青海东昆仑阿斯哈金矿矿床地质特征及成因研究
|
摘要
阿斯哈金矿位于东昆中隆起带东段，紧邻昆中岩石圈断裂，为印支早期形成的脉型金矿床。矿区内地层简单，仅出露有古元古界金水口群白沙河组。矿体受印支早期构造、岩浆活动控制。矿区内构造主要为断裂构造，近EW向断裂及不同等级的次级断裂分布全区，控制矿化形成和分布的断裂多为NNE向和NW向断裂，这两组断裂局部又是容矿构造。区内侵入岩分布广泛，主要为印支早期形成的花岗闪长岩、闪长岩岩基和岩株状产出的花岗岩。脉岩主要为云煌岩。
矿区内发现规模不等的含金蚀变破碎带（矿脉）十余条，其中以Ⅰ、Ⅱ号矿脉最为重要，其次是Ⅳ号矿脉。Ⅰ号矿脉受NNE向左旋张扭性断裂控制，Ⅱ号矿脉受NW向右旋压扭性断裂控制。矿石类型主要为石英脉型，其次为构造蚀变岩型；矿石矿物主要有黄铁矿、黄铜矿、毒砂、自然金及方铅矿、辉铅铋矿、辉铋银铅矿等铅矿物；脉石矿物主要有石英、黑云母、绢云母、绿泥石、绿帘石、长石、方解石等。具有它形粒状结构、自形—半自形粒状结晶结构、碎裂结构、交代结构等；浸染状构造、团块状构造、脉状构造和网脉状构造。与矿化关系最为密切的近矿围岩蚀变主要为硅化、绢英岩化等。成矿过程由早到晚划分为石英-黄铁矿-毒砂阶段，石英-多金属硫化物阶段，石英-碳酸盐阶段三个阶段。
作为阿斯哈金矿容矿围岩的闪长岩—花岗闪长岩和花岗岩的岩石地球化学研究分别显示出碰撞前（俯冲晚期）活动大陆边缘特征和后碰撞花岗岩特征。昆仑洋壳向北不断俯冲拼合导致底侵作用发生，使来自幔源的基性岩浆提供巨量热动力导致地壳物质熔融，在该带区域上形成了规模宏大的花岗质岩带。花岗质岩体Au含量低，不太可能为成矿提供主要矿质。云煌岩空间上与矿脉密切伴生，通过研究表明其可能来源于交代富集地幔，推测其形成的构造环境为陆内造山由挤压向伸展转换的相对松弛阶段，与矿床时间近一致，成因上联系密切。
含金石英脉中流体包裹体主要有富CO_2三相、气液两相2种类型。成矿流体具有低的盐度(1.83～8.13wt%NaCl.eqv)、低密度（0.69～0.96g/cm3）、中等温度(155.3℃～425.6℃)。流体包裹体气相成分主要有CO_2，CH_4，N_2和H_2O，属H_2O-CO_2-N_2-CH_4体系。成矿Ⅰ阶段流体为低盐度、富CO_2的高温流体。成矿Ⅱ阶段富CO_2型和气液两相流体包裹体共存，发生了以CO_2逸失为特征的不混溶或沸腾，致使残余流体盐度升高。成矿Ⅲ阶段为气液两相包裹体。
阿斯哈金矿含金石英脉δ~(18)O值为11.3‰~15.1‰， δD_(V-SMOW)值为-59.6‰~-117.7‰，δ~(18)O_(H_2O)值为2.7‰~9.2‰。氢氧同位素和流体包裹体激光拉曼光谱研究显示，阿斯哈金矿成矿流体应以含有幔源物质、富含CO_2的岩浆流体为主，在成矿晚阶段有大气水混入。矿床中黄铁矿样品δ~(34)S值的变化范围为+5.0‰～+7.4‰，平均值为+5.8‰，硫同位素特征以及煌斑岩与矿脉空间上的密切关系显示成矿物质主要来源于幔源岩浆，在上升运移的过程中萃取所流经围岩的成矿物质。
通过对阿斯哈金矿的成因研究，认为成矿作用应发生在早印支期陆内造山由挤压构造体制由向伸展作用的转换时期，成旷时期应略晚于花岗质岩浆的侵位时间。阿斯哈金矿在矿床成因上与造山型金矿具有相似的基本特征，成矿构造背景为陆内造山环境，矿床成因类型为中成造山型金矿。
Asiha gold ore deposit is located in the eastern part of middle uplifted basementand granitic belt, adjacent to the central Kunlun fault. It is a vein-type gold depositsformed in the early Indosinian. The strata outcropped in the mining area is simple, justthe Palaeoproterozoic Jinshuikou group only.The ore bodies are controlled by earlyIndosinian tectonic and magmatic activities. Fault structure is the main structure in themining area,nearly EW trending faults and different grades of secondary faultswidely distributed in the area, while the NNE and NW trending faults are the mainlyore-bearing structures.Intrusive rocks are widely distributed, mainly for the earlyIndosinian granodiorite, diorite batholith and granite stock.Vein rocks mainly forminette.
There are more than ten different scales of gold altered fracture (veins) found inthe mining area,1#vein and2#vein are the most important veins, followed by4#vein.1#vein was controlled by the NNE trending left lateral tension-torsional fault,while2#vein was controlled by the NW trending right lateral compression-torsional fault.Ore types can be classified into quartz vein type and structurally altered rocktype,maily of quartz vein type. Ore minerals are pyrite, chalcopyrite, arsenopyrite,galena, native gold, galenobismutite and gustavite, etc. Gangue minerals are quartz,sericite, plagioclase, calcite, chlorite and biotite, etc. Major ore textures are anhedralgranular texture, euhedral-subhedral granular crystal texture, cataclastic texture andmetasomatic texture,etc. Ore structures are mainly disseminated structure, massivestructure, vein structure and net-vein structure,etc. Alteration consists of sericitization, silicification, chloritization and carbonation,etc. Mineralization can be divided intoquartz pyrite arsenopyrite stage, quartz polymetallic sulfide stage and quartzcarbonate stage from early to late.
