新疆和布克赛尔县白杨河铀—铍矿床成因研究
|
摘要
白杨河铀铍矿床位于新疆西北部,属新疆雪米斯坦火心岩带的一部分,是新疆铀铍矿勘探生产的主要基地之一。本文在细致的野外地质工作基础上,对矿石进行了系统的显微鉴定,还通过稀土元素、流体包裹体、同位素地球化学(C、O、S)对比分析研究,从而对白杨河铀铍矿床的成矿作用及其成因进行了探讨。论文取得如下认识：
1晚古生代,本区处于由造山挤压环境向拉张环境转换时期。在区域拉张环境下,深大断裂控制了区域花岗岩、次火山岩的产出,从而具备了形成西准北部火山岩型铀矿化的有利构造环境。
2.花岗斑岩的稀土含量较高,轻稀土较重稀土富集,且具明显的负铕异常,表明其物质来源为壳源型。
3.白杨河花岗斑岩的成矿元素U、Be丰度值很高,为成矿提供物质基础。
4.本区铀铍矿主要发育于花岗斑岩与地层的内外接触带上,这种沿接触带发育的矿体表明与岩浆热液成矿作用有关。
5.本区萤石有四种颜色(紫黑、紫色、绿色、无色),但含铍较高的萤石主要为紫黑色和紫色(浅紫色)萤石；且萤石中包体主要分为两期,一期表现为成群分布,包体较小,经测试结果表明为低温极低盐度,另一期表现为孤立分布,包体直径较大,测试结果呈现中温低盐。表明成矿作用至少有两期以上。
6.白杨河铀铍矿床成因是：深部地壳重熔产生的岩浆沿断裂上侵,大量深部的成矿元素带到地壳浅部,形成了U、Be丰度值较高的花岗斑岩,地下深源的热流体上升运移时,活化了花岗斑岩中的成矿物质,这些富含成矿元素的热液在中低温条件下,运移到沿接触带发育的构造裂隙中时,成矿元素在发生沉淀,后期的低温热液对已形成的矿体进行了多次叠加改造,最终形成此类中低温热液型矿床。
Baiyanghe uranium-beryllium deposit is located in northwestern Xinjiang,it is one of the main base of exploration and production of uranium-beryllium ore of volcanic rock belt of Xuemistan in Xinjiang. Detailed studies on the regional geology and the local geology of the deposit have been carried out in this study,systematic microscopic observation of the ores,the contents of trace elements,rare earth elements and the C,O,S isotopic compositions of the ores have been analyzed.Based on these data,discus on metallogeny and genesis of Baiyanghe uranium-beryllium deposit.Finally, Papers obtained by the knowledge:
1.Neopaleozoic, this area was in the time of orogenic crumpling to extensional. In the Environment of regional tension, geofracture control the granite and subvolcanic rocks, With the formation of the West Junggar area volcanic-type uranium-beryllium mineralization potential favorable structural environment.
2. High content of rare earth in granite porphyry,LREE was enrich than HREE, and has a strong negative Eu anomaly, show that the crustal source of the material type.
3.Granite porphyry's trace elements of Be,U abundance value was very high, to provide source for metallogenic.
4.Uranium-beryllium deposit growing in contact zone that between granite porphyry with stratigraphic,it is suggested that metallogenic have to do with hydrothermalism.
5.Fluorite have different four color in this deposit, and the rare earth element have different four distribution pattern,but fluorite with high beryllium is purple-black and purple; Inclusions in fluorite are divided into two,one is show groups distribution, small,the test results reveal low salt and low temperature;and another is show Isolated distribution,big, the test results reveal low salt and medium temperature. Above these two aspects point the mineralization is multiple phases.
6. Genesis of the Baiyanghe uranium-beryllium deposit:Remelting of the crust produced by the intrusion of magma along the fault. Forming a large number of elements deep into the shallow crust and Formation of U, Be a high abundance of granite porphyry.Activation of the granite porphyry's Mineralization when deep underground source of hot fluid migration increased, these are rich in ore-forming elements in the low temperature hydrothermal, migrated along the contact zone when the development of fissures in the ore-forming elements in the precipitation,late the formation of epithermal ore have been conducted a number of superimposed. The final, formation of such low temperature hydrothermal deposits.
