Ore Geology Reviews 53 (2013) 422–433

Contents lists available at SciVerse ScienceDirect

Ore Geology Reviews

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

Geology and molybdenite Re–Os age of the Dahutang granite-relatedveinlets-disseminated tungsten ore field in the Jiangxin Province, China

Zhihao Mao a,⁎, Yanbo Cheng a,⁎, Jiajun Liu a, Shunda Yuan b, Shenghua Wu b, Xinkui Xiang c, Xiaohong Luo d

a Faculty of Earth Science and Mineral Resources, China University of Geosciences, Beijing 100083, Chinab MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, Chinac No. 916 Geological Team, Jiangxi Bureau of Geology, Mineral Resources, Exploration and Development, Jiujiang 332000, Chinad Northwestern Geological Team, Jiangxi Bureau of Geology, Mineral Resources, Exploration and Development, Shahe 332100, China

⁎ Corresponding authors. Tel.: +86 13810919614.E-mail addresses: Alexander.mao0712@gmail.com (

(Y. Cheng).

0169-1368/$ – see front matter © 2013 Elsevier B.V. Allhttp://dx.doi.org/10.1016/j.oregeorev.2013.02.005

a b s t r a c t

a r t i c l e i n f o

Article history:Received 15 October 2012Received in revised form 12 February 2013Accepted 13 February 2013Available online 19 February 2013

Keywords:Veinlets-disseminated tungsten depositWorld-class depositMolybdenite Re–Os age datingMiddle–Lower Yangtze River ValleyNew tungsten belt

This is a brief research report about the recently-discovered and currently being explored Dahutang tungsten de-posit (or ore field) in northwestern Jiangxi, south-central China. The deposit is located south of the Middle–LowerYangtze River valley Cu–Au–Mo–Fe porphyry–skarn belt (YRB). The mineralization is genetically associated withCretaceous porphyritic biotite granite and fine-grained biotite granite and is mainly hosted within aNeoproterozoic biotite granodiorite batholith. The Dahutang ore field comprises veinlets-disseminated (~95% ofthe total reserve), breccia (~4%) and wolframite–scheelite quartz vein (~1%) ore styles. The mineralization andalteration are close to the pegmatite shell between the Cretaceous porphyritic biotite granite and Neoproterozoicbiotite granodiorite and the three styles of ore bodies mentioned above are related to zoned hydrothermalalteration that includes greisenization, K-feldspar alteration, silicification, carbonatization, chloritization andfluoritization arranged in time (early to late) and space (bottom to top).Five samples of molybdenite from the three types of ores have been collected for Re/Os dating. The results showRe/Os model ages ranging from 138.4 Ma to 143.8 Ma, with an isochron age of 139.18±0.97 Ma (MSWD=2.9).The quite lowRe content inmolybdenite falls between 0.5 ppmand 7.8 ppm that is indicative of the upper crustalsource. This is quite different frommolybdenites in the YRB Cu–Au–Mo–Fe porphyry–skarn deposits that containbetween 53 ppm and 1169 ppm Re, indicating a mantle source.The Dahutang tungsten system is sub-parallel with the YRB porphyry–skarn Cu–Au–Mo–Fe system. Both aresituated in the north margin of the Yangtze Craton and have a close spatial–temporal relationship. This pos-sibly indicates a comparable tectonic setting but different metal sources. Both systems are related to subduc-tion of the Paleo-Pacific plate beneath the Eurasian continent in Early Cretaceous. The Cu–Au–Mo–Feporphyry–skarn ores are believed genetically related to granitoids derived from the subducting slab, whereasthe porphyry W deposits are associated with S-type granitoids produced by remelting of the upper crust byheat from upwelling asthenoshere.

© 2013 Elsevier B.V. All rights reserved.

1. Introduction

TheMiddle–Lower Yangtze (or Chang Jiang) River Basin (hereinafterreferred to as YRB) is a host to a major metallogenic province inEast-Central China that has a great economic value. Themassive reservesof high grade Cu and Fe ores and locally supportivemining conditions ac-count for a longmining history that can be traced back to the Bronze Age(~3800 years before present). Even after several millennia ofmetal min-ing, the YRB still shows a strong vitality and active exploration and min-ing continue to this day. YRB is characterized by both porphyry–skarnCu–Au–Mo–Fe deposits, and magnetite–apatite deposits (Mao et al.,

Z. Mao), chamboll@yahoo.cn

rights reserved.

2011). A substantial progress in understanding both types of ore de-posits, their relation to granitic magmatism, and their setting has beenachieved in the past decades (Chang et al., 1991; Ling et al., 2009; Maoet al., 2006, 2011; Pan and Dong, 1999; Zhai et al., 1992; Zhou et al.,2008).

Recently a number of granite-related W and W–Mo deposits havebeen discovered and explored to the south of the YRB, along theYangxing–Changzhou Fault (Fig. 1) and this includes the Dahutang(DHT) ore field. Dahutang was initially discovered by the JiangxiBureau of Geology in 1957, by heavy mineral prospecting. Subsequentexploration in 1958, 1966, 1979 and 1984 proved the existence of asmall tungsten deposit there. Detailed exploration (including drillingprograms, underground working and trenches at surface), restartedin 2010, has so far established a tungsten resource that exceeds 1.1Mt tons of WO3 (~880 Kt W) at an average grade of 0.152% W.There is also 500 Kt Cu @ 0.12% and 80.2 Kt Mo @ 0.098% Mo. Further

Fig. 1. Map showing the distribution of the mineral deposits along the Middle–Lower Yangtze River belt (YRB) and the porphyry–skarn W and W–Mo deposits south of it. YCFYangxing–Changzhou Fault, TLF Tancheng–Lujiang Fault, XGF Xiangfan–Guangji Fault.

423Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

investigation is underway and the local geological survey departmentspeculates that the WO3 resource could reach up to 2,000,000 t.

There are two distinct metallogenic provinces in South-CentralChina: 1) the Cu–Au–Mo–Fe porphyry–skarn YRB province, and 2) thebroadly contemporaneous W–Sn province in the Nanling area, in thecentral part of the Cathaysia Block (Fig. 1) (Chang et al., 1991; Chen etal., 1989; Mao et al., 2004, 2012; Zhai et al., 1992). The newly exploredDahutang ore field and the other previously known veinlets and skarnW and W–Mo deposits in the same belt (Fig. 1) are situated along thenorthernmargin of the Yangtze Craton, close to the YRB, but their char-acteristics havemore similarities with the granite-relatedW andW–Sndeposits in the Nanling area (see the inset of Fig. 1). This makes under-standing of their geology, formation age and tectonic environment ofgreat scientific and practical importance. This paper is a contributionto understanding the geological characteristics of the Dahutang tung-sten ore field, integrated with new molybdenite Re/Os age determina-tions, leading to a discussion about the metallogeny and geodynamics.

