东昆仑印支期中酸性岩浆岩特征及构造背景
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摘要
东昆仑地区出露大面积多期次的岩浆岩体,构成一条巨大的岩浆岩带。通过对东昆仑近年来获得的印支期中酸性岩浆岩锆石U-Pb及部分39Ar-40Ar测年结果的分析,东昆仑印支期岩浆岩可以分为早期和晚期2个形成阶段。早期中酸性岩浆岩形成于260-230Ma左右,岩性主要为英云闪长岩、花岗闪长岩和二长花岗岩;晚期中酸性岩浆岩形成于230-195Ma左右,岩性主要正长花岗岩和二长花岗岩。这些广泛分布的中酸性岩浆岩表明东昆仑地区在印支期经历了复杂的岩浆和构造作用过程,早期岩浆岩的形成与东昆仑洋壳大规模俯冲碰撞有关,晚期岩浆岩的形成与东昆仑碰撞后的伸展作用有关。
A large area of multi- stage magmatic rocks constitute a huge magmatic belt in the Eastern Kunlun. A summary of the recently obtained zircon U- Pb or39Ar-40Ar ages of Indo- Chinese epoch intermediate- acidic magmatic rocks in Eastern Kunlun indicates that two stages of magmatism, including early stage(260- 230Ma) and later stage(230- 195Ma).The main components of the early stage are tonalite, granodiorite and adamellite. Rocks from the late stage are composed mainly of syenogranite and adamellite. The wide distribution of the intermediate- acidic magmatic rocks indicates a very complex tectonomagmatic history of the Eastern Kunlun during the Indo- Chinese epoch. The early stage rocks are probably related to massive subduction of oceanic crust collide in the Eastern Kunlun. The formation of later stage rocks might have resulted from post- collisional/post- orogenic lithospheric extension after collision.
A large area of multi- stage magmatic rocks constitute a huge magmatic belt in the Eastern Kunlun. A summary of the recently obtained zircon U- Pb or39Ar-40Ar ages of Indo- Chinese epoch intermediate- acidic magmatic rocks in Eastern Kunlun indicates that two stages of magmatism, including early stage(260- 230Ma) and later stage(230- 195Ma).The main components of the early stage are tonalite, granodiorite and adamellite. Rocks from the late stage are composed mainly of syenogranite and adamellite. The wide distribution of the intermediate- acidic magmatic rocks indicates a very complex tectonomagmatic history of the Eastern Kunlun during the Indo- Chinese epoch. The early stage rocks are probably related to massive subduction of oceanic crust collide in the Eastern Kunlun. The formation of later stage rocks might have resulted from post- collisional/post- orogenic lithospheric extension after collision.
引文
[1]姜春发,杨靖绥,冯秉贵,等.昆仑开合构造[M].北京:地质出版社,1992,1-224
[2]张德全,丰成友,李大新,等.柴北缘——东昆仑地区的造山型金矿床[J].矿床地质,2001,20(2):137-146
[3]殷鸿福,张克信.东昆仑造山带的一些特点[J].地球科学——中国地质大学学报,1997,22(4):339-342
[4]郭晓东,张玉杰,刘桂阁,等.东昆仑地区金铜等成矿规律及找矿方向[J].黄金地质,2004,10(4):16-22
[5]莫宣学,罗照华,邓晋福,等.东昆仑造山带花岗岩及地壳生长[J].高校地质学报,2007,13(3):403-414
[6]郭正府,邓晋福,许志琴,等.青藏东昆仑晚古生代末——中生代中酸性火成岩与陆内造山过程[J].现代地质,1998,12(3):344-352.
[7]古凤宝,吴向农,姜常义.东昆仑华力西——印支期花岗岩组合及构造环境[J].青海地质,1996,18-36.
[8]袁万明,莫宣学,喻学惠,等.东昆仑印支期区域构造背景的花岗岩记录[J].地质论评,2000,46(2):203-211.
