内蒙古中部渣尔泰山群元素地球化学特征及铀成矿指示
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摘要
位于华北地台北缘的渣尔泰山群,是中元古代裂谷沉积的一套碎屑岩─碳酸盐─碎屑岩建造,自下而上分为书记沟组、增隆昌组、阿古鲁沟组和刘鸿湾组。渣尔泰山群是我国的重要含矿层位之一,蕴涵了许多大型─超大型铜、铅、锌等多金属硫化物矿床,而且也是一个重要的含铀层位。
本文主要以内蒙古中部的渣尔泰山群作为研究对象,对该群的四个岩性组从微量元素、稀土元素地球化学角度进行对比研究,运用地球化学的理论和方法及软件作图,分析对比各岩性组的地球化学特征的异同点,从元素的富集迁移角度来探讨物源特征和古环境特点等;结合601铀矿点的特征,与阿古鲁沟组非矿点进行对比,综合研究热液来源及对铀有指示作用的元素。得出以下几点结论:
1)从整个渣尔泰山群来看,各微量元素的含量与岩性有关,富集的微量元素有W、Re、Pb、Sb、Ba、Hf、Ta,表现为亏损的元素有Ni、Cu、Sr、Nb、In。增隆昌组灰岩中的微量元素亏损较严重,书记沟组和刘鸿湾组的碎屑岩次之,阿古鲁沟组的碳质板岩富集的微量元素最多。
2)阿古鲁沟组是前寒武纪的一个重要成矿层位,产有Cu、Pb、Zn、Au、U矿等,所以对该组的研究是工作的重中之重。其古环境的探讨可以由以下指标得出:通过δU=2U/(U+Th/3)大于1和w (V)/ w (V+Ni)值得出该组处于还原环境。将阿古鲁沟组样品的投入w(Zn)-w(Co)-w(Ni)三元图中,大部分靠近海底热水沉积区,表明本区阿古鲁沟组大部分都受到了热水沉积的影响。
3)渣尔泰山群ΣREE的变化范围总体较大,稀土含量配分模式表现为LREE富集,HREE亏损,稀土元素含量随岩性而异。通过w(La) /w(Yb) -w(ΣREE)的投点,表明阿古鲁沟组沉积时期物源与其他组有较大差异。
4)601铀矿点位于渣尔泰山群的阿古鲁沟组中,铀矿化与铁帽关系密切;元素Th、U在601矿点发生了分离。稀土元素在碳质板岩和脉体的变化比较大,表明在成矿期有组分的重新分配。
5)通过相关性分析,表明601矿点与非矿点中的元素U与W、Re、Mo、Ta相关性较好,表明成矿流体可能来源于深部;元素Fe、Pb、Cd、Re、Ni对铀成矿具有一定指示作用。
Zha Ertaishan group, a sedimentation rift valley of proterozoic era,lying in the North China Platform, is made up of a clastic rock-carbonate-clastic rock construction.From bottom to top it consists of Shu jigou group,Zheng longchang group,A gulugou group,Liu hongwan group. Zha Ertai group is one of a most important concentrating mineral stratum in our country.There are many large and over-large sale Copper,Leading,Zinc polymetallic sulfide deposits,it is also an important uranium layer.
This article mainly regards Zha Ertaishan group in Inner Mongolia as a central object of study,it is compared four groups with the trace elements and rare earth elements,using geochemical theory,methods and software for mapping to compare the geochemical characteristics of each group with similarities and differences,and the article tries to explore the source characteristics and environmental characteristics of ancient from the enrichment and migration of elements; Combining the characteristics of 601 Uranium ore-spot, focal point of the work is the contrast of non-ore spot, synthesize the research for the source of ore-forming fluids and the role of the element uranium instructions. Draw the following conclusions:
1) In tatol view of the Zha Eertai shan group,the content of each trace elements is related with lithology.The enriched trace elements include W、Re、Pb、Sb、Ba、Hf、Ta, the deficient of the trace elements include Ni、Cu、Sr、Nb、In. specially,Zheng longchang group is most deficient of the trace elements, clastic rock of Shu jigou group and Liu hongwan group takes second place,the most enriched trace elements is A gulugou group’s carbonaceous slate.
