西藏甲玛铜多金属矿床成因模式
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摘要
西藏甲玛铜多金属矿位于全球第二大斑岩成矿域-特提斯-喜马拉雅巨型斑岩成矿域冈底斯成矿带中东段，属于与中新世中酸性浅成岩浆建造有关的铜、钼、铅锌、钨、金、银矿床成矿亚系列，是“后碰撞”构造环境中斑岩铜多金属矿的典型代表。论文以矿床地质为基础，总结了矿床岩浆岩的分布及气液蚀变-矿化特征，结合岩石/矿物地球化学、包裹体、同位素组成及年代学资料，讨论了矿床岩浆岩的起源、演化、流体出溶和矿质来源及富集机制，气-液蚀变的来源、演化及矿质沉淀机制，建立了初步的矿床成因模式。主要有以下几点认识：
1、以精细地质调查为基础，通过室内镜下鉴定、常量元素、微量元素、稀土元素和同位素的综合分析研究，揭示了甲玛矿区中新世的浅成侵入岩主要为云斜煌斑岩、闪斜煌斑岩、闪长玢岩、二长花岗斑岩、花岗闪长斑岩和花岗斑岩，表现花岗斑岩→闪长玢岩→云斜煌斑岩→二长花岗斑岩→闪斜煌斑岩→花岗闪长斑岩→闪斜煌斑岩的侵位序列。其中云斜煌斑岩和闪斜煌斑岩为同源岩浆，分属于钙碱性煌斑岩的钾质系列和钠质系列，源区为受俯冲板片释放的流(熔)体交代的地幔楔；闪长玢岩为I型高钾钙碱性系列，显示埃达克岩的地球化学亲和性，源区为新生下地壳；花岗斑岩属于S型钾玄岩系列，为后碰撞强过铝质花岗岩类，源区为中下地壳的变质杂砂岩；二长花岗斑岩和花岗闪长斑岩为I型高钾钙碱性系列，是上述三种岩浆熔体不同比例岩浆混合的产物。
2、通过精细的野外地质填图、钻孔编录和岩矿鉴定，确定了矿床的蚀变类型和蚀变分带及与矿化的关系。甲玛矿床的斑岩矿化体系发育钠硅酸盐化(电气石)、钾硅酸盐化、矽卡岩化、石英-绢云母化、青磐岩化和泥化，并叠加不同类型的铁矿化。矿床浅成低温热液体系主要发育石英-碳酸盐化、泥化、玉髓化、萤石化和锰化。不同蚀变类型的矿化特征不同，钠硅酸盐化(电气石)与岩体内部的黄铜矿-辉钼矿矿化囊和岩体顶部隐爆状的黄铜矿-辉钼矿矿化有关；以石英+黑云母为主的钾硅酸盐化与黄铜矿矿化有关；以硅灰石为主的晚期矽卡岩化与斑铜矿矿化有关；石英-绢云母化与辉钼矿、黄铜矿矿化关；青磐岩化与黄铜矿矿化有关；浅成低温热液矿化与Cu、Au、Pb-Zn的二次矿化有关。
3、通过流体包裹体、H-O同位素和稀有气体同位素研究，确定了矿床钠硅酸盐化、钾硅酸盐化、矽卡岩化、石英-绢云母化、青磐岩化和浅成低温热液矿化6个蚀变阶段的流体包裹体特征及成矿流体来源。流体包裹体类型包括富气相包裹体、富液相包裹体和含子晶多相包裹体。钠硅酸盐化的均一温度为437～650℃，盐度为2～46.2%NaCl；钾硅酸盐化的均一温度为315～457℃，盐度为1.0～47.1%NaCl；矽卡岩化的均一温度为220～413℃，盐度为2.7～47.3%NaCl；石英-绢云母化的均一温度为230～378℃，盐度为4.1～43.8%NaCl；青磐岩化的均一温度为80～410℃，盐度为1.7～5.7%NaCl；浅成低温热液阶段的均一温度为170～253℃，盐度为2.8～5.5%NaCl；各蚀变阶段流体包裹体离子成分主为K~++Na~++Ca~+，气相成分为H_2O-CO_2-CH_4-N_2型。岩浆热液过渡阶段的成矿元素Cu、Au、Zn-Pb均在气相流体包裹体的中富集，液相中的金属元素浓度较低。值得注意的是，钠硅酸盐化阶段的I-2型流体包裹体可能是捕获的超临界流体，温度为625℃，盐度为9.8%NaCl。成矿流体主要来自地壳深部的岩浆，在演化过程中不断有沉积或大气降水的混入；
4、总结了矿区斑岩成因模式和蚀变-矿化成因模式。18Ma之前，印度大陆板片断离诱发软流圈上涌，导致岩石圈对流减薄、拆沉，岩石圈各不同源区的部分熔融，形成含Cu-Mo、富水和碱、高fO_2的玄武质熔体、含Cu-Mo-Au-Pb-Zn、富水和碱、高fO_2的闪长质熔体和花岗质熔体，18～14Ma，在区域应力挤压-伸展构造转换过程中，三种类型的熔体沿近东西向和近南北向的走滑断裂运移、侵位过程中发生岩浆混合作用，形成二长花岗斑岩和花岗闪长斑岩。随着不混溶阶段形成的超临界流体在深部岩浆房内发生相分离，形成低密度的气相和高盐度的流体相。低密度气相在岩体上部，形成弥散性的含Cu-Au的钠-钾硅酸盐化，高盐度的流体相是最早的成矿流体，以富钠为特征，是引起钠硅酸盐化的流体。Na、K分馏导致了钾硅酸盐化流体的形成，在钾硅酸盐化晚阶段，随着磁铁矿、石膏的大规模晶出导致还原硫释放，形成以石英+黑云母为主的钾硅酸盐化，并伴生黄铜矿；同时，成矿流体与大理岩、角岩发生矽卡岩化，形成石榴子石和硅灰石等，Ca离子的活化导致流体还原硫释放度的相对减弱，形成斑铜矿化；之后，随着流体压力由静岩压力转向静水压力，大气降水的混入导致流体K+/H+比值的减小，逐渐形成石英-绢云母化，并伴生辉钼矿、黄铜矿矿化；晚期，在地热系统的热对流作用下，长石分解蚀变后的元素重新组合，生成低温蚀变矿物，包括玉髓、方解石、萤石和软锰矿等，并伴生Cu、Au、Pb-Zn；最后，青藏高原的隆升和剥蚀，原生矿体抬升至地表，在表生氧化作用和次生富集作用下，Cu、Au再次富集，形成辉铜矿+褐铁矿+赤铁矿+硅孔雀石+铜蓝+金矿化。
