龙门山推覆构造带新生代热演化历史研究及其对青藏高原东缘隆升机制的约束
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摘要
龙门山作为青藏高原的东边界，是一个从青藏高原到四川盆地的陡直的过渡地带，其新生代的造山运动受到约50Ma年前印度板块和欧亚板块碰撞的影响。2008汶川地震及其后续的研究证明了其晚更新世以来的活跃性，但是对于龙门山推覆构造带及其邻近地区的新生代的演化过程的认识还较缺乏。另外前人对于青藏高原东缘的隆升起始时间以及隆升机制等问题，做了大量研究，但仍存在不一致的看法。高原东缘隆升起始时间主要有两类观点：一、高原东缘隆升开始于20-30Ma，并经历过几次冷却事件；二、约10Ma以来高原东缘开始隆升，之前处于稳定状态。对于青藏高原东缘龙门山推覆构造带的隆升机制存在两种截然不同的看法：一、刚性块体的侧向挤出；二、下地壳流动。
本研究采用锆石和磷灰石裂变径迹法，对龙门山推覆构造带不同地区的岩石进行系统的新生代以来的热演化历史研究。结合前人已有的热年代学数据，揭示龙门山推覆构造带及其邻近构造单元的岩石新生代剥露过程以及其与断层活动的关系，并对青藏高原东缘的隆升机制进行了讨论。
龙门山推覆构造带整体表现为从南往北裂变径迹年龄逐渐变老的特征，表明新生代平均剥蚀速率从南往北逐渐降低的趋势。南段断层上盘离断层较近的位置样品锆石裂变径迹（ZFT）年龄大多为11-14Ma，随着离断层距离的增加，年龄增大到25-35Ma，高原内部的样品的ZFT年龄进一步增大到200Ma左右；中段的ZFT最年轻年龄出现在位于汶川-茂县断层上盘的雪隆包杂岩，为10.6Ma，其余样品均大于（或等于）40Ma；北段ZFT则全部大于60Ma，表明其新生代未发生退火。对于磷灰石裂变径迹（AFT）年龄来说，南段大部分样品年龄分布在1.9-5Ma之间，高原内部的样品年龄则大于10Ma；中段最年轻的样品仍出现在雪隆包杂岩，为2.1Ma，其它AFT年龄大多在8Ma附近，盆地内的AFT年龄则大多30Ma；北段AFT年龄明显较老，分布在30-189Ma之间。南段最快剥蚀速率达约2.1mm/yr（约1.9Ma以来），中段最快剥蚀速率达约1.9mm/yr（2.1Ma以来），北段最快剥蚀速率为0.1mm/yr（33Ma以来）。另外，南段、中段、北段多条断层表现出上盘年龄较小、下盘年龄较大的现象，表明新生代以来断层两侧存在差异剥蚀，且全部断层表现为逆冲性质。南段和中段断层两侧的差异剥蚀量较大，而北段较小，表明南段和中段的断层逆冲运动速率大于北段。龙门山推覆构造带中段的总剥蚀宽度明显较大，揭示出其主断层的低倾角（约30°）特征。南段断层活动有逐渐向盆地迁移的特征，青藏高原和四川盆地现今的运动差异主要被山前断裂和盆地内的隐伏断层所吸收。
位于龙门山推覆构造带西南的贡嘎山岩体新生代晚期快速冷却，也表现出南快北慢的特征。南端约1Ma以来的隆升速率超过3.3±0.8mm/a，北端隆升速率约1.0-1.9mm/a (约6Ma以来)。岩体周边的三叠系地层剥蚀较慢，表明青藏高原在整体横向挤出、缓慢隆升的基础上，还存在着一些特殊的局部快速隆升区域。通过对川滇地块水平运动的矢量分析，我们认为贡嘎山花岗岩体是鲜水河断裂至安宁河断裂间挤压弯曲段吸收、转换青藏高原块体向东、向南东水平运动，导致局部快速隆升的产物。
位于龙门山推覆构造带南段西侧的丹巴背斜，出露了一套从前寒武杂岩到三叠系变质岩的完整地层，为研究松潘-甘孜褶皱带中生代-新生代的变质、构造变形的重要“窗口”。前人做了大量研究，但是30Ma以来冷却历史仍然模糊不清。本研究在丹巴背斜获得了30个AFT和ZFT年龄，给出了丹巴背斜不同部位新生代以来的冷却历史。研究显示丹巴背斜地区的岩石从约25Ma开始持续冷却至今，平均冷却速率从核心部位的13.0±1.2℃/Ma，降低到次核心的10.5±1.1℃/Ma，进一步降低到背斜边缘的6.0±1.0℃/Ma，约25Ma以来的总剥蚀量从核心的13-15千米降低到边缘的5-7千米。根据岩石的最高变质温度以及新生代的冷却量，新生代以来丹巴背斜的变形占总变形的1/4-1/2。研究表明丹巴背斜地区约25Ma开始受到印度板块和欧亚板块碰撞的影响，表现为北东向缩短，且新生代的构造变形受到中生代或更老的构造背景所影响。
