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Porphyry CuAuMoepithermal AgPbZndistal hydrothermal Au deposits in theDexing area, Jiangxi province, East ChinaA linked ore system

Jingwen Mao a,, Jiandong Zhang a,c, Franco Pirajno a,b, Daizo Ishiyama c, Huimin Su d,Chunli Guo a, Yuchuan Chen a

a MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, Chinab Geological Survey of Western Australia, 100 Plain Street, East Perth, WA 6004, Australiac Center for Geo-environmental Science, Faculty of Engineering and Resource Science, Akita University, Japand China University of Geosciences, Beijing 100029, Beijing, China

a b s t r a c ta r t i c l e i n f o

Article history:

Received 19 May 2010

Received in revised form 2 August 2011

Accepted 13 August 2011

Available online 27 August 2011

Keywords:

Porphyry CuAuMo deposits

Epithermal CuAgAuZnPb deposit

Shear zone-hosted gold deposit

Mesozoic

Dexing area

East China

Based on previous studies and detailed eld investigations of the Dexing porphyry copper deposit, the Yin-

shan Ag-Pb-Zn deposit and the Jinshan shear zonehosted gold deposit in the Dele Jurassic volcanic basin,

in the northeastern Jiangxi province, East China, we propose that the three deposits share spatial, temporal

andgenetic relationships andbelong to thesame metallogenicsystem. Dexingis a typicalporphyryCuAu

Mo deposit in which both ore-forming uid and metals are derived from the granite porphyry. The Yinshan

deposit consistsof a porphyry copperore located in the cupola ofa quartzporphyrystock, in thelower part,

and AgPbZn oreveinsin theupperpart.The hydrothermaluids were mainlyderived from themagmain

the early stages of the mineralizing event and became mixed with meteoric waters in the late stages. Its ore

metalsare magma-derived. Both theJinshanbasemetalveinsand theHamashi, Dongjie andNaikengquartz

vein-type gold deposit are hosted by brittleductile structures, which are distal in relation to the porphyry

intrusions and were formed by mixed magmatic uids and meteoric water, whereas the gold was mainly

leached from the country rocks (Mesoproterozoic Shuangqiaoshan Group phyllite and schist). The deposits

show a distinct spatial arrangement from porphyry Cu,to epithermal AgPbZnanddistalAu. Wesuggest a

porphyryepithermaldistal vein ore system model for this group of genetically related mineral deposits.They were formedin a back-arc setting in a MiddleJurassicactive continentalmargin, with magmasderived

from the subducted slab.

2011 Published by Elsevier B.V.

1. Introduction

The Dele Mesozoic volcanic basin in the northern Jiangxin province,

Southeastern China (Fig. 1) hosts three signicant ore deposits: the

Dexing porphyry CuAuMo deposit; the Yinshan AgPbZn vein de-

posit; and the Jinshan shear zone-hosted gold deposit. Mining of these

deposits began in the Sui and Tang Dynasties (605908 A.D.) for Dexing

and Yinshan, and in the Song Dynasty (9601279 A.D.) for Jinshan. Ex-

tensive geological surveying and mineral exploration were conducted

in the Dexing and Yinshan areas by the Jiangxi Bureau of Geology, Min-

eral Resources, Exploration and Development from the 1950s to the

1970s and in the Jinshan area by the Jiangxi Bureau of Nonferrous Geol-

ogy and Mineral Resources in the 1980s. By 2000, the Dexing porphyry

CuAuMo deposit, which consists of three orebodies (Tongchang,

Fujiawu and Zhushahong) was reported to contain the following mea-

sured reserves: 5.2 Mt Cu at 0.45%, 128,000 t Mo at 0.01%, 215 t Au at

0.19 g/t, 1279 t Ag (Tongchang); 2.57 Mt Cu at 0.5%, 168,000 t Mo at

0.03% (Fujiawu) and 600,000 t Cu at 0.42% (Zhushahong) (Qian et al.,

1996). The Yinshan epithermal AgPbZn vein deposit has measured

reserves of 2600 t Ag at 196 g/t, 382,886 t Pb at 1.75%, 418,201 t Zn at

1.91%, and 858,803 t Cu at 0.53%, and 114 t Au at 0.62 g/t. The Jinshan

shear zone gold deposit has Au reserve of 300 tat 6 g/t.

Previousand ongoingresearch addresses the geology and geochemis-

try of these deposits. The geochemical work encompassed stable isotope

studies and uid inclusions, radiometric dating of ores and host rocks

(e.g., Fan and Li, 1992; Li et al., 1994, 1997; Wang et al., 1999; Wei,

1985). Zhuet al. (1983)and Ye (1987)providedcomprehensive summa-

ries of the geology, geochemistry and prospecting techniques for the

Dexing porphyry CuAuMo and the Yinshan epithermal AgCuZnPb

deposits. However, the essential features and characteristics of these de-

posits have not been described in English language journals. Rui et al.

(2005) rst introduced the Dexing porphyry CuAuMo deposits in an

English language publication, based on data contributed by Zhu et al.

(1983). Li and Sasaki (2007), Zhang et al. (2007) and Li et al. (2010) con-

ducted uid inclusion studies on the Dexing, Yinshan and Jinshan de-

posits. Lu et al. (2005), Wang et al. (2006) and Li et al. (2007b)

Ore Geology Reviews 43 (2011) 203216

Corresponding author. Tel.: +86 10 68327333; fax: +86 10 68327142.

E-mail address:[email protected](J. Mao).

0169-1368/$ see front matter 2011 Published by Elsevier B.V.

doi:10.1016/j.oregeorev.2011.08.005

Contents lists available at SciVerse ScienceDirect

Ore Geology Reviews

j o u r n a l h o m e p a g e : w w w . e l s e v i e r . c o m / l o c a t e / o r e g e o r e v
http://dx.doi.org/10.1016/j.oregeorev.2011.08.005http://dx.doi.org/10.1016/j.oregeorev.2011.08.005http://dx.doi.org/10.1016/j.oregeorev.2011.08.005mailto:[email protected]://dx.doi.org/10.1016/j.oregeorev.2011.08.005http://www.sciencedirect.com/science/journal/01691368http://www.sciencedirect.com/science/journal/01691368http://localhost/var/www/apps/conversion/tmp/scratch_2/Unlabelled%20imagehttp://dx.doi.org/10.1016/j.oregeorev.2011.08.005http://localhost/var/www/apps/conversion/tmp/scratch_2/Unlabelled%20imagemailto:[email protected]://dx.doi.org/10.1016/j.oregeorev.2011.08.005


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reportedon dating of molybdenite(ReOs), mica (ArAr), andzircon (UPb) for both Dexing and Yinshan.

Since these three different deposits occur within a small area, a pos-

sible genetic link between them needs to be considered. In this paper,

based on detailed eld investigations and, comprehensive reviews of

the available geology, geochemistry and exploration work, we attempt

to focus on the question of a genetic link between the three deposits

and propose a new model, which may aid further prospecting for new

deposits or extensions of the existing ones.

2. Geological setting

South China consists of the Yangtze Craton in the northwest and the

Cathaysia Block in the southeast, separated by QinzhouHangzhou fault

zone (Fig. 1) in which the eastern part is well-known as the JiangshanShaoxing (simplied as Jiangshao) fault zone or shear zone (Pirajno and

Bagas, 2002). This is considered to be a Neoproterozoic suture zone,

along which the two tectonic units amalgamated at ~1.1 Ga to 0.9 Ga

(Chen and Jahn, 1998; Li et al., 2002, 2007a, 2007b, 2007c; Shui, 1988,

Ye et al., 2007; Zhou and Zhu, 1993). The Dexing ore cluster (or Dexing

area) is located in the Jiangnan shield, on the southern margin of the

Yangtze Craton, 50 km north of the JiangshanShaoxing Neoproterozoic

fault zone. The basement of the Yangtze Craton consists of Archean to

Proterozoic rocks exposed in theKangdianshield in thewestern margin,

the Jiangnan shield in thesouthern marginand theDahongshan areas in

the north margin (e.g.,Cheng, 1994; Greentree and Li, 2008; Qiu et al.,

2000; Wang and Mo, 1995). Zircons from Early Paleozoic lamproite dia-

tremes in the Dahongshan area give UPb ages of 2.92.8 Ga and Hf

model ages of 2.63.5 Ga (Zheng et al., 2006). Phanerozoic cover in

the Yangtze Craton comprises Cambrian to Early Triassic carbonates in-tercalated with clastic rocks, and Jurassic to Cretaceous clastic rocks in-

tercalated with volcanic rocks. The Cathaysia Block has a Proterozoic

basement in the Wuyishan uplift in the east, the Dayaoshan uplift be-

tween the Guangdong and Guangxi provinces and the western Hainan

Island uplift. Sinian (Neoproterozoic) to Ordovician metasandstone

and slate occur in the Nanling region, central portion of the Cathaysian

Block, overlain by Devonian to Permian carbonate rocks. Jurassic clastic

rocks intercalated with volcanic rocks, as well as Cretaceous red-bed

sandstones, occur in a series of NE-trending rift basins (Cheng, 1994;

Jiangxi Bureau of Geology and Mineral Resources, 1984, 2005).

Thestratigraphic sequence in theDexingarea consists of theMesopro-

terozoic Shuangqiaoshan Group, the Neoproterozoic Dengshan Group,

the Lower Cambrian Hetang Formation, the Lower Jurassic Linshan and

Ehuling Formations and the Cretaceous Shixi Formation (Fig. 2). TheMesoproterozoic Shuangqiaoshan Group has extensive outcrops, ac-

counting for about 70% of the total area, and consists of a lower greens-

chist facies of sandstone, volcaniclastic rocks, intercalated with basaltic

lavas. It can be further divided into an upper subgroup and a lower sub-

group. The lower subgroup comprises abyssal facies siltstone and mud-

stone intercalated with volcaniclastic rocks, characterized by a ysch

setting that is suggested to have developed in a marginal depression of

a stable continent at ca. 1515 Ma (Liu et al., 1989, 1993). The upper sub-

group is composed of graygreen turbidite and basaltic lavas developed

in a 1371 Ma active continent marginal depression setting (Jiangxi Bureau

of Geology and Mineral Resources, 1984). Neoproterozoic rocks out-

crop in the southeast of the area and overlie the Mesoproterozoic

Shuangqiaoshan Group along a sheared contact (Fig. 2). They are

composed of terrestrial volcaniclastic and clastic rocks of paralic

Fig. 1.Simplied geology of Cathaysian Block and the distribution of the granitoid-related CuAuAgPbZn ore deposits along the Shihang (or QinzhouHangzhou) rift belt and

adjacent areas (modied fromGuo et al.(2010)).