Jiama polymetallic copper deposit locates in the middle-east of the Gangdesemetallogenetic belt which belong to the world’s second lagest porphyry metallogenicdomain-Tethys-Himalayan giant prophyry metallogenic domain. It’s a typicalrepresentative of porphyry copper polymetallic ore in “post collision” tectonicenvironment and an important part of the Miocene intermediate-acid hypabyssalmagmatic formation related to submetallogenic series of copper, molybdenum, leadand zinc, wolfram,gold and silver diposits. Based on the geology, geochemistry,fluid/melt inclusions, isotopic composition and chronology, we disscussed the originand evolution of magmatic rocks, fluid exsolution,origin and enrichment mechanismof the mineral source, origin and evolution of gas-liquid alteration and the mechanismof mineral precipitation, established a preliminary complete ore deposit genetic mode,Mainly the following understandings:
1、Detailed field geological investigation, geochemistry, isotopic compositionsand the chronology make clear that the hypabyssal intrusive rocks in Jiama depositincluding minettes, spessarite, diorite porphyrite, monzo-granite porphyry, grano-diorite porphyry and granitic porphyry.Their emplacement age between17Ma-13.2Ma and their evolution sequence express granite porphyry->diorite porphyrite->minettes->monzogranite porphyry->spessartite->granite diorite porphyry->spessartite.The minettes and spessartite which belong to potassic calc-alkaline and sodiumcalcium alkaline lamprophyres severally are isogenesis and origin from meta-somatized mantle wedge by the flow (molten) from subducting slab;The dioriteporphyrite are metaluminous high-K calc-alkali rocks with the characteristics ofI-type granites and adakites origin from the new lower crust;The granite porphyry arealuminum shoshonite, and with the characteristics of the S-type granites origin frommetamorphic sandstone in lower crust;The monzogranite porphyry and the granitediorite porphyry are I-type high-K calc-alkali rocks, both are the mixing result of thethree magmatic melt.