2. Regional geological background

The YRB is located at the northern margin of the Yangtze Craton,south of the North China Craton and Qinling–Dabie orogenic belt,characterized by several large strike-slip fault systems, i.e. theXiangfan–Guangji Fault in the northwest, the Tancheng–LujiangFault in the northeast and the Yangxing–Changzhou Fault (YCF) inthe south (Fig. 1). Five successions of exposed rocks are generallyfound in YRB, from base to top: 1) Mesoproterozoic low-grademetamorphic basement; 2) Neoproterozoic to Silurian clastic rocks;3) Middle Devonian to Early Triassic carbonates; 4) Middle Triassicto Early Jurassic marine and terrigenous sedimentary rocks; and 5) EarlyCretaceous units which comprise four cycles of andesitic volcanic rockscontrolled by several parallel NE-trending extensional basins. Rocky

outcrops in the south of the YCF zone include the NeoproterozoicShuangqiaoshan Group phyllite and Banxi Group of metamorphosedslate locally intercalated with basalt–rhyolite volcanics in the Jiangnanmassif (or shield). SHRIMP zircon U–Pb determination performed byGao et al. (2011) on volcanic rocks from both Groups indicated their for-mation ages as 822 Ma±10 Ma and 803 Ma±7.6 Ma, respectively. APhanerozoic cover is generally developed outside the Jiangnan massifand it includes clastic and carbonate rocks. There, as in the YRB, theSilurian to Early Triassic strata are marine clastic and carbonate rocks,Middle Triassic to Early Jurassic are paralic clastic rocks, whereas Middleto Late Jurassic–Cretaceous are sedimentary and volcanic rocks occurwithin a series of NE-trending continental basins.

Neoproterozoic and Yanshanian granitic rocks are present in thearea. The JiulingNeoproterozoic granitic intrusion, the largest compositegranitoid complex in south-eastern China with an outcrop area greaterthan 2500 km2 (Zhong et al., 2005). Mesozoic (Yanshanian) graniticrocks (more details below) in the study area occur asmany small stocks,intruding in both Neoproterozoic granodiorite batholith and Precambri-an strata.

Mao et al. (2011) distinguished two ore types in the YRB: the Cu–Au–Mo–Fe porphyry–skarn type dated at 143–137 Ma, and the“porphyrite iron ore” of magnetite–apatite (close to the Kirunatype) dated at 135–123 Ma. The tungsten veinlet-disseminated andskarn belt located south of the YRB includes the Xianglushan,Dahutang, Yangchuling, Qimei, Matou, Jitoushan and other deposits,shown in Fig. 1.

3. Geology of the Dahutang tungsten ore field

The Dahutang tungsten ore field is located in the western segmentof the Jiuling-Zhanggong uplift within the Yangtze Craton; all tung-sten mineralizations are found within the Neoproterozoic Jiuling

424 Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

granodiorite batholith (Fig. 2). The relatively monotonous strata inthe mine area include the gray–green to dark gray phyllite and slateof the Neoproterozoic Shuangqiaoshan Group, intercalated withmeta-sandstone characterized by rhythmic turbiditic (flysch) banding.These rocks are discontinuously distributed as roof pendants in theJiuling biotite granodiorite and they include a relatively large outcroparea in the southern part of the mine area, south of the Shiweidongore deposit (Fig. 2). Products of thermal metamorphism in the rockunits at contact with the Neoproterozoic biotite granodiorite arehornfelsed and characterized by andalusite and cordierite spots inslate and greywacke, or silicification.

Deformation structures are extensively distributed in the area andinclude faults and joints. An EW-striking ductile shear zone formed inthe Neoproterozoic biotite granodiorite batholith within the Shimensideposit area, with outcrop width of approximately 100 m. The shearzone crosses the Xin'anli W property (Fig. 2) in the east and extendsoutside Fig. 2 at both sides. This shear zone displays a significantzoning of the fault rock, from the periphery to the center: myloniticbiotite granodiorite→mylonite→phyllonite→mylonitic schist. In themine area the shear zone is highly silicified and mainly acted as anore-controlling structure. North of the Shimensi deposit this shear zoneis intersected by the NNE-trending Xianguoshan–Dahutang-Shiweidongbasement fault with total length of up to 25 km. These two sets of faultsare considered to have been the channels of the ore fluids, and they notonly controlled the distribution of the deposits, but also determined theemplacement of Cretaceous granite. In addition to this, several NNE–NEand NNW–NW trending, NW and NE dipping faults of variable length

Fig. 2. Geological map of the Dahutang tungsten ore field that includes the Shimensi, YikNeoproterozoic Jiuling granodiorite intrusion and is genetically related to Cretaceous (Yanof Geology, Mineral Resources, Exploration and Development, 2012).

between 100 m and 500 m, can be observed within the mining area,where they contain wolframite–scheelite quartz veins. As another im-portant ore-controlling structure, the stockwork fractures are denselydeveloped at the contact of the Cretaceous porphyritic biotite graniteand the surrounding country rocks of the Neoproterozoic biotite grano-diorite batholith, and are interpreted as the result of post-emplacementdilation due to volume reduction of the solidifying Cretaceous granitestock.

The exposed intrusive rocks within the mining area are part of theNeoproterozoic Jiuling composite intrusion of predominantly gray,medium to coarse crystalline quartz-phyric granodiorite composedof 25–30% quartz, 20–40% plagioclase, 5–10% K-feldspar, 6–13%biotite, 1–5% cordierite, and 2–5% muscovite. Zircon, apatite, garnet,magnetite and ilmenite are the most common accessory minerals.

The Cretaceous biotite granite emplaced into the Jiuling granodioritebatholith (Fig. 2) consists of porphyritic biotite granite, fine-grainedbiotite granite, and granite porphyry dykes. The porphyritic biotitegranite is gray to white with ~60 vol.% of plagioclase and ~40 vol.% ofquartz phenocrysts in fine-grained matrix. The common length of pla-gioclase phenocrysts is 0.5–1 cm, with the largest crystals reaching upto 2 cm. Thematrix is composed of 30 vol.% quartz, 40–50 vol.% plagio-clase, and 5–10% biotite. The gray fine-grained granite has 20–21% ofplagioclase, 33–34% of K-feldspar, 39–40% of quartz and ~7% of biotite.The tabular plagioclase crystals that measure between 0.6×0.8 and1.4×2.4 mm are subhedral and commonly exhibit polysynthetictwins, less often as compound carlsbad–albite twins. Biotite flakes aremainly euhedral. Post-mineralization medium to fine-grained, light

uangdai and Shiweidong deposits. The tungsten mineralization developed within theshanian) granitic intrusions. (Modified from No. 916 Geological Team, Jiangxi Bureau

425Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

flesh-colored granite porphyry dykes intersect the above-mentionedgranitoids and the ore veins. They have 10–15% plagioclase, 20% quartzand 5% biotite phenocrysts in matrix of K-feldspar, quartz andsericite. The Dahutang tungsten ore field consists of three ore de-posits (or sections): the Shimensi deposit in the north, Dalingshang(or Yihaomai) deposit in the center and the Shiweidong deposit inthe south (Fig. 2). Shimensi was explored by the No. 916 GeologicalTeam, Jiangxi Bureau of Geology, Mineral Resources, Explorationand Development proving a reserve of 758,500 t @ 0.19% WO3.Shiweidong was explored by the Northwestern Geological Team,Jiangxi Bureau of Geology, Mineral Resources, Exploration and De-velopment who calculated a reserve of up to 299,000 t @ 0.17%WO3. At present,more drilling is in progress around theDalingshang de-posit. There, the mineralization is predominantly in the Neoproterozoicbiotite granodiorite close to contact with the Cretaceous biotite granitestock, although some ore bodies are in Cretaceous biotite graniteendocontact (Fig. 3a, b) and a few extend into the Neoproterozoic

Fig. 3. Geological map at elevation 1055 m (a), and A–B–C longitudinal section (b), showingmainly by the Neoproterozoic biotite granodiorite. The ore bodies extend towards the easBureau of Geology, Mineral Resources, Exploration and Development, 2012).

phyllite and slate (Fig. 4). The ore body has usually a layered to lenticularform with a maximum thickness of ~390 m. Subeconomic tungstenmineralization is more widespread, especially between the delineatedhigher grade zones.

