四川盆地震旦系—古生界热液作用及其成藏成矿效应初探
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摘要
震旦纪—古生代期间四川盆地发生过兴凯地裂运动及峨眉地裂运动两次强烈的构造热液活动。盆地周缘的金属成矿作用主要发生于晚二叠世,与峨眉山岩浆活动相关,形成了会泽、大梁子、天宝山等一系列MVT型铅锌矿,及会理小石房、汉源黑区-雪区SEDEX型铅锌矿。盆地内部常见热液矿物组合,有:白云石-石英-黄铁矿组合、黄铜矿-黄铁矿-孔雀石组合、天青石-硬石膏-石英及白云石-萤石组合、白云石-天青石等组合;其主要呈溶蚀脉或孔洞状、以及交代状交代白云岩、页岩及生物屑含云灰岩或灰岩等。四川盆地二叠系长兴组礁白云岩与阳新统灰岩中发育的砂糖状白云岩可能均是热液作用产物,或经历过热液蚀变。震旦系87Sr/86Sr比值对比表明在深埋过程中,震旦系具有三期外来侵蚀性富87Sr/86Sr比值的流体充注;震旦系裂缝中白云石,奥陶、志留系裂缝中的方解石的87Sr/86Sr比值明显高于自身围岩与同期海水87Sr/86Sr比值,三者相近的值表明在后期构造隆升过程中超压热液释放,发生跨层流动。热液可影响区域热流值,使川西南地区地温梯度明显高于川东(北)地区,致使二叠系-三叠系及下寒武统具有相对较高的沉积期地温。盆地周缘铅锌矿床与有机质及盆地油田卤水具有密切关系。热液作用为震旦系—古生界储层中与构造相关的溶蚀孔洞缝提供了一种新的溶蚀机理,以及先前多解释成埋藏成因砂糖状白云石、礁白云岩可能均是热液成因;热液白云岩与围岩基质相比具有相对较高储层物性,特别是在区域性低孔隙度低渗透率的震旦系—古生界中形成热液白云岩优质储层,为今后四川盆地震旦系—古生界碳酸盐岩勘探提供了一个重要方向。
There are two stages of tectonic hydrothermal fluid activities forming in Xingkai taphrogeny and Emei taphrogeny in Sichuan basin during the Sinian-Palaeozoic periods.Mineral accumulation around Sichuan basin mainly formed in late Permian,which was related to Emei magmatic activity,and formed a series of MVT Pb-Zn ore bodies,such as Huize,Daliangzi,Tianbaoshan,and formed SEDEX Pb-Zn ore bodies in Xiaoshifang of Huili,Heiqu-Xuequ of Hanyuan.The commonly hydrothermal mineral combinations are dolomite-quartz-pyrite,chalcopyrite-pyrite-malachite,celestite-anhydrite-quartz,dolomite-fluorite and dolomite-celestite.These combinations mainly replace dolomite,shale,bioclastic dolomitic limestone or limestone etc.The genesis of reef dolomite in the Changxing Formation of upper Permian and saccharoidal limestone in the Yangxing series may be affected by hydrothermal fluid process,or suffered by hydrothermal alterations.Geochemistry is characterized by poor in strontium or natrium,and rich in ferrum or manganese,depleted in 18O with homogenization temperature of 156 ℃～256 ℃.Hydrothermal fluids can affect provincial heat value,leading to geothermal gradient in the southwest Sichuan province being higher than that in the northeast Sichuan province,and resulting in a situation of relatively high sedimentary geothermal temperature in Permian-Triassic and lower Cambrian periods.Pb-Zn ore bodies occurred around the basin margin,organic and brine in oil field are of close relatiionship.Hydrothermal fluid process provides a new dissolution mechanism for dissolution pores,cavies and dissolution fractures which are related to tectonic activities in the Sinian-Palaeozoic reservoirs.The genetic factor of saccharoidal dolomite and reef dolomite,which were previously interpreted as burial origin,may be resulted from hydrothermal fluid activity.There is much better reservoir physical property in hydrothermal dolomite than that in matrix host rock,especially in provincial low porosity and low permeability rocks which can form high quality reservoir in the Sinian-Palaeozoic.