2、Determine the alteration types, alteration zoning and their relationship to themin-eralization. Porphyry mineralization system in Jiama deposit develop sodium silication (tourmaline), potassium silication, skarnization, sericitization, propylitiz-ation and argillization, and superposed different types of iron ore. Epithermal systemin Jiama deposit develop quartz-carbonatization, argillization, chalcedonization,fluorite-zation and manganesation. Sodium silication (tourmaline) are related to thechalco-pyrite-molybdenite mineralization capsule in the interior pluton and cryptoexplosive chalcopyrite-molybdenite mineralization in the top of pluton. The mainlyquartz-biotite potassium silicattion are related to chalcopyrite mineralization. Theskarni-zation and potassium silication which developed simultaneously are related tocopper mineralization; Sericitization are related to chalcopyrite and molybdeniteminerali–zation. Propylitization are related to copyrite mineralization. Epithermalminerali-zation related to Cu,Au,Pb-Zn mineralization.
3、Ascertain the characters of the fluid/melt inclusions and the source of the fluidby the H-O and inert gases isotopes. The fluid inclusions in the Jiama deposits aremainly gas phase rich inclusions, liquid phase rich inclusions and daughter crystalscontaining multiphase inclusions. The homogenization temperature of the the silicatephase fluid inclusions change in437～650℃,salinity changes in2～46.2%NaCl;Thehomogeniz ation temperature of potassium silicate phase fluid inclusions changes in315～457℃, salinity changes in1.0～47.1%NaCl;The homogenization temperatureof the skarn stage fluid inclusions changes in220～413℃, salinity changes in2.7～47.3%NaCl;The homogenization temperature of phyllic stage fluid inclusionschanges in230～378℃, salinity changes in the4.1～43.8%NaCl;Thehomogenization temperature propylitic rock stage fluid inclusions changesin380～410℃and salinity changes in the1.7～5.7%NaCl;The homogenization temperatureof shallow epithermal stage fluid inclusions changes in170～253℃, salinity changesin2.8～5.5%NaCl;Each alteration phase ion composition of fluid inclusions LordK++Na++Ca+,the gas phase composition is H2O-CO_2-CH_4-N_2type. Fe, Cu, Zn, Pb andAu in magmatic hydrothermal transition stages are all enriched in the vapor phase ofthe fluid inclusions, but the metal element concentration in the liquid phase isrelatively lower,suggesting a strong gas-liquid fractionation of metallogenicmaterials.Noting that the I-2type fluid inclusions in sodium silicate salinization stagemay be supercritical fluid captured with temperature of625℃and9.8%NaClsalinity.The alteration and mineralization fulids mainly come from deep crust andmixed some deposition or precipitation fulid.
4、Summarize the porphyry genetic model and alteration genetic model of theJiama deposit.18Ma before, the upwelled asthenosphere leaded to convection anddelamin-ation of the thinned lithosphere,.cause partial melting of the different sourcearea of the lithosphere, foming basaltic melts containing Cu-Mo, water and alkali richand high fO_2, granodioritic and granitic melt containing Cu-Mo-Au-Pb-Zn,water andalkali rich and high fO_2.During18～14Ma, In the extrusion and extension structureconversion process, the three types of melt migrated and emplaced along the EW andNS-trending strike-slip fracture fromed lamprophyre、diorite porphyrite and graniteporphyry respectively, the monzogranite porphyry and the granite diorite porphyry arethe mixing result of the three magmatic melt. The supercritical fluid formed inimmiscible phase and separate into low-density gas and high salinity fluid during the magmatic hydrothermal transitional stage. Low-density gas formed the earliestscattered Na-K silication alteration with Cu-Au mineralization and later fromed theepidotization by addition of the meteoric water. High salinity fluid caused sodiumalteration is the earlier ore-forming fluid. The potassium alteration fluid origin fromthe fractionation of the sodium and potassic of the high salinity fluid, in the later, thesulfur fugacity of the potassic fluid reduced with the magnetite and gypsum crystaledcaused quartz+biotite potassium silication associated chalcopyrite; Meanwhile, theskarnizationwhich origined from the fulid interacted with hornfels and marble caucedthe activation of the Ca2+and induced content of the sulfur,mainly fromed thebornite.After then, the fluid pressure turn lithostatic pressure to hydrostatic pressure,the increasion of atmospheric precipitation decreased the H+/K+ratio, and formedsericitization associated molybdenum and chalcopyrite mineralization. In the heatconvection of the geothermal system, the mineral (Cu, Au, Pb-Zn) recombinated andformed a series of low temperature alteration, including chalcedony, calcite, fluoriteand pyrolusite, etc. Finaly, owing to the uplift and denudation of the Tibet plateau, theprimary ore upraise to the surface, Cu and Au enrichment again under supergeneoxidation and secondary enrichment, formed chalcocite+limonite+hematite+chryso-colla+covellite+gold mineralization.
