山西平顺地区西安里铁矿床地质特征及成因分析
|
摘要
西安里铁矿位于山西省南部,是华北地区重要的矽卡岩铁矿矿集区。铁矿石不仅品位高,而且岩体出露较好,适合矿体开采及理论研究。矿体形态复杂,大小不一,主要赋存于中生代中性侵入体与中奥陶统碳酸盐岩接触带及附近。褶皱和断层以及接触带是重要的控矿构造。矿石类型单一,主要矿物为磁铁矿。矿化蚀变具明显的分带现象。
本文以区域地质背景为基础,通过对西安里铁矿床特征、成矿流体、侵位方式、蚀变特征、成矿物质来源、运移等问题的研究,得出如下主要认识：
1.岩体围岩主要是泥灰岩和灰岩互层的中奥陶统碳酸盐岩,矿化受其性质较纯较脆灰岩的控制,主要成矿层位为O22地层、次为024地层；
2.晚期侵入岩体是主要的成矿母岩,而早期侵入岩体也间接为铁矿提供了一定的物质来源；
3.在分析含矿地层特征、矿化蚀变带元素分布特征、矿床物理化学条件及成矿物质来源的基础上,分析了矿床成因,并提出了成矿模式；
4.第一构造岩浆岩带和第二构造岩浆岩带分别具有不同的侵位机制,制约着铁矿体空间定位特征：第一岩浆岩带内杂岩体属被动就位机制,岩体内部可形成呈捕虏体状赋存的铁矿体,远离接触带的深部仍具找矿潜力；第二岩浆岩带内杂岩体属主动就位机制,岩体内部捕虏体罕见,相应的铁矿床主要产于岩体与围岩接触带处,捕虏体状赋存的铁矿体很少见到；
5.褶皱和断裂耦合关系决定了岩浆岩空间定位具有等距性分布的特征,间距一般为4km～5km,制约着铁矿体的形成和定位；
6.南北向、北北东向构造控制岩浆岩带的产出。两个方向构造交叉节点部位,岩浆活动强烈,也是成矿的有利部位。
Located in the south Shanxi province, Pingshun area is an important locality for skarn iron deposits in the North China. Pingshun's skarn iron deposits are rich in high-quality iron ore, having intrusive rocks with a great outcrop area, so it is advantageous to our study. With diverse shapes and different scale, the ore bodies are hosted along the contact belt between the intrusives and carbonate rocks. Folds, faults and contact zones are the dominating ore control and host structures. The ore type is monotonous magnetite. The mineralization and alteration are characterized by obvious zoning.
The article bases on the geological setting, researching on the point of characteristics of typical Fe desposit, Ore-forming fluid, Emplacement method, Alteration features, Ore sources and Migration of Xi'an li,as a result,we have the understanding as follows:
1.The wall rock of the rock is Middle Ordovician carbonate which have the alternating layers of marl and limestone, Mineralization is controlled by the more brittle and pure limestone and its mainly into the seam position is the stratum of O22,the second is O24.
2.The mainly ore rock is the late intrusions.But the early intrusions also provided a source of material indirectly.
3. Based on the analysis of the characteristics of ore-bearing stratum, the distribution of elements of the mineralization alteration zone, physical and chemical conditions of the deposit and the ore sources,analyzed the causes of the deposit and proposed mineralization model.
4.It is pointed out that the first and second tectonomagmatic belt with different mechanisms of emplacement have influence on the formation of ore deposits. The first belt belongs to positive emplacement mechanism. Within the pluton,the ore bodies show themselves as xenoliths, and there is the metallogenic potential far away from the contact zone between the intrusives and the carbonate rock while the second belt belongs to the passive emplacement mechanism. The xenoliths seldom occurs within the intrusive rocks, neither does the ore xenoliths. The iron deposits are mainly hosted along the contact zone between the intrusives and the carbonate rock, a minority within the carbonate country rocks.
5.Coupling between fold and fault determined the equidistant distribution of magmatic rocks and control the formation and location of iron ore, with the features of distribution range from 4 to 5km.
6. The structure of north-south control the output of magmatic rocks.The favorable parts of the mineralization is the cross-node of two fault where magmatic activity is strong.