龙门山推覆构造带北段西侧的岷山为新生代晚期快速抬升的山体(Kirby etal.,2002)。本研究在岷山地区获得了12个AFT年龄和径迹长度分布。通过HeFTy软件，对这些数据进行热历史模拟，获得了10个样品的冷却历史，揭示出其新生代经历了两次冷却事件，时间分别为30-50Ma和5-0Ma。5-0Ma的总冷却量约40℃，对应的剥蚀量约1-2千米，剥蚀速率0.2-0.4mm/yr。岷山地区的断层活动也表现出随时间向东转移的特征。GPS资料揭示的岷山地区2-3mm/yr的缩短速率，可以造成岷山0.2-0.4mm/yr的隆升，不需要下地壳流动假说的支持。
通过对以上不同构造单元的冷却历史研究，揭示出研究区约30Ma开始受到印度板块和欧亚板块碰撞的影响而开始抬升，冷却速率总体表现为南快北慢的特征。龙门山推覆构造带以及岷江断裂带的断层活动均表现出向盆地转移的趋势。本研究所揭示的上地壳变形样式以及抬升的起始时间等结论，均不支持下地壳流动假说对青藏高原东缘隆升机制的解释。主要表现在以下五个方面：
（1）龙门山推覆构造带汶川—茂县断层表现为逆冲运动性质，并非下地壳流动所认为的正断性质；剥蚀量最大的区域位于后山断裂上盘，与下地壳流动假说所认为的剥蚀量最大的区域（宝兴杂岩和彭灌杂岩）有所不同。
（2）龙门山推覆构造带中段的汶川-茂县断裂、北川-映秀断裂以及彭灌断层控制的抬升区域很宽，表明其断层较缓，即断层倾角较低，而下地壳流动假说通常认为龙门山推覆构造带为高角度逆断层。
（3）高原东缘龙门山区及其附近地区的抬升起始时间在30Ma左右，而下地壳流动假说通常认为高原东缘不同区域的抬升起始时间较一致，且非常年轻，距今约10Ma (Clark等，2005)。
（4）丹巴背斜的变形，受到中生代老构造的控制，表明青藏高原并非均匀的连续变形的物质。丹巴背斜的变形表现出北东向上地壳挤压缩短，这种现象用下地壳流动假说无法解释。
（5）岷山大部分地区的剥蚀速率较低，仅0.2-0.4mm/yr，GPS揭示的岷山2-3mm/yr的缩短速率可以通过虎牙断裂的逆冲运动控制岷山的隆升，无需下地壳流动的支持。
The Longmenshan (LMS) range which constitutes the eastern border of the Tibetanplateau is characterized by a steep topographic transition from the Sichuan Basin tothe plateau with about400km in length. The Cenozoic orogeny of this range wasresulted from the collision between the India plate and Eurasia since50Ma. The2008Wenchuan earthquake and the researches on the earthquake confirm the activity of theLMS since Late Pleistocene, but the Cenozoic evolution of the Longmenshan ThrustBelt (LTB) is still ambiguous, especially in the south segment. Furthermore,researchers have different views on the initial time and the mechanis of the uplift inthe eastern margin of the Tibetan plateau. For the initial time, there are two differentopinions: the first suggests that the eastern margin of the Tibet plateau uplift began20-30Ma, and expearenced several cooling event; the second contends that the theeastern margin of the Tibetan plateau remained stable from60-10Ma, and began touplift quickly from about10Ma to present. For the uplift mechanism, there are twoentirely different explanations: rigid lithospheric extrusion model and low-crustalchannel flow model.
