Re–Os Geochronology of Molybdenite from Yinyan Porphyry Sn ...€¦ · Short Communication Re–Os Geochronology of Molybdenite from Yinyan Porphyry Sn Deposit in South China Wei

Short Communication

Re–Os Geochronology of Molybdenite from YinyanPorphyry Sn Deposit in South China

Wei ZHENG,1 JING-WEN MAO,2 CAI-SHENG ZHAO,3 HE-GEN OUYANG2AND XIAO-YU WANG

1

1School of the Earth Science and Mineral Resources, China University of Geosciences, Beijing 100083, 2MLR Laboratory ofMetallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, and3Technology and International Cooperation Department, Ministry of Land and Resources, Beijing 100812, China

Abstract

The Yinyan Sn deposit, one of the three typical porphyry Sn deposits in China, is located in the westernGuangdong province of the Cathaysia Block. Rhenium and osmium isotopes of molybdenites from theYinyan deposit were first used to constrain the age of mineralization. Rhenium concentrations in molybde-nite samples range from 0.13 to 1.3μgg�1, indicating a crustal source for the ore-forming materials. TheRe–Os dating yield model ages ranging from 78.1 to 79.52Ma, with an average of 78.65 ± 0.98Ma, and givean isochron age of 78.8 ± 2.6Ma. Evidently, isochron age is consistent with model ages in the error within theallowable range, so we can constrain the precise age of Yinyan Sn deposit at the Late Cretaceous. Based onthe geological history and spatial-temporal distribution of the Sn deposits, it is proposed that the formationof Sn deposits in the Cathaysia Block were related to lithospheric extension that are associated with a changein the polarity of the subduction of the Paleo-Pacific Plate from oblique subduction to parallel the easternmargin of the Eurasian Plate after 135Ma.

Keywords: molybdenite, porphyry Sn deposit, Re–Os geochronology, Yinyan, Cathaysia Block.

1. Introduction

Most of the primary tin deposits of the world occur inor adjacent to intrusive granitoids (Groves &McCarthy,1978), although lavas and/or subvolcanic felsic intru-sives may be important hosts to tin mineralization(Sillitoe et al., 1975; Taylor, 1976). The majority of de-posits are confined to Palaeozoic, Mesozoic or Tertiaryorogenic belts (Itsikson, 1960), particularly around thePacific margin (Hosking, 1970; Mitchell & Garson,1972). South China is famous for its large-scalemagmatism and mineralization in the Mesozoic, withmore than 50% of the world’s W and Sb reserves and20% of the world’s total Sn reserves, all of which rank

No.1 in the world (Sun et al., 2012). The Yinyan depositis one of the three typical porphyry Sn deposits inChina, located in the western Guangdong province ofthe Cathaysia Block (Fig. 1).

Accurate and precise age determination of minerali-zation is critical in understanding the timing of ore-formings as well as for providing indicators for mineralexploration (Yuan et al., 2008a). During recent decades,direct isotopic dating of ore minerals has received in-creasing attention (Mao et al., 1999, 2002, 2006; Yuanet al., 2008b, 2015; Zheng et al., 2013a, b), especiallyRe–Os dating of molybdenite is a well-establishedmethod for obtaining ages for intrusion-associatedmineralization (Stein et al., 2001; Mao et al., 2002). This

Received 27 May 2015. Accepted for publication 17 September 2015.Corresponding author: W. ZHENG, School of the Earth Science and Mineral Resources, China University of Geosciences, 29 XueyuanRoad, Beijing 100083, China. Email: [email protected]

doi: 10.1111/rge.12087 Resour Geol Vol. 66, No. 1: 63–70

© 2015 The Society of Resource Geology63

bs_bs_banner

study firstly reports Re–Os ages of molybdenite as-sociated with cassiterite in the Yinyan porphyry Sn de-posit in order to constrain the age of Sn mineralizationof the deposit and provide constraints on the regionalgeodynamic process of ore genesis.