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swamp facies (the Dengshan Group). Lower Cambrian carbonate rocks

of the Hetang Formation occur in the southeastern corner of the Dexing

area and are overlain by Sinian clastic rocks (Fig. 2). The lower Jurassic

units can be divided into clastic rocks of alluvialat and lake swampy

facies of the Linshan Formation in the lower part, and the Ehuling For-

mation, comprising from bottom upwards, conglomerate, rhyolitic ag-

glomerate breccias, hornblende rhyolite, dacitic agglomerate and

dacitic lava. The Cretaceous red-bed sandstone of the Shixi Formation

occurs in the NE-trending rift basins in the south of the area. Host

rocks for the mineralization are both Mesoproterozoic metamorphic

rocks and Lower Jurassic volcanic rocks.The NE-trending Le'anjiang deep fault zone in the northwest,

northeastern Jiangxi deep fault (or Maoqiao ophiolite shear zone) in

the southeast and Sizhoumiao anticlinoria in the center constitute

the dominating structural features of the studied area (Fig. 2). The

BashiyuanTongchang and JiangguangFujiawu sub-parallel ductile

shear zones are developed between the Le'anjiang and northeastern

Jiangxi deep fault zone. The Jinshan shear zone, the major host for

the Jinshan gold deposit, consisting of several groups of sub-parallel

EW-trending brittleductile shear zones, occur as subordinate struc-

tures between BashiyuanTongchang and JiangguangFujiawu duc-

tile shear zones.

Rocks in the areamainly consistsof Neoproterozoic marine facies vol-

caniclastic (dacitic) clastic rocks, basic volcanics and ophiolite fragments

dated at 9291160 Ma, which developed along the Miaoqiao ophiolite

ductile shear zone (Xu and Qiao, 1989; Zhou and Zhao, 1991), and Mid-

dle Jurassic daciticrhyolitic volcanic rocks and associated subvolcanic

rocks, such as quartz porphyry, dacitic porphyry (183 Ma;Li and Sasaki,

2007) and granodiorite porphyry (171 Ma;Wang et al., 2004) in the

southwest and southeast.

3. Geology and geochemistry of the deposits

3.1. Dexing porphyry Cu ore system

The Dexing porphyry copper system lies in the northeastern part oftheDele oredistrict(Fig. 2) andis hostedin theTongchang, Zhushahong,

and Fujiawu granitic porphyries and surrounding county rocks (Zhu et

al., 1983). These granitic porphyries occur as small stocks and lie at the

intersections of NWW-trending and NE-trending faults (Fig. 1). Each

porphyry stock exhibits a pipe-like shape plunging to NW (Fig. 3). The

country rocks intruded by the granodiorite porphyries are sericitic phyl-

lite, tuffaceous phyllite and meta-sedimentary tuff of the Mesoprotero-

zoic Shuangqiaoshan Group.

3.1.1. Granitoids

The Tongchang granodiorite porphyry has a surface outcrop area of

ca. 0.7 km2; the Fujiawu granodiorite porphyry has a outcrop area of

0.2 km2; and the Zhushahong granodiorite porphyry occurs as a group

of dykes, in which the largest dykes has an outcrop area of ca. 0.06 km2

.

Fig. 2.Sketch map of geology and the distribution of granitoid-related CuAuAg polymetallic deposits in the Dele Mesozoic basin (or Dexing area), northeastern Jiangxi Province

(modied fromZhu et al.(1983) and Li and Sasaki(2007)).

205J. Mao et al. / Ore Geology Reviews 43 (2011) 203216


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Zhu et al. (1983) recognized ve magmatic phases: three phases of

granodiorite porphyry (major part) and two phases of diorite porphyry

(supplementary part). Li and Sasaki (2007) further suggested three

stages of emplacement, pre-mineralization aplite, mineralized granodio-rite (major phase) and post-mineralization quartz diorite. Wang et al.

(2004)described granodiorite and quartz diorite porphyries in the Dex-

ing area. They are characterized by idiomorphic phenocrysts of andesine

(An3045), 0.54 mm in length, which exhibit weak normal zoning. Other

phenocryst minerals are idiomorphichypidiomorphic hornblende (0.5

2 mm) and biotite (0.53 mm), tabular K-feldspar (15 mm) and quartz

(13 mm). The matrix has a micro- orne-granular (0.050.3 mm grain

size) texture and consists of hypidiomorphic oligoclase (An1620), horn-

blende and biotite, and xenomorphic quartz and K-feldspar. The rock-

forming and accessory mineral contents of the different intrusive rocks

in the Dexing area show only small variations. For example, the Tong-

chang intrusive rocks consist of plagioclase (4652%), quartz (1623%),

K-feldspar (1417%), amphibole (711%) and biotite (29%). Accessory

minerals in these rocks include magnetite, apatite, titanite, and rare

ilmenite, zircon, pyrite, chalcopyrite and molybdenite (Rui et al., 1984;

Zhu et al., 1983).

The Fujiawu intrusive rocks comprise plagioclase (4355%), quartz

(1823%), K-feldspar (1318%), amphibole (710%) and biotite (37%). Accessory minerals are magnetite, apatite, titanite, and zircon

(Rui et al., 1984; Zhu et al., 1983). The Zhushahong intrusive rocks are

composed of plagioclase (4752%), quartz (1921%), K-feldspar (13

16%), amphibole (810%) and biotite (47%). Their accessory minerals

are magnetite, apatite, and zircon (Rui et al., 1984; Zhu et al., 1983).

Magnetite is the dominant accessory phase; ilmenite is absent in the

Dexing granitic porphyries. Granodiorite porphyries are characterized

by 6263 wt.% SiO2, ~15 wt.% Al2O3, 1.942.07 wt.% K2O, low

K2O/(Na2O +K2O) (0.330.84), enrichment in large ion lithophile ele-

ments (LILE) and LREE, low high eld strength elements (HFSE) and

HREE depletion (REE=24.9~ 216.2 ppm, LREE= 22.2~ 206.3 ppm,

HREE=2.7~17.0 ppm, La/Yb=8~44). Zhu et al. (1983)reported the

initial strontium isotopic value (Isr) of 0.7043, and a date of 171

3 Ma using the SHRIMP zircon UPb method (Wang et al., 2004).

Fig. 3.Plans and sections of the Zhuashahong, Tongchang, and Fujiawu in the Dexing porphyry CuAuMo ore district, Northeastern Jiangxi (modied fromZhu et al.(1983) and Rui

et al.(2005)).



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3.1.2. Orebodies and ore components

The orebodies of all of three deposits, form classic stockworks, and

disseminated ores, overprinted on both granodiorite and the country

rocks, and exhibit cylindrical shapes concentrated around the granodio-

rite porphyries. CuAuMo mineralization is developed at the endo-

and exo-contact zone, with main orebodies (about two thirds) in the

country rocks (exo-contact zone) (Rui et al., 2005; Zhu et al., 1983)

(Fig. 3). The Tongchang orebody is the largest of the three. It is oval-

shaped at the surface, with a NW

SE-strike 2.54 km length and aninner barren core, measuring 400 m by 700 m. The Fujiawu orebody

has a round shape witha diameterof 100 m and an inner barrencoredi-

ameter of 800 m. Both the Tongchang and Fujiawu orebodies are about

1000 m deep, whereas the Zhushahong orebody comprises several

smalleren-echelonore zones (Rui et al., 2005). The suldes in the ores

are mainly pyrite and chalcopyrite, and lesser molybdenite, tennantite

and bornite, and minorchalcocite, galena, sphalerite, digenite, bismuthi-

nite, cubanite, pyrrhotite, arsenopyrite, aikinite, carrollite, siegenite,

bravoite, millerite, gersdorfte, seligmannite and matildite. The gangue

minerals are mainly quartz, hydromuscovite (illite), chlorite and anhy-

drite. Silver, rhenium, sulfur, selenium, tellurium and cobalt also can

be recovered as by-products in addition to copper, molybdenum and

gold.

3.1.3. Alteration and mineralization

Rui et al. (1984, 2005) recognized three alteration zones: quartz

sericite; chlorite(epidote)sericite; and chloriteepidoteillite sur-

rounding the granodiorite porphyry outwards and upwards. There is

weak K-feldspar and biotite alteration in the Fujiawu, but these are not

present at Tongchang and Zhushahong. Li and Sasaki (2007) recognized

four types of vein systems as follows: (1) granular quartzK-feldspar

sulde or K-feldspar veins (A vein); (2) quartzmolybdenitechalcopy-

rite veins (B vein); (3) suldequartz veins (D vein); and(4) carbonate

sulfateoxide veins (H vein). The D veins are the most important for the

mineralization in the Dexing porphyry deposit. Primary uid inclusions

in the D vein include liquid-rich, vapor-rich and halite-bearing ones.

Based on the thermometric measurements ofuid inclusions and stable

isotope systematicsLi and Sasaki (2007)suggested that the tempera-tures of mineralization of D veins are between 115 and 430 C, at a cor-

responding pressure range of 20400105 Pa.

The hydrothermal uids responsible for muscovite in the D vein

have an isotopic composition (18Ovalues=3.6 to 5.4,Dvalues=49

to 46), similar to that of typical magmatic uids (D=80to

40; 18Owater=5.5 to 9.5), as suggested by Ohmoto (1986)

and Sheppard (1986), indicating that hydrothermal uids of the late al-

teration stages are predominantly magmatic. Carbon and oxygen iso-

tope values for hydrothermal calcite in H veins are 4.8 to 6.2

and 6.818.8, respectively. The 34S of pyrite in the D vein ranges

from 0.1 to 3, whereas34S for chalcopyrite in H vein ranges from

4 t o 5, suggesting a magmatic originfor sulfur. Theabovedata indicate

that the ore-forming uids of the Dexing porphyry copper ore system

are derived from the exsolution ofuids from the cooling magma. The-oretically, a connate uid that circulates through the magmatic system

at low uid rock ratios also would end up with the same isotopic signa-

ture. However, there are no evidences to prove a connate uid kept in

the phyllite of the Mesoproterozoic Shuangqiaoshan Group, the host

rocks for the ore-related porphyries. The O, Nd and Sr isotopic composi-

tions of different altered rocks in the Tongchang (Jin et al., 2002) indi-

cate that there are three types of hydrothermal uids: 1) magmatic; 2)

deep-seated non-magmatic; and 3) meteoric water. Magmatic uids

play a predominant role in the ore-forming process. Jin et al. (2002)

also explained that strontium isotope (87Sr/86Sr)ivalues increase grad-

ually from the interior of a porphyry body towards the contact with

country rocks (0.7050.711), possibly indicating that the hydrother-

mal uids carrying the ore-forming metals from the interior of the por-

phyry to the discharge zone along the contacts with country rocks.

The ReOs molybdenite age of 170.41.8 Ma (Lu et al., 2005) is

consistent with the granodiorite age of 1713 Ma (Wang et al.,

2004), indicating that the mineralization event occurred in the Mid-

dle Jurassic.

3.2. Yinshan AgPbZnCu deposits

Yinshan AgPbZnCu deposit is a volcanicsubvolcanic hydro-

thermal deposit or porphyry

epithermal deposit. The mineralizationis spatially, temporally and genetically related to the Middle Jurassic

volcanic and/or subvolcanic quartz porphyry.

