河西走廊及其邻区活动构造图像及构造变形模式
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摘要
印度板块与欧亚板块的碰撞后,形成了世界最大最高的高原—青藏高原,高原的大幅度隆升造就和改变了整个亚欧大陆的构造格局,同时对亚洲地区的气候和环境也产生了巨大的影响。河西走廊及其邻区是青藏高原北部高原向北扩展的最前缘,也是对高原变形响应最为敏感的地区之一。该地区发育有大量的晚第四纪活动断裂,是通过断裂构造活动习性及构造转换研究高原变形过程的理想区域,同时这一地区也是在青藏高原北部两大主控边界断裂—阿尔金断裂和海原—祁连山断裂带所夹持下的构造转换和构造变形的关键位置。高原边缘主控边界走滑断裂的变形是怎样分布的和如何消失的?变形是如何被吸收转换成不同走向、不同性质构造的?变形是如何迁移到与其平行构造上而不发生衰减的?这些和其他许多有关断裂滑动速率的问题及高原北部断裂的相关问题,对于研究青藏高原北部的构造变形和构造转换具有十分重要的意义。
本论文通过对位于青藏高原北部的河西走廊及其邻区主要断裂滑动速率的精细研究,同时总结前人在该地区的研究成果特别是主控边界断裂上滑动速率的研究成果,获得较为完整的青藏高原北部活动构造几何图像和运动学特征。并以断裂带上滑动速率(位移分布)及构造转换为研究的主要内容,结合现今GPS观测数据,归纳总结了该地区晚新生代以来的构造变形模式,探讨了构造变形的动力学机制以及高原北部地区构造变形与构造隆升的关系。本论文主要取得的认识如下：
合黎山南缘断裂是位于河西走廊盆地北侧的控盆断裂,断裂以挤压逆冲为主要活动方式,合黎山的地貌隆升伴随着断裂的活动。断裂分段与地貌分段有完全的一致性,说明合黎山隆升的主要构造作用方式是断层作用。断裂依据几何结构分为三段,各段断错位移的分布具有明显的弧形分布特征,整个断层的断错位移则显示不对称的东高西低的弧形分布,断层的平均逆冲滑动速率东段(猴儿头段)为(0.34±0.10)mm/a,东段北侧分支(梧桐井段)为(0.14±0.10)mm/a,中段(0.24±0.06)mm/a,西段为(0.18±0.07)mm/a,断裂仅在两端存在局部的左旋位移特征。
沿合黎山南缘断裂探槽开挖、地表破裂带遗迹的考察及历史地震考证结果证实,合黎山南缘断裂上至少发生过三次强地震事件,最早一次是距今约5000年左右的一次强地震事件,形成了全断裂破裂,另外两次该地区有历史记载的地震事件,公元180年表氏71/2级地震形成不少于60公里的地表破裂,而公元756年的高台北7级地震仅在断裂东段发生了地表破裂,破裂长度20～30公里。地震不具备准周期复发的特征,与断裂活动模式相统一的是地震活动均是自东向西发生断裂破裂的和断裂扩展的。
横跨合黎山不同段落的DEM剖面显示了不同地貌单元段的断层作用方式是有差异的,但总体是断层活动促使合黎山地区向河西走廊盆地内掀斜为主要特征。平行于山脉走向的DEM剖面和断裂带上位移(滑动速率)的分布有相同的模式,均为自东向西倾斜,地貌单元的特征也反映了合黎山自东向西逐渐隆起的构造活动特征。断裂位移的分布特征与断裂带上强地震分布与规模确定了断层带上的位移分布是一种特征地震模式与位移变化模式的结合。断裂的构造变形模式和运动特征是以挤压隆升为主,伴随着合黎山及两侧向河西走廊盆地内整体掀斜,其动力来源主要是南侧的青藏高原的挤压和北部阿拉善板块南缘一带的上地壳的缩短弯曲挤出。
河西走廊北侧及内部的一些断层研究结果表明：嘉峪关黑山断裂是晚更新世活动的高角度逆冲断层,其晚更新世以来的逆冲滑动速率为(0.26±0.06)mm/a；金塔南山断裂全新世有活动,断层性质也以逆冲为主,其晚更新世以来的逆冲滑动速率为(0.22±0.05)mm/a；嘉峪关—文殊山断裂是河西走廊盆地内部的一条分隔酒西盆地和酒东盆地的断层,断裂全新世活动具有明显的分段性,现代地貌及构造变形显示了“反向翘起”的构造模式,断裂带上晚第四纪的逆冲滑动速率为(0.30±0.05)mm/a；对于河西走廊北部向东扩展的慕少梁断裂和大车场—阿右旗断裂,其地貌调查和遥感解译结果认为断裂活动主要以自北向南的高角度逆冲为主要运动方式,断裂晚第四纪活动性较弱。
祁连山北缘断裂的断层运动学特征的调查结果显示,佛洞庙—红崖子断裂西段以逆冲为主,东段转变为逆冲兼具左旋走滑的特征,断裂全新世活动明显,局部保留有地震破裂带的遗迹,断裂晚第四纪逆冲滑动速率为(0.41±0.09)mm/a,其东段的左旋走滑速率为(1.20±0.15)mm/a；榆木山北缘断裂断错了全新世早期的地貌面,其断裂西段的晚第四纪逆冲滑动速率为(0.55±0.15)mm/a,左旋走滑速率为(0.95±0.11)mm/a,而对“骆驼城陡坎”的调查结果认为,该地貌特征不是断层陡坎,而是古代水利工程的遗迹,榆木山的构造变形是祁连山向北的扩展过程,其隆升变形为近对称形态的发育和发展过程；古浪断裂的滑动速率补充研究的结果为皇城—双塔断裂全新世逆冲滑动速率为(0.39±0.04)mm/a,而天桥沟—黄羊川断裂全新世以来的左旋走滑速率为(2.66±0.38)mm/a；祁连山西端昌马断裂西段滑动速率的补充测量和估算结果是晚第四纪逆冲滑动速率为(0.14±0.02)mm/a,左旋走滑速率为(1.17±0.04)mm/a,远比前人研究结果的3.3-4.3 mm/a的左旋滑动速率要小的多。
青藏高原北部断裂晚第四纪滑动速率及现今GPS观测揭示了青藏高原向北扩展与高原边缘隆升的运动特征。主要断裂晚第四纪滑动速率及跨断裂GPS应变速率的结果表明,青藏高原北部边缘的断裂以低滑动速率(<10 mm/a)为主,特别是两条边界断裂阿尔金断裂和海原—祁连山断裂。两条主要控边界断裂上的滑动速率沿断裂的分布变化特征显示了断裂间滑动速率转换及调整。阿尔金断裂自95°E以西的8-12 mm/a稳定滑动速率,向东逐渐降低到最东端约为1-2 mm/a,而海原断裂自哈拉湖一带开始发育后滑动速率为1-2 mm/a,到祁连一带(101°E以东)增大到相对稳定的4-5 mm/a,直到过海原后转向六盘山一带,滑动速率降低到1-3 mm/a,甚至更低。滑动速率的变化及分布特征显示,阿尔金断裂的左旋滑动主要是通过祁连山内部隆起及两侧新生代盆地变形引起的缩短来吸收的,海原—祁连山断裂的低滑动速率及沿断裂运动学特征表明断裂尾端的陇西盆地变形及六盘山的隆起是断裂左旋走滑速率的主要吸收方式。