2. Geologic background

The South China Block consists of two blocks in-volving the Cathaysia Block to the southeast and theYangtze Block to the northwest (Fig. 1a; Wang et al.,2007). As one of the major continents in Asia, the SouthChina Block (SCB) has experienced significant, epi-sodic intra-continental magmatism and deformationsince the Neo-proterozoic (Zhou & Li, 2000; Li & Li,2007). It is a complex continental plate resulting frommultiple amalgamation, breakup and re-amalgamationof the Cathaysian and Yangtze blocks during its geo-logical historic evolution (Mao et al., 2006). TheCathaysian and Yangtze blocks have distinctive crustalages and tectonic histories (Qiu et al., 2000). The base-ment of the Yangtze Block comprises of Archean toProterozoic rocks exposed in the western regions(Zheng et al., 2006) while the Cathaysia Block has awidespread Proterozoic basement (Chen & Jahn, 1998;Xu et al., 2007). During the late Mesozoic, South Chinawas characterized by widespread and intensivemagmatism, associated with the deposition of econom-ically significant polymetallic mineralization. In theMesozoic, especially the Cretaceous, the relationshipsbetween large-scale geological events, granite

generation and related mineralization have receivedconsiderable attention from many researchers (Maoet al., 2007, 2013; Yuan et al., 2015).

3. Deposit geology

The main strata of Yinyan deposit seen in outcrop arefrom the Cambrian Bacun group, and are composedof quartz schist and biotite gneiss (Fig. 2). The fracturesystems in the Yinyan deposit are well-developed, andare filled with the cassiterite-sulfide veins and quartz-porphyry veins. Based on the fieldmapping and petrog-raphy observation, the intrusive rocks include graniteporphyry, quartz porphyry and fine grainedmonzoniticgranites, in which granite porphyry and quartz por-phyry are closely related to mineralization. The ore-bearing porphyries show ellipse shapes at the surface,and the interface against the wall rocks is quite steep.Quartz porphyries crop out along the fractures in thearea, and graduate into granite porphyry in depth.

There are two types of tin mineralization in the orefield: porphyry-type tin deposit and adjacent vein-typetin deposit. Most of the orebodies are distributed in theinterior of granite porphyry, with some of the orebodieshosted in the quartz-porphyry veins and the fracturesof wall rock. The ore grade of granite porphyry de-creases from the center to the edge of the orebody, inthe lower parts of which occur the Sn–Mo–Worebodies.Themainmetallic minerals in the deposit are cassiterite,wolframite, bismuthinite, molybdenite, pyrite, chalco-pyrite, with small amounts of galena, sphalerite and

Fig. 1 Distribution of tin deposits in theCathaysia block (adapted from Maoet al., 2007).

W. Zheng et al.


magnetite. Gangue minerals mainly are quartz, sericite,chlorite and topaz, followed by fluorite, and biotite etc.Mineralization styles include disseminations and veins,exhibiting euhedral-subhedral andmetasomatic-residualcorrosion textures. Cassiterite shows brown and lightbrown in color, and coexists with other ore minerals inthe following two forms: (i) disseminated or conglomer-atic forms in the altered rock with grain size of 0.05–0.15mm; (ii) showing veinlet forms in the quartz-topazfine vein, greisen fine vein and clinochlore fine vein withgrain size of 0.01–0.08mm.In the mining district, hydrothermal alteration is

dominated by potassic-silicate alteration, greisenization,and sericite–quartz alteration as well as some silicifica-tion. The mineralization is closely related to the hydro-thermal alteration. Hydrothermal alteration in Yinyanore district is well zoned, and characterized by potassic-silicate alteration in the inner zone, potassic-silicate al-eration zone overprinted by greisenization alterationzone, topaz-greisenization alteration zone, and sericite–quartz alteration zone in the ore-bearing granite por-phyry in the outer zone (Fig. 3, Guan et al., 1985). TheSn–Mo–W mineralization is restricted to the potassic-silicate alteration zone overprinted by greisenization al-teration zone and topaz-greisenization alteration zone.As the greisenization alteration becomes stronger, theSn mineralization is more enriched. Correspondingly,the metal zoning is as follows: tungsten–molybdenum–tin→ tin–molybdenum–bismuth→ tin.

