A review of the geological characteristics and geodynamic setting of the late Early Cretaceous molybdenum deposits in the East Qinling–Dabie molybdenum belt, East China

Accepted Manuscript A review of the geological characteristics and geodynamic setting of the late Early Cretaceous molybdenum deposits in the East Qinling–Dabie molybdenum belt, East China Yang Gao, Jingwen Mao, Huishou Ye, Fang Meng, Yongfeng Li PII: DOI: Reference:

S1367-9120(15)00234-5 http://dx.doi.org/10.1016/j.jseaes.2015.04.025 JAES 2354

To appear in:

Journal of Asian Earth Sciences

Received Date: Revised Date: Accepted Date:

8 November 2014 10 April 2015 14 April 2015

Please cite this article as: Gao, Y., Mao, J., Ye, H., Meng, F., Li, Y., A review of the geological characteristics and geodynamic setting of the late Early Cretaceous molybdenum deposits in the East Qinling–Dabie molybdenum belt, East China, Journal of Asian Earth Sciences (2015), doi: http://dx.doi.org/10.1016/j.jseaes.2015.04.025

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A review of the geological characteristics and geodynamic setting of the late Early Cretaceous molybdenum deposits in the East Qinling–Dabie molybdenum belt, East China

Yang Gaoa*, Jingwen Maob, Huishou Yeb, Fang Mengc, Yongfeng Lid

a

College of Earth Sciences, Jilin University, Changchun 130061, China

b

MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral

Resources, Chinese Academy of Geological Sciences, Beijing 100037, China c

School of Jewelry, China University of Geosciences, Beijing 100083, China

d

Henan Provincial Non–ferrous Metals Geological and Mineral Resources Bureau,

Zhengzhou 450016, China

*Corresponding author: Yang Gao, College of Earth Sciences, Jilin University, No. 2199 Jianshe Street, Changchun 130061, China, E–mail: [email protected]

Abstract The East Qinling–Dabie molybdenum belt, which is located in the nearly east–west trending Qinling–Dabie orogen, East China, is the largest Mo belt in the world and is characterized by extensive Mesozoic mineralization. Although the late Early Cretaceous (ca. 120–100 Ma) is the latest stage of the Mo mineralization in the East Qinling–Dabie Mo belt, this period shows relatively intensive Mo mineralization, such as the world–class Shapinggou Mo deposit. All of the late Early Cretaceous Mo deposits are closely related to granitic magmatism, some of which are typical porphyry–type deposits (e.g., Donggou, Tangjiaping, Shapinggou). Homogenization temperatures of fluid inclusions in the late Early Cretaceous Mo deposits range from 115 to 550℃, with salinities ranging from 0.02 to 62.1 wt % NaCl equivalent. Different amount of CO2 have been recognized in the hydrothermal systems of these Mo deposits, indicating H2O–NaCl–CO2 systems. The ore–forming fluids in these Mo deposits were magmatic water mixed with different amount of meteoric water. Except the Donggou deposit, the δ34S values of sulfides from the late Early Cretaceous Mo deposits have a narrow range of 0.4 to 6.3 ‰, suggesting a deep magmatic source for the sulfur. The Donggou Mo deposit has slightly higher δ34S values (7.5 to 9.4‰), reflecting that the ore sulfur was mainly derived from magma, probably with some upper crust materials. Available isotopic data show that the ore–associated magmas of the late Early Cretaceous Mo deposits were mainly derived from crustal materials, probably with some contribution of mantle or newly added crust. The Donggou, Tangjiaping, and Shapinggou Mo deposits are genetically related to A–type magmatism, suggesting that they formed in an extensional setting. The late Early Cretaceous Mo deposits in the East Qinling–Dabie Mo belt formed in an intraplate extensional setting accompanied by the lithospheric thinning and asthenospheric

upwelling. Keywords: Late Early Cretaceous Mo deposits; Geological characteristics; Tectonic setting; East Qinling–Dabie Mo belt; East China

1. Introduction A large amount of Mesozoic ore deposits formed the giant East China Mesozoic metallogenic province (Mao et al., 2011a). The formation of these deposits is coeval with the large–scale Mesozoic tectono–magmatic events in East China. The East Qinling–Dabie molybdenum belt, which is a part of the East China Mesozoic metallogenic province, is located in the nearly east–west trending Qinling–Dabie orogen. The East Qinling–Dabie Mo belt is the largest Mo ore district in the world (Mao et al., 2011b). This belt has been the most important Mo producer in China since the 1950’s. A series of super–large Mo deposits (including Jinduicheng, Nannihu–Sandaozhuang, Shangfanggou) have been discovered from the 1950’s to 1980’s. During the last thirty years, research on Mo deposits and related granitoids in the East Qinling–Dabie Mo belt has achieved progress and focused on geology and ages of ore deposits (e.g., Gao et al., 2010; Guo et al., 2006; Huang et al., 1987; Li et al., 2003; Stein et al., 1997; Zhou et al., 2009), fluid inclusion and stable isotope systematics (e.g., Chen et al., 2014; Gao et al., 2013; Huang et al., 1984, 1985; Li et al., 2009b; Liu and Sun, 1989; Yang et al., 2009), and ages and sources of ore–associated granitoids (e.g., Li et al., 2006; Nie, 1994; Yan et al., 1986; Yang et al., 2013; Ye et al., 2008; Zhao et al., 2010). Although a few pre–Mesozoic Mo deposits have been reported (e.g., Li et al., 2009a; Wei et al., 2009), most important Mo mineralization in the East Qinling–Dabie Mo belt is confined to Mesozoic (Mao et al., 2008, 2011b). Especially, a large number

of significant porphyry Mo deposits formed in Jurassic-Cretaceous (e.g., Huang et al., 2011; Li et al., 2003; Ye et al., 2008). Therefore, the late Mesozoic tectono–magmatic events have a decisive significance to the Mo mineralization in the East Qinling–Dabie Mo belt. However, the tectonic regimes related to the late Mesozoic Mo mineralization remains controversial. Li et al. (2007) argued that the Late Jurassic to Early Cretaceous Mo deposits and related porphyries in the East Qinling area formed in continental collision regimes. However, most geologists proposed that the East Qinling–Dabie area was in an intraplate regime in late Mesozoic, which was closely related to the evolution of the Izanagi (or Paleopacific) Plate (e.g., Li et al., 2005; Lu et al., 2002; Mao et al., 2008; Zhu et al., 2008). In the East Qinling–Dabie Mo belt, extensive Mesozoic magmatism–mineralization obviously weakened or even finished in late Early Cretaceous (ca. 120–100 Ma). Although late Early Cretaceous is the latest stage of the tectono–magmatic–metallogenic process in the East Qinling–Dabie Mo belt, this period shows relatively intensive Mo mineralization (e.g., Yang, 2007a; Ye et al., 2008; Zhang et al., 2014). The Mo deposits formed in late Early Cretaceous provide at least 3 Mt Mo metal. The discuss of genesis and geodynamic setting of late Early Cretaceous Mo deposits (mainly including the Donggou,

Nangou,

Saozhoupo,

Donggoukou,

Laojieling,

Tangjiaping,

and

Shapinggou Mo deposits) in the East Qinling-Dabie Mo belt is significant to understand the Mesozoic mineralization process and metallogenic regularity. On the basis of previous studies and combined with our study, we describe and review the geological and geochemical characteristics of the late Early Cretaceous Mo deposits and Mo–related magmas in the East Qinling–Dabie Mo belt. Then we consider and discuss the geodynamic setting within which these deposits developed.

