Geochemistry, and zircon U Pb and molybdenite Re Os ... · Geochemistry, and zircon U–Pb and molybdenite Re–Os geochronology of Jilongshan Cu–Au deposit, southeastern Hubei

Geochemistry, and zircon U–Pb and molybdenite Re–Os geochronology ofJilongshan Cu–Au deposit, southeastern Hubei Province, China

A-JUAN PANG1,2, SHENG-RONG LI1,2*, M. SANTOSH2, QING-YU YANG3, BAO-JIAN JIA1

and CHENG-DONG YANG1

1State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Beijing, 100083,China

2School of Earth Science and Resources, China University of Geosciences, Xueyuan Road, Haidian District, Beijing,100083, China

3Hubei Jilongshan Gold Mining Limited Company, Yangxin, Hubei, 435231, China

The Jilongshan skarn Cu–Au deposit is located at the Jiurui ore cluster region in the southwestern part of the Middle–Lower Yangtze Rivervalley metallogenic belt. The region is characterized by NW-, NNW- and EW-trending faults and the mineralization occurs at the contact oflower Triassic carbonate rocks and Jurassic granodiorite porphyry intrusions. The intrusives are characterized by SiO2, K2O, and Na2Oconcentrations ranging from 61.66 to 67.8wt.%, 3.29 to 5.65wt.%, and 2.83 to 3.9wt.%, respectively. Their A/CNK (A/CNK= n(Al2O3)/[n(CaO) + n(Na2O) + n(K2O)]) ratio, dEu, and dCe vary from 0.77 to 1.17, 0.86 to 1, and 0.88 to 0.96, respectively. The rocks showenrichment in light rare earth elements ((La/Yb)N = 7.61–12.94) and large ion lithophile elements (LILE), and depletion in high fieldstrength elements (HFSE), such as Zr, Ti. They also display a peraluminous, high-K calc-alkaline signature typical of intrusivesassociated with skarn and porphyry Cu–Au–Mo polymetallic deposits. Laser ablation inductively coupled plasma spectrometry(LA-ICP-MS) zircon U–Pb age indicates that the granodiorite porphyry formed at 151.75� 0.70Ma. A few inherited zircons witholder ages (677� 10Ma, 848� 11Ma, 2645� 38Ma, and 3411� 36Ma) suggest the existence of an Archaean basement beneaththe Middle–Lower Yangtze River region. The temperature of crystallization of the porphyry estimated from zircon thermometerranges from 744.3 �C to 751.5 �C, and 634.04 �C to 823.8 �C. Molybdenite Re–Os dating shows that the Jilongshan deposit formedat 150.79� 0.82Ma. The metallogeny and magmatism are correlated to mantle–crust interaction, associated with the subduction ofthe Pacific Plate from the east. Copyright © 2013 John Wiley & Sons, Ltd.

Received 28 September 2012; accepted 28 January 2013

KEY WORDS Middle–Lower Yangtze River valley metallogenic belt; Jilongshan Cu–Au deposit; whole-rock geochemistry; Zircon U–Pb LA-ICP-MSgeochronology; Molybdenite Re–Os dating

1. INTRODUCTION

The Middle–Lower Yangtze River valley metallogenic belt,located at the intersection of the northern margin of theYangtze Craton, Qinling–Dabie orogenic belt and the south-ern margin of the North China Craton (Fig. 1), is aporphyry–skarn Fe–Cu–Au metallogenic belt in China (Xieet al., 2011b). The belt extends for about 450 km fromWuhan (Hubei Province) to Zhenjiang (Jiangsu Province)and consists of seven ore clusters. These are, from westto east: the Edong (southeastern Hubei Province), Jiurui(Jiujiang–Ruichang), Anqing–Guichi, Tongling, Luzong,

Ningwu and Ningzhen (Zhao et al., 1999; Xie et al.,2005). The ore deposits in this metallogenic belt have beenextensively studied in the past decades and these investiga-tions revealed that the mineralization is controlled bytectonics, sedimentation, and magmatism (Chang et al.,1991; Zhai et al., 1996). The region underwent a long andcomplex evolutionary process from the end of the Protero-zoic to the Yanshanian (Old Alpedic, Late Jurassic to LateCretaceous), when the tectonic activity reached its peak(Chang et al., 1991; Zhai et al., 1996; Zhou et al., 2006).The magmatism in this region has been classified intothree types by Zhai et al. (1996) as follows. (1) High-Kcalc-alkaline, intermediate to acid intrusive rocks relatedto skarn and porphyry Cu–Au–Mo polymetallic deposits,all of which belong to I-type (Pei and Hong, 1995) ormagnetite-type granitoids (Ishihara, 1977). The timing of

*Correspondence to: S.-R. Li, State key Laboratory of Geological Processesand Mineral Resources, China University of Geosciences, 29 XueyuanRoad, Beijing 100083, China. E-mail: [email protected]

Copyright © 2013 John Wiley & Sons, Ltd.

GEOLOGICAL JOURNALGeol. J. 49: 52–68 (2014)Published online 4 March 2013 in Wiley Online Library(wileyonlinelibrary.com). DOI: 10.1002/gj.2494

mineralization is estimated as 170 to 130Ma, based onstudies in the Tongling, Jiujiang and Yangxin areas. (2)The Na-rich calc-alkaline, intermediate to felsic intrusiverocks, with related skarn and magmatic Fe–Cu–Au deposits,and timing of mineralization estimated as 150 to 120Ma,such as from the Daye and Anqing areas. (3) Andesitic rocksin the volcanic basin, associated with porphry Fe depositsand mineralization ages of 130 to 95Ma, as studied fromthe Wuhu and Ningwu areas. The mineralization in theMiddle–Lower Yangzte River valley metallogenic belt hasbeen broadly classified into two genetic types: (1) porphyry/skarn/stratabound Cu–Au–Mo–Fe deposits and (2) magne-tite–apatite porphyry deposits related to andesitic rocks (Xieet al., 2005; Mao et al., 2006, 2011). The Jilongshan Cu–Audeposit of the present study belongs to the skarn-type Cu–Au–Mo association, and the major associated intrusive rocksare high-K calc-alkaline granodiorite porphyry with quartzdiorite porphyry occurring along the margin.Several studies have addressed the genetic aspects of the

ore deposits in the Jiurui ore cluster during the previousyears (Zhao et al., 1990; Chang et al., 1991; Shu et al.,1992; Xie et al., 2007, 2009, 2011a, 2011b; Li et al.,2008). However, the Jilongshan deposit has been poorly in-vestigated, except for drilling and geochemical–geophysicalexploration (e.g. Zhao et al., 1999). In this study, we attemptto characterize the timing and duration of mineralization, theformation age of the host rocks, and the tectonic environ-ment of ore formation based on LA-ICP-MS zircon U–Pbdating, molybdenite Re–Os geochronology, and whole-rock

geochemical analysis of representative samples from theJilongshan deposit, as well as from the adjacent Baiguoshuand the Fengshandong plutons in Jurui.