There are two stages of tectonic hydrothermal fluid activities forming in Xingkai taphrogeny and Emei taphrogeny in Sichuan basin during the Sinian-Palaeozoic periods.Mineral accumulation around Sichuan basin mainly formed in late Permian,which was related to Emei magmatic activity,and formed a series of MVT Pb-Zn ore bodies,such as Huize,Daliangzi,Tianbaoshan,and formed SEDEX Pb-Zn ore bodies in Xiaoshifang of Huili,Heiqu-Xuequ of Hanyuan.The commonly hydrothermal mineral combinations are dolomite-quartz-pyrite,chalcopyrite-pyrite-malachite,celestite-anhydrite-quartz,dolomite-fluorite and dolomite-celestite.These combinations mainly replace dolomite,shale,bioclastic dolomitic limestone or limestone etc.The genesis of reef dolomite in the Changxing Formation of upper Permian and saccharoidal limestone in the Yangxing series may be affected by hydrothermal fluid process,or suffered by hydrothermal alterations.Geochemistry is characterized by poor in strontium or natrium,and rich in ferrum or manganese,depleted in 18O with homogenization temperature of 156 ℃～256 ℃.Hydrothermal fluids can affect provincial heat value,leading to geothermal gradient in the southwest Sichuan province being higher than that in the northeast Sichuan province,and resulting in a situation of relatively high sedimentary geothermal temperature in Permian-Triassic and lower Cambrian periods.Pb-Zn ore bodies occurred around the basin margin,organic and brine in oil field are of close relatiionship.Hydrothermal fluid process provides a new dissolution mechanism for dissolution pores,cavies and dissolution fractures which are related to tectonic activities in the Sinian-Palaeozoic reservoirs.The genetic factor of saccharoidal dolomite and reef dolomite,which were previously interpreted as burial origin,may be resulted from hydrothermal fluid activity.There is much better reservoir physical property in hydrothermal dolomite than that in matrix host rock,especially in provincial low porosity and low permeability rocks which can form high quality reservoir in the Sinian-Palaeozoic.
引文
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[2]Sangster D F.World class MVT and SEDEX lead_zinc deposit[A].Geol.Survey of Canada Min.Colloquium,No.1[C].Ottawa:OttawaCongress Centre,1994:556-568.
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[4]Davies G R,Smith L B.Structurally controlled hydrothermal dolomite reservoir facies:An overview[J].AAPG Bulletin,2006,90(11):1 641-1 690.
[5]罗志立.中国西南地区晚古生代以来地裂运动对石油等矿产形成的影响[J].四川省地质学报,1981,2(1):1-22.
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[9]林方成.扬子地台西缘大渡河谷超大型层状铅锌矿床地质地球化学特征及成因[J].地质学报,2005,79(4):540-558.
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[11]金之钧,朱东亚,胡文?,等.塔里木盆地热液活动地质地球化学特征及其对储层影响[J].地质学报,2006,80(2):245-253
[12]胡受奚,叶瑛,方长泉,等.交代蚀变岩岩石学及其找矿意义[M].北京:地质出版社,2004.
[13]郑荣才,胡忠贵,冯青平,等.川东北地区长兴组白云岩储层的成因研究[J].矿物岩石,2007,27(4):79-84.
[14]强子同,文应初,雷卞军,等.川东鄂西上二叠系生物礁白云岩化的岩石和地球化学[J].地球化学,1992,21(2):158-166.
[15]Veizer J,Hoefs I.The nature of18O/16O and13C/12C secular trends in sedimentary carbonate rocks[J].Geochim.Cosmochim Acta,1976,40(11):1 387-1 395.