本文以区域地质背景为基础,通过对西安里铁矿床特征、成矿流体、侵位方式、蚀变特征、成矿物质来源、运移等问题的研究,得出如下主要认识：
1.岩体围岩主要是泥灰岩和灰岩互层的中奥陶统碳酸盐岩,矿化受其性质较纯较脆灰岩的控制,主要成矿层位为O22地层、次为024地层；
2.晚期侵入岩体是主要的成矿母岩,而早期侵入岩体也间接为铁矿提供了一定的物质来源；
3.在分析含矿地层特征、矿化蚀变带元素分布特征、矿床物理化学条件及成矿物质来源的基础上,分析了矿床成因,并提出了成矿模式；
4.第一构造岩浆岩带和第二构造岩浆岩带分别具有不同的侵位机制,制约着铁矿体空间定位特征：第一岩浆岩带内杂岩体属被动就位机制,岩体内部可形成呈捕虏体状赋存的铁矿体,远离接触带的深部仍具找矿潜力；第二岩浆岩带内杂岩体属主动就位机制,岩体内部捕虏体罕见,相应的铁矿床主要产于岩体与围岩接触带处,捕虏体状赋存的铁矿体很少见到；
5.褶皱和断裂耦合关系决定了岩浆岩空间定位具有等距性分布的特征,间距一般为4km～5km,制约着铁矿体的形成和定位；
6.南北向、北北东向构造控制岩浆岩带的产出。两个方向构造交叉节点部位,岩浆活动强烈,也是成矿的有利部位。
Located in the south Shanxi province, Pingshun area is an important locality for skarn iron deposits in the North China. Pingshun's skarn iron deposits are rich in high-quality iron ore, having intrusive rocks with a great outcrop area, so it is advantageous to our study. With diverse shapes and different scale, the ore bodies are hosted along the contact belt between the intrusives and carbonate rocks. Folds, faults and contact zones are the dominating ore control and host structures. The ore type is monotonous magnetite. The mineralization and alteration are characterized by obvious zoning.
The article bases on the geological setting, researching on the point of characteristics of typical Fe desposit, Ore-forming fluid, Emplacement method, Alteration features, Ore sources and Migration of Xi'an li,as a result,we have the understanding as follows:
1.The wall rock of the rock is Middle Ordovician carbonate which have the alternating layers of marl and limestone, Mineralization is controlled by the more brittle and pure limestone and its mainly into the seam position is the stratum of O22,the second is O24.
2.The mainly ore rock is the late intrusions.But the early intrusions also provided a source of material indirectly.
3. Based on the analysis of the characteristics of ore-bearing stratum, the distribution of elements of the mineralization alteration zone, physical and chemical conditions of the deposit and the ore sources,analyzed the causes of the deposit and proposed mineralization model.
4.It is pointed out that the first and second tectonomagmatic belt with different mechanisms of emplacement have influence on the formation of ore deposits. The first belt belongs to positive emplacement mechanism. Within the pluton,the ore bodies show themselves as xenoliths, and there is the metallogenic potential far away from the contact zone between the intrusives and the carbonate rock while the second belt belongs to the passive emplacement mechanism. The xenoliths seldom occurs within the intrusive rocks, neither does the ore xenoliths. The iron deposits are mainly hosted along the contact zone between the intrusives and the carbonate rock, a minority within the carbonate country rocks.
5.Coupling between fold and fault determined the equidistant distribution of magmatic rocks and control the formation and location of iron ore, with the features of distribution range from 4 to 5km.
6. The structure of north-south control the output of magmatic rocks.The favorable parts of the mineralization is the cross-node of two fault where magmatic activity is strong.
引文
[1]翟裕生.矽卡岩矿床[M].矿床学教学参考书(上册).北京：地质出版社,1985124-135.
[2]黄华盛.矽卡岩矿床的研究现状[M].北京：中国地质大学出版社.1994,1(3--4).
[3]刘建朝,刘淑文,张海东,高坡.山西省平顺县西安里铁矿矿产预测项目报告[R].北京：中国地质调查局,2008
[4]Einaudi M T,Meinert L D and Newberry R J.Skarn deposits[J]. Economic Geology,1981,75:317-381.