As the ore-bearing wall rocks of Asiha gold deposit, diorite-granodiorite andgranite show the characteristics of pre-collisional(late stage of subduction) activecontinental margin and post-collisional granite through the rock geochemistry studies.The northward subduction and collage effect of Kunlun oceanic crust lead to theunderplating process that makes the mafic magma from the mantle provide hugeamount of thermal dynamic and leads the crustal material to melt,then formlarge-scale granitic rock band in this area. The granitic rocks content low grade ofgold,are not likely to provide the main mineral for the mineralization. The minette isclosely associated with veins in space and it may originate from the metasomaticenriched mantle.We speculate that its tectonic setting is the relative relaxation stage ofcompression converting to extension which is after the continent-continent collisionand orogenesis.This is nearly consistent with the deposit in time and closelyassociated with its genesis.
Fluid inclusions of quartz crystals can be classified into aqueous two-phase andCO_2-rich three phase. Ore-forming fluids are characterized by low salinities,Low-densities and medium temperatures. The salinities of fluid inclusions range from1.83to8.13wt%NaCl.eqv，the densities of fluid inclusions range from0.69to0.87g/cm~3, and the homogenization temperatures of fluid inclusions range from155.3℃to425.6℃. The main gas-phase of fluid inclusions make up of CO_2，CH_4, N_2and H_2O, it belongs to the H_2O-CO_2-N_2-CH_4system. In Mineralization Stage Ⅰ, fluidinclusions characterize by low salinity, high-temperature, and CO2-rich. InMineralized stage Ⅱ, CO_2-rich fluid inclusions and gas-liquid two-phase inclusionscoexist, because of immiscibility or boiling characterized by CO_2escaping, whichleads to salinity increasing of the residual fluid. Fluid inclusions in mineralized stageⅢ are the gas-liquid two-phase inclusions.
The variation range of δ~(18)O、δD_(V-SMOW) and δ~(18)O_(H_2O)of gold-bearing quartz veinfrom Asiha gold deposit is respectively11.3‰~15.1‰,-59.6‰~-117.7‰and 2.7‰~9.2‰. Hydrogen oxygen isotopes and laster Raman spectroscopy of fluidinclusion research shows that ore-forming fluid of Asiha gold deposit is mainly frommagmatic fluid which contains mantle material and rich in CO_2, organic water such asmeteoric water interfused at late ore-forming stage.The δ~(34)S values of pyrites varybetween+5.0‰and+7.4‰, average value is+5.8‰.Both the characteristic of sulfurisotope and the close relationship which lamprophyre dykes and ore vein have inspace show that the metallogenic material is mainly from deep mantle-derivedmagma,which extract metallogenic material from stratum and rocks at the process ofrise and migration.
By the genesis study of Asiha gold deposit,the author considers that themineralization may occurs in the transition period from compression to extensiontectonic environment during the intracontinental orogenic movement in the earlyIndosinian, the mineralization phases should be a little later than the emplacementtime of granitoid magma. In the aspect of ore genesis, Asiha gold deposit’scharacteristic is similar to the orogenic gold deposits, the metallotectonic setting isintracontinental orogeny. The genetic type of ore deposit is mesozonal orogenic golddeposit.
矿区内发现规模不等的含金蚀变破碎带（矿脉）十余条，其中以Ⅰ、Ⅱ号矿脉最为重要，其次是Ⅳ号矿脉。Ⅰ号矿脉受NNE向左旋张扭性断裂控制，Ⅱ号矿脉受NW向右旋压扭性断裂控制。矿石类型主要为石英脉型，其次为构造蚀变岩型；矿石矿物主要有黄铁矿、黄铜矿、毒砂、自然金及方铅矿、辉铅铋矿、辉铋银铅矿等铅矿物；脉石矿物主要有石英、黑云母、绢云母、绿泥石、绿帘石、长石、方解石等。具有它形粒状结构、自形—半自形粒状结晶结构、碎裂结构、交代结构等；浸染状构造、团块状构造、脉状构造和网脉状构造。与矿化关系最为密切的近矿围岩蚀变主要为硅化、绢英岩化等。成矿过程由早到晚划分为石英-黄铁矿-毒砂阶段，石英-多金属硫化物阶段，石英-碳酸盐阶段三个阶段。
作为阿斯哈金矿容矿围岩的闪长岩—花岗闪长岩和花岗岩的岩石地球化学研究分别显示出碰撞前（俯冲晚期）活动大陆边缘特征和后碰撞花岗岩特征。昆仑洋壳向北不断俯冲拼合导致底侵作用发生，使来自幔源的基性岩浆提供巨量热动力导致地壳物质熔融，在该带区域上形成了规模宏大的花岗质岩带。花岗质岩体Au含量低，不太可能为成矿提供主要矿质。云煌岩空间上与矿脉密切伴生，通过研究表明其可能来源于交代富集地幔，推测其形成的构造环境为陆内造山由挤压向伸展转换的相对松弛阶段，与矿床时间近一致，成因上联系密切。
含金石英脉中流体包裹体主要有富CO_2三相、气液两相2种类型。成矿流体具有低的盐度(1.83～8.13wt%NaCl.eqv)、低密度（0.69～0.96g/cm3）、中等温度(155.3℃～425.6℃)。流体包裹体气相成分主要有CO_2，CH_4，N_2和H_2O，属H_2O-CO_2-N_2-CH_4体系。成矿Ⅰ阶段流体为低盐度、富CO_2的高温流体。成矿Ⅱ阶段富CO_2型和气液两相流体包裹体共存，发生了以CO_2逸失为特征的不混溶或沸腾，致使残余流体盐度升高。成矿Ⅲ阶段为气液两相包裹体。
阿斯哈金矿含金石英脉δ~(18)O值为11.3‰~15.1‰， δD_(V-SMOW)值为-59.6‰~-117.7‰，δ~(18)O_(H_2O)值为2.7‰~9.2‰。氢氧同位素和流体包裹体激光拉曼光谱研究显示，阿斯哈金矿成矿流体应以含有幔源物质、富含CO_2的岩浆流体为主，在成矿晚阶段有大气水混入。矿床中黄铁矿样品δ~(34)S值的变化范围为+5.0‰～+7.4‰，平均值为+5.8‰，硫同位素特征以及煌斑岩与矿脉空间上的密切关系显示成矿物质主要来源于幔源岩浆，在上升运移的过程中萃取所流经围岩的成矿物质。
通过对阿斯哈金矿的成因研究，认为成矿作用应发生在早印支期陆内造山由挤压构造体制由向伸展作用的转换时期，成旷时期应略晚于花岗质岩浆的侵位时间。阿斯哈金矿在矿床成因上与造山型金矿具有相似的基本特征，成矿构造背景为陆内造山环境，矿床成因类型为中成造山型金矿。