[9]张雪亭.青海省大地构造格架研究[M].北京:地质出版社,2007:52-98
[10]奎明娟,柏红喜,古凤宝,等.东昆仑构造岩浆带的划分及晚华力西期——燕山期岩石构造组合[J].青海大学学报(自然科学版),2010,28(5):49-55.
[11]刘建楠,丰成友,亓锋,等.青海都兰县下得波利铜钼矿区锆石U-Pb测年及流体包裹体研究[J].岩石学报,2012,28(2),679-690
[12]宋忠宝,张雨莲,陈向阳,等.东昆仑哈日扎含矿花岗闪长斑岩LA-ICP-MS锆石U-Pb定年及地质意义[J].矿床地质,2013,32(1):157-168
[13]奚仁刚,校培喜,伍跃中,等.东昆仑肯德可克铁矿区二长花岗岩组成、年龄及地质意义[J].西北地质,2010,43(4):195-202
[14]丰成友,王雪萍,舒晓峰,等.青海祁漫塔格虎头崖铅锌多金属矿区年代学研究及地质意义[J].吉林大学学报(地球科学版),2011,41(6):1806-1817.
[15]孙雨,裴先治,丁仨平,等.东昆仑哈拉尕吐岩浆混合花岗岩:来自锆石U-Pb年代学的证据[J].地质学报,2009,83(7):1000-2010.
[16]王松,丰成友,李世金,等.青海祁漫塔格卡尔却卡铜多金属矿区花岗闪长岩锆石SHRIMP U-Pb测年及其地质意义[J].中国地质,2009,36(2):74-83
[17]刘成东,莫宣学,罗照华,等.东昆仑壳-幔岩浆混合作用:来自锆石SHRIMP年代学的证据[J].科学通报,2004,49(6):596-602
[18]李世金,孙丰月,丰成友,等.青海东昆仑鸭子沟多金属矿的成矿年代学研究[J].地质学报,2008,82(7):949-955
[19]Liu C D,Mo X X,Luo Z H,et al.2004.Mixing events between the crust-and mantle-derived magmas in Eastern Kunlun:Evidence fromzircon SHRIMPⅡchronology[J].Chinese Science Bulletin,49:823-834.
[20]丰成友,王松,李国臣,等.青海祁漫塔格中晚三叠世花岗岩:年代学、地球化学及成矿意义[J].岩石学报,2012,28(2):665-678
[21]常有英,李建放,张军,等.青海那陵郭勒河东晚三叠世侵入岩形成环境及年代学研究[J].西北地质,2009,42(1):57-59
[22]刘云华,莫宣学,喻学惠,等.东昆仑野马泉地区景忍花岗岩锆石SHRIMP U-Pb定年及其地质意义[J].岩石学报,2006,22(10):2457-2463
[23]佘宏全,张德全,景向阳,等.青海省乌兰乌珠尔斑岩铜矿床地质特征与成因[J].中国地质,2007,34(2):306-314
[24]刘成东,周肃,莫宣学,等.东昆仑造山带后碰撞花岗岩岩石学地球化学和39Ar-40Ar同位素年代学约束[J].华东地质学院学报,2003,26(4):301-305
[25]朱云海,朱耀生,林启祥,等.东昆仑造山带海德乌拉一带早侏罗世火山岩特征及其构造意义[J].地球科学—中国地质大学学报,2003,28(6):653-659
[26]许荣华,Harris N B W,Lewis C L.等.拉萨至格尔木的同位素地球化学.见:中英青藏高原综合地质考察队.青藏高原地质演化[M].北京:科学出版社,1990,282-302
[2]张德全,丰成友,李大新,等.柴北缘——东昆仑地区的造山型金矿床[J].矿床地质,2001,20(2):137-146
[3]殷鸿福,张克信.东昆仑造山带的一些特点[J].地球科学——中国地质大学学报,1997,22(4):339-342
[4]郭晓东,张玉杰,刘桂阁,等.东昆仑地区金铜等成矿规律及找矿方向[J].黄金地质,2004,10(4):16-22
[5]莫宣学,罗照华,邓晋福,等.东昆仑造山带花岗岩及地壳生长[J].高校地质学报,2007,13(3):403-414
[6]郭正府,邓晋福,许志琴,等.青藏东昆仑晚古生代末——中生代中酸性火成岩与陆内造山过程[J].现代地质,1998,12(3):344-352.
