江西冷水坑斑岩型铅锌银矿床地质特征、热液蚀变与成矿时限
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摘要
江西冷水坑铅锌银矿床是我国重要的铅锌银矿床之一,也是世界上少有的斑岩型铅锌银矿床。冷水坑斑岩型铅锌银矿床位于中国东部中生代月凤山火山盆地边缘,含矿斑岩为燕山中期碱性花岗斑岩,侵位于上侏罗统火山岩地层内,斑岩体边部发育大量的隐爆角砾岩。矿区发育两种矿化类型,即斑岩型矿化与层状改造型矿化,此两种均与碱性花岗斑岩有关。矿化以Pb、Zn、Ag为主,伴生少量的Cu、Au。斑岩型的铅锌银矿化发生在斑岩体内以及接触带中,具有面型矿化特点并显示出明显的矿化分带性。层状改造型以铁锰银铅锌矿化为主,矿体均为隐伏状分布于碱性花岗斑岩附近的火山岩含铁锰地层中,产状与火山岩地层一致。铁锰碳酸盐铅锌银矿体在靠近斑岩体时,银铅锌矿化相应逐渐增强,而远离花岗斑岩体,矿化明显较弱。围岩蚀变作用明显,主要为绢云母化、绿泥石化、碳酸盐化、硅化和黄铁矿化。矿化蚀变特征、蚀变类型与典型的斑岩型铜(钼)矿床不同,缺少斑岩铜(钼)矿床早期蚀变的钾交代作用(黑云母化与钾长石化),发育大量铁锰碳酸盐蚀变。矿田矿化蚀变具有一定的分带性,由岩体内向外蚀变可以分为三个带:绿泥石绢云母化带、绢云母化碳酸盐化硅化黄铁矿化带和碳酸盐化绢云母化带。斑岩型矿床的铅锌银矿化与绢云母化和绿泥石化蚀变密切相关。通过对蚀变矿物绢云母的40Ar/39Ar同位素测定,获得冷水坑斑岩型铅锌银矿化年龄为162.8±1.6Ma,与含矿斑岩形成时间一致,说明冷水坑斑岩型铅锌银成矿作用发生于中国东部燕山中期陆内环境。
Lengshuikeng deposit in Jiangxi Province is one of the most important Pb-Zn-Ag deposits in China,which is also a rare,typical porphyry Pb-Zn-Ag deposit in the world. It is hosted in the Yuefengshan Mesozoic volcanic basin,eastern China. The ore-bearing porphyry is alkaline granite porphyry intruding into upper Jurassic volcanic rocks in the Middle Yanshanian period. A large number of cryptoexplosion breccia is developed around the edge of the ore-bearing porphyry. In the Lengshuikeng ore district,there are two types of mineralization,porphyry-type and layered transformation type,both of which are related to the alkaline granite porphyry. Porphyry-type Pb-Zn-Ag mineralization occurs in the porphyry and the contact zone of the porphyry to the volcanic rocks,showing a distinct mineralization zoning. The layered transformation type is characterized by Fe-Mn-Ag-Pb-Zn Mineralization,with the orebodies concealing in the volcanic rocks containing ferrous manganese carbonate,which is adjacent to the alkaline granite porphyry. Pb-Zn-Ag mineralization becomes weak from porphyry mass outward. The alteration of wall-rocks in the Lengshuikeng deposit includes sericitization,chloritization,carbonatization,silicification and pyritization. The Lengshuikeng porphyry Pb-Zn-Ag deposit differs from the typical porphyry Cu-Mo deposit in its abundant Fe-Mn carbonate alteration instead of potassium replacement appearing at the early alteration stage of porphyry Cu(Mo) deposits. The ore district,however,is of three distinct zones based on the altered mineral assemblages. Three zonations classified are chlorite sericite zone,the sericite carbonate silicate pyrite zone,and the carbonate sercite zone from the inner of the porphyry outward. The Pb-Zn-Ag mineralization of the porphyry deposit is closely related to the sercite and chlorite alteration. 40Ar/39Ar dating of sericite yields an isochron age of 162.8 ±1.6Ma,which is consistent with that of the ore-bearing porphyry,indicating that the deposit formed on the intracontinental setting in Eastern China during the mid-Yanshanian period.