青藏高原北部地区是由北东东向的阿尔金断裂、北西西向的海原—祁连山断裂带及隆起的祁连山区及其北部的河西走廊及阿拉善板块的边缘所组成,主边界断裂的左旋走滑,祁连山北部及边缘断裂的挤压逆冲、河西走廊内部隆起及北部断裂的调节作用是高原边缘活动构造图像的主要特征,这三部分共同构成了高原北部边缘完整的活动构造图像。阿尔金断裂和海原—祁连山断裂之间的转换是通过高原北部边缘隆起山区的逆冲断层来完成的,高原变形的吸收主要是通过控边断层上的走滑速率、过渡转换区逆冲断层的逆冲滑动速率和高原边缘的高海拔来完成,另外是不同块体内部和边缘的主要新生代盆地的褶皱变形也吸收了少部分地壳变形。祁连山内部及边缘的逆冲断层提供了高原边缘近60%的地壳缩短,阿尔金断裂及海原—祁连山断裂控制下的青藏高原北部边缘的构造变形机制,是在三个刚性块体所阻挡下的通过内部旋转或构造性质转换来完成的。河西走廊不同位置构造形态和地貌特征的变化,是青藏高原北部两大块体相互作用过程中,运动方向和动力变化的结果。河西走廊北部山脉地貌形态、断裂构造活动及构造隆升的特征显示了走廊北部的各主要断裂的发育发展可能是相互独立,其形态和扩展方向说明了其构造形成和扩展的趋势和动力方向,各断层有明显的不一致,不是以往所说的自西向东的发育发展过程,河西走廊北部的断裂(特别是中段)是青藏高原挤压作用下地壳缩短作用的结果。
青藏高原北部变形模式及变形机制讨论表明,青藏高原北部边缘的变形是一种分布式的连续变形,变形发生自高原内部,边界断裂的走滑被高原内部变形所吸收。同时,祁连山北缘和内部断裂及河西走廊北部的断裂所表现的逆冲为主的活动性质,对地壳增厚模式所强调的由逆冲断层和地壳增厚及局部高海拔来分解吸收地壳变形的说法是支持的。
Collision between Indian and Eurasian plates not only created Tibetan Plateau, "the roof of the world", but also posed significant impacts on climate and environments of western China and central Asia. Hexi Corridor consists of a series of western northwest-trending Cenozoic basins along range front of the Qilian Shan. Tectonic setting of the Hexi Corridor marks the northern margin of Tibetan Plateau where abundant active faults and historical earthquakes attests significant on-going tectonic deformation due to outward growth of the Tibetan Plateau. Tectonic deformation of the region is dominated by two major strike-slip faults bounding different deforming units, the Altyn Tagh fault and the Haiyuan fault. Other structures with different styles and senses of motion form complex pattern of active tectonic deformation. It is thus an ideal place to study active tectonic deformation to gain understandings of the processes of Tibetan Plateau's northward growth. Key scientific questions regarding tectonic processes associated with outward growth of Tibetan Plateau includes: what is major process governing tectonic deformation of the northern margin of the Tibetan Plateau; what are relationships between strike-slip faulting and crustal shortening; how the slips on strike-slip fault are transferred into crustal shortening in other structures; what are slip rates along major faults in the region. Answers to these and other similar questions bear important implications for understanding tectonic processes associated with the outward growth of the Tibetan Plateau.
Based on systematic studies on the late Quaternary slip rates along major active faults in Hexi Corridor and adjacent regions in northern Tibet, this paper provides an integrated information to show geometric pattern and kinematics features of active tectonic deformation in northern margin of the Tibetan Plateau. In combining active faulting studies with GPS measurements, we also discuss models of the late Cenozoic deformation and its dynamic mechanism of the northern margin of Tibetan Plateau especially the Qilian Shan and Hexi Corridor. Main conclusions are drawn as follows:
The South Heli Shan Fault is the north boundary of the Hexi Corridor basin, and it is typical of transpression feature with predominant reverse faulting and minor left-slip near its ends. The topographic features of the Heli Shan correlate to slips on the fault suggesting active fault controls on mountainous geomorphology. The South Heli Shan Fault can be divided into three segments based on its geometry. Slip of the individual segment is of arch shape distribution, and the slip distribution of the whole fault zone depicts an asymmetric arch shape as eastern side with higher rates and west side with lower rates. Average slip rates are (0.34±0.10)mm/a for the Houertou segment, (0.14±0.10)mm/a for the Wutongjing region, (0.24±0.06)mm/a for central segment, and (0.18±0.07)mm/a for western segment. Left-lateral movements are only observed at local sites near two terminals of the South Heli Shan Fault.
Trenching and field survey along the surface ruptures, together historic earthquake investigation indicate that there might be three strong earthquakes occurred along the South Heli Shan Fault. The first event ruptured along the whole fault about 5000a ago, and the other two occurred during the documented history, in 180 A.D and 756 A.D. respectively. More than 60km long surface ruptures was associated with the M71/2 event in 180 A.D. and 20-30km ruptures might have formed during the M 7 event in 756 A.D. The behavior of paleoearthquake activity does not show quasi-periodic pattern.
Tectonic deformation and kinematics pattern in the northern Hexi Corridor is characterized by thrust fault related uplift with southward movement and westward tilting, that resulted from the outward growth of the Tibet Plateau toward the relative tectonic stable Alashan block. Topographic profiles constructed from DEM perpendicular to the Heli Shan show that different fault segments are associated with different geomorphology. The primary geomorphic feature is the tilting towards Hexi Corridor basin along the fault. Along the strike of Heli Shan mountain, topographic profile shows westward tilting of geomorphology. This kind of east to west tilting corroborates larger displacements in eastern part of the fault and less offset in western part of the fault. Thus, the topographic expression is representative of the activity of the Heli Shan fault. Slip distribution along the fault and strong earthquake activity suggest the recurrent pattern of strong earthquake may be a combination of characteristic and temporal clustering.