4. Alteration and mineralization

4.1. Mineralization styles

Three mineralization styles are represented in the Dahutang orefield: 1) Veinlet-disseminated (Fig. 5a, b); 2) quartz vein (Fig. 5c);and 3) hydrothermal breccia (Fig. 5d). Style 1 accounts for morethan 90% of total tungsten reserve. These three styles frequentlyco-exist in space and overlap each other (Fig. 6).

Style 1 mineralization is most common in granitoids of both agegroups. The Neoproterozoic biotite granodiorite hosts more than57.3% of the total tungsten reserves of the veinlet-disseminated

the major ore bodies in the Shimensi deposit of the Dahutang tungsten ore field, hostedt, west and south outside the scope of Fig. 3a. (After No. 916 Geological Team, Jiangxi

Fig. 4. The Shiweidong cross section of the Dahutang ore field showing most ore bodies hosted by the Neoproterozoic phyllite and slate and less in the Cretaceous granite (Modifiedfrom Northwestern Geological Team, Jiangxi Bureau of Geology, Mineral Resources, Exploration and Development, 2012).

426 Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

style and the ore has a relatively high grade (0.18–0.40% WO3).Wolframite is slightly more common than scheelite among the oreminerals. The corresponding ore style in the Cretaceous biotitegranite accounts for up to 32.7% of the total resource but the gradeof 0.16–0.30% WO3 is slightly lower. The ore consists of fine-grainedanhedral scheelite, wolframite, chalcopyrite and other metallicminerals in a gangue of quartz, biotite and muscovite. The distribu-tion of veinlet-disseminations ranges from sparse to dense (Fig. 5a).

Breccia-hosted mineralization is developed in central parts of theShimensi and Shiweidong deposits, in apical part of the Cretaceousbiotite granite stock (Fig. 6). The breccia fragments have been derivedmore from the Neoproterozoic granodiorite than from the Cretaceousporphyritic biotite granite. Most of the breccias exhibit internaljigsaw texture (hydraulic fracturing) filled by quartz-dominated orecomponent (Fig. 5d). The interfragmental hydrothermal fill has, inaddition to quartz, subordinate muscovite, biotite, K-feldspar, fluorite,tourmaline and other gangue minerals. Wolframite, scheelite, chalco-pyrite and molybdenite have the form of scattered lumps, dissemina-tions and diffuse admixtures in the gangue and rarely in the brecciafragments. It is interesting to see the presence of dendritic biotite,within the breccia ore, growing inward towards the cementing mate-rial. This ore style contributes some 5% of the total WO3 reserve in theore field.

Quartz, wolframite, and scheelite veins cut through the entirearea. They follow the NE-, NW- and NS-striking faults, are most wide-spread in the western and central areas, and account for about 1% ofthe total ore reserve. In these veins, wolframite usually occurs inthick tabular crystals, rooted in both vein walls, forming a symmetri-cal comb-like structure (Fig. 5c). This ore variety has a higher tung-sten grade (average of 0.282% WO3) compared with the remainingore types in the deposits, and wolframite is more common thanscheelite. It also can be seen that scheelite aggregations replace thewolframite crystals. The ore metals are vertically zoned, from thetop downwards: W→W+Cu→Cu+Mo.

4.2. Mineralization and alteration events

In the light of mineral paragenesis, cross-cut relationships, tex-tures/structures and related wall rock alteration, the ore formingevents at Dahutang can be divided into three stages: 1) Cretaceousbiotite granite emplacement accompanied by thermal metamorphismand pegmatite formation; 2) magmatic-hydrothermal alterationand mineralization that can be further subdivided into a pre-oreK-feldspathization, ore-related silicification and greisenization, andpost-ore carbonatization; and 3) post-Cretaceous supergene modifica-tion. This paragenetic sequence is illustrated in Fig. 7.

Thermal metamorphism resulted from the intrusion of graniticmagma into roof rocks. The degree of resulting changes is controlledby the heat regime and the nature of the rocks undergoing thermalmetamorphism, especially their composition. Therefore, changes pro-duced by the emplacement of the Cretaceous granite into Proterozoicgranodiorite in the Dahutang area are slight to barely discernible. Onthe other hand, wall rocks other than this granodiorite weresubjected to substantial thermal modifications, such as hornfelsingand porphyroblastic growth of minerals. The Shuangqiaoshan Groupschist in Cretaceous granite exocontact is spotted with and andalusiteand cordierite porphyroblasts and is locally silicified.

Generally Sn–W granites orthomagmatic pegmatite shells orlenses overlap with hydrothermally altered rocks, dominated byK-feldspar and/or albite (Pirajno, 2012). The pegmatoidal shells inthe classical localities such as those of the central European Erzgebirge(Altenberg) (Rösler et al., 1968), seem to combine both volatile magmaemplacement and hydrothermal alteration, and are often transitionalinto greisen (quartz, muscovite) and quartz, topaz, zinnwaldite, cassiter-ite, and wolframite ore veins that fill concentric dilations in graniteparallel with cupola surfaces as in Cínovec, Czech Republic (Štemproket al., 1995). In the Dahutang ore field such pegmatoidal shells are devel-oped along contacts of Cretaceous granite cupolas against the Proterozoicgranitoid exocontact. They consist of K-feldspar, quartz, and small

Fig. 5. Veinlet scheelite ore exhibited in drill cores (a), and in the underground mine (b), a thick quartz–wolframite (scheelite) vein ore showing large crystals of wolframite that grewinward from thewall towards thevein center,with interstitial scheelite,molybdenite and chalcopyrite assemblages (c); scheelite-mineralized ore in jigsaw-style hydrothermal breccias (d).

427Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

amounts of biotite and muscovite perpendicular to the contact zone(Fig. 8a, b). Truemagmatic pegmatite veins, however, also exist in the cu-polas. They have cross-cutting relationships, sharp contacts, and arecomposed of K-feldspar megacrysts, albite, and quartz with interstitialmuscovite. Metallic mineralization, however, is absent here.