2) A gulugou group is a very important ore formation stratum of Precambrian, it births Cu、Pb、Zn、Au、U and so on.Therefore, the research group is the most important task. The ancient environment of indicators can be derived by the following:Due toδU=2U/(U+Th/3) greater than 1 and w (V)/ w (V+Ni) obtained in a reducing environment of this group.Input the samples of A gulugou group to the w(Zn)-w(Co)-w(Ni) ternary diagram,most are near the seabed hydrothermal area,it indicates that most area of A gulugou group is influenced by deposition of water.
3) There is a large range ofΣREE of Zha etaishan group, distribution patterns of rare earth is the enrichment of LREE,and the deficient of HREE, the rare earth elements content varies with the lithology.With the input the samples of w(La) /w(Yb) -w(ΣREE),it indicates that the source of A gulugou group is different from other groups.
4)601 uranium deposit lies in the A gulugou group of Zha ertaishan group, the uranium mineralization is closely related with the iron cap,with the separation of Th、U.The rare earth elements are with big change between carbonaceous slate and veins, it indicates that there is a composition redistribution during the mineralization period.
5)Through the correlation analysis,the element U is closely linked with W、Re、Mo、Ta both 601 uranium deposit and non-ore spot,it is possible that the ore-forming fluids originated from mantle; in conclusion,Fe、Pb、Cd、Re、Ni give certain direction on the role of U mineralization.
本文主要以内蒙古中部的渣尔泰山群作为研究对象,对该群的四个岩性组从微量元素、稀土元素地球化学角度进行对比研究,运用地球化学的理论和方法及软件作图,分析对比各岩性组的地球化学特征的异同点,从元素的富集迁移角度来探讨物源特征和古环境特点等;结合601铀矿点的特征,与阿古鲁沟组非矿点进行对比,综合研究热液来源及对铀有指示作用的元素。得出以下几点结论:
1)从整个渣尔泰山群来看,各微量元素的含量与岩性有关,富集的微量元素有W、Re、Pb、Sb、Ba、Hf、Ta,表现为亏损的元素有Ni、Cu、Sr、Nb、In。增隆昌组灰岩中的微量元素亏损较严重,书记沟组和刘鸿湾组的碎屑岩次之,阿古鲁沟组的碳质板岩富集的微量元素最多。
2)阿古鲁沟组是前寒武纪的一个重要成矿层位,产有Cu、Pb、Zn、Au、U矿等,所以对该组的研究是工作的重中之重。其古环境的探讨可以由以下指标得出:通过δU=2U/(U+Th/3)大于1和w (V)/ w (V+Ni)值得出该组处于还原环境。将阿古鲁沟组样品的投入w(Zn)-w(Co)-w(Ni)三元图中,大部分靠近海底热水沉积区,表明本区阿古鲁沟组大部分都受到了热水沉积的影响。
3)渣尔泰山群ΣREE的变化范围总体较大,稀土含量配分模式表现为LREE富集,HREE亏损,稀土元素含量随岩性而异。通过w(La) /w(Yb) -w(ΣREE)的投点,表明阿古鲁沟组沉积时期物源与其他组有较大差异。
4)601铀矿点位于渣尔泰山群的阿古鲁沟组中,铀矿化与铁帽关系密切;元素Th、U在601矿点发生了分离。稀土元素在碳质板岩和脉体的变化比较大,表明在成矿期有组分的重新分配。
5)通过相关性分析,表明601矿点与非矿点中的元素U与W、Re、Mo、Ta相关性较好,表明成矿流体可能来源于深部;元素Fe、Pb、Cd、Re、Ni对铀成矿具有一定指示作用。
Zha Ertaishan group, a sedimentation rift valley of proterozoic era,lying in the North China Platform, is made up of a clastic rock-carbonate-clastic rock construction.From bottom to top it consists of Shu jigou group,Zheng longchang group,A gulugou group,Liu hongwan group. Zha Ertai group is one of a most important concentrating mineral stratum in our country.There are many large and over-large sale Copper,Leading,Zinc polymetallic sulfide deposits,it is also an important uranium layer.