2. Geological setting The geology and tectonic evolution of the Qinling–Dabie orogen have been extensively described (e.g., Hacker et al., 1996; Meng and Zhang, 2000; Ratschbacher et al., 2003; Zhang et al., 1996, 2001). It formed by two collision events during Early Silurian and Late Triassic (Ames et al., 1993; Hacker et al., 1996; Kröner et al., 1993). The Shangdan suture is generally considered to have formed following subduction of the Shangdan Ocean and multistage accretion of the South Qinling to the North Qinling (Ratschbacher et al., 2003; Zhang et al., 2001). The Mianlue suture represents the Triassic collision belt between the South Qinling and the Yangtze Craton (Zhang et al., 2001). The East Qinling–Dabie orogenic belt (Fig. 1) is part of the 2000 km long Qinling–Dabie orogen and could be further divided by the Nanyang basin into the East Qinling and Dabie orogens. The dominant structures in the East Qinling–Dabie orogenic belt are WNW-trending faults, secondly for NW-trending faults. The intersection of these two trending of faults usually controlled the distribution of the late Mesozoic intermediate-felsic stocks and related Mo deposits. In the East Qinling orogen, four tectonic units can be recognized from north to south: the southern margin of the North China Craton, the North Qinling, the South Qinling, and the northern margin of the Yangtze Craton. The Luanchuan, Shangdan, and Mianlue faults (sutures) define the boundaries among the four tectonic units from north to south. Mo deposits in the East Qinling orogen are present in the southern margin of the North China Craton and the North Qinling. The basement of the southern margin of the North China Craton comprises gneiss, granulite and migmatite of the Late Archaean Taihua Group (Zhang et al., 2001). These rocks are discomformably overlain by mafic–intermediate to felsic volcanic rocks of the Mesoproterozoic Xiong’er Group (Peng et al., 2008; Pirajno et al., 2009), which is

overlain by the Mesoproterozoic Guandaokou Group littoral clastic and carbonate rocks, and the Neoproterozoic Luanchuan Group shallow–sea facies clastic and carbonate rocks. The carbonate rocks of Guandaokou and Luanchuan Groups were critical to the formation of the skarn Mo mineralization in some important porphyry-skarn Mo deposits (e.g., Li et al., 2003; Yang et al., 2009). Cambrian and Lower Ordovician strata in this unit belong to the sedimentary platform cover succession of the North China Craton (Zhang et al., 2001). Upper Ordovician to Lower Carboniferous strata are absent from this region. Middle–Upper Carboniferous terrigenous clastic rocks intercalated with marine carbonate rocks and coal seams overlain by Permian coal seam–bearing terrigenous clastic rocks. Triassic, Jurassic, and Cretaceous sediments are locally present (Mao et al., 2008 and references therein). In the North Qinling, the Qinling Group occurs along the Shangdan suture, consisting of

biotite–plagioclase

gneiss,

biotite–amphibole–plagioclase

gneiss,

two

feldspar–granulites, and graphitic marbles. Ultrahigh–pressure (UHP) metamorphic eclogite and high–pressure granulites occur in its northern and southern margins, respectively (Chen et al., 2004; Yang et al., 2005). The Erlangping Group distributes to the north of the Qinling Group, comprising an early Paleozoic ophiolitic suite and volcanic–sedimentary rocks (Sun et al., 1996). To the north of the Erlangping Group is the Kuanping Group, composed of middle–low grade metamorphosed greenschist and amphibolite rocks (Zhang et al., 1994a). In addition, the minor amounts of Lower Paleozoic and Triassic marine clastic rocks and carbonates are also present in the North Qinling. The Dabie orogen is bounded by the Nanyang basin and the Tancheng–Lujiang Fault to the west and east, respectively. It is further divided by the Shangcheng–Macheng Fault into eastern and western parts. The eastern Dabie orogen

can be divided into four units with the Xiaotian–Mozitan, Wuhe–Shuihou, and Taihu–Mamiao faults from north to south: (1) The North Huaiyang zone (NHZ), consisting of a low–grade metamorphic terrane detached from the subducting crust of the YC (Zheng et al., 2005), the protoliths of which have zircon ages of 700–800 Ma (Hacker et al., 2004); (2) The Northern Dabie zone (NDZ) mainly comprises large–scale Cretaceous granitic and minor mafic–ultramafic intrusive rocks, Neoproterozoic tonalite–trondhjemite–granodiorite orthogneisses and amphibolites, and Triassic high–temperature eclogites (Bryant et al., 2004; Hacker et al., 2000; Zheng et al., 2003); (3) The Southern Dabie zone (SDZ) mainly comprises eclogites, garnet–bearing peridotites, jadeite quartzites, marble, garnet–mica schists, and gneisses (Hacker et al., 2000); (4) The Susong high pressure metamorphic zone (SHPZ) consists mainly of Meso– to Neoproterozoic metasedimentary and metavolcanic rocks, and Sinian marbles (You et al., 1996). The western Dabie consists of tectonic units similar to those in the eastern Dabie, but lacks a middle unit similar to the NDZ, which is suggested due to stronger Cretaceous (~140–120 Ma) NW–SE extension in the Dabie orogen (Hacker et al., 2000). The Mo deposits in the Dabie orogen formed a WNW-trending belt and distributed in the North Huaiyang zone and its adjacent areas. Six pulses of granitoid magmatism in the East Qinling–Dabie orogen have been recognized (Lu, 1999 and references therein): Late Archaean (2.9–2.5 Ga) tonalite–trondhijemite–granodiorite, Early Proterozoic (2.0–1.6 Ga) A–type granites, Late Proterozoic (1.1–0.8 Ga) and Early Paleozoic (600–420 Ma) subduction–, collision– and post–collision related granites, and Mesozoic granite emplacement. The Mesozoic, especially during the Jurassic to Cretaceous, is the most significant period for granitoid emplacement in the East Qinling–Dabie belt. The late Mesozoic

