西昆仑山前东段新生代褶皱冲断带构造特征与变形机制
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摘要
本次论文主要利用地震数据,结合地表地质调查和遥感影像解译,并综合钻井、测井数据等资料,分析了塔西南地区和田—柯克亚挤压构造带西段克里阳—甫沙构造的构造特征,并建立了西昆仑山前东段新生代褶皱冲断带的构造框架,进而厘定了和田—柯克亚挤压构造带的变形时间,确定了其变形演化过程和变形机制,并讨论西昆仑山的隆升时间。
克里阳—甫沙构造位于和田—柯克亚挤压构造带西段,东到桑株河,西至甫沙。东部克里阳段由南向北发育柯东构造和合什塔格背斜两排构造,西部甫沙段发育甫东构造、柯克亚背斜和固满背斜三排构造。铁克里克断层是西昆仑山体和塔西南凹陷的盆山分界断层,其下盘发育克里阳—甫沙断层贯穿柯东构造—甫东构造,克里阳—甫沙断层在克里阳段地表卷入侏罗系—上新统形成一条北东延伸的高陡构造带。柯东构造和甫东构造发育基底卷入构造,柯克亚背斜和合什塔格背斜—固满背斜是低幅度挤压背斜,挤压位移量向北东逆冲传递到麻扎塔格构造带。甫东构造向东、向柯东构造尖灭消失,柯克亚背斜向东、向柯东构造汇合克里阳段两排构造和甫沙段三排构造之间是连续渐变的转换,不发育横向走滑断层,柯东构造和柯克亚背斜为侧向生长的硬连接。在中新世中期(安居安组),阿其克(克里阳)构造(是甫沙构造的东端)开始形成；早上新世,柯东构造与柯克亚背斜的隐伏断层同期变形；到晚上新世,柯东构造持续变形,柯克亚背斜开始发育。
西昆仑山前东段新生代褶皱冲断带挤压根带的和田—柯克亚挤压构造带东起和田,西到柯克亚,东西延伸近270Km,其挤压位移量沿古近系底部阿尔塔什组膏泥岩向北向塔里木盆地内滑脱,经过麦盖提斜坡传递到约220Km以外的北端前沿麻扎塔格构造带冲出地表,在地表形成一条北东向延伸的地形凸起。受和田—柯克亚挤压构造带的范围所限,麻扎塔格构造带东侧的玛东构造和西侧的群苦恰克构造、巴什托普构造没有在新近纪发育这套古近系底部膏泥岩作为滑脱层、且由南向北逆冲的挤压构造。西昆仑山前东段新生代褶皱冲断带适用临界锥形楔模型,古近系阿尔塔什组膏泥岩作为底部滑脱层,导致这个锥形楔的顶面坡度α近似水平并与底部滑脱层倾角β拆离。由于受到前陆沉降负载机制以及巴楚隆起的基底隆起影响,褶皱冲断带新生界沉积自身形成一套向盆地方向减薄的楔状体,楔形体内部不需变形调节形态,所以在中部麦盖提斜坡没有明显构造变形发生。
和田南背斜以及克里阳-甫沙构造的生长地层指示和田-柯克亚挤压构造带的变形起始时间是中新世中期。结合西昆仑山前东段新生代褶皱冲断带区域剖面中显示的从中新世开始、向盆地内减薄的沉积楔形体,认为西昆仑山从中新世开始明显隆升。
Using sesmic datas,combing with surface geological survey and remote sensing image、well data,this thesis constructued structural model of Keliyang—Fusha structure and eastern section of the piedmont of West Kunlun,analyzed deformation time of Hetian—Kekeya thrust belt、evolutionary process and deformation mechanism.
