127, 146–147.

Zhai, M.G., Santosh, M., 2011. The early Precambrian odyssey of the North ChinaCraton: a synoptic overview. Gondwana Res. 20, 6–25.

Zhai, M.G., Santosh, M., 2013. Metallogeny of the North China Craton: link with secularchanges in the evolving Earth. Gondwana Res. http://dx.doi.org/10.1016/j.gr.2013.02.007.

Zhai, M.G., Guo, J.H., Yan, Y.H., Li, Y.G., Zhang, W.H., 1992. The preliminary studyand discovery of high pressure granulites in North China. Sci. China B 12,1325–1330.

Zhai, Y.S., Deng, J., Li, X.B., 1999. Regional Metallogeny. Geological Publish House, Beijing(in Chinese with English abstract).

Zhai, M.G., Bian, A.G., Zhao, T.P., 2000. The amalgamation of the supercontinent ofNorth China Craton at the end of the neoarchean and its break up during late Pro-terozoic and Mesoproterozoic. Sci. China D 43, 219–232.

Zhai, M.G., Yang, J.H., Fan, H.R., Miao, L.C., Li, Y.G., 2002. A large-scale cluster of gold de-posits and metallogenesis in the eastern North China Craton. Int. Geol. Rev. 44,458–476.

Zhai, Y.S., Peng, R.M., Xiang, Y.C., Wang, J.P., Deng, J., 2004. Methodology of RegionalMetallogeny Research. China Land Press, Beijing, pp. 1–183 (in Chinese with Englishabstract).

Zhai, M.G., Guo, J.H., Liu, W.J., 2005. Neoarchean to Paleoproterozoic continental evolu-tion and tectonic history of the North China Craton: a review. J. Asian Earth Sc. 24,547–561.

Zhang, Z.C., Chen, H.X., 1996. Geology and geochemistry of the Shuiquangouweakly alkaline complex in Horthern Hebei Province. Sci. Geol. Sin. 5,447–468.

Zhang, J.J., Jia, X.M., Chen, P., Tian, Y.Q., 2003. Metallogenic Series and Models in ShanxiProvince.Coal Industry Publishing House, Beijing 1–267 (in Chinese).

Zhang, H.F., Sun, M., Zhou, M.F., Fan, W.M., Zhou, X.H., Zhai, M.G., 2004. Highly het-erogeneous Mesozoic lithospheric mantle beneath the North China Craton: evi-dences from Sr–Nd–Pb isotopic systematics of mafic igneous rocks. Geol. Mag.141, 55–62.

Zhang, H.F., Zhou, X.H., Fan, W.M., Sun, M., Guo, F., Ying, J.F., Tang, Y.J., Zhang, J., Niu,L.F., 2005. Nature, composition, enrichment processes and its mechanism of theMesozoic lithospheric mantle beneath the southeastern North China Craton. ActaPetrol. Sin. 21, 1271–1280 (in Chinese with English abstract).

Zhang, S.H., Zhao, Y., Song, B., Yang, Z.Y., Hu, J.M., Wu, H., 2007. Carboniferous graniticplutons from the northern margin of the North China block: implications for a latePalaeozoic active continental margin. Geol. Soc. Lond. 164, 451–463.

Zhang, H.F., Goldstein, S.L., Zhou, X.H., Sun, M., Zheng, J.P., Cai, Y., 2008. Evolution ofsubcontinental lithospheric mantle beneath eastern China: Re–Os isotopic evi-dence from mantle xenoliths in Paleozoic kimberlites and Mesozoic basalts.Contrib. Mineral. Petrol. 155, 271–293.

Zhang, S.H., Zhao, Y., Yang, Z.Y., He, Z.F., Wu, H., 2009. The 1.35 Ga diabase sills from thenorthern North China Craton: implications for breakup of the Columbia (Nuna) su-percontinent. Earth Planet. Sci. Lett. 288, 588–600.

Zhang, H.F., Zhai, M.G., Santosh, M., Diwu, C.R., Li, S.R., 2011. Geochronology andpetrogenesis of Neoarchean potassic meta-granites from Huai'an Complex:implications for the evolution of the North China Craton. Gondwana Res. 20,82–105.

Zhang, H.F., Zhai, M.G., Santosh, M., Li, S.R., 2012a. Low-Al and high-Al trondhjemites inthe Huai'an Complex, North China Craton: geochemistry, zircon U–Pb and Hf iso-topes, and implications for Neoarchean crustal growth and remelting. J. AsianEart Sci. 49, 203–213.