In this work, I use the zircon and apatite fission track method to research thethermal history of dozens of rocks at the LTB. Combining with previouslow-temperature thermochronology data, the fission track data reveal the Cenozoicexhumation process of the rocks and their relations with the activities of the faults atLTB. On that basis, I discuss the uplift mechanism of the eastern margin of theTibetan Plateau.
In general, the fission track ages of the rocks at the LTB become older from southto north, which indicates that the average exhumation rate decreases from south tonorth of the LTB. In the southern segment, the Zircon Fission Track (ZFT) ages rangefrom11Ma to14Ma for the hanging wall of and close to the faults at south segmentof the LTB, and increase to about25-35Ma, following the increasing distance to thefault. In the middle segment, the youngest ZFT age of10.6Ma appeared at theXuelongbao Complex, the hanging wall of the Wenchuan-Maoxian fault, and the other ZFT ages are more than40Ma. In the northern segment, all the ZFT ages areover60Ma, which indicates all samples are not reset in the Cenozoic. Apatite FissionTrack (AFT) ages range from1.9Ma to5.0Ma in the southern segment. In the middlesegment, the youngest age also appears at same place with ZFT, and is in data of2.1Ma, while others are about8Ma. The AFT ages in the northern segment are obviousolder than that in the southern and middle segments, and range from30Ma to189Ma.The maximum average exhumation rates are2.1mm/yr from1.9Ma to present at thesouthern segment,1.9mm/yr from2.1Ma to present at the middle segment, and0.1mm/yr from33Ma to present at the northern segment, respectively. Moreover, thereare obvious differences in the ages cross faults, showing that the ages at the hangingwall are younger than the footwall, which indicates there are differential exhumationson the two sides of the faults, and all faults have thrust component in the Cenozoic.The differential exhumations are greater in the southern and middle segments thanthat in the northern segment, further indicating that the faults at the southern andmiddle segments have a larger thrust rate than that at the northern segment. Accordingto the width of the exhumation at the middle segment and the depth of the detachmentplane, I estimate the dip angles of the major faults, which are about30°, revealing thatthe faults at the middle segment are low dip angle faults. At the southern segment, theactivity of the faults migrate to the basin, and the present difference of movementbetween the Tibetan Plateau and the Sichuan Basin is mainly absorbed by front rangefaults and blind faults in the basin.
The Gonggashan Granite located to the southwest of the LTB is cooling quicklyfrom late Cenozoic to present, and also shows the characteristics of a decreasing trendfrom south to north in the cooling rate. The biggest uplift rate from about1Ma topresent may equal or be more than3.3±0.8mm/a, while the uplift rate of the Triassicrocks is much smaller. The phenomena indicate that the partial area of the TibetanPlateau uplifted quickly when most of the plateau uplifted slowly. According to theresolution of vectors of the Sichuan-Yunnan Block’s horizontal movement, I think thatthe rapid uplift of the Gonggashan Granite is caused by the change of the strike of theXianshuihe fault, which absorbs and converts the eastward or southeastward horizontal movement of the Sichuan-Yunnan Block. The Gonggashan Granite may bethe product of this progress.
The Danba Anticline to the west of the southern segment of the LTB is animportant region for research of Mesozoic-Cenozoic deformation, as it exposes arelated complete set of rocks, but the cooling history from30Ma to present is stillambiguous. In this work, I get16Apatite fission track and14Zircon fission trackages, and determine the cooling histories in different regions of the Danba Anticline.The result shows that the rocks in the Danba Anticline cooled quickly from ca.25Mato present, and the average cooling rates decreased from13.0±1.2℃/Ma at the core, tothe10.5±1.1℃/Ma at the subcenter, then to6.0±1.0℃/Ma at the periphery of theDanba Anticline. Supposing the paleo-geothermal gradient is25±5℃/km, thedenudation thicknesses from ca.25Ma to present decreased from13-15km at the coreto5-7km at the periphery of the Danba Anticline. According to the metamorphictemperature, the Cenozoic deformation takes up the1/4to1/2of the total deformationin the Danba Anticline. This research indicates that the Danba Anticline began to beaffected by the India-Asia collision at ca.25Ma and behaved as crustal shorteningtoward northeast.
