Characteristics of Ore-forming Fluid of the Gaoshan Gold—Silver Depositin the Longquan Area，Zhejiang Province and its Implications for the

Ore Genesis

JIANG Biao‘，WANG Chenghuil’，CHEN Yuchuanl一，、舢Baogui3，LIAO Pen93，

CHEN Zhengle4 and HAN Fengbin4

1 MLR Key Laboratory ofMetallogeny and Mineral Assessment,Institute ofMineral Resources，Chinese

Academy ofGeological Sciences，Bering 10003Z China

2 ChineseAcademy ofGeological Sciences，Beoing 1 0003 7J China

3 No．7 Geological Team ofZhejiang Province,L括huL Zhejiang 323000

4 Institute ofGeomechanics，Chinese Academy ofGeological Sciences，Beo'ing 1 00081

Abstract：The Gaoshan gold—silver deposit．10cated between the Yuyao—Lishui Fault and Jiangshan—

Shaoxing fault in Longquan Area，Occurs in the Suichang-Longquan gold—silver polymetallic

metallogenic belt．This study conducted an investigation for ore．forming fluids using

microthermometry．D-O isotope and trace element．The results show that two types of fluid inclusions

involved into the formation of the deposit are pure liquid phase and gas-liquid phase aqueous

inelusions．The homogenization temperature and salinity of maior mineralization phase ranges from

1560C to 2360C(average 2000C)and 0．35％to 8．68％(NaCleqv)(average 3．68％)，respectively，

indicating that the ore-forming fluid is characteristic of low temperature and low salinity．The ore．

forming pressure ranges between in 1 18．02 to 232．13’105 pa．and it is estabmiated that the ore．

forming depth ranges from O．39 to 0．77 km．indicating it is a hypabyssal deposit in genesis．The low

rare earth elements content in pyrites．widely developed fluorite in late ore-forming stage and Iack of

chlorargyrite(AgCl)．indicates that the ore-forming fluid is rich in F rather than C1．The ratios of Y／

Ho，Zr／Hf and Nb／Ta of between difierent samples have little difierence，indicating that the later

hydrothermal activities had no effects on the former hydrothermal fluid．The chondrite-normalized

REE patterns of pyrites from country rocks and ore veins are basically identical，with the

characteristies of light REE enrichment and negative Eu anomalies．implying that the ore—forming

fluid was oxidative and derived partly from the country rocks．The dD and否“O of fluid inclusions in

quartz formed during the main metallogenic stage range from-105％o to-69‰and-6．01‰to

-3．8l‰．respectively．The D．O isotopic diagram shows that the metallogenic fluid is characterized by

the mixing of formation water and meteoric water．without involvement of magmatic water．The

geological and geochemical characteristics of the Gaoshan gold—silver deposit are similar to those of

continental volcanic hydrothermal deposit．and could be assigned to the continental volcanic

hydrothermal gold．silver deposit type．

Key words：ore-forming fluid，trace elements，D—O isotope，ore genesis，Gaoshan glod-silver deposit

1 Introduction

The genesis of gold，silver，iron，and copper related to

volcanic rock as well as the prospecting have long been a

hot topic．Generally speaking，the gold and silver deposits

related to volcanic rocks can be preliminarily divided into

+Corresponding author．E-mail：wangchenghui 1 3 l@sina．com

epithermal type，porphyry type，and porphyrite type，etc．

fSillitoe．1 997)．The gold．silver deposits hosted in the

continental．subvolcanic rocks in the southeast of Zhejiangare mainly epithermal type．Epithermal gold deposit is the

research frontier and one of the hot spots of the

international deposit community(Deng and Wang．

20 1 61．The epithermal deposit was initially defined by

Lindgren f 1 933)as a kind of deposit with the depth leSS

◎20 1 6 Geological Society ofChina

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than l km and temperature below 2000C．In the 1 980s，

Bonham(1 986)divided the epithermal gold deposits into

low．sulphidation(LS)，high—sulphidation(HS)andalkaline rock type while Heald et a1．f 1 987)divided them

into alunite．kaolinite type(acid sulphate type)and

adularia．sericite type，which are widely applied in the

deposit community，especially the HS and LS terms which

frequently appear in the epithermal gold deposit

description．In recently years，with the constantly

deepened research，Hedenquist et a1．(2000)proposed the

intermediate sulphidation(IS)deposit between HS and

LS．Circum．pacific magmatic arc environment is an

important metallogenic environment for the epithermal

gold deposit(Corbett，2002)．Most of epithermal gold-

silver deposits found now were formed in the Mesozoic—

Cenozoic．with 1ess formed in the Late Paleozoic，such as

the Axi gold deposit hosted in the Carboniferous

pyroclastic rock in Xinjiang Province，China(Qin et a1．，

2002)，and very few of them may occurred in the

Proterozoic。such as the Hope Brook deposit in

Newfoundland， Canada， which was formed in

Neoproterozoic．The research showed that the epithermal

gold—silver deposits were closely related to alkali rock

(Sillitoe，1 997)．For example，Kelley and Ludington

(2002、proposed that the most important factor that formedthe Cripple Creek gold deposit is the invasion of oxidized

alkaline magma containing volatile matters to the near

surface．A large number of studies have shown that

conversion relation often exists between the epithermal

gold deposits and porphyry deposits(Hedenquist et a1．，

1 998；Muntean and Einaudi，200 1；So Chil．Sup et a1．，

1 998；Feng et a1．．2014)．The study of fluid inclusions can

help constrain the conditions at which diagenetic minerals

precipitated，leading to a better understanding of the

geologic controls and relative timing of changes in

porosity and／or mineralising events(Merangh，20 1 5)．Ore

forming hydrothermal fluids，consisting largely of silicate

melt，H20，C02 and NaCl，formed most of Earth。s mineral

deposits．The ore forming fluids exist as magma，

magmatic fluids，meteoric water，seawater，basinal brine，

and metamorphic fluids．Ore deposit research has been

and will continue to be the main field of application of

fluid inclusions(Chi et a1．，2003；Lu and Shan，20 1 5)．A

series of new concepts，techniques and methods are put

forward and developed，which can promote the study of

geology，especially the study of mineral deposits(Chi and

Lu，2008；Chu and Chi，2015；Zhu et a1．．2015)．

The Gaoshan gold．silver deposit area is under the

jurisdiction of Xianxi Village，Pingnan Town，Longquan

City，Zhejiang province．The metal minerals in the

southeast of Zhejiang are mainly related to widely

distributed magmatic rocks and volcanic rocks，but only

few of them can reach large and medium—sized scale．For

example，the Wubu deposit in Huangyan district is a large

lead—zinc deposit；the Xianlinbu molybdenum—iron deposit

in Yuhang District，the Lizhu iron deposit in Shaoxing，the

Wuao lead—zinc deposit in Longquan，the Shangyang lead-

zinc deposit in Huangyan district．the Qiwan lcad-zinc

deposit in Zhuji，the Xiqiu copper deposit in Shaoxing，the

Linghou copper deposit in Jiande．the Zhilingtou gold—

silver deposit in Suichang，the Dalingkou silver-lead—zinc

deposit in Tiantai and Shipingchuan molybdenum deposit

in Oingtian．etc．are medium．sized deposits．The Gaoshan

gold．silver deposit．which is 10cated between Yuyao—

Lishui fault and Jiangshan．Shaoxing fault and in the west

of Chencai-Suichang uplift in the southeast of Zhejiang，occurs in the Suichang--Longquan gold--silver polymetallic