Asiha gold ore deposit is located in the eastern part of middle uplifted basementand granitic belt, adjacent to the central Kunlun fault. It is a vein-type gold depositsformed in the early Indosinian. The strata outcropped in the mining area is simple, justthe Palaeoproterozoic Jinshuikou group only.The ore bodies are controlled by earlyIndosinian tectonic and magmatic activities. Fault structure is the main structure in themining area,nearly EW trending faults and different grades of secondary faultswidely distributed in the area, while the NNE and NW trending faults are the mainlyore-bearing structures.Intrusive rocks are widely distributed, mainly for the earlyIndosinian granodiorite, diorite batholith and granite stock.Vein rocks mainly forminette.
There are more than ten different scales of gold altered fracture (veins) found inthe mining area,1#vein and2#vein are the most important veins, followed by4#vein.1#vein was controlled by the NNE trending left lateral tension-torsional fault,while2#vein was controlled by the NW trending right lateral compression-torsional fault.Ore types can be classified into quartz vein type and structurally altered rocktype,maily of quartz vein type. Ore minerals are pyrite, chalcopyrite, arsenopyrite,galena, native gold, galenobismutite and gustavite, etc. Gangue minerals are quartz,sericite, plagioclase, calcite, chlorite and biotite, etc. Major ore textures are anhedralgranular texture, euhedral-subhedral granular crystal texture, cataclastic texture andmetasomatic texture,etc. Ore structures are mainly disseminated structure, massivestructure, vein structure and net-vein structure,etc. Alteration consists of sericitization, silicification, chloritization and carbonation,etc. Mineralization can be divided intoquartz pyrite arsenopyrite stage, quartz polymetallic sulfide stage and quartzcarbonate stage from early to late.
As the ore-bearing wall rocks of Asiha gold deposit, diorite-granodiorite andgranite show the characteristics of pre-collisional(late stage of subduction) activecontinental margin and post-collisional granite through the rock geochemistry studies.The northward subduction and collage effect of Kunlun oceanic crust lead to theunderplating process that makes the mafic magma from the mantle provide hugeamount of thermal dynamic and leads the crustal material to melt,then formlarge-scale granitic rock band in this area. The granitic rocks content low grade ofgold,are not likely to provide the main mineral for the mineralization. The minette isclosely associated with veins in space and it may originate from the metasomaticenriched mantle.We speculate that its tectonic setting is the relative relaxation stage ofcompression converting to extension which is after the continent-continent collisionand orogenesis.This is nearly consistent with the deposit in time and closelyassociated with its genesis.
Fluid inclusions of quartz crystals can be classified into aqueous two-phase andCO_2-rich three phase. Ore-forming fluids are characterized by low salinities,Low-densities and medium temperatures. The salinities of fluid inclusions range from1.83to8.13wt%NaCl.eqv，the densities of fluid inclusions range from0.69to0.87g/cm~3, and the homogenization temperatures of fluid inclusions range from155.3℃to425.6℃. The main gas-phase of fluid inclusions make up of CO_2，CH_4, N_2and H_2O, it belongs to the H_2O-CO_2-N_2-CH_4system. In Mineralization Stage Ⅰ, fluidinclusions characterize by low salinity, high-temperature, and CO2-rich. InMineralized stage Ⅱ, CO_2-rich fluid inclusions and gas-liquid two-phase inclusionscoexist, because of immiscibility or boiling characterized by CO_2escaping, whichleads to salinity increasing of the residual fluid. Fluid inclusions in mineralized stageⅢ are the gas-liquid two-phase inclusions.
The variation range of δ~(18)O、δD_(V-SMOW) and δ~(18)O_(H_2O)of gold-bearing quartz veinfrom Asiha gold deposit is respectively11.3‰~15.1‰,-59.6‰~-117.7‰and 2.7‰~9.2‰. Hydrogen oxygen isotopes and laster Raman spectroscopy of fluidinclusion research shows that ore-forming fluid of Asiha gold deposit is mainly frommagmatic fluid which contains mantle material and rich in CO_2, organic water such asmeteoric water interfused at late ore-forming stage.The δ~(34)S values of pyrites varybetween+5.0‰and+7.4‰, average value is+5.8‰.Both the characteristic of sulfurisotope and the close relationship which lamprophyre dykes and ore vein have inspace show that the metallogenic material is mainly from deep mantle-derivedmagma,which extract metallogenic material from stratum and rocks at the process ofrise and migration.