3.2.1. Country rocks

Thehost rocks for theYinshanorebodies areMiddle Jurassicvolcanic

subvolcanic rocks (porphyry) of the Ehuling Formation and phyllite and

tuffaceous phyllite of the Mesoproterozoic Shuangqiaoshan Group.

Three discontinuous cycles of felsic, felsicintermediate and intermediate

magmatic activities have been identied in the Yinshan area. Felsic and

felsicintermediate magmaticactivities began with pyroclastic eruptions,

to lavaextrusion and ending with subvolcanic intrusions. During therst

cycle rhyolitic dacite and rhyoliteeruptedalong fractures, at the intersec-

tions of approximately EW-trending structures and NE-trending struc-

tures in the northeastern and eastern parts of the deposit area.

Subvolcanic quartz porphyries were emplaced as EW-trending

dykes or small porphyries (Fig. 4), hosted by phyllite of the Meso-

proterozoic Shuangqiaoshan Group at the margin of the volcanic

basin in the Qiulongshangtian-Beishan area, in the northern part of

the mine area. The second cycle of magmatic rocks, comprising

dacite and dacitic porphyries (Fig. 4) dated at 181 3 Ma bySHRIMP

zircon UPb method (Li et al., 2007b), are mainly distributed in

Xishan and surrounding areas. Volcanism in this stage started

along fractures and ended as calderas in Xishan ( Fig. 4). The third

cycle of magmatic activity is characterized by only a small amount

of andesitic lava conned to the volcanic edice of Xishan in the

west of the deposit area (No. 11 porphyry) (Ye, 1987).

3.2.2. Structures

The major structures in the Yinshan deposit area are the YinshanNE-plunging anticline and faults that controlled volcanic activity

and the formation of explosive breccias pipes. Major faults trend

NNE, NE and NNW, with subordinate NW- and NWW-trending

splays, as well as small scale NS faults. A series of NNE-, NE-, and

NNW-trending faults hosts the mineralization (Ye, 1987). The quartz

porphyry associated with the ores was emplaced at intersections of

the NE-trending and the EW-trending faults, exhibiting equidistant

right-lateral distribution along the NE-trending hanging wall (NW

side) of the Yinshan anticline axis (Li, 1994).

3.2.3. Orebodies and mineral assemblages

The Yinshan deposit can be divided into ve ore sections and twelve

ore belts, comprising Nanshan, Yinshan, Jiulongshangtian (simplied as

Jiuqu) Xishan, and Beishan (Fig. 4) from south to north, where AgPbZn mineralization occurs as veins, that connect with the porphyry sys-

tem below (Fig. 5). The dominant ore belts are No. 7 and No. 8, in the

Nanshan section, No. 2, No. 3, No. 4, and No. 5 in Yinshan area, No. 12

in the Xishan section, No. 9 and No. 11 in the Jiuqu section, No. 10 in

the Beishan area. Each of the belts comprises about ten ore veins. The

PbZnAg ore veins occur in Beishan, Jiuqu and Yinshan. In the rst

two, the ore veins show nearly EW-trends with steep dips either to

theN or S. The oreveins in theXishan section show NE-and NNE-strikes,

with steep dips to the NS or NNW, whereas in the Yinshan section they

strike NW with steep dips to the SW or SE. These ore veins are 300 and

600 m long, 1 to 15 mwideandextendto depthsof 200 to 600 m (rarely

to 1050 m). The major ore minerals are galena, sphalerite, siderite, a

small amount of pyrite and arsenopyrite, and minor pyragyrite, chlorar-

gyrite native silver and a number of PbAgSb-sulphosalts. Gangue



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minerals include sericite, chlorite, quartz, dickite, kaolinite, illite, barite,uorite, dolomite and chalcedony (Ye, 1987).

Apart from these large AgPbZn ore veins, there are also stringer

veins, veinlets and disseminated CuAu ores hosted by quartz porphyries

and andesitic volcanic rocks. Surrounding the quartz porphyry in the

Jiuqu andXishansections, CuAu orebodiesare present in thealteredpor-

phyry in the roof pendants, then along the south and north contacts, to

the explosive breccia pipes nearby, with stringer veins, stockworks and

disseminated ores. The larger CuAu orebodies exhibit tabular shapes.

Major ore minerals are pyrite, chalcopyrite, tennantite, enargite, tetrahe-

drite, galena, and sphalerite; gangue mineralogy is dominated by quartz,

sericite, chlorite, calcite and kaolinite. In past 2 years a new orebody

with Cu reserve of 200,000 t was explored at depth within the Jiuqu sec-

tion, where pyritechalcopyrite assemblages occur along the shear zone

(Fig. 6).

3.2.4. Mineralization and alteration

Ye (1987)reported the presence of two mineralization episodes: 1)

early Cu-pyrite stage;and2) latePbZnAg stage. Li et al.(2007b) applied

muscovite 40Ar/39Ar methods to obtain ages for these two mineralization

stages, resulting inan early ageof 178.2 1.4 Ma and a late ageof 175.4

1.2 Ma. After detailed investigationZhang et al. (2007) recognized four

stages, from early to late: 1) barren quartz; 2) pyritequartz; 3) pyrite

chalcopyritequartz; and 4) pyritesphaleritegalenaquartz.

Ye (1987) recognized alteration zoningof sericitization, sericitization

carbonation and chloritizationcarbonation, and associated metal zoning

of Cu, CuPbZn, PbZn, Pb, surrounding the quartz porphyry or dacitic

porphyry.Yang et al. (2004)proposed a similar zoning, characterized by

(from the daciticporphyry outwards):(weak) sericitized dacite porphyry

zonepyritic and sericitized dacite porphyry zone and phyllite zone-pyritic, sericitized and chloritized (carbonate) phyllite zonechloritized

and carbonated phyllite zonecarbonated and chloritized pyroclastic

rocks zone. The mineralization also shows a metal zoning of CuCu

PbZnPbZnPb (Ag) from the dacitic porphyry outwards. These al-

teration and metal zoning are similar to those in the classic porphyry Cu

systems (Seedorff et al., 2005; Pirajno, 2009).

Zhang et al. (2007)carried out systematic uid inclusion studies in

the Yinshan district area, and recognized thatthreemajor types ofuids

were involved in the ore-forming process. They are: type I vapor-rich;

type II liquid-rich (accounting for N90% of total); and type III halite-

bearinginclusionswithin the H2ONaCl system. Textural characteristics

indicative of boiling are commonly seen in the Yinshan deposit. The

early uids exsolved from such silicate melts (represented by type I in-

clusions) have a very low salinity due to the low pressure conditions.Such a dilute hot uid is considered responsible for the development

of early barren and possibly some pyrite-bearing quartz veins. With

continued crystallization saline uids were then exsolved from the

crystallizing magmas. Under high pressure conditions (N900 bar)

high-salinity uids were trapped. Collapse of the overpressured system

through explosion and accompanied by introduction of meteoric water

resulted in the generation of low to moderate salinityuid inclusions.

Therefore, the latter two mineralization stages are mainly dominated

by vaporliquid inclusions, locally with coexisting high-salinity and

low to moderate salinityuid inclusions indicating boiling.Zhang et al.

(1997)obtained 18O values ofuids from 6.6 to 9.5and D values

of inclusion uids from 48 to 34 with calculated temperatures

from 390 C to 270 C.Zhang et al. (1996) proposed that the isotopic

compositions of the late mineralization

uids related to galena and

Fig. 4.Plan of the Yinshan porphry CuAu vein-type AgPbZn deposit in the Dele Mesozoic basin. There is an apparent mineralization zonation with the CuAuS in the center and

AgPbZn at the outer margin (modied fromYe(1987), and Li et al.(2007a, 2007b, 2007c)).



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calcite, are characteristics of meteoric waters (18OH2O=0.5 and

DH2O=70). The uid inclusion characteristics of the Yinshan de-

posit area are typical of porphyry Cu polymetallic deposits.

3.3. Jinshan Au deposits

The Jinshan gold deposit, located about 34 km SW of Dexing, is

hosted in the Jinshan brittleductile EW, and NE-trending shear

zone, which also hosts other gold deposits, including Huaqiao and

Bashiyuan (Fig. 2). The country rocks in the Jinshan mine area are

Mesoproterozoic metamorphic rocks, which are similar to those in

the Dexing porphyry Cu deposit area.

3.3.1. Structures

The Jinshan brittleductile shear zone is composed of several parallel

deformation bands at scales ranging from 0.1 m to 650 m in width that

consist of mylonite, protomylonite and ultramylonite, having dip angles

of 5 to 35NW, N and NE, locally enclosing lenses of undeformed rocks,

linking the regional NE-trending strike-slip shear zone along the margins

of the deposit area.

3.3.2. Orebodies and mineral assemblages

The gold orebodies in the Jinshan mine are layer-like, tabular and

lenticular and parallel to the main shear plane (C foliation). They have

thicknesses ranging from 1.2 m to 16 m, averaging 3.5 m, and are

conned within the quartzpyriteankerite alteration zone at the

center of the Jinshan shear zones (Fig. 7). The Au grade is irregular,averaging 6 g/t, with the single highest value of 1687 g/t. Gold miner-

alization occurs in altered rocks (silica, pyrite and ankerite) and in

quartz veins. Ore mineral assemblages are simple, including mainly

pyrite, subordinate magnetite, hematite, arsenopyrite, sphalerite,

chalcopyrite and galena. Gangue minerals are quartz, subordinate

sericite, albite, ankerite and chlorite. Pyrite is the most important

gold-bearing mineral host. Native gold has a neness of 953.6969.4

(Wei, 1995). The ne-grained and xenomorphic native gold occurs

as disseminations or as micro-veinlets hosted in pyrite and quartz

coexisting with chalcopyrite, galena and tetrahedrite.

3.3.3. Mineralization and alteration

Alteration of country rock in the Jinshan gold deposit is expressed as

silicication, albitization, pyritization, sericitization, chloritization and

Fig. 5.Section through the Yinshan ore deposit showing the mineralization zoning with CuAuS in the depth and AgPbZn upward (afterNi(2010)).

Fig. 6. Photograph showing the porphyry CuAu ore taken in the adit in the Jiuqu mine,

Yinshan ore deposit. The ore displays a structure of orientation arrangement mainly

consisting of quartz, sericite and pyrite.

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carbonation; both silicication and pyritization are closely associated

with gold mineralization.Wei (1996) recognized a distinct alteration

zoning along the Jinshan shear zone, from the margin to the center of

the shear zone, consisting of a chloritecalcite zone, a quartzsericite

dolomite zone and a quartzpyriteankerite zone. Based on the meta-

morphism and deformation of the rocks and mineral paragenesis,Li et

al. (2007a, 2010)proposed that alteration patterns can be divided into

three zones from the center of the shear zone outward, as follows: (1)

quartz

albite

ankerite

pyrite, occurring around the main shear zonewith the highest strain and a vertical thickness of several meters to

tens of meters, but generally less than 50 m, and containing the highest

gold grades; (2) quartzsericiteankerite, developed on both sides of

the rst alteration zone with vertical thickness of ca. 100 m; and (3)

chloritecalcitesericite, occurring in the outermost parts of the shear

zone but not extending beyond it.