2. GEOLOGICAL SETTING

The Middle–Lower Yangzte River valley metallogenic beltis bounded by several large strike–slip fault systems. Theseare the Xiangfan–Guangji Fault (XGF) in the northwest,the Tangcheng–Lujiang regional strike-slipe fault (TLF)in the northeast, and the Yangxin–Changzhou Fault (YCF)in the south (Fig. 1). The Jiurui ore field is located in adepression on the Yangtze platform margin, to the east ofNE–ENE striking TLF and to the north of NW–WNW strik-ing Yangxin Fault. The late Proterozoic metamorphic rockswhich constitute the crystalline basement in the region arepoorly exposed. The main exposures of sedimentary stratain the Jiurui ore field are Ordovician, Silurian, Devonian,Carboniferous, Permian, Triassic and Quaternary, andconsist of limestone, dolomitic limestone, dolomite, sandstoneand shale (Mo et al., 2011). More than 60 plutons are exposedin the Fengshan polymetallic ore cluster which is situated inthe western part of the Jiurui district. The main plutonsinclude the Baiguoshu (0.15 km2), Jilongshan (1.8 km2),Lijiawan (0.4 km2), Fengshandong (1.6 km2), Dengjiashan(0.4 km2), and Dongleiwan (0.9 km2) (Li et al., 2010; Moet al., 2011) (Fig. 2). These intrusives are compositionally

Figure 1. Distribution of metallic deposits in the Middle–Lower Yangtze River belt, based on the map of Mao et al. (2011) and Zhao et al. (1999). Legend forsymbols in the figure: circle: porphyry–skarn–stratabound Cu–Au–Mo–Fe deposits; triangle: magnetite–apatite deposits. YCF, Yangxing–Changzhou Fault;XGF, Xiangfan–Guangji Fault; TLF,Tancheng–Lujiang Fault. The area in the box shown in the inset map of China represents the main figure. This figure is

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GEOCHEMISTRY AND GEOCHRONOLOGY OF CU–AU DEPOSIT, CHINA 53

Copyright © 2013 John Wiley & Sons, Ltd. Geol. J. 49: 52–68 (2014)

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granodiorite porphyry, quartz diorite porphyry and a few otherintermediate-acid rocks.

The main exposed strata in the Jilongshan deposit includethe Lower Triassic Daye Formation, consisting of limestone,dolomite, dolomitic limestone and calcite dolomite, andQuaternary sand, gravel, clay and soil (Fig. 3). The Jilongshanarea shows a complex structure, with well-developedfolds and fractures. The folds are characterized by closely

linear overturned and flip anticline and syncline, such as theKejiatang overturned anticline, Zhulintang overturned anti-cline, Guijiashan flip anticline and syncline and Jilongshan flipanticline. The fractures are NW compressional, NNW and EWtensional, such as the Jilongshan fracture (Fig. 3; Mo et al.,2011).The Jilongshan pluton, a composite intrusion, shows

multiple pulses of magmatism, and is located at the western

Figure 2. Geological sketch map of the Jiurui district (Shu et al., 1992; Li et al., 2010). This figure is available in colour online at wileyonlinelibrary.com/journal/gj

Figure 3. Geological sketch map of the Jilongshan area, Hubei (Mo et al., 2011). This figure is available in colour online at wileyonlinelibrary.com/journal/gj

A.-J. PANG ET AL.54




domain of the outer edge of the Huaiyang Mountain(Liu, 1989; Bi and Yang, 2008). The central part of the plu-ton is granodiorite porphyry and the marginal domain isquartz diorite porphyry. The intrusion plunges SW at mod-erate angles of 33� to 55�. The pluton is dumb-bell shapedin horizontal section and shows a mushroom shape in verti-cal section (Bi and Yang, 2008; Geological ExplorationInstitute of South China, 2011).The Cu–Au ore bodies occur mainly in the 3 to 6 members

of the Lower Triassic Daye Formation limestone at the contactzones with granodiorite porphyry (Fig. 3; Zhao et al., 1999).The Jilongshan deposit is comprised of north ore zone, middleore zone, and south ore zone, and the main orebodies aredistributed in the north and middle ore zones. The orebodiesshow various shapes as veins, saddle, stratoid beds, lensoid,nest, and cystic form. The ores are mainly skarn-type, withminor marble type and granodiorite porphyry type. The mainmetallic minerals in the ore are chalcopyrite, pyrite, magnetite,malachite, azurite, bornite, and molybdenite, and the gangueminerals include garnet, plagioclase, calcite, diopside, wollas-tonite, serpentine, chlorite, and quartz. The representativezoning of mineralization from the pluton to the wall rockmarble is as follows: unmineralized granodiorite porphyryaltered granodiorite porphyry with low-grade Mo–Cu miner-alization (silicified, sericitized, chloritized, garnetized,kaolinized, carbonated)! andradite skarn with Mo–Cumineralization! essonite–diopside skarn with Au–Cu miner-alization!wollastonite skarn with Cu–Au mineralizationmarble with small vein quartz Au mineralization.

3. SAMPLES AND ANALYTICAL TECHNIQUES

3.1. Major and trace elements

Twelve representative samples of the plutons were collectedfor chemical analyses. Nine fresh rock samples of the Jilongshanpluton were collected from the drill cores (0ZK1-24, 4ZK3-13,4ZK3-16 and ZK39-1-12) and different levels of the mine(170-38-02, 170-SNC-1, 440-04, 490-142-1 and 490-22),and two samples of the Baiguoshu pluton (BGS andW2ZK2-5) and one (FSD) of the Fengshandong pluton werecollected from the ground surface.The samples from the Jilongshan pluton are granodiorite

porphyry and quartz diorite porphyry. The granodiorite por-phyry is characterized by grey colour, porphyritic textureand massive structure (Fig. 4a and 4b). The phenocrystphases include plagioclase (25–40%), amphibole (5–10%),biotite (5–10%), quartz (2–5%), and K-feldspar (1–2%).Most of the plagioclases are prismatic and platy with sizesof 0.5–2.5mm. The amphiboles are prismatic with sizes of0.15mm� 0.5mm–0.3mm� 2mm and rhombic with sizesof 0.3–0.5mm, and the biotites are schistose with sizes of0.15mm� 0.5mm–0.2mm� 2.5mm or hexagonal with

sizes of 0.5–2.5mm. Quartz grains are granular with sizesof 0.3–0.8 mm (Figs. 4b and 5b). The plagioclases showpolysynthetic twin, carlsbad–albite compound twin, interpene-tration twin and girdle texture (Figs. 4f and 5a).Thegroundmass with grain-sizes of 0.05–0.1mm is xenomorphicand consists of plagioclase (15–25%), quartz (15–25%), amphi-bole (2–5%), biotite (2–5%) and accessory apatite (Fig. 5d),magnetite (Fig. 5b), sphene (Fig. 5f), and zircon (Fig. 5e).

The quartz diorite porphyry shows grey-green colour,inequigranular porphyritic texture and massive structure(Fig. 4c and 4d). The phenocrysts consist of plagioclases(15–20%) with sizes of 0.2mm� 0.3mm–0.5mm� 1.5mm, quartzs (5–20%) with sizes of 0.2–2.5mm, amphiboles(3–5%) with sizes of 0.2mm� 0.2mm–0.7mm� 1.5mmand biotites (3–5%)with sizes of 0.1mm� 0.2mm–1mm� 2.5mm. The groundmass with grain-sizes of 0.01–0.02mm showsa micro-granitic texture and consists of plagioclase (20–35%),quartz (10–25%), amphibole (2–5%), biotite (2–5%) andaccessory apatite, magnetite (Fig. 5c), sphene, and zircon.