By the genesis study of Asiha gold deposit,the author considers that themineralization may occurs in the transition period from compression to extensiontectonic environment during the intracontinental orogenic movement in the earlyIndosinian, the mineralization phases should be a little later than the emplacementtime of granitoid magma. In the aspect of ore genesis, Asiha gold deposit’scharacteristic is similar to the orogenic gold deposits, the metallotectonic setting isintracontinental orogeny. The genetic type of ore deposit is mesozonal orogenic golddeposit.
引文
[1] At herton M P，Petferd N．Cenaration of sedium-rich magmas from newly underplatedbasaltic crust[J]．Nature，1993，362：144-146．
[2] Boynton W V．Geochemistry of the rare earth elements：meteorite studies．In：HendersonP，ed．Rare Earth Element Geochemistry．New York：Elsevier Science Publishers，1984，63-114．
[3] Bozzo A T，Chen J R，Barduhn A J．The properties of hydrates of chlorine and carbondioxide[C]．DelyannisA．Delyannis E．Fourth International Symposium on Fresh Water fromthe Sea，19733：437-451．
[4] Barnicot A C，Fare R J，Groves D I，et al．Synmetamorphic lode-gold deposits in high-gradeArchean settings[J]．Geology，1991，19：921-924．
[5] Cox SF，Sun SS，Etheridge MA，et al．Structural and geochemical controls on thedevelopment of turbidite-hosted gold quartz vein deposits，Wattle Cully mine，centralVictoria，Australia[J]．Economic Geology，1995，90：1722-1746．
[6] David H G，Trevor J F，Stephen M E and Gregory M Y．Primary magmas and mantletemperatures[J].Eur. J. Mineral，2001，13：437-451．
[7] Foley S F，Jackson S E， Fryer B J，et al．Trace element partition coefficients forclinopyroxene and phlogophite in an alkaline lamprophyre from Newfoundland byLAM-ICP-MS[J]．Geochim Cosmochim Acta，1996，60(4)：629-638．
[8] Groves D I．The crustal continuum mod el for late-Archaeanlode-gold deposits of th eYilgarn Block，Western Australia[J]．Mineral Deposita，1993，28：366-374．
[9] Groves D I，Goldfarb R J，Gebre-Mariam M et al．Orogenic gold deposit s：a proposedclassification in the cont ext of their crust al distribution and relationship to other golddeposits types[J]．Ore Geology Reviews，1998，13：7-27.
[10] Goldfarb R.J，Gebre-Mariam M et al．Orogenic gold deposits：A proposed classification inthe context of their crustal distribution and relationship to other gold deposit types[J]．OreGeology Reviews，1998，13(1-5)：7-27；185-216．
[11] Goldfarb R J，Groves D I and Gardoll S．Orogenic gold and geologic time：a globalsynthesis[J]．Or e Geology Reviews，2001，18：1-75．
[12] Ionov D A，Griffin W L，O,Reilly S Y．Volatile-bearing minerals and lithophile traceelements in the upper mantle[J]．Chem Geol，1997，141(3-4)：153-184．
[13] Kerrich R，Goldfarb RJ，Groves DI，et al．The characteristics，origins and geodynamicsettings of supergiant gold metallogenic province[J]．Science in China Series D，2000，43(Suppl.)：1-68．
[14] Kerrich R and Wyman D.A.．The masothermal gold–lamprophyre association：Significanceon accretionary geodynamic setting，supercontinent cycles，and metallog-Enic processes[J]Mineralogy and Petrology，1994，51：147-172，
[15] Morrison G W． Characteristics and tectonic setting of the shoshonite rockassociation[J]．Lithos，1980，13(1)：97-108．
[16] Mernagh T P，Bastrakov E N，Zaw K，et al．Comparison of fluid inclusion data andmineralization processes for Australian orogenic gold and intrusion-related goldsystems[J]．Acta Petrologica Sinica，2007，23：21-32.
[17] Mullen E D．MnO/TiO2/P2O5：a minor element discrimination for basaltic tacks of oceanicenvironments and its implications for petrogenesis[J]．Earth Planet Sci Let，1983，62：53-62．
[18] Naden J and Shepherd TJ． Role of methane and carbon dioxide in golddepositions[J]．Nature，1989，342：793-795．