Active fault studies in the northern and interior of the Hexi Corridor basin indicate that the Jiayuguan-Heishan fault is a high angle reverse fault with late Pleistocene activity. The slip rate is (0.26±0.06) mm/a since late Pleistocene. The Jinta Nan Shan fault is a Holocene active fault is with a slip rate of (0.22±0.05) mm/a since late Pleistocene. The Jiayuguan-Wenshu Shan fault, a transverse fault obliquely cuts the Hexi Corridor to separate the Jiuquan basin in the east and the Yumen basin in the west. The fault appears to be high-angle reverse fault with hangingwall tilting to the west, and observed slip rate is (0.30±0.05)mm/a. As for the Mushaoliang fault and Dachechang-Ayouqi fault along the north Hexi Corridor, geomorphological pattern and remote sensing interpretation suggest that these faults are of high-angle reverse slipping from north to south.
Kinematics of tectonic deformation along the northern Qilian Shan fault shows that the western segment of the Fodongmiao-Hongaizi fault is a premary reverse fault, and its eastern segment is associated with left-lateral components. This fault presents obvious evidence of Holocene activity, and remnant of surface rupture of historical earthquake can still be found in many places. The slip rate of reverse faulting is (0.41±0.09) mm/a and left lateral slip rate is (1.20±0.15) mm/a. Early Holocene geomorphic surface is offset by the northern Yumu Shan fault with slip rate (0.55±0.15) mm/a of reverse faulting and the left lateral slip rate (0.95±0.11) mm/a. Out investigation show that the so called "Luotuocheng fault scarp " is in fact remnants of ancient irrigation canal rather than an active fault. Tectonic deformation of the Yumu Shan is a consequence of the northward growth of the Qilian Shan, and the symmetric topographic shape of Yumu Shan suggests that slip distribution along the Yumu Shan fault is also symmetric. Additional study on slip rate of the Gulang fault shows that Holocene dip-slip rate of the Huangcheng-Shuangta fault is (0.39±0.04) mm/a and left-slip rate of the Tianqiaogou-Huangyangchuan fault is (2.66±0.38) mm/a. Survey on west segment of the Changma fault near west Qilian Shan indicates that late Quaternary throw rate is (0.14±0.02) mm/a and left lateral slip rate is (1.17±0.04) mm/a, which is much less than previous reported 3.3-4.3mm/a.
GPS measurements and late Quaternary fault slip rates reveal the kinematic pattern of outward growth of the northern margin of the Tibetan Plateau. Base on the geologic data and GPS velocity slip rates of major boundary faults are less than 10 mm/a including the Altyn-Tagh fault and Haiyuan- Qilianshan fault. The distributions of slip rates along the two major faults show constant slip rate along their middle portion and decrease toward their ends. For example, the left-lateral slip rates on the central segment of Altyn-Tagh Fault appear to be in the range of 8-12 mm/a, but decreases eastward to only 1-2 mm/a near 97°E. On the Haiyuan-Qilian Shan fault, slip rates are 1-2 mm/a in its western segment, and increase to 4-5mm/a in its eastern and middle segments, and then decrease to 1-3 mm/a near its eastern end near the Liupan Shan. This kind of slip distribution suggests that almost all motion along a strike-slip fault is accommodated by crustal shortening or convergence near the ends of the strike-slip fault. The crustal shortening across the Qilian Shan absorbs strike-slip along the Altyn Tagh fault. The convergence in Liupan Shan accommodates left-lateral slip along the Qilian-Haiyuan fault.
Northern Tibetan Plateau includes the NNE-teending Altyn Tagh Fault, NWW-striking Haiyuan-Qilian Shan Fault and uplifted Qilian Shan mountain belt, Hexi Corridor basin and Alashan block. Tectonic processes in the region can be described as combination of three structural styles. First, outward growth of the northern Tibetan Plateau cause west northwest trending reverse faulting and folding in the Qilian Shan and Hexi Corridor, and the deformation might have migrated to north of the Hexi Corridor caused reverse faulting and earthquake rupturing in Heli Shan and Longshou Shan. Second, left-lateral strike slip on the main boundary faults (The Altyn Tagh fault and the Qilian-Haiyuan fault) cause reverse faulting, folding and uplifting of mountains to accommodate the lateral motions. And third, internal deformation within the Qilian Shan, Hexi Corridor, and even with the interior of tectonically stable Alashan Block. These three tectonic deformations contribute to outward and upward growth of the northern margin of Tibetan Plateau. Our studies show that tectonic deformation occurred mainly within the northern Tibetan Plateau, and that the rule of strike slip faulting has been reconciling differences of crustal shortening or crustal thickening rather than extruding crustal blocks out of the plateau interior.