The samples (BGS and W2ZK2-5) from Baiguoshu plu-ton are quartz diorite porphyry which are characterized bygrey–green colour, inequigranular porphyritic texture andmassive structure. The phenocrysts with sizes of 0.2–3.5mmconsist of plagioclases (15–20%), quartzs (5%), amphiboles(10–15%) and biotites (5%). The groundmass with grain-sizesof 0.01–0.02mm shows a micro-granitic texture and consistsof plagioclase (30–35%), quartz (15%), amphibole (3%),biotite (2%).

The sample FSD is a granodiorite porphyry which showsgrey colour, porphyritic texture and massive structure. Thephenocryst phases with sizes of 0.5–3mm include plagio-clase (28%), amphibole (10%), biotite (15%), quartz (3%),and K-feldspar (2%). The groundmass with grain-sizes of0.05–0.2mm is xenomorphic and consists of plagioclase(28%), quartz (15%), amphibole (5%), biotite (3%).

The samples were crushed and powdered in 75 mm forgeochemical analysis. Whole-rock major and trace elementsanalysis were performed in the Analytical Laboratory ofBRIUG (Beijing Research Institute of Uranium Geology).Major elements were determined by X-ray fluorescence(XRF) spectroscopy with a Philips PW2402. The analyticalprecision is better than 5%. Trace elements were analysedby high-resolution inductively coupled plasma massspectrometry (HR-ICP-MS) using a Finnigan MAT-6493(ElementI, instrument number 6493) spectrometer, whichhas an analytical uncertainty within 7%.

3.2. Zircon U–Pb dating

A representative sample of the granodiorite porphyry fromdrill core No.39-1 was selected for age determination by la-ser ablation inductively coupled plasma spectrometry(LA-ICP-MS) at the State Key Laboratory of Geological



Processes and Mineral Resources (GPMR), China Uni-versity of Geosciences in Beijing. Detailed analytical pro-cedures are described by Hou et al. (2007), Yuan et al.(2008), Kooijman et al. (2011), Bouman et al. (2011)and Li et al. (2012). Zircon internal textures werestudied by cathodoluminescence (CL) technique on amicroprobe JXA-8800R at the Electron MicroprobeLaboratory, Chinese Academy of Geological Sciences(CAGS) prior to zircon U–Pb dating. The operating con-ditions were 20 kV accelerating voltage and 50 nA primarybeam current. An Agilent 7500a ICP-MS and New-WaveUP193SS laser beam were used for zircon U–Pb isotopicanalysis. The laser diameter was 36 mm and wavelengthwas 193 nm. Helium was used as carrier gas totransport the ablated sample from the laser-ablation cell tothe ICP-MS torch via a mixing chamber mixed with Argon.The common Pb correction followed the method of Andersen

(2002).The Glitter 4.4.1 software and ISOPLOT 3.0program (Ludwig, 2003) were used for data processingand age calculation respectively. The details of analyticalprocedures have been described by Yuan et al. (2004) andLiu et al. (2008).

3.3. Molybdenite Re–Os dating

Four molybdenite samples were collected from the al-tered granodioritic porphyry ore (ZK39-1, Zk39-2 fromdrill core No.39) and the skarn ore (210CM28-1,210CM28-2 from �210m level of the mine) in theJilongshan Cu–Au deposit. They were analysed at theKey Laboratory of Isotope Geochronology and Geochem-istry, Guangzhou Institute of Geochemistry, ChineseAcademy of Sciences. The molybdenite is usually distrib-uted in altered granodiorite porphyry ore or skarn ore

Figure 4. Petrography of the rock types in Jilongshan deposit. (a) Hand specimen photograph of granodiorite porphyry (ZK39-1-16). (b) Thin section photomicro-graph (crossed nicols) of the granodiorite porphyry (ZK39-1-16). (c) Hand specimen photograph of quartz diorite porphyry (210-snc-5). (d) Thin section photomi-crograph (crossed nicols) of the quartz diorite porphyry (210-snc-5). (e) Photograph of the ore assemblage with molybdenite (4ZK-05) flakes. (f) Thin sectionphotomicrograph (crossed nicols) of granodiorite porphyry showing twinned and zoned crystals of feldspar (440-13). See Figure 5 for mineral abbreviations. This

figure is available in colour online at wileyonlinelibrary.com/journal/gj

A.-J. PANG ET AL.56



(Fig. 4e) and is characterized by a lead grey colour,hypautomorphic–allotriomorphic inequigranular textureand association with chalcopyrite and pyrite.Du et al. (1995a, 1995b, 2001, 2004), Li et al. (2005),

Yang and Ling (2006), Shirey and Walker (1995), Markeyet al. (1998), Mao et al. (1999, 2006), Stein et al. (2001),Sun et al. (2010) and Liu et al. (2012) have described thedetails of the Re–Os dating procedure, which is briefly sum-marized here. X series-7 quardrupole ICP-MS (Thermo Sci-entific, USA) with glass spray chamber and concentric glassnebulize was used to determine the Re and Os isotope ratio.The average blanks and standard deviation are 2.8� 1.1 pgfor Re and 0.7� 0.3 pg for common Os, respectively. Theseblanks have a negligible effect on the measured Re and Osabundances. In general, the precision for isotopic measure-ments is better than 0.2% (2 s, n= 15).

Each sample was digested using concentrated HNO3 bythe Carius tube (a thick-walled borosilicate glass ampoule).The weighed sample (0.025–1 g), 185Re spike and naturalOs standard solutions were loaded into a Carius tube througha small U-shape funnel with long neck. To this 10mlconcentrated HNO3 was added while the lower half of itwas immersed in ethanol-liquid nitrogen slush. The tubewas sealed and opened in a way similar to that describedby Shirey and Walker (1995). The sealed tube was heatedat 225–230 �C for 24 h. The tube was refrozen after sampledigestion and then opened. An approximate amount ofthe supernatant (depending on the estimated Re concen-tration in the molybdenite) was transferred to a 30mlquartz beaker and heated to dryness at 150 �C. 0.5mlconcentrated HNO3 was added and dried-down. This stepwas repeated twice to ensure the removal of Os as OsO4.

Figure 5. (a) (490-22), (b) (0ZK1-24), (d) (490-25), (e) (0ZK1-24), (f) (490-25): Thin section photomicrographs of granodiorite porphyry. (c) (440-04):Thin section photomicrographs of quartz diorite porphyry. Mineral abbreviations: Q, quartz; Am, amphibole; Bi, biotite; Mo, molybdenite; Mag, magnetite;

Zr, zircon; Pl, plagioclase; Ap, apatite; Spn, sphene. This figure is available in colour online at wileyonlinelibrary.com/journal/gj




Then remnant was diluted to a volume of 10ml using 2%HNO3 for Re determination by ICP-MS. The remaining su-pernatant was directly poured into a 50ml distillation flaskand distilled at 110 �C for 20min for Os. OsO4 distilled wastrapped using 5ml of H2O and then Os was analysed byICP-MS.