[19] McNeil A M，Kerrich R．Archean lamprophyre dykes and gold mineralization，Matheson，Ontario: the conjunction of LILE-enriched mafic magmas, deep crustal structures, and Auconcentration[J]．Can.J.Earth.Sci，1986，23：324-343．
[20] Potter R W Ⅱ，Ciynne M A．Solubility of highly soluble salts in aqueous media-part1，NaCl， KCl， CaCl2，Ca2Cl， Na2SO4and K2SO4solubilities to100℃[J]． ResearchU．S．Geol．Surv．，1978，(6)：701．
[21] Rock N M S．Lamprophyres[M]．Glasgow：Blackie，1990．
[22] Roedder E， Bodnar R J． Geologic pressure determinations from fluid inclusionstudies[J]．Annual Review of Earth and Planetary Sciences．1980，（8）：263-301．
[23] Shepherd T J，Rankin A H，Alderton D H M．A Practical Guide to Fluid InclusionStudies[M]．Glasgow Blackie＆Son Limited，1985：1-154．
[24] Sun S-s，McDonough W F．Chemical and isotopic systematics of oceanic basalts：Implications for mantle composition and processes[M]．//Saunders A D，Norry MJ．Magmatism in the Ocean Basins．Geol Soc Spee Publ42，1989：313-345．
[25] Sibson R H．Crustal stress，faulting and fluid flow．In：Parnell J，ed．Geofluids：origin，migration and evolution of fluids in sedimentary basins[J]．Geological Society SpecialPublications，1994，78：69-84．
[26] Shenberger，D．M， Barnes，H．L．Solubility of gold in aqucous sulfide solufions from150℃to350℃[J]．Geochim Cosmochim Acta，1989，53：269-278．
[27] Wyman D，Kerrich R．Alkaline magmatism.major structures, and gold deposits: implicationsfor greenstone belt gold metallogeny[J]．Eeon.Geol.，1988，83：454-461．
[28] Wood D A，Joron J L，Treuil M．A re-appraisal of the use of trace elements to classify anddiscriminate between magma series erupted in different tectonic settings[J]．Earth Planet SciLet，1979，45：326-336．
[29]程裕琪．中国区域地质概论[M]．北京：地质出版社，1994：152-159．
[30]陈衍景．造山型矿床成矿模式及找矿潜力[J]．中国地质，2006，33（5）：1181-1196．
[31]陈衍景，倪培，范宏瑞，等．不同类型金矿床的流体包裹体特征[J]．岩石学报，2007，23(9)：2085-2108．
[32]陈衍景，李晶，Franco Pirajno等．东秦岭上宫金矿流体成矿作用：矿床地质和包裹体研究[J].矿物岩石，2004，24（3）：1-12．
[33]长安大学，青海有色地勘局，青海有色地质八队．青海省都兰县沟里地区I47E003010(沟里乡)1：5万矿产地质、水系沉积物测量综合调查报告，2007（内部资料）．
[34]邓军，刘伟，孙忠实，等．慢源流体判别标志及多层循环成矿作用动力学—以山东夏甸金矿床为例[J]．中国科学(D辑)，2002，32（增刊）：96-104．
[35]邓晋福，杨建军，赵海玲等．格尔木—额济纳旗断面走廊域火成岩－构造组合与大地构造演化[J]．现代地质，1996，10（3）：330-343．
[36]丁清峰，王冠，孙丰月等．青海省曲麻莱昙丈场金矿床成矿流体包裹体研究和毒砂及文集的证据[J]．岩石学报，2010，12（26）．
[37]范宏瑞，谢奕汉，翟明国，等．豫陕小秦岭脉状金矿床三期流体运移成矿作用[J]．岩石学报，2003，19（2）：260-266．
[38]丰成友．青海东昆仑地区的复合造山过程及造山型金矿床成矿作用[D]．北京：中国地质科学院，2002．
[39]丰成友，张德全，王富春等．青海东昆仑复合造山过程及典型造山型金矿地质[J]．地球学报，2004，25（4）：415-422．
[40]胡荣国．青海省果洛龙洼金矿地质地球化学特征及矿床成因研究[D]．长沙：中南大学，2008．
[41]姜春发，杨经绥，冯秉贵等．昆仑开合构造[M]．北京：地质出版社，1992：183-271．
[42]姜春发，王宗起，李锦轶．中央造山带开合构造[M]．北京：地质出版社，2000：1-54．
[43]李廷栋，肖序常．青藏高原地体构造分析[A]．见:中国地质科学院地质研究所,编.青藏高原岩石圈结构构造和形成演化[C].北京:地质出版社,1996：6-20．
[44]李碧乐，孙丰月，王昭坤．山东招远金岭金矿埠南矿区1#脉流体特征及成矿物理化学条件研究[J]．大地构造与成矿学，2004，28（3）：314-319．
[45]李碧乐，王力，霍亮等．胶东玲珑金矿52#脉群成矿流体特征及成因[J]．自然科学进展，2009，19（1）：51-60．
[46]李碧乐，孙丰月，于晓飞等．青海东昆仑卡尔却卡地区野拉塞铜矿床成因类型及成矿机制[J]．岩石学报，2010，26（12）：3696-3708．
[47]李碧乐，孙丰月，于晓飞等．东昆中隆起带东段闪长岩U-Pb年代学和岩石地球化学研究[J]．岩石学报，2012，28（4）：1163-1172．
[48]李献华，孙贤鉥．”煌斑岩”与金矿的实际观察与理论评述[J]，地质论评，1995，41（3）：252-260
[49]刘斌，沈昆．流体包裹体热力学[M]．北京：地质出版社，1999：1-290．
[50]刘成东，莫宣学，罗照华等．东昆仑壳一役岩浆混合作用：来自锆石SHRIMP年代学的证据[J]．科学通报，2004，49(6)：596-602．
[51]罗照华，邓晋福，曹永清等．青海省东昆仑地区晚古生代-早中生代火山活动与区域构造演化[J]．现代地质，1999，13（1）：51-56．
[52]罗照华，柯珊，曹永清等．东昆仑印支晚期幔源岩浆活动[J]．地质通报，2002，21（6）：292-297．
[53]毛景文，李厚民，王义天等．地幔流体参与胶东金矿成矿作用的氢氧碳硫同位素证据[J]．地质学报，2005，79（6）：839-857．
[54]倪师军等．中基性脉岩对金矿成矿的贡献—以小秦岭金矿区为例[J]．成都理工学院学报，1994，21(3)：70-7821．
[55]潘裕生，周伟明，许荣华等．昆仑山早古生代地质特征与演化[J]．中国科学（D辑），1996，26(4)：302-307．
[56]潘桂堂，陈智梁，李振兴等．东特提斯地质构造形成演化[M]．北京：地质出版社，1997．
[57]钱壮志，冯本智．东昆仑中带金矿成矿特征及成矿模式[J]．矿床地质，2000，19(4)：315-321．
[58]青海有色地质八队．青海省都兰县阿斯哈金矿预查报告，2009（内部资料）．
[59]青海有色地质八队．青海省都兰县阿斯哈金矿普查设计，2010（内部资料）．
[60]青海有色地质八队．青海省都兰县果洛龙洼金矿普查报告，2009（内部资料）．
[61]孙丰月，金巍，李碧乐，等．关于脉状热液金矿床成矿深度的思考[J]．长春科技大学学报，2000，30(增刊)：27-30．
[62]孙丰月，石准立，冯本智．胶东金矿地质及幔源C-H-O流体分异成岩成矿[M]．长春：吉林人们出版社，1995．
[63]孙丰月，陈国华，迟效国等．新疆—青海东昆仑成矿带成矿规律和找矿方向综合研究成果报告，2003（内部资料）．
