新疆及周边古地磁研究与构造演化

新疆古地磁研究始于1979年,20年来通过对塔里木、准噶尔、昆仑山等地区的古地磁研究,获得了古生代—新生代塔里木板块、准噶尔板块和青藏板块古地磁极移曲线和古纬度资料。震旦纪以前塔里木板块尚未形成,晚震旦世在赤道附近各地块才联合成塔里木板块的主体部分。后经历了两次快速北移,一次快速南移。准噶尔板块早古生代为一个独立的微板块,在晚古生代与哈萨克斯坦板块联合成一体,组成了哈萨克斯坦-准噶尔板块;塔里木板块震旦纪时还属冈瓦纳大陆的一个组成部分,早古生代逐渐脱离了冈瓦纳大陆,快速向北漂移,晚古生代早期与准噶尔板块首次在东部碰撞,成为劳亚大陆南缘的一个增生体。将介于劳亚大陆和冈瓦纳大陆之间的古陆体,称之谓华夏古陆群。晚古生代末—中生代早期,华夏古陆群先后增生到劳亚大陆南缘;早古生代早期古特提斯洋尚未形成,诸地块处于冈瓦纳大陆范围内,位于南半球的赤道附近。在中-晚志留世,这些地(板)块才快速向北漂移,由于洋扩张,形成了古特提斯洋,构成了三大陆块群夹两个大洋的古地理格局;二叠纪是特提斯构造演化关键时期,晚侏罗-早白垩世昆仑地块与柴达木地块和塔里木地块发生碰撞,联合成一体。早侏罗世早期柴达木地块等与塔里木地块发生碰撞联合,造成了古特提斯洋消亡。早侏罗世中期,开     

中国大陆的组成、结构、演化和动力学

中国大陆是由众多微陆块和小陆块组合而成的复合大陆，微、小陆块的软碰撞和多旋回缝合以及由此而产生的多旋回复合造山带、多旋回叠合盆地和多彷回构造岩浆成矿作用是其非常重要的特征。中国大陆具有清晰的多旋回分阶段演化过程和复杂的多层次镶叠式与立交桥式结构。古生代以来，中国大构造发展受古亚洲洋、特提斯洋、太平洋三大全球性动力学体系之控制。其主要动力过程表现为冈瓦纳裂离、陆块北移、褶皱带南迁、亚洲增生。     

重新认识中国斑岩铜矿的成矿地质条件

根据中国大陆洋陆作用的关系和造山带的演化，重新划分了中国斑岩铜矿成矿域和成矿带，将其分为古亚洲、北部特提斯、南部特提斯(喜马拉雅)和环太平洋4个成矿域。古亚洲成矿域又分为华北陆块北缘早-中古生代成矿带、哈萨克斯坦地块东北缘晚古生代成矿带、哈萨克斯坦地块南缘中晚古生代成矿带、西伯利亚板块西南缘晚古生代成矿带。特提斯北部成矿域分为中咱地块西缘晚三叠世义敦成矿带、羌塘地块(昌都-思茅地块)北缘古近纪玉龙成矿带、塔里木地块南缘晚古生代-新生代成矿带、扬子地块西缘古近纪成矿带。南部特提斯(喜马拉雅)成矿域分为班公错成矿带和冈底斯成矿带。环太平洋成矿域分晚中生代活动陆缘成矿带和台湾古近纪-新近纪岛弧成矿带。综合分析中国大陆地质演化史与斑岩铜矿成矿地质背景，对中国斑岩铜矿勘查工作具有重要参考价值。     

古亚洲洋与古特提斯洋关系初探

从板块构造研究中国古生代洋陆关系和构造-岩浆-成矿作用,离不开对古亚洲洋和古特提斯洋的关系判断,特别是对于中国西北部的研究,两个古生代大洋形成演化和关系是理清重要地质构造和成矿事件的关键。本文认为早古生代的原特提斯洋与古亚洲洋应连为一体,合称古亚洲-原特提斯洋,简称古亚洲洋。古亚洲洋是发育于早古生代劳亚大陆与冈瓦纳大陆之间的大洋,金川超大型铜镍矿床的形成是元古宙罗迪尼亚超大陆裂解三叉裂谷开启大洋的开始,塔里木陆块作为古亚洲洋南岸的一个陆块,早古生代的昆仑洋、祁连洋和秦岭洋只是古亚洲洋的分支或次生洋盆,这些次生洋盆于志留纪末闭合,古亚洲洋主洋则直到晚古生代泥盆纪末才闭合。石炭纪天山及邻区是古亚洲洋闭合后板块构造后碰