4. RESULTS

4.1. Whole-rock chemical composition

4.1.1. Major elementsThe major and trace element data of all samples are listed inTable 1. The samples in this study show SiO2 concentrationranging from 61.66 to 67.8wt.%, and MgO, Al2O3, TiO2

contents ranging from 1.4 to 2.81wt.%, 13.51 to 15.55wt.%, and 0.44 to 0.66wt.%, respectively. The average SiO2,MgO, Al2O3 and TiO2 abundances of Yangtze Block grano-diorites is 67.37wt.%, 1.59wt.%, 15.22wt.% and 0.46wt.%, respectively (Chi and Yan, 2007). Thus, the characteris-tics of the Jilongshan pluton are similar to those of YangtzeBlock granodiorites. The samples of the present study have ahigh alkali content with K2O+Na2O ranging from 5.51 to8.72wt.% and high K2O contents up to 5.67wt.%. The rocksplot in the sub-alkalic field in Figure 6a, calc-alkaline field inFigure 6d and high-K calc-alkaline and shoshonitic field inFigure 6b, similar to the Yangtze Block granodiorites. TheA/CNK ratio of the samples varies from 0.77 to 1.17, andmost of them fall in the range of 0.8 to 0.9. All samples ex-cept two plots in the metaluminous field in Figure 6c, asagainst the Yangtze Block granodiorites which are mostlyperaluminous.

4.1.2. Trace elementsThe samples in this study are enriched in light rare earth ele-ments (LREE) relative to high rare earth elements (HREE)((La/Yb)N = 7.61–12.94, 8.74–11.21 and 22.51 in the rocksof Jilongshan, Baiguoshu and Fengshandong, respectively)and their chondrite-normalized REE distribution patternsshow a smooth declining trend from LREE to HREE(Fig. 5a). Total REE concentrations of samples from theJilongshan pluton, the Baiguoshu pluton and the Fengshanpluton are 98.37–159.12 ppm, 112.97–132.04 ppm and186.88 ppm, respectively. The samples in this study showweak negative Eu anomalies (dEu= 0.86–1, 0.95–0.96 and0.93 for Jilongshan, Baiguoshu and Fengshandong, respec-tively) and weak negative Ce anomalies (dCe= 0.88–0.96,0.88–0.98 and 0.93 for Jilongshan, Baiguoshu andFengshandong, respectively). The average total REE con-tent, (La/Yb)N, dEu and dCe of Yangtze Block granodioriteswith the same REE distribution pattern as the samples in thisstudy are 160.85 ppm, 13.59, 0.74 and 0.99, respectively.

Primitive mantle normalized distribution patterns of thesamples of the present study and those of the YangtzeBlock granodiorites are similar (Fig. 7b). Our samplesare characterized by enrichment of large ion lithophileelements (LILE, such as Rb, Ba, Sr, K and Pb) and lightREE, and depletion in high field strength elements(HFSE, such as Zr, Ti). Rb, Sr, Ba, Th, U and Zrcontents in the samples are 67.2–116 ppm, 378–1108 ppm,752–1021 ppm, 5.59–11.4 ppm, 1.48–2.44 ppm and61.8–246 ppm, respectively with Rb/Sr, Sr/Ba and Th/Uratios ranging from 0.07 to 2.1, from 0.41 to 1.31 andfrom 2.97 to 5.79, respectively.

4.2. Zircon U–Pb ages

The zircon U–Pb data from 40 spots in 38 zircon grainsare presented in Table 2. The zircon crystals are mostlyeuhedral, transparent, colourless, tetragonal prism andtetragonal bipyramid combinations, with the prism facedeveloped better than the pyramidal face. The grainsrange in size from 50 to 180 mm. The internal microstruc-ture of zircon grains as studied from their CL imagesshow well-developed oscillatory zoning, typical ofmagmatic zircons. The representative CL images andLA-ICP-MS measurement spots, together with theapparent 206Pb/238U ages of zircons are shown in Figure 8.The uranium and thorium concentrations range from26.33 to 760.9 ppm, 16.89 to 517.64 ppm, and thecorresponding Th/U ratios are in the range of 0.19–1.46.The high Th/U ratios further confirm their magmatic cry-stallization history. Among the analysed grains, four zirconsyielded Precambrian ages, indicating their inherited orcaptured nature. Thirty-six spots yield a coherent group(Fig. 9c) with a weighted mean 206Pb/238U age of151.75� 0.70Ma (95% conf., MSWD=0.26, n=36,Fig. 9b). We interpret this age is the crystallization ageof the Jilongshan pluton.

4.3. Molybdenite Re–Os ages

The concentrations of Re, Os and Re–Os model age ofmolybdenite from Jilongshan ores are given in Table 3.The model age is measured with the contents of 187Reand 187Os in molybdenite and calculated with theequation: t = (1/l) In(1+187Os/187Re), where l is thedecay constant of 187Re, 1.666� 10�11 year�1 (Smoliaret al., 1996). Molybdenites from Jilongshan ores inthis study yielded Re–Os model ages ranging from149.17� 1.01Ma to 152.62� 1.00Ma, with a mean valueof 150.79� 0.82Ma.

A.-J. PANG ET AL.58


Table1.

Major

andtraceelem

entsof

theJilongshan

pluton,B

aiguoshu

pluton,and

Fengshandongpluton

comparedwith

themeangranodiorite

compositio

nof

Yangtze

Block.

The

averagemajor

andtraceelem

entscompositio

nof

Yangtze

Block

granodiorite

isfrom

Chi

andYan

(2007)