[64]王鸿祯，杨森南，刘本培．中国及邻区构造古地理和生物古地理[M]．武汉：中国地质大学出版社，1990：1-17．
[65]王枫，许文良，李军等．吉林中部烟筒山早白垩世辉长闪长岩的年代学和地球化学[J].世界地质，2009，28（4）：403-413．
[66]王凤林，肖小强，陈世顺．青海沟里地区金矿地质特征及找矿前景[J]．黄金科学技术，2011，19（4）：45-48．
[67]汪云亮，李巨初，韩文喜等．幔源岩浆岩源区成分判别原理及峨眉山玄武岩地幔源区性质[J]．地质学报，1993，67(01)：52-62．
[68]武广，孙丰月，朱群等．上黑龙江盆地金矿床地质特征及成因探讨[J]．矿床地质，2006，25（3）：215-230．
[69]吴庭祥，张绍宁，安汝龙等．青海东昆仑东段金矿区地层含矿性分析[J]．矿产与地质，2009，23（5）：431-441．
[70]许志琴，崔军文，张建新．大陆山链变形构造动力学[M]．北京：冶金工业出版社，1996，204-225．
[71]殷鸿福，张克信．东昆仑造山带的一些特点[N]．地球科学—中国地质大学学报．1997，22(4)：339-342．
[72]殷鸿福，张克信．中央造山带的演化及其特点[J]．地球科学—中国地质大学学报．1998，23(5)：438-442．
[73]赵财胜．青海东昆仑造山带金,银成矿作用[D]长春：吉林大学，2004．
[74]赵俊伟．青海东昆仑造山带造山型金矿床成矿系列研究[D]。长春：吉林大学，2008．
[75]赵振华．微量元素地球化学原理[M]．北京：科学出版社，1997：1-169．
[76]翟建平，胡凯，陆建军．有关煌斑岩与金矿化新成因模式的讨论[J]．矿床地质，1996，15（1）：80-86．
[77]朱桂田，朱世戎．煌斑岩与金矿成矿关系探讨[J]．矿产与地质，1996，10(6)：368-376.
[78]邹定喜，杨小斌，芦文泉．青海果洛龙洼金矿床同位素特征及成因[J]．黄金科学技术，2011，19(2)：26-30.
[79]张理刚．稳定同位素在地质科学中的应用[M]．西安：陕西科技出版社，1985．
[80]张德全，丰成友，李大新等．柴北缘-东昆仑地区的造山型金矿床[J]．矿床地质，2001，20（2）：137-146．
[81]张德全，党兴彦，佘宏全等．柴北缘-东昆仑地区造山型金矿床的Ar-Ar测年及其地质意义[J]．矿床地质，2005，24（2）：87-98．
[82]周军，祁世军．造山带金矿研究现状与存在的问题[J]．地球科学与环境学报，2004，26(2)：16-23．
[2] Boynton W V．Geochemistry of the rare earth elements：meteorite studies．In：HendersonP，ed．Rare Earth Element Geochemistry．New York：Elsevier Science Publishers，1984，63-114．
[3] Bozzo A T，Chen J R，Barduhn A J．The properties of hydrates of chlorine and carbondioxide[C]．DelyannisA．Delyannis E．Fourth International Symposium on Fresh Water fromthe Sea，19733：437-451．
[4] Barnicot A C，Fare R J，Groves D I，et al．Synmetamorphic lode-gold deposits in high-gradeArchean settings[J]．Geology，1991，19：921-924．
[5] Cox SF，Sun SS，Etheridge MA，et al．Structural and geochemical controls on thedevelopment of turbidite-hosted gold quartz vein deposits，Wattle Cully mine，centralVictoria，Australia[J]．Economic Geology，1995，90：1722-1746．
[6] David H G，Trevor J F，Stephen M E and Gregory M Y．Primary magmas and mantletemperatures[J].Eur. J. Mineral，2001，13：437-451．
[7] Foley S F，Jackson S E， Fryer B J，et al．Trace element partition coefficients forclinopyroxene and phlogophite in an alkaline lamprophyre from Newfoundland byLAM-ICP-MS[J]．Geochim Cosmochim Acta，1996，60(4)：629-638．
[8] Groves D I．The crustal continuum mod el for late-Archaeanlode-gold deposits of th eYilgarn Block，Western Australia[J]．Mineral Deposita，1993，28：366-374．
[9] Groves D I，Goldfarb R J，Gebre-Mariam M et al．Orogenic gold deposit s：a proposedclassification in the cont ext of their crust al distribution and relationship to other golddeposits types[J]．Ore Geology Reviews，1998，13：7-27.
[10] Goldfarb R.J，Gebre-Mariam M et al．Orogenic gold deposits：A proposed classification inthe context of their crustal distribution and relationship to other gold deposit types[J]．OreGeology Reviews，1998，13(1-5)：7-27；185-216．
[11] Goldfarb R J，Groves D I and Gardoll S．Orogenic gold and geologic time：a globalsynthesis[J]．Or e Geology Reviews，2001，18：1-75．
[12] Ionov D A，Griffin W L，O,Reilly S Y．Volatile-bearing minerals and lithophile traceelements in the upper mantle[J]．Chem Geol，1997，141(3-4)：153-184．
[13] Kerrich R，Goldfarb RJ，Groves DI，et al．The characteristics，origins and geodynamicsettings of supergiant gold metallogenic province[J]．Science in China Series D，2000，43(Suppl.)：1-68．
[14] Kerrich R and Wyman D.A.．The masothermal gold–lamprophyre association：Significanceon accretionary geodynamic setting，supercontinent cycles，and metallog-Enic processes[J]Mineralogy and Petrology，1994，51：147-172，
[15] Morrison G W． Characteristics and tectonic setting of the shoshonite rockassociation[J]．Lithos，1980，13(1)：97-108．
[16] Mernagh T P，Bastrakov E N，Zaw K，et al．Comparison of fluid inclusion data andmineralization processes for Australian orogenic gold and intrusion-related goldsystems[J]．Acta Petrologica Sinica，2007，23：21-32.