4. Analytical methods

Molybdenite samples (Fig. 4) for Re–Os analyses wascollected from the outcrop of the Yinyan Sn deposit.YY-4 and YY-5 were recovered from 111°18′2″ E, 22°20′32″ N and 111°18′21″ E, 22°20′27″ N, respectively;YY-7 and YY-9 were obtained from 111°17′43″ E, 22°20′33″ N and 111°17′56″ E, 22°20′35″ N, respectively.Re–Os isotope analyses were performed in the Re–OsLaboratory, National Research Center of Geoanalysis,Chinese Academy of Geological Sciences in Beijing.The detailed process of analysis was described in somelisted references (Du et al., 2004). The chemical separa-tion procedure is briefly described here.

Enriched 190Os and 185Re were obtained from theOak Ridge National Laboratory. A Carius tube diges-tion was used. The weighed sample was loaded in aCarius tube through a thin-neck long funnel. Themixed 185Re and 190Os spike solutions and 2mL of10mol/L HCl and 6mL of 16mol/L HNO3 wereloaded while the bottom part of the tube was frozenat –80 °C to –50 °C in an ethanol–liquid nitrogen slush;the top was sealed using an oxygen-propane torch. Thetube was then placed in a stainless-steel jacket andheated for 10 h at 230 °C. Upon cooling, the bottompart of the tube was kept frozen, the neck of the tubewas broken, and the contents of the tube were pouredinto a distillation flask and the residue was washedout with 40mL of water.

Fig. 2 Simplified geological map of theYinyan porphyry Sn deposit (adaptedfrom Wu, 1983).

Re–Os geochronology, Yinyan Porphyry Sn deposit


Os was distilled twice. In the first distillation step,OsO4 was distilled at 105–110 °C for 50min andtrapped in 10mL of water. The residual Re-bearing so-lution was saved in a 50-mL beaker for Re separation.The water trap solution plus 40mL of water was dis-tilled a second time. The OsO4 was distilled for 1 hand trapped in 10mL of water, which was used forICPMS (TJA PQ ExCell) determination of the Os iso-tope ratio.

The Re-bearing solution was evaporated to dryness,and 1mL of water was added twice with heating tonear-dryness. An aliquot of 10mL of 5mol/L NaOHwas added to the residue followed by Re extractionwith 10mL of acetone in a 120-mL teflon separationfunnel. The water phase was then discarded and theacetone phase washed with 2mL of 5mol/L NaOH.

The acetone phase was transferred to a 100-mL beakerthat contained 2mL of water. After evaporation to dry-ness, the Re was picked up in 1mL of water, which wasused for the ICPMS determination of the Re isotope ra-tio. Cation-exchange resin was used to remove Na ifthe salinity of the Re-bearing solution was greater than1mg/mL.

The instrument used in this work was a TJA PQExCell inductively coupled plasma (ICP)-mass spec-trometer. Selected isotopes for the measurement ofRe were 185Re and 187Re. Sometimes a Re-bearing so-lution contained a little incompletely separated 187Os,which would contribute to 187Re. 190Os was selectedas the monitor for 187Os. The isotopes selected for Osmeasurement were 187Os, 190Os and 192Os. Sometimesthe OsO4 trap solution contained a little 187Re, which

Fig. 3 Geological profile of No. 50exploration line in the Yinyan Sndeposit (adapted from Guan et al.,1985). Abbreviations: K–Q, potassic–silicate alteration zone; K–G, potassic–silicate alteration zone overprinted bygreisenization alteration; T–G, topaz–greisenization alteration zone; S–Q,sericite–quartz alteration zone.

W. Zheng et al.


had not been separated and would thus contribute to187Os. 185Re was selected as the monitor for this 187Recontribution.