本论文通过对位于青藏高原北部的河西走廊及其邻区主要断裂滑动速率的精细研究,同时总结前人在该地区的研究成果特别是主控边界断裂上滑动速率的研究成果,获得较为完整的青藏高原北部活动构造几何图像和运动学特征。并以断裂带上滑动速率(位移分布)及构造转换为研究的主要内容,结合现今GPS观测数据,归纳总结了该地区晚新生代以来的构造变形模式,探讨了构造变形的动力学机制以及高原北部地区构造变形与构造隆升的关系。本论文主要取得的认识如下：
合黎山南缘断裂是位于河西走廊盆地北侧的控盆断裂,断裂以挤压逆冲为主要活动方式,合黎山的地貌隆升伴随着断裂的活动。断裂分段与地貌分段有完全的一致性,说明合黎山隆升的主要构造作用方式是断层作用。断裂依据几何结构分为三段,各段断错位移的分布具有明显的弧形分布特征,整个断层的断错位移则显示不对称的东高西低的弧形分布,断层的平均逆冲滑动速率东段(猴儿头段)为(0.34±0.10)mm/a,东段北侧分支(梧桐井段)为(0.14±0.10)mm/a,中段(0.24±0.06)mm/a,西段为(0.18±0.07)mm/a,断裂仅在两端存在局部的左旋位移特征。
沿合黎山南缘断裂探槽开挖、地表破裂带遗迹的考察及历史地震考证结果证实,合黎山南缘断裂上至少发生过三次强地震事件,最早一次是距今约5000年左右的一次强地震事件,形成了全断裂破裂,另外两次该地区有历史记载的地震事件,公元180年表氏71/2级地震形成不少于60公里的地表破裂,而公元756年的高台北7级地震仅在断裂东段发生了地表破裂,破裂长度20～30公里。地震不具备准周期复发的特征,与断裂活动模式相统一的是地震活动均是自东向西发生断裂破裂的和断裂扩展的。
横跨合黎山不同段落的DEM剖面显示了不同地貌单元段的断层作用方式是有差异的,但总体是断层活动促使合黎山地区向河西走廊盆地内掀斜为主要特征。平行于山脉走向的DEM剖面和断裂带上位移(滑动速率)的分布有相同的模式,均为自东向西倾斜,地貌单元的特征也反映了合黎山自东向西逐渐隆起的构造活动特征。断裂位移的分布特征与断裂带上强地震分布与规模确定了断层带上的位移分布是一种特征地震模式与位移变化模式的结合。断裂的构造变形模式和运动特征是以挤压隆升为主,伴随着合黎山及两侧向河西走廊盆地内整体掀斜,其动力来源主要是南侧的青藏高原的挤压和北部阿拉善板块南缘一带的上地壳的缩短弯曲挤出。
河西走廊北侧及内部的一些断层研究结果表明：嘉峪关黑山断裂是晚更新世活动的高角度逆冲断层,其晚更新世以来的逆冲滑动速率为(0.26±0.06)mm/a；金塔南山断裂全新世有活动,断层性质也以逆冲为主,其晚更新世以来的逆冲滑动速率为(0.22±0.05)mm/a；嘉峪关—文殊山断裂是河西走廊盆地内部的一条分隔酒西盆地和酒东盆地的断层,断裂全新世活动具有明显的分段性,现代地貌及构造变形显示了“反向翘起”的构造模式,断裂带上晚第四纪的逆冲滑动速率为(0.30±0.05)mm/a；对于河西走廊北部向东扩展的慕少梁断裂和大车场—阿右旗断裂,其地貌调查和遥感解译结果认为断裂活动主要以自北向南的高角度逆冲为主要运动方式,断裂晚第四纪活动性较弱。
祁连山北缘断裂的断层运动学特征的调查结果显示,佛洞庙—红崖子断裂西段以逆冲为主,东段转变为逆冲兼具左旋走滑的特征,断裂全新世活动明显,局部保留有地震破裂带的遗迹,断裂晚第四纪逆冲滑动速率为(0.41±0.09)mm/a,其东段的左旋走滑速率为(1.20±0.15)mm/a；榆木山北缘断裂断错了全新世早期的地貌面,其断裂西段的晚第四纪逆冲滑动速率为(0.55±0.15)mm/a,左旋走滑速率为(0.95±0.11)mm/a,而对“骆驼城陡坎”的调查结果认为,该地貌特征不是断层陡坎,而是古代水利工程的遗迹,榆木山的构造变形是祁连山向北的扩展过程,其隆升变形为近对称形态的发育和发展过程；古浪断裂的滑动速率补充研究的结果为皇城—双塔断裂全新世逆冲滑动速率为(0.39±0.04)mm/a,而天桥沟—黄羊川断裂全新世以来的左旋走滑速率为(2.66±0.38)mm/a；祁连山西端昌马断裂西段滑动速率的补充测量和估算结果是晚第四纪逆冲滑动速率为(0.14±0.02)mm/a,左旋走滑速率为(1.17±0.04)mm/a,远比前人研究结果的3.3-4.3 mm/a的左旋滑动速率要小的多。
青藏高原北部断裂晚第四纪滑动速率及现今GPS观测揭示了青藏高原向北扩展与高原边缘隆升的运动特征。主要断裂晚第四纪滑动速率及跨断裂GPS应变速率的结果表明,青藏高原北部边缘的断裂以低滑动速率(<10 mm/a)为主,特别是两条边界断裂阿尔金断裂和海原—祁连山断裂。两条主要控边界断裂上的滑动速率沿断裂的分布变化特征显示了断裂间滑动速率转换及调整。阿尔金断裂自95°E以西的8-12 mm/a稳定滑动速率,向东逐渐降低到最东端约为1-2 mm/a,而海原断裂自哈拉湖一带开始发育后滑动速率为1-2 mm/a,到祁连一带(101°E以东)增大到相对稳定的4-5 mm/a,直到过海原后转向六盘山一带,滑动速率降低到1-3 mm/a,甚至更低。滑动速率的变化及分布特征显示,阿尔金断裂的左旋滑动主要是通过祁连山内部隆起及两侧新生代盆地变形引起的缩短来吸收的,海原—祁连山断裂的低滑动速率及沿断裂运动学特征表明断裂尾端的陇西盆地变形及六盘山的隆起是断裂左旋走滑速率的主要吸收方式。
青藏高原北部地区是由北东东向的阿尔金断裂、北西西向的海原—祁连山断裂带及隆起的祁连山区及其北部的河西走廊及阿拉善板块的边缘所组成,主边界断裂的左旋走滑,祁连山北部及边缘断裂的挤压逆冲、河西走廊内部隆起及北部断裂的调节作用是高原边缘活动构造图像的主要特征,这三部分共同构成了高原北部边缘完整的活动构造图像。阿尔金断裂和海原—祁连山断裂之间的转换是通过高原北部边缘隆起山区的逆冲断层来完成的,高原变形的吸收主要是通过控边断层上的走滑速率、过渡转换区逆冲断层的逆冲滑动速率和高原边缘的高海拔来完成,另外是不同块体内部和边缘的主要新生代盆地的褶皱变形也吸收了少部分地壳变形。祁连山内部及边缘的逆冲断层提供了高原边缘近60%的地壳缩短,阿尔金断裂及海原—祁连山断裂控制下的青藏高原北部边缘的构造变形机制,是在三个刚性块体所阻挡下的通过内部旋转或构造性质转换来完成的。河西走廊不同位置构造形态和地貌特征的变化,是青藏高原北部两大块体相互作用过程中,运动方向和动力变化的结果。河西走廊北部山脉地貌形态、断裂构造活动及构造隆升的特征显示了走廊北部的各主要断裂的发育发展可能是相互独立,其形态和扩展方向说明了其构造形成和扩展的趋势和动力方向,各断层有明显的不一致,不是以往所说的自西向东的发育发展过程,河西走廊北部的断裂(特别是中段)是青藏高原挤压作用下地壳缩短作用的结果。