This article mainly regards Zha Ertaishan group in Inner Mongolia as a central object of study,it is compared four groups with the trace elements and rare earth elements,using geochemical theory,methods and software for mapping to compare the geochemical characteristics of each group with similarities and differences,and the article tries to explore the source characteristics and environmental characteristics of ancient from the enrichment and migration of elements; Combining the characteristics of 601 Uranium ore-spot, focal point of the work is the contrast of non-ore spot, synthesize the research for the source of ore-forming fluids and the role of the element uranium instructions. Draw the following conclusions:
1) In tatol view of the Zha Eertai shan group,the content of each trace elements is related with lithology.The enriched trace elements include W、Re、Pb、Sb、Ba、Hf、Ta, the deficient of the trace elements include Ni、Cu、Sr、Nb、In. specially,Zheng longchang group is most deficient of the trace elements, clastic rock of Shu jigou group and Liu hongwan group takes second place,the most enriched trace elements is A gulugou group’s carbonaceous slate.
2) A gulugou group is a very important ore formation stratum of Precambrian, it births Cu、Pb、Zn、Au、U and so on.Therefore, the research group is the most important task. The ancient environment of indicators can be derived by the following:Due toδU=2U/(U+Th/3) greater than 1 and w (V)/ w (V+Ni) obtained in a reducing environment of this group.Input the samples of A gulugou group to the w(Zn)-w(Co)-w(Ni) ternary diagram,most are near the seabed hydrothermal area,it indicates that most area of A gulugou group is influenced by deposition of water.
3) There is a large range ofΣREE of Zha etaishan group, distribution patterns of rare earth is the enrichment of LREE,and the deficient of HREE, the rare earth elements content varies with the lithology.With the input the samples of w(La) /w(Yb) -w(ΣREE),it indicates that the source of A gulugou group is different from other groups.
4)601 uranium deposit lies in the A gulugou group of Zha ertaishan group, the uranium mineralization is closely related with the iron cap,with the separation of Th、U.The rare earth elements are with big change between carbonaceous slate and veins, it indicates that there is a composition redistribution during the mineralization period.
5)Through the correlation analysis,the element U is closely linked with W、Re、Mo、Ta both 601 uranium deposit and non-ore spot,it is possible that the ore-forming fluids originated from mantle; in conclusion,Fe、Pb、Cd、Re、Ni give certain direction on the role of U mineralization.
引文
[1]内蒙古自治区第一区域地质调查队七分队,渣尔泰地区1:50000区域地质调查报告[M].内部资料.1985.
[2]内蒙古自治区地层表编写组.华北地区区域地层表,内蒙古分册[M].地质出版社,1978.
[3]王楫等.狼山-白云鄂博裂谷系[M].北京市:北京大学出版社, 1992.01.1-123.
[4]王楫等.内蒙古渣尔泰山群与白云鄂博群时代对比及含矿性[M].呼和浩特:内蒙古人民出版社,1989.5-140.
[5]董申保.中国变质作用及其地壳演化的关系[M].北京:地质出版社,1986.233—234.
[6]张选阳译编,1989,层序底层学与海平面变化.据The Special Issue-The GSGP Project on Cretaceous Resources, Events and Rhythms(CRER).岩相古地理,1期,第1-10页.
[7]谭琳,朱绅玉,周盛德,等.内蒙古渣尔泰山群岩相古地理[M] .北京:地质出版社,1991. 1—126.
[8]乔秀夫,姚培毅,王成述,等.内蒙古渣尔泰山群层序地层学及构造环境[J].地质学报, 1991,65(1): 1—14.
[9]王思源,杨海明.狼山造山带喷溢成矿研究[M].武汉:中国地质大学出版社,1993.