1、以精细地质调查为基础，通过室内镜下鉴定、常量元素、微量元素、稀土元素和同位素的综合分析研究，揭示了甲玛矿区中新世的浅成侵入岩主要为云斜煌斑岩、闪斜煌斑岩、闪长玢岩、二长花岗斑岩、花岗闪长斑岩和花岗斑岩，表现花岗斑岩→闪长玢岩→云斜煌斑岩→二长花岗斑岩→闪斜煌斑岩→花岗闪长斑岩→闪斜煌斑岩的侵位序列。其中云斜煌斑岩和闪斜煌斑岩为同源岩浆，分属于钙碱性煌斑岩的钾质系列和钠质系列，源区为受俯冲板片释放的流(熔)体交代的地幔楔；闪长玢岩为I型高钾钙碱性系列，显示埃达克岩的地球化学亲和性，源区为新生下地壳；花岗斑岩属于S型钾玄岩系列，为后碰撞强过铝质花岗岩类，源区为中下地壳的变质杂砂岩；二长花岗斑岩和花岗闪长斑岩为I型高钾钙碱性系列，是上述三种岩浆熔体不同比例岩浆混合的产物。
2、通过精细的野外地质填图、钻孔编录和岩矿鉴定，确定了矿床的蚀变类型和蚀变分带及与矿化的关系。甲玛矿床的斑岩矿化体系发育钠硅酸盐化(电气石)、钾硅酸盐化、矽卡岩化、石英-绢云母化、青磐岩化和泥化，并叠加不同类型的铁矿化。矿床浅成低温热液体系主要发育石英-碳酸盐化、泥化、玉髓化、萤石化和锰化。不同蚀变类型的矿化特征不同，钠硅酸盐化(电气石)与岩体内部的黄铜矿-辉钼矿矿化囊和岩体顶部隐爆状的黄铜矿-辉钼矿矿化有关；以石英+黑云母为主的钾硅酸盐化与黄铜矿矿化有关；以硅灰石为主的晚期矽卡岩化与斑铜矿矿化有关；石英-绢云母化与辉钼矿、黄铜矿矿化关；青磐岩化与黄铜矿矿化有关；浅成低温热液矿化与Cu、Au、Pb-Zn的二次矿化有关。
3、通过流体包裹体、H-O同位素和稀有气体同位素研究，确定了矿床钠硅酸盐化、钾硅酸盐化、矽卡岩化、石英-绢云母化、青磐岩化和浅成低温热液矿化6个蚀变阶段的流体包裹体特征及成矿流体来源。流体包裹体类型包括富气相包裹体、富液相包裹体和含子晶多相包裹体。钠硅酸盐化的均一温度为437～650℃，盐度为2～46.2%NaCl；钾硅酸盐化的均一温度为315～457℃，盐度为1.0～47.1%NaCl；矽卡岩化的均一温度为220～413℃，盐度为2.7～47.3%NaCl；石英-绢云母化的均一温度为230～378℃，盐度为4.1～43.8%NaCl；青磐岩化的均一温度为80～410℃，盐度为1.7～5.7%NaCl；浅成低温热液阶段的均一温度为170～253℃，盐度为2.8～5.5%NaCl；各蚀变阶段流体包裹体离子成分主为K~++Na~++Ca~+，气相成分为H_2O-CO_2-CH_4-N_2型。岩浆热液过渡阶段的成矿元素Cu、Au、Zn-Pb均在气相流体包裹体的中富集，液相中的金属元素浓度较低。值得注意的是，钠硅酸盐化阶段的I-2型流体包裹体可能是捕获的超临界流体，温度为625℃，盐度为9.8%NaCl。成矿流体主要来自地壳深部的岩浆，在演化过程中不断有沉积或大气降水的混入；
4、总结了矿区斑岩成因模式和蚀变-矿化成因模式。18Ma之前，印度大陆板片断离诱发软流圈上涌，导致岩石圈对流减薄、拆沉，岩石圈各不同源区的部分熔融，形成含Cu-Mo、富水和碱、高fO_2的玄武质熔体、含Cu-Mo-Au-Pb-Zn、富水和碱、高fO_2的闪长质熔体和花岗质熔体，18～14Ma，在区域应力挤压-伸展构造转换过程中，三种类型的熔体沿近东西向和近南北向的走滑断裂运移、侵位过程中发生岩浆混合作用，形成二长花岗斑岩和花岗闪长斑岩。随着不混溶阶段形成的超临界流体在深部岩浆房内发生相分离，形成低密度的气相和高盐度的流体相。低密度气相在岩体上部，形成弥散性的含Cu-Au的钠-钾硅酸盐化，高盐度的流体相是最早的成矿流体，以富钠为特征，是引起钠硅酸盐化的流体。Na、K分馏导致了钾硅酸盐化流体的形成，在钾硅酸盐化晚阶段，随着磁铁矿、石膏的大规模晶出导致还原硫释放，形成以石英+黑云母为主的钾硅酸盐化，并伴生黄铜矿；同时，成矿流体与大理岩、角岩发生矽卡岩化，形成石榴子石和硅灰石等，Ca离子的活化导致流体还原硫释放度的相对减弱，形成斑铜矿化；之后，随着流体压力由静岩压力转向静水压力，大气降水的混入导致流体K+/H+比值的减小，逐渐形成石英-绢云母化，并伴生辉钼矿、黄铜矿矿化；晚期，在地热系统的热对流作用下，长石分解蚀变后的元素重新组合，生成低温蚀变矿物，包括玉髓、方解石、萤石和软锰矿等，并伴生Cu、Au、Pb-Zn；最后，青藏高原的隆升和剥蚀，原生矿体抬升至地表，在表生氧化作用和次生富集作用下，Cu、Au再次富集，形成辉铜矿+褐铁矿+赤铁矿+硅孔雀石+铜蓝+金矿化。
Jiama polymetallic copper deposit locates in the middle-east of the Gangdesemetallogenetic belt which belong to the world’s second lagest porphyry metallogenicdomain-Tethys-Himalayan giant prophyry metallogenic domain. It’s a typicalrepresentative of porphyry copper polymetallic ore in “post collision” tectonicenvironment and an important part of the Miocene intermediate-acid hypabyssalmagmatic formation related to submetallogenic series of copper, molybdenum, leadand zinc, wolfram,gold and silver diposits. Based on the geology, geochemistry,fluid/melt inclusions, isotopic composition and chronology, we disscussed the originand evolution of magmatic rocks, fluid exsolution,origin and enrichment mechanismof the mineral source, origin and evolution of gas-liquid alteration and the mechanismof mineral precipitation, established a preliminary complete ore deposit genetic mode,Mainly the following understandings:
1、Detailed field geological investigation, geochemistry, isotopic compositionsand the chronology make clear that the hypabyssal intrusive rocks in Jiama depositincluding minettes, spessarite, diorite porphyrite, monzo-granite porphyry, grano-diorite porphyry and granitic porphyry.Their emplacement age between17Ma-13.2Ma and their evolution sequence express granite porphyry->diorite porphyrite->minettes->monzogranite porphyry->spessartite->granite diorite porphyry->spessartite.The minettes and spessartite which belong to potassic calc-alkaline and sodiumcalcium alkaline lamprophyres severally are isogenesis and origin from meta-somatized mantle wedge by the flow (molten) from subducting slab;The dioriteporphyrite are metaluminous high-K calc-alkali rocks with the characteristics ofI-type granites and adakites origin from the new lower crust;The granite porphyry arealuminum shoshonite, and with the characteristics of the S-type granites origin frommetamorphic sandstone in lower crust;The monzogranite porphyry and the granitediorite porphyry are I-type high-K calc-alkali rocks, both are the mixing result of thethree magmatic melt.
2、Determine the alteration types, alteration zoning and their relationship to themin-eralization. Porphyry mineralization system in Jiama deposit develop sodium silication (tourmaline), potassium silication, skarnization, sericitization, propylitiz-ation and argillization, and superposed different types of iron ore. Epithermal systemin Jiama deposit develop quartz-carbonatization, argillization, chalcedonization,fluorite-zation and manganesation. Sodium silication (tourmaline) are related to thechalco-pyrite-molybdenite mineralization capsule in the interior pluton and cryptoexplosive chalcopyrite-molybdenite mineralization in the top of pluton. The mainlyquartz-biotite potassium silicattion are related to chalcopyrite mineralization. Theskarni-zation and potassium silication which developed simultaneously are related tocopper mineralization; Sericitization are related to chalcopyrite and molybdeniteminerali–zation. Propylitization are related to copyrite mineralization. Epithermalminerali-zation related to Cu,Au,Pb-Zn mineralization.