In the initial magmatic-hydrothermal stage potassic alterationconverted albite in the Neoproterozoic granodiorite to K-feldspar.This was followed by the introduction of ore metals producing thethree ore styles described above (veinlets-disseminations, hydrother-mal breccias, wolframite–scheelite quartz veins) with the followingmineral associations:

quartz–K-feldspar–wolframite–cassiteritequartz–muscovite–wolframite–scheelite–cassiteritequartz–wolframite–scheelitequartz–wolframite–scheelite–chalcopyritequartz–scheelite–chalcopyrite–(bornite)quartz–molybdenite–chalcopyrite.

Among them the quartz–wolframite–scheelite veins, veinlet andbreccias are dominant. Greisen and silica alterations are closely associat-ed with the mineralization. Pervasive quartz–muscovite greisenizationis the standard feature of the veinlet-disseminated ore style, whereasthe quartz–wolframite–scheelite veins have greisen selvages that are

proportional to the vein thickness, ranging from several centimeters totens of centimeters. In the breccia ore greisenization also occurs in thecountry rocks along the quartz–wolframite–scheelite cements. Carbon-ate veinlets and short discontinuous veins of purple fluorite infill dila-tions in the closing, post-ore stage of the hydrothermal event and theyare superimposed on all ore style varieties as well as on unmineralizedgranitoids.

Retrograde supergene modification of the hypogene ores, as wellas their host rocks, took place after erosion that removed severalthousand meters of the roof and exhumed the primary mineraliza-tion. Oxidation and hydration at the higher supergene levels wereresponsible for conversion of sulfides into goethite, malachite, covel-lite and chalcocite, whereas wolframite and scheelite were oxidizedinto tungstite. In the deeper secondary sulfides zone chalcocite andcovellite replaced chalcopyrite and bornite, whereas wolframite andscheelite remained as relics. Silicateminerals weathered into hydromicaand kaolinite locally pigmented by manganite, and carbonate and fluo-rite were leached out.

5. Sampling, analytical methods and results

Re/Os isotope analysis of molybdenite is a powerful method to de-termine the ore-forming ages. It has been extensively applied to dateores in past fifteen years (e. g. Mao et al., 1999; Stein et al., 1997). In

Fig. 6. NW–SE cross-section of the Shimensi deposit showing three tungsten ore types: veinlets-disseminated breccia and wolframite (scheelite)–quartz vein. (After No. 916 Geo-logical Team, Jiangxi Bureau of Geology, Mineral Resources, Exploration and Development, 2012).

428 Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

order to establish the precise mineralization age of the Dahutangporphyry tungsten system we collected five molybdenite samplesnumbered DHT-1, DHT-7, DHT-8, DHT-13 and DHT-14 from theShimensi deposit for analysis. The sample set comprised two repre-sentatives of the veinlet-disseminated style, two from the quartz–wolframite–scheelite veins and one from the breccia style. In thefirst ore style molybdenites occur as fine-crystals in veinlets-disseminated ores hosted in porphyritic biotite granite (Fig. 9a). Inthe vein ore style molybdenite flakes tend to accumulate along thevein-wall rock contact and reach into the altered selvage (Fig. 9b).In the breccia-hosted ore molybdenite is scattered in the internalfragmental space.

Molybdenite concentrates for analysis were prepared using theconventional method. After crushing the samples were subjected togravity and magnetic separation after which the molybdenite grainswere handpicked under a binocular microscope to achieve >99%sample purity. The analyzed molybdenite was fine-grained (b0.1 mm)to minimize possible decoupling of Re and Os within large molybdenitegrains (Selby and Creaser, 2004; Stein et al., 2003). The analyses wereperformed in the Re–Os Laboratory, National Research Center of Geoanalysis, Chinese Academyof Geological Sciences in Beijing using a Ther-mo Electron TJA X-series ICP-MS. The analytical procedures followedthose described by Shirey and Walker (1995), Mao et al. (1999) andDu et al. (2004). Themodel ageswere calculated following the equation:t=[ln (1+187Os/187Re)]/λ, where λ is the decay constant of 187Re,1.666×10−11/year (Smoliar et al., 1996).

In our samples the concentrations of 187Re and 187Os ranged from354 to 4952 ppb to 0.82 to 11.60 ppb, respectively. In order to checkthe accuracy we have ran a duplicate analysis of sample DHT-7. Wehave obtained a range of Re–Os model ages of 138.4–143.8 Ma, witha weighted mean age of 140.4±1.9 Ma. All three styles of ore distri-bution returned the same mineralization age, implying an almost

simultaneous emplacement. Our data, processed using the ISOPLOT/Ex program (Ludwig, 2004), yielded an isochron age of 139.2±1.0 Ma, with MSWD=1.7 (Fig. 10). The identical model ages and iso-chron ages of the five samples suggest that the analytical results arereliable.

6. Discussion

6.1. Principal characteristics of granite-related tungsten deposits

Both skarn and wolframite–quartz vein types of tungsten depositsare the major source of tungsten metal in China and the world (Černýet al., 2005; Laznicka, 2006, 2010; Li, 1993; Mao et al., 2009; Pirajno,2009). Compared to the porphyry Cu–Mo deposits, porphyry tungstendeposits are less known. So far, several porphyry W–Mo, W–Mo–Sn de-posits are reported inNewBrunswick, Canada (Noble et al., 1984; Parrishand Tully, 1978; Sinclair, 2007), the Logtung deposit, south-centralYukon Territory (Noble et al., 1984), the Lianhuashan porphyry W de-posit, the YangchulingW–Modeposit and JitoushanporphyryW–Mode-posit (Man and Wang, 1988; Song et al., 2012; Tan, 1985), and Weolagand Dae Hwain Korea (Shelton et al., 1987; So et al., 1983a,b). However,these porphyry W deposits are small scale with less economic value(Sinclair, 2007). Among them the Lungton is described as a largetonnage, low-gradeW(scheelite)–Moporphyry deposit, itsWO3 reserveis 210,600 t (Noble et al., 1984; Sinclair, 2007), much less thanthe Dahutang tungsten deposit. It's worth to point out that porphyryCu–Mo, porphyry Cu–Au and porphyry Mo deposits usually have a typi-cal alteration zoning, i.e. potassic alteration, quartz sericite and propyliticalteration from the core outwards. However, the porphyry tungsten de-posits are characterized by strong greisenization, and weak potassic al-teration and propylitization. In this case, Davis and William-Jones(1985) named it as porphyry–greisen tungsten deposit.

Fig. 7. Paragenetic sequence of alteration and ore minerals in the Dahutang tungsten deposit.

429Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

Rundqvist et al. (1971) recognized greisen Sn (W) at the cupolas ofgranite intrusions in the Erzgebirge area of Germany and Czech, Tasma-nia, Australia and Mongolia. The greisen ore mainly consisting of quartz,

Fig. 8. Pegmatite shell between the Cretaceous porphyritic biotite granite stock and the Neoconsisting of K-feldspar, quartz and a small amount of biotite and muscovite that are aligne

muscovite, cassiterite and minor wolframite occurs as massive and dis-seminated ore styles. There are a few typical greisen tungsten depositsin China. Feng et al. (2011a,b) reported a greisen tungsten deposit in

proterozoic biotite granodiorite batholith in Shimensi (a) and Dalingshang (b), mainlyd perpendicularly to the contact.