1晚古生代,本区处于由造山挤压环境向拉张环境转换时期。在区域拉张环境下,深大断裂控制了区域花岗岩、次火山岩的产出,从而具备了形成西准北部火山岩型铀矿化的有利构造环境。
2.花岗斑岩的稀土含量较高,轻稀土较重稀土富集,且具明显的负铕异常,表明其物质来源为壳源型。
3.白杨河花岗斑岩的成矿元素U、Be丰度值很高,为成矿提供物质基础。
4.本区铀铍矿主要发育于花岗斑岩与地层的内外接触带上,这种沿接触带发育的矿体表明与岩浆热液成矿作用有关。
5.本区萤石有四种颜色(紫黑、紫色、绿色、无色),但含铍较高的萤石主要为紫黑色和紫色(浅紫色)萤石；且萤石中包体主要分为两期,一期表现为成群分布,包体较小,经测试结果表明为低温极低盐度,另一期表现为孤立分布,包体直径较大,测试结果呈现中温低盐。表明成矿作用至少有两期以上。
6.白杨河铀铍矿床成因是：深部地壳重熔产生的岩浆沿断裂上侵,大量深部的成矿元素带到地壳浅部,形成了U、Be丰度值较高的花岗斑岩,地下深源的热流体上升运移时,活化了花岗斑岩中的成矿物质,这些富含成矿元素的热液在中低温条件下,运移到沿接触带发育的构造裂隙中时,成矿元素在发生沉淀,后期的低温热液对已形成的矿体进行了多次叠加改造,最终形成此类中低温热液型矿床。
Baiyanghe uranium-beryllium deposit is located in northwestern Xinjiang,it is one of the main base of exploration and production of uranium-beryllium ore of volcanic rock belt of Xuemistan in Xinjiang. Detailed studies on the regional geology and the local geology of the deposit have been carried out in this study,systematic microscopic observation of the ores,the contents of trace elements,rare earth elements and the C,O,S isotopic compositions of the ores have been analyzed.Based on these data,discus on metallogeny and genesis of Baiyanghe uranium-beryllium deposit.Finally, Papers obtained by the knowledge:
1.Neopaleozoic, this area was in the time of orogenic crumpling to extensional. In the Environment of regional tension, geofracture control the granite and subvolcanic rocks, With the formation of the West Junggar area volcanic-type uranium-beryllium mineralization potential favorable structural environment.
2. High content of rare earth in granite porphyry,LREE was enrich than HREE, and has a strong negative Eu anomaly, show that the crustal source of the material type.
3.Granite porphyry's trace elements of Be,U abundance value was very high, to provide source for metallogenic.
4.Uranium-beryllium deposit growing in contact zone that between granite porphyry with stratigraphic,it is suggested that metallogenic have to do with hydrothermalism.
5.Fluorite have different four color in this deposit, and the rare earth element have different four distribution pattern,but fluorite with high beryllium is purple-black and purple; Inclusions in fluorite are divided into two,one is show groups distribution, small,the test results reveal low salt and low temperature;and another is show Isolated distribution,big, the test results reveal low salt and medium temperature. Above these two aspects point the mineralization is multiple phases.
6. Genesis of the Baiyanghe uranium-beryllium deposit:Remelting of the crust produced by the intrusion of magma along the fault. Forming a large number of elements deep into the shallow crust and Formation of U, Be a high abundance of granite porphyry.Activation of the granite porphyry's Mineralization when deep underground source of hot fluid migration increased, these are rich in ore-forming elements in the low temperature hydrothermal, migrated along the contact zone when the development of fissures in the ore-forming elements in the precipitation,late the formation of epithermal ore have been conducted a number of superimposed. The final, formation of such low temperature hydrothermal deposits.
引文
[1]H.W.利特尔著.铀矿勘探地质[M].王木清译.北京：原子能出版社,1978：20-40.
[2]李妩巍.热液型铀矿床可能的铀源——以俄罗斯斯特列措夫铀矿田为例[J].世界核地质科学,2007,24(2)：68-72.
[3]于宝山,田万文,等.内蒙古喇叭地铀矿点成矿特征及成矿类型讨论[J].世界核地质科学,2009,26(1)：1-8.
[4]范洪海,凌洪飞,等.相山铀矿田成矿机理研究[J].铀矿地质,2003,19(4)：208-213.
[5]王剑锋.浙西北火山岩型铀矿床的成矿条件及成矿规律研究[J].铀矿地质,1992,8(4)：200-207.
[6]王勇,陈正乐,等.伊犁盆地南部新构造特征及其对砂岩型铀矿的控制作用[J].大地构造与成矿学,2006,30(4)：486-493.
[7]王剑锋.铀地球化学教程[M].北京：原子能出版社,1984：3-6.
[8]张振奋,冼林.华南下庄地区花岗岩型铀矿成矿规律分析[J].西部探矿工程,2007,2：93-94.
[9]王剑锋.浙西北火山岩型铀矿床的成矿条件及成矿规律研究[J].铀矿地质,1992,8(4)：200-207.