Lengshuikeng deposit in Jiangxi Province is one of the most important Pb-Zn-Ag deposits in China,which is also a rare,typical porphyry Pb-Zn-Ag deposit in the world. It is hosted in the Yuefengshan Mesozoic volcanic basin,eastern China. The ore-bearing porphyry is alkaline granite porphyry intruding into upper Jurassic volcanic rocks in the Middle Yanshanian period. A large number of cryptoexplosion breccia is developed around the edge of the ore-bearing porphyry. In the Lengshuikeng ore district,there are two types of mineralization,porphyry-type and layered transformation type,both of which are related to the alkaline granite porphyry. Porphyry-type Pb-Zn-Ag mineralization occurs in the porphyry and the contact zone of the porphyry to the volcanic rocks,showing a distinct mineralization zoning. The layered transformation type is characterized by Fe-Mn-Ag-Pb-Zn Mineralization,with the orebodies concealing in the volcanic rocks containing ferrous manganese carbonate,which is adjacent to the alkaline granite porphyry. Pb-Zn-Ag mineralization becomes weak from porphyry mass outward. The alteration of wall-rocks in the Lengshuikeng deposit includes sericitization,chloritization,carbonatization,silicification and pyritization. The Lengshuikeng porphyry Pb-Zn-Ag deposit differs from the typical porphyry Cu-Mo deposit in its abundant Fe-Mn carbonate alteration instead of potassium replacement appearing at the early alteration stage of porphyry Cu(Mo) deposits. The ore district,however,is of three distinct zones based on the altered mineral assemblages. Three zonations classified are chlorite sericite zone,the sericite carbonate silicate pyrite zone,and the carbonate sercite zone from the inner of the porphyry outward. The Pb-Zn-Ag mineralization of the porphyry deposit is closely related to the sercite and chlorite alteration. 40Ar/39Ar dating of sericite yields an isochron age of 162.8 ±1.6Ma,which is consistent with that of the ore-bearing porphyry,indicating that the deposit formed on the intracontinental setting in Eastern China during the mid-Yanshanian period.
引文
陈繁荣,裘愉卓.1995.江西贵溪冷水坑多金属矿床成矿过程流体地球化学模拟及其地质意义.地球化学,24(1)(增刊):24~32.
陈克荣,陈武,周建平,等.1988.江西冷水坑火山-侵入杂岩体岩石化学及地球化学特征.岩石矿物学杂志,6(1):18~28.
陈武,周建平.1988.江西冷水坑斑岩型银铅锌矿床矿化特征.矿物岩石,8(2):84~91.
邓绍明.1985.江西贵溪冷水坑银铅锌矿区控岩控矿构造基本特征.江西地质科技,16~25.
邓绍明.1991.江西贵溪冷水坑古火山岩区隐爆碎屑岩类型及成因探讨.江西地质科技,18(1):28~32.
董绍芳.1994.江西冷水坑含金斑岩及金矿化特征.江西地质,8(1):14~20.
侯增谦,莫宣学,高永丰,等,2003,埃达克岩:斑岩铜矿的一种可能的重要含矿母岩。矿床地质,22(1):1~12
侯增谦,高永丰,曲晓明,等.2004.西藏冈底斯中新世斑岩铜矿带:埃达克质斑岩成因与构造控制.岩石学报,20(2):239~248.
黄振强.1992a.冷水坑碳酸盐型银矿床成因探讨.江西地质,6(1):1~8.
黄振强.1992b.冷水坑银矿田的发现与评价.江西地质,6(4):309~314.
黄振强.1993.冷水坑银矿田成矿条件及矿床特征.贵金属地质,2(4):284~291.
李兆鼐,权恒,李之彤,等.2003.中国东部中新生代火成岩及其深部过程.北京:地质出版社.
刘讯,申世亮.1991.江西冷水坑银铅锌矿田构造地球化学的若干问题.大地构造与成矿学,15(1):41~54.
罗诒爵.1985.冷水坑斑岩型铅锌矿床地质特征.矿床地质,4(4):15~24.
罗治爵.1991.冷水坑斑岩型银铅锌矿床围岩蚀变特征。江西地质,5(1):3~10.
孟祥金,侯增谦,高永丰,等.2004.碰撞造山型斑岩铜矿蚀变分带模式-以西藏冈底斯斑岩铜矿带为例.地学前缘,11(1):201~214.
戚建中,芮行健,章纯荪.1986.江西贵溪冷水坑矿区岩浆演化模式探讨.中国地质科学院南京地质矿产研究所所刊,7(1):34~40.
齐进英.1987.江西冷水坑斑岩类型及其矿化特征.岩石学报,(1):40~49.
芮宗瑶,黄崇轲,齐国明等,1984.中国斑岩铜(钼)矿床.北京:地质出版社,1~350.
唐仁鲤,罗怀松.1995.西藏玉龙斑岩铜(钼)矿带地质.北京:地质出版社.
涂光炽等.1989.中国铅锌矿床.见:《中国矿床》编委会,中国矿床(上册).北京:地质出版社.116~204.
王安城.1991.冷水坑斑岩银铅锌矿银的赋存状态及富集规律.江西地质,5(3):227~237.
