安徽省铜山矽卡岩型铜矿床流体成矿作用研究
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摘要
长江中下游是我国东部重要的铁、铜、金多金属成矿带,安徽铜山铜矿位于扬子地块的西北缘,北临大别造山带,是该成矿带安庆~(-)贵池矿集区中的一个典型的矽卡岩型矿床。矿床产于燕山期铜山岩体与石炭系黄龙~(-)船山组、二叠系栖霞组地层的接触带中,受岩浆岩、构造、地层和围岩蚀变的共同控制。NE和EW向断裂构造交汇部位控制成矿岩体的就位,控矿和容矿构造主要为接触带构造及不整合面构造等。成矿过程可分为三个阶段:矽卡岩阶段、石英~(-)硫化物阶段和碳酸盐阶段。
各成矿阶段的石榴石、石英和方解石中的流体包裹体岩相学研究结果表明,包裹体主要类型有NaCl~(-)H_2O型流体包裹体(W型)、含子矿物流体包裹体(S型)。在石榴石和石英中发现晶质熔融包裹体。矽卡岩阶段的流体包裹体主要为W型和S型,均一温度为478~769℃,盐度为55.47 wt%,成矿流体具有高温、高盐度的特征;石英~(-)硫化物阶段的流体包裹体主要为W型,S型次之,均一温度为86.2~399.5℃,盐度为0.18~22.91wt%,成矿流体具有中低温、中低盐度的特征;碳酸盐阶段的流体包裹体全为W型,均一温度为154.6~368.5℃,盐度为0.53~22.91wt%,成矿流体具有中低温、低盐度的特征。从矽卡岩阶段到石英~(-)硫化物阶段,均一温度和盐度快速降低,从石英~(-)硫化物阶段到碳酸盐阶段均一温度和盐度变化不明显。经估算,铜山铜矿的成矿压力大约为21Mpa,形成深度可能为2.3km。
流体包裹体主要气体组成为H_2O、CO_2、CH_4,液相离子主要为Ca~(2~(+))、K~(+)、SO4~(2~(-))、Cl~(-)。从矽卡岩阶段到碳酸盐阶段,CO_2、CH_4、Ca~(2~(+))、SO4~(2~(-))、Cl~(-)含量逐渐降低,K~(+)含量逐渐上升,H_2O先减少后增加。
包裹体的氢氧同位素表明,成矿流体主要来源于岩浆热液,后期有大气降水混入。硫铅同位素表明,成矿物质来源于岩浆;Re~(-)Os同位素定年表明,铜山铜矿的成矿时间是150.98±0.78 Ma,为燕山早期。根据不同类型包裹体共生组合及流体演化特征,认为熔体~(-)流体的不混溶作用和流体的混合作用是金属沉淀的主要原因。
The Tongshan copper deposit in Anqing-Guichi Cu-Fe-Au-Mo district is a typical skarn deposit in The Lower Yangtze River metallogentic belt, which is located at the northern margin of the Yangze craton and bordered by the Dabieshan orogenic belt to the north.
The ore bodies are related to Tongshan granodiorite and quartz monzonite porphyry, which intruded mainly into Middle Carboniferous Huanglong-Chuanshan Formation, Lower Permian Qixia Formation carbonates and is characterized by porphyritic textures and carbonatization. The location of ore-forming intrusions were controlled by the intersecting places between the NE and EW trending fault structures. The ore-controlling and ore-bearing structures mainly include contact zone, interlayer fractures zone and unconformity structure, etc. The metalogenic processs can be devided into the skarn stage, the quartz-sulfide stage and the carbonate stage. In recent years, new ore layers have been discovered, but the study on fluid inclusions is urgently needed which restricts the ore genesis and metallogenic laws.
This paper made further discussion on the source of ore-forming materials and the ore genesis in terms of fluid inclusions. Petrographic observations and temperature results indicate that the main types of fluid inclusions are aqueous inclusions, daughter-mineral-bearing multiphase inclusions, occasionally crystalline melt inclusions(recognized in garnet, quartz) which are the evidence of magmatic skarn. In the skarn stage, the ore-forming fluid is characterized by high temperature and high salinity, Th (homogenization temperature) is 478~769℃with salinity of 55.47 wt%. In the quartz-sulfide stage, the ore-forming fluid is characterized by middle-low temperature and middle-low salinity, Th is 86.2~399.5℃with salinity 0.18~22.91wt%; In the carbonate stage, the ore-forming fluid is characterized by middle-low temperature and low salinity, Th ranges from 154.6 to 368.5℃with salinity from 0.53 to 22.91wt%. The Metallogenic pressure is approximately 21Mpa, Metallogenic depth is 2.3km.