5. Re–Os geochronology

The Re concentrations usually are high while thecommon Os concentrations in molybdenite are verylow, so almost all the osmium in molybdenite is ra-diogenic 187Os decayed from 187Re. Thus, the Re–Osage is calculated with the concentrations of 187Osand 187Re in molybdenite using the equation: t = (1/λ)ln(1 + 187Os/187Re), assuming the common Os inmolybdenite is negligible. The decay constant of187Re, λ, is 1.666 × 10-11a-1 (Smoliar et al., 1996). Theconcentrations of Re and Os and the osmium isotopiccompositions of molybdenite from the Yinyan depositare shown in Table 1. The total Re concentrations ofmolybdenite range from 0.13 to 1.27 μg g-1 and

commonOs concentrations of molybdenite range from0.11 to 1.05 ng g-1. The ages of different analyses aresimilar to each other within error, ranging from 78.1to 79.5Ma for the four samples and a weighted meanage of 78.65 ± 0.98Ma (Fig. 5). The data, processedusing the SOPLOT/Ex program (Ludwig, 2003),yielded an isochron age of 78.8 ± 2.6Ma and withMSWD=4.5 (Fig. 5), which is identical to the averageof the four analyses within error, representing the for-mation age of the molybdenite.

Guan et al. (1985) obtained a crystallization age of80Ma for the Yinyan granite porphyry using thewhole-rock K–Ar isochron method. Fu and Chen(1992) reported U–Pb concordant age of 78.10Ma forthe granite porphyry. Although rock-forming age ofYinyan granite still lack a precise age, it is consistentwith the molybdenite Re–Os isochron age within therange of allowable error, which indicates that there isprobably a closely temporal and genetic relationshipbetween the mineralization and granite intrusion. The

Fig. 4 Photographs of molybdenite samples from the Yinyan deposit. (a) Pellicular molybdenite; (b) Fine grained molybde-nite occurring as disseminated sulfides in the quartz; (c) Molybdenite occurring as sulfide veins in quartz; (d) Molybdenitein dissemination in granite porphyry.



age data show that Yinyan deposit has a close relation-ship with the Late Cretaceous magmatic activities inwestern Guangdong.

6. Source of ore-forming material

Based on the published Re content in molybdenitefrom different types of Mo deposits in China, Maoet al. (1999) suggested that the rhenium contents inmolybdenite increase from a crust source via mixturesbetween mantle and crust to mantle (Mao et al., 1999).Stein et al. (2001) also suggested that deposits with acrust component in their source have significantlylower Re content than those deposits that are mantle-derived. Re–Os isotope analyses indicate that the Recontent in molybdenite from the Yinyan Sn depositranges from 0.13 to 1.27 ppm, with an average of0.74 ppm. The low Re content of molybdenites fromthe Yinyan porphyry Sn deposit may show that ore-forming material have a significant crustal component.

7. Implications for regional geodynamics

South China is characterized by its Mesozoic large-scale igneous event and associated mineralization

(Zhou & Li, 2000; Li & Li, 2007). There are manyfamous Sn-polymetallic deposits occurring on theCathaysia Block in South China, which mainly consistof porphyry, skarn, epithermal vein deposits, e.g. theworld-class Gejiu Sn–Cu deposit (83.4 ± 2.1Ma, Yanget al., 2008) and Dachang Sn deposit (94.52 ± 0.33Ma,Wang et al., 2004), Jiepailing Sn–Be–F deposit (92.1± 0.7Ma, Yuan et al., 2015), the Dajinshan granite-related W–Sn deposit (80.07 ± 1.19Ma, Yu et al.,2012), Dulong Sn deposit (82.0 ± 9.6Ma, Liu et al.,2007); Yingwuling W–Sn–Mo deposit (83.0 ± 1.7Ma,Zheng et al., 2013b); Damingshan W–Sn deposit(95.40 ± 0.97Ma, Li et al., 2008); which represented animportant Late Cretaceous W–Sn metallogenic eventin South China. The geodynamic setting of miner-alization in the late Mesozoic (135–80Ma) has beenattributed to a change in the polarity of the sub-duction of the Izanagi (or Paleo-Pacific) Plate fromoblique subduction to parallel the eastern margin ofthe Eurasian after 135Ma (Mao et al., 2011, 2013),which led to large-scale continental extension, accom-panied by significant granite magmatism, volcanism,and the formation of granite-related tin-tungstenmineralization. Therefore, the Yinyan deposit isthought to be the product of such a tectono-magmaticevent.