The Min Shan, located to the west of the north segment of the LTB, is also arange that uplifted quickly in late Cenozoic. I get12AFT ages and data of tracks’length, for thermal history modeling that shows that the Minshan range underwenttwo cooling events, which happened from50to30Ma and5Ma to present,respectively. The cooling amount in the later cooling event was about40℃, and theexhumation thickness and the exhumation rate were about1-2km and0.2-0.4mm/yr.Like the southern segment of the LTB, the activity of the faults in the Minshan regionalso moves east. The2-3mm/yr shortening revealed by GPS can cause the uplift witha rate of0.2-0.4mm/yr, and the low-crustal channel flow hypothesis is not needed forthe Minshan uplift.
The thermal history research in different tectonic regions suggest that the easternmargin of the Tibetan plateau building, affected by the collision between the Indiaplate and the Eurasia plate, initialed at about30Ma, and the cooling rates decreased from south to north. The fault activity shows a tendency of moving to the Sichuanbasin. All of the phenomena revealed in this work, for example, the deformation styleof upper crust, and the initial time of the plateau building, don’t support thelow-crustal channel flow hypothesis. The reasons are mainly in the following fiveaspects:
(1) The Wenchuan-Maoxian fault in the LTB is a thrust fault, while thelow-crustal channel flow hypothesis considers it as a normal fault. Themaximum exhumation regions are located on the hanging wall of theWenchuan-Maoxian fault, and not the Baoxing Complex and the PengguanComplex, which are thought to be the region with the biggest exhumation ratein the low-crustal channel flow explaination.
(2) The Wenchuan-Maoxian fault, Beichuan-Yingxiu fault and Peng-Guan faultin the middle segment of the LTB control wide region uplift, which indicatesthat the ramps of those faults have slow slope. In other words, the faults havesmall dip angles, while the dip angles should be much bigger in thelow-crustal channel flow hypothesis.
(3) The uplift of the Longmenshan and the other regions in the eastern margin ofthe Tibetan plateau initiated at about30Ma according to this research.However, the low-crustal channel flow hypothesis suggests that the easternmargin of Tibetan plateau uplifted quickly from about10Ma to present(Clark et al.,2005).
(4) Cenozoic deformation of the Danba Anticline is controlled by Mesozoictectonics, which indicates the Tibetan plateau is not a homogeneous andcontinuous deformed material. The Danba Anticline behaves as upper crustalnortheast shortening, which is difficult to be explained by the low-crustalchannel flow hypothesis.
(5) The uplift rates in most areas of the Min Shan are between0.2-0.4mm/yr, andthe2-3mm/yr shortening revealed by GPS can accomodate the uplift of theMin Shan, so the low-crustal channel flow hypothesis is not needed.
本研究采用锆石和磷灰石裂变径迹法，对龙门山推覆构造带不同地区的岩石进行系统的新生代以来的热演化历史研究。结合前人已有的热年代学数据，揭示龙门山推覆构造带及其邻近构造单元的岩石新生代剥露过程以及其与断层活动的关系，并对青藏高原东缘的隆升机制进行了讨论。