Fan and Li (1992)divided the mineralization into three stages, and

then determined the uid inclusion characteristics of each: (1) quartz

pyrite, with trapping temperatures of quartz uid inclusions ranging

from 250 C to 215 C; (2) quartzsulde, with homogenization temper-

atures ranging from 225 C to 190 C; and (3) carbonate with homogeni-

zation temperatures ranging from 190 C to 160 C. Salinities of 12.3 to

14.5 wt.% NaCl were determined for medium- and low-temperature

uids.Fan and Li (1992)reported a large number of universally small

uid inclusions dominated by liquid-dominant or liquid-only uid inclu-

sions. Zhang and Tan (1998) recognized fourtypes ofuid inclusions: (1)

gasliquid brine inclusions, making up 8085% of the total; (2) pure hy-

drocarbon inclusions (1015%); (3) saline daughter mineral-bearing

polyphase inclusions (~1%); and (4)pure CO2 inclusions, as well as liquid

CO2-bearing three-phase inclusions (b1%).Zou (1993), Zhang and Tan

(1998) proposed that high contents of organic matter in ore-forming

uids are important for gold transportation and precipitation. According

to the characteristics ofuid inclusions,Fan and Li (1992), Zhang and

Tan(1998)suggestedthatmineralization in theJinshan gold depositis re-

lated to a granitic intrusion at depth. He/Ar isotopic systematics investi-

gated byLi et al. (2009)suggest that the ore-forming uids are mainly

crustally-derived, but with involvement of a small amount of mantle

uids. Hydrogen and oxygen isotopic systematics have led researchers

to propose several different and contradictory sources of ore-forminguids such as mixtures of magmatic and meteoric waters (Fan and Li,

1992; Zhang and Tan, 1998), mixture of magmatic and metamorphic

water (Huang and Yang, 1990; Yang et al., 2000), metamorphic waters

(Li et al., 2007a, 2009; Wei, 1996), mixtures of metamorphic and meteoric

water (Ji et al., 1994), and nally mixtures of magmatic water, metamor-

phic water and meteoric water (Liu et al., 2005).

Apart from the three large deposits mentioned above, other quartz

vein-type gold deposit include Hamashi, Dongjia and Naikengalso

withina NE-trending shear zone, to thenortheast of theYinshan deposit

and southwest of the Zhushahong (Fig. 2). Small-scale auriferous quartz

vein-type gold mineralization is also developed along a steep strike-slip

brittleductile shear zones. The altered wall rocks have low grade gold

on both sides of the auriferous quartz veins. Wall rock hydrothermal al-teration consists of silicication accompanied by arsenopyrite and

pyrite.

Li et al. (2009)suggested that mineralization in the Hamashi gold

deposit can be divided into three (a) quartzpyrite stagecomprising

dominant quartz and a small amount of pyrite and native gold; (b)

sulde stagecharacterized by massive sulde (pyrite, arsenopyrite,

chalcopyrite, minor galena and sphalerite); and (c) carbonatesulde

or sulfatesulde stageconsisting of abundant calcite, siderite and

ankerite. Ore minerals are native gold, pyrite and arsenopyrite, with

small amounts of galena and sphalerite; gangue minerals comprise

quartz, calcite and sericite.

4. Discussion and conclusions

4.1. Porphyry copperepithermal AgPbZndistal hydrothermal Au

deposits: a new mineral system

Porphyry mineral systems are usually divided into porphyry CuAu

and porphyry CuMo, but most porphyry deposits in China are porphyry

CuMoandCuMoAu deposits; porphyry CuAu depositsare quite rare.

These differences in the element associations of porphyrysystems can be

related to tectonic setting and its implications to the composition of the

magmatic system. Copper could be derived from the mantle (including

remelting of subducted slab andmantle or basalticunderplates), whereas

Mo would be mainly from the lower crust. In the southwest Pacic

islands arcs there are many porphyry CuAu deposits and these are usu-

ally associated with epithermal Au and/or AuAg deposits. Along the

western South American continental margin and in the southwestern

part of theUnited Statesof America andthe northwestern part of MexicoCuMo porphyry deposits are dominant (Cooke et al., 2008). Recently,

the Pebble porphyry CuAuMo deposit in southwest Alaska (Kelley et

al., 2010; Lang et al., 2008; Rebagliati and Payne, 2005 ) has been shown

to contain a similar element association as the Dexing porphyry deposit.

Fig. 7. Section through the Jinshan shear zone-hosted gold deposit, reecting the relationship of the gold orebodies to the mylonitic rocks (modied from Wei(1996); Li et al.

(2007a)).



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Porphyry CuAu deposits are associated with low-K, mid-K and high-K

calc-alkaline granitoids, whereas porphyry CuMo deposits are related

to alkali-rich granitoids (Cooke et al., 2008). Ifthe denudation of a metal-

logenic belt is comparatively shallow, one can observe the coexistence of

a porphyry copperdepositdeveloped in the lower part of the volcanic ed-

ice, evolvingupward to epithermal systemsin andesitic to dacitic volca-

nic rocks (Seedorff et al., 2005) and laterally to base metal (CuPbZn)

vein systems (Pirajno, 2009). Comparable systems are known, for exam-

ple, from the Metaliferi Mts., Romania (Cook and Ciobanu, 2004).In the recent past, almost all calc-alkaline granitoids related to

porphyry (or porphyryskarn) Cu deposits have been argued to be

adakitic rocks (Zhang et al., 2001), which used to be classied as

magnetite-series granitoids (Ishihara, 1977) or crustmantle syn-

tectic granitoids (or syntexis type) (Xuet al., 1982). These granitoids

are derived from a deep source (lower crust), high level of emplace-

ment and high oxidation degree. As mentioned above, these porphy-

ry deposits are also associated with epithermal AuAg deposits,

skarn deposits (if carbonate rocks are present), and vein-like Ag

PbZn deposits. The Yinshan AgPbZn deposit in Northeastern

Jiangxi province is genetically related to the Mesozoic volcanicsub-

volcanic rocks, similar to deposits in Mexico (Simmons et al., 2005).

More specically, the epithermal AgPbZn ore veins in the Yinshan

mine are connected with the porphyry CuAu at depth, forming a

mineral system.

Dexing is a typical porphyry CuAuMo deposit. In outlining a ge-

netic model, Rui et al. (1984) and Pei et al. (1998) proposed that

when 3560% of phenocrysts crystallized from the magma in a shallow

chamber, secondary boilingwould leadto exsolution of an independent

criticalsupercritical magmatic uid phase. This uid phase is alkali and

silica-rich, and has high concentration of volatiles (i.e., H2O, HCl, HF,

SO2, and P2O5) as well as ore-forming metals. At temperatures of

650 C to 750 C and salinities of 0.155 wt.% NaCl equiv., the nature

and composition of this uid has two remarkable implications for the

deposition of mineralization. Firstly, the uids replaced (altered) the

porphyry and country rocks, resulting in a hydrothermal alteration

that is expressed as spotted biotite and K-feldspar (alkali metasoma-

tism). Secondly, its large volume triggers formation of a stockwork frac-

ture system in the roof pendants of the porphyry intrusion which, inturn, is conduciveto extensive convective circulation of magmaticuids

and meteoric water and the precipitation of ore. In fact, theuids that

exsolved from the magma adjusted or changed constantly with temper-

ature decrease, depressurization, immiscibility of brine and gas (phase

separation), water/rock reaction and mixing with meteoric water. All

these contribute to the formation of signicant mineralization, hydro-

thermal alteration and their zoning from the intrusion outwards (see

Pirajno, 2009, and reference therein).

Since the Dexing porphyry and Yinshan porphyry CuAuepithermal

AgPbZn deposits occur within a small area and share the same Middle

Jurassic age it can be reasonably assumed that they belong to the same

mineralizing system(Chen et al., 1989; Pei et al., 1998; Ye, 1987). Follow-

ing a comparative study of available geochemical data and Sr/Nd isotopic

systematics, we can safely assume that the granodiorite in the Dexingarea and the andesitic volcanicsubvolcanic rocks in the Yinshan area

are part of thesame magmatic event. The igneousrocksof the Yinshan de-

posit plot in the elds of both high-K calc-alkaline granitoids and shosho-

nite, whereas those of the Dexing deposits plot in theeld of high-K calc-

alkaline granitoids (Fig. 8). Igneous rocks from both deposits have similar

REE patterns (Fig. 9) and both have an adakitic signature (Fig. 10), sug-

gesting that they originated from enriched mantle with some mixing

with upper crustal material (Fig. 11). We therefore propose that the Dex-

ing porphyry and Yinshan porphyry CuAuepithermal AgPbZn de-

posits belong to the same mineral system, with Dexing porphyry Cu

AuMo at depth and epithermal AgPbZn at shallow levels.

Whether the Jinshan gold deposit is genetically associated with the

Dexing porphyry CuAuMoYinshan porphyryvein CuAgAuMo

deposit system remains debatable. This is because of the lack of suitable

minerals for sufcientlyprecise dating to reveal the age of mineralization

and consequently provide some constraints for a genetic model. In the

past 30 years a large number of dating attemptshaveresulted in a variety

of different age data. For example,Wu and Liu (1989)obtained a whole

rock RbSr isochron age of 168 Ma on illite taken from auriferous sili-

ceous mylonite.Zhang (1994) dated a whole rock chloritized phyllite

byRbSr methods, yielding 161 6 Ma. However,Zhang (1994) also ap-

plied the whole rock RbSr method to date ultramylonite and quartz

veins and obtained an age of 7176 Ma.Mao et al. (2008a)reported aRbSr isochron age of 838 Ma for pyrite from the quartz ore vein. Li et

al. (2007a) reported two K/Ar ages of 299.52.7 Ma and 317.9

1.8 Ma from illite in the auriferous mylonite, and a K/Ar age of 269.9

1.7 Ma for illite in the auriferous quartz veins. Wang et al. (1999)

obtained a RbSr isochron age of 40625 Ma from uid inclusions in

quartz vein and shear zone rocks. Mao et al. (2008b) used the same

method to date the auriferous quartz vein, but obtained an age of

37949 Ma. Due to the limitation of these dating techniques, it is

difcult to verify the reliability of these data. However, although

not accurate, the age data are nevertheless consistent with impor-

tant tectonic events in the geological history of South China. Thus,

the age of 7176 Ma and 838 Ma coincide with the period of con-

vergence of the Yangtze Craton and Cathaysia block, possibly reect-

ing the earliest stages of the formation of the ENE-trending strike-

slip fault. The 40625 Ma age is associated with uplift of the Cath-

aysia Block. The age range between 317.91.8 and 269.91.7 Ma

are not concordant with the convergence between the North China

Craton and South China Block, although the research area is located

far from the continent margin. The ages ranging from 167.9 Ma to

161 6 Ma are consistent with the Late Jurassic magmatism and re-

lated Dexing and Yinshan porphyryepithermal mineralization,

respectively.