The results of Raman analysis indicate that major components of gaseous or supercritical species are H_2O, CO_2, CH_4; the major ions in solution are Ca~(2+), K~+, SO4~(2-), Cl~-. From early to late stage, the contents of CO_2, CH_4, Ca~(2+), SO4~(2-), Cl~- decreased, K~+ increased, H_2O decreased firstly and then increased.
The D-O isotopic analysis indicates that the ore-forming fluids were mainly magmatic hydrothermal fluids and mixed with meteoric water during the later mineralization stage; The S and Pb isotopic analysis indicate that metallogenic material derived from magma; the Re-Os dating indicates Metallogenic age is 150.98±0.78 Ma, Early Yanshanian.
According to the assemblage and evolution characteristics of different fluid inclusions, the immiscibility of melt-fluids and the mixing of fluids are the main causes for mineralization.
各成矿阶段的石榴石、石英和方解石中的流体包裹体岩相学研究结果表明,包裹体主要类型有NaCl~(-)H_2O型流体包裹体(W型)、含子矿物流体包裹体(S型)。在石榴石和石英中发现晶质熔融包裹体。矽卡岩阶段的流体包裹体主要为W型和S型,均一温度为478~769℃,盐度为55.47 wt%,成矿流体具有高温、高盐度的特征;石英~(-)硫化物阶段的流体包裹体主要为W型,S型次之,均一温度为86.2~399.5℃,盐度为0.18~22.91wt%,成矿流体具有中低温、中低盐度的特征;碳酸盐阶段的流体包裹体全为W型,均一温度为154.6~368.5℃,盐度为0.53~22.91wt%,成矿流体具有中低温、低盐度的特征。从矽卡岩阶段到石英~(-)硫化物阶段,均一温度和盐度快速降低,从石英~(-)硫化物阶段到碳酸盐阶段均一温度和盐度变化不明显。经估算,铜山铜矿的成矿压力大约为21Mpa,形成深度可能为2.3km。
流体包裹体主要气体组成为H_2O、CO_2、CH_4,液相离子主要为Ca~(2~(+))、K~(+)、SO4~(2~(-))、Cl~(-)。从矽卡岩阶段到碳酸盐阶段,CO_2、CH_4、Ca~(2~(+))、SO4~(2~(-))、Cl~(-)含量逐渐降低,K~(+)含量逐渐上升,H_2O先减少后增加。
包裹体的氢氧同位素表明,成矿流体主要来源于岩浆热液,后期有大气降水混入。硫铅同位素表明,成矿物质来源于岩浆;Re~(-)Os同位素定年表明,铜山铜矿的成矿时间是150.98±0.78 Ma,为燕山早期。根据不同类型包裹体共生组合及流体演化特征,认为熔体~(-)流体的不混溶作用和流体的混合作用是金属沉淀的主要原因。
The Tongshan copper deposit in Anqing-Guichi Cu-Fe-Au-Mo district is a typical skarn deposit in The Lower Yangtze River metallogentic belt, which is located at the northern margin of the Yangze craton and bordered by the Dabieshan orogenic belt to the north.
The ore bodies are related to Tongshan granodiorite and quartz monzonite porphyry, which intruded mainly into Middle Carboniferous Huanglong-Chuanshan Formation, Lower Permian Qixia Formation carbonates and is characterized by porphyritic textures and carbonatization. The location of ore-forming intrusions were controlled by the intersecting places between the NE and EW trending fault structures. The ore-controlling and ore-bearing structures mainly include contact zone, interlayer fractures zone and unconformity structure, etc. The metalogenic processs can be devided into the skarn stage, the quartz-sulfide stage and the carbonate stage. In recent years, new ore layers have been discovered, but the study on fluid inclusions is urgently needed which restricts the ore genesis and metallogenic laws.
This paper made further discussion on the source of ore-forming materials and the ore genesis in terms of fluid inclusions. Petrographic observations and temperature results indicate that the main types of fluid inclusions are aqueous inclusions, daughter-mineral-bearing multiphase inclusions, occasionally crystalline melt inclusions(recognized in garnet, quartz) which are the evidence of magmatic skarn. In the skarn stage, the ore-forming fluid is characterized by high temperature and high salinity, Th (homogenization temperature) is 478~769℃with salinity of 55.47 wt%. In the quartz-sulfide stage, the ore-forming fluid is characterized by middle-low temperature and middle-low salinity, Th is 86.2~399.5℃with salinity 0.18~22.91wt%; In the carbonate stage, the ore-forming fluid is characterized by middle-low temperature and low salinity, Th ranges from 154.6 to 368.5℃with salinity from 0.53 to 22.91wt%. The Metallogenic pressure is approximately 21Mpa, Metallogenic depth is 2.3km.