龙门山推覆构造带整体表现为从南往北裂变径迹年龄逐渐变老的特征，表明新生代平均剥蚀速率从南往北逐渐降低的趋势。南段断层上盘离断层较近的位置样品锆石裂变径迹（ZFT）年龄大多为11-14Ma，随着离断层距离的增加，年龄增大到25-35Ma，高原内部的样品的ZFT年龄进一步增大到200Ma左右；中段的ZFT最年轻年龄出现在位于汶川-茂县断层上盘的雪隆包杂岩，为10.6Ma，其余样品均大于（或等于）40Ma；北段ZFT则全部大于60Ma，表明其新生代未发生退火。对于磷灰石裂变径迹（AFT）年龄来说，南段大部分样品年龄分布在1.9-5Ma之间，高原内部的样品年龄则大于10Ma；中段最年轻的样品仍出现在雪隆包杂岩，为2.1Ma，其它AFT年龄大多在8Ma附近，盆地内的AFT年龄则大多30Ma；北段AFT年龄明显较老，分布在30-189Ma之间。南段最快剥蚀速率达约2.1mm/yr（约1.9Ma以来），中段最快剥蚀速率达约1.9mm/yr（2.1Ma以来），北段最快剥蚀速率为0.1mm/yr（33Ma以来）。另外，南段、中段、北段多条断层表现出上盘年龄较小、下盘年龄较大的现象，表明新生代以来断层两侧存在差异剥蚀，且全部断层表现为逆冲性质。南段和中段断层两侧的差异剥蚀量较大，而北段较小，表明南段和中段的断层逆冲运动速率大于北段。龙门山推覆构造带中段的总剥蚀宽度明显较大，揭示出其主断层的低倾角（约30°）特征。南段断层活动有逐渐向盆地迁移的特征，青藏高原和四川盆地现今的运动差异主要被山前断裂和盆地内的隐伏断层所吸收。
位于龙门山推覆构造带西南的贡嘎山岩体新生代晚期快速冷却，也表现出南快北慢的特征。南端约1Ma以来的隆升速率超过3.3±0.8mm/a，北端隆升速率约1.0-1.9mm/a (约6Ma以来)。岩体周边的三叠系地层剥蚀较慢，表明青藏高原在整体横向挤出、缓慢隆升的基础上，还存在着一些特殊的局部快速隆升区域。通过对川滇地块水平运动的矢量分析，我们认为贡嘎山花岗岩体是鲜水河断裂至安宁河断裂间挤压弯曲段吸收、转换青藏高原块体向东、向南东水平运动，导致局部快速隆升的产物。
位于龙门山推覆构造带南段西侧的丹巴背斜，出露了一套从前寒武杂岩到三叠系变质岩的完整地层，为研究松潘-甘孜褶皱带中生代-新生代的变质、构造变形的重要“窗口”。前人做了大量研究，但是30Ma以来冷却历史仍然模糊不清。本研究在丹巴背斜获得了30个AFT和ZFT年龄，给出了丹巴背斜不同部位新生代以来的冷却历史。研究显示丹巴背斜地区的岩石从约25Ma开始持续冷却至今，平均冷却速率从核心部位的13.0±1.2℃/Ma，降低到次核心的10.5±1.1℃/Ma，进一步降低到背斜边缘的6.0±1.0℃/Ma，约25Ma以来的总剥蚀量从核心的13-15千米降低到边缘的5-7千米。根据岩石的最高变质温度以及新生代的冷却量，新生代以来丹巴背斜的变形占总变形的1/4-1/2。研究表明丹巴背斜地区约25Ma开始受到印度板块和欧亚板块碰撞的影响，表现为北东向缩短，且新生代的构造变形受到中生代或更老的构造背景所影响。
龙门山推覆构造带北段西侧的岷山为新生代晚期快速抬升的山体(Kirby etal.,2002)。本研究在岷山地区获得了12个AFT年龄和径迹长度分布。通过HeFTy软件，对这些数据进行热历史模拟，获得了10个样品的冷却历史，揭示出其新生代经历了两次冷却事件，时间分别为30-50Ma和5-0Ma。5-0Ma的总冷却量约40℃，对应的剥蚀量约1-2千米，剥蚀速率0.2-0.4mm/yr。岷山地区的断层活动也表现出随时间向东转移的特征。GPS资料揭示的岷山地区2-3mm/yr的缩短速率，可以造成岷山0.2-0.4mm/yr的隆升，不需要下地壳流动假说的支持。
通过对以上不同构造单元的冷却历史研究，揭示出研究区约30Ma开始受到印度板块和欧亚板块碰撞的影响而开始抬升，冷却速率总体表现为南快北慢的特征。龙门山推覆构造带以及岷江断裂带的断层活动均表现出向盆地转移的趋势。本研究所揭示的上地壳变形样式以及抬升的起始时间等结论，均不支持下地壳流动假说对青藏高原东缘隆升机制的解释。主要表现在以下五个方面：
（1）龙门山推覆构造带汶川—茂县断层表现为逆冲运动性质，并非下地壳流动所认为的正断性质；剥蚀量最大的区域位于后山断裂上盘，与下地壳流动假说所认为的剥蚀量最大的区域（宝兴杂岩和彭灌杂岩）有所不同。
（2）龙门山推覆构造带中段的汶川-茂县断裂、北川-映秀断裂以及彭灌断层控制的抬升区域很宽，表明其断层较缓，即断层倾角较低，而下地壳流动假说通常认为龙门山推覆构造带为高角度逆断层。
（3）高原东缘龙门山区及其附近地区的抬升起始时间在30Ma左右，而下地壳流动假说通常认为高原东缘不同区域的抬升起始时间较一致，且非常年轻，距今约10Ma (Clark等，2005)。
（4）丹巴背斜的变形，受到中生代老构造的控制，表明青藏高原并非均匀的连续变形的物质。丹巴背斜的变形表现出北东向上地壳挤压缩短，这种现象用下地壳流动假说无法解释。
（5）岷山大部分地区的剥蚀速率较低，仅0.2-0.4mm/yr，GPS揭示的岷山2-3mm/yr的缩短速率可以通过虎牙断裂的逆冲运动控制岷山的隆升，无需下地壳流动的支持。
The Longmenshan (LMS) range which constitutes the eastern border of the Tibetanplateau is characterized by a steep topographic transition from the Sichuan Basin tothe plateau with about400km in length. The Cenozoic orogeny of this range wasresulted from the collision between the India plate and Eurasia since50Ma. The2008Wenchuan earthquake and the researches on the earthquake confirm the activity of theLMS since Late Pleistocene, but the Cenozoic evolution of the Longmenshan ThrustBelt (LTB) is still ambiguous, especially in the south segment. Furthermore,researchers have different views on the initial time and the mechanis of the uplift inthe eastern margin of the Tibetan plateau. For the initial time, there are two differentopinions: the first suggests that the eastern margin of the Tibet plateau uplift began20-30Ma, and expearenced several cooling event; the second contends that the theeastern margin of the Tibetan plateau remained stable from60-10Ma, and began touplift quickly from about10Ma to present. For the uplift mechanism, there are twoentirely different explanations: rigid lithospheric extrusion model and low-crustalchannel flow model.