metallogenic belt．In terms of minerogenetic series，it

belongs to the minerogenetic series of gold，silver，lead，

zinc and molybdenum deposits related to the continental

marginal volcanism in the Yanshanian period(Zhu et a1．．

2009)．Typical deposits include the Zhilingtou gold-silver

(1ead-zinc)deposit in Suichang，the Babaoshan gold—silver

deposit in Longquan，the Luoshan gold—silver deposit in

Dongyang，and the Nongkeng silver deposit in Wuyi．

Previous research on the deposits above，especially the

Zhilingtou deposit，is relatively deeply(Zhou，1 985；

Zheng and Liu，1987；Peng，1989；Hu，1993；Chen and

Lin，1994；Zhou，2004，2005；Pu，2009；Qian et a1．；2010；

Duan，201 5)．The Gaoshan gold-silver deposit is located

in the Junxi Gaoshan-·Nannong lead·-zinc polymetallic

metallogenie prospective area，and it is one of the 1 1

metallogenic prospective areas divided in the prospecting

project in the old workings of ancient silver mining．

Though it has a long history in mining，the existing

research are only limited to the analysis of metallogenic

tectonics of the area(Zhang et a1．，2016)，and the study of

mineral deposits is almost blank and urgent to be carried

out．Ore—forming fluid is important part for the study of

mineral deposit and also all important basis for

determining the genesis．This paper，taking the ore—

forming fluid of the Gaoshan gold—silver deposit as the

important research content，reported the characteristics of

fluid inclusions，stable isotopes and rare-earth elements of

hydrothermal mineral of this deposit for the first time，

determined the nature of ore—forming fluids，explored the

source of ore-forming fluid as well as depositional

mechanism and its constraints on the genesis．

2 Regional Geology and Deposit Geology

The strata exposured in

relatively simple，which

the southeast of Zhejiang are

belong to the Proterozoic

metamorphic rock and Mesozoic volcanic rock that

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unconformably cover on the top．and the structure iS

dominated by fault structure and volcanic structure．The

Yanshanian Period saw the most spectacular and violent

igneous activities in the geohistory of Zhejiang．In termsof the area．9 1．5％of intrusive rocks and 97．4％of

volcanic rocks were formed in this Period．and are the

results of continental margin volcanism in the Mesozoic

era(Zhu et a1．，2009)．The Mesozoic volcanic activity in

the southeast of Zhejiang played an important controlling

role in the formation ofpolymetallic depositssuch as lead．

zinc(silver)deposits(Yang et a1．，1 990)．In the late

Jurassic period，strong volcanic activities occurred，

resulting in the formation of very thick continental

volcanic rocks，mixed with the volcanic debris sediment

and normal sedimentary rocks(Fig．1)，which was closely

related to the formation of many metallic deposits and

nonmetallic deposits．The Gaoshan gold—silver deposit in

Longquan iS one of those hosted within the very thick

Jurassic volcanic sedimentary strata．

The strata exposured in the mining area are a set of

continentalintermediate acid．acid volcanic complex of the

Moshishan Group of the upper Jurassic(J3m)(Fig．2)．It

mainly consists of the Jiuliping(J∥)，Xishantou(J3x)，

Gaowu(J39)，and Dashuang formations(J3力．Thestructure of this mining area iS dominated by faults

including regional NE-trending faults and its secondary

／,4E．NW and nearlv FW—trendine faults．The secondary

NE．-trending faults and EW．．trending faults are the ore．．

control faults of this mining area(Fig．2、．Silicificationalteration and green—colored alteration developed on both

sides ofthose faults．

In the mining area，four mineralization alteration zones

have been found and delineated．The No．1 zone Controlled

bv fault F l and distributed in the northwest of the mining

area is the largest in scale．with the length of 935 m and

width of 4-17 m．and its country rock iS rhyolitic crystal

and vitroclastic welded tuff．The mineralized rock types

mainly include metasomatic(vein)quartzite，strongsilicification crystal pyroclast welded tuff and tectonic

breccia．According to coastean(old workings)and shallow

excavated sampling analysis，the mineralized belt contains

gold of 0．05_2．66卧，maximally 4．16 g／t，and silver of

3．2^70．8鲈，maximally 500 g／t(according to the No．7

Geological Team ofZhejiang Province，2014)．The ore bodies in the Gaoshan gold—silver deposit are

mainly distributed in the old working as well as in drilling

cores．The bodies in the old workings mainly include ore

bodies I一1．I一2 and I-3，with the silver grade of 48．8-500

g／t and gold grade of 0．32-2．66卧．The samples studied

this time were mainly taken from the quartz vein ores in

the drill core．

The ore bodies occur mainly as veins(Fig．41．Duringthe main metallogenic period，the ore type is dominatd by

quartz—sulfide veins(Fig．3、．and occurs mainly aS a

Fig．1．Geological structure map of the southeast Zhejiang Province(revised according to the Geologica

Mineral Recordes ofZhejiang Province)．

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竺 竺!竺 盟世：⋯!墨要筮鉴簋篁兰笠盥墨娑型型竺竺生! 竺竺

Fig．2．Geological map for the Gaoshan gold—silver deposit area

Q。 Quaternary

J， Jiuliping Formation

X兀，， Rhyolite porphyry

Ⅱ“Andesitic porphyry

／／Geological boundary

jL

[

Fig．3．Main ore types ofthe Gaoshan gold—silver deposit．

(a)，quartz banded。sulfide vein type：(h)，quartz spotted-sulfide vein type：(c)，quartz-calcite-sulfide vein type in the late metallogenic

period；(d)．fluorite-calcite—sulfide、7cin type in thc mctallogcnic period

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竺竺 坠!型尘!竖。!盒羔黑撅聪妻燮A。墨黜i，鬟竺k扎㈣讹。。V01．。呲．4 啦s———————————二二———————————．．．．—j!!!巳；：!兰．!!∑．：坚!旦i竺!!翌!璺!!：!翌：!三苎!竺翌!!!!』翌!!兰：!!巳： !竖巳2：里!!：!!!皇翌!!!!垒已!￡兰旦!ral com／a苎s

’u1‘7u 1、u’叶 1j￡J

Fig．4．Profile map ofNo．1 1 exploration line(a)and No．0 exploration line【b)ofthe Gaoshan gold—silver deposit

mineral association of quartz(70％)，galena(8％)，

sphalerite(5％)，pyrite(6％)，stromeyerite(3％)，argentite

(3％)，chalcopyrite(2％)，covellite(<l％)，and calcite

(2％)．In the late stage，fluorite．sulphide vein ores are

present，with a mineral association of fluorite(65％)，

calcite(1 5％)，quartz(5％)，galena(5％)，sphalerite(5％)，

chalcopyrite(3％)，stromeyerite(1％)，and argentite(1％)．The ores occur as the subhedral—xenomorphic congregated

grain structure，metasomatic relict crystalloblastic texture，

angular，crumby，stockwork，and disseminated structure

(Fig．5)．The characteristics and components of majorminerals are briefly introduced as follows．