青藏高原北部变形模式及变形机制讨论表明,青藏高原北部边缘的变形是一种分布式的连续变形,变形发生自高原内部,边界断裂的走滑被高原内部变形所吸收。同时,祁连山北缘和内部断裂及河西走廊北部的断裂所表现的逆冲为主的活动性质,对地壳增厚模式所强调的由逆冲断层和地壳增厚及局部高海拔来分解吸收地壳变形的说法是支持的。
Collision between Indian and Eurasian plates not only created Tibetan Plateau, "the roof of the world", but also posed significant impacts on climate and environments of western China and central Asia. Hexi Corridor consists of a series of western northwest-trending Cenozoic basins along range front of the Qilian Shan. Tectonic setting of the Hexi Corridor marks the northern margin of Tibetan Plateau where abundant active faults and historical earthquakes attests significant on-going tectonic deformation due to outward growth of the Tibetan Plateau. Tectonic deformation of the region is dominated by two major strike-slip faults bounding different deforming units, the Altyn Tagh fault and the Haiyuan fault. Other structures with different styles and senses of motion form complex pattern of active tectonic deformation. It is thus an ideal place to study active tectonic deformation to gain understandings of the processes of Tibetan Plateau's northward growth. Key scientific questions regarding tectonic processes associated with outward growth of Tibetan Plateau includes: what is major process governing tectonic deformation of the northern margin of the Tibetan Plateau; what are relationships between strike-slip faulting and crustal shortening; how the slips on strike-slip fault are transferred into crustal shortening in other structures; what are slip rates along major faults in the region. Answers to these and other similar questions bear important implications for understanding tectonic processes associated with the outward growth of the Tibetan Plateau.
Based on systematic studies on the late Quaternary slip rates along major active faults in Hexi Corridor and adjacent regions in northern Tibet, this paper provides an integrated information to show geometric pattern and kinematics features of active tectonic deformation in northern margin of the Tibetan Plateau. In combining active faulting studies with GPS measurements, we also discuss models of the late Cenozoic deformation and its dynamic mechanism of the northern margin of Tibetan Plateau especially the Qilian Shan and Hexi Corridor. Main conclusions are drawn as follows:
The South Heli Shan Fault is the north boundary of the Hexi Corridor basin, and it is typical of transpression feature with predominant reverse faulting and minor left-slip near its ends. The topographic features of the Heli Shan correlate to slips on the fault suggesting active fault controls on mountainous geomorphology. The South Heli Shan Fault can be divided into three segments based on its geometry. Slip of the individual segment is of arch shape distribution, and the slip distribution of the whole fault zone depicts an asymmetric arch shape as eastern side with higher rates and west side with lower rates. Average slip rates are (0.34±0.10)mm/a for the Houertou segment, (0.14±0.10)mm/a for the Wutongjing region, (0.24±0.06)mm/a for central segment, and (0.18±0.07)mm/a for western segment. Left-lateral movements are only observed at local sites near two terminals of the South Heli Shan Fault.
Trenching and field survey along the surface ruptures, together historic earthquake investigation indicate that there might be three strong earthquakes occurred along the South Heli Shan Fault. The first event ruptured along the whole fault about 5000a ago, and the other two occurred during the documented history, in 180 A.D and 756 A.D. respectively. More than 60km long surface ruptures was associated with the M71/2 event in 180 A.D. and 20-30km ruptures might have formed during the M 7 event in 756 A.D. The behavior of paleoearthquake activity does not show quasi-periodic pattern.
Tectonic deformation and kinematics pattern in the northern Hexi Corridor is characterized by thrust fault related uplift with southward movement and westward tilting, that resulted from the outward growth of the Tibet Plateau toward the relative tectonic stable Alashan block. Topographic profiles constructed from DEM perpendicular to the Heli Shan show that different fault segments are associated with different geomorphology. The primary geomorphic feature is the tilting towards Hexi Corridor basin along the fault. Along the strike of Heli Shan mountain, topographic profile shows westward tilting of geomorphology. This kind of east to west tilting corroborates larger displacements in eastern part of the fault and less offset in western part of the fault. Thus, the topographic expression is representative of the activity of the Heli Shan fault. Slip distribution along the fault and strong earthquake activity suggest the recurrent pattern of strong earthquake may be a combination of characteristic and temporal clustering.