In this work, I use the zircon and apatite fission track method to research thethermal history of dozens of rocks at the LTB. Combining with previouslow-temperature thermochronology data, the fission track data reveal the Cenozoicexhumation process of the rocks and their relations with the activities of the faults atLTB. On that basis, I discuss the uplift mechanism of the eastern margin of theTibetan Plateau.
In general, the fission track ages of the rocks at the LTB become older from southto north, which indicates that the average exhumation rate decreases from south tonorth of the LTB. In the southern segment, the Zircon Fission Track (ZFT) ages rangefrom11Ma to14Ma for the hanging wall of and close to the faults at south segmentof the LTB, and increase to about25-35Ma, following the increasing distance to thefault. In the middle segment, the youngest ZFT age of10.6Ma appeared at theXuelongbao Complex, the hanging wall of the Wenchuan-Maoxian fault, and the other ZFT ages are more than40Ma. In the northern segment, all the ZFT ages areover60Ma, which indicates all samples are not reset in the Cenozoic. Apatite FissionTrack (AFT) ages range from1.9Ma to5.0Ma in the southern segment. In the middlesegment, the youngest age also appears at same place with ZFT, and is in data of2.1Ma, while others are about8Ma. The AFT ages in the northern segment are obviousolder than that in the southern and middle segments, and range from30Ma to189Ma.The maximum average exhumation rates are2.1mm/yr from1.9Ma to present at thesouthern segment,1.9mm/yr from2.1Ma to present at the middle segment, and0.1mm/yr from33Ma to present at the northern segment, respectively. Moreover, thereare obvious differences in the ages cross faults, showing that the ages at the hangingwall are younger than the footwall, which indicates there are differential exhumationson the two sides of the faults, and all faults have thrust component in the Cenozoic.The differential exhumations are greater in the southern and middle segments thanthat in the northern segment, further indicating that the faults at the southern andmiddle segments have a larger thrust rate than that at the northern segment. Accordingto the width of the exhumation at the middle segment and the depth of the detachmentplane, I estimate the dip angles of the major faults, which are about30°, revealing thatthe faults at the middle segment are low dip angle faults. At the southern segment, theactivity of the faults migrate to the basin, and the present difference of movementbetween the Tibetan Plateau and the Sichuan Basin is mainly absorbed by front rangefaults and blind faults in the basin.