Sam

ple

490-22

0ZK1-24

4ZK3-16

ZK39-1-12

440-04

170-38-02

4ZK3-13

490-142-1

170-SNC-1

BGS

W2Z

K2-5

FSD

Yangtze

Rocktype

Granodiorite

porphyry

Quartzdiorite

porphyry

Granodiorite

porphyry

Granodiorite

SiO

267.8

63.55

63.81

65.77

63.66

62.91

63.07

65.82

65.49

63.62

61.66

66.09

67.37

Al 2O3

14.38

15.38

14.93

13.94

14.95

15.55

15.16

14.05

14.15

15.15

14.77

13.51

15.22

Fe 2O3

2.34

4.27

2.39

5.03

3.82

3.58

2.63

4.53

5.23

5.68

5.15

3.62

1.28

FeO

1.35

2.15

1.3

2.05

1.95

1.95

1.5

2.1

2.5

1.8

2.5

1.5

2.34

MgO

1.4

2.41

1.55

1.96

1.92

1.94

1.94

1.96

2.05

1.72

2.81

2.13

1.59

CaO

3.37

2.45

4.24

3.59

4.41

4.63

5.02

4.15

3.86

3.46

3.84

3.75

3.03

Na 2O

3.28

2.83

3.07

3.45

3.78

3.9

3.54

3.56

3.89

2.76

3.31

3.74

3.57

K2O

4.94

3.72

5.65

3.4

3.51

4.22

5.01

3.89

3.29

2.75

2.93

3.85

2.95

MnO

0.042

0.03

0.062

0.063

0.055

0.072

0.051

0.066

0.094

0.081

0.086

0.026

0.063

TiO

20.44

0.56

0.45

0.58

0.53

0.51

0.55

0.57

0.61

0.62

0.56

0.66

0.463

P 2O5

0.15

0.19

0.16

0.18

0.17

0.18

0.18

0.2

0.17

0.17

0.19

0.24

0.15

LOI

1.74

4.54

3.59

1.91

3.05

2.37

2.73

1.08

1.05

3.77

4.59

2.12

1.69

Total

101.232

102.08

101.202

101.923

101.805

101.812

101.381

101.976

102.384

101.581

102.396

101.236

99.716

A/CNK

0.852

1.171

0.791

0.878

0.829

0.801

0.744

0.798

0.833

1.097

0.947

0.788

1.044

Li

7.88

14.2

8.57

11.5

9.32

7.28

9.91

9.86

10.1

13.7

18.2

12.9

32Be

1.36

1.81

1.76

1.62

1.79

1.55

1.63

1.28

1.87

1.41

1.45

1.82

1.2

Sc

7.19

10.3

8.38

9.83

9.78

8.88

10.7

10.5

10.9

11.7

11.5

8.71

16.2

V75

.9104

76.8

92.3

105

90.1

103

107

114

116

120

101

82Cr

13.1

18.3

16.6

31.8

19.7

16.5

2128.5

28.7

39.5

34.2

532625

Co

7.06

10.6

7.46

10.1

10.4

10.4

7.78

12.4

12.6

12.5

13.5

11.3

105

Ni

5.89

21.8

6.55

11.8

8.32

7.54

8.86

10.7

9.86

13.9

1420.7

1960

Cu

168

4.57

78.7

271

712

207

314

432

64.5

25.7

13.5

246

30Zn

4040.8

42.2

290

54.3

51.1

50.5

51.2

64.2

68.5

60.5

31.3

55Ga

17.9

19.5

18.2

20.3

18.5

1818.9

21.3

20.6

19.5

17.9

21.1

18.2

Rb

86.4

96.7

104

98.8

67.2

85.4

88.7

77.8

90.8

7678.5

116

97Sr

481

450

646

724

694

545

760

599

478

378

1108

624

330

Y15

.317.4

16.8

18.5

1918.3

20.1

22.2

19.6

1719.1

14.3

17Nb

12.6

16.8

14.1

17.6

14.6

15.5

16.2

17.5

15.8

10.7

12.4

12.9

11.4

Mo

30.802

3.92

2.24

8.11

6.8

1.84

1.66

2.19

0.584

0.443

221

0.39

Cd

0.256

0.022

0.06

2.07

0.225

0.12

0.326

0.19

0.121

0.084

0.037

0.205

0.052

Sb

0.89

0.409

0.335

4.75

1.46

0.64

0.445

0.401

1.26

0.244

0.192

0.479

0.11

Cs

0.847

5.44

0.952

2.43

0.879

1.1

0.915

1.08

1.86

1.02

2.44

3.3

5.7

Ba

856

917

1017

901

781

752

1021

940

845

933

848

1003

730

La

20.2

25.5

27.6

33.5

2521

36.1

34.6

26.4

30.8

22.3

43.3

36Ce

3948.3

50.3

63.2

48.8

41.6

63.3

64.3

51.4

52.9

45.2

79.7

69Pr

4.84

5.73

5.94

7.35

5.83

4.97

7.93

7.64

5.98

6.24

5.44

9.12

7.1

Nd

19.3

22.3

22.9

26.4

24.2

20.9

30.2

29.5

2423.3

21.4

34.9

29Sm

3.91

3.99

4.29

4.69

4.31

4.06

5.02

5.41

4.82

4.28

4.14

5.81

5Eu

1.05

1.22

1.29

1.27

1.29

1.21

1.35

1.51

1.39

1.3

1.27

1.59

1.18

Gd

3.1

3.38

3.65

4.17

3.39

3.67

3.85

4.59

4.18

3.82

3.89

4.35

4.6

Tb

0.516

0.627

0.654

0.72

0.657

0.607

0.746

0.8

0.731

0.627

0.693

0.649

0.62

Dy

2.7

3.43

3.29

3.99

3.82

3.6

3.7

4.41

4.06

3.56

3.61

3.44

3.2

(Contin

ues)



5. DISCUSSION

5.1. Timing of magmatism and mineralization in Jilongshandeposit

The Re–Os system in molybdenite is considered to be rela-tively robust, and not affected by prolonged (i.e. 2–8Ma)and high temperature (400–500 �C) hydrothermal activity(Selby et al., 2002), post-ore metamorphic and/or tectonicevents (Stein et al., 1998), as compared with K–Ar, Ar–Arand Rb–Sr ages (Li et al., 2008b). Re–Os ages can di-rectly record the timing of the primary sulphide mineral-ization event (Stein et al., 2001; Xie et al., 2011b)because the closure temperature of the Re–Os systemreaches up to 500 �C (Suzuki et al., 1996). Therefore, weinterpret the molybdenite Re–Os average model age(150.79� 0.82Ma) from the ores in this study as a reliableage that indicates the timing of mineralization in theJilongshan deposit.U–Pb ages from zircons have been widely used to con-

strain the timing of magmatism (e.g. Yang et al., 2010;Xie et al., 2011a; Li et al., 2012; Li et al., 2013; Rogeret al., 2012). The zircon U–Pb data obtained in this studyconstrain the timing of emplacement of the Jilongshanpluton as 151.75� 0.70Ma. Although there are youngermafic dykes in the region, the main mineralization isrelated to the pluton which was emplaced at151.75� 0.70Ma, as indicated by the zircon U–Pb agein this study. The inherited zircons in the granodioriteporphyries show ages of 677� 10Ma, 848� 11Ma,2645� 38Ma, and 3411� 36Ma. These zircons witholder ages indicate the incorporation of basementmaterial in the magma. The presence of old zircon withages of 2645 to 3411Ma implies the existence of anArchaean basement beneath the Middle–Lower YangtzeRiver, and confirms similar interpretations given in Gaoet al. (2001), Zhang et al. (2003) and Di et al. (2005).The close concordance between the timing of emplace-

ment of the Jilongshan pluton as estimated from U–Pbzircon data, and the formation of the skarn ore minerali-zation, as indicated by the Re–Os data, confirms theintimate link between magmatism and metallogeny in thisregion. The available isotopic age data of some of theintrusions and ore deposits in the Jiurui district are listedin Table 4. These data indicate that the magmas in theJiurui district started to be emplaced at about 152Ma,achieved their peak at about 145Ma, and continued untilabout 138Ma. Among the three types of magmatismrecognized in the Middle–Lower Yangtze River beltaccording to Zhai et al. (1996), the intrusives in theJiurui region mostly belong to the first type, with themagma characterized by high-K calc-alkaline, intermedi-ate to silicic composition, with related to skarn andT

able

1.(Contin

ued)