Active fault studies in the northern and interior of the Hexi Corridor basin indicate that the Jiayuguan-Heishan fault is a high angle reverse fault with late Pleistocene activity. The slip rate is (0.26±0.06) mm/a since late Pleistocene. The Jinta Nan Shan fault is a Holocene active fault is with a slip rate of (0.22±0.05) mm/a since late Pleistocene. The Jiayuguan-Wenshu Shan fault, a transverse fault obliquely cuts the Hexi Corridor to separate the Jiuquan basin in the east and the Yumen basin in the west. The fault appears to be high-angle reverse fault with hangingwall tilting to the west, and observed slip rate is (0.30±0.05)mm/a. As for the Mushaoliang fault and Dachechang-Ayouqi fault along the north Hexi Corridor, geomorphological pattern and remote sensing interpretation suggest that these faults are of high-angle reverse slipping from north to south.
Kinematics of tectonic deformation along the northern Qilian Shan fault shows that the western segment of the Fodongmiao-Hongaizi fault is a premary reverse fault, and its eastern segment is associated with left-lateral components. This fault presents obvious evidence of Holocene activity, and remnant of surface rupture of historical earthquake can still be found in many places. The slip rate of reverse faulting is (0.41±0.09) mm/a and left lateral slip rate is (1.20±0.15) mm/a. Early Holocene geomorphic surface is offset by the northern Yumu Shan fault with slip rate (0.55±0.15) mm/a of reverse faulting and the left lateral slip rate (0.95±0.11) mm/a. Out investigation show that the so called "Luotuocheng fault scarp " is in fact remnants of ancient irrigation canal rather than an active fault. Tectonic deformation of the Yumu Shan is a consequence of the northward growth of the Qilian Shan, and the symmetric topographic shape of Yumu Shan suggests that slip distribution along the Yumu Shan fault is also symmetric. Additional study on slip rate of the Gulang fault shows that Holocene dip-slip rate of the Huangcheng-Shuangta fault is (0.39±0.04) mm/a and left-slip rate of the Tianqiaogou-Huangyangchuan fault is (2.66±0.38) mm/a. Survey on west segment of the Changma fault near west Qilian Shan indicates that late Quaternary throw rate is (0.14±0.02) mm/a and left lateral slip rate is (1.17±0.04) mm/a, which is much less than previous reported 3.3-4.3mm/a.
GPS measurements and late Quaternary fault slip rates reveal the kinematic pattern of outward growth of the northern margin of the Tibetan Plateau. Base on the geologic data and GPS velocity slip rates of major boundary faults are less than 10 mm/a including the Altyn-Tagh fault and Haiyuan- Qilianshan fault. The distributions of slip rates along the two major faults show constant slip rate along their middle portion and decrease toward their ends. For example, the left-lateral slip rates on the central segment of Altyn-Tagh Fault appear to be in the range of 8-12 mm/a, but decreases eastward to only 1-2 mm/a near 97°E. On the Haiyuan-Qilian Shan fault, slip rates are 1-2 mm/a in its western segment, and increase to 4-5mm/a in its eastern and middle segments, and then decrease to 1-3 mm/a near its eastern end near the Liupan Shan. This kind of slip distribution suggests that almost all motion along a strike-slip fault is accommodated by crustal shortening or convergence near the ends of the strike-slip fault. The crustal shortening across the Qilian Shan absorbs strike-slip along the Altyn Tagh fault. The convergence in Liupan Shan accommodates left-lateral slip along the Qilian-Haiyuan fault.
Northern Tibetan Plateau includes the NNE-teending Altyn Tagh Fault, NWW-striking Haiyuan-Qilian Shan Fault and uplifted Qilian Shan mountain belt, Hexi Corridor basin and Alashan block. Tectonic processes in the region can be described as combination of three structural styles. First, outward growth of the northern Tibetan Plateau cause west northwest trending reverse faulting and folding in the Qilian Shan and Hexi Corridor, and the deformation might have migrated to north of the Hexi Corridor caused reverse faulting and earthquake rupturing in Heli Shan and Longshou Shan. Second, left-lateral strike slip on the main boundary faults (The Altyn Tagh fault and the Qilian-Haiyuan fault) cause reverse faulting, folding and uplifting of mountains to accommodate the lateral motions. And third, internal deformation within the Qilian Shan, Hexi Corridor, and even with the interior of tectonically stable Alashan Block. These three tectonic deformations contribute to outward and upward growth of the northern margin of Tibetan Plateau. Our studies show that tectonic deformation occurred mainly within the northern Tibetan Plateau, and that the rule of strike slip faulting has been reconciling differences of crustal shortening or crustal thickening rather than extruding crustal blocks out of the plateau interior.
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