Although there are four different opinions about the source of the

ore-forminguids responsible forthe Jinshan gold deposit, the principal

difference is that they are either related to Neoproterozoic metamor-

phism or to Middle Jurassic granitic magmatism. This implies that the

Jinshan is either an orogenic gold or intrusion-related gold deposit.Li

et al. (2007a)pointed out that the formation of the Jinshan gold deposit

is mainly associated with Proterozoic metamorphic uids, possiblyoverprinted by Mesozoic magmatic uids. Through eld investigations

and the examination of existing data, we propose that the NE-trending

strike-slip shear zones throughout the Dexing area were initiated in the

Neoproterozoic and were subsequently reactivated several times. Ex-

cept for the ages above, the other evidence (below) all points to a

Fig. 8.SiO2vs. K2O (wt.%) diagram for the igneous rocks in the Dexing area. The chem-

ical analyzed data are from Zhu et al. (1983), Liu (1994), Ye et al. (1998), Le et al.

(2000), Zhang (2001), and Wang et al. (2004).



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MiddleLate Jurassic age of mineralization. First, the mineralized struc-

tures in Dexing area closely match the Late Jurassic regional tectonic

events. As the Izanagi plate began to subduct beneath the Eurasian con-

tinent at ca. 180 Ma (Dong et al., 2007, Mao et al., 2007, 2008a, 2008b,

2008c; Maruyama et al., 1997; Zhang et al., 2009), oblique compression

from the southeast triggered strike-slip movement on the Anlejiang,

Sizhoumiao, BashiyuanTongchang and JiangguangFujiawu faults in

the Dexing area. Furthermore, the Jinshan shear zone and its parallel

shear zones, which are oblique to the above mentioned regional

strike-slip shear zones appeared as extensional (Fig. 2). Li et al.

(2007a)identied three types of orebodies in Jinshan ore district: 1)

veins associated with fracture-lling; 2) extensional veins; and 3)

stockwork veins. These three types of veins indicate that they are the

products of hydrothermallling and precipitation in an extensional tec-

tonic regime.

Thenature of the ore-forminguid system mustexcludean orogenic-

type gold model. The most prominent features of orogenic-type gold de-

posits are ore-forminguids enriched in CO2and18O, low- to medium-

salinity, and a temperature range from 250 to 350 C (Goldfarb et al.,2005). Ore uids in the Jinshan gold deposit, as revealed by abundant

but small uid inclusions, are, however, of signicantly lower tempera-

ture, medium- to high-salinity and are signicantly depleted in CO2(Fan and Li, 1992; Hua et al., 2002; Zhang and Tan, 1998). Stable isotope

systematics suggests the involvement of magmatic uids. The sulfur iso-

topic values for pyrite in theJinshandeposit (34S=+2.1to +6.7; Fan

and Li, 1992) and for pyrite in Hamashi gold deposit (34S= +2.8 to +

3.4), are sufciently close to those of pyrite from the Dexing porphyry

deposit (34S=2.8 to 3.1;Zhu et al., 1983). However, isotopic ex-

change with the sulfur from the country rocks during ore formation

caused an increase of 34S, as has been shown for lode gold systems of

the Jiangnan Shield (Mao et al., 2002c). Hydrogen and oxygen isotope

compositions show a small range of values in the OH2O vs. D plot,

which are different from metamorphic uids, typically characterized by

a relative wide range. This suggests that the gold mineralization-related

uids are initially magmatic, and then gradually become dominated by

meteoric water. In the Dexing area, shear zones not only control the for-

mation of gold deposits, but also aremajor controlling structures for por-

phyry CuAu and epithermal AgPbZn mineralization. For example, a

shear zone in the Yinshan mine hosts the epithermal AgPbZn ore

veins in the open pit, and also hosts disseminated and orientated CuAu ores(Fig. 6) in the quartz porphyry in the underground workings be-

neath the open pit. In both the North China Craton and the South China

block, Precambrian metamorphic rocks are the most important host

rocks for gold mineralization (Hart et al., 2002; Liu et al., 1993; Mao et

al., 2002a, 2002b; Mao and Li, 1997; Nie et al., 2003; Zhou et al., 2002)

and these rocks are thought to have originally contained more leachable

gold. This is probably a feature of Precambrian metamorphic rocks that

have been subjected to later tectonicmagmaticthermal events, during

which gold is leached out and transported into a new uid system, and

thendeposited in a lodesystem. However, the questionremainswhether

granite intrusions could induce and maintain a high-heat in a localized

area, which is available to mineralization.Seedorff et al. (2005) estimated

that theactivity of a porphyry ore-forming system canlast from 50,000to

500,000 years, during multistage emplacement of intrusions over a peri-od of a few millionyears. Thus,during theLate Jurassic, theemplacement

of deeply-sourced high-K calc-alkaline granites in the Dexing area not

only formed a porphyry CuAuMu depositepithermal-type Ag poly-

metallic deposit system after strong fractionation, but also triggered a

temperature increase in the whole area, leading to a series of convective

hydtrothermal cells (Fig. 12). The magmatic hydrothermal uids migrat-

ed fromhigh potential energy to low potential energy, along ancientfrac-

tures or shear zones, away from the magma chamber, increasingly

becoming mixed with meteoric water and leaching out gold from the

country rocks. These uids precipitated gold ores within suitable struc-

tural host zones upon change in the physico-chemical conditions.

In summary, the Dexing porphyry CuAuMo deposit, Yinshan

porphyry CuAu-epithermal AgPbZn deposit and Jinshan distal

hydrothermal gold deposits formed in the Middle Jurassic and are

Fig. 9. REE patterns of igneous rocks from the Dexing area. Data are from Ye et al.

(1998), Le et al. (2000), Ling and Liu (2001), Zhang (2001), Wang et al. (2004), and

Qian and Lu (2005).

Fig. 10. La/Yb vs. Yb diagram distinguishing the types of the igneous rocks in the

Dexing area. Data are fromLiu (1994), Ye et al. (1998), Le et al. (2000), Ling and

Liu (2001), Wang et al. (2004) and Qian and Lu (2005) .

Fig. 11. Nd(t) vs. (87Sr/86Sr)i diagram showing the source of the igneous rocks in the

Dexing area. The elds in the diagrams are from Jahn et al. (1999) and Zindler and

Hart (1986). Isotopic data are from Zhu et al. (1983), Ye (1987), Zhu et al. (1990)

and Jin et al. (2002).

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genetically associated with high-K calc-alkaline granitoids. They are

thus different from classic porphyry Cu and porphyry Cuepithermal

AuAg deposit systems. They may represent a new ore system, as sche-

matically illustrated inFig. 12.

4.2. Metallogenic geodynamic setting

In thepast 15 years,studies of themetallogenic and geodynamic pro-

cesses in South China have made important progress. Shu et al. (2004),Shu and Wang (2006)proposed that before the Middle Jurassic, South

China block waspart of theTethyan domainand wasstronglyinuenced

by Indosinian orogenesis, characterized by EW-trending faults and folds.

From theMiddle Jurassic,South China becomepart of the Pacic domain

and was mainly inuenced by Paleo-Pacic plate subduction and associ-

ated back-arc extension, associated with intracontinental deep struc-

tures, NNE-trending faults and basin-and-range type rift systems, as

well as forming a large granite province.Gilder et al. (1996)recognized

a lowTDMand high Nd(t) belt from Shiwandashan (or Qinzhou City) in

Guangxi Province, to the northeastern Guangxi Province, Hunan Prov-

ince, central Jiangxi Province to Hangzhou in Zhejiang Province. This is

commonly referred to as the Shihang belt or QinzhouHangzhou belt

and is presumed to be a Mesozoic rift zone.Chen and Jahn, 1998and

Hong et al. (1998)further pointed out that there are a few belts of low

TDMand high Nd(t) on the eastern side of the QinzhouHangzhou belt,

which can be considered as the result of lithospheric extension and

crust/mantle interaction. Li and Li (2007) proposed that South China ex-

perienced at subduction during 250190 Ma, affectinga large area with

a width of 1300 km. This was followed by slab break off at 180155 Ma,

triggering large scale magmatism. Support for this hypothesis comes

from the ca. 500 km long 178173 Ma volcanic belt, extending from

southern Hunan Province, through southern Jiangxi Province to the

southwest Fujian Province (Chen et al., 1999, 2002; Li et al., 2003; Tao

et al., 1998; Wang et al., 2003; Xu, 1992; Zhao et al., 1998; Zhou et al.,

2006). The belt includes bimodal volcanic rocks (alkali basalt, tholeiitic

basalt, rhyolite and a small amount of andesite). This was followed by

the intrusion of Jurassic highly-differentiated I-type granitoids (Li et al.,

2007a, 2007b, 2007c), containing W-Sn ore deposits along NE-trending

faults in South China.Mao et al. (2007, 2008)indicated that Nanling inthe center of the Cathysian block and adjacent northeastern areas, east-

wards from the regional QinzhouHangzhou fault zone is a large W-Sn

metallogenic province, inferred to be related to a MiddleLate Jurassic

slab window event.