Sam

ple

490-22

0ZK1-24

4ZK3-16

ZK39-1-12

440-04

170-38-02

4ZK3-13

490-142-1

170-SNC-1

BGS

W2Z

K2-5

FSD

Yangtze

Rocktype

Granodiorite

porphyry

Quartzdiorite

porphyry

Granodiorite

porphyry

Granodiorite

Ho

0.508

0.634

0.642

0.706

0.61

0.637

0.738

0.812

0.778

0.672

0.681

0.58

0.65

Er

1.47

1.8

1.75

2.02

1.89

1.92

2.06

2.42

2.29

1.95

1.9

1.63

2Tm

0.193

0.298

0.256

0.326

0.297

0.303

0.312

0.384

0.362

0.308

0.302

0.223

0.3

Yb

1.34

1.76

1.53

1.87

1.76

1.98

2.07

2.41

2.17

1.97

1.83

1.38

1.9

Lu

0.241

0.301

0.252

0.297

0.315

0.331

0.35

0.333

0.307

0.317

0.318

0.211

0.3

Ta

1.05

1.35

1.2

1.34

1.1

1.25

1.22

1.18

1.13

0.714

1.02

0.835

0.86

W2.27

0.95

0.728

1.66

2.83

2.03

2.88

0.784

1.12

0.602

0.792

5.84

0.55

Pb

10.5

10.7

8.68

79.9

26.3

12.7

8.24

8.8

12.9

10.5

13.9

8.82

22Bi

0.145

0.174

0.319

0.666

2.04

0.101

0.183

0.309

0.664

0.166

0.007

0.833

0.16

Th

5.64

6.89

6.48

8.56

6.43

5.59

8.82

7.9

6.36

7.25

5.97

11.4

10.3

U1.65

1.95

1.65

2.05

1.96

1.87

1.55

2.12

2.14

1.48

1.68

2.44

2.1

Zr

71.3

103

70.9

72.7

78.4

74.3

8080.6

92.9

246

109

61.8

160

Hf

2.14

3.18

2.19

2.51

2.74

2.3

2.68

2.93

2.89

6.11

3.29

2.1

4.9

PREE

98.368

119.27

124.344

150.509

122.169

106.788

157.726

159.119

128.868

132.044

112.974

186.883

160.85

PLREE

8.77

8.75

9.34

9.68

8.59

7.18

10.41

8.85

7.66

8.99

7.54

14.00

10.85

dEu

0.89

0.99

0.97

0.86

1.00

0.94

0.90

0.90

0.92

0.96

0.95

0.93

0.74

dCe

0.94

0.94

0.92

0.94

0.96

0.96

0.88

0.93

0.96

0.88

0.98

0.93

0.99

La/Sm

5.17

6.39

6.43

7.14

5.80

5.17

7.19

6.40

5.48

7.20

5.39

7.45

7.20

(La/Yb)

N10.81

10.39

12.94

12.85

10.19

7.61

12.51

10.30

8.73

11.21

8.74

22.51

13.59

Table

I.(Contin

ued)

A.-J. PANG ET AL.60


porphyry Cu–Au–Mo polymetallic deposits. The geo-chemistry of Jilongshan pluton rocks also agrees withthe character of the first type magma.

5.2. Source of pluton and orebody

The Nb/Ta values of the intrusive range from 11.75 to 15.45,spanning the range for lower crust (8.3) to depleted mantle

(>17.0) (Sun and McDonough, 1989). The Fe2O3/FeO ratioof the samples in this study is >1.7, suggesting a relativelyoxidized magma. The chondrite normalized REE distributionpattern coincides with the characteristics of a crust–mantlemixed source. The whole-rock chemical data imply magmamainly derived from upper mantle sources and partial mixingwith sialic crustal material. Bi and Yang (2008) also proposed

Figure 6. Chemical classification diagrams for the Jilongshan and other granites in the Yangtze Block. (a) Alkalis (K2O+Na2O) versus SiO2 diagram (Middlemost, 1994),the division between alkaline and sub-alkaline is after Irvine andBaragar (1971). (b)K2Oversus SiO2 diagram (compositionalfieldsmodified fromRollinson, 1993). (c) A/NKversus A/CNK diagram (after Peccerillo and Taylor, 1976), A/NK=n(Al2O3)/[n(Na2O)+n(K2O)], A/CNK=n(Al2O3)/[n(CaO)+n(Na2O)+n(K2O)]. (d) FAM diagram

(Irvine and Baragar, 1971), F=w(FeO+Fe2O3), A=w(Na2O+K2O), M=w(MgO). This figure is available in colour online at wileyonlinelibrary.com/journal/gj

Figure 7. Chondrite-normalized REE patterns and primitive mantle normalized trace element diagrams for the Jilongshan pluton rocks and other granites in theYangtze Block. This figure is available in colour online at wileyonlinelibrary.com/journal/gj





Table

2.LA-ICP-M

SU–P

banalytical

results

ofzircon

grains

from

theJilongshan

intrusiverocks

Spot

Conc.(ppm

)Isotoperatio

sAges(Ma)