Mo mineralization in the East Qinling–Dabie Mo belt is temporally–spatially related to the contemporaneous intermediate–felsic magmatism in the region (e.g., Mao et al., 2010; Li et al., 2013). The ore-associated porphyries of the majority of porphyry (-skarn) type Mo deposits are the products of the magmatism. Additionally, several Mo deposits (such as the Saozhoupo and Zhuyuangou Mo deposits) are related to emplacement of granite batholith, which also formed during the late Mesozoic magmatism in the belt. 3. Geological features of Molybdenum deposits The principal geological characteristics of the late Early Cretaceous Mo deposits in the East Qinling–Dabie Mo belt are summarized in Table 1. The geological characteristics of the representative Mo deposits (Donggou, Saozhoupo, Tangjiaping, and Shapinggou) are described below. 3.1 Donggou Mo deposit The Donggou Mo deposit (112°22′~112°23′E, 33°56′30″~33°57′30″N) is located in Ruyang County, Henan Province. It was discovered by No. 2 Team of Henan Bureau of Geology and Mineral Resources in 1984 and was explored in 2005, which resulted in a resource estimation of 62.5×104t of Mo at a grade of 0.113% (Ye et al., 2006). The ore district is located on the southern limb of the Bocaiping anticline. The Donggou porphyry–type Mo deposit is surrounded by several hydrothermal vein–type Pb–Zn deposits (Fig. 2). The rocks exposed in the Donggou Mo ore district are mainly rhyolite and andesite intercalated with basalt and tuffaceous siltstone of Mesoproterozoic Xiong’er Group (Fig. 3). There are four groups of faults (EW–, NW–, NE–, and NS–trending) have been recognized in the ore district. Intrusive rocks in the Donggou Mo deposit are the ore–associated granite porphyry and Mesoproterozoic dioritic dikes, which intruded into Mesoproterozoic Xiong’er Group

volcanic rocks. The Donggou granite porphyry has a surface outcrop area of only ca. 0.01 km2. It is composed of phenocrysts of quartz, plagioclase, and K–feldspar, set in a groundmass of quartz, plagioclase, perthite, and K–feldspar with minor amounts of biotite and accessory minerals of magnetite, sphene, zircon, and rutile. The Donggou porphyry was dated by Ye et al. (2006) at 112±1 Ma, Dai et al. (2009) at 114–117 Ma, and Yang et al. (2013) at 117–118 Ma. Mo Mineralization was developed mainly within the Xiong’er Group volcanic rocks above the Donggou granite porphyry, whereas minor mineralization also took place in the roof zone of the granite porphyry (Fig. 4). The main orebody has a tabular shape and is situated over the porphyry. The thickness of the orebody ranges from 46.60 to 253.92 m, with an average value of 189.76 m. The Mo mineralization is dominantly hosted in Mo–bearing quartz veinlets and stockworks, with minor disseminated mineralization distributed locally. Ore minerals mainly include molybdenite, pyrite, chalcopyrite, galena, sphalerite and scheelite. Gangue minerals are mainly Quartz, K–feldspar, plagioclase, clinopyroxene, hornblende, biotite, chlorite, epidote, sericite, and fluorite. Wall rock alteration in the Donggou deposit is well developed in both the porphyry and the Xiong’er Group volcanic rocks. The alteration minerals mainly include quartz, K–feldspar, and biotite, with minor sericite, chlorite, fluorite, and carbonate. Four mineralization stages have been recognized in the Donggou deposit (Ye et al., 2006). Stage I is characterized by quartz + K–feldspar veins and barren K–feldspar veins, with no molybdenite; Stage II is characterized by the assemblage of quartz + K–feldspar + molybdenite; Stage III is characterized by quartz + molybdenite + polymetal sulfides veins; Stage IV is characterized by calcite veins that crosscut Mo–bearing veins. The mineralization age of the Donggou deposit has been

constrained by Ye et al. (2006) at 116 ± 1.7 Ma by molybdenite Re–Os dating. 3.2 Saozhoupo Mo deposit The Saozhoupo Mo deposit (111°18′~111°20′E, 33°48′~33°50′N), located in Luanchuan County, Henan Province, is a newly discovered Mo deposit in the East Qinling–Dabie Mo belt. The deposit is situated at the western margin of the 394 km2 Laojunshan granite batholith, which is located at the southern side of the Luanchuan fault. In addition to spatial relationship, the mineralization ages of the Saozhoupo, as well as the Donggoukou and Laojieling Mo deposits all coincide with the age of the Laojunshan granite batholith (Meng et al., 2012a, b). The temporal–spatial relationship of the Saozhoupo, Donggoukou, and Laojieling Mo deposits with the Laojunshan granite batholith is comparable with the Yuchiling and Zhuyuangou Mo deposits, which are spatially and temporally associated with the Heyu batholith and the Taishanmiao batholith, respectively, in the East Qinling–Dabie Mo belt (Huang et al., 2010; Li et al., 2012; Zhou et al., 2009). The rocks exposed in the Saozhoupo deposit include Meso–Neoproterozoic Kuanping Group two–mica quartz schist, biotite quartz schist, sericite quartz schist, with minor amphibole quartz schist (Fig. 5). Several small faults exist in the ore district, including SN–, NE–, and NW–trending ones. The magmatic rocks in the Saozhoupo deposit are mainly phase 3 porphyraceous monzogranite of the Laojunshan granite batholith. The monzogranite contains 5%–7% K–feldspar phenocrysts. The matrix has a coarse granular (2–6 mm) texture and consists of K–feldspar, quartz, plagioclase, and biotite. Accessory minerals include magnetite, ilmenite, apatite, zircon, and titanite. In addition, there is also an amphibolite dyke in the ore district, with molybdenite and pyrite distributed in the dyke locally. Mo Mineralization in the Saozhoupo Mo deposit was developed within the

Laojunshan granite and the two–mica quartz schist in the external contact zone. Three Mo orebodies have been recognized in the ore district, length and thickness of which are 90–210m and 3.60–22.42m, respectively. The orebodies occur as lenses and irregular veins. The ore types in the deposit are represented by molybdenite–bearing veins, stockwork ores, and small amount of disseminated molybdenite ores. Ore minerals are mainly molybdenite and pyrite, with minor magnetite and limonite. Gangue minerals are mainly Quartz, K–feldspar, plagioclase, biotite, muscovite, sericite, hornblende, and chlorite. Hydrothermal alteration minerals closely related to Mo mineralization include quartz, K–feldspar, pyrite, and sericite. Three mineralization stages have been recognized in the Saozhoupo Mo deposit by Meng et al. (2012b): (1) Stage I is characterized by barren quartz veins, with rare molybdenite locally; (2) Stage II is the molybdenite deposition stage, which is characterized by quartz + molybdenite ± pyrite stockworks and veinlets; (3) Stage III is characterized by quartz + pyrite veins. Meng et al. (2012b) obtained molybdenite ages of the Saozhoupo, Donggoukou, and Laojieling Mo deposits, ranging from 109.8 ± 1.6 to 114.5 ± 1.7 Ma, which are consist with the age of the Laojunshan granite batholith (Meng et al., 2012a). 3.3 Tangjiaping Mo deposit The Tangjiaping Mo deposit is the first large–scale metal deposit discovered in the Dabie orogen. It was explored by the No. 3 Party of Geological Survey of Henan Province in 2004, resulting in a resource of 23.5×104 t Mo metal, grading at 0.063% (Wang et al., 2009; Yang, 2007a). The Tangjiaping Mo deposit (115°19′~115°20′E, 31°31′~31°32′N) is located in Shangcheng County, Henan Province. The strata outcropped in the ore district are mainly Proterozoic biotite–plagioclase gneiss and amphibole–plagioclase gneiss (Fig. 6a). Structures related to mineralization are faults