[16]雷卞军,强子同,文应初.川东及邻区上二叠统生物礁的白云岩化[J].地质论评,1994,40(6):534-543.
[17]储昭宏.川东北长兴组-飞仙关组碳酸盐岩储层研究.博士论文[D].北京:中国地质大学,2006.
[18]Allan J R,Wiggins W D.Dolomite reservoirs:geochemical techniques for evaluating origin and distribution(AAPG Continuing EducationCourse Note series#36)[J].Tulsa(Oklahoma,U.S.A):AAPG,1993.
[19]黄智龙,陈进,刘从强,等.峨眉山玄武岩与铅锌成矿关系初探-以云南会泽铅锌矿为例[J].矿物学报,2001,21(4):681-688.
[20]Anderson G M.Organic maturation and Ore precipitation in Southeast Missouri[J].Economic Geology,1991,86(5):909-926.
[21]刘文均,郑荣才.花垣铅锌矿床包裹体气相组份研究-MVT矿床有机成矿作用研究(Ⅱ)[J].沉积学报,1999,17(4):608-614.
[22]Sverjensky D A,Rye D M.The lead and sulfide isotopic compositions of galena from a Mississippi valley-type deposit in the New lead belt,Southeast Missouri[J].Economic Geology,1979,74(1):1 491-1 543.
[23]李发源,顾雪祥,付绍洪,等.有机质在MVT铅锌矿床形成中的作用[J].矿物岩石地球化学通报,2002,21(4):272-276.
[24]李泽琴,王奖臻,倪师军,等.川滇密西西比河谷型铅锌矿床成矿流体来源研究:流体Na-Cl-Br体系的证据[J].矿物岩石,2002,22(4):38-41.
[25]彭晓蕾,高玉巧,刘立,等.含油气盆地中热流体活动的流体包裹体依据[J].世界地质,2005,24(4):350-356.
[26]郭正吾,邓康龄.四川盆地形成与演化[M].北京:地质出版社,1994.
[27]罗志立.中国地裂运动[J].石油实验地质,2001,23(2):232-240.
[28]刘树根,罗志立,庞家黎,等.四川龙门山地区的峨眉地裂运动[J].四川地质学报,1991,11(3):174-180.
[29]Oliver J,Fluids expelled tectonically from orogenic belts:Their role in hydrocarbon migration and other geo1gical phenomena[J].Geology,1986,14(2):99-102.
[30]邓军,王庆飞,高帮飞,等.鄂尔多斯盆地多种能源矿产分布及其构造背景[J].地球科学-中国地质大学学报,2006,31(3):330-336.
[31]潘爱芳,赫英,黎荣剑,等.鄂尔多斯盆地基底断裂与能源矿产成藏成矿的关系[J].大地构造与成矿学,2005,29(4):459-464.
[2]Sangster D F.World class MVT and SEDEX lead_zinc deposit[A].Geol.Survey of Canada Min.Colloquium,No.1[C].Ottawa:OttawaCongress Centre,1994:556-568.
[3]Bjrlykke K.Fluid flow in sedimentary basins[J].Sedimentary Geology,1993,86(1):137-158.
[4]Davies G R,Smith L B.Structurally controlled hydrothermal dolomite reservoir facies:An overview[J].AAPG Bulletin,2006,90(11):1 641-1 690.
[5]罗志立.中国西南地区晚古生代以来地裂运动对石油等矿产形成的影响[J].四川省地质学报,1981,2(1):1-22.
[6]罗志立,刘树根,刘顺,等.峨眉地幔柱对扬子板块和塔里木板块的离散作用及其找矿意义[J].地球学报,2004,25(5):515-522.
[7]骆耀南,傅德明,何虹.峨眉山地幔柱活动的成矿作用及其成矿系列———峨眉山地幔柱与资源环境效应学术研讨会文集[C].成都,2003,99-100.
[8]李英.论热液矿床的分类[J].地质与勘探,1992,28(9):1-8.
