黔东凯里—三都断裂结构及形成演化
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摘要
通过宏观描述、地震解译、有限应变测量、显微构造分析及包裹体测温等方法对黔东凯里-三都断裂进行了研究。认为凯里-三都断裂是黔东南推覆体的前锋断裂,呈向NWW突出的弧形,总体表现为由数条断层组成的逆冲断裂带,主断裂倾向SEE,为黔南拗陷和雪峰古陆的分界线。断裂带以浅层脆性变形为主,断裂带上盘向NWW推覆的水平位移达12～15km,是多条断层多期挤压、拉张和平移剪切作用叠加的结果。断裂带经历了多期演化过程,燕山期以来的演化历史主要受太平洋构造域控制,早中燕山期为主挤压逆冲阶段、晚燕山期为拉张正滑阶段、喜马拉雅期为再次挤压-定型阶段。
The Kaili-Sandu fault is the forward fracture of the thrust nappe in Southeast Guizhou.It shows an arcuate thrust-belt bulging to NWW and consists of several faults.The main fault of the Kaili-Sandu fault belt dips to SEE and separates the South Guizhou depression from the Xuefengshan uplift and is characterized by the brittle deformation.The horizontal displacement of the hanging wall of the Kaili-Sandu fault thrusting to NWW is about 12~15 km.This is the result of numerous faults' multi-stage compression,extension and strike slip shearing movements.The Kaili-Sandu fault belt has undergone multi-tectonic movement,mainly controlled by the Pacific tectonic domain since Yanshanian.Early and middle Yanshanians are the main compression and thrusting stages,late Yanshanian is the extension and slipping stage,and Himalayan is the compression and final structure-shaping stage.
The Kaili-Sandu fault is the forward fracture of the thrust nappe in Southeast Guizhou.It shows an arcuate thrust-belt bulging to NWW and consists of several faults.The main fault of the Kaili-Sandu fault belt dips to SEE and separates the South Guizhou depression from the Xuefengshan uplift and is characterized by the brittle deformation.The horizontal displacement of the hanging wall of the Kaili-Sandu fault thrusting to NWW is about 12~15 km.This is the result of numerous faults' multi-stage compression,extension and strike slip shearing movements.The Kaili-Sandu fault belt has undergone multi-tectonic movement,mainly controlled by the Pacific tectonic domain since Yanshanian.Early and middle Yanshanians are the main compression and thrusting stages,late Yanshanian is the extension and slipping stage,and Himalayan is the compression and final structure-shaping stage.
引文
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[2]丁道桂,郭彤楼,刘运黎,等.对江南-雪峰带构造属性的讨论[J].地质通报,2007,26(7):801-809.
[3]刘洪磊.黔东南推覆构造之认识[J].贵州地质,1990,7(3):271-279.
[4]崔敏,汤良杰,郭彤楼,等.黔东南地区褶皱构造样式及其断层突破模式[J].地球科学:中国地质大学学报,2009,34(6):907-913.
[5]刘丽萍,李三忠,戴黎明,等.雪峰山西侧贵州地区中生代构造特征及其演化[J].地质科学,2010,45(1):228-242.
[6]丘元禧.从梵净山“飞来峰”到兰田构造窗对江南-雪峰推(滑)体的若干认识[J].安徽地质,1994,4(增刊1):23-26.
[7]朱夏.试论古全球构造与古生代油气盆地[J].石油与天然气地质,1983,4(1):1-29.
[8]丘元禧,张渝昌,马文璞.雪峰山陆内造山带的构造特征与演化[J].高校地质学报,1998,4(4):432-443.
[9]王文楷,侯明才,林良彪,等.黔南拗陷独山上司组储层特征及主控因素[J].成都理工大学学报:自然科学版,2011,38(2):229-235.
[10]杨坤光,刘强,刘育燕,等.大别山双河同构造花岗岩体显微构造与磁组构研究[J].中国科学:D辑,2003,33(11):1050-1056.
[11]Ferrill D A,Morris A P,Evans M A,et al.Calcitetwin morphology a low temperature deformationgeothermometry[J].Journal of Structural Geology,2004,26:1521-1569.
[12]Weber J C,Ferrill D A.Calcite and quarts micro-structure geothermometry of low grade metasedi-mentary rocks northern range Trinidad[J].Journalof Structural Geology,2001,23:93-112.
[13]吴堑虹.国外断裂研究中包裹体测温技术的某些应用[J].地质科技情报,1999,18(1):19-23.
[14]Newton R C.Fluid and shear zones in the deep crust[J].Tectonophysics,1990,182:22-37.
[15]万天丰,朱鸿.中国大陆及邻区中生代—新生代大地构造与环境变迁[J].现代地质,2002,16(2):108-121.
[16]杨坤光,梁兴中,谢建磊,等.ESR定年:一种确定脆性断层活动年龄的方法原理与应用[J].地球科学进展,2006,21(4):430-435.
[17]徐政语,姚根顺,郭庆新,等.黔南坳陷构造变形特征及其成因解析[J].大地构造与成矿学,2010,34(1):20-31.
[18]朱光,刘国生,宋传中,等.郯庐断裂带的脉动式伸展活动[J].高校地质学报,2000,6(3):396-404.
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