associated with the porphyry system. The ore–hosting Tangjiaping granite porphyry is ca. 0.4 km2. It shows porphyritic texture and contains about 10 to 20 vol. % phenocrysts which consist of K–feldspar, plagioclase, quartz, and biotite. Its fine–grained matrix is composed of similar minerals as phenocrysts. Accessory minerals (<1 vol. %) include zircon, titanite, apatite, and Fe–Ti oxides. Hornblende andesite enclaves are locally distributed in the stock. The contact between porphyry and enclaves is sharp. These enclaves are generally several centimeters to twenty centimeters in diameter, and are generally angular–subangular in shape. The enclaves show a porphyritic texture with 5 to 10 vol. % phenocrysts of predominant plagioclase and minor hornblende, K–feldspar, quartz, and biotite. The matrix consists of micro–granular plagioclase, quartz, K–feldspar, and biotite. Accessory minerals are magnetite and apatite. Zircon U–Pb dating constrains the timing of crystallization of the Tangjiaping granite porphyry to 121.6±4.6 Ma (Wei et al., 2010). Mo mineralization in the Tangjiaping deposit is hosted in the granite porphyry and its contact zones (Fig. 6b). The main orebody define an area of mineralized rocks approximately 1760 × 960 m, with an average thickness of 125.8 m, and dips southwestward at an angle of about 20°. Supergene oxide zones are developed locally, with thicknesses of about 20 m. Overall, the Mo mineralization is more strongly developed in the central part of the stock and decreases outward and downward. There is no significant post–mineralization faults and dike in the orebody. Molybdenite is dominantly hosted in Mo–bearing quartz veinlets and stockworks, with minor disseminated mineralization distributed in the porphyry locally. The main ore minerals comprise molybdenite and pyrite, with minor chalcopyrite, magnetite, galena, sphalerite, and hematite. Gangue minerals include quartz, sericite, muscovite, calcite, plagioclase, biotite, chlorite, and epidote.

Wall rock alteration in the Tangjiaping Mo deposit can be divided into two zones from the center to the periphery: (1) K–silicate alteration–silicification zone, occurring in the center part of the porphyry and is characterized by assemblage of K–feldspar–quartz ± biotite ± magnetite. This zone is associated with the highest Mo grades; (2) silicification–phyllic alteration zone, developed outside of the first zone, with the related minerals of sericite, quartz, pyrite, and minor calcite. Along the contact zone between the country rock and the stock, the Proterozoic gneiss underwent propylitic alteration, leading to the formation of secondary chlorite. Wang et al. (2009) recognized three stages of mineralization: (1) Stage I is characterized by the mineral assemblage of quartz, K–feldspar, magnetite, pyrite, and minor molybdenite. The granite underwent K–feldspar alteration, silicification, and weak sericitization during this stage; (2) Stage II is the main molybdenite deposition stage, which is characterized by the mineral assemblage of quartz, sericite, muscovite, molybdenite, pyrite, and minor galena and chalcopyrite. The alteration types are mainly silicification and phyllic alteration in this stage. (3) Stage III is characterized by quartz + calcite + pyrite veins or calcite veins. The Re–Os isochron age of molybdenite is 113.1 ± 7.9 Ma (Yang, 2007b), indicating that the mineralization is coeval with the Early Cretaceous igneous activity. 3.4 Shapinggou Mo deposit The Shapinggou Mo deposit in Jinzhai County, Henan Province is located in the eastern part of the Yinshan complex, which intruded into the North Huaiyang zone, Dabie orogen. The Yinshan complex has a surface outcrop area of ca. 2.76 km2, consisting of quartz syenite (porphyry), biotite syenite, breccia, syenite porphyry, granite porphyry, and quartz trachyte (Huang et al., 2011; Zhang et al., 2010a). In addition to Mo mineralization, several Pb–Zn deposits are also present in the Yinshan

region, including Hongjiadashan, Gaijing, Cangfang, and Dayinshan (Fig. 7) (Zhang et al., 2010a). Huang et al. (2011) obtained molybdenite Re–Os ages of 112.2 ± 1.7~113.9 ± 1.7 Ma for the Shapinggou Mo deposit. The Shapinggou Mo deposit is the largest Mo deposit in the East Qinling–Dabie Mo belt and China, with proven of 214.06×104 t of Mo at a grade of 0.179% (Zhang et al., 2012). It was discovered in 2006 by following up the geochemical anomaly of Mo–Pb–Zn–Ag selected during geological survey at a scale of 1: 500,000 performed by No. 313 Geological Team of Anhui Bureau of Geology, Mineral Resources and Development (Zhang et al., 2010a, b). The strata in the ore district mainly consist of the Neoproterozoic Luzhenguan Group gneiss, which exposed in western and northern parts of the ore district. Faults are well developed in the ore district and at least two groups of faults can be distinguished: NE–trending and NW–trending faults, which controlled the development of Pb, Zn, Ag ore veins at the surface (Zhang et al., 2012). Mesozoic intrusive rocks are widely developed in the ore district and mainly include quartz monzonite, syenogranite, early granite porphyry, quartz monzonite porphyry, monzogranite, biotite diorite, biotite monzonite, quartz syenite, and late concealed Mo–associated granite porphyry. Wang et al. (2014) identified that granitoids in the Shapinggou ore district formed during an interval of ca. 138–114 Ma. The Mo–associated porphyry yielded zircon U–Pb age of 114 ± 1 Ma, which is consist with the molybdenite Re–Os isochron age of 113.2 ± 0.5 Ma (Huang et al., 2011). The main Mo orebody has an irregular ellipse–shape (Fig. 8) and is 1350 m long in E–W direction and 1000 m wide, with an average thickness of 661.32m (Zhang et al., 2012). The Mo mineralization is characterized by stockwork, which developed in the Mo–associated granite porphyry and the quartz syenite in the external contact

zone. Ore minerals mainly include molybdenite, pyrite, with minor magnetite, ilmenite, and galena. Gangue minerals are mainly K–feldspar, Quartz, and plagioclase, with minor sericite, biotite, muscovite, fluorite, gypsum, and calcite. Four main mineral assemblages have been recognized by Zhang et al. (2010a, b) comprising quartz – Kfeldspar – molybdenite – magnetite – pyrite, quartz – molybdenite – pyrite, quartz – chalcopyrite – sphalerite – galena – pyrite – molybdenite and quartz – molybdenite – fluorite. Wall rock alteration in the Shapinggou deposit is extensive and shows a well–defined alteration zoning of K–feldspar–quartz, pyrite–sericite–quartz, and chlorite–calcite from center outward (Zhang et al., 2010b). Quartz and K–feldspar are the most important alteration minerals related to Mo mineralization. Zhang et al. (2012) recognized five main mineralization stages: post–magma metasomatism stage (stage

