赣北大湖塘地区昆山钨-钼-铜矿床流体包裹体研究和稳定同位素特征
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摘要
昆山矿床位于大湖塘钨多金属矿田的南部,产出石英细脉带型W-Mo-Cu矿体。该矿床的成矿过程可以划分为黑钨矿-石英阶段(Ⅰ)、辉钼矿-石英阶段(Ⅱ)、黄铜矿-石英阶段(Ⅲ)及石英-方解石阶段(Ⅳ)。本文通过流体包裹体岩相学、显微测温、激光拉曼光谱和稳定同位素研究,探讨了昆山矿床的成因机制。研究结果表明,昆山矿床发育纯气相型(PG)、纯液相型(PL)、富液两相水溶液型(WL)三类包裹体。Ⅰ阶段主要发育WL型流体包裹体,并有少量PG型包裹体,均一温度为236～388℃,盐度为0. 5%～13. 8%NaCleqv,密度为0. 54～0. 90g/cm~3;Ⅱ阶段亦主要发育WL型和少量PG型包裹体,其均一温度为221～390℃,盐度为0. 5%～12. 7%Na Cleqv,密度为0. 51～0. 93g/cm~3;Ⅲ阶段主要发育WL型包裹体,均一温度为228～376℃,盐度为0. 7%～11. 2%NaCleqv,密度为0. 57～0. 91g/cm~3;Ⅳ阶段主要发育WL型包裹体,并有少量的PL型包裹体,其均一温度为173～288℃,盐度为0. 4%～11. 8%NaCleqv,密度为0. 76～0. 97g/cm~3。主成矿阶段流体属于中高温、中低盐度、中等密度流体,成矿晚阶段流体属于中低温、中低盐度、中高密度流体。包裹体气相成分主要是H_2O,亦有少量CH_4和CO_2,成矿流体总体上属于H_2O-NaCl-(CH_4-CO_2)体系。Ⅰ、Ⅱ和Ⅲ阶段成矿流体的δD值为-92‰～-56‰,计算获得的δ~(18)O水值为3. 8‰～6. 4‰;石英-方解石阶段的δD值为-68‰～-58‰,δ~(18)O水值为0. 5‰～0. 7‰。H-O同位素结果表明,昆山矿床主成矿阶段的流体以岩浆水为主,成矿晚阶段有少量的大气降水加入。金属硫化物的δ~(34)S值分布集中,其值为-1. 5‰～3. 0‰,表明成矿流体中的硫主要来自深源岩浆。辉钼矿-石英阶段的石英包裹体中CO_2的δ~(13)CV-PDB值为-6. 6‰和-5. 9‰,平均-6. 3‰;晚阶段石英-方解石脉中方解石的δ~(13)CV-PDB值为-12. 3‰～-10. 2‰,平均-11. 0‰,表明昆山矿床主成矿阶段流体中的碳主要由花岗岩浆提供,且受低温蚀变作用的影响,而晚阶段方解石脉中的碳还受到了双桥山群沉积有机物质的影响。成矿流体的冷却作用是导致昆山矿床钨、钼和铜沉淀的主要机制。
The quartz veinlet-type Kunshan W-Mo-Cu deposit is located in the southern part of the Dahutang ore field,situated in the central area of the Jiuling tungsten-polymetallic ore cluster in northern Jiangxi Province. The ore-forming process of the deposit can be divided into four stages: wolframite-quartz stage( Ⅰ),molybdenite-quartz stage( Ⅱ),chalcopyrite-quartz stage( Ⅲ) and quartzcalcite stage( Ⅳ). In this paper,based on the previous research results and field geological survey,a systematic study of fluid inclusions and H-O-C-S isotopes was conducted. Three types of fluid inclusions( FIs) have been distinguished in various quartz veins including pure liquid( PL),pure gas( PG),liquid-rich two-phase( WL) inclusions. The FIs in the stage I are mainly WL-type with minor PG-type,and their homogenization temperatures,salinities and densities vary from 236℃ to 388℃,0. 5% to 13. 8% Na Cleqv and 0. 54 g/cm~3 to 0. 90 g/cm~3,respectively. The FIs in the stage Ⅱ are also mainly WL-type with minor PG-type,and their homogenization temperatures,salinities and densities vary from 221℃ to 390℃,0. 5% to 12. 7% Na Cleqv and 0. 51 g/cm~3 to 0. 93 g/cm~3,respectively. The FIs of the stage Ⅲ are composed of WL-type FIs,and their homogenization temperatures,salinities and densities vary from 228℃ to 376℃,0. 7% to 11. 2% Na Cleqv and 0. 57 g/cm~3 to 0. 91 g/cm~3,respectively. The FIs in the stage Ⅳare mainly WL-type with minor PL-type,and their homogenization temperatures,salinities and densities vary from 173℃ to 288℃,0. 4% to 11. 8% Na Cleqv and 0. 76 g/cm~3 to 0. 97 g/cm~3,respectively. The main ore-forming stage( stages Ⅰ,Ⅱ and Ⅲ) fluid is characterized by medium-high temperature,medium-low salinity and medium density,while the fluid of the stage Ⅳ is characterized by medium-low temperature,medium-low salinity and medium-high density. The gas-phase composition of the FIs is mainly H_2O with minor amounts of CH4 and CO_2,indicating that the ore-forming fluid of the Kunshan deposit belongs to an H_2O-NaCl-( CH_4-CO_2)system. The δ~(18) OH_2Oand δDH_2Ovalues of the main ore-forming stage vary from 3. 8‰ to 6. 4‰ and-92‰ to-56‰,respectively;the δ~(18) OH_2Oand δDH_2Ovalues of the stage Ⅳ vary from 0. 5‰ to 0. 7‰ and-68‰ to-58‰,respectively; indicating that the fluid of the main ore-forming stage mainly consists of magmatic water and that the fluid in late stage is a mixture of magmatic and meteoric water. The δ~(34) S values of chalcopyrite,pyrite and molybdenite samples range from-1. 5‰ to 3. 0‰,indicating that the ore-forming metals and sulfur mainly came from magma. The δ~(13) C values are in the ranges varying from-6. 6‰ to-5. 9‰ for FIs in quartz of the stage Ⅱ and -12. 3‰ to -10. 2‰ for calcite in the stage Ⅳ,respectively,suggesting that the carbon is mainly derived from the magma.Moreover,the carbon derived from the magma was affected by low-temperature alteration in the main ore-forming stage and mixed with sedimentary organic material of the Shuangqiaoshan Group in the late stage.The cooling of the ore-forming fluids was the dominant mechanism for precipitation of tungsten,molybdenum and copper in the Kunshan deposit.