The results of Raman analysis indicate that major components of gaseous or supercritical species are H_2O, CO_2, CH_4; the major ions in solution are Ca~(2+), K~+, SO4~(2-), Cl~-. From early to late stage, the contents of CO_2, CH_4, Ca~(2+), SO4~(2-), Cl~- decreased, K~+ increased, H_2O decreased firstly and then increased.
The D-O isotopic analysis indicates that the ore-forming fluids were mainly magmatic hydrothermal fluids and mixed with meteoric water during the later mineralization stage; The S and Pb isotopic analysis indicate that metallogenic material derived from magma; the Re-Os dating indicates Metallogenic age is 150.98±0.78 Ma, Early Yanshanian.
According to the assemblage and evolution characteristics of different fluid inclusions, the immiscibility of melt-fluids and the mixing of fluids are the main causes for mineralization.
引文
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Liu L M, Zhao Y L and Zhao X L. Computational modeling oncoupled MTH processes for forming skarn Cu deposits and its signifi-cance for deep ore exploration: Examples from Tongling-Anqing district, China. Journal of Geochemical Exploration, 2009, 101: 63
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Clayton R N, O'Neil J R,. Mayeda T K. Oxygen isotope exchange between quartz and water. Journal of Geophysical Research, 1972, 77: 3057~3067
Einaudi M T, Burt D M. Introduction: Terminology, classification and composition of skarn deposit. Economic Geology, 1982, 77(4): 745~760
Einaudi M T, Meinert L D, Newberry R J. Skarn deposits.Econ Geology, 75 th Anniv, 1981: 317~391
Hall DL, Sterner SM and Bodnar RJ. Freezing point depression of NaCl-KCl-H_2O solutions. Econ. Geol. 1988, 83: 197~202
Helgeson HC. Thermodynamics of Hydrothermal systems at elevated and pressures. Am Jour Sci, 1969, 59: 729~804
Liu L M, Zhao Y L and Zhao X L. Computational modeling oncoupled MTH processes for forming skarn Cu deposits and its signifi-cance for deep ore exploration: Examples from Tongling-Anqing district, China. Journal of Geochemical Exploration, 2009, 101: 63
Meinert L D. A review of skarn that contain gold. In: LentzD R, ed. Mineralized intrusion- related skarn systems. Quebec. Short Course Series, 1998, 26: 359~414
Meinert L D. Application of skarn deposit zonation models tomineral exploration. Explor. Mining Geol., 1997a, 6 (2): 185~208
Meinert L D. Dipple G M and Nicolescu S. World skarn deposits. Econ Geol., 2005, 100: 299~336 Naden J, Shepherd T J. Role of methane and carbon dioxide in good deposition. Nature, 1989, 243: 793~795
O’Neil J R, Clayton R N and Mayeda T K. Oxygen isotope fractionation in divalent mental carbonates. J. Chem. Phys, 1969, 51: 5547~5558
Pan Y M, Dong P. The lower Changjiang(Yangzi/Yangtze River)metallogenetic belt, east central China: intrusion-and wall rock-hosted Cu-Fe-Au, Mo, Zn, Pb, Ag deposits. Ore Geology Reviews, 1999, 15(4): 177~242
Rodder E. Fluid inclusion evidence on the genesis of ores in sedimentary and volcanic rocks// Wolf K H. Handbook of Strata-bound and stratiform Ore Deposits: I. Principles and General Studies: Vol. 2, Geochemical Studies. New York: Elsevier, 1976: 67~110
Roedder E. The composition of fluid inclusions. U. S. Geological Survey prof. paper 440 JJ,1972,164
Sun YL, Xu P, Li J et al. A practical method for determination of molybdenite Re-Os ages by inductively coupled plasma-mass spectrometry combined with Carius tube-HNO_3 digestion. The Royal Society of Chemistry: Analytical Methods, 2010, 2: 575~581
Talor H P. The application of oxygen and hydrogen isotope studies to problems of hydrothermal alteration and ore deposition. Econ. Geol., 1974, 69: 843~883
Zartman R. E, Doe B. R. Plumbotectonics-the model. Tectonophysics, 1981, 75: 135~162
Zhou Tao-fa, Yuan Feng, Yue Shu-cang, et al. Geochemistry and evolution of ore-forming fluids of the Yueshan Cu-Au skarn and vein-type deposits, Anhui Province, South China. Ore Geology Reviews, 2005, 31: 279~303
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