In contrast, studies on the metallogenic setting for the porphyry Cu

epithermal Ag polymetallicdistal hydrothermal gold deposits in the

Dexing area are relatively rare, although Zhu et al. (1983) speculated

that it is an intracontinental mineral system.Mao et al. (2004) and Hou

et al. (2007)inferred that this mineralization is related to post-collision

extension, between the North China and South China plates. Wang et

al. (2006) concluded that granodiorite porphyries have adaktic afni-

tiesthat is they represent a product of remelting caused by delaminated

lower crust, along the Shihang rift valley. The Dexing porphyry copperdeposit occurs 50 km north of the Shihang rift zone (Wang et al., 2006),

whereas the Yongping MiddleLate Jurassic skarn-type Cu-deposit occurs

ca. 30 kmsouth of Dexing. Mao et al. (2004, 2007, 2008c) noted that there

is a NE-trending polymetallic metallogenic belt extending for more than

1000 km, which includes the Dexing porphyry CuAuMo, Yinshan por-

phyryepithermal-type silver polymetallic deposit, Lengshuikeng

epithermal-type AgPbZn, Yongping skarn-type copper, Dongxiang hy-

drothermal copper, Qibaoshan and Baoshan porphyry Cu, Shuikoushan

hydrothermal vein PbZn, Tongshan porphyry copper, Yuanzhuding por-

phyry CuMo and Dabaoshan porphyryskarn CuMo deposits (Fig. 1)

inboard of theSouth China continental margin. Thedeposits in this metal-

logenic belt along the QinzhouHangzhou rift belt (or Neoproterozoic su-

ture zone) have ages ranging from 180 Ma to 165 Ma (2008a, 2008b,

2008c, Li et al., 2007b; Mao et al., 2004), and are spatially, temporally

and genetically associated with high oxidation magnetite-series granodi-

oriteand diorite, as dened by Ishihara (1977)or crustmantlesyntectic-

type granites, as dened byXu et al. (1982). Recently,Guo et al. (2010)

carried out petrological and geochemical studies on these granitic rocks

and summarized their characteristics as follows. (A) The mac minerals

of these granitic rocks are predominatly hornblende with lesser biotite;

plagioclase shows zonal textures, K-feldspar is mostly microcline, and

themagnetite content is larger than that of ilmenite. (B)These granitoids

are peraluminous high-K calc-alkaline with 56.24%68.8% SiO2, 4.02%

10.55% (K2O+Na2O), K2ONNa2O and A/CNK=0.791.57. (C) Their REE

distribution patterns show generally a right inclined smooth curve,

(La/Yb)N=4.4329.07, a weak negative Eu anomaly, Eu=0.621.36,en-

richment of LILE and depletion of NbTa, Ba, Sr and Ti. (D) Their initial

(87Sr/86Sr)i=0.7050280.722376, Nd=12.31.80, are related to high

Nd(t) values, lowTDMof high-K calc-alkaline series rocks. (E). The ore-forming elements are Cu, Mo, Fe, Au, Ag, Pb, and Zn. These granitoids

may be derived from the upwelling mantle, which produced partialmelt-

ing of mixed crustmantle materials (Arnaud et al., 1992; Thompson,

1996; Wang et al., 2003). In comparison with melts formed by simple

Fig. 12.Schematic model of porphyry CuAu, epithermal AgPbZn and distal hydrothermal Au deposits in the Dexing area.

http://localhost/var/www/apps/conversion/tmp/scratch_2/image%20of%20Fig.%E0%B1%B2


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granulite anatexis, they are characterized by positive Eu anomalies, low

K2O, high Na2O (N4.3%), Nd=6.0 to 5.8 (Kong et al., 2000, Rapp

and Watson, 1995; Sen and Dunn, 1994). Therefore, the granitoids in

the South China belt cannot have formed by anatexis of granulite facies

lower crust. The e Ndvs. 87Sr/86Sr diagram shows that these granitoids

plot on the evolutionary line of the mantle and lower crust in which it is

shown that the Dexing granodiorite porphyry is derivedfrom the mantle,

whereas other granitoids have varying degrees of contamination with

crustalmaterials. Themetal associations and the components of the relat-ed granitoids, indicate that as more crustal materials were involved in the

formation of the mantle-derived magmatic systems, the metal associa-

tions typically evolve from CuAuMoCuAgPbZnAgPbZn.

Considering that the 1000 km long NE-trending metallogenic belt of

porphyryskarn and epithermal CuAuMoPbZn deposits and related

magmatic rocks is oblique to the subduction zone of the Izanagi plate

(or Paleo-pacic plate), the presence of Jurassic extensive transpressional

structures and thrust nappes in thebeltcan be considered to have formed

in the back-arc setting of an active continental margin. In contrast, the

aforementioned 500 km long belt of 178173 Ma bimodal volcanic

rocks in southern Hunan Province, through southern Jiangxi Province to

the southwest Fujian Province, is perpendicular to the line of subduction.

Thus, unlikethese bimodal volcanic rocks the magmatic rocks in the poly-

metallic ore belt are possibly the product of partial remelting of the sub-

ducted slab or underplating mantle in an active continental margin.

When the magma derived from the mantle rises to a shallow level in

the crust, porphyry CuAuMo deposits are formed. After more contam-

ination with the crust these magmas will form porphyry CuAuMo to

epithermal AgPbZn deposits, and locally skarn-vein AgPbZn de-

posits. Where Precambrian metamorphic rocks are present, leachable

gold is extracted and precipitated in suitable fractures, such as existing

ductilebrittle shear zones.

Acknowledgments

This research was jointly supported by the Projects 2007CB411405 of

the State Key Fundamental Program, Geological Survey Project

(1212010634001) and the National Natural Science Foundation of China

(No. 40434011). We thank Dr. Xiangyun Chen and Prof. Shuibao Huang

and their teams, as well as local geologists from the mines visited, for pro-

viding invaluable assistance and constructive discussions during oureld

investigations. We are also grateful to Dr. Xiaofen Li and Prof. ZongyaoRui

for their constructive discussions and suggestions. We are indebted to the

two anonymous referees for their constructive and critical reviews, which

greatly helped us to improve this paper.

References

Arnaud, N.O., Vidal, P.H., Tapponier, P., Matte, P.H., Deng, W.M., 1992. The high-K2Ovolcanism of northwestern Tibet: geochemistry and tectonic implications. EarthPlanet. Sci. Lett. 111, 353367.

Chen, J.F., Jahn, B.M., 1998. Crustal evolution of southeastern China: Nd and Sr isotopicevidence. Tectonophysics 284, 101133.

Chen, Y.C., Pei, R.F., Zhang, H.L., Bai, G., Li, C.Y., Hu, Y.J., Liu, H.Q., Xian, B.Q., 1989. TheGeology of Non-ferrous and Rare Metal Deposits Related to Mesozoic Granitoidsin Nanling Regions. Geological Publishing House, Beijing. 506 pp. (in Chinese).

Chen, P.R., Kong, X.G., Wang, Y.X., Ni, Q.S., Zhang, B.T., Ling, H.F., 1999. RbSr isotopicdating and signicance of Early Yanshanian bimodal volcanicintrusive complexfrom South Jiangxi Province. Geol. J. Chin. Univ. 5, 378383 (in Chinese with En-glish abstrast).

Chen, P.R., Hua, R.M., Zhang, B.T., Lu, J.J., Fan, C.F., 2002. Early Yanshanian post-orogenicgranitoids in the Nanling region: petrological constraints and geodynamic settings.Sci. China (Ser. D) 32, 279289 (in Chinese).

Cheng, Y.Q., 1994. An Introduction to Regional Geology of China. Geological PublishingHouse, Beijing. 517 pp. (in Chinese).

Cook,N.J., Ciobanu, C.L., 2004. Bismuth tellurides and sulphosalts fromthe Larga hydro-thermal system, Metaliferi Mts., Romania: paragenesis and genetic signicance.Mineral. Mag. 68, 301321.

Cooke, D., Hollings, P., Holliday, J., 2008. Circum-Pacic porphyry copper, gold andmolybdenum deposits. The Pacic Rim: Mineral Endowment, Discovery &Exploration Frontiers. The Australasian Institute of Mining and Metallurgy,pp. 714.

Dong, S.W., Zhang, Y.Q., Long, C.X., Yang, Z.Y., Ji, Q., Wang, T., Hu, J.M., Chen, X.H., 2007. Ju-rassicTectonicRevolutionin China andNew Interpretation of theYanshan Movement.Acta Geol. Sin. 81, 14491461 (in Chinese with English abstract).

Fan, H.R., Li, Z.L., 1992. Geological characteristics, physico-chemical conditions andsource materials for mineralization of the Jinshan gold deposit. Sci. Geol. Sin. 17(suppl.), 147160 (in Chinese with English abstract).

Gilder, S.A., Gill, J., Coe, R.S., Zhao, X.X., Liu, Z.W., Wang, G.X., Yuan, K.R., Liu, W.L.,Kuang, G.D., Wu, H.R., 1996. Isotopic and paleomagnetic constraints on the Meso-zoic tectonic evolution of South China. J. Geophys. Res. 101, 1613716154.

Goldfarb, R.J., Baker, T., Dub, Groves, D.I., Hart, C.J.R., Gosselin, P., 2005. Distribution,character of gold deposits in metamorphic terranes. Economic Geology 100th An-

niversary Volume, pp. 407450.Greentree, M.R., Li, Z.-X., 2008. The oldest known rocks in south-western China:SHRIMP UPb magmatic crystallisation age and detrital provenance analysis ofthe Paleoproterozoic Dahongshan Group. J. Asian Earth Sci. 33, 289302.

Guo, C.L., Mao, J.W., Chen, Y.C., 2010. Zircon SHRIMP UPb dating, geochemistry,SrNdHf isotopic analysis of the Yingqian intrusion in Jiangxi Province,South China and its geological signicance. Acta Petrol. Sin. 26, 919937 (inChinese with English abstract).

Hart, C.J.R., Goldfarb, R.J., Qiu, Y., Snee, L.W., Miller, L.D., Miller, M.L., 2002. Gold de-posits of the northern margin of the North China craton: multiple late Paleozoic Mesozoic mineralizing events. Miner. Deposita 37, 326351.

Hong, D.W., Xie, X.L., Zhang, J.S., 1998. Isotope geochemistry of granitoids in SouthChina and their metallogeny. Resour. Geol. 48, 251264.

Hou, Z.Q., Pan, X.F., Yang, Z.M., Qu, X.M., 2007. Porphyry Cu(MoAu) deposits not re-lated to oceanic-slab subduction: examples from Chinese porphyry deposits incontinental settings. Geoscience 21, 332351 (in Chinese with English abstract).

Hua, R.M., Li, X.F., Zhang, K.P., Qiu, D.T., Yang, F.G., 2002. Geochemical features of ore-forming uid in the Jinshan gold deposit, Jiangxi Province. J Nanjing Univ. (Nat.Sci.) 38, 408417 (in Chinese with English abstract).

Huang, H.L., Yang, W.S., 1990. Geological characteristicsand genesis of Jinshangold deposit inthe northeasternJiangxiprovince. Contrib.Geol. Min.Resour.Res. 5, 2939 (in Chinese).

Ishihara, S., 1977. The magnetite-series and ilmenite-series granitic rocks. Min. Geol.27, 293305.

Jahn, B.M., Wu, F.Y., Lo, C.H., Tsai, C.H., 1999. Crustmantle interaction induced by deepsubduction of the continental crust: geochemical and SrNd isotopic evidencefrom post-collisional mac-ultramac intrusions of the northern Dabie complex,central China. Chem. Geol. 157, 119146.

JBGMR (Jiangxi Bureau of Geology and Mineral Resources), 2005. Assessment for TungstenResource of Zhangyuan Mining Corporation in Chongyi County of Jiangxi Province. 58pp. (in Chinese).

JBGMR (Jiangxi Bureau of Geology & Mineral Resources), 1984. Regional Geology ofJiangxi Province. Geological Publishing House, Beijing. 921 pp. (in Chinese).

Ji, J.F., Shun, C.Y., Zheng, Q., 1994. The metallogenetic characteristics of auriferousquartz veins in the Jinshan shear zone type gold deposit, Jiangxi Province. Geol.Rev. 40, 361367 (in Chinese with English abstract).