2．1 Pyrite

It runs through this deposit．It OCCURS in both country

rocks and ores and develops in various stages of the

metallogenic period．Its granular sizes are wide in range，

from several pm to several hundredⅢ：Il，with few reaching

rnrn level．Before the metallogenic period and in the late

stage of the metallogenic period，pyrite presents in cubic

shape(Fig．5)or pentagonal dodecahedron(Fig．5b)，etc．；

dURing the metallogenic period，pyrite OCCURS often as

veinlike(Fig．5c)，allotriomorphic texture(Fig．5d，f)orskeletal texture(Fig．5h)，with pits or pocking marks on the

sURface and showing hydrothermal genesis characteristics．

2．2Zinc

Zinc is only found in the quartz-sulfide ores in the main

metallogenic period，but in minor amount．Besides normal

sphalerite．tllere iS also a small amount of marmatite in the

early stage ofthe metallogenic period(Fig．59)，indicating a

high formation temperature of minerals．and in the late stage

of metallogenic period，sphalerite often shows irregular

shape，with small amount of grains，and mainly coexists

with quartz．part ofwhich formed skeletal texture due to the

metasomatism ofepigenetic pyrite or quartz(Fig．5b，e)．

Z．3 Galenite

Galenite iS also only found in the quartz．sulfide ore in the

main metallogenic period，and Occurs occasionally as

extremely small grains．which iS invisible to the naked eyes．

It shows light grey under the microscope，with strong

metallic luster．It was mainly formed during the early stage

of the metallogenic period and OCCURS in rag，sieve and

helicitic textures due to the metasomatism of epigenetic

minerals．111e independent minerals such as galenite and

silver show no paragenic and associated relationships，but

the result of electronic probe shows that Ag content in

galenite is relatively high．Therefore，silver may exist in

galenite in the form of micro inclusion or isomorphism．

2．4 Stromeyerite

Stromeyerite is one of the major silver minerals in this

area，and only develops in quartz—sulfide ores，with the

grain size of generally not more than 200岬，and few over

500 pm．It is white and lavender gray under the microscope，

and wraps and metasomatizes the antecedent minerals

(generally pyrite)and forms rimmed texture(Fig．5h)．

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竺 竺!竺 坠皿坐坐壁笾金显盟邕望登盛竺竺当坚生!型型 竺竺

Fig．5．Main mineral association and mineral phase characteristics of the Gaoshan Gold—silver deposit

Arg．argentite；Cal—calcite；Ccp—chalcop)rite；Cv—COX ellite；Gn—galena；Oz—quartz：Sph—sphalerite；Stm—stromeyerite

2．5 Argentite

Argentite iS another important siIver mineral in this

area．and iS only found in quartz．sulfide minerals．Its

content in the late metallogenic stage is higher than that in

the early stage．It is grayish purple color and occurs in

allotriomorphic granular texture with small grain sizes，

generally not more than 200 lam．It coexists with

chalcopyrite and often metasomatized the antecedent

chalcopyrite，forming skeleton crystal．

2．6 Chalcopyrite

It is one of the important carriers of silver in this area，

and is mainly found in the early metallogenic period ofthe

quartz—sulfide ores，and its content was slightly reduced in

the late period．It is distributed in quartz vein in a spotted

shape(Fig．5d，i)．It has a brassy yellow color and

allotriomorphic granular texture。and its grain size iS

small，feW of which are visible to naked eyes and Can

reach about 0．5 mm．It iS also found that veinlet—shaped

copper ore with intersertal texture fills in the pyrite veins

rFig．5c)．It iS closely related to silver mineralization，and

it is often found that the silver minerals wraps and

metasomatizes the chalcopyrite particles and makes the

latter show a skeletal texture．

2．7 Covelline

Less covelline develops in this area and it is mainly

found in quartz·sulfide ore．It was formed in the early

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metallogenic stage，and shows allotriomorphic granular

texture．It closely coexists with pyrite，chalcopyrite，and

sphalerite in quartz vein．Its grain size is small，generally

invisible to naked eyes．Covelline iS also one of the

important carrier minerals in this area，with silver content

reaching about 5％．Ag may show isomorphism to replace

Cu and enters the mineral crystal lattice．

2．8 Quartz

It iS a major and also the most common and most

widely distributed gangue mineral in the mining area，

mainly produced in volcanic tufr in a veinlike shape．

Besides the wider quartz vein in the main metallogenic

period，less thin vein shaped quartz developed before the

metallogenic period，and didn’t develop after the

metallogenic period．It has a milk white color，and the

major mark for the mineral formation iS that the silver

mineral and its coexisting ror associated)ore sulfide are

dis仃ibuted in the quartz vein in the metallogenic period in

a star·like shape．

2．9 Calcite

Calcite is the major gangue mineral in the late

metallogenic period and after the metallogenic period in

this mining area．During the metallogenic period，the

calcite coexisted with quartz and developed in the late

metallogenic period，and its content was less，mainly

showing allotriomorphic granular aggregation and a white—

milk white color．After the metallogenic period．1ess

calcite developed，showing fine veinlike shape．

2．10 Fluorite

Less fluorite developed in the late metallogenic period

of the deposit，and mainly has a light green color and light

purple．It shows a cryptocrystalline texture，with little

content of pyrite and silver inside．

3 Sampling and Testing

The Gaoshan gold．silver deposit iS a typical

hydrothermal deposit．and its mineralization iS primarily

related to hydrothermal quartz veins．According to the

intercalated relationship of veins，ore structure，formation，

mineral association． and mineral typomorphic

characteristics， combined with electron microprobe

analysis，the mineralization of the mining area Can be

divided into pre—metallogenic period，hydrothermal

metallogenic period and supergene period，of which the

Fig．6．Characteristics ofhydrothermal minerals ofthe Gaoshan gold—silver deposit in the metallogenic period．

(’al—Calcite；FI—Fluorite；Qz-Quanz(a)，quartz of stringer、+ein i11 the pre·metallogenic period(Qz)：(b)．calcite in the earl)metallogenic period

((a11j：(c)．calcite((’aI：)and fluorite(FI)in the late metal／ogenic period；(d)．white quartz in the carl)'stage of mctallogenic period(Qzr)and dark

quartz in the late metallogenic period(Qz2)

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hydrothermal mineralization can be divided into early

stage and late stage(Fig．61．

Pre．metallogenic period is featured by development of

metal minerals related with diagenesis，mainly rutile and

magnetite。with a small amount of thorianite．The main

metallogenic period presents the combination of galena，

sphalerite，marmatite，arsenopyrite，pyrite，stromeyerite，

argentite(acanthite)，chalcopyrite，covellite，quartz，calcite，fluorite，etc．The mineral assemblages in the early

and late metallogenic period are slightly different and the

mineralization intensity in these stages also varies．

Supergene period is featured by development of a large

number of chlorite，epidote and kaolinite。as well as local

limonite development．Division of metallogenic period

and the corresponding mineral association and

development intensity are shown in Table 1．

Gangue mineral samples used in the microthermometry

study of fluid inclusions and stable isotope test were taken

from different parts of the exlbosed mining area and

different drill cores．covering the different stages of

mineralization and ensuring that the samples are

representative．Samples used for the test of trace elements

were mainly taken from different parts of the exposed

mining area(the sample with the beginning of GS in No．)and different drill cores(the sample with the beginning of