I);

quartz–K–feldspar–molybdenite

stage

(stage

II);

quartz–sericite–molybdenite stage (stage III); quartz–sericite–pyrite stage (stage IV); quartz–fluorite–gypsum stage (stage V). Of these mineralization stages only stages 2 and 3 are responsible for Mo mineralization. 4. Characteristics of ore–forming fluids and sulfur isotope 4.1 Characteristics of ore–forming fluids Homogenization temperatures and salinities of fluid inclusions, as well as δ34S values of sulfides from the late Early Cretaceous porphyry Mo deposits in the East Qinling–Dabie Mo belt are summarized in Table 2. The previous studies of fluid inclusions indicate a wide range of homogenization temperatures from 115 to 550℃ and salinities ranging from 0.02 to 62.1 wt % NaCl equivalent. Salinities of the ore–forming fluids of the Donggou and Shapinggou deposits are highly varied: the low to medium salinities vary from 0.02 to 19.3 wt.% NaCl equivalent; the high

salinities vary from 31.71 to 50.85 wt.% NaCl equivalent (Yang et al., 2011; Yu et al., 2012). In contrast, the salinities of the ore–forming fluids of the Saozhoupo, Laojieling, and Donggoukou Mo deposits are relatively low, ranging from 0.35 to 16.24 wt.% NaCl equivalent (Meng et al., 2012b). Yang et al. (2011) suggested that the ore–forming fluids of the Donggou Mo deposit evolved from high temperature, CO2–bearing magmatic fluid to low temperature, CO2–poor meteric fluid. As for the Tangjiaping and Shapinggou porphyry Mo deposits, fluid–boiling was a very important mechanism for precipitation of the ore–forming materials (Wang et al., 2009; Yu et al., 2012). In addition, Wang et al. (2009) observed daughter mineral–bearing CO2–H2O fluid inclusions in the early and middle stages quartz from the Tangjiaping Mo deposit, which were rarely reported in previous studies of porphyry deposits. Overall, the temperatures and salinities of the ore–forming fluids decreased from early to late mineralization stage of these Mo deposits (Meng et al., 2012b; Wang et al., 2009; Yang et al., 2011; Yu et al., 2012). Notably, different amounts of CO2–bearing fluid inclusions have been recognized in these Mo deposits, suggestive of H2O–NaCl–CO2 system fluids. The δD values of the ore–forming fluids of these deposits are between -108 and -58 ‰, with the δ18Ofluid values varying from -3.18 to 7.5 ‰ (Table 2). In the δD vs. δ18Ofluid diagram (Fig. 9), the data points of the deposits are between the magmatic water field and the meteoric water line, indicating a different amount of meteoric water that input into the fluid systems (e.g., Meng et al., 2012b). The data plots of the Shapinggou, Tangjiaping and Donggou deposits are relatively close to the primary magmatic water field than those of the Saozhoupo, Laojieling, and Donggoukou deposits, suggesting a greater proportion of the magmatic water involved in the Mo

mineralization. To summarize, the ore–forming fluids in these Mo deposits were magmatic water mixed with different amount of meteoric water. 4.2 source of sulfur 48 δ34S values of sulfide samples (one is sphalerite sample, others are molybdenite and pyrite samples) from the late Early Cretaceous Mo deposits have been summarized in Table 2 and Fig. 10. The δ34S values of sulfide samples from the Donggou Mo deposit have a narrow range between 7.5 and 9.4 ‰, with a peak value of 8.6 ‰. The δ34S values of sulfide samples from the Saozhoupo, Laojieling, and Donggoukou Mo deposits vary from 3.4 to 6.3 ‰, 3.6 ‰, and 2.4 to 4.6 ‰, with peak values as 4.5 ‰, 3.6 ‰, and 3.5 ‰, respectively. The δ34S values of sulfide samples from the Tangjiaping Mo deposit range from 0.4 to 4.1 ‰, with a peak value of 2.3 ‰. The δ34S values of sulfides from the Shapinggou Mo deposit vary between 2.1 and 5.9 ‰, with a peak value of 3.8 ‰. In these Mo deposits, sulfur dominantly exists in sulfides, and the δ34S values of sulfides from these deposits are uniform, indicating no sulfur fractionation. Therefore, the average δ34S value could represent the δ34S∑S of the ore–forming system. Based on comparison, Mao et al. (2011b) proposed that sulfur of Jurassic–Cretaceous Mo deposits in the East Qinling–Dabie Mo belt have similar isotopic compositions, and was possibly derived from granitic magma. As mentioned above, the sulfides from the Saozhoupo, Laojieling, Donggoukou, Tangjiaping, and Shapinggou Mo deposits exhibit relatively low positive δ34S values, indicating a deep magmatic source for the sulfur. This is comparable with Mo deposits developed in other areas (e.g., Liu et al., 2014; Shelton et al., 1986). Although the sulfides from the Donggou Mo deposit have slightly higher δ34S values (the peak value of 8.6‰) than those of other late Early Cretaceous Mo deposits, its sulfur

isotopic characteristic is analogous to other Yanshanian Mo deposits in the East Qinling–Dabie Mo belt, reflecting that the ore sulfur of the Donggou Mo deposit could have derived mainly from magmatic source, probably with some upper crust materials. 5. Geochemistry of magmas associated with Mo mineralization All of the late Early Cretaceous Mo deposits in the East Qinling–Dabie Mo belt were spatially and temporally related to intermediate–felsic magmatism. Among these deposits, the Donggou, Tangjiaping, and Shapinggou Mo deposits have large proven Mo metal reserves and show typical characteristics of porphyry type deposits. In addition, the ore–related porphyries of these deposits have been studied in detail. Furthermore, the Saozhoupo, Donggoukou, and Laojieling Mo deposits were associated with the magmatism that formed the Laojunshan batholith, showing different characteristics with typical porphyry type Mo deposits. Therefore, we mainly chose these porphyries and batholith as representatives to describe the geochemical characteristics of the Mo–related magmas. The main isotopic characteristics of the Donggou, Tangjiaping, and Shapinggou porphyries have been summarized in Table 3. The Donggou granite porphyry samples are high in silica and potassium, and belong to high–K calc–alkaline series. The granites are metaluminous to weakly peraluminous. Chondrite–normalized rare earth elements (REE) patterns of the Donggou granites are characterized by enrichment of light rare earth elements (LREE) over middle REE, decreasing light and middle REE and increasing heavy rare earth elements (HREE) concentrations. The rocks show significant negative Eu anomalies (Eu/Eu*=0.24–0.66) (Yang et al., 2013). They also display enrichment in Rb, Th, Ta, Pb, Zr, and Hf and depletion in Ba, Sr, P, and Ti. The Donggou granites have a wide range of initial 87Sr/86Sr ratios (calculated back to 118 Ma), varying from 0.70892 to