Table 1 Re–Os ages for molybdenite from the Yinyan porphyry Sn deposit

Samples Weight (g)Re (±2σ )(μg/g)

Common Os(±2σ ) (ng/g)

187Re (±2σ )(μg/g)

187Os (±2σ )(ng/g)

Model age(±2σ ) (Ma)

YY-4 0.12244 0.1324 0.0011 0.0051 0.0031 0.0832 0.0007 0.1097 0.0022 79.08 1.82YY-5 0.30016 0.9694 0.0077 0.0041 0.0004 0.6093 0.0048 0.8077 0.0071 79.52 1.14YY-7 0.05014 1.273 0.004 0.0497 0.0008 0.8001 0.0025 1.048 0.005 78.6 0.88YY-9 0.05015 0.5782 0.0017 0.0294 0.0006 0.3634 0.0011 0.4732 0.0022 78.1 0.87

Fig. 5 Re–Os isochron ages andweightedmean of Re-Os model ages of molybde-nites from the Yinyan Sn deposit.

W. Zheng et al.


Acknowledgments

This study was supported by National Science Founda-tion of China (Grant No. 41203036), the Beijing outstand-ing PhD research project (Grant No. 519002650744), theNational Basic Research Program of China (Grant No.2012CB416704). We thank Li Chao from Re–Os Labora-tory of National Research Center of Geoanalysis, ChineseAcademy of Geological Sciences in Beijing, for help withICP-MS analyses. We are grateful to Sun Jia and LuoMaocheng for a critical and constructive review of themanuscript and for many helpful suggestions.

References

Chen, J. F. and Jahn, B. (1998) Crustal evolution of southeasternChina: Nd and Sr isotopic evidence. Tectonophysics, 284,101–133.

Du, A. D., Wu, S. Q., Sun, D. Z., Wang, S. X., Qu, W. J., Markey, R.,Stein, H., Morgan, J. W. and Malinovskiy, D. (2004) Prepara-tion and certification of Re-Os dating reference materials: mo-lybdenite HLP and JDC. Geostand. Geoanal. Res., 28, 41–52.

Fu, C. L. and Chen, W. K. (1992) Descriptive model of the Yinyanporphyry tungsten deposit, Xinyi, Guangdong Province.Geol. China, 1, 20–23(in Chinese with English abstract).

Groves, D. I. and McCarthy, T. S. (1978) Fractional crystallizationand the origin of tin deposits in granitoids. Miner. Deposita, 8,171–181.

Guan, Y. F., Zhou, Y. Q., Xiao, J. H., Liang, S. Z. and Li, J. M.(1985) Yinyan porphyry tin deposit-a new type of tin depositsin China. Acta Geol. Sin., 59, 155–162(in Chinese with Englishabstract).

Hosking, K. F. G. (1970) The primary tin deposits of South-EastAsia. Min. Sci. Eng., 2, 24–50.

Itsikson, M. I. (1960) The distribution of tin-ore deposits withinfolded zones. Internat. Geol. Rev., 2, 397–417.

Li, S. L., Wang, D. H., Liang, T., Qu, W. J. and Ying, L. J. (2008)Metallogenic epochs of the Damingshan tungsten deposit inGuangxi and its prospecting potential. Acta Geol. Sin., 82,873–878(in Chinese with English abstract).

Li, Z. X. and Li, X. H. (2007) Formation of the 1300-km-wideintracontinental orogen and postorogenic magmatic provincein Mesozoic South China: a flat-slab subduction model.Geology, 35, 179–182.

Liu, Y. P., Li, Z. X. and Li, H. M. (2007) U-Pb geochronology ofcassiterite and zircon from the Dulong Sn-Zn deposit: evi-dence for Cretaceous large-scale granitic magmatism andmineralization events in southeastern Yunnan Province,China. Acta Petrol. Sin., 23, 967–976(in Chinese with Englishabstract).