00 1，002 and l 1 02 in No．)，which are monominerals

selected from samples that can represent the fluid

properties in the diagenetic and hydrothermal metallogenic

period．Sample details are shown in Table 2．The

microthermometry of inclusions was carried out in the fluid

inclusions laboratory of the Institute of Mineral Resources．

Chinese Academy of Geological Sciences，in which the

research method of fluid inclusions refered to Lu et a1．

r2004)．The test instrument was Linkam MD$600 Cooling-

Heating Stage，with the measuring temperature range of

-1 96 to 5500C．The measuring accuracy was土0．1oC and

士20C when the temperature was-100 to 4000C and more

than 400。C．respectively．The heating rate in the test was

0．2-5。C／min．For aqueous inclusions。the corresponding

salinitv of fluid inclusions can be found in me freezing

point．salinity table provided by Lu et a1．(20041 based on

the measured temperature of freezing point．

D and O isotope analysis was carried out at the Test and

Analysis Center of the Institute of Mineral Resources．

Chinese Academy of Geological Sciences．in which the

analysis instrument was MAT 253 EM mass spectrometer．

witll O isotope analysis precision superior to士O．2 and H

isotope analysis precision superior to士2％o．The O isotope

in quartz water was obtained by the fractionation

equations 10001naquanz．waler=3．38x100T～一3．40(Clayton

Table 1 The formation order of minerals of Gaoshan gold-silver deposit

Mi⋯als Prc-nlc{aIIogcnic叫-iod——___监业堕坚也型丝掣业唑生—一 SLl叫圳1c PcriodLarl＼sla址e Late sta2c

Rulile —Ma}znctitc-_____________

I'horianite-_____________一Quartz-___·-______________-______________Ga]cna lMarmatite-．．_____

Sphalcritc-·__l__P、r“c 一 一-_·____·___Arsenopyrite-_·-___-

Stt+Olllt2＼trite_-___-_______

At‘gcntitc_l l·l_·(1halcopvrite lCoxellite---一．．．一

(’alcitc 一 一lquorite．．．．-__．．

Epidote．．．．．．．．．．．．．．．Chlotitc．．．．．．．．．．．．．．．．．一Kaolin．__________．___

Limonite-________________

Table 2 Characteristics and parameters of fluid inclusion of Gaoshan gold-silver deposit in Longquan

Pre·metallogenic period Quartz

Early metallogenic

periodLate metallogenic

period

Late metallogenic

periodLate metallogenic

period

Quartz

Quartz

calcite

Fluorite

33

9

Gas。liquid 2—15

G譬liquid 2-20

G鼍1iqui8 2之5

G譬liquid 2-20

G冀1iquio¨o

2—20

2—20

2—15

5—25

5—40

225-305 -6．6一一l-2 2．07_9．98

192—236

202—208

173-188

156—192

-5．6一一O．3 0．53-8．68

—3．8一-0．8 1．4__6．16

-2．7一．0．2

—2．1一一0．2

0．35．4．99

O．35_3．55

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et a1．，1 9721 based on the O isotopes in the tested quartz．

Analysis oftrace and REEs was completed in the National

Geological Testing Center．in which the detection method

was based on the DZ／T0223—200 1 and the testing

instrument was plasma mass spectrometer(PE300D)，withthe detection limit of 0．05 ppm and relative standard

deviation superior to 5％．

4 Fluid Inclusion Petrography and Micro-

thermometry

4．1 Types and characteristics of the fluid inclusions

The gangue minerals in the Gaoshan gold．silver deposit

are mainly quartz，calcite，and fluorite．The microscopic

observation and microthermometry on the fluid inclusions

in gangue mineral of different mineralization stages were

performed．The fluid inclusions are mainly dis仃ibuted in

the crack．1ike，beaded，planar，isolated and other form

(Fig．7)．According to the composition and phase states at

the room temperature．inclusions can be divided into two

types：type I(pure liquid phase)and type II(gas—liquid

phase aqueous inclusions)．

Type I inclusions are composed of pure liquid at room

temperature．composition，with size ranging from 2 to 1 4

lam，in the form of oval，long column，square，etc．These

inclusions account for about 5％of the total．

Type II inclusions are composed of aqueous phase and

bubble phase at room temperature，with gas．1iquid ratio of

5 to 30％，mostly 1 0 to l 5％，which are uniformly changedto the liquid phase after heating．Such kind of inclusion

accounts for 95％of the total and appeared throughout the

metallogenic period，with size of 2 to 20 U，mostly 2 to 6

gm．Its shapes include oval，long column，square，water

droplets，irregular shape，etc．

4．2 Homogenization temperature and salinity of fluid

inclusions

Microthermometry and salinity of fluid inclusions in the

pre-metallogenic period，the early stage and late stage of

the main metallogenic period were estimated and

histogram of homogenization temperature distribution

were made(Fig．8)，with well developed host minerals

(quartz，calcite and fluorite)convenient for observation as

the research object．with the intercalated relationship

between the main gangue minerals，mineral assemblage

characteristics，ore microscopy characteristics and others

of the Gaoshan gold．silver deposit as fluid phase division

basis．The results showed that the homogenization

F嘻7．Characteristics of fluid inclusions of the Gaoshan gold—silver deposit in the metallogenic period．

(a)，quartz in the earl)metallogenic period；(b)，quartz in the late metallogenic period；(c)，fluorite in the late metallogenic period；(d)calcite in the

late metallogenic period

万方数据

20

18

16

14

80 200 220 240 260 280 300 320

Homogenization temperature(℃)

Fig．8．Histograms showing homogenization temperature and homogenization temperature。salinity of fluid inclusions in the