[17] Mullen E D．MnO/TiO2/P2O5：a minor element discrimination for basaltic tacks of oceanicenvironments and its implications for petrogenesis[J]．Earth Planet Sci Let，1983，62：53-62．
[18] Naden J and Shepherd TJ． Role of methane and carbon dioxide in golddepositions[J]．Nature，1989，342：793-795．
[19] McNeil A M，Kerrich R．Archean lamprophyre dykes and gold mineralization，Matheson，Ontario: the conjunction of LILE-enriched mafic magmas, deep crustal structures, and Auconcentration[J]．Can.J.Earth.Sci，1986，23：324-343．
[20] Potter R W Ⅱ，Ciynne M A．Solubility of highly soluble salts in aqueous media-part1，NaCl， KCl， CaCl2，Ca2Cl， Na2SO4and K2SO4solubilities to100℃[J]． ResearchU．S．Geol．Surv．，1978，(6)：701．
[21] Rock N M S．Lamprophyres[M]．Glasgow：Blackie，1990．
[22] Roedder E， Bodnar R J． Geologic pressure determinations from fluid inclusionstudies[J]．Annual Review of Earth and Planetary Sciences．1980，（8）：263-301．
[23] Shepherd T J，Rankin A H，Alderton D H M．A Practical Guide to Fluid InclusionStudies[M]．Glasgow Blackie＆Son Limited，1985：1-154．
[24] Sun S-s，McDonough W F．Chemical and isotopic systematics of oceanic basalts：Implications for mantle composition and processes[M]．//Saunders A D，Norry MJ．Magmatism in the Ocean Basins．Geol Soc Spee Publ42，1989：313-345．
[25] Sibson R H．Crustal stress，faulting and fluid flow．In：Parnell J，ed．Geofluids：origin，migration and evolution of fluids in sedimentary basins[J]．Geological Society SpecialPublications，1994，78：69-84．
[26] Shenberger，D．M， Barnes，H．L．Solubility of gold in aqucous sulfide solufions from150℃to350℃[J]．Geochim Cosmochim Acta，1989，53：269-278．
[27] Wyman D，Kerrich R．Alkaline magmatism.major structures, and gold deposits: implicationsfor greenstone belt gold metallogeny[J]．Eeon.Geol.，1988，83：454-461．
[28] Wood D A，Joron J L，Treuil M．A re-appraisal of the use of trace elements to classify anddiscriminate between magma series erupted in different tectonic settings[J]．Earth Planet SciLet，1979，45：326-336．
[29]程裕琪．中国区域地质概论[M]．北京：地质出版社，1994：152-159．
[30]陈衍景．造山型矿床成矿模式及找矿潜力[J]．中国地质，2006，33（5）：1181-1196．
[31]陈衍景，倪培，范宏瑞，等．不同类型金矿床的流体包裹体特征[J]．岩石学报，2007，23(9)：2085-2108．
[32]陈衍景，李晶，Franco Pirajno等．东秦岭上宫金矿流体成矿作用：矿床地质和包裹体研究[J].矿物岩石，2004，24（3）：1-12．
[33]长安大学，青海有色地勘局，青海有色地质八队．青海省都兰县沟里地区I47E003010(沟里乡)1：5万矿产地质、水系沉积物测量综合调查报告，2007（内部资料）．
[34]邓军，刘伟，孙忠实，等．慢源流体判别标志及多层循环成矿作用动力学—以山东夏甸金矿床为例[J]．中国科学(D辑)，2002，32（增刊）：96-104．
[35]邓晋福，杨建军，赵海玲等．格尔木—额济纳旗断面走廊域火成岩－构造组合与大地构造演化[J]．现代地质，1996，10（3）：330-343．
[36]丁清峰，王冠，孙丰月等．青海省曲麻莱昙丈场金矿床成矿流体包裹体研究和毒砂及文集的证据[J]．岩石学报，2010，12（26）．
[37]范宏瑞，谢奕汉，翟明国，等．豫陕小秦岭脉状金矿床三期流体运移成矿作用[J]．岩石学报，2003，19（2）：260-266．
[38]丰成友．青海东昆仑地区的复合造山过程及造山型金矿床成矿作用[D]．北京：中国地质科学院，2002．