魏明秀.1997,江西冷水坑斑岩银矿床的蚀变碳酸盐矿物与银矿化关系.矿产与地质,11(57):39~45.
徐文炘,肖孟华,陈民扬.2001.江西冷水坑银铅锌矿床同位素地球化学研究.矿物岩石地球化学通报,20(4):370~372.
严学信,赵志刚,何细荣.2007.贵溪冷水坑银矿田银元素富集规律研究.资源调查与环境,28(1):46~53.
杨扬.1987.江西贵溪冷水坑铅锌银矿田的成矿类型.地质与勘探,5:11~16.
杨存来.1993.江西冷水坑铅锌银矿床地球化学异常特征及找矿模型。物探与化探,17(3):173~181.
张乾.1990.山东香夼斑岩型铅锌矿床的地球化学特征及成因探讨.地质找矿论丛,5(2):12~20.
朱训,黄崇轲,芮宗瑶,等,1983.德兴斑岩铜矿.北京:地质出版社.
左力艳,孟祥金,杨竹森.2008.冷水坑斑岩型银铅锌矿床含矿岩系岩石地球化学及Sr、Nd同位素研究.矿床地质,27(3):367~372.
Defant MJ,Drummond MS.1990.Derivation of some modern arcmagmas by melting of young subductedlithosphere:Nature,v.347,p.662~665.
Gustafson L B,Orgrera W,Mewilliams M,et al.2001.Multiplecenters of mineralization in the Indio Muerto district,ElSlavador,Chile,Econ.Geol.v.96,p.325~350.
Lowell J D,Guilbert J M.1970.Lateral and vertical alteration-mineralization zoningin porphyry ore deposits.Econ.Geol.,v.65,p.373~408.
Hollister V F.1974.Regional characteristics of porphyry copperdeposits of south America.Trans,SME-AI ME,256:45~53.
Hou Z Q,Ma H W,Khin Zaw,and Zhang,Y Q.2003.TheYulong Porphyry Copper Belt:Product of Large-Scale Strike-Slip Faulting in Eastern Tibet:Economic Geology,v.98,p.125~145.
Kerrich R,Goldfarb R,Groves D,Garwin S.2000.Thecharacteristics,origins,and geodynamic settings of supergiantgold metallogenic provinces:Sicence in China,v.43,p.1~68.
Sillitoe R H.1972.Aplate tectonic modle for the origin of porphyrycopper deposits.Econ.Geol.,v.67,p.184~197.
Sillitoe R H.1998.Major regional factors favouringlarge size,highhypogene grade,elevated gold content and supergene oxidationand enrichment of porphyry copper deposits.Porter T M.Porphyry and Hydrothermal Copper and Gold Deposits-a globalperspective.Perth,Adelaide:Australian Mineral Foundation/PGC Publishing,p.49~60.
Skewes M A,Stern C R.1995.Genesis of the giant late Miocene toPliocene copper deposits of central Chile in the context ofAndean magmatic and tectonic evolution.International GeologyReview.V.37(10),p.893~909.
Titley S R,Beane R E.1989.Porphyry copper deposits,part I,Geologic setting,petrology and tectogenesis.Econ.Geol.75th.Anniv.v.1,p.214~235.
陈克荣,陈武,周建平,等.1988.江西冷水坑火山-侵入杂岩体岩石化学及地球化学特征.岩石矿物学杂志,6(1):18~28.
陈武,周建平.1988.江西冷水坑斑岩型银铅锌矿床矿化特征.矿物岩石,8(2):84~91.
邓绍明.1985.江西贵溪冷水坑银铅锌矿区控岩控矿构造基本特征.江西地质科技,16~25.
邓绍明.1991.江西贵溪冷水坑古火山岩区隐爆碎屑岩类型及成因探讨.江西地质科技,18(1):28~32.
董绍芳.1994.江西冷水坑含金斑岩及金矿化特征.江西地质,8(1):14~20.
侯增谦,莫宣学,高永丰,等,2003,埃达克岩:斑岩铜矿的一种可能的重要含矿母岩。矿床地质,22(1):1~12
侯增谦,高永丰,曲晓明,等.2004.西藏冈底斯中新世斑岩铜矿带:埃达克质斑岩成因与构造控制.岩石学报,20(2):239~248.
黄振强.1992a.冷水坑碳酸盐型银矿床成因探讨.江西地质,6(1):1~8.
黄振强.1992b.冷水坑银矿田的发现与评价.江西地质,6(4):309~314.
黄振强.1993.冷水坑银矿田成矿条件及矿床特征.贵金属地质,2(4):284~291.