Ludwig, K. R. (2003) User’s manual for Isoplot 3.00: a geochronologicaltoolkit for Microsoft Excel, Vol. 4, Berkeley GeochronologyCenter Special Publication, 1–70.

Mao, J. W., Zhang, Z. C., Zhang, Z. H. and Du, A. D. (1999) Re-Osisotopic dating of molybdenite in the Xiaoliugou W (Mo)deposit in the northern Qilian Mountain and its geologicalsignificance. Geochim. Cosmochim. Acta, 63, 1815–1818.

Mao, J. W., Lehmann, B., Du, A. D., Zhang, G. D., Ma, D. S.,Wang, Y. T., Zeng, M. G. and Kerrich, B. (2002) Re-Os datingof polymetallic Ni-Mo-PGE-Au mineralization in lowerCambrian black shales of South China and its geologic sig-nificance. Econ. Geol., 97, 1037–1049.

Mao, J. W., Xie, G. Q., Li, X. F., Zhang, C. Q. and Wang, Y. T.(2006) Mesozoic large-scale mineralization and multiple litho-spheric extensions in South China. Acta Geol. Sin. (Engl. Ed.),80, 420–431.

Mao, J. W., Xie, G. Q., Guo, C. L. and Chen, Y. C. (2007) Large-scale tungsten-tin mineralization in the Nanling region, SouthChina: metallogenic ages and corresponding geodynamic pro-cesses. Acta Petrol. Sin., 23, 2329–2338.

Mao, J. W., Chen, M. H., Yuan, S. D. and Guo, C. L. (2011) Geolog-ical characteristics of the Qinhang (or Shihang) metallogenicbelt in South China and spatial–temporal distribution regular-ity of mineral deposits. Acta Petrol. Sin., 85, 636–658 (inChinese with English abstract).

Mao, J. W., Cheng, Y. B., Chen, M. H. and Pirajno, F. (2013) Majortypes and time-space distribution of Mesozoic ore deposits inSouth China and their geodynamic settings. Miner. Deposita,48, 267–294.

Mitchell, A. H. G. and Garson, M. S. (1972) Relationship of por-phyry copper and circure-Pacific tin deposits to palaeo-Benioff zones. Trans. Instn. Mining Metall., 81B, 10–25.

Qiu, Y. M., Gao, S., McNaughton, N. J., Groves, D. I. and Ling, W.L. (2000) First evidence of >3.2 Ga continental crust in theYangtze craton of south China and its implications forArchean crustal evolution and Phanerozoic tectonics. Geology,28, 11–14.

Sillitoe, R. H., Halls, C. and Grant, J. N. (1975) Porphyry tin de-posits in Bolivia. Econ. Geol., 70, 913–927.

Smoliar, M. I., Walker, R. J. and Morgan, J. W. (1996) Re-Os ages ofgroup IIA, IIIA, IVA, and IVB iron meteorites. Science, 271,1099–1102.

Stein, H. J., Markey, R. J., Morgan, J. W., Hannah, J. L. andSchersten, A. (2001) The remarkable Re-Os chronometer inmolybdenite: how and why it works. Terra Nova, 13, 479–486.

Sun, W. D., Yang, X. Y., Fan, W. M. and Wu, F. Y. (2012) Mesozoiclarge scale magmatism and mineralization in South China:Preface. Lithos, 150, 1–5.

Taylor, R. G. (1976) Porphyry tin deposits in Bolivia: Discussion.Econ. Geol., 71, 1064–1065.

Wang, D. H., Chen, Y. C., Chen, W., Sang, H. Q., Li, H. Q., Lu, Y.F., Chen, K. L. and Lin, Z. M. (2004) Dating the Dachang gianttin-polymetallic deposit in Nandan, Guangxi. Acta Geol. Sin.,78, 132–139 (in Chinese with English abstract).