Error

correlation

Th

UTh/U

207Pb/

206Pb

1207Pb/

235U

1206Pb/

238U

1207Pb/

206Pb

1207Pb/

235U

1206Pb/

238U

1

174.85

273.74

0.27

0.0571

0.0050

0.1878

0.0160

0.0239

0.0006

494

147

175

14152

41.04E-09

2256.92

525.9

0.49

0.0495

0.0020

0.1625

0.0066

0.0238

0.0004

169

68153

6152

24.66E-11

374.33

399

0.19

0.0513

0.0024

0.1685

0.0077

0.0238

0.0004

256

78158

7152

27.29E-11

4114.36

382.31

0.30

0.0491

0.0020

0.1618

0.0067

0.0239

0.0004

153

69152

6152

24.75E-11

5229.28

359.53

0.64

0.0489

0.0025

0.1609

0.0084

0.0239

0.0004

141

91152

7152

29.57E-11

6115.64

323.12

0.36

0.0492

0.0020

0.1616

0.0067

0.0238

0.0004

155

68152

6152

24.86E-11

7148.59

318.41

0.47

0.0558

0.0039

0.1840

0.0127

0.0239

0.0004

445

121

172

11152

34.09E-10

8266.59

440.85

0.60

0.0478

0.0018

0.1576

0.0060

0.0239

0.0004

9159

149

5152

23.49E-11

974.43

310.56

0.24

0.0520

0.0028

0.1713

0.0090

0.0239

0.0004

287

92161

8152

21.23E-10

1083.85

402.74

0.21

0.0535

0.0026

0.1755

0.0083

0.0238

0.0004

350

78164

7152

29.82E-11

11299.66

470.54

0.64

0.0493

0.0019

0.1617

0.0062

0.0238

0.0003

162

63152

5152

23.69E-11

12168.69

339.91

0.50

0.0492

0.0033

0.1620

0.0108

0.0239

0.0004

158

119

152

9152

22.20E-10

13122.14

294.03

0.42

0.0490

0.0030

0.1610

0.0097

0.0238

0.0004

148

107

152

8152

21.57E-10

14282.87

402.95

0.70

0.0481

0.0026

0.1585

0.0086

0.0239

0.0004

104

89149

8152

31.18E-10

15257.08

371.25

0.69

0.0523

0.0051

0.1717

0.0165

0.0238

0.0006

300

173

161

14152

41.16E-09

16109.56

347.02

0.32

0.0490

0.0023

0.1607

0.0075

0.0238

0.0004

145

79151

7152

27.34E-11

17278.29

520.3

0.53

0.0491

0.0018

0.1610

0.0058

0.0238

0.0003

151

58152

5152

23.02E-11

18163.66

396.53

0.41

0.0492

0.0027

0.1616

0.0087

0.0238

0.0004

159

94152

8152

21.14E-10

19161.22

479.07

0.34

0.0490

0.0022

0.1597

0.0071

0.0236

0.0004

148

74150

6151

25.91E-11

20112.31

323.99

0.35

0.0491

0.0020

0.1619

0.0064

0.0239

0.0004

150

65152

6152

24.34E-11

21124.34

271.41

0.46

0.0511

0.0034

0.1684

0.0112

0.0239

0.0004

243

123

158

10152

22.44E-10

22494.63

760.91

0.65

0.0483

0.0027

0.1585

0.0087

0.0238

0.0004

112

91149

8152

31.21E-10

2385.94

83.14

1.03

0.0635

0.0024

0.9698

0.0366

0.1108

0.0017

724

55688

19677

104.05E-08

2497.19

298.33

0.33

0.0492

0.0028

0.1617

0.0091

0.0239

0.0004

156

100

152

8152

21.28E-10

25168.14

278.49

0.60

0.0491

0.0021

0.1621

0.0069

0.0239

0.0004

155

71153

6152

25.55E-11

26180.35

223.36

0.81

0.0492

0.0043

0.1600

0.0137

0.0236

0.0005

155

153

151

12150

35.85E-10

2790.16

322.68

0.28

0.0497

0.0027

0.1633

0.0087

0.0239

0.0004

179

95154

8152

21.09E-10

2883.07

224.34

0.37

0.3709

0.0080

35.6748

0.7930

0.6974

0.0094

3795

183658

223411

362.34E-03

29207.08

500.57

0.41

0.0484

0.0018

0.1529

0.0058

0.0229

0.0003

119

61144

5146

22.98E-11

30289.47

694.66

0.42

0.0491

0.0015

0.1615

0.0051

0.0239

0.0003

151

48152

4152

22.07E-11

31241.84

426.7

0.57

0.0500

0.0023

0.1648

0.0075

0.0239

0.0004

193

78155

7152

26.69E-11

32190.94

130.48

1.46

0.0669

0.0020

1.2963

0.0397

0.1406

0.0020

834

40844

18848

116.30E-08

33241.39

374.18

0.65

0.0489

0.0022

0.1605

0.0072

0.0238

0.0004

141

75151

6152

26.55E-11

34517.64

519.23

1.00

0.0493

0.0024

0.1622

0.0078

0.0239

0.0004

163

82153

7152

28.10E-11

35117.02

506.13

0.23

0.0481

0.0017

0.1582

0.0055

0.0239

0.0004

104

53149

5152

22.60E-11

3616.89

26.33

0.64

0.1728

0.0058

12.0883

0.4010

0.5072

0.0090

2585

322611

312645

382.89E-04

37135.5

274.69

0.49

0.0489

0.0022

0.1613

0.0070

0.0239

0.0004

144

73152

6152

25.84E-11

38189.22

387.85

0.49

0.0497

0.0044

0.1637

0.0143

0.0239

0.0004

182

162

154

12152

35.79E-10

39156.75

362.2

0.43

0.0530

0.0026

0.1741

0.0085

0.0238

0.0004

330

83163

7152

21.04E-10

40111.89

383.51

0.29

0.0521

0.0031

0.1713

0.0101

0.0238

0.0004

290

105

161

9152

31.89E-10

A.-J. PANG ET AL.62


a similar view based on oxygen isotope and sulphur isotope(d18O from 7.3% to 10.8%, d34S = 2.1%).The d34S data on sulphide minerals from the ores are

broadly similar to those from intrusions in the JilongshanCu–Au deposit (Jia, 2012), indicating that the copper andgold mineralization are closely related to the LateJurassic magmatism in the Jilongshan area. This argu-ment is also supported by geochronological datadiscussed in the previous section. The sulphur isotopic dataon the ore minerals and the associated intrusion suggest adominant mantle component. This might indicate the involve-ment of mantle materials in the ore-forming processes. Thehelium isotopic data from the Jilongshan (Jia, 2012) displaymajor contribution of crust helium, with only subordinatemantle signature for the mineralization in the Jilongshandeposit. Thus, a mixed mantle and crust source, with the latterdominating, is inferred for the generation of the magma and itsrelated ore mineralization.

5.3. Zircon thermometer and geodynamic environment

Zircon saturation temperature has been widely employed as a ro-bust thermometer, using the following equation (Watson and

Harrison, 1983): In

DZrzircon/melt =�3.80� [0.85(M� 1)] + 12900/T(K),

where DZrzircon/melt is the concentration ratio of Zr in thestoichiometric zircon to that in the melt, T is the absolutetemperature, and M is the cation ratio (Na +K+2Ca)/(Al�Si).An alternative method to compute zircon crystallization tem-perature is based on the equation (Ferry and Watson, 2007):

log(Ti)=5.711� 0.072� (4800� 86)/T(K).

Zr and Ti contents of zircons in this study vary from497698.8 ppm to 544455.2 ppm and from 2.63 ppm to21.63 ppm. We thus compute zircon saturation andcrystallization temperatures in the range of 744.3 �C to751.5 �C and 634.04 �C to 823.8 �C, with mean temperaturesof 747.2 �C and 681.5 �C. Zircon saturation temperature suggeststhe temperature of magma when it is saturated with zirconiumelement, and is taken to represent the formation temperature.

In order to evaluate the tectonic setting of the Jilongshanpluton, we plotted the geochemical data in Nb vs Yb andY+Nb vs Rb diagrams (Pearce et al., 1984). All rocks in thisstudy fall in the syn-collision granites field and the volcanicarc granites field in Figure 10 (Drawn by software CGDK,Qiu et al., 2013). The Yangtze Block is considered to havestarted its cratonization from the Late Archaean and thecrystalline basement was formed until Jinning (Gortic–Grenvillian and Asyntian) age (Neoproterozoic Cryogenianstage) (Wan, 2011). Following the Jinning (Gortic–Grenvillianand Asyntian) movement, the Yangtze Craton witnessed anextensional environment. From Sinian to Middle Triassic, thecraton was a relatively stable platform, filled with sedimentaryunits comprising carbonate and clastic rocks of marine facies(Wu, 1992, 1993). Between Middle Triassic to MiddleJurassic, the Yangtze and North China Craton collided (238–218Ma) (Li et al., 1989; Ames et al., 1993, 1996; Chenet al., 1995; Chavagnac and Jahn, 1996; Li et al., 1997; Rowleyet al., 1997; Li, 2001 and Mao et al., 2006, 2011). EW-, NW-trending linear folds and NW-trending faults developed. Thesestructures provided excellent pathways for the emplacement ofthe Yanshanian (Old Alpedic) intrusions. At this stage, theMiddle–Lower Yangtze River valley metallogenic belt was aforeland basin located south of the Dabie Orogen(Tang et al., 1998). Due to westward subduction of thePalaeo-Pacific Plate (160–130Ma), NNE-trending struc-tures were superimposed in the Yangtze Craton leadingto the development of the NNE- and NNW-trendingtensile shear faults (Ren et al., 1998; Yang, 1999; Maoet al., 2003, 2006; Niu et al., 2003), and triggeringextensive magmatic activity, termed as the Yanshanianmovement. During this period, the Yangtze Cratonexperienced a tensional or transition environment, with