[5]Cameron D E, Garmoe W J. Geology of Skarn and high-grade gold in the Carr Fork mine[J],Utah.Eco-nom is Geology,1987,82(5):1319-1333.
[6]吴言昌,常印佛.关于岩浆矽卡岩问题[J].地学前缘.1998,5(4).
[7]潘凤雏等.西藏甲马铜多金属矿床矽卡岩的喷流成因[J].现代地质.2002,16(4).
[8]张乾等.论接触交代矽卡岩型多金属矿床的矿质来源一以铅同位素组成为依据[J].矿物学报.1994,14(4).
[9]秦克章,汪东波,王之田等.中国东部铜矿床类型、成矿环境、成矿集中区与成矿系统[J].矿床地质.1999,18(4).
[10]雷文秀.层控式矽卡岩铜铁矿床的典型特征及其地质工作实践[J].有色金属(矿山部分).2004,56(5)
[11]赵一鸣,吴良士,白鸽,等.中国主要金属矿床成矿规律[M].北京：地质出版社,2004.1-411
[12]山西省地质局212地质队.芦沟矿区地质勘探报告[R].1960
[13]山西省地质局212地质队. 后墁—水沟岭矿区地质勘探报告[R].1973
[14]山西省地质局212地质队.北洛峡、茴菜峡、廿亩、水沟四矿区地质勘探报告[R].1963
[15]山西省地质局212地质队.山西省壶关县石河沐—陵川县六泉一带地质普查报[R].1963
[16]山西省地质局212地质队. 北洛峡矿区地质勘探报告[R].1973
[17]山西省地质局212地质队.山西省平顺县西安里铁矿交界坡矿区详细勘探地质[R].1982
[18]山西省地质局212地质队.西安里地区矽卡岩型铁矿控矿地质因素的初步认识[R].华 北富铁矿工作经验交流会议资料汇编.1975,5
[19]华北地质科学研究所一室铁矿研究队、河北地质学院地勘系.西安里接触交代型铁矿的蚀变交代作用特征[J].华北地质科技学报.1975.5
[20]二一二地质队.1979.再论“邯邢式”铁矿的钠化成矿机制[J].山西地质科技,(2)：1-9
[21]马润则,魏显贯,肖渊普.米仓地区一种与超基性岩有关的矽卡岩[J].同济大学学报,2001,29(11)：1322-1326
[22]章百明,赵国良,马国玺,等.河北省主要成矿区带矿床成矿系列及成矿模式[M].北京：石油工业出版社,1996,1-273
[23]林新多.岩浆成因矽卡岩的某些特征及形成机制初探[J].现代地质,1989,3(3)：351-358
[24]张京俊,贾琇明,陈平,田永清.山西省矿床成矿系列特征及成矿模式[M].北京：煤炭工业出版社,2003：15-50
[25]牛树银,陈路,许传诗等.太行山区地壳演化及成矿规律[M].北京：地震出版社,1994.1-200
[26]罗照华,邓晋福,赵国春,等.1997.太行山造山带岩浆活动特征及其造山过程反演[J].地球科学,22(3)：279-284
[27]董建华,陈斌,周凌.2003.太行山南段浮山岩体的成因：岩石学和地球化学证据[J].自然科学通报,13(7)：767-774
[28]Zindler A, Hart S. Chemical geodynamics. Ann. Rev, Earth Planet. Sci.,1986,14: 493-571
[29]邓晋福,赵国春, 赵海玲,等.2000.中国东部燕山期火山岩构造组合与造山：深部过程[J].地质论评,46(1)：41-43
[30]陈斌,刘超群,田伟.2006.太行中生代岩浆作用过程中的壳幔岩浆混合作用：岩石学和地球化学证据[J].地学前缘,13(2)：140-147
[31]陈斌,田伟,等.2005.太行山和华北其他地区中生代岩浆作用的锆石U-Pb年代学和地球化学特征及其岩浆成因和地球动力学意义[J].岩石学报,11(1)：13-23
[32]郑建平,路凤香,S.Y.O' Reilly.等.1999.华北地台东部古生代与新生代岩石圈地幔特征及其演化[J].地质学报,73(1)：47
[33]陈斌,崔明国,田伟,等.2005.太行山南段中生代杂岩体的岩石成因：元素和Nd-Sr-Pb同位素地球化学证据[J].矿物岩石地球化学通报,24(2)：93-101
[34]Rapp R P., Watson E B.,1995. Dehydration melting of metabasalt at 8-32 kbar: implications for continental growth and crust mantle recycling[J]. J. Petrol.,36:91-931.