Gaoshan gold·silver deposit．

temperature for the quartz fluid inclusion in the pre-

metallogenic period is ranging from 225 to 3050C(with

extreme difference of 800C and mean of 2650C)and the

metallogenic salinity of 2．07 to 9．98％rwith extreme

difference of 7．92％and mean of 4．91％)：the temperature

for quartz fluid inclusion in the early metallogenic period

is ranging from 1 92 to 236。C fwith extreme difference of

44℃，peak of 210 to 2200C and mean of 2130C)and the

metallogenic salinity of 0．53 to 8．68％fwith extreme

differenee of 8．51％and mean of4．72％)；the temperature

for the quartz fluid inclusion in the late metallogenic

period is ranging fi-om 202 to 208。C fwith extreme

difference of 60 C and mean of 2050 C、and the

metallogenic salinity of 1．4 to 6．1 6％rwith extreme

difference of 4．76％and mean of 4．32％)：the temperature

for the calcite fluid inclusion in the late metallogenic

period is ranging from 1 73 to 1 880C(with extreme

differenee of 15。C and mean of 1810 C)and the

metallogenic salinity of 0．35 to 4．99％(with extreme

difference of 4．64％and mean of 2．05％)；the temperature

for the fluorite fluid inclusion in the late metallogenic

period is ranging from 1 56 to 1 920C(with extreme

difference of 360C and mean of 1 730 C、and the

metallogenic salinity of 0．35 to 3．55％(with extreme

difference of 3．2％and mean of 1．3 l％1．Generally

speaking，the homogenization temperature for the

inclusions in the 1ate metallogenic period is ranging from

1 56 to 2080C(with extreme difference of 520C．peak of

1 70 to 1 90。C and mean of l 870C1 and the metallogenic

salinitv of 0-35 to 6．16％(with extreme difference of

5．81％and mean of2．57％1．

As shown in the diagram of homogenization

temperature—salinity drawn from the comprehensive data

of fluid inclusions in different stages(Fig．8)，the fluid in

the pre．metallogenic period has a wide temperature and

saliIlity value range。while the fluid inclusions in the early

metallogenic period is characterized by small temperature

difference and the coexistance of two kinds of inclusions

with significantly different salinity．Quartz．calcite and

fluorite in the late metallogenic period are characterized

by relatively concentrated distribution of temperature and

salinity．Although there are overlaps in their cast points，

the fluid inclusions in quartz have significantly higher

temperature and salinity than that in calcite and fluorite，

and the temperature and salinity of calcite and fluorite are

close to each other．

5 Trace Elements and D-0 Isotopes

5．1 Trace element characteristics of pyrite

Pyrite is a mineral existing extensively in the Gaoshan

gold—silver deposit，generally developed in the diagenesis

and mineralization．and is all ideal object for the study of

the ore—forming fluid properties and metallogenic

environment of this deposit．

Pyrite selected in this study is from the fresh crystal-

vitric tuff(ore—hosting rock)，felsite(vein rock)，quartz-

sulphide and fluorite—sulphide veins for the testing of仃ace

elements(Table 31．The result shows that the total rare

earth ofpyrite is 207．78 in the felsite．97．01 t0 97．01 in the

crystal．vitric tuff,with an average of 128．86；62．92 to

1 35．41 in the fluorite．sulfide vein．with an average of

99．165；and 4．82 to 198．51 in the quartz．sulfide vein．with

an average of 45．86，respectively．It can be seen that the

total rare earth of pyrite significantly decreases in the

order from felsite，crystal．vitric tuff,fluorite．sulfide vein

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to quartz．sulfide vein．As to the LREE／HREE

differentiation．the LREE／HREE of pyrite is 1 2．93

in the felsite．7．0 1 to 1 0．56 in the crystal．vitric tuff,

with an average of 8．75．1．67 to 5．98 in the

fluorite．sulfide vein，with an average of 3．825，and

4．1 4 to 1 3．34 i11 the quartz．sulfide vein．with an

average of 6．70．respectively．The samples above

are characterized by enrichment of LREE，but the

LREE／HREE differentiation decreases in the order

from felsite。crystal—vitric tuff,and fluorite．sulfide

vein to quartz．sulfide vein(Fig．9)．As to the JEu，

the JEu of pyrite is 0．32 in the felsite．0．44 to 0．47

in the crystal．vitric tuff,with an average of 0．455．

0．22 t0 0．9 1 in the fluorite．sulfide vein．with an

average of 0．57．and 0．28_0．66 in the quartz．sulfide

vein，with an average of 0．52，respectively．Pvrites

from different sources show a significant negative

anomaly of Eu(Fig．9)，and a pyrite and fluorite

sample from the fluorite．sulfide vein shows no

obvious anomaly of Eu(Fig．91．As to the 8Ce．the

6Ce of pyrite is 0．95 in the felsite．0．84 to 1．12 in

the crystal—vitric tuff,with an average of 0．98，0．86

to 0．90 in the fluorite—sulfide vein．with an average

of 0．88，and 0．59 to 0．96 in the quartz．sulfide vein，

with an average of 0．78，respectively．Pyrites from

different sources show a slight negative anomaly of

Ce fFig．91．

For the pyrite in the felsite．crystal．vitric tuff,

fluorite—sulfide vein to quartz．sulfide vein，the Hf／

Sm ration is 1．02，0．52 to 1．43(with an average of

0．98)，0．02 to 0．77(with an average of 0．40)，and0．15 to 1．48(with an average of 0．46)．

respectively．The Nb／La ration is 0．23．0．14 to 0．27

(with an average of 0．2 1)，0．05 to 1．24 fwith an

average of 0．65)，and 0．4 to 7．32 fwith an average

of 1．96)，respectively．The Th／La ration is 0．28．

0．22 to 0．5 fwith an average of 0．36)．0．06 to 0．78

(with an average of 0．42)．and 0．1 6 to 0．46(withan average of 0．29)．respectively．The Y／Ho ration

is 25．51，24．85 to 32．22(with an average of28．54)，

24．08 to 56．17(with an average of40．161，and 22

to 28．8(with an average of 24．81)．respectively．The Zr／Hf ration is 3 1．38．29．47 to 34．05(with an

average of 3 1．76)，1．38 to l 9．62(with an average

of 10．51，and 13．2 to 28．38(with an average of

20．89)，respectively．Cu，Pb and Zn closely

associated with Ag mineralization also present

certain regularity in the content．Specifically．in

terms of Cu and Zn content，present the regularity

of quartz-sulfide vein>crystal—vitric tuff>felsite

≈fluorite—sulfide vein．while in terms of Pb

content，present the regularity of crystal—vitric tuff

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Fig．9．The REE patterns of pyrites of the Gaoshan gold—silver deposit(Chondrite—normalized values according to Boynton