Keliyang—Fusha strcture located in western section of Hetian-Kekeya thrust belt,from Sangzhu river to Fusha.Keliyang section in the eastern section of Keliyang—Fusha strcture developed Kedong structure and Heshitage anticline from south to north,but Fusha section in the western section developed Fudong structure,Kekeya anticline and Guman anticline from south to north.Tiekelike fault is boundary fault of West Kunlun mountain and Yecheng—Hetian sag,Keliyang—Fusha fault was through Kedong structure and Fudong structure, it involved steep belt which continued from Jurassic to Pliocene in outcrop at Keliyang section. Kedong structure and Fudong structure were basement involved strctures,but Kekeya anticline、Heshitage anticline、 Guman anticline were low relief anticlines, their displacement transformed to Mazrtagh structure。Fudong structure was pinch—out towards Kedong structure,Kekeya anticline converged with Kedong structure eastwardly.Transverse fault didn't developed between Keliyang section and Fusha section.Kedong structure and Kekeya anticline were lateral growth and converged,they were hard linkage. Aqike(Keliyang) structure (located in western section of Fudong structure) deformed from Miocene;the deformation of Kedong structure and the blind fault below backlimb of Kekeya anticline started at Early Pliocene; at Late Pliocene, Kekeya anticline strated deforming,Kedong structure continued deforming,they developed by break—forward sequence.
Hetian—Kekeya thrust belt located in southern margin of Cenozoic fold and thrust belt in eastern section of the piedmont of West Kunlun, extend about270Km from Hetian to Kekeya. Mazartagh structural belt is leading edge of Hetian—Kekeya structural belt,the Cenozoic compressive deformation of Hetian—Kekeya along the gypsum—mudstone of Aertashi Formation of Paleogene slided to Mazartagh and transformed to Fault—propagation—folds,leaded obvious topographic rise in Tarim basin.Madong structure which located at east and Qunkuqiake structure、 Bashituopu structure which located at west didn't involved this deformation.The taper wedge angle of this fold and thrust belt is less than those active orogenies,it's means the gypsum—mudstone of Aertashi Formation and the shape of Cenozoic deposition are key factors, the gypsum—mudstone controls a of taper wedge,the shapes of basement and depositive wedge control β of taper wedge.
Growth strata of Hetian—Kekeya structural belt deposited from Miocene. So,Hetian—Kekeya structural belt deoformed from Miocene.Combineing with wedge shape sediment of Cenozoic fold and thrust belt in eastern section of the piedmont of West Kunlun,Western Kunlun mountain uplift from Miocene.
克里阳—甫沙构造位于和田—柯克亚挤压构造带西段,东到桑株河,西至甫沙。东部克里阳段由南向北发育柯东构造和合什塔格背斜两排构造,西部甫沙段发育甫东构造、柯克亚背斜和固满背斜三排构造。铁克里克断层是西昆仑山体和塔西南凹陷的盆山分界断层,其下盘发育克里阳—甫沙断层贯穿柯东构造—甫东构造,克里阳—甫沙断层在克里阳段地表卷入侏罗系—上新统形成一条北东延伸的高陡构造带。柯东构造和甫东构造发育基底卷入构造,柯克亚背斜和合什塔格背斜—固满背斜是低幅度挤压背斜,挤压位移量向北东逆冲传递到麻扎塔格构造带。甫东构造向东、向柯东构造尖灭消失,柯克亚背斜向东、向柯东构造汇合克里阳段两排构造和甫沙段三排构造之间是连续渐变的转换,不发育横向走滑断层,柯东构造和柯克亚背斜为侧向生长的硬连接。在中新世中期(安居安组),阿其克(克里阳)构造(是甫沙构造的东端)开始形成；早上新世,柯东构造与柯克亚背斜的隐伏断层同期变形；到晚上新世,柯东构造持续变形,柯克亚背斜开始发育。
西昆仑山前东段新生代褶皱冲断带挤压根带的和田—柯克亚挤压构造带东起和田,西到柯克亚,东西延伸近270Km,其挤压位移量沿古近系底部阿尔塔什组膏泥岩向北向塔里木盆地内滑脱,经过麦盖提斜坡传递到约220Km以外的北端前沿麻扎塔格构造带冲出地表,在地表形成一条北东向延伸的地形凸起。受和田—柯克亚挤压构造带的范围所限,麻扎塔格构造带东侧的玛东构造和西侧的群苦恰克构造、巴什托普构造没有在新近纪发育这套古近系底部膏泥岩作为滑脱层、且由南向北逆冲的挤压构造。西昆仑山前东段新生代褶皱冲断带适用临界锥形楔模型,古近系阿尔塔什组膏泥岩作为底部滑脱层,导致这个锥形楔的顶面坡度α近似水平并与底部滑脱层倾角β拆离。由于受到前陆沉降负载机制以及巴楚隆起的基底隆起影响,褶皱冲断带新生界沉积自身形成一套向盆地方向减薄的楔状体,楔形体内部不需变形调节形态,所以在中部麦盖提斜坡没有明显构造变形发生。