[10]芮宗瑶,等.华北陆块北缘及邻区有色金属矿床地质[M].北京:地质出版社,1994,121-126.
[11]施林道,谢贤俊,巩正基.狼山-渣尔泰山中元古代裂陷槽有色金属矿床[A].见:芮宗瑶,施林道,方如恒,等编.华北陆块北缘及邻区有色金属矿床地质[C].北京:地质出版社.1994.121-126.
[12]黄占起,沈存利,王守光.内蒙古狼山—渣尔泰山地区与黑色岩系有关的铂族元素矿床找矿前景[J].地质通报,2002,21(10).
[13]沈存利,王守光,苏新旭,等.内蒙古中元古界渣尔泰山群区域成矿地质特征研究[J].地学前缘,2004,11(1).
[14]李永明,陈安平等.内蒙古固阳地区铀矿普查地质报告[R].核工业二○八大队.内部资料.1984.
[15]张日辉,李承厚等.固阳县康兔沟601地段地质工作总结报告[R].核工业二○八大队.内部资料.1985.
[16]内蒙古自治区地质矿产局.内蒙古自治区区域地质志[M].北京:地质出版社,1991.
[17]内蒙古自治区地质矿产局.内蒙古自治区岩石地层[M].中国地质大学出版社,1996.
[18]黄午兴.狼山地区元古代多金属硫化物矿床成矿特征探讨[D].成都:成都理工大学,2009.
[19]涂光炽等.低温地球化学[M].北京市:科学出版社, 1998.
[20]戴塔根,刘汉元.微量元素地球化学及应用[M].长沙:中南工业大学出版社, 1992:3.
[21]刘云. 1998.皖南晚震旦世硅质岩的成因研究.地层学杂志,22(2):154-160.
[22]王中刚,于学元,赵振华.稀土元素地球化学[M].北京:科学出版社, 1989:1-278.
[23]赵红格,刘池洋.2003.物源分析方法及研究进展.沉积学报,21(3):409-415.
[24]韩吟文,马振东.地球化学[M].北京:地质出版社,2003:189-202.
[25]王益友,郭文莹,张国栋.几种地化标志在金湖凹陷阜宁群沉积环境中的应用[J].同济大学学报, 1979, 7(2): 51-60.
[26]吴朝东,陈其英.1999.湘西磷块岩的岩石地球化学特征及成因.地质科学,34(2):213-222.
[27] Steiner M, Wallis E, Erdtmann B-D, et al. 2001. Submarine-hydrothermal exhalative ore layers in black shales from SouthChina and associated fossils—insights into a Lower Cambrianfacies and bio-evolution. Palaeogeography, Palaeoclimatology,Palaeoecology,169: 165-191.
[28] Hatch JR, Leventhal JS. Relationship between inferred redoxpo-tential of the depositional environment and geochemistry of theUp- perPennsylvanian(Missourian)Stark ShaleMember of the DennisLimestone, Wabaunsee County, Kansas, U·S·A. [J]. ChemicalGeology, 1992, 99: 65-82.
[29] JaiH C, Yu H. Geochemistry and depositional environmentofMnoxide deposits in the Tokoro Belt, northeastern Hokkaido, Japan[J]. EconomicGeology, 1992, 87(5):1265-1274
[30]杨剑等,2004.黔北黑色岩系的岩石化学特地球征和成因.矿物学报,24(3).
[31]翟裕生,邓军,汤中立,等.古陆边缘成矿系统[M].北京市:地质出版社,2002.
[32] Girty G H,Hanson A D,Knaack C,Johnson D,1994,Provenancedetermined by REE, Th and Sc analyses of metasedimentaryrock,Boyden Cave Pendant,central Sierra Nevada,California.Journal of Sedimentary Research,64(1b):68-73.
[33] McLennan S M,1989,Rare earth elements in sedientary rocks:influences of provenance and sedimentary processes.Reviews inMineralogy,21:169-200.
[34]李胜荣,高振敏.1995.湘黔地区牛蹄塘组黑色岩系稀土特征—兼论海相热水沉积岩稀土模式.矿物学报,15(2):225-229.