1984)．

>quartz-sulfide vein>fluorite．sulfide vein>felsite．

5．2 D-O isotope characteristics of gangue minerals

Test results for the O isotope of 8 pieces of quartz

minerals and the D isotope of their fluid inclusions in the

Gaoshan gold—silver deposit are Iisted in Table 4．

According to the results．the 6”0 of 5 pieces of quartz

minerals in the main metallogenic period ranges from

4．5％0 to 6．7％o．while the 8D of fluid inclusions is between

一1 05％o and一69％o and the calculated d埔0wa时is between

6．01％o and 3．8l％o．The 6"O of 3 pieces of quartz

minerals in the late period of mineralization ranges from

6．1％o to 7．7％o．while the JD offluid inclusions is between

一1 08％o and一92％o，and the calculated 6埔O、vater is between

-5．6％o and一4％o．In D．0 isotopic composition diagram

(Fig．1 O)，some sample points fall in the formation water

area．other sample points faU near the atmospheric

precipitation line．and all the data points are far away from

the initial range of magmatic water．AD。ater is between

一108 and一69，while 6”O、vater iS between一6．59 and一3．39．

The data point distribution is relatively concentrated．

showing no obvious oxygen drifi．

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≥0主

鬯；9

o。。，(SMOW,‰

Fig．10．D-O isotopic diagrams ofthe ore-forming fluids ofthe

Gaoshan gold—silver deposit(base map is after Sheppard，

1986)．

6 Discussion

6．1 Fluid properties and source

As shown in the homogenization temperature．salinity

diagram of fluid inclusions(Fig．8)，the fluid in the pre·

metallogenic period has a wide temperature and salinity

value range，which may indicate that the fluid in the pre—

metallogenic period is complicated．The fluid inclusion in

quartz in the early metallogenic period is characterized by

small temperature difference and the coexisting of two

kinds of inclusions with significantly different salinitv．

which suggests that mixing action of two kinds of

inclusions with small temperature difference and

significant salinity difference exists and leads to the start

of the silver mineralization．Quartz．calcite and fluorite in

the late metallogenic period are characterized by relatively

concentrated distribution of temperature and salinity．

Although there are overlaps in their cast poillts，the fluid

inclusions in quartz have significantly higher temperature

and salinity than calcite and fluorite，and the temperature

and salinity of calcite and fluorite are close to each other．

The main cause of this phenomenon may be that quartz

often has higher crystallization temperature than calcitere

and fluorite．so it crystallized earlier and inherited the ore—

foITUing fluid properties and characteristics in the early

metallogenic period to the greatest extent，while calcitere

and fluorite crystallized later in a longer time．and the ore．

forming fluid has higher evolution degree and is even

subject to the influence of addition of external fluid．

change in physical and chemical conditions and other

factors，so they have greater differences from the fluid

characteristics in the early metallogenic period．

Temperature and salinity characteristics of fluid inclusions

indicate ore．forming fluid overall is fluid with low

temperature and low salinity．Temperature measurement

results and salinity difference at different stages indicate

mat the ore．forming fluid has experienced the evolution in

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万方数据

which temperature and salinity gradually reduce．D and O

isotope characteristics and composition diagram shows

that the ore．forming fluid may come from the mixture of

the formation water evolved from the atmospheric

precipitation driven by the magma thermal and the 1ater

atmospheric precipitation of surface infiltration．The

change in physical and chemical conditions caused by

fluid mixing may be the important mechanism for mineral

precipitation mineralization．

In a hydrothermal system，the rare earth elements

geochemistry can be used to quite effectively trace the

source of ore．forming fluids and water—rock interaction

(Henderson．1 984)．The trace element content in pyrite is

res仃icted by the trace element content in ore—formingfluids(Moh．1 980)．Rare earth elements may be included

in the pyrite inclusion．the mineralinclusion rich in trace

elements or the lattice imperfection．Despite the low

content of rare earth and trace elements in ore—forming

fluids．due to its distribution particularity and the stable

chemical property，they often play an important role in

indicating material sources and fluid evolution．The rare

earth elements of sulfide sample form the property that

can be used to trace ore．forming fluids(Zhao，1 991：Mao

el a1．，2006；Map et a1．，2009)，in order to judge the

physicochemical conditions for metallization(Sasmaz et

a1．，2005)．Despite the relative stability and source rock

gene of rare earth elements，the geological process and

physicochemical conditions of the environment have

obvious impact on them．The value state of Ce and Eu is

often the reaction of the ambient condition of ore．formingnuids and the important index that indicates the change of

oxygen fugacity of metallogenic environment(Chen，1 996)．Eu anomaly is in essence the separation of Eu from

other rare earth elements．It has two states of Eu”and

Eu”，while other rare earth elements usually have only

one state of R”．Such obviously different geochemical

behavior of Eu2+and Eu”and Rj+causes the separation of

Eu．Among which，归2(oxygen fugacity)is a significant

cause for Eu separation besides the genetic factor．When

70，is low。it is the reducing environment，and the

coordination anions are dominated by low value．state soft

base like HS。，S6，SC卜r，CN—and S20’3．At this moment，

Eu2+can form the stable coordination complex and

precipitate．since Eu3+and R”can not coordinate，they

have to be stabilized in water in ionic state．which causes

positive anomaly of Eu and low total content of rare earth

elements．Conversely，when J02 is high，there may be

negative anomaly of Eu and high total rare earth elements

in the precipitation(Chen and Deng．1 993)．The pyrite in

felsite and crystal and vitric tuff and the pyrite in ore have

an overall consistent rare earth element partition pattern in

the Gaoshan gold．silver deposit，but the former one is

richer in light rare earth elements．The similar rare earth

element partition pattem of the three indicates that there is

certain genetic relation among them．and it indicates that

the country rocks also made contributions to ore—forming

fluids．The relatively strong negative anomaly of Eu and

slight negative anomaly of Ce in pyrite in quartz—sulfide

vein and the slight negative anomaly of Eu and Ce in

pyrite in fluorite．sulfide vein indicate that me ore-formingfluids from which pyrite precipitated might be relative

oxidizing fluids．

The HF and F．rich hydrothermal fluids can form R”．F．

complexwith R3+．which keep the REE positive ions in the

fluids and show the characteristic ofrelatively low content

of total rare earth elements in precipitation(Bau and

Dulski，1995；Gramaccioli et a1．，1999；Deng et a1．，2014)．Enrichment of 1ight rare earth elements is the an important

characteristic of fluorite formed in low—PH environment

(Ehya，2012)．Besides，some scholars believe that，F-rich

hydrothermal fluids can easily be enriched with light rare

earth elements and high field strength elements，and Hf／

Sm，Nb／La and Th／La values are generally greater than 1，

while C1．rich hydrothermal fluids can easily be enriched

with light rare earth elements．and Hf／Sm．Nb／La and T11／

La values are generally smaller than 1 fOreskes and

Einaudi，1990；Keppler，1996；Bi et a1．，2004)．The Y／I-Io

ratio of hydrothermal mineral has nothing to do with the

material SOurCe but mainly depends on the material

composition and transport process of the fluids(Bau and

Dulski．1 995)．Y／Ho．Zr门Hf and Nb／7Ta values have the

ionic radius and valence similar to each other and the ratio

is relatively stable in the same hydrothermal system．

However．when there is interference in the system，for

example． when there is water—rock reaction or

metasomatism，these element pairs may have obvious

万方数据

differentiation．which is shown in the way that the ratio of

the same element pair in different samples have relatively

greater variation range(Yaxley，1998)．This is of

relatively good indicative significance for fluid property．

The rare earth element partition pattern of fluorite in the

Gaoshan deposit shows that the differentiation between

light and heavy rare earth is not obvious，indicating that

fluorite was formed in low temperature．and it was the

product evolved from ore．forming fluids to the late stage．

The H∥Sm．Nb／La and Th／La values of pyrite in the ore

are mostly smaller than 1．showing the trace element

characteristic of Cl—rich fluid as a general rule．But the

fluid in the Gaoshan deposit is suggested to be C1．rich

fluid because the geological fact that fluorite development

and chlorargyrite(AgCl)hasn’t been discovered yet in the

deposit．Furthermore，previous research results also show

that， South Zhejiang is an area of high．fluorine

background value，the high．fluorine base metamorphic

rocks and caprock volcanic rocks have a consistent

distribution density with the fluorite ore in this area．and it

is also related to the formation of deposits like precious

metals(gold and silver)，nonferrous metals(1ead and zinc)and even pyrite(Han et a1．，1988)．It happens that there is