0.73816. In contrast, the εNd(t) values of them are relatively uniform, ranging from −17.0 to −13.2. Pb isotopic compositions of the Donggou granites are similar to lower crust of the North China block, but evidently higher than that of the Xiong’er Group and the Taihua Group (Yang et al., 2013). The calculated εHf(t) values of zircons from the Donggou granites vary negatively from −17.4 to −6.1. These zircons have old two–stage Hf model ages (TDM2), which are similar to whole–rock Nd model ages. Combined whole–rock Nd with zircon Hf isotopic characteristics, Yang et al. (2013) suggested that the Donggou Mo–associated magma was derived from a mixture of Archaean/Proterozoic crustal rocks and mantle–derived or newly added crust. The Tangjiaping granite porphyry samples show high SiO2 contents. All samples are relatively high in total alkalis, and all sample data fall into the high–K calc–alkaline series or shoshonitic series fields in the SiO2 vs. K2O diagram. They are metaluminous granites with A/CNK values ranging from 0.98 to 1.00. They also have relatively low MgO contents, Mg# (molar [Mg/(Mg+Fe)]) values, and Cr, Ni contents. The Tangjiaping granites are enriched in LREE relative to HREE. All rocks have moderately negative Eu anomalies. Normalized to primitive mantle, Rb, Th, U, and Pb of the Tangjiaping granites display positive anomalies, whereas Ba, Nb, Ta, Sr, P, and Ti show negative anomalies. The Tangjiaping granites have high age–corrected initial

87

Sr/86Sr ratios (t=115 Ma), ranging from 0.707367 to 0.70941, and low εNd(t)

values varying from –15.0 to –14.2. The two–stage Nd model ages range from 2.06 to 2.13 Ga. Zircons from the Tangjiaping porphyry have negative εHf(t) values of –17.0 to –6.0, with two–stage Hf model ages ranging from 1.82 to 2.25 Ga. Several geochemical results obtained in this study, such as the whole rock Nd and zircon Hf isotope characteristics, are similar to that reported by Wei et al. (2010). Based on the geochemistry characteristics, Wei et al. (2010) suggested that the Tangjiaping granite

was formed by partial melting of crust materials. The Shapinggou Mo–bearing granite porphyry is high in SiO2 contents. The calculated A/CNK ratios are concentrated in the range of 1.01 to 1.05, indicating that the granites are weakly peraluminous (Wang et al., 2014). The granites show high K2O concentrations and fall into high–K calc–alkaline series field in the SiO2 vs. K2O diagram. In contrast, they have low CaO, MgO, and P2O5 contents. The REE of the granites show similar distribution patterns. They are enriched in LREE and have significant negative Eu anomalies. The primitive mantle normalized trace elements patterns of the granites show enrichment in Rb and Pb, and depletion in Ba, Nb, Sr, P, Eu, and Ti. The Mo–associated porphyry from the Shapinggou deposit have initial Sr ratios (t=114 Ma) of 0.6229 to 0.7019 (just for reference) and negative εNd(t) values of –13.1 to –12.6. The two–stage Nd model ages are from 1.94 to 1.98 Ga. The most zircons from granite porphyry yield εHf(t) values of −18.6 to −10.4 (except one of −23.4). The corresponding two–stage Hf model ages (TDM2) range from 1.83 to 2.35 Ga (except one of 2.64 Ga). The Shapinggou ore–related granite porphyry shows similar zircon Hf isotope components to those of the Donggou and Tangjiaping porphyries (Fig. 11), reflecting enriched characteristics and crustal origin. Wang et al. (2014) proposed that the Shapinggou Mo–associated granite porphyry was likely generated by partial melting of the middle crust without or with little mantle materials involved. The Mo mineralization in the Saozhoupo, Donggoukou, and Laojieling Mo deposits, which is obviously different from that in the Donggou, Tangjiaping, and Shapinggou Mo deposits, was associated with the Laojunshan granite batholith. Three stages of magmatism from early to late can be identified in the Laojunshan batholith: small phenocryst medium-fine grained monzogranite; moderate phenocryst medium

grained monzogranite; large phenocryst medium-coarse grained monzogranite. All of the three stages of granites are transitional between being metaluminous and weakly peraluminous and fall into high–K calc–alkaline series field in the SiO2 vs. K2O diagram. The granites have high K2O, MgO, but low CaO contents. From early to late stage, SiO2, K2O, and A/CNK increase, whereas MgO, CaO, and Na2O decrease. The Laojunshan granites are enriched in LREE and have significant negative Eu anomalies. The granites also show enrichment in Rb and Pb, and depletion in P and Ti. Overall, the geochemical characteristics of the Laojunshan granites show a crustal origin (Meng et al., 2012a), which is similar to that of the Donggou, Tangjiaping, and Shapinggou porphyries. Previous studies of the Donggou granite porphyry show that it belongs to aluminous A–type granites (Dai et al., 2009; Yang et al., 2013). In contrast, the classification of the Tangjiaping granite has been a controversial issue. Wei et al. (2010) proposed that the Tangjiaping granite porphyry belongs to weakly peraluminous S–type granites. Whereas Wang (2009) suggested that they are aluminous A–type granites. Our new petrographic and geochemical study of the fresh granites from the Tangjiaping porphyry shows that no muscovite occurred in the unaltered rocks, and most geochemical characteristics show A–type affinity (Gao, 2014). Wang et al. (2014) proposed that the Shapinggou Mo–related porphyry is highly fractionated I–type granites. However, the quartz syenite in the deposit, which was coeval with the Mo–related porphyry, could be classified as aluminous A–type granites. In addition, the quartz syenite can be considered as the starting point for the crystallization fractionation modeling of the granite porphyry (Wang et al., 2014). In summary, the Donggou, Tangjiaping, and Shapinggou Mo deposits are directly or indirectly related to A–type granitic mamgmatism.

The geochemical characteristics of the Donggou, Tangjiaping, and Shapinggou porphyries indicate that they have high differential degree. These highly differentiated magmas could have evolved from voluminous magmas, which are comparable to the magma that formed the Laojunshan batholith. Additionally, the last stage of the Laojunshan batholith also has relatively high differential degree as a result of evolution. These highly differentiated magmas could be rich in F, Cl, S, CO2, and H2O. Therefore, the magmatic water that released from these magmas could be rich in corresponding ions, which could formed numerous soluble complexes with Mo in the magmas and then initial ore-forming fluids formed. Along with the evolution of the ore-forming fluids, Mo precipitated at certain physico-chemical conditions and formed the Mo deposits finally. 6. Geodynamic constraints An understanding of the geodynamic evolution of the Qinling–Dabie orogen is of paramount importance to examine the timing of the tectonic events that contributed to the formation of Mesozoic Mo deposits. Additionally, an understanding of ore–forming processes is essential for successful deposit exploration and discovery. The tectonic evolution of the Qinling–Dabie orogen could be divided into four stages: (1) Sinian–Early Ordovician, the Qinling continent breakup and the Proto–Tethyan Qinling Ocean opened; (2) Early Ordovician–Silurian, Shangdan oceanic plate subducted northward and Erlangping back–arc basin opened; (3) Devonian–Middle Triassic, the closing of Erlangping back–arc basin and Shangdan suture, as well as the opening of Mianlue suture took place; (4) Late Triassic–Cenozoic, the Qinling–Dabie orogen underwent the stage of complete orogeny and intraplate evolution (Zhang et al., 1996, 2001). The studies of ultrahigh–pressure metamorphic rocks and collisional granites