[10]向伟东,陈肇博,陈祖伊,等.吐哈盆地西南部层间氧化带型砂岩铀矿成矿条件与成矿规律[J].中国核情报中心,2002,1-12.
[11]陈肇博,谢佑新,等.华东南中生代火山岩中的铀矿床[J].地质学报,1982,3：235-243.
[12]张玲,林德松.我国稀有金属资源现状分析[J].地质与勘探,2004,40(1)：26-30.
[13]Burt,D.M,Sheridan, M.F, Model for the formation of uranium/lithophile element deposits in fluorine-rich volcanic rocks [J].American Association of Petroleum Geologists, Studies in Geology,1981,13:99-109.
[14]Beus, A.A., Geochemistry of beryllium and genetic types of beryllium deposits [J]. San Francisco,1966,401.
[15]特列提·阿不都热合曼.新疆阿尔泰伟晶岩铍锂钽铌矿化特征探讨[J].新疆有色金属,1998,1：1-8.
[16]王建国.新疆阿尔泰哈拉苏钽铌铍矿床地质特征[J].新疆有色金属,2008,3：17-21.
[17]刘玉潭,孙绪德,等.荣成市大疃刘家铍矿地质特征[J].山东国土资源,2006,22(6-7)：85-88.
[18]Chapin, C.E., Wilks, M., and McIntosh, W.C., Space-time patterns of Late Cretaceous to present magmatism in New Mexico [J]. New Mexico Bureau of Geology Minerals Resources,2004,13-40.
[19]陈奋雄,李清海,刘刚,等.新疆和布克赛尔县杨庄地区东段铀—稀有金属矿详查(技术报告)[R].核工业二一六队,2008,7-10.
[20]刘晓文,毛小西,刘庄,等.羟硅铍石型铍矿的工艺矿物学研究[J].矿物学报,2010,增刊：61-63.
[21]朱宝清,冯益民.新疆西准噶尔板块构造及演化[J].新疆地质,1994,12(2)：91-105.
[22]李久庚.新疆某铀铍矿田的赋存状态及铀铍关系[J].矿物岩石地球化学通讯,1991,2：2-4.
[23]王苹.矿石学教程[M].武汉：中国地质大学出版社,2008：121-156.
[24]中国科学院地球化学研究所包裹体实验室.矿物中的包裹体及其在地质上的应用[M].北京：地质出版社,1977：26-36,44-55.
[25]田建吉,胡瑞忠,等.661铀矿床矿石U—-Pb等时线年龄及其成矿构造背景[J].矿床地质,2010,29(3)：452-460.
[26]郑永飞.华南某花岗岩型铀矿床成矿模式研究[J].中国地质科学院南京地质矿产研究所所刊,1986,7(1)：51-60.
[27]朱宝清,冯益民.新疆西准噶尔板块构造及演化[J].新疆地质.1994,12(2)：91-105.
[28]苏玉平,唐红峰.A型花岗岩的微量元素地球化学[J].矿物岩石地球化学通报,2005,24(3)：245-251.
[29]骆庭川.稀土元素地球化学在花岗岩类研究中的意义[J].地质科技情报,1986,5(2)：140-146.
[30]谭运金.两类重熔花岗岩的地质地球化学特征[J].地质地球化学.1980,11：1-13.
[31]杨学明,杨晓勇.花岗质岩石形成过程中稀土元素分馏特征[J].安徽地 质,1998,8(2)：1-7.
[32]B.A.格里年科.硫同位素地球化学[M].赵瑞译.北京：科学出版社,1980：122-128.
[33]杨国华,刘福昶.稳定同位素[M].北京：原子能出版社,1988：86-92,137-155.
[34]赵伦山,张本仁.地球化学[M].北京：地质出版社,1998：199-212.
[35]卢焕章.包裹体地球化学[M].北京：地质出版社,1990：74-115,,182-192.
[36]李宗怀,韩宝福,等.新疆准噶尔地区花岗岩中微粒闪长质包体特征及后碰撞花岗质岩浆起源和演化[J].岩石矿物学杂志,2004,23(3)：214-227.
[2]李妩巍.热液型铀矿床可能的铀源——以俄罗斯斯特列措夫铀矿田为例[J].世界核地质科学,2007,24(2)：68-72.
[3]于宝山,田万文,等.内蒙古喇叭地铀矿点成矿特征及成矿类型讨论[J].世界核地质科学,2009,26(1)：1-8.
[4]范洪海,凌洪飞,等.相山铀矿田成矿机理研究[J].铀矿地质,2003,19(4)：208-213.
[5]王剑锋.浙西北火山岩型铀矿床的成矿条件及成矿规律研究[J].铀矿地质,1992,8(4)：200-207.