a similar case．The independent silver deposit in Poshan of

Henan Province has also been proved to have close

genetic relation with F．rich fluids，and that silver is mainly

kept in the fluids in the form of fluoride complex fYe et

a1．，2003)．To sum up the evidences above，the author

tends to believe that the ore．forming fluids in the deposit

are mainly F．rich，but yet is open to the existence of C1．

This also reminds us that，we should not simply take the

geochemical characteristic as the only basis，and we

should give overall considerations to other evidences，

especially the geological facts．Y／Ho．Zr／Hf and Nb／Ta

ration values of pyrite in metallization epoch show little

difference in different samples，which indicates that the

hydrothermal system in the Gaoshan gold．silver deposit

was not influenced by the hydrothermal fluids in later

stage．

To sum up．the fluids in the Gaoshan gold．silver deposit

are relative oxidizing fluids of medium-low temperature，

low．salinity and F．enrichment．The ore．forming fluids are

possibly the mixture of the formation water formed by

circulating atmospheric precipitation driven by magma

and the atmospheric precipitation infiltrated in the earth’s

surface in later stage．

6．2 Metallogenie pressure and depth

Metallogenic depth is an important basis to study the

genesis of deposits and potential for exploration．Among

the geological and geochemical methods to estimate the

metallogenic depth，one of the most commonly used is to

estimate according to the

inclusion．While studying

continental volcanic rocks

proposed the empirical

trapping pressure of fluid

the gold—silver deposit in

in Zhejiang，Shao(1988)formula to calculate the

metallogenic pressure and metallogenic depth of such type

of deposits，which proved to be scientific and feasible by

mutual verification with the results calculated by other

means．The empirical formula is as follows：

％(initial temperature)=374+920×S(salinity of ore-

forming fluid)oC)

P0(initial pressure=219+2620×S(salinity of ore-

forming fluid)f 1 03Pa)

凰(initial depth)=Pox 1／300(km)

P1(metallogenic pressure)2 P0x T1(actually measured

metallogenic temperature in the deposit)／％(1 03Pa)

H1(metallogenic depth)印l x 1／300(km)

By substituting the actually measured salinity and

homogenization temperature data，the metallogenic

pressure calculated of this deposit is centralized around

118．02 to 232．13x103 Pa． corresponding to the

metallogenic depth of around 0．39 to 0．77 km．

To vein．1ike hydrothermal fluids con仃oiled by fracture、

ore．forming fluid system may be lithostatic pressure or

hydrostatic pressure．or alternate between the two．It is

generally acknowledged that，when depth<5km or at

brittle deformation belt，the fluid is hydrostatic pressure，

while depth>16km or at ductile deformation belt，the

fluid is lithostatic pressure．and when depth is around 5 to

1 6km or brittle．ductile deformation belt，the fluid shows

the alternation between lithostatic and hydrostatic pressure

(Sibson et a1．，1 988；Cox，l 995)．The calculation result of

metallogenic pressure and metallogenic depth of this

deposit indicates that this deposit was formed within the

depth range of supergene brittle deformation belt，which

conforms to the geological fact that there developed a

large number of brittle structures in the deposit(Zhang et

a1．，20 1 6)，such as conjugated shear joints，tensile fractures

andangular breccia．

6．3 Possible precipitation mechanism

The formation of continental volcanic hydrothermal

siIver deposit is generally related to the large amount of

Ag provided by volcanic magma．and most of the source

beds that form the silver deposit are obviously related to

volcanic activities．Though some source beds belong to

common sedimentary rocks．metallogenesis has indirect

relationship with volcanism．They may be sedimentary

rocks from far volcano fsuch as Jianzhupo deposit in

Guangxi province)，or be metallized by Ag brought in

from deep in the sedimentary rocks of antique volcano

(such as Qixia deposit in Jiangsu province)，and in some

deposits(superimposed type)，lnvaslve magma also

万方数据

provided appreciable quantity of Ag and other metals，

such as Xinmin and Tianpingshan deposit(Tu et a1．，

l 987)．Some experiments show that，whatever the initial

reactant is，AgCl，A92S or Ag，buffered by FeS2 or FeS，

Ag will finally generate silver—sulfur complex and be

dissolved out．When there is finely scattered FeS2 or FeS

in the source bed of silver deposit．the process above is

feasible in the nature fTu et a1．，1 987)．The test result of

electronic probe in this research shows that，there

extensively developed Ag—bearing pyrite in the

sedimentary rocks in the Gaoshan gold．silver deposit。

which provided material basis for Ag mineral mobilization

and migration．A large amount of pyrite developed in the

country rocks of the Gaoshan gold．silver deposit provided

important conditions for the precipitation and

metallization of silver-fluoride complex．

In this study，the rare earth elemem partition pattern

between the main geological body and pyrite in ore is

consistent in the Gaoshan gold—silver deposit(Fig．61．Content of Au and Ag element in flesh rocks is also quite

close(Table 5)，showing the homology and gene of

material．Meantime，Ag content of the former is around

0．7ppm．exceeding 1 0 times of the average value of

0．056ppm for the earth crust fRudllick and Gao．2003)．By

separately comparing the Au and Ag content in the

samples of sedimentary tuff(country roc蚰and granite

porphyry before and after hydrothermal alteration，Au and

Ag content in altered samples is obviously lower than that

in fresh samples(Table 5)，which indicates that there was

mobilization and migration of Au and Ag elements．The

result above further proves that the extensive volcanic

sedimentary rocks and scattered vein rocks in the deposit

are the important metal sources for silver metallization．

Besides．the extensively developed sulfide such as pyrite

can provide a large amount of S for metallization and play

a role of mineralizer．Ag elements in the Gaoshan gold—

silver deposit may be kept in the fluids mainly in the state

of silver—fluoride complex．The temperature—salinity

diagram of fluid inclusion shows that．there is sharp fall of

temperature from metallogenic period to early

metallogenic stage， showing the fluid composite

characteristic of two kinds with close temperatures and

different salinity in early metallogenic stage．From early to

late metallogenic stage．both temperature and salinity

show gradual decline．indicating that there is small amount

and low—temperature and low—salinity fluids slowing

addition．Atmospheric precipitation is the possible source

of such kind of fluids．

To sum up，the possible precipitation mechanism of the

Gaoshan gold—silver deposit is that，Ag elements are kept

in the fluids in the state of silver．fluoride complex ions

and keep extracting the metallogenic materials and

combining with large amount of S ions in country rocks in

the fluid migration and evolution process．As the fluids

keep migrating to shallow strata and mixing with the

atmospheric precipitation infiltrated from the earth’s

surface，when the physiochemical conditions such as PH，

EH，pressure，and temperature reach the appropriate

section，ore-forming fluids may unload，precipitate，and

metallize silver sulfide in favorable structures and host

space for metallization．As the ore—forming fluids keep

evolving and migrating upwards， atmospheric

precipitation keeps joining in，metallogenic temperature

and pressure keep declining，and metallogenic materials

are precipitated and depleted，and then the metallogenic

process comes to a close．

6．4 Genesis

The hVdromermaI metallization process is restricted by

various geological factors such as structure，magma，

stratum and fluids．Due to the diversity of deposit

occurrences，and in addition，the complexity of fluid

metallogenic system and the subjectivity and uncertaintyof the cognition of researchers，the classification is varied

and disputed．In specific to the above problems，Chen

(20 1 0)proposed to classify hydrothermal deposits into

magmatic hydrothermal deposits，altered hydrothermal

deposits，and supergene hydrothermal deposits，name the

hydrothermal deposits formed by geological process with

a temperature of 50 to 3000C and depth of 0 to 10 km as

supergene hydrothermal deposits．It is also suggested to

name the epigenetic low-temperature hydrothermal type

metallic deposits of gold，silver，lead-zinc，copper，and

uranium as well as some nonmetal deposits formed by the

hydrothermal process of circulating atmospheric

precipitation driven by magma as volcanic．hosted

supergene hydrothermal type deposits，namely，the

conventionally called continental volcanic and sub．

volcanic hydrothermal deposits．The composition of their

fluid inclusion iS dominated by H，O and 1acks of H70—

CO，inclusion．The mineral composition is dominated by

clay minerals or amorphous—chalcedony quartz．

Distinctive development of low—temperature minerals like

adularia，illite(or sericite)，slate calcite，and alunite is the

Table 5 Content ofAu and Ag in the main geological bodies of Gaoshan gold—silver deposit