suggested that the final collision between the North China and Yangtze cratons occurred in Late Triassic (Ames et al., 1993; Hacker et al., 1998; Zhang et al., 1994b). After that, the Qinling–Dabie orogenic belt underwent the stage of intraplate evolution. During Late Triassic–Early Jurassic, strong overthrusting–stacking, as well as the lithosphere further shortened and thickened took place in the orogenic belt (Shi et al., 2004; Ren et al., 1992). Middle–Late Jurassic, the Qinling–Dabie orogenic belt was characterized by the transition from EW–trending to NE–NNE–trending fractures, as well as the transition from compressional tectono–magmatic systems to extensional basin–mountain systems, resulting from a major tectonic regime transition from the Paleo–Tethys tectonic system to the Circum–Pacific active continental margin occurred in East China (Gilder et al., 1993; Zhao et al., 1994). Intensive Early Cretaceous magmatism-mineralization is of outstanding significance in the East Qinling–Dabie Mo belt. The late Early Cretaceous Mo mineralization that discussed here was closely related to the contemporaneous granitic magmatism. H-O-S isotopic analysis of the late Early Cretaceous Mo deposits in the East Qinling–Dabie Mo belt indicate that the ore-forming magmas are the major provider of the original ore-forming fluids and sulfur. Therefore, these Mo deposits have closely genetic relationship with the ore-forming granites. Additionally, the ages of the ore-forming granites are consistent with the molybdenite Re-Os isochron ages of these Mo deposits, also indicating that the granites and Mo mineralization are genetically related. Although the molybdenite Re-Os age of the Saozhoupo Mo deposit is slightly older than the age of the Laojunshan batholith (Meng et al., 2012a, b), our field investigations revealed that the mineralization in the deposit was later than the formation of the granite, suggesting that they formed in a same magmatic-metallogenic event and had a same tectonic setting.

It is generally accepted that A-type granites formed in an extensional environment and can provide important tectonic implications (e.g., Maniar and Picooli, 1989; Wang et al., 1995). As described earlier, the Mo mineralization in the Donggou, Tangjiaping, and Shapinggou deposits all genetically related to A–type granitic magmatism, suggesting that these Mo deposits formed in an extensional setting. In addition, the generation of A–type granitic magmas generally require a high melting temperature, the heat source of which can be provided by upwelling of hot asthenospheric mantle, resulting from the lithospheric delamination in Mesozoic (Gao et al., 1998a, b; Zhang et al., 2001). Furthermore, a series of extensional structures developed in the orogenic belt also suggested the extensional setting. For example, the extension of the detachment fault system of the Xiaoqinling metamorphic core complex in the East Qinling continued from 135 to 123 Ma, and the main activity of the extensional system within it occurred at ca. 116 Ma (Zhang and Zheng, 1999). NW–SE subhorizontal extension took place in northern Dabie during 133 to 122 Ma (Hacker et al., 1996), which is similar in age to the late Early Cretaceous Mo deposits in the Dabie area, indicating an extensional setting as well. Besides the 120–100 Ma Mo deposits and related granites, volcanic rocks formed during this period had also been recognized in the East Qinling–Dabie orogenic belt (Wang et al., 2002; Xie et al., 2007), reflecting the asthenospheric upwelling and lithospheric thinning. In fact, the 120–100 Ma magmatism is not restricted to the East Qinling–Dabie orogenic belt, but also developed in other areas in East China, such as Yanliao (e.g., Zheng et al., 2004), Shandong Province (e.g., Ling et al., 2007), and the Tan–Lu fault zone (e.g., Xie et al., 2008). The most of 120–100 Ma magmatism in these areas are characterized by volcanism, developing along or close to the Tan–Lu fault zone. In addition, a series of Cretaceous to Paleogene extensional basins also

occurred in the Tan–Lu fault zone (Zhu et al., 2001). These facts implied that the East China was in the uniform geodynamic setting during 120–100 Ma on the whole, which might have resulted from the changing of motion direction of Izanagi or Paleopacific plate to northeast, paralleling the Eurasian continent margin (Maruyama et al., 1997; Goldfarb et al., 2007). In an intraplate setting, delamination, large–scale lithospheric thinning, and asthenospheric upwelling occurred in the East Qinling–Dabie orogen in Early Cretaceous. At the same time, intensive magmatism and large–scale fluids activity developed under an extensional background, resulting in the formation of the late Early Cretaceous Mo deposits in the East Qinling–Dabie Mo belt. 7. Conclusions The late Early Cretaceous (ca. 120–100 Ma) molybdenum deposits in the East Qinling–Dabie orogen distribute in tectonic units of the southern margin of the North China Craton, North Qinling, and Dabie orogen. The formation of these Mo deposits is closely related to granitic magmatism. Fluid inclusions of the late Early Cretaceous Mo deposits have wide ranges of homogenization temperatures and salinities, varying from 115 to 550℃ and 0.02 to 62.1 wt % NaCl equivalent, respectively. Different amount of CO2 have been recognized in the ore–forming fluids of these Mo deposits, reflecting that they are H2O–NaCl–CO2 systems. The δ34S values of sulfides from the late Early Cretaceous Mo deposits range from 0.4 to 9.4 ‰, indicating a deep magmatic source on the whole. Compared with other deposits, the Donggou deposit has a slightly higher δ34S values, suggesting some upper crust materials involved in the source of sulfur. The Donggou, Tangjiaping, and Shapinggou Mo deposits are genetically related

to A–type granitic magmatism. The ore–related magmas of the late Early Cretaceous Mo deposits were mainly derived from crustal materials. The late Early Cretaceous Mo deposits in the East Qinling–Dabie Mo belt formed in an intraplate extensional setting. Acknowledgements This

research

is

jointly

funded

by

the

Geological

Survey

Project

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Figure Captions Fig. 1. Simplified geology of the East Qinling–Dabie orogenic belt, showing the distribution of Mo deposits (after Mao et al., 2011b).

Fig. 2. Geology and the distribution of the Donggou porphyry Mo deposit and surrounding hydrothermal vein Pb–Zn deposits in the Donggou area (after Ye, 2006).

Fig. 3. Geological map of the Donggou Mo deposit (modified from Ye et al., 2006).

Fig. 4. No. 20 cross–section for the Donggou Mo deposit (after Ye, 2006).

Fig. 5. Geological sketch map of the Saozhoupo Mo deposit (after Meng et al., 2012b).

Fig. 6. Geological map (a) and No. 8 section (b) of the Tangjiaping Mo deposit (after Yang, 2007a).

Fig. 7. Geological map of the Yinshan region showing the distribution of the Shapinggou Mo and sounding Pb–Zn deposits (modified from Xu et al., 2009).

Fig. 8. No. 0 section of the Shapinggou porphyry Mo deposit (modified from Zhang et al., 2010a, b).

Fig. 9. Fluid δD and δ18O characteristics of the ore–forming fluids (after Taylor, 1974). Data sources: Meng et al., 2012b; Yang et al., 2008; Ni et al., in press; this paper

Fig. 10. Histogram of sulfur isotope (δ34S) of sulfides in the late Early Cretaceous Mo deposits in the East Qinling–Dabie Mo belt.