Fig. 9. Sample of veinlets-disseminated W ore fromwhich emolybdenite samples were collected for Re/Os dating, showing disseminated coexisting molybdenite and chalcopyrite inporphyritic biotite granite (a); Molybdenite in the quartz–wolframite (scheelite) vein usually occurs along the vein/wall rock contact and in altered vein selvages (b).

430 Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

south Jiangxi province, Nanling region, where an elongated greisen orebody mainly consisting of quartz, muscovite, and wolframite developedalong a fracture within the Jiulongnao biotite granite batholith. Theother example is Shizhuyuan, a world class skarn–greisen W–Sn–Mo–Bi deposit in southern China, where the large stockwork greisen orescomprising quartz–biotite, quartz–muscovite and quartz–topaz oreveins overprint the skarn ores (Mao and Li, 1996). Unlike the typical grei-sen deposits, the Dahutang contains veinlets-disseminated, wolframiteand scheelite quartz vein and hydrothermal breccia-hosted ore styles.They have limited amounts of muscovite and cassiterite but areenriched in wolframite, scheelite, and chalcopyrite within the veinletsand quartz vein and breccia ores. All three ore types have the samemin-eral associations and are characterized by strong greisenization mainlycomprising quartz and muscovite, and weak potassic and propylitic al-teration. Hydrothermal potassic (K-feldspar) alteration at the base ofthe exposedmineral system overlaps with pegmatite and is gradationalto greisen in themid-section (especially in the Shimensi deposit), indic-ative of extensive Ca, Na and Mg removal from the host granites. Silici-fication (in the Shiweidong deposit) or dilations-filling by quartzfollowed, all spatially associated with mineralization. In the distal envi-ronment as in the Neoproterozoic granodiorite, chlorite formed in place

Fig. 10. Molybdenite Re/Os age of the Shimensi ore section constructed using ISOPLOTsoftware of Ludwig (1999). The calculated isochron age using the decay constant:λ(187Re) is 1.666×10-11/year (Smoliar et al., 1996); absolute uncertainty at 2σ haserror of 1.02%.

of biotite. On the whole, the Dahutang ore field shares similarities toboth porphyry and greisen ore systems.

6.2. Timing of metal introduction and metal sources in the Dahutang orefield and comparison with other W deposits in southern China

We consider the geochronological data obtained by application ofthe Re/Os dating technique to Dahutangmolybdenite samples (modelages ranging from138.4 Ma to143.8 Ma; Table 1, Re–Os isochron ageof 139.18±0.97 Ma (MSWD=2.9) (Fig. 10)) to closely approximatethe age of molybdenite crystallization and tungsten mineralization.These mineralization age data also compare well with the agesreported from other porphyry W–Mo deposits in the same ore beltin the Middle–Lower Yangtze River region. Song et al. (2012)reported the Re/Os molybdenite age of 137 Ma for the W ore, andU–Pb zircon age of 138 Ma for the parent granite, in the Jitoushanporphyry W–Mo deposit. Man and Wang (1988) obtained muscoviteK–Ar ages of 137.1±3.4 Ma and 137.8±3.1 Ma for breccia ore, andwhole rock Rb–Sr isochron ages of 140.5±4.7 Ma for ore-relatedgranodiorite in the Yangchuling porphyry W deposit. It explains theDahutang granite related tungsten ore field shares a nearly contem-poraneous age with the porphyry W–Mo deposits and the porphyry–skarn Cu–Au–Mo–Fe deposits in the mineral province.

The trace Re content in molybdenite has been used to trace thesource of the Mo in the ores and by implication of the associatedmetals such as W. Literature data indicate progressive Re decreasefrom >100 ppm in Mo derived from mantle sources through tens ofppm for mixed mantle/crust source to b10 ppm for crustal sources(Berzina et al., 2005; Mao et al., 1999, 2008). As shown in Table 1,the Re contents in the Dahutang molybdenite are between 0.5 ppmand 7.8 ppm, suggesting an upper crustal Mo source genetically relat-ed to granitic magmas formed by partial melting of the continentallithosphere. The same order of magnitude of trace Re in molybdenite(Re: 0.03–2.6 ppm) was reported by Li and Mao (1996), Peng et al.(2006), Mao et al. (2004, 2007) and Feng et al. (2011a,b) for thegranite-related W–Sn deposits in the Nanling region in South China.This, however, contrasts with the Re in molybdenite values inporphyry–skarn type Cu–Au–Mo–Fe in the Middle–Lower Yangtzeregion, reported as ranging from 53 ppm to 1169 ppm and con-sidered sourced from melts derived from the subducting slab(Mao et al., 2006, 2011) and/or oceanic ridge (Ling et al., 2009).

The metallogenic contrast between two roughly parallel mineral-ized belts of approximately the same age in the Yangtze ore provincementioned earlier: the YRB porphyry–skarn Cu–Au–Mo–Fe belt andthe granite-related W-(Mo, Cu) belt but have different metal sources.On the other hand, the latter is comparable with the Nanling W–Sn

Table 1Molybdenite Re/Os values of the Dahutang tungsten deposits, northwestern Jiangxi, China.

Analyzed no. Sample no. Ore types Weight (g) Re ng/g 187Re ng/g 187Os ng/g Model ages (Ma)

Measured 2σ Measured 2σ Measured 2σ Measured 2σ

120605-17 DHT-1 Type 2 0.10222 4059 36 2551 23 5.994 0.050 140.9 2.1120605-18 DHT-13 Type 1 0.15423 2417 24 1519 15 3.569 0.033 140.8 2.2120605-19 DHT-14 Type 1 0.15054 2508 22 1576 14 3.651 0.037 138.9 2.2120525-18 DHT-7 Type 3 0.10486 7872 67 4948 42 11.42 0.09 138.4 2.0120516-1 DHT-7 Duplication 0.10100 7879 62 4952 39 11.60 0.14 140.4 2.3120510-3 DHT-8 Type 3 0.30124 549.5 5.7 345.4 3.6 0.8281 0.0082 143.8 2.4

Note: Type 1: veinlets-disseminated ore, type 2: crypto-explosive brecciated ore, type 3: wolframite–scheelite quartz veins.Decay constant: The ISOPLOT software of Ludwig (1999) was used to calculate the isochron age, decay constant: λ(187Re)=1.666×10–11/year (Smoliar et al., 1996), uncertaintiesare absolute at 2σ with error on Re and 187Os concentrations and the uncertainty in the 187Re decay constant.

Fig. 11. Proposed model showing the spatial disposition of the W deposits, related tocrustal melting along NYCT and the porphyry–skarn Cu–Mo–Au–Fe deposits alongthe YRB (a), triggered by slab window, and the three types of tungsten ores:veinlets-disseminated, quartz–wolframite (scheelite) vein and breccia ores (b).

431Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

province of crustal derivation (Chang et al., 1991; Chen, 1983; Chen etal., 1989; Zhai et al., 1992). In the early 1980's, the Yangchulingporphyry W–Mo deposit was discovered and explored in the north-ern margin of the Yangtze Craton, followed by the Xianglushanskarn-type tungsten deposit explored in 1990's (Fig. 1). Althoughgeographically close to the YRB, the metallogenic type and ore styleare more similar to the Nanling Sn–W system related to crustal gra-nitic melts.