[35]Alberade F.,1998. The growth of continental crust. Tetonophysics.196,1-14
[36]吴言昌.论岩浆矽卡岩—一种新型矽卡岩[J].安徽地质,1992,1(2)：12-26
[37]Yang, J.H., Wu, F. Y., Chung, S. L., Wilde, S.A., Wu, F.Y.,2007. Sources and petrogenesis of late Triassic dolerite dikes in the Liaodong Peninsula:implications for post-collsional lithosphere thinning of the eastern North China Craton. [J]. Petro.48, 1973-1997.
[38]Janousek V., Braithwaite CJ R., Bowesb D R., et al.2004. Magma-mixing in the genesis of herecynian calc-alkaline granitoids:an integrated petrographic and geochemical study of the Sa zava intrusion, Central Bohemian Pluton, Czech Republic [J]. Lithos,78: 67-99.
[39]Deng J F., Mo X X., Zhao H L., Wu Z X., et al,2004. A new model for the dynamic evolution of Chinese lithosphere:continental roots-plume tectonics'. Earth Science, Rew.,65:223-275.
[40]郁建华.1999.北京地区岩浆深成作用[M].北京：地质出版社.10-85
[41]廖宗廷,马婷婷,李玉加.永平矿区层状矽卡岩的成因及成矿意义[J].同济大学学报,2001,2(11)：1322-1326
[42]I.Yu. Safonova.,2008. Intraplate magmatism and oceanic plate stratigraphy of the Paleo-Asian and Paleo-Pacific Oceans from 600 to 140 Ma[J]. Ore Geology Reviews. Available online.
[43]Meinert L D.1989.Gold skarn deposits-geology and exploration criteria[J]. Econ. Geol., (Monograp 6):537-552.
[44]Jun Yan., Jiang-Feng Chen., Xi-Sheng Xu.,2008. Geochemistry of Cretaceous mafic rocks from the Lower Yangtze region, eastern China:Characteristics and evolution of the lithospheric mantle[J]. Journal of Asian Earth Sciences,33,177-193.
[45]罗照华,邓晋福,韩秀卿.1999.太行山造山带岩浆活动及其造山过程反演[M].北京： 地质出版社,1-124
[46]李宁,冯钟燕,于方.1989.山西北落峡铁矿床流体包裹体研究与矿床成因讨论[J].矿床地质,1(3)：113-124
[47]山西省地质局212地质队.1979.再论“邯邢式”铁矿的钠化成矿机制[J].山西地质科技,1(2)：1-9
[48]张守林.矽卡岩型铜矿成矿地质环境、成矿地质特征及找矿标志[J].矿产与地质,2001,15(5)：315-319
[49]邢集善,杨巍然,邢作云,等.2007.中国东部深部构造特征及其与矿集区关系[J].地学前缘,14(3)：114-129
[50]余元昌,李刚,肖国荃,等.1985.铜绿山接触交代铜铁矿床[M],1-128
[51]李兴海.西安里地区接触交代型铁矿控矿地质因素及矿床成因的初步探讨[R].山西省地质局212地质队,1976
[52]吴进甫,吴娜.安林地区接触交代型铁矿成矿规律探讨[J].安阳大学学报,2004,1：23-31
[53]田建涛.喻亨祥.扬准等.矽卡岩成因及成矿作用研究进展综述[J].中国科技信息,2005(23)：107.
[54]陈正乐.华北陆块铁矿床成矿规律总结研究2009年续作设计书[R].2009
[2]黄华盛.矽卡岩矿床的研究现状[M].北京：中国地质大学出版社.1994,1(3--4).