Data sources: Meng et al., 2012b; Yang et al., 2008; Ni et al., in press; this paper

Fig. 11. εHf(t) vs. Age plots for zircons from the Donggou, Tangjiaping, and Shapinggou porphyries. Data sources: Yang et al., 2013; Wang et al., 2014; this paper

Table Captions Table. 1. Characteristics of the late Early Cretaceous Molybdenum deposits in the East Qinling–Dabie molybdenum belt.

Table. 2. Microthermometric and stable isotopic data of the late Early Cretaceous Molybdenum deposits in the East Qinling–Dabie molybdenum belt.

Table. 3. Summarized isotopic data for the ore–related porphyries from the Donggou, Tangjiaping, and Shapinggou deposits in the East Qinling–Dabie molybdenum belt.

Table 1 No.

Deposit/ore spot

Location

Reserve/104 t

Mineralization age/Ma

Ore-bearing rocks

Grade

1

Donggou

Southern margin of NCC

62.5

116 ± 1.7

Granite porphyry, Xiong’er Group volcanic rocks

Average 0.113%

2

Nangou

North Qinling

–

106.3–108.2

K–feldspar granite

1%–2%

3

Saozhoupo

North Qinling

2

111.5–114.5

Laojunshan granite, Kuanping Group quartz schist

0.03–0.15%

4

Donggoukou

North Qinling

–

113.1–113.6

Kuanping Group quartz schist

–

5

Laojieling

North Qinling

–

109.8

Laojunshan granite

–

6

Tangjiaping

Dabie orogen

23.5

113.1 ± 7.9

Granite porphyry

Average 0.063%

7

Shapinggou

Dabie orogen

220

113.2 ± 0.5

Granite porphyry, quartz syenite, breccia

Average 0.15%

Table 1 (continued) N o.

Deposit

Hydrothe rmal alteration

Ore mineral assembl age

Gangue mineral assembla ge

Wall rock

Ore–contro lling structures

Lengt h, thickn ess of orebo dy

Refere nces

1

Donggo u

Silicifica tion,

Molybde nite, pyrite, chalcopy rite, galena,

Quartz,

Mesoproter ozoic Xiong’er Group volcanic rocks

EW, NW, NE, and

2000 m, averag e 189.7 6m

Ye et al., 2006; Yang et al., 2013

K–feldsp ar alteration ,

K–feldsp ar, plagioclas e, clinopyro

NS–extendi ng faults

biotitizat ion, sericitiza tion, chloritiza tion, fluoritiza tion, calcitizat ion

sphalerit e, scheelite

xene, hornblend e, biotite, chlorite, epidote, sericite, fluorite

2

Nangou

–

Molybde nite, chalcopy rite

Quartz

Granite

NW–exten ding faults

–

Yang et al., 2010

3

Saozhou po

Silicifica tion,

Molybde nite, pyrite, limonite, magnetit e

Quartz,

Kuanping Group

NWW–exte nding faults

102 m, averag e 22.42 m

Meng, 2010; Meng et al., 2012b

NWW–exte nding faults

–

NWW–exte nding faults

–

K–feldsp ar alteration , Pyritizati on, sericitiza tion, chloritiza tion, biotitizat ion 4

Donggo ukou

Silicifica tion, K–feldsp ar alteration , Pyritizati on, sericitiza tion

5

Laojieli ng

Silicifica tion, K–feldsp ar alteration ,

Molybde nite, pyrite

Molybde nite, pyrite

K–feldsp ar, plagioclas e, biotite, muscovit e, sericite, hornblend e, chlorite

Quartz, K–feldsp ar, biotite, sericite

Quartz, K–feldsp ar, biotite, sericite

mica–quart z schist

Kuanping Group mica–quart z schist

Laojunsha n granite

Pyritizati on, sericitiza tion 6

7

Tangjiap ing

Shaping gou

K–silicat e alteration , silicificat ion, sericitiza tion, and pyritizati on

Molybde nite, pyrite, chalcopy rite, magnetit e, galena, sphalerit e, hematite .

quartz, sericite, muscovit e, calcite, plagioclas e, biotite, chlorite, and epidote

Proterozoic gneiss

K–feldsp ar alteration , biotitizat ion, silicificat ion, sericitiza tion, chloritiza tion, Pyritizati on, fluoritiza tion, calcitizat ion, kaoliniza tion

Molybde nite, pyrite, galena, chalcopy rite, sphalerit e, magnetit e

Quartz, K–feldsp ar, plagioclas e, biotite, sericite

Neoprotero zoic Luzhengua n Group gneiss and amphibolit e

Second ordered structures of nearly SN– and NNW–exte nding faults

NEE–, nearly EW– extending faults

1760 m, averag e 125.8 m

Yang, 2007a, b

1350 m, averag ing 661.3 2m

Huang et al., 2011; Zhang et al., 2010a, 2012

Table 2 Deposit

Thomogeniza tion (℃)

Salinity (wt % NaCl eq.)

δDSMOW ‰

δ18OSMOW ‰

δ18Ofluid ‰

δ34SV-CDT/( ‰)

Data sourc es

Donggou

125–550

0.5–19.3, 31.71–49.

-92 to -69

8.1–10.9

-2.6–5.1

7.5–9.4

Yang et a.,

22

2011; this paper

Saozhoup o

198–343

1.57–8.95

-94 to -82

7.4–10.4

-2.54–0. 92

3.4–6.3

Laojieling

115–445

2.74–10.3 6

-93

7.6

0.26

3.6

Donggouk ou

138–418

0.35–16.2 4

-108 to -90

6.3–8.1

-3.18 to -0.48

2.4–4.6

Tangjiapi ng

>375,

1.06–62.1

-84 to -58

8.6–11.1

-0.11–4. 44

0.4–4.1

Wang et al., 2009; Yang et al., 2008; this paper

Shapingg ou

170–550

0.02–16.8 9,

-90 to -63

6.4–11.8

-0.5–7.5

2.1–5.9

Yu et al., 2012; Ni et al., 2015

115–335

32.92–50. 85

Meng et al., 2012 b; this paper

Table 3 Deposit

Ore-related igneous rock

Age/Ma

(87Sr/86Sr)i

εNd(t)

Zircon εHf(t)

Data sources

Donggou

Granite porphyry

112 ± 1

0.70892–0.73816

-17.0 to -13.2

-17.4 to -6.1

Yang et al., 2013; Ye et al., 2006

Tangjiaping

Granite porphyry

115 ± 1

0.706937–0.70941

-15.2 to -14.2

-17.0 to -6.0

This paper

Shapinggou

Granite porphyry

114 ± 1

0.6229–0.7019

-13.1 to -12.6

-23.4 to -10.4

Wang et al., 2014

Figure

Fig. 1.

Fig. 2.

Fig. 3.

Fig. 4.

Fig. 5.

Fig. 6.

Fig. 7.

Fig. 8.

Fig. 9.

Fig. 10.

Fig. 11.