Figure 8. Cathodoluminescence (CL) images of zircons from Jilongshangranodiorite porphyry. The analytical spots and ages in Ma are also shown.This figure is available in colour online at wileyonlinelibrary.com/journal/gj




mantle upwelling and magma underplating (Zhou andYue, 2000). Extensive alkaline basaltic magmas weregenerated and their mixing with the basement crust unitsresulted in the formation of dioritic magmas. The dioriticmagmas migrated along the faults and other favourablestructures, finally precipitating the associated ore depos-its. Most orebodies and related granitic intrusions arelocated at the intersection of EW- and NNE-trendingfaults. The Middle–Lower Yangtze River valley devel-oped a series of parallel NNE-trending fault basins andintense volcanism at 125 to 115Ma, resulting in theformation of the magnetite porphyry systems associated

with Cretaceous andesitic volcanic and subvolcanicrocks in the Ningwu–Luzhong volcanic fault basins(Mao et al., 2006).The Jilongshan deposit is located at the north of the

Yangtze Craton. The magma emplacement occurredalong a major fault controlled by nearly E-W-trendingfold, as also displayed by the shape of the pluton (Liu,1989). The rocks in the contact zone were skarnizedleading to the formation of magnetites, gold, copper andother metallogenic elements. Gold–copper mineralizationappeared at the contact zone resulting in the formationof the skarn Cu–Au deposit.

Figure 9. Relative probability plots of U–Pb age, weighed mean age and concordia diagrams of zircons from the Jilongshan granodiorite porphyry. This figureis available in colour online at wileyonlinelibrary.com/journal/gj

Table 3. Re–Os isotopic data for the molybdenite in the ores from the Jilongshan Cu–Au deposit

Sample W-sample(g)

Re/mg g�1 187Re/mg g�1 187Os/ng g�1 Model age(Ma)

Measured 2s Measured 2s Measured 2s Measured 2s

ZK39-1 0.0337 298.806 1.13 187.811 0.71 467.336 2.626 149.17 1.01ZK39-2 0.0345 347.754 0.696 218.577 0.438 556.477 3.493 152.62 1210CM28-1 0.0324 470.15524 1.91544 295.51096 1.20393 747.52566 1.47791 151.65 0.69210CM28-2 0.0298 466.09567 0.93132 292.95936 0.58537 731.59859 2.46779 149.71 0.59

A.-J. PANG ET AL.64



6. CONCLUSIONS

The zircon U–Pb and molybdenite Re–Os analyses inthis study constrain the timing of the emplacement of theJilongshan pluton and formation of the ore deposit as151.75� 0.70Ma and 150.79� 0.82Ma. The inherited zir-cons with late Archaean and Neoproterozoic ages are corre-lated to the basement rocks in the Yangtze Craton and thebreakup of the Rodinia Supercontinent. Zircon saturationand crystallization temperatures vary from 744.3 �C to751.5 �C, and from 634.04 �C to 823.8 �C. The geochemicalfeatures classify the Jilongshan pluton as a peraluminous,high-K calc-alkaline granitoid, with enrichment in LREEand LILE, with volcanic arc affinities. The emplacementof the magma into carbonate wall rocks resulted in skarnand porphyry type Cu–Au–Mo polymetallic deposits. The

magmatism and metallogeny are correlated to mantle–crustinteraction, associated with the subduction of the PacificPlate from the east.

ACKNOWLEDGEMENTS

We thank Editor-in-Chief Prof. Ian Somerville and twoanonymous referees for their comments which improvedour manuscript. This work is supported by the Key Programof National Natural Science Foundation of China (grant no.90914002), Scheduled Program of China Geological Survey(grant no. 1212011220926), the China State AdministrativeOffice of Ore-Prospecting Project for Critical Mines (grantnos. 200714009, 20089937) and the 111 Project under theChina Ministry of Education (B07011). This is also a

Figure 10. Nb–Yb and Rb–(Y +Nb) diagrams of Jilongshan pluton rocks and other granites in the Yangtze Block. Syn-COLG, syn-collision granites; WPG,within plate granites; VAG, volcanic arc granites; ORG, ocean ridge granites. This figure is available in colour online at wileyonlinelibrary.com/journal/gj.

Table 4. Compilation of isotopic ages for the intrusions and ore deposits in the Jiurui district

Locality Rock Age (Ma) Method Reference

Jilongshan Porphyry 151.75� 0.70 LA-ICP-MS zircon U–Pb This studyJilongshan Orebody 150.79� 0.82 Molybdenite Re–Os model age This studyFengshandong Porphyry 146� 2 SHRIMP zircon U–Pb Xie et al., 2011Fengshandong Orebody 144.0� 2.1 Molybdenite Re–Os model age Xie et al., 2007Dengjiashan Porphyry 145.4� 1.0 Cameca SIMS zircon U–Pb Li et al., 2010Dengjiashan Porphyry 138� 2 SHRIMP zircon U–Pb Li and Jiang, 2009Dongleiwan Porphyry 145.8� 1.0 Cameca SIMS zircon U–Pb Li et al., 2010Qianjiawan Orebody 137.7� 1.7 Molybdenite Re–Os model age Xie et al., 2007Ruanjiawan Orebody 143.6� 1.7 Molybdenite Re–Os model age Xie et al., 2007Wushan Porphyry 145� 3.9 Cameca SIMS zircon U–Pb Ding et al., 2005Wushan Porphyry 146� 1 Cameca SIMS zircon U–Pb Li et al., 2010Wushan Orebody 146.4� 2.6 Molybdenite Re–Os isochron age Li et al., 2007Chengmenshan Porphyry 144.5� 1.3 Cameca SIMS zircon U–Pb Li et al., 2010Chengmenshan Porphyry 140.6� 1.6 LA-ICP-MS zircon U–Pb Zeng et al., 2010Chengmenshan Orebody 140� 2 Molybdenite Re–Os model age Wu and Zhou,1997Chengmenshan Orebody 142� 2 Molybdenite Re–Os model age Mao et al., 2006



contribution to the Talent Award to M. Santosh under the1000 talent plan of the Chinese Government and theResearch Program of the Hubei Jilongshan Gold MiningLimited Company. We thank Mr. Wen JS and Xiong Wfor their kind support and help during the field investigation.

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Geochemistry, and zircon U Pb and molybdenite Re Os ... · Geochemistry, and zircon U–Pb and molybdenite Re–Os geochronology of Jilongshan Cu–Au deposit, southeastern Hubei