Jin, Z.D., Zhu, J.C., Li, F.C., 2002. O, Sr and Nd isotopic tracing of ore-forming process inDexing porphyry copper deposit, Jiangxi Province. Min. Deposits 21, 341349 (inChinese with English abstract).

Kelley, K.D., Lang, J., Eppinger, R.G., 2010. Exploration geochemistry at the giant pebbleporphyry CuAuMo deposit, Alaska. SEG Newsl. 80, 123.

Kong, H., Jin, Z.M., Lin, Y.X., 2000. Petrology and chronology of granulite xenolith inDaxian County, Hunan Province. J. Changchun Univ. Sci. Technol. 30, 115119 (inChinese with English abstract).

Lang, J.R., Rebagliati, C.M., Roberts, K., Payne, J.G., 2008. The Pebble coppergoldmolybdenum porphyry deposit, South-West Alaska, USA. The Pacic Rim: Min-eral Endowment, Discovery & Exploration Frontiers. The Australasian Instituteof Mining and Metallurgy, pp. 2732.

Le, X.H., Xu, X.R., Hao, Q.Z., 2000. Research on magma origin and minerogenetic back-ground of subvolcanic rock in Yinshan ore district, Jiangxi Province. Geotect.Metall. 24, 385389 (in Chinese with English abstract).

Li, C.M., 1994. The geological characteristics of Yinshan copperzinclead deposit,Jiangxi Province. Geol. Prospect. 6, 38 (in Chinese).

Li, Z.X., Li, X.H., 2007. Formation of the 1300-km-wide intracontinental orogen andpostorogenic magmatic province in Mesozoic South China: a at-slab subductionmodel. Geology 35, 179182.

Li, X.F., Sasaki, M., 2007. Hydrothermal alteration and mineralization of Middle Jurassic

Dexing porphyry CuMo deposit, southeast China. Resour. Geol. 57, 409426.Li, X.H., Zhou, G.Q., Zhao, J.X., Fanning, C.M., Compston, W., 1994. SHRIMP ion micro-

probe zircon UPb age of the northeastern Jiangxi ophiolite and its tectonic impli-cations. Geochimica 23, 125131 (in Chinese with English abstract).

Li, X.H., Zhao, J.X., McCulloch, M.T., Zhou, G.Q., Xing, F.M., 1997. Geochemical and SmNdisotopic study of Neoproterozoic ophiolites from southeastern China: petrogenesisand tectonic implications. Precambrian Res. 81, 129144.

Li, Z.X., Li, X.H., Zhou, H., Kinny, P.D., 2002. Grenvillian continental collision in SouthChina: new SHRIMP UPb zircon results and implications for the conguration ofrodinia. Geology 29, 211214.

Li, X.H., Chen, Z.G., Liu, D.Y., Li, W.X., 2003. Jurassic grabbrosyenite suites from south-ern Jiangxi province, SE China: age, origin, and tectonic signicance. Int. Geol. Rev.45, 898921.

Li,X.F., Wang, C.Z., Yi,X.K., Feng, Z.H., Wang, Y.T., 2007a. Deformationstructures at variousscales andtheir roles during goldmineralization at Jinshangold deposit,Jiangxi Prov-ince. Geol. Rev. 53, 774782 (in Chinese with English abstract).

Li, X.F., Watanabe, Y., Mao, J.W., Liu, S.X., Yi, X.K., 2007b. Sensitive high-resolution ionmicroprobe UPb zircon and 40Ar39Ar muscovite ages of the Yinshan deposit inthe northeast Jiangxi Province, South China. Resour. Geol. 57, 325337.



13/14

Li,X.H.,Li, Z.X., Li,W.X., Liu, Y., Yuan, C., Wei, G.J., Qi, C.S., 2007c. UPb zircon, geochem-ical and SrNdHf isotopic constraints on age and origin of Jurassic I- and A-typegranites from central Guangdong, SE China: a major igneous event in response tofoundering of a subducted at-slab? Lithos 96, 186204.

Li, X.F., Yi, X.K., Zhu, H.P., 2009. Source of ore-forming uids in Jinshan gold deposit ofDexing County: constraints from microstructures and stable isotope. Min. Deposits28, 4252 (in Chinese with English abstract).

Li, X.F., Wang, C.Z., Hua, R.M., Wei, X.L., 2010. Fluid origin and structural enhancementduring mineralization of the Jinshan orogenic gold deposit, South China. Miner.Deposita 45, 583597.

Ling, Q.C., Liu, C.Q., 2001. Geochemistry of trace elements during ore-forming processes

in Yinshan deposit. Earth Sci.J. China Univ. Geosci. 26, 473485 (in Chinese withEnglish abstract).Liu,J.Y., 1994. Subvolcanic magmatism and Au, Cu polymetallization in Yinshan,Jiangxi. J.

Guilin Coll. Geol. 14 (3), 244254 (in Chinese with English abstract).Liu, Y.J., Sha, P., Zhu, K.J., 1989. The study on geochemistry of the gold-bearing formation

of Middle Proterozoic Shuangqiaoshan Group in Dexing district, Jiangxi.J. Guilin Coll.Geol. 9, 115126 (in Chinese with English abstract).

Liu, Y.J., Sun, C.Y., Ma, D.S., 1993. Gold Deposits in Jiangnan Region and its GeochemicalBackground of Ore Formation. Nanjing University Press, Nanjing, pp. 6186 (inChinese).

Liu, Z.Y., Jin, C.Z., Wang, R.H., Liang, J.H., 2005. Ore uid geochemistry and the discussionon ore genesis of Jinshan gold deposit, Jiangxi Province. Contrib. Geol. Min. Resour.Res. 20, 93105 (in Chinese with English abstract).

Lu, J.J., Hua, R.M., Yao, C.L., 2005. ReOs age for molybdenite from the Dexing porphyryCuAu deposit in Jiangxi province, China. Geochim. Cosmochim. Acta 69 (suppl.),A882.

Mao, J.W., Li, H.Y., 1997. Research on genesis of the gold deposits in the Jiangnan Terrain.Geochimica 26, 7181 (in Chinese with English abstract).

Mao, J.W., Qiu, Y.M., Goldfarb, R.J., Zhang, Z.C., Ren, F.S., 2002a. Geology, distribution,

and classication of gold deposits in the Western Qinling belt, central China.Min. Deposita 37, 352377.

Mao, J.W., Goldfarb, R.J., Zhang, Z.W., Xu, W.Y., Qiu, Y.M., Deng, J., 2002b. Gold depositsin the XiaoqinlingXiong'ershan region, Qinling Mountains, central China. Min.Deposita 37, 306325.

Mao, J.W., Mao, J.W., Kerrich, R., Li, H.Y., Li, Y.H., 2002c. High 3He/ 4He ratios in theWangu gold deposit, Hunan Province, China; implications for mantle uids alongthe Tanlu deep fault zone. Geochem. J. 36, 197208.

Mao, J.W., Xie, G.Q., Li, X.F., Zhang, C.Q., Mei, Y.X., 2004. Mesozoic large scale mineraliza-tionand multiple lithospheric extension in South China. Earth Sci.Front. (China Univ.Geosci., Beijing) 11, 4555 (in Chinese with English abstract).

Mao, J.W., Xie, G.Q., Guo, C.L., Chen, Y.C., 2007. Large-scale tungstentin mineralizationin the Nanling region, South China: metallogenic ages and corresponding geody-namic processes. Acta Petrol. Sin. 23, 23292338 (in Chinese with Englishabstract).

Mao, G.Z., Hua, R.M., Gao, J.F., Long, G.M., Lu, H.J., 2008a. RbSr age of gold-bearing py-rite of the Jinshan gold deposit, Jiangxi Province. Acta Geosci. Sin. 29, 599606 (inChinese with English abstract).

Mao, G.Z., Hua, R.M., Long, G.M., Lu, H.J., 2008b. Discussion on the mineralogeneticepoch of the Jinshan gold deposit, Jiangxi Province: based on the quartz uids in-clusion RbSr dating. Acta Geol. Sin. 82, 532539 (in Chinese with Englishabstract).

Mao, J.W., Xie, G.Q., Guo, C.L., Yuan, S.D., Cheng, Y.B., Chen, Y.C., 2008c. Spatialtemporaldistribution of Mesozoic ore deposits in South China and their metallogenic settings.Geol. J. China Univ. 14, 510526 (in Chinese with English abstract).

Maruyama, S., Isozaki, Y., Kimura, G., Terabayashi, M., 1997. Paleogeographic maps ofthe Japanese Islands: plate tectonic synthesis from 750 Ma to the present. IslandArc 6, 121142.

Ni, P., 2010. Research Report of the Metalogenic Regularities of Copper Deposits in theAdjacent Region of Fujian, Jiangxihand Zhejiang Provinces in Eastern China. Nan-

jing, Nanjing University, Internal Report (in Chinese).Nie, F.J., Jiang, S.H., Liu, Y., 2003. Intrusion-related gold deposits of North China craton,

People's Republic of China. Resour. Geol. 54, 299324.Ohmoto, H., 1986. Stable isotope geochemistry of ore deposits. Rev. Mineral. 16,

491559.Pei, R.F., Wu, L.S., Xiong, Q.Y., 1998. Metalogenic Preferentiality and Exceptional Metal-

lotect Convergence of Giant Ore Deposits in China. Geological Publishing House,

Beijing, pp. 6972 (in Chinese).Pirajno, F., 2009. Hydrothermal Processes and Mineral Systems. Springer, Berlin. 1250pp.Pirajno, F., Bagas, L., 2002. Gold and silver metallogeny of the South China Fold Belt: a

consequence of multiple mineralizing events? Ore Geol. Rev. 20, 109126.Qian, P., Lu, J.J., 2005. The material resources of granodiorite porphyry in the Dexing

copper ore district: a study on trace elements. Contrib. Geol. Min. Resour. Res. 20(2), 7579 (in Chinese with English abstract).

Qian, D.D., Zhang, S.W., Wang, Z.T., 1996. The Discovery History of Mineral Depositsof China (Jiangxi Province). Geological Publishing House, Beijing. 243 pp.(in Chinese).

Qiu, Y.M., Gao, S., McNaughton, N., Groves, D.I., Ling, W.L., 2000. First evidence of3.2 Ga continental crust in the Yangtze craton of South China and its implica-tions for Archean crustal evolution and Phanerozoic tectonics. Geology 28,1114.

Rapp, R.P., Watson, E.B., 1995. Dehydration melting of metabasalt at 8 32 kbar: implica-tions for continental growth and crustmantle recycling. J. Petrol. 36, 891931.

Rebagliati, C.M., Payne, J.G., 2005. Summary report on the pebble porphyry coppergold project [online], Northern Dynasty Minerals Ltd., N43-101, llingAvailablefromhttp://www.sedar.com2005.