3、Ascertain the characters of the fluid/melt inclusions and the source of the fluidby the H-O and inert gases isotopes. The fluid inclusions in the Jiama deposits aremainly gas phase rich inclusions, liquid phase rich inclusions and daughter crystalscontaining multiphase inclusions. The homogenization temperature of the the silicatephase fluid inclusions change in437～650℃,salinity changes in2～46.2%NaCl;Thehomogeniz ation temperature of potassium silicate phase fluid inclusions changes in315～457℃, salinity changes in1.0～47.1%NaCl;The homogenization temperatureof the skarn stage fluid inclusions changes in220～413℃, salinity changes in2.7～47.3%NaCl;The homogenization temperature of phyllic stage fluid inclusionschanges in230～378℃, salinity changes in the4.1～43.8%NaCl;Thehomogenization temperature propylitic rock stage fluid inclusions changesin380～410℃and salinity changes in the1.7～5.7%NaCl;The homogenization temperatureof shallow epithermal stage fluid inclusions changes in170～253℃, salinity changesin2.8～5.5%NaCl;Each alteration phase ion composition of fluid inclusions LordK++Na++Ca+,the gas phase composition is H2O-CO_2-CH_4-N_2type. Fe, Cu, Zn, Pb andAu in magmatic hydrothermal transition stages are all enriched in the vapor phase ofthe fluid inclusions, but the metal element concentration in the liquid phase isrelatively lower,suggesting a strong gas-liquid fractionation of metallogenicmaterials.Noting that the I-2type fluid inclusions in sodium silicate salinization stagemay be supercritical fluid captured with temperature of625℃and9.8%NaClsalinity.The alteration and mineralization fulids mainly come from deep crust andmixed some deposition or precipitation fulid.
4、Summarize the porphyry genetic model and alteration genetic model of theJiama deposit.18Ma before, the upwelled asthenosphere leaded to convection anddelamin-ation of the thinned lithosphere,.cause partial melting of the different sourcearea of the lithosphere, foming basaltic melts containing Cu-Mo, water and alkali richand high fO_2, granodioritic and granitic melt containing Cu-Mo-Au-Pb-Zn,water andalkali rich and high fO_2.During18～14Ma, In the extrusion and extension structureconversion process, the three types of melt migrated and emplaced along the EW andNS-trending strike-slip fracture fromed lamprophyre、diorite porphyrite and graniteporphyry respectively, the monzogranite porphyry and the granite diorite porphyry arethe mixing result of the three magmatic melt. The supercritical fluid formed inimmiscible phase and separate into low-density gas and high salinity fluid during the magmatic hydrothermal transitional stage. Low-density gas formed the earliestscattered Na-K silication alteration with Cu-Au mineralization and later fromed theepidotization by addition of the meteoric water. High salinity fluid caused sodiumalteration is the earlier ore-forming fluid. The potassium alteration fluid origin fromthe fractionation of the sodium and potassic of the high salinity fluid, in the later, thesulfur fugacity of the potassic fluid reduced with the magnetite and gypsum crystaledcaused quartz+biotite potassium silication associated chalcopyrite; Meanwhile, theskarnizationwhich origined from the fulid interacted with hornfels and marble caucedthe activation of the Ca2+and induced content of the sulfur,mainly fromed thebornite.After then, the fluid pressure turn lithostatic pressure to hydrostatic pressure,the increasion of atmospheric precipitation decreased the H+/K+ratio, and formedsericitization associated molybdenum and chalcopyrite mineralization. In the heatconvection of the geothermal system, the mineral (Cu, Au, Pb-Zn) recombinated andformed a series of low temperature alteration, including chalcedony, calcite, fluoriteand pyrolusite, etc. Finaly, owing to the uplift and denudation of the Tibet plateau, theprimary ore upraise to the surface, Cu and Au enrichment again under supergeneoxidation and secondary enrichment, formed chalcocite+limonite+hematite+chryso-colla+covellite+gold mineralization.
引文
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