[9]林方成.扬子地台西缘大渡河谷超大型层状铅锌矿床地质地球化学特征及成因[J].地质学报,2005,79(4):540-558.
[10]沈苏,金明霞.西昌-滇中地区主要矿产成矿规律及找矿方向[M].重庆:重庆出版社,1988.
[11]金之钧,朱东亚,胡文?,等.塔里木盆地热液活动地质地球化学特征及其对储层影响[J].地质学报,2006,80(2):245-253
[12]胡受奚,叶瑛,方长泉,等.交代蚀变岩岩石学及其找矿意义[M].北京:地质出版社,2004.
[13]郑荣才,胡忠贵,冯青平,等.川东北地区长兴组白云岩储层的成因研究[J].矿物岩石,2007,27(4):79-84.
[14]强子同,文应初,雷卞军,等.川东鄂西上二叠系生物礁白云岩化的岩石和地球化学[J].地球化学,1992,21(2):158-166.
[15]Veizer J,Hoefs I.The nature of18O/16O and13C/12C secular trends in sedimentary carbonate rocks[J].Geochim.Cosmochim Acta,1976,40(11):1 387-1 395.
[16]雷卞军,强子同,文应初.川东及邻区上二叠统生物礁的白云岩化[J].地质论评,1994,40(6):534-543.
[17]储昭宏.川东北长兴组-飞仙关组碳酸盐岩储层研究.博士论文[D].北京:中国地质大学,2006.
[18]Allan J R,Wiggins W D.Dolomite reservoirs:geochemical techniques for evaluating origin and distribution(AAPG Continuing EducationCourse Note series#36)[J].Tulsa(Oklahoma,U.S.A):AAPG,1993.
[19]黄智龙,陈进,刘从强,等.峨眉山玄武岩与铅锌成矿关系初探-以云南会泽铅锌矿为例[J].矿物学报,2001,21(4):681-688.
[20]Anderson G M.Organic maturation and Ore precipitation in Southeast Missouri[J].Economic Geology,1991,86(5):909-926.
[21]刘文均,郑荣才.花垣铅锌矿床包裹体气相组份研究-MVT矿床有机成矿作用研究(Ⅱ)[J].沉积学报,1999,17(4):608-614.
[22]Sverjensky D A,Rye D M.The lead and sulfide isotopic compositions of galena from a Mississippi valley-type deposit in the New lead belt,Southeast Missouri[J].Economic Geology,1979,74(1):1 491-1 543.
[23]李发源,顾雪祥,付绍洪,等.有机质在MVT铅锌矿床形成中的作用[J].矿物岩石地球化学通报,2002,21(4):272-276.
[24]李泽琴,王奖臻,倪师军,等.川滇密西西比河谷型铅锌矿床成矿流体来源研究:流体Na-Cl-Br体系的证据[J].矿物岩石,2002,22(4):38-41.
[25]彭晓蕾,高玉巧,刘立,等.含油气盆地中热流体活动的流体包裹体依据[J].世界地质,2005,24(4):350-356.
[26]郭正吾,邓康龄.四川盆地形成与演化[M].北京:地质出版社,1994.
[27]罗志立.中国地裂运动[J].石油实验地质,2001,23(2):232-240.
[28]刘树根,罗志立,庞家黎,等.四川龙门山地区的峨眉地裂运动[J].四川地质学报,1991,11(3):174-180.
[29]Oliver J,Fluids expelled tectonically from orogenic belts:Their role in hydrocarbon migration and other geo1gical phenomena[J].Geology,1986,14(2):99-102.
[30]邓军,王庆飞,高帮飞,等.鄂尔多斯盆地多种能源矿产分布及其构造背景[J].地球科学-中国地质大学学报,2006,31(3):330-336.
[31]潘爱芳,赫英,黎荣剑,等.鄂尔多斯盆地基底断裂与能源矿产成藏成矿的关系[J].大地构造与成矿学,2005,29(4):459-464.
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