The Gonggashan Granite located to the southwest of the LTB is cooling quicklyfrom late Cenozoic to present, and also shows the characteristics of a decreasing trendfrom south to north in the cooling rate. The biggest uplift rate from about1Ma topresent may equal or be more than3.3±0.8mm/a, while the uplift rate of the Triassicrocks is much smaller. The phenomena indicate that the partial area of the TibetanPlateau uplifted quickly when most of the plateau uplifted slowly. According to theresolution of vectors of the Sichuan-Yunnan Block’s horizontal movement, I think thatthe rapid uplift of the Gonggashan Granite is caused by the change of the strike of theXianshuihe fault, which absorbs and converts the eastward or southeastward horizontal movement of the Sichuan-Yunnan Block. The Gonggashan Granite may bethe product of this progress.
The Danba Anticline to the west of the southern segment of the LTB is animportant region for research of Mesozoic-Cenozoic deformation, as it exposes arelated complete set of rocks, but the cooling history from30Ma to present is stillambiguous. In this work, I get16Apatite fission track and14Zircon fission trackages, and determine the cooling histories in different regions of the Danba Anticline.The result shows that the rocks in the Danba Anticline cooled quickly from ca.25Mato present, and the average cooling rates decreased from13.0±1.2℃/Ma at the core, tothe10.5±1.1℃/Ma at the subcenter, then to6.0±1.0℃/Ma at the periphery of theDanba Anticline. Supposing the paleo-geothermal gradient is25±5℃/km, thedenudation thicknesses from ca.25Ma to present decreased from13-15km at the coreto5-7km at the periphery of the Danba Anticline. According to the metamorphictemperature, the Cenozoic deformation takes up the1/4to1/2of the total deformationin the Danba Anticline. This research indicates that the Danba Anticline began to beaffected by the India-Asia collision at ca.25Ma and behaved as crustal shorteningtoward northeast.
The Min Shan, located to the west of the north segment of the LTB, is also arange that uplifted quickly in late Cenozoic. I get12AFT ages and data of tracks’length, for thermal history modeling that shows that the Minshan range underwenttwo cooling events, which happened from50to30Ma and5Ma to present,respectively. The cooling amount in the later cooling event was about40℃, and theexhumation thickness and the exhumation rate were about1-2km and0.2-0.4mm/yr.Like the southern segment of the LTB, the activity of the faults in the Minshan regionalso moves east. The2-3mm/yr shortening revealed by GPS can cause the uplift witha rate of0.2-0.4mm/yr, and the low-crustal channel flow hypothesis is not needed forthe Minshan uplift.
The thermal history research in different tectonic regions suggest that the easternmargin of the Tibetan plateau building, affected by the collision between the Indiaplate and the Eurasia plate, initialed at about30Ma, and the cooling rates decreased from south to north. The fault activity shows a tendency of moving to the Sichuanbasin. All of the phenomena revealed in this work, for example, the deformation styleof upper crust, and the initial time of the plateau building, don’t support thelow-crustal channel flow hypothesis. The reasons are mainly in the following fiveaspects:
(1) The Wenchuan-Maoxian fault in the LTB is a thrust fault, while thelow-crustal channel flow hypothesis considers it as a normal fault. Themaximum exhumation regions are located on the hanging wall of theWenchuan-Maoxian fault, and not the Baoxing Complex and the PengguanComplex, which are thought to be the region with the biggest exhumation ratein the low-crustal channel flow explaination.
(2) The Wenchuan-Maoxian fault, Beichuan-Yingxiu fault and Peng-Guan faultin the middle segment of the LTB control wide region uplift, which indicatesthat the ramps of those faults have slow slope. In other words, the faults havesmall dip angles, while the dip angles should be much bigger in thelow-crustal channel flow hypothesis.
(3) The uplift of the Longmenshan and the other regions in the eastern margin ofthe Tibetan plateau initiated at about30Ma according to this research.However, the low-crustal channel flow hypothesis suggests that the easternmargin of Tibetan plateau uplifted quickly from about10Ma to present(Clark et al.,2005).
(4) Cenozoic deformation of the Danba Anticline is controlled by Mesozoictectonics, which indicates the Tibetan plateau is not a homogeneous andcontinuous deformed material. The Danba Anticline behaves as upper crustalnortheast shortening, which is difficult to be explained by the low-crustalchannel flow hypothesis.
(5) The uplift rates in most areas of the Min Shan are between0.2-0.4mm/yr, andthe2-3mm/yr shortening revealed by GPS can accomodate the uplift of theMin Shan, so the low-crustal channel flow hypothesis is not needed.
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