和田南背斜以及克里阳-甫沙构造的生长地层指示和田-柯克亚挤压构造带的变形起始时间是中新世中期。结合西昆仑山前东段新生代褶皱冲断带区域剖面中显示的从中新世开始、向盆地内减薄的沉积楔形体,认为西昆仑山从中新世开始明显隆升。
Using sesmic datas,combing with surface geological survey and remote sensing image、well data,this thesis constructued structural model of Keliyang—Fusha structure and eastern section of the piedmont of West Kunlun,analyzed deformation time of Hetian—Kekeya thrust belt、evolutionary process and deformation mechanism.
Keliyang—Fusha strcture located in western section of Hetian-Kekeya thrust belt,from Sangzhu river to Fusha.Keliyang section in the eastern section of Keliyang—Fusha strcture developed Kedong structure and Heshitage anticline from south to north,but Fusha section in the western section developed Fudong structure,Kekeya anticline and Guman anticline from south to north.Tiekelike fault is boundary fault of West Kunlun mountain and Yecheng—Hetian sag,Keliyang—Fusha fault was through Kedong structure and Fudong structure, it involved steep belt which continued from Jurassic to Pliocene in outcrop at Keliyang section. Kedong structure and Fudong structure were basement involved strctures,but Kekeya anticline、Heshitage anticline、 Guman anticline were low relief anticlines, their displacement transformed to Mazrtagh structure。Fudong structure was pinch—out towards Kedong structure,Kekeya anticline converged with Kedong structure eastwardly.Transverse fault didn't developed between Keliyang section and Fusha section.Kedong structure and Kekeya anticline were lateral growth and converged,they were hard linkage. Aqike(Keliyang) structure (located in western section of Fudong structure) deformed from Miocene;the deformation of Kedong structure and the blind fault below backlimb of Kekeya anticline started at Early Pliocene; at Late Pliocene, Kekeya anticline strated deforming,Kedong structure continued deforming,they developed by break—forward sequence.
Hetian—Kekeya thrust belt located in southern margin of Cenozoic fold and thrust belt in eastern section of the piedmont of West Kunlun, extend about270Km from Hetian to Kekeya. Mazartagh structural belt is leading edge of Hetian—Kekeya structural belt,the Cenozoic compressive deformation of Hetian—Kekeya along the gypsum—mudstone of Aertashi Formation of Paleogene slided to Mazartagh and transformed to Fault—propagation—folds,leaded obvious topographic rise in Tarim basin.Madong structure which located at east and Qunkuqiake structure、 Bashituopu structure which located at west didn't involved this deformation.The taper wedge angle of this fold and thrust belt is less than those active orogenies,it's means the gypsum—mudstone of Aertashi Formation and the shape of Cenozoic deposition are key factors, the gypsum—mudstone controls a of taper wedge,the shapes of basement and depositive wedge control β of taper wedge.
Growth strata of Hetian—Kekeya structural belt deposited from Miocene. So,Hetian—Kekeya structural belt deoformed from Miocene.Combineing with wedge shape sediment of Cenozoic fold and thrust belt in eastern section of the piedmont of West Kunlun,Western Kunlun mountain uplift from Miocene.
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