[39]丰成友，张德全，王富春等．青海东昆仑复合造山过程及典型造山型金矿地质[J]．地球学报，2004，25（4）：415-422．
[40]胡荣国．青海省果洛龙洼金矿地质地球化学特征及矿床成因研究[D]．长沙：中南大学，2008．
[41]姜春发，杨经绥，冯秉贵等．昆仑开合构造[M]．北京：地质出版社，1992：183-271．
[42]姜春发，王宗起，李锦轶．中央造山带开合构造[M]．北京：地质出版社，2000：1-54．
[43]李廷栋，肖序常．青藏高原地体构造分析[A]．见:中国地质科学院地质研究所,编.青藏高原岩石圈结构构造和形成演化[C].北京:地质出版社,1996：6-20．
[44]李碧乐，孙丰月，王昭坤．山东招远金岭金矿埠南矿区1#脉流体特征及成矿物理化学条件研究[J]．大地构造与成矿学，2004，28（3）：314-319．
[45]李碧乐，王力，霍亮等．胶东玲珑金矿52#脉群成矿流体特征及成因[J]．自然科学进展，2009，19（1）：51-60．
[46]李碧乐，孙丰月，于晓飞等．青海东昆仑卡尔却卡地区野拉塞铜矿床成因类型及成矿机制[J]．岩石学报，2010，26（12）：3696-3708．
[47]李碧乐，孙丰月，于晓飞等．东昆中隆起带东段闪长岩U-Pb年代学和岩石地球化学研究[J]．岩石学报，2012，28（4）：1163-1172．
[48]李献华，孙贤鉥．”煌斑岩”与金矿的实际观察与理论评述[J]，地质论评，1995，41（3）：252-260
[49]刘斌，沈昆．流体包裹体热力学[M]．北京：地质出版社，1999：1-290．
[50]刘成东，莫宣学，罗照华等．东昆仑壳一役岩浆混合作用：来自锆石SHRIMP年代学的证据[J]．科学通报，2004，49(6)：596-602．
[51]罗照华，邓晋福，曹永清等．青海省东昆仑地区晚古生代-早中生代火山活动与区域构造演化[J]．现代地质，1999，13（1）：51-56．
[52]罗照华，柯珊，曹永清等．东昆仑印支晚期幔源岩浆活动[J]．地质通报，2002，21（6）：292-297．
[53]毛景文，李厚民，王义天等．地幔流体参与胶东金矿成矿作用的氢氧碳硫同位素证据[J]．地质学报，2005，79（6）：839-857．
[54]倪师军等．中基性脉岩对金矿成矿的贡献—以小秦岭金矿区为例[J]．成都理工学院学报，1994，21(3)：70-7821．
[55]潘裕生，周伟明，许荣华等．昆仑山早古生代地质特征与演化[J]．中国科学（D辑），1996，26(4)：302-307．
[56]潘桂堂，陈智梁，李振兴等．东特提斯地质构造形成演化[M]．北京：地质出版社，1997．
[57]钱壮志，冯本智．东昆仑中带金矿成矿特征及成矿模式[J]．矿床地质，2000，19(4)：315-321．
[58]青海有色地质八队．青海省都兰县阿斯哈金矿预查报告，2009（内部资料）．
[59]青海有色地质八队．青海省都兰县阿斯哈金矿普查设计，2010（内部资料）．
[60]青海有色地质八队．青海省都兰县果洛龙洼金矿普查报告，2009（内部资料）．
[61]孙丰月，金巍，李碧乐，等．关于脉状热液金矿床成矿深度的思考[J]．长春科技大学学报，2000，30(增刊)：27-30．
[62]孙丰月，石准立，冯本智．胶东金矿地质及幔源C-H-O流体分异成岩成矿[M]．长春：吉林人们出版社，1995．
[63]孙丰月，陈国华，迟效国等．新疆—青海东昆仑成矿带成矿规律和找矿方向综合研究成果报告，2003（内部资料）．
[64]王鸿祯，杨森南，刘本培．中国及邻区构造古地理和生物古地理[M]．武汉：中国地质大学出版社，1990：1-17．
[65]王枫，许文良，李军等．吉林中部烟筒山早白垩世辉长闪长岩的年代学和地球化学[J].世界地质，2009，28（4）：403-413．
[66]王凤林，肖小强，陈世顺．青海沟里地区金矿地质特征及找矿前景[J]．黄金科学技术，2011，19（4）：45-48．
[67]汪云亮，李巨初，韩文喜等．幔源岩浆岩源区成分判别原理及峨眉山玄武岩地幔源区性质[J]．地质学报，1993，67(01)：52-62．
[68]武广，孙丰月，朱群等．上黑龙江盆地金矿床地质特征及成因探讨[J]．矿床地质，2006，25（3）：215-230．
[69]吴庭祥，张绍宁，安汝龙等．青海东昆仑东段金矿区地层含矿性分析[J]．矿产与地质，2009，23（5）：431-441．
[70]许志琴，崔军文，张建新．大陆山链变形构造动力学[M]．北京：冶金工业出版社，1996，204-225．
[71]殷鸿福，张克信．东昆仑造山带的一些特点[N]．地球科学—中国地质大学学报．1997，22(4)：339-342．
[72]殷鸿福，张克信．中央造山带的演化及其特点[J]．地球科学—中国地质大学学报．1998，23(5)：438-442．
[73]赵财胜．青海东昆仑造山带金,银成矿作用[D]长春：吉林大学，2004．
[74]赵俊伟．青海东昆仑造山带造山型金矿床成矿系列研究[D]。长春：吉林大学，2008．
[75]赵振华．微量元素地球化学原理[M]．北京：科学出版社，1997：1-169．
[76]翟建平，胡凯，陆建军．有关煌斑岩与金矿化新成因模式的讨论[J]．矿床地质，1996，15（1）：80-86．
[77]朱桂田，朱世戎．煌斑岩与金矿成矿关系探讨[J]．矿产与地质，1996，10(6)：368-376.
[78]邹定喜，杨小斌，芦文泉．青海果洛龙洼金矿床同位素特征及成因[J]．黄金科学技术，2011，19(2)：26-30.
[79]张理刚．稳定同位素在地质科学中的应用[M]．西安：陕西科技出版社，1985．
[80]张德全，丰成友，李大新等．柴北缘-东昆仑地区的造山型金矿床[J]．矿床地质，2001，20（2）：137-146．
[81]张德全，党兴彦，佘宏全等．柴北缘-东昆仑地区造山型金矿床的Ar-Ar测年及其地质意义[J]．矿床地质，2005，24（2）：87-98．
[82]周军，祁世军．造山带金矿研究现状与存在的问题[J]．地球科学与环境学报，2004，26(2)：16-23．