Zhang, Z., Wu, J., Deng, Y., Teng, J., Zhang, X., Chen, Y., Panza, G., 2012b. Lateral variationof the strength of lithosphere across the eastern North China Craton: new con-straints on lithospheric disruption. Gondwana Res. 22, 1047–1057.

Zhang, H.F., Chen, L., Santosh, M., Menzies, M.A., 2013. Construction and destruction ofcratons: preface. Gondwana Res. 23, 1–3.

Zhao, Z.P., Zhai, M.G., Wang, K.Y., Yan, Y.H., Guo, J.H., Liu, Y.G., 1993. PrecambrianCrustal Evolution of Sino-Korean Paraplatform.Science Press 366–384 (inChinese).

Zhao, G.C., Sun, M., Wilde, S.A., Li, S.Z., 2005. Late Archean to Paleoproterozoic evo-lution of the North China Craton: key issues revisited. Precambrian Res. 136,177–202.

Zhao, Y.M., Wu, L.S., Rui, Z.Y., Deng, X.P., 2006. Map of the copper resources in China(1:5000000). Beijing: Geological Publishing House (in Chinese).

Zhao, Y.M., Wu, L.S., Ye, Q.T., Sheng, J.F., Deng, X.P., 2006. Map of the lead–zinc re-sources in China (1:5000000). Beijing: Geological Publishing House (in Chinese).

Zhao, G.C., Kröner, A., Wilde, S.A., Sun, M., Li, S.Z., Li, X.P., Zhang, J., Xia, X.P., He, Y.H.,2007. Lithotecton ic elements and geological e vents in the Hengshan–Wutai–Fuping belt: a synthesis and implications for the evolution of the Trans-NorthChina Orogen. Geol. Mag. 144, 753–775.

Zheng, J.P., 1999. Mesozoic–Cenozoic Mantle Replacement and Lithospheric Thinning,East China.China University of Geosciences Press, Wuhan (in Chinese).

Zhou, X.H., 2006. Major transformation of subcontinental lithosphere beneath easternChina in the Cenozoic–Mesozoic: review and prospect. Earth Sci. Front. 13, 50–64(in Chinese with English abstract).



http://dx.doi.org/10.1007/s11430-009-0137-5



414 S.-R. Li, M. Santosh / Ore Geology

Zhou, X.H., 2009. Major transformation of subcontinental lithosphere beneath NorthChina in Cenozoic–Mesozoic: revisited. Geol. J. China Univ. 15, 1–18 (in Chinesewith English abstract).

Zhu, R.X., Chen, L., Wu, F.Y., Liu, J.L., 2011. Timing, scale and mechanism of the destruc-tion of the North China Craton. Sci. China Earth Sci. 54, 789–797.

Sheng-Rong Li is Professor at the China University ofGeosciences Beijing (China). B.Sc. (1981) from Hebei Insti-tute of Geology, Visiting scholar (1986) from GeologicalSurvey of India Traning Institute, D.Sc. (1992) from ChinaUniversity of Geosciences Beijing, and Postdoctorial fellow(1994) from Institute of Geochemistry, Chinese Academyof Sciences. Research fields include genetic mineralogy,petrology, geochemistry and ecomomic geology. Publishedover 200 research papers and several monographs andtextbook. Recipient of Beijing Municipality OutstandingTeacher Award.

M. Santosh is Professor at the China University ofGeosciences Beijing (China) and Emeritus Professor atthe Faculty of Science, Kochi University, Japan. B.Sc.(1978) from Kerala University, M.Sc. (1981) from Uni-versity of Roorkee, Ph.D. (1986) from Cochin Universityof Science and Technology, D.Sc. (1990) from Osaka CityUniversity and D.Sc. (2012) from University of Pretoria.Founding Editor of Gondwana Research as well as thefounding Secretary General of the International Associa-tion for Gondwana Research. Research fields include pe-trology, fluid inclusions, geochemistry, geochronologyand supercontinent tectonics. Published over 350 re-search papers, edited several memoir volumes and jour-

Reviews 56 (2014) 376–414

nal special issues, and co-author of the book ‘Continentsand Supercontinents’ (Oxford University Press, 2004). Recipient of National Miner-al Award, Outstanding Geologist Award, Thomson Reuters 2012 Research FrontAward, Global Talent Award.

Unlabelled image

Unlabelled image

Documents

Ore Geology Reviews - Cugb...Tectonics The link between metallogeny and craton destruction in the North China Craton (NCC) remains poorly under-stood, particularly the mechanisms within