[6]王勇,陈正乐,等.伊犁盆地南部新构造特征及其对砂岩型铀矿的控制作用[J].大地构造与成矿学,2006,30(4)：486-493.
[7]王剑锋.铀地球化学教程[M].北京：原子能出版社,1984：3-6.
[8]张振奋,冼林.华南下庄地区花岗岩型铀矿成矿规律分析[J].西部探矿工程,2007,2：93-94.
[9]王剑锋.浙西北火山岩型铀矿床的成矿条件及成矿规律研究[J].铀矿地质,1992,8(4)：200-207.
[10]向伟东,陈肇博,陈祖伊,等.吐哈盆地西南部层间氧化带型砂岩铀矿成矿条件与成矿规律[J].中国核情报中心,2002,1-12.
[11]陈肇博,谢佑新,等.华东南中生代火山岩中的铀矿床[J].地质学报,1982,3：235-243.
[12]张玲,林德松.我国稀有金属资源现状分析[J].地质与勘探,2004,40(1)：26-30.
[13]Burt,D.M,Sheridan, M.F, Model for the formation of uranium/lithophile element deposits in fluorine-rich volcanic rocks [J].American Association of Petroleum Geologists, Studies in Geology,1981,13:99-109.
[14]Beus, A.A., Geochemistry of beryllium and genetic types of beryllium deposits [J]. San Francisco,1966,401.
[15]特列提·阿不都热合曼.新疆阿尔泰伟晶岩铍锂钽铌矿化特征探讨[J].新疆有色金属,1998,1：1-8.
[16]王建国.新疆阿尔泰哈拉苏钽铌铍矿床地质特征[J].新疆有色金属,2008,3：17-21.
[17]刘玉潭,孙绪德,等.荣成市大疃刘家铍矿地质特征[J].山东国土资源,2006,22(6-7)：85-88.
[18]Chapin, C.E., Wilks, M., and McIntosh, W.C., Space-time patterns of Late Cretaceous to present magmatism in New Mexico [J]. New Mexico Bureau of Geology Minerals Resources,2004,13-40.
[19]陈奋雄,李清海,刘刚,等.新疆和布克赛尔县杨庄地区东段铀—稀有金属矿详查(技术报告)[R].核工业二一六队,2008,7-10.
[20]刘晓文,毛小西,刘庄,等.羟硅铍石型铍矿的工艺矿物学研究[J].矿物学报,2010,增刊：61-63.
[21]朱宝清,冯益民.新疆西准噶尔板块构造及演化[J].新疆地质,1994,12(2)：91-105.
[22]李久庚.新疆某铀铍矿田的赋存状态及铀铍关系[J].矿物岩石地球化学通讯,1991,2：2-4.
[23]王苹.矿石学教程[M].武汉：中国地质大学出版社,2008：121-156.
[24]中国科学院地球化学研究所包裹体实验室.矿物中的包裹体及其在地质上的应用[M].北京：地质出版社,1977：26-36,44-55.
[25]田建吉,胡瑞忠,等.661铀矿床矿石U—-Pb等时线年龄及其成矿构造背景[J].矿床地质,2010,29(3)：452-460.
[26]郑永飞.华南某花岗岩型铀矿床成矿模式研究[J].中国地质科学院南京地质矿产研究所所刊,1986,7(1)：51-60.
[27]朱宝清,冯益民.新疆西准噶尔板块构造及演化[J].新疆地质.1994,12(2)：91-105.
[28]苏玉平,唐红峰.A型花岗岩的微量元素地球化学[J].矿物岩石地球化学通报,2005,24(3)：245-251.
[29]骆庭川.稀土元素地球化学在花岗岩类研究中的意义[J].地质科技情报,1986,5(2)：140-146.
[30]谭运金.两类重熔花岗岩的地质地球化学特征[J].地质地球化学.1980,11：1-13.
[31]杨学明,杨晓勇.花岗质岩石形成过程中稀土元素分馏特征[J].安徽地 质,1998,8(2)：1-7.
[32]B.A.格里年科.硫同位素地球化学[M].赵瑞译.北京：科学出版社,1980：122-128.
[33]杨国华,刘福昶.稳定同位素[M].北京：原子能出版社,1988：86-92,137-155.
[34]赵伦山,张本仁.地球化学[M].北京：地质出版社,1998：199-212.
[35]卢焕章.包裹体地球化学[M].北京：地质出版社,1990：74-115,,182-192.
[36]李宗怀,韩宝福,等.新疆准噶尔地区花岗岩中微粒闪长质包体特征及后碰撞花岗质岩浆起源和演化[J].岩石矿物学杂志,2004,23(3)：214-227.