[7]古凤宝,吴向农,姜常义.东昆仑华力西——印支期花岗岩组合及构造环境[J].青海地质,1996,18-36.
[8]袁万明,莫宣学,喻学惠,等.东昆仑印支期区域构造背景的花岗岩记录[J].地质论评,2000,46(2):203-211.
[9]张雪亭.青海省大地构造格架研究[M].北京:地质出版社,2007:52-98
[10]奎明娟,柏红喜,古凤宝,等.东昆仑构造岩浆带的划分及晚华力西期——燕山期岩石构造组合[J].青海大学学报(自然科学版),2010,28(5):49-55.
[11]刘建楠,丰成友,亓锋,等.青海都兰县下得波利铜钼矿区锆石U-Pb测年及流体包裹体研究[J].岩石学报,2012,28(2),679-690
[12]宋忠宝,张雨莲,陈向阳,等.东昆仑哈日扎含矿花岗闪长斑岩LA-ICP-MS锆石U-Pb定年及地质意义[J].矿床地质,2013,32(1):157-168
[13]奚仁刚,校培喜,伍跃中,等.东昆仑肯德可克铁矿区二长花岗岩组成、年龄及地质意义[J].西北地质,2010,43(4):195-202
[14]丰成友,王雪萍,舒晓峰,等.青海祁漫塔格虎头崖铅锌多金属矿区年代学研究及地质意义[J].吉林大学学报(地球科学版),2011,41(6):1806-1817.
[15]孙雨,裴先治,丁仨平,等.东昆仑哈拉尕吐岩浆混合花岗岩:来自锆石U-Pb年代学的证据[J].地质学报,2009,83(7):1000-2010.
[16]王松,丰成友,李世金,等.青海祁漫塔格卡尔却卡铜多金属矿区花岗闪长岩锆石SHRIMP U-Pb测年及其地质意义[J].中国地质,2009,36(2):74-83
[17]刘成东,莫宣学,罗照华,等.东昆仑壳-幔岩浆混合作用:来自锆石SHRIMP年代学的证据[J].科学通报,2004,49(6):596-602
[18]李世金,孙丰月,丰成友,等.青海东昆仑鸭子沟多金属矿的成矿年代学研究[J].地质学报,2008,82(7):949-955
[19]Liu C D,Mo X X,Luo Z H,et al.2004.Mixing events between the crust-and mantle-derived magmas in Eastern Kunlun:Evidence fromzircon SHRIMPⅡchronology[J].Chinese Science Bulletin,49:823-834.
[20]丰成友,王松,李国臣,等.青海祁漫塔格中晚三叠世花岗岩:年代学、地球化学及成矿意义[J].岩石学报,2012,28(2):665-678
[21]常有英,李建放,张军,等.青海那陵郭勒河东晚三叠世侵入岩形成环境及年代学研究[J].西北地质,2009,42(1):57-59
[22]刘云华,莫宣学,喻学惠,等.东昆仑野马泉地区景忍花岗岩锆石SHRIMP U-Pb定年及其地质意义[J].岩石学报,2006,22(10):2457-2463
[23]佘宏全,张德全,景向阳,等.青海省乌兰乌珠尔斑岩铜矿床地质特征与成因[J].中国地质,2007,34(2):306-314
[24]刘成东,周肃,莫宣学,等.东昆仑造山带后碰撞花岗岩岩石学地球化学和39Ar-40Ar同位素年代学约束[J].华东地质学院学报,2003,26(4):301-305
[25]朱云海,朱耀生,林启祥,等.东昆仑造山带海德乌拉一带早侏罗世火山岩特征及其构造意义[J].地球科学—中国地质大学学报,2003,28(6):653-659
[26]许荣华,Harris N B W,Lewis C L.等.拉萨至格尔木的同位素地球化学.见:中英青藏高原综合地质考察队.青藏高原地质演化[M].北京:科学出版社,1990,282-302