[35]赵红格,刘池洋. 2003.物源分析方法及研究进展.沉积学报,21(3):409-415).
[36] Allegre C J, Minster J F. Quantitative models of trace elementsbehavior inmagmatic processes [J]. Earth and Planetary ScienceLetters, 1978, 38(1): 1-25.
[37]魏怀瑞,杨瑞东,鲍淼,等.贵州寒武世黑色页岩地球化学特征及其意义[J].贵州大学学报(自然科学版),2006(04).
[38]王成善,胡修棉,李祥挥.古海洋溶解氧与缺氧和富氧问题研究[J].海洋地质与第四纪地质, 1999, 19(3): 39-47.
[39]李胜荣.湘黔地区下寒武统黑色岩系金银铂族元素地球化学研究[D].贵阳:中国科学院地球化学研究所博士后论文,1994:1-118.
[40]赵振华.微量元素地球化学原理[M].北京:科学出版社,1997.
[41]陈良友.若尔盖地球碳硅泥岩型铀矿床成矿流体成因和成矿模式研究[D].成都:成都理工大学,2008
[42]沈保丰,翟安民,陈文明,等.中国前寒武纪成矿作用[M].北京:地质出版社, 2006.1-362
[43]王旺章等,用地球化学特征判别川北含铀砂岩,成都理工学院学报,1994第2期31-35
[2]内蒙古自治区地层表编写组.华北地区区域地层表,内蒙古分册[M].地质出版社,1978.
[3]王楫等.狼山-白云鄂博裂谷系[M].北京市:北京大学出版社, 1992.01.1-123.
[4]王楫等.内蒙古渣尔泰山群与白云鄂博群时代对比及含矿性[M].呼和浩特:内蒙古人民出版社,1989.5-140.
[5]董申保.中国变质作用及其地壳演化的关系[M].北京:地质出版社,1986.233—234.
[6]张选阳译编,1989,层序底层学与海平面变化.据The Special Issue-The GSGP Project on Cretaceous Resources, Events and Rhythms(CRER).岩相古地理,1期,第1-10页.
[7]谭琳,朱绅玉,周盛德,等.内蒙古渣尔泰山群岩相古地理[M] .北京:地质出版社,1991. 1—126.
[8]乔秀夫,姚培毅,王成述,等.内蒙古渣尔泰山群层序地层学及构造环境[J].地质学报, 1991,65(1): 1—14.
[9]王思源,杨海明.狼山造山带喷溢成矿研究[M].武汉:中国地质大学出版社,1993.
[10]芮宗瑶,等.华北陆块北缘及邻区有色金属矿床地质[M].北京:地质出版社,1994,121-126.
[11]施林道,谢贤俊,巩正基.狼山-渣尔泰山中元古代裂陷槽有色金属矿床[A].见:芮宗瑶,施林道,方如恒,等编.华北陆块北缘及邻区有色金属矿床地质[C].北京:地质出版社.1994.121-126.
[12]黄占起,沈存利,王守光.内蒙古狼山—渣尔泰山地区与黑色岩系有关的铂族元素矿床找矿前景[J].地质通报,2002,21(10).
[13]沈存利,王守光,苏新旭,等.内蒙古中元古界渣尔泰山群区域成矿地质特征研究[J].地学前缘,2004,11(1).
[14]李永明,陈安平等.内蒙古固阳地区铀矿普查地质报告[R].核工业二○八大队.内部资料.1984.
[15]张日辉,李承厚等.固阳县康兔沟601地段地质工作总结报告[R].核工业二○八大队.内部资料.1985.
[16]内蒙古自治区地质矿产局.内蒙古自治区区域地质志[M].北京:地质出版社,1991.
[17]内蒙古自治区地质矿产局.内蒙古自治区岩石地层[M].中国地质大学出版社,1996.
[18]黄午兴.狼山地区元古代多金属硫化物矿床成矿特征探讨[D].成都:成都理工大学,2009.