Sample No．ZK002—010 15一GS一02 15．GS一03 ZK002—012 ZK001—07

Rock type Fresh granite porphyry Altered granite porphyry Fresh sedimentary tuff Altered sedimentary tuff Felsite

Ag(ppml 0．67 0．54 0．73 0．71 O．49

Au(ppbl 60 50 40 40 50

万方数据

most important mark to identify supergene low．

temperature hydrothermal metallogenic system from other

kinds of metallogenic systems(Chen et a1．，2007)．

The Gaoshan gold．silver deposit is positioned in the

extra—thick volcanic sedimentary strata in the Mesozoic．

Ore bodies are mainly controlled by fractures，ore types

are mainly quartz—sulfide vein type and secondly is calcite

and fluorite—sulfide vein type．Mineral association is

galena，sphalerite，chalcopyrite and the independent

mineral association of silver，moreover。there developed

low．temperature hydrothermal altered minerals 1ike

epidote，chlorite，pyrophyllite，and kaolin．The fluid

inclusion and trace element research result shows that．the

fluid inclusion of the Gaoshan gold—silver deposit is

dominated by gas—liquid phase，it is mainly H20 inclusion

and no H，O．CO，inclusion discovered．Homogenization

temperature of fluid inclusion in the metallogenic period

is ranging from 1 56 to 236。C with average of 200。C．

salinity is ranging from 0．35 to 8．68％(NaCleqv)with

average of 3．68％(NaCleqv)，showing the characteristics

of medium．10w temperature and low．salinity fluids．The

metallogenic pressure concentrate mainly on ll 8．02 to

232．13x10’Pa．corresponding to metallogenic depth of

0．39 to 0．77 km．indicating that it is a supergene deposit．

Characteristics in the deposit like high．fluorine

background value，development of fluorite，and low

amount of rare earth elements for pyrites in the

metallogenic period indicate that the fluids are rich in F．

Y／Ho．Zr／Hf and Nb／Ta values have little difference

among different hydrothermal mineral samples，

indicating that the hydrothermal fluids in the metallogenic

period was not influenced by hydrothermal fluids in 1ater

stage．Content of rare earth elemnts for Pyrites in country

rocks and veins have an overall consistent partition

paRern，showing a‘‘sea gull’’type with enrichment of

light rare earth elements and obvious Eu negative

anomaly，which indicates that the megallogenic fluids are

relative oxidizing fluids and derived partly from the

country rocks．5D of quartz fluid inclusion in the main

metallogenic period is ranging from——1 05 to——69％0 and

the di sowater value calculated is ranging from一6．01 to

一3．81％o．which is near the formation water and

atmospheric precipitation line in D-O isotopic diagram

and is far from the initial magmatic water．indicating that

the ore．forming fluid is the mixture of formation water

and atmospheric precipitation in late stage，and the final

source of formation water is mainly the circulating

atmospheric precipitation driven by magma．

Combined with the geological and geochemical

characteristics．the Gaoshan gold．silver deposit is

assigned to continental volcanic hydrothermal gold—silver

deposit type．

7 Conclusions

(1)The microthermometry and corresponding salinity

calculating results of the fluid inclusions in the Gaoshan

gold．silver deposit show that the ore．forming fluids in this

deposit are low temperature and Iow salinity．and the D

and O isotope results indicate that the source of the ore—

forming fluids may possibly be the mixture of circulating

atmospheric precipitation driven by magmatic thermal and

the atmospheric precipitation infiltrated in the earth’s

surface in the late stage．

(2)The REE partition patterns indicate that pyrites in

the ores have genetic relation with those in country rocks．

while Au and Ag elements in flesh country rocks are

significantly lower than those in hydrothermally altered

country rocks．This indicates that country rocks

con仃ibuted a lot to ore．forming fluids and materials．

(3)After mobilization，Ag elements may migrate in the

form of silver—fluoride complex in the hydrothermal fluids

dominated with circulating atmospheric precipitation

driven by magmatic thermal．They combine with the

reduced S in country rocks in the migration process．、№enmigrated close to the earth’s surface，they mixed with the

filtrated atmospheric precipitation and fmally unloaded，

precipitated and metallized under the physiochemical

conditions of low temperature．10w pressure，and relative

oxidizing，and thus form the gold—silver deposit in

favorable structures and host spaces．

(4)The metallogenic pressure in the Gaoshan gold—

silver deposit concentrates mainly on 11 8．02 to

232．13x105Pa and a corresponding metallogenic depth

ranges from 0．39 to 0．77 km．And in combination with the

geological and geochemical characteristics，this deposit is

assigned to the continental volcanic hydrothermal gold—

silver deposit type．

Acknowledgements

This paper is jointly funded by“Preliminary Study On

the Metallogenic Conditions and Prospecting Direction of

Gold-Silver Deposits，Suichang—Longquan Area，Zhejiang

(No．：YKl4011’’．“Summary and Research Project of the

Mineral Geology of China by Mineral Type(Group)(No．：121201 140396011 ”， “Research Project of the

Metallogenic Regularity of the National Important Mineral

Areas(No．： 121201 1 121037)”．and“Comprehensive

Research Project of China’s Mineral Geology and

Regional Metallogenic Regularity(China’s Mineral

Geology、(No．：121201 1220369)”．Our field study and

sampling work has received great support from leaders of

No．7 Geological Team of the Zhejiang Province and

received generous help from geological scientists and

万方数据

engineers of the deposit．Here we would like to express

our sincere thanks to them!The microthermometry

experiments of inclusions have received generous help

from researcher Li Jiankang from the Institute of Mineral

Resources，China Academy of Geological Sciences．We

would like to express our sincere thanks to him too!We

also appreciate the sincere help from Dr．Li Chap from

National Geological Experiment and Test Center with Au

and Ag element tests 1 0ur thanks also go to the reviewers

for their corrections and constructive opinions．

Manuscript received June 20，201 6

accepted July 10，2016

edited by Fei Hongcai

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201 5．Raman micro--spectroscopic study of sulfate Ion in the

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About the first author

JIANG Biao，Male；born in 1 986 in Xuancheng City．Anhui

Province；Postdoctor of Institute of Mineral Resources．

Chinese Academy of Geological Sciences；he iS now

interested in the study on metallogenic regularity of silver

deposits in China．

Email：jiangbia0334223@163．com；Phone：151 10093082．

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