[3]刘建朝,刘淑文,张海东,高坡.山西省平顺县西安里铁矿矿产预测项目报告[R].北京：中国地质调查局,2008
[4]Einaudi M T,Meinert L D and Newberry R J.Skarn deposits[J]. Economic Geology,1981,75:317-381.
[5]Cameron D E, Garmoe W J. Geology of Skarn and high-grade gold in the Carr Fork mine[J],Utah.Eco-nom is Geology,1987,82(5):1319-1333.
[6]吴言昌,常印佛.关于岩浆矽卡岩问题[J].地学前缘.1998,5(4).
[7]潘凤雏等.西藏甲马铜多金属矿床矽卡岩的喷流成因[J].现代地质.2002,16(4).
[8]张乾等.论接触交代矽卡岩型多金属矿床的矿质来源一以铅同位素组成为依据[J].矿物学报.1994,14(4).
[9]秦克章,汪东波,王之田等.中国东部铜矿床类型、成矿环境、成矿集中区与成矿系统[J].矿床地质.1999,18(4).
[10]雷文秀.层控式矽卡岩铜铁矿床的典型特征及其地质工作实践[J].有色金属(矿山部分).2004,56(5)
[11]赵一鸣,吴良士,白鸽,等.中国主要金属矿床成矿规律[M].北京：地质出版社,2004.1-411
[12]山西省地质局212地质队.芦沟矿区地质勘探报告[R].1960
[13]山西省地质局212地质队. 后墁—水沟岭矿区地质勘探报告[R].1973
[14]山西省地质局212地质队.北洛峡、茴菜峡、廿亩、水沟四矿区地质勘探报告[R].1963
[15]山西省地质局212地质队.山西省壶关县石河沐—陵川县六泉一带地质普查报[R].1963
[16]山西省地质局212地质队. 北洛峡矿区地质勘探报告[R].1973
[17]山西省地质局212地质队.山西省平顺县西安里铁矿交界坡矿区详细勘探地质[R].1982
[18]山西省地质局212地质队.西安里地区矽卡岩型铁矿控矿地质因素的初步认识[R].华 北富铁矿工作经验交流会议资料汇编.1975,5
[19]华北地质科学研究所一室铁矿研究队、河北地质学院地勘系.西安里接触交代型铁矿的蚀变交代作用特征[J].华北地质科技学报.1975.5
[20]二一二地质队.1979.再论“邯邢式”铁矿的钠化成矿机制[J].山西地质科技,(2)：1-9
[21]马润则,魏显贯,肖渊普.米仓地区一种与超基性岩有关的矽卡岩[J].同济大学学报,2001,29(11)：1322-1326
[22]章百明,赵国良,马国玺,等.河北省主要成矿区带矿床成矿系列及成矿模式[M].北京：石油工业出版社,1996,1-273
[23]林新多.岩浆成因矽卡岩的某些特征及形成机制初探[J].现代地质,1989,3(3)：351-358
[24]张京俊,贾琇明,陈平,田永清.山西省矿床成矿系列特征及成矿模式[M].北京：煤炭工业出版社,2003：15-50
[25]牛树银,陈路,许传诗等.太行山区地壳演化及成矿规律[M].北京：地震出版社,1994.1-200
[26]罗照华,邓晋福,赵国春,等.1997.太行山造山带岩浆活动特征及其造山过程反演[J].地球科学,22(3)：279-284
[27]董建华,陈斌,周凌.2003.太行山南段浮山岩体的成因：岩石学和地球化学证据[J].自然科学通报,13(7)：767-774
[28]Zindler A, Hart S. Chemical geodynamics. Ann. Rev, Earth Planet. Sci.,1986,14: 493-571
[29]邓晋福,赵国春, 赵海玲,等.2000.中国东部燕山期火山岩构造组合与造山：深部过程[J].地质论评,46(1)：41-43
[30]陈斌,刘超群,田伟.2006.太行中生代岩浆作用过程中的壳幔岩浆混合作用：岩石学和地球化学证据[J].地学前缘,13(2)：140-147
[31]陈斌,田伟,等.2005.太行山和华北其他地区中生代岩浆作用的锆石U-Pb年代学和地球化学特征及其岩浆成因和地球动力学意义[J].岩石学报,11(1)：13-23
[32]郑建平,路凤香,S.Y.O' Reilly.等.1999.华北地台东部古生代与新生代岩石圈地幔特征及其演化[J].地质学报,73(1)：47
[33]陈斌,崔明国,田伟,等.2005.太行山南段中生代杂岩体的岩石成因：元素和Nd-Sr-Pb同位素地球化学证据[J].矿物岩石地球化学通报,24(2)：93-101
[34]Rapp R P., Watson E B.,1995. Dehydration melting of metabasalt at 8-32 kbar: implications for continental growth and crust mantle recycling[J]. J. Petrol.,36:91-931.