[19]涂光炽等.低温地球化学[M].北京市:科学出版社, 1998.
[20]戴塔根,刘汉元.微量元素地球化学及应用[M].长沙:中南工业大学出版社, 1992:3.
[21]刘云. 1998.皖南晚震旦世硅质岩的成因研究.地层学杂志,22(2):154-160.
[22]王中刚,于学元,赵振华.稀土元素地球化学[M].北京:科学出版社, 1989:1-278.
[23]赵红格,刘池洋.2003.物源分析方法及研究进展.沉积学报,21(3):409-415.
[24]韩吟文,马振东.地球化学[M].北京:地质出版社,2003:189-202.
[25]王益友,郭文莹,张国栋.几种地化标志在金湖凹陷阜宁群沉积环境中的应用[J].同济大学学报, 1979, 7(2): 51-60.
[26]吴朝东,陈其英.1999.湘西磷块岩的岩石地球化学特征及成因.地质科学,34(2):213-222.
[27] Steiner M, Wallis E, Erdtmann B-D, et al. 2001. Submarine-hydrothermal exhalative ore layers in black shales from SouthChina and associated fossils—insights into a Lower Cambrianfacies and bio-evolution. Palaeogeography, Palaeoclimatology,Palaeoecology,169: 165-191.
[28] Hatch JR, Leventhal JS. Relationship between inferred redoxpo-tential of the depositional environment and geochemistry of theUp- perPennsylvanian(Missourian)Stark ShaleMember of the DennisLimestone, Wabaunsee County, Kansas, U·S·A. [J]. ChemicalGeology, 1992, 99: 65-82.
[29] JaiH C, Yu H. Geochemistry and depositional environmentofMnoxide deposits in the Tokoro Belt, northeastern Hokkaido, Japan[J]. EconomicGeology, 1992, 87(5):1265-1274
[30]杨剑等,2004.黔北黑色岩系的岩石化学特地球征和成因.矿物学报,24(3).
[31]翟裕生,邓军,汤中立,等.古陆边缘成矿系统[M].北京市:地质出版社,2002.
[32] Girty G H,Hanson A D,Knaack C,Johnson D,1994,Provenancedetermined by REE, Th and Sc analyses of metasedimentaryrock,Boyden Cave Pendant,central Sierra Nevada,California.Journal of Sedimentary Research,64(1b):68-73.
[33] McLennan S M,1989,Rare earth elements in sedientary rocks:influences of provenance and sedimentary processes.Reviews inMineralogy,21:169-200.
[34]李胜荣,高振敏.1995.湘黔地区牛蹄塘组黑色岩系稀土特征—兼论海相热水沉积岩稀土模式.矿物学报,15(2):225-229.
[35]赵红格,刘池洋. 2003.物源分析方法及研究进展.沉积学报,21(3):409-415).
[36] Allegre C J, Minster J F. Quantitative models of trace elementsbehavior inmagmatic processes [J]. Earth and Planetary ScienceLetters, 1978, 38(1): 1-25.
[37]魏怀瑞,杨瑞东,鲍淼,等.贵州寒武世黑色页岩地球化学特征及其意义[J].贵州大学学报(自然科学版),2006(04).
[38]王成善,胡修棉,李祥挥.古海洋溶解氧与缺氧和富氧问题研究[J].海洋地质与第四纪地质, 1999, 19(3): 39-47.
[39]李胜荣.湘黔地区下寒武统黑色岩系金银铂族元素地球化学研究[D].贵阳:中国科学院地球化学研究所博士后论文,1994:1-118.
[40]赵振华.微量元素地球化学原理[M].北京:科学出版社,1997.
[41]陈良友.若尔盖地球碳硅泥岩型铀矿床成矿流体成因和成矿模式研究[D].成都:成都理工大学,2008
[42]沈保丰,翟安民,陈文明,等.中国前寒武纪成矿作用[M].北京:地质出版社, 2006.1-362
[43]王旺章等,用地球化学特征判别川北含铀砂岩,成都理工学院学报,1994第2期31-35