李兆鼐,权恒,李之彤,等.2003.中国东部中新生代火成岩及其深部过程.北京:地质出版社.
刘讯,申世亮.1991.江西冷水坑银铅锌矿田构造地球化学的若干问题.大地构造与成矿学,15(1):41~54.
罗诒爵.1985.冷水坑斑岩型铅锌矿床地质特征.矿床地质,4(4):15~24.
罗治爵.1991.冷水坑斑岩型银铅锌矿床围岩蚀变特征。江西地质,5(1):3~10.
孟祥金,侯增谦,高永丰,等.2004.碰撞造山型斑岩铜矿蚀变分带模式-以西藏冈底斯斑岩铜矿带为例.地学前缘,11(1):201~214.
戚建中,芮行健,章纯荪.1986.江西贵溪冷水坑矿区岩浆演化模式探讨.中国地质科学院南京地质矿产研究所所刊,7(1):34~40.
齐进英.1987.江西冷水坑斑岩类型及其矿化特征.岩石学报,(1):40~49.
芮宗瑶,黄崇轲,齐国明等,1984.中国斑岩铜(钼)矿床.北京:地质出版社,1~350.
唐仁鲤,罗怀松.1995.西藏玉龙斑岩铜(钼)矿带地质.北京:地质出版社.
涂光炽等.1989.中国铅锌矿床.见:《中国矿床》编委会,中国矿床(上册).北京:地质出版社.116~204.
王安城.1991.冷水坑斑岩银铅锌矿银的赋存状态及富集规律.江西地质,5(3):227~237.
魏明秀.1997,江西冷水坑斑岩银矿床的蚀变碳酸盐矿物与银矿化关系.矿产与地质,11(57):39~45.
徐文炘,肖孟华,陈民扬.2001.江西冷水坑银铅锌矿床同位素地球化学研究.矿物岩石地球化学通报,20(4):370~372.
严学信,赵志刚,何细荣.2007.贵溪冷水坑银矿田银元素富集规律研究.资源调查与环境,28(1):46~53.
杨扬.1987.江西贵溪冷水坑铅锌银矿田的成矿类型.地质与勘探,5:11~16.
杨存来.1993.江西冷水坑铅锌银矿床地球化学异常特征及找矿模型。物探与化探,17(3):173~181.
张乾.1990.山东香夼斑岩型铅锌矿床的地球化学特征及成因探讨.地质找矿论丛,5(2):12~20.
朱训,黄崇轲,芮宗瑶,等,1983.德兴斑岩铜矿.北京:地质出版社.
左力艳,孟祥金,杨竹森.2008.冷水坑斑岩型银铅锌矿床含矿岩系岩石地球化学及Sr、Nd同位素研究.矿床地质,27(3):367~372.
Defant MJ,Drummond MS.1990.Derivation of some modern arcmagmas by melting of young subductedlithosphere:Nature,v.347,p.662~665.
Gustafson L B,Orgrera W,Mewilliams M,et al.2001.Multiplecenters of mineralization in the Indio Muerto district,ElSlavador,Chile,Econ.Geol.v.96,p.325~350.
Lowell J D,Guilbert J M.1970.Lateral and vertical alteration-mineralization zoningin porphyry ore deposits.Econ.Geol.,v.65,p.373~408.
Hollister V F.1974.Regional characteristics of porphyry copperdeposits of south America.Trans,SME-AI ME,256:45~53.
Hou Z Q,Ma H W,Khin Zaw,and Zhang,Y Q.2003.TheYulong Porphyry Copper Belt:Product of Large-Scale Strike-Slip Faulting in Eastern Tibet:Economic Geology,v.98,p.125~145.
Kerrich R,Goldfarb R,Groves D,Garwin S.2000.Thecharacteristics,origins,and geodynamic settings of supergiantgold metallogenic provinces:Sicence in China,v.43,p.1~68.
Sillitoe R H.1972.Aplate tectonic modle for the origin of porphyrycopper deposits.Econ.Geol.,v.67,p.184~197.
Sillitoe R H.1998.Major regional factors favouringlarge size,highhypogene grade,elevated gold content and supergene oxidationand enrichment of porphyry copper deposits.Porter T M.Porphyry and Hydrothermal Copper and Gold Deposits-a globalperspective.Perth,Adelaide:Australian Mineral Foundation/PGC Publishing,p.49~60.
Skewes M A,Stern C R.1995.Genesis of the giant late Miocene toPliocene copper deposits of central Chile in the context ofAndean magmatic and tectonic evolution.International GeologyReview.V.37(10),p.893~909.
Titley S R,Beane R E.1989.Porphyry copper deposits,part I,Geologic setting,petrology and tectogenesis.Econ.Geol.75th.Anniv.v.1,p.214~235.
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