Wang, X. L., Zhou, J. C., Griffin, W. L., Wang, R. C., Qiu, J. S.,O’Reilly, S. Y., Xu, X. S., Liu, X. M. and Zhang, G. L. (2007)Detrital zircon geochronology of Precambrian basementsequences in the Jiangnan orogen: dating the assembly of theYangtze and Cathaysia blocks. Precambrian Res., 159,117–131.

Wu, Z. L. (1983) Geological features of porphyry tin ore deposit inYinyan. Geol. Explor., 7, 21–25(in Chinese with Englishabstract).

Xu, X. S., Reilly, S. Y. O., Griffin, W. L., Wanga, X. L., Pearson, N. J.and He, Z. Y. (2007) The crust of Cathaysia: Age, assemblyand reworking of two terranes. Precambrian Res., 158, 51–78.

Yang, Z. X., Mao, J. W., Chen, M. H., Tong, X., Wu, J. D., Cheng, Y.B. and Zhao, H. J. (2008) Re-Os dating of molybdenite from



the Kafang skarn copper (tin) deposit in the Gejiu tinpolymetallic ore district and its geological significance. ActaPetrol. Sin., 24, 1937–1944 (in Chinese with English abstract).

Yuan, H. L., Gao, S., Dai, M. N., Zong, C. L., Günther, D.,Fontaine, G. H., Liu, X. M. and Diwu, C. R. (2008a) Simulta-neous determinations of U-Pb age, Hf isotopes and traceelement compositions of zircon by excimer laser-ablationquadrupole and multiple-collector ICP-MS. Chem. Geol.,247, 100–118.

Yuan, S. D., Peng, J. T., Hu, R. Z., Li, H. M., Shen, N. P. andZhang, D. L. (2008b) A precise U-Pb age on cassiterite fromthe Xianghualing tin-polymetallic deposit (Hunan, SouthChina). Miner. Deposita, 43, 375–382.

Yuan, S. D., Mao, J. W., Cook, N. J., Wang, X. D., Liu, X. F. andYuan, Y. B. (2015) A Late Cretaceous tin metallogenic eventin Nanling W-Sn metallogenic province: Constraints fromU-Pb, Ar-Ar geochronology at the Jiepailing Sn-Be-F deposit,Hunan, China. Ore Geol. Rev., 65, 283–293.

Yu, Z. F., Mao, J. W., Zhao, H. J., Chen, M. H., Luo, D. L. and Guo,M. (2012) Geological characteristics and ages of granites and

related mineralization in the Dajinshan tungsten-tinpolymetallic deposit, western Guangdong Province. ActaPetrol. Sin., 28, 3967–3979 (in Chinese with English abstract).

Zheng, J. N., Griffin, W. L., O’Reilly, S. Y., Zhang, M., Pearson, N.and Pan, Y. M. (2006) Wide-spread Archean basement be-neath the Yangtze craton. Geology, 34, 417–420.

Zheng, W., Chen, M. H., Xu, L. G., Zhao, H. J., Ling, S. B., Wu, Y.,Hu, Y. G., Tian, Y. andWu, X. D. (2013a) Rb-Sr isochron age ofTiantang Cu-Pb-Zn polymetallic deposit in GuangdongProvince and its geological significance. Miner. Deposits, 32,259–272 (in Chinese with English abstract).

Zheng, W., Zhao, H. J., Chen, M. H., Xu, L. G., Liu, J. X., Luo, D. L.and Hu, Y. G. (2013b) Re-Os isotopic dating of molybdenitesfrom the Yingwuling polymetallic deposit in GuangdongProvince and its geological significance. J. Mineral. Petrol.,33, 38–46 (in Chinese with English abstract).

Zhou, X. M. and Li, W. X. (2000) Origin of Late Mesozoic igneousrocks in Southeastern China: implications for lithosphere sub-duction and underplating of mafic magmas. Tectonophysics,326, 269–287.

W. Zheng et al.


Documents

Re–Os Geochronology of Molybdenite from Yinyan Porphyry Sn ...€¦ · Short Communication Re–Os Geochronology of Molybdenite from Yinyan Porphyry Sn Deposit in South China Wei