The quartz veinlet-type Kunshan W-Mo-Cu deposit is located in the southern part of the Dahutang ore field,situated in the central area of the Jiuling tungsten-polymetallic ore cluster in northern Jiangxi Province. The ore-forming process of the deposit can be divided into four stages: wolframite-quartz stage( Ⅰ),molybdenite-quartz stage( Ⅱ),chalcopyrite-quartz stage( Ⅲ) and quartzcalcite stage( Ⅳ). In this paper,based on the previous research results and field geological survey,a systematic study of fluid inclusions and H-O-C-S isotopes was conducted. Three types of fluid inclusions( FIs) have been distinguished in various quartz veins including pure liquid( PL),pure gas( PG),liquid-rich two-phase( WL) inclusions. The FIs in the stage I are mainly WL-type with minor PG-type,and their homogenization temperatures,salinities and densities vary from 236℃ to 388℃,0. 5% to 13. 8% Na Cleqv and 0. 54 g/cm~3 to 0. 90 g/cm~3,respectively. The FIs in the stage Ⅱ are also mainly WL-type with minor PG-type,and their homogenization temperatures,salinities and densities vary from 221℃ to 390℃,0. 5% to 12. 7% Na Cleqv and 0. 51 g/cm~3 to 0. 93 g/cm~3,respectively. The FIs of the stage Ⅲ are composed of WL-type FIs,and their homogenization temperatures,salinities and densities vary from 228℃ to 376℃,0. 7% to 11. 2% Na Cleqv and 0. 57 g/cm~3 to 0. 91 g/cm~3,respectively. The FIs in the stage Ⅳare mainly WL-type with minor PL-type,and their homogenization temperatures,salinities and densities vary from 173℃ to 288℃,0. 4% to 11. 8% Na Cleqv and 0. 76 g/cm~3 to 0. 97 g/cm~3,respectively. The main ore-forming stage( stages Ⅰ,Ⅱ and Ⅲ) fluid is characterized by medium-high temperature,medium-low salinity and medium density,while the fluid of the stage Ⅳ is characterized by medium-low temperature,medium-low salinity and medium-high density. The gas-phase composition of the FIs is mainly H_2O with minor amounts of CH4 and CO_2,indicating that the ore-forming fluid of the Kunshan deposit belongs to an H_2O-NaCl-( CH_4-CO_2)system. The δ~(18) OH_2Oand δDH_2Ovalues of the main ore-forming stage vary from 3. 8‰ to 6. 4‰ and-92‰ to-56‰,respectively;the δ~(18) OH_2Oand δDH_2Ovalues of the stage Ⅳ vary from 0. 5‰ to 0. 7‰ and-68‰ to-58‰,respectively; indicating that the fluid of the main ore-forming stage mainly consists of magmatic water and that the fluid in late stage is a mixture of magmatic and meteoric water. The δ~(34) S values of chalcopyrite,pyrite and molybdenite samples range from-1. 5‰ to 3. 0‰,indicating that the ore-forming metals and sulfur mainly came from magma. The δ~(13) C values are in the ranges varying from-6. 6‰ to-5. 9‰ for FIs in quartz of the stage Ⅱ and -12. 3‰ to -10. 2‰ for calcite in the stage Ⅳ,respectively,suggesting that the carbon is mainly derived from the magma.Moreover,the carbon derived from the magma was affected by low-temperature alteration in the main ore-forming stage and mixed with sedimentary organic material of the Shuangqiaoshan Group in the late stage.The cooling of the ore-forming fluids was the dominant mechanism for precipitation of tungsten,molybdenum and copper in the Kunshan deposit.
引文
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