Rui, Z.Y., Huang, C.K., Qi, G.M., Xu, Y., Zhang, H.T., 1984. Porphyry Copper (Molybdenum)Deposits of China. Geological Publishing House, Beijing. 350 pp. (in Chinese with En-glish abstract).

Rui, Z.Y., Zhang, L.S., Wu, C.Y., Wang, L.S., Song, X.Y., 2005. Dexing porphyry copper de-posits in China. In: Porter, D.M. (Ed.), Supper Porphyry Copper & Gold Deposits: AGlobal Prospecting, vol. 2. PGC Publishing, Adelaide, pp. 409421.

Seedorff, E., Dilles, J.H., Proffett Jr., J.M., Einaudi, M.T., Zurcher, L., Stavast, W.J.A., Johnson,D.A., Barton, M.D., 2005. Porphyry deposits: characteristics and origin of hypogenefeatures. Economic Geology 100th Anniversary Volume, pp. 251298.

Sen, C., Dunn, T., 1994. Dehydration melting of a basaltic composition amphibolite at1.5 and 2.0 Gpa: implications for the origin of adakites. Contrib. Mineral. Petrol.

117, 394409.Sheppard, S.M.F., 1986. Characterization and isotopic variations in natural waters. Rev.Mineral. 16, 165183.

Shu, L.S., Wang, D.Z., 2006. A comparison study of basin and range tectonics in thewestern North America and southeastern China. Geol. J. China Univ. 12, 113 (inChinese with English abstract).

Shu, L.S., Zhou, X.M., Deng, P., Yu, X.Q., Wang, B., Zu, F.P., 2004. Geological features andtectonic evolution of Meso-Cenozoic basins in southeastern China. Geol. Bull.China23, 876884 (in Chinese with English abstract).

Shui, T., 1988. Tectonic framework of the continental basement of southeast China. Sci.China (Ser. B) 31, 885895.

Simmons, S., White, N.C., John, N.C., 2005. Geological characteristics of epithermal pre-cious and base metal deposits. Economic Geology 100th Anniversary Volume, pp.485522.

Tao, K.Y., Mao, J.R., Yang, Z.L., Zhao, Y., Xing, G.F., Xue, H.M., 1998. Mesozoic petro-tectonic associations and records of the geodynamic processes in southeastChina. Earth Sci. Front. (China Univ. Geosci., Beijing) 5, 183190 (in Chinese withEnglish abstract).

Thompson, A.B., 1996. Fertility of crustal rocksduring anatexis. Trans. R. Soc. Edinburgh

(Earth Sci.) 87, 110.Wang, H., Mo, X., 1995. An outline ofthe tectonic evolution of China.Episodes 18,616.Wang, X.Z., Liang, H.Y., Shan, Q., Cheng, J.P., Xia, P., 1999. Metallogenic age of the Jin-

shan gold deposit and Caledonian gold mineralization in South China. Geol. Rev.45, 1925 (in Chinese with English abstract).

Wang, Y.J., Fan, W.M., Guo, F., Peng, T.P., Li, C.W., 2003. Geochemistry of Mesozoic ma crocks adjacent to the ChenzhouLinwu fault, South China: i mplication for the litho-sphere boundary between the Yangtze and Cathysia Blocks. Int. Geol. Rev. 45,263286.

Wang, Q., Zhao, Z.H., Jian, P., Xu, J.F., Bao, Z.W., Ma, J.L., 2004. SHRIMP zircon geochro-nology and NdSr isotopic geochemistry of the Dexing granodiorite porphyries.Acta Petrol. Sin. 20, 315324 (in Chinese with English abstract).

Wang, Q., Xu, J.F., Jian, P., Bao, Z.W., Zhao, Z.H., Li, C.F., Xiong, X.L., Ma, J.L., 2006. Petro-genesis of adakitic porphyries in an extensional tectonic setting, Dexing, SouthChina: implications for the genesis of porphyry copper mineralization. J. Petrol.47, 119144.

Wei, X.L., 1985. Geological characteristics and metallogenic process of Jinshan gold de-posit, Jiangxi Province. Min. Resour. Geol. 9, 471480 (in Chinese).

Wei, X.L., 1995. Geological characteristics and gold mineralization of the Jinshan golddeposit. Min. Resour. Geol. 9, 471478 (in Chinese).

Wei, X.L., 1996. The geological characteristics of Jinshan ductile shear zone-type golddeposit in Jiangxi. Geol. Jiangxi 10, 5264 (in Chinese with English abstract).

Wu, Q.S., Liu, Q.L., 1989. Metallogenic age determine and discussion on ore-depositgenesis of Jinshan gold deposit. Article (abstract) Corpus of the 4th National Iso-tope Geology Ages and Isotope Geochemistry Forum (in Chinese).

Xu, M.H., 1992. Early Jurassic bimodal volcanic rocks and their structure environmentin Yongding County, Fujian Province. Geol. Fujian 11, 115125(in Chinesewith En-glish abstract).

Xu, B., Qiao, G.S., 1989. SmNd isotopic age and tectonic setting of the Late Proterozoicophiolites in northeastern Jiangxi Province. J. Nanjing Univ.-Earth Sci. (3), 108114(in Chinese with English abstract).

Xu, K.Q., Hu, S.X., Sun, M.Z., Ye, J., 1982. On the two genetic series of granites inSoutheastern China and their metallogenetic characteristics. Min. Deposits 1,114 (in Chinese with English abstract).

Yang, W.M., Li, C.C., Han, X.L., 2000. Study on uid inclusion of Jinshan gold deposit inJiangxi. Gold 21, 911 (in Chinese with English abstract).

Yang, B., Peng, S.L., Yang, M., Lin,D.S., He, G.C., 2004. Mechanism of hydrothermal convec-

tion and alterationmineralization zoning in Yinshan CuPbZn deposit, Jiangxi.J. Guilin Inst. Technol. 24, 395401 (in Chinese with English abstract).

Ye, Q.T., 1987. Metallogenetic Series of LeadZinc Ore Deposits in Northeast Jiangxi.Beijing Science & Technology Press. 114 pp. (in Chinese with English abstract).

Ye,S., Wang,Q., Mo,X.X.,1998. Petrology of thevolcanicsubvolcanic rocks fromYinshan inDexing County, Jiangxi Province. Geoscience 12 (3), 353359 (in Chinese with Englishabstract).

Ye, M.-F., Li, X.-H., Li, W.-X., Liu, Y., Li, Z.-X., 2007. SHRIMP zircon UPb geochronologicaland whole-rock geochemical evidence for an early Neoproterozoic Sibaoan magmaticarc along the southeastern margin of the Yangtze Block. Gondwana Res. 12, 144156.

Zhang, J.C., 1994. Study on mineralization geochemistry of Jinshan ductile shear zonetype gold deposit in Jiangxi. Unpublished M.Sc. Thesis, Nanjing University, 78 pp.(in Chinese with English abstract).

Zhang, W.L., 2001. Contrasts of the sub-dacitic porphyry in Xiangshan, Yinshan andZijinshan oreelds. Geol. Prospect. 37 (4), 3842 (in Chinese with Englishabstract).

Zhang, W.H., Tan, T.L., 1998. Relationship between organic uids and goldmineralization in the Jinshan gold deposit, Jiangxi Province. Min. Deposits 17,1524 (in Chinese with English abstract).

http://www.sedar.com/http://www.sedar.com/


14/14

Zhang, L., Liu, J., Yu, G., Chen, Z., 1996. Hydrogen and oxygenisotopes of the waterrockinteraction in the Yinshan CuPbZnAg deposit, Jiangxi Province. Acta Geol. Sin.(English Edition) 9, 274289.

Zhang, D., Yu, C., Bao, Z., Tang, Z., 1997. Ore zoning and the dynamics of ore-formingprocesses in the Yinshan polymetallic deposit, Jiangxi. Chin. J. Geochem. 16,123132.

Zhang, Q., Wang, Y., Qian, Q., Yang, J.H., Wang, Y.L., Zhao, T.P., Guo, G.J., 2001. The charac-teristics and tectonicmetallogenic signicances of the adakites in Yanshan periodfrom eastern China. Acta Petrol. Sin. 17, 236244 (in Chinese with English abstract).

Zhang, D.H., Xu, G.J., Zhang, W.H., Golding, S.D., 2007. High salinityuid inclusions in theYinshan polymetallic deposit from the LeDe metallogenic belt in Jiangxi Province,

China: their origin and implications for ore genesis. Ore Geol. Rev. 31, 247260.Zhang, Y.Q., Xu, X.B., Jia, D., Shu, L.S., 2009. Deformation record of the change fromIndosinian collision-related tectonic system to Yanshanian subduction-related tec-tonic system in South China during the Early Mesozoic. Earth Sci. Front. 16,234247 (in Chinese with English abstract).

Zhao, Z.H., Bao, Z.W., Zhang, B.Y., 1998. The geochemistry characteristics of Mesozoicbasalts in the South Hunan Province. Sci. China (Ser. D) 28 (suppl), 714 (inChinese).

Zheng, J.P., Grifn, W.L., O'Reilly, S.Y., Zhang, M., Pearson, N., Pan, Y.M., 2006. Wide-spread Archean basement beneath the Yangtze Craton. Geology 34 (6), 417420.

Zhou, G.Q., Zhao, J.X., 1991. Study of SmNd isotopic composition of ophiolites fromsoutheastern margin of Yangtze Craton of South China in the eastern Jiangxi prov-ince. Bull. Chin. Sci. 36, 129132 (in Chinese).

Zhou, X.M., Zhu, Y.H., 1993. Late Proterozoic collisional orogen and geosuture in south-eastern China: petrological evidence. Chin. J. Geochem. 12, 239251.

Zhou, T.H., Goldfarb, R.J., Phillips, G.N., 2002. Tectonics and distribution of gold depositsin China: an overview. Min. Deposita 37, 249282.

Zhou, X.M., Sun, T., Shen, W.Z., Shu, L.S., Niu, Y.L., 2006.Petrogenesis of Mesozoic granitoidsand volcanic rocks in South China: a response to tectonic evolution. Episodes 29,2633.

Zhu, X., Huang, C.K., Rui, Z.Y., Zhou, Y.H., Zhu, X.J., Hu, Z.S., Mei, Z.K., 1983. The Geology

of Dexing Porphyry Copper Ore Field. Geological Publishing House, Beijing. 336 pp.(in Chinese with English abstract).Zhu, J.C., Shen, W.Z., Liu, C.S., 1990. NdSr isopopic characteristics and genetic discussion

of Mesozoic granitoids of syntexis series. Acta Petrol. Mineral. 9 (2), 177184 (inChinese).

Zindler, A., Hart, S.R., 1986. Chemical Geodynamics. Ann. Rev. Earth Planet. Sci. 14,493571.

Zou, H.Y., 1993. Relationship between organic matter and gold mineralization in ductileshear belt, Jinshan gold deposit, Jiangxi Province. Gold Sci. Technol. (3), 1012 (inChinese).


Epithermal. Franco Pirajno 2011

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