秦岭凤太地区金矿床成矿地质条件与时空分布特征
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摘要
秦岭凤太地区金矿床产于商丹板块对接带和南秦岭边缘海盆区,含金建造为火山碎屑岩和细碎屑(热水)沉积建造,赋矿围岩以绿片岩相细碎屑岩为主。区内的金矿床主成矿年龄为220～170Ma,属晚印支期,主成矿期后叠加燕山期构造热液。空间上金矿带与铅锌矿带呈平行展布,金矿与韧性构造关系密切,显示了构造边界对金矿带的控制,具有继承性特征的脆韧性剪切带为含矿构造,北北东向与近东西向(北西西向)断裂的复合是金矿富集的主要构造特征。
Gold deposits in Fengtai area of Qinling Mountains occur in the butt joint of Shangdan plate and the basin area on the margin of South Qinling Mountains. Gold-bearing formations are pyroclastic rocks and fine clastic(hot water) sedimentary formations. The host rocks are mainly fine clastic rocks of greenschist facies. The main metallogenic age of the gold deposits in this area is 220-170 Ma, which belongs to the Late Indosinian Period. After the main metallogenic period, the structural hydrothermal fluid of the Yanshanian Period was superimposed. Spatially, the gold ore belts are parallel to the lead-zinc ore belt. Gold deposits are closely related to ductile structures, which shows that tectonic boundaries control the gold ore belt. The brittle-ductile shear zone with inherited characteristics is ore-bearing structure. The main structural feature of gold enrichment is the combination of NNE trending and near EW trending(NW trending) faults.
Gold deposits in Fengtai area of Qinling Mountains occur in the butt joint of Shangdan plate and the basin area on the margin of South Qinling Mountains. Gold-bearing formations are pyroclastic rocks and fine clastic(hot water) sedimentary formations. The host rocks are mainly fine clastic rocks of greenschist facies. The main metallogenic age of the gold deposits in this area is 220-170 Ma, which belongs to the Late Indosinian Period. After the main metallogenic period, the structural hydrothermal fluid of the Yanshanian Period was superimposed. Spatially, the gold ore belts are parallel to the lead-zinc ore belt. Gold deposits are closely related to ductile structures, which shows that tectonic boundaries control the gold ore belt. The brittle-ductile shear zone with inherited characteristics is ore-bearing structure. The main structural feature of gold enrichment is the combination of NNE trending and near EW trending(NW trending) faults.
引文
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[4] 方维萱,黄转盈.陕西凤太拉分盆地构造变形样式与动力学及金多金属成矿[J].中国地质,2012,39(5):1211～1228.
[5] 李永军,赵仁夫,李志武,等.西秦岭三叠纪沉积盆地演化[J].中国地质,2003,30(3):268～273.
[6] 杨志华,郭俊峰,苏生瑞,等.秦岭造山带基础地质研究新进展[J].中国地质,2002,29(3):246～255.
[6] 冯建忠,汪东坡,王学明,等.陕西凤县八卦庙超大型金矿床成矿地质特征及成矿作用[J].地质学报,2003,77(3):387～398.
[7] 李宗会,宋晓霞,李根根,等.秦岭成矿带Pb、Zn化探异常与铅锌矿无对应关系的原因[J].地质通报,2012,31(5):794～798 .
[8] 冯建忠,汪东坡,王学明,等.西秦岭三个典型金矿床稳定同位素地球化学特征[J].中国地质,2004,31(1):78～84.
[9] 吴孔运,高利鹏.陕西庞家河金矿成矿地质特征及成矿物质来源研究.中国地质[J].2011,38(3):716～723.
[10] 冯建忠,汪东坡,王学明,等.甘肃礼县李坝大型金矿床成矿地质特征及成因[J].矿床地质,2003,22(3):257～263.
[11] 陕西地矿局第三地质队.陕西省太白县双王金矿床KT8矿体地球化学特征研究报告[R].1988.
[12] 冯建忠,汪东坡,王学明.西秦岭泥盆系Au背景值的确定、元素地球化学特征及其地质意义[J].中国地质,2005,32(1):100～106.
[13] 张岳桥,马寅生、杨农,等.西秦岭地区东昆仑—秦岭断裂系晚新生代左旋走滑历史及向东的扩展[J].地球学报,2005,26(1):1～8.
[14] 陕西省地调院.1∶2 5万“汉中幅、宝鸡幅”区域地质调查报告[R].2004.
[15] 贺永平.陕西省凤(县)太(白)地区金矿成矿地质背景与富集规律研究[D].中国地质大学(北京),2017.