[35]Alberade F.,1998. The growth of continental crust. Tetonophysics.196,1-14
[36]吴言昌.论岩浆矽卡岩—一种新型矽卡岩[J].安徽地质,1992,1(2)：12-26
[37]Yang, J.H., Wu, F. Y., Chung, S. L., Wilde, S.A., Wu, F.Y.,2007. Sources and petrogenesis of late Triassic dolerite dikes in the Liaodong Peninsula:implications for post-collsional lithosphere thinning of the eastern North China Craton. [J]. Petro.48, 1973-1997.
[38]Janousek V., Braithwaite CJ R., Bowesb D R., et al.2004. Magma-mixing in the genesis of herecynian calc-alkaline granitoids:an integrated petrographic and geochemical study of the Sa zava intrusion, Central Bohemian Pluton, Czech Republic [J]. Lithos,78: 67-99.
[39]Deng J F., Mo X X., Zhao H L., Wu Z X., et al,2004. A new model for the dynamic evolution of Chinese lithosphere:continental roots-plume tectonics'. Earth Science, Rew.,65:223-275.
[40]郁建华.1999.北京地区岩浆深成作用[M].北京：地质出版社.10-85
[41]廖宗廷,马婷婷,李玉加.永平矿区层状矽卡岩的成因及成矿意义[J].同济大学学报,2001,2(11)：1322-1326
[42]I.Yu. Safonova.,2008. Intraplate magmatism and oceanic plate stratigraphy of the Paleo-Asian and Paleo-Pacific Oceans from 600 to 140 Ma[J]. Ore Geology Reviews. Available online.
[43]Meinert L D.1989.Gold skarn deposits-geology and exploration criteria[J]. Econ. Geol., (Monograp 6):537-552.
[44]Jun Yan., Jiang-Feng Chen., Xi-Sheng Xu.,2008. Geochemistry of Cretaceous mafic rocks from the Lower Yangtze region, eastern China:Characteristics and evolution of the lithospheric mantle[J]. Journal of Asian Earth Sciences,33,177-193.
[45]罗照华,邓晋福,韩秀卿.1999.太行山造山带岩浆活动及其造山过程反演[M].北京： 地质出版社,1-124
[46]李宁,冯钟燕,于方.1989.山西北落峡铁矿床流体包裹体研究与矿床成因讨论[J].矿床地质,1(3)：113-124
[47]山西省地质局212地质队.1979.再论“邯邢式”铁矿的钠化成矿机制[J].山西地质科技,1(2)：1-9
[48]张守林.矽卡岩型铜矿成矿地质环境、成矿地质特征及找矿标志[J].矿产与地质,2001,15(5)：315-319
[49]邢集善,杨巍然,邢作云,等.2007.中国东部深部构造特征及其与矿集区关系[J].地学前缘,14(3)：114-129
[50]余元昌,李刚,肖国荃,等.1985.铜绿山接触交代铜铁矿床[M],1-128
[51]李兴海.西安里地区接触交代型铁矿控矿地质因素及矿床成因的初步探讨[R].山西省地质局212地质队,1976
[52]吴进甫,吴娜.安林地区接触交代型铁矿成矿规律探讨[J].安阳大学学报,2004,1：23-31
[53]田建涛.喻亨祥.扬准等.矽卡岩成因及成矿作用研究进展综述[J].中国科技信息,2005(23)：107.
[54]陈正乐.华北陆块铁矿床成矿规律总结研究2009年续作设计书[R].2009