Our results integrated with published data, now make it possibleto define an independent tungsten metallogenic belt that is parallelwith the long known Yangtze River Fe–Cu–Au–Mo porphyry–skarnbelt (YRB). We propose to name the Dahutang ore field and depositsin the same area as the North Yangtze Craton tungsten belt (NYCT). Inaddition to the near super large Dahutang tungsten ore field it alsocontains Jitoushan and other recently discovered porphyryW–Mo de-posits (Fig. 1). Both metallogenic belts originated at approximatelythe same time with ages between 143 and 137 Ma(Li et al., 2010;Mao et al., 2006, 2011; Xie et al., 2007; Zhao et al., 2006; Zhou et al.,2008).

6.3. Geodynamic interpretation

Both metallogenic belts defined above: YRB and NYCT, are close inspace and time, but have a different selection of the ore metals. Thissuggests different source relationships at the onset of developmentof the ore-forming system.

Chang et al. (1991) and Zhai et al. (1992) proposed a strong inter-action between mantle and crust to explain the origin of theYanshanian I-type granitoids parental to the YRB metallogenic belt.Zhang et al. (2001a,b) compared the same granitoids with theadakites, produced by partial melting of intermediate-mafic granu-lites in the deep lower crust under high P–T conditions. Mao et al.(2006) placed the origin of the porphyry–skarn Cu–Au–Mo–Fe de-posits into the 160 to 135 Ma time interval during which the principalN–S stress field in eastern China continent changed progressively toan E–W orientation, due to the subduction of the Paleo-Pacific Platebeneath the Eurasian Plate. Ling et al. (2009), by contrast, proposeda Cretaceous oceanic ridge subduction to explain the 140–125 Mamagmatism and associated metallogenesis. Most recently, using geo-logical observations, petrochemistry and Sr/Nd isotopic data, Mao etal. (2011) concluded that the eastern part of the Eurasian continentwas an active continental margin at ca. 180 Ma, as the Izanagi Platesubducted orthogonally beneath the continent. At ca. 160 Ma thisplate rotated clockwise towards the north with subduction orienta-tion becoming oblique with respect to the continental margin.This triggered emplacement of large amounts of granite magmain the back-arc setting associated with metallic mineralization con-trolled by regional NE–SW strike-slip faults. The geochronologicaldata obtained for the Middle–Lower Yangtze River region consis-tently indicate that the Tan–Lu regional strike-slip fault zone wasinitiated between 233±6 and 225±6 Ma and, due to the Izanagi

oblique subduction, underwent reactivation at ca. 160 Ma. High-Kcalc-alkaline granitoid magmas, derived from slab melting withinputs from the crust, were intruded at N–E and E–W fault inter-sections, followed by the YRB Fe–Cu–Au–Mo-deposits between143 and 137 Ma.

The peraluminous (S-type, ilmenite-series) granites, generated bypartial melting of crustal material, with their genetically-relatedNYCT tungsten metallogenic belt, developed in the same tectonicsetting as the YRB, but from different magma source materials.During the 143–137 Ma period the asthenosphere rising alongthe window in the subducting slab induced melting of the overly-ing continental crust producing the peraluminous magma (Fig. 11a).The ascent of the fractionating volatiles-rich buoyant magma into thenear-surface region resulted in exsolution of the magmatic

432 Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

hydrothermal fluid resulting in strong alkali metasomatism,greisenization and silicification in the roof zones and roof pendants ac-companied by, or followed by, the W-(Mo, Cu) metallic mineralizationin three styles (Fig. 11b).

7. Conclusions

The recently discovered and explored Dahutang is the world'slargest tungsten ore fields. It is located south of the Middle–Lower Yangtze River Fe–Cu–Au–Mo–porphyry–skarn belt datedat 143–137 Ma. In this contribution we discuss the essential char-acteristics of the Dahutang deposit in terms of geology, style ofmineralization, hydrothermal alteration and mineralization. Wealso provide new Re/Os isotopic data in molybdenite, resultingin a model age of the W mineralization ranging from 138.4 Mato 143.8 Ma, and an isochron age of 139.18±0.97 Ma (MSWD=2.9).The very low trace Re content in molybdenite of 0.5 to 7.8 ppm in-dicates the involvement of upper continental crustal as a source forthe parental granite magmas. This contrasts with the 53 ppm to1169 ppm Re values in molybdenites from the YRB Fe–Cu–Au–Mometallogeny, indicative of a mantle source for parent magmasand metals. We have defined a new NYCT tungsten-dominatedmetallogenic belt along the northern margin of the Yangtze Cratonthat, despite the close time–space relationship and comparable set-ting with the YRB belt, had a different source of magmas; this wasresponsible for the formation of two subparallel mineralized beltswith contrasting selection of ore metals.

Acknowledgments

We would like to thank Prof. Peter Laznicka for project supervi-sion, and Prof. Franco Pirajno and other anonymous reviewers fortheir critical and constructive reviews. We are also grateful toMr. Huang Shuibao, Mr. Liu Xianmu, Mr. Wu Jianping and theirco-workers from the Jiangxi Bureau of Geology, Mineral Resources,Exploration and Development, and its affiliated No. 916 GeologicalTeam and Northwestern Geological Team, for field guidance andconstructive discussions. This research is jointly funded by the Na-tional Nature Science Foundation of China (no. 40930419) and theproject of China Geological Survey (no. 121201112083).

References

Berzina, A.N., Sotnikov, V.L., Economou-Eliopoulos, M., Eliopoulos, D.C., 2005. Distribu-tion of rhenium in molybdenite from porphyry Cu–Mo and Mo–Cu deposits ofRussia (Siberia) and Mongolia. Ore Geol. Rev. 26, 91–113.

Černý, P., Blevin, P.L., Cuney, M., London, D., 2005. Granite-related ore deposits. Eco-nomic Geology 100th Anniversary Vol, pp. 337–370.

Chang, Y.F., Liu, X.P., Wu, C.Y., 1991. The Copper–Iron Belt of the Lower and Middle Reachesof the Changjiang River. Geological Publishing House, Beijing (234 pp. (in Chinese)).

Chen, Y.C., 1983. The metallogenic series of the rare-earth, rare and nonferrous metal de-posits related to the Yanshanian granites in south China. Miner. Deposits 2 (2), 15–24.

Chen, Y.C., Pei, R.F., Zhang, H.L., 1989. The Geology of Non-Ferrous and Rare Metal De-posits Related to Mesozoic Granitoids in Nanling Region. Geological PublishingHouse, Beijing, pp. 1–506 (in Chinese).

Davis, W.J., William-Jones, A.E., 1985. A fluid inclusion study of the porphyry–greisen,tungsten–molybdenum deposit at Mount Pleasant, New Brunswick, Canada.Miner. Deposita 20, 94–101.

Du, A.D., Wu, S.Q., Sun, D.Z., Wang, S.X., Qu, W.J., Markey, R., Stein, H., Morgan, J.W.,Malinovskiy, D., 2004. Preparation and certification of Re–Os dating referencematerials: molybdenite HLP and JDC. Geostand. Geoanal. Res. 28, 41–52.

Feng, C.Y., Zeng, Z.L., Zhang, D.Q., Qu, W.J., Du, A.D., Li, D.X., She, H.Q., 2011a. SHRIMPzircon U–Pb and molybdenite Re–Os isotopic dating of the tungsten deposits inthe Tianmenshan–Hongtaoling W–Sn orefield, southern Jiangxi Province, China,and geological implications. Ore Geol. Rev. 43, 8–25.

Feng, C.Y., Huang, F., Zeng, Z.L., Qu, W.J., Ding, M., 2011b. Isotopic chronology ofJiulongnao granite and Hongshuizhai greisens-type tungsten deposit in SouthJiangxi Province. J. Jilin Univ. (Earth Sci. Ed.) 41, 112–121.

Gao, L.Z., Chen, J., Ding, X.Z., Liu, Y.R., Zhang, C.H., Zhang, H., Liu, Y.X., Pang, W.H., Zhang,Y.H., 2011. Zircon SHRIMP U–Pb dating of the tuff bed of Lengjiaxi and BanxiGroups, northeastern Hunan: constraints on the Wuling Movement. Geol. Bull.China 30, 1001–1008 (in Chinese with English abstract).

Laznicka, P., 2006. Giant Metallic Deposits, Future Sources of Industrial Metals. Springer,Heidelberg (732 pp.).

Laznicka, P., 2010. GiantMetallic Deposits, Future Sources of Industrial Metals, 2nd Edition.Springer, Heidelberg (961 pp.).

Li, Y.D., 1993. Poly-type models for tungsten deposits and vertical structural zoningmodel for vein-type tungsten deposits in South China. In: Kirkham, R.V., Sinclair,W.D., Duke, J.M. (Eds.), Mineral Deposit Modeling: Geol. Assoc Can. Special paper,40, pp. 555–568.

Li, H.Y., Mao, J.W., 1996. Re–Os isotopic chronology of molybdenites in the Shizhuyuanpolymetallic tungsten deposit, South China. Geol. Rev. 42, 261–267 (in Chinesewith English abstract).

Li, J.W., Deng, X.D., Zhou, M.F., Liu, Y.S., Zhao, X.F., Guo, J.L., 2010. Laser ablation ICP-MStitanite U–Th–Pb dating of hydrothermal ore deposits: a case study of the TonglushanCu–Fe–Au skarn deposite, SE Hubei Province, China. Chem. Geol. 270, 56–67.

Ling, M.X., Wang, F.Y., Ding, X., Hu, Y.H., Zartman, R.E., Xiong, X.L., Sun, W.D., 2009. Cre-taceous ridge subduction along the Lower Yangtze River belt, Eastern China. Econ.Geol. 104, 303–321.

Ludwig, K.R., 1999. Isoplot/Ex, version 2.0: a geochrological toolkit for Microsoft Excel.Special Publication, 1a. Geochronology Center, Berkeley.

Ludwig, K.R., 2004. Isoplto/Ex, Version 3.0: A Geochronological Toolkit for MicrosoftExcel. Berkeley Geochronology Center, Berkeley, California.

Man, F.S., Wang, X.S., 1988. Isotopic geochronolgy of the Yangchuling porphyrytungsten–molybdenum deposit. Geol. Miner. Resour. (1) (6-1-66 (in Chinese)).

Mao, J.W., Li, H.Y., 1996. Geology and metallogeny of the Shizhuyuan skarn–greisen de-posit, Hunan Province, China. Int. Geol. Rev. 38, 1020–1039.

Mao, J.W., Zhang, Z.C., Zhang, Z.H., Du, A.D., 1999. Re–Os dating of molybdenites in theXiaoliugou W-(Mo) deposit in the northern Qilian Mountains and its geologicalsignificances. Geochim. Cosmochim. Acta 63, 1815–1818.

Mao, J.W., Xie, G.Q., Li, X.F., 2004. Mesozoic large scale mineralization and multiplelithospheric extensions from South China. Earth Sci. Front. 11 (1), 45–56 (in Chinesewith English abstract).

Mao, J.W., Wang, Y.T., Lehmann, B., Yu, J.J., Du, A.D., Mei, Y.X., Li, Y.F., Zang, W.S., Stein,H.J., Zhou, T.F., 2006. Molybdenite Re–Os and albite 40Ar/39Ar dating of Cu–Au–Moand magnetite porphyry systems in the Changjiang valley and metallogenic impli-cations. Ore Geol. Rev. 29, 307–324.

Mao, J.W., Xie, G.Q., Guo, C.L., Chen, Y.C., 2007. Large-scale tungsten–tin mineralizationin Nanling area of South China: metallogenic ages and corresponding geodynamicprocess. Acta Petrol. Sin. 23, 2329–2338 (in Chinese with English abstract).

Mao, J.W., Xie, G.Q., Guo, C.L., Yuan, S.D., Cheng, Y.B., Chen, Y.C., 2008. Spatial–temporaldistribution of Mesozoic ore deposits in South China and their metallogenic set-tings. Geol. J. China Univ. 14, 510–526 (in Chinese with English abstract).

Mao, J.W., Shao, Y.J., Xie, G.Q., Zhang, J.D., Chen, Y.C., 2009. Mineral deposit model forporphyry–skarn polymetallic copper deposits in Tongling ore dense district of Middle–Lower Yangtze Valley metallogenic belt. Miner. Deposits 28, 109–119 (in Chinese withEnglish abstract).

Mao, J.W., Xie, G.Q., Duan, C., Pirajno, F., Ishiyama, D., Chen, Y.C., 2011. A tectonogeneticmodel for porphyry–skarn-strata bound Cu–Au–Mo–Fe and magnetite–apatite de-posits along the Middle–Lower Yangtze River Valley, Eastern China. Ore Geol. Rev.43, 294–314.

Mao, J.W., Cheng, Y.B., Chen, M.H., Pirajno, F., 2012. Major types and time–space distri-bution of Mesozoic ore deposits in South China and their geodynamic settings.Miner. Deposita. http://dx.doi.org/10.1007/s00126-012-0446-z.

No. 916 Geological Team, Jiangxi Bureau of Geology, Mineral Resources, Explorationand Development, 2012. The Exploration Report of the Shimensi, North Portionof the Dahutang Tungsten Deposit, Wuning County, Jiangxi Province. Jiangxi JutongMining Corporation (224 pp.).

Noble, S.R., Spooner, E.T.C., Harris, F.H., 1984. The Logtung large tonnage, low-grade W(scheelite)–Mo porphyry deposit, south-central Yukon Territory. Econ. Geol. 79,848–868.

Northwestern Geological Team, Jiangxi Bureau of Geology, Mineral Resources,Exploration and Development, 2012. The Exploration Report of the Shiweidong,South Portion of the Dahutang Tungsten Deposit, Wuning County, Jiangxi Province.Jiangxi Jutong Mining Corporation (108 pp.).

Pan, Y.M., Dong, P., 1999. The Lower Changjiang (Yangzi/Yangtze River) metallogenicbelt, East China: intrusion- and wall rock-hosted Cu–Fe–Au, Mo, Zn, Pb, Ag de-posits. Ore Geol. Rev. 15, 177–242.

Parrish, I.S., Tully, J.V., 1978. Porphyry tungsten zones at Mt Pleasant, New Brunswick.C.I.M. Bull. , pp. 93–100 (June 1978).

Peng, J.T., Zhou, M.F., Hu, R.Z., 2006. Precise molybdenite Re–Os and mica Ar–Ar datingof the Mesozoic Yaogangxian tungsten deposit, central Nanling district, SouthChina. Miner. Deposita 41, 661–669.

Pirajno, F., 2009. Hydrothermal Processes and Mineral Systems. Springer, Berlin (1250 pp.).Pirajno, F., 2012. Effects of metasomatism on mineral systems and their host rocks:

alkali metasomatism, skarns, greisens, tourmalinites, rodingites, black-wall alter-ation and listvenites. In: Harlov, D.E., Austrheim, H. (Eds.), Metasomatism andMetamorphism: The Role of Fluids in Crustal and Upper Mantle Processes. : LectureSeries in Earth Science. Springer, pp. 203–252.

Rösler, H.J., Baumann, L., Jung, W., 1968. Postmagmatic mineral deposits of the north-ern edge of the Bohemian Massif. 23th Intern. Geol. Congress, Prague, Guide to Ex-cursions 22 AC (57 pp.).

Rundqvist, D.V., Denisenko, V.R., Pavlova, I.G., 1971. Greisen Deposits. NEDRA Publish-ing House, Moscow, p. 328 (in Russian).

Selby, D., Creaser, A., 2004. Macroscale NTIMS and microscale LA-MC-ICP-MS Re–Osisotopic analysis of molybdenite: testing spatial restrictions for reliable Re–Osage determinations, and implications for the decoupling of Re and Os within mo-lybdenite. Geochim. Cosmochim. Acta 68, 3897–3908.

433Z. Mao et al. / Ore Geology Reviews 53 (2013) 422–433

Shelton, K.L., Taylor, R.P., So, C.S., 1987. Stable isotope studies of the DaeHwa tungsten–molybdenum mine, Republic of Korea: evidence of progressive meteoric water in-teraction in a tungsten-bearing hydrothermal system. Econ. Geol. 82, 471–481.

Shirey, S.B., Walker, R.J., 1995. Carius tube digestion for low-blank rhenium–osmiumanalysis. Anal. Chem. 67, 2136–2141.

Sinclair, D., 2007. Porphyry deposit. In: Goodfellow, W.D. (Ed.), Mineral Deposits ofCanada. A Synthesis of Major Deposit Types: Geol. Association of Canada, MineralDeposit Division, Special Publication No.5, Ottawa, pp. 223–243.

Smoliar, M.I., Walker, R.J., Morgan, J.W., 1996. Re–Os ages of group IIA, IIIA, IVA and VIBiron meteorites. Science 271, 1099–1102.

So, C.S., Rye, D.M., Shelton, K.L., 1983a. Carbon, hydrogen, oxygen, and sulfur isotopeand fluid inclusion study of the Weolag tungsten–molybdenum deposit, Republicof Korea: fluid histories of metamorphic and ore-forming events. Econ. Geol. 78,1551–1573.

So, C.S., Shelton, K.L., Seidemann, D.E., Skinner, B.J., 1983b. The DaeHwa tungsten–molybdenum mine, Republic of Korea: a geochemical study. Econ. Geol. 78,920–930.

Song, G.X., Qin, K.Z., Li, G.M., Liu, T.B., Li, J.X., Chang, Z.S., 2012. Geochronologic and isotopegeochemical constraints on magmatism and associated W–Mo mineralization of theJitoushan W–Mo deposit, middle–lower Yangtze Valley. Int. Geol. Rev. 54, 1532–1547.

Stein, H.J., Markey, R.J., Morgan, J.W., 1997. Highly precise and accurate Re–Os ages formolybdenite from the East Qinling molybdenum belt, Shaanxi Province, China.Econ. Geol. 92, 827–835.

Stein, H.J., Scherste'n, K., Hannah, J.L., Markey, R., 2003. Subgrain-scale decoupling of Reand 187Os and assessment of laser ablation ICP-MS spot dating in molybdenite.Geochim. Cosmochim. Acta 92, 827–835.

Štemprok, M., Pivec, E., Lang, M., Novák, J.K., 1995. Phosphorus in the younger granitesof the KrušnéHory (Erzgebirge) batholith. In: Pašava, J., Kribek, B., Zak, K. (Eds.),

Mineral Deposits, From Their Origin to Their Environmental Impact. Balkema,Rotterdam, pp. 535–537.

Tan, Y.J., 1985. Ore-forming mechanism of the Lianhuashan porphyry tungsten deposit.Sci. China B 563–570 (in Chinese).

Xie, G.Q., Mao, J.W., Li, R.L., Qu, W.J., Pirajno, F., Du, A.D., 2007. Re–Os molybdenite andAr–Ar phlogopite dating of Cu–Fe–Au–Mo (W) deposits in southeastern Hubei,China. Mineral. Petrol. 90, 249–270.

Zhai, Y.S., Yao, S.Z., Lin, X.D., Zhou, X.N., Wan, T.F., Jin, F.Q., Zhou, Z.G., 1992. Fe–Cu–AuMetallogeny of the Middle–Lower Changjiang Region. Geological PublishingHouse, Beijing (235 pp. (in Chinese)).

Zhang, Q., Qian, Q., Wang, E.C., Wang, Y., Zhao, T.P., Hao, J., Guo, G.J., 2001a. Existence ofEast China plateau in mid-late Yanshan period: implication from adakites. Sci.Geol. Sin. 36, 248–255 (in Chinese with English abstract).

Zhang, Q., Wang, Y., Qian, Q., Yang, J.H., Wang, Y.L., Zhao, T.P., Guo, G.J., 2001b. The char-acteristics and tectonic–metallogenic significances of the adakites in Yanshan periodfrom eastern China. Acta Petrol. Sin. 17, 236–244 (in Chinese with English abstract).

Zhao, X.F., Li, J.W., Ma, C.Q., 2006. 40Ar/39Ar geochronology of the Tongshankou Cu(Mo) deposit in the Southeastern Hubei Fe–Cu Province: implication for regionalmetallogeny. Acta Geol. Sin. 86, 849–862 (in Chinese with English abstract).

Zhong, Y.F., Ma, C.Q., She, Z.B., Lin, G.C., Xu, H.J., Wang, R.J., Yang, K.G., Liu, Q., 2005.SHRIMP U–Pb zircon geochronology of the Jiuling granitic complex batholith inJiangxi province. Earth Sci. 30, 685–691 (in Chinese with English abstract).

Zhou, T.F., Fan, Y., Yuan, F., 2008. Advances on petrogenesis and metallogenic study ofthe mineralization belt of the Middle–Lower Reaches of the Yangtze River area.Acta Petrol. Sin. 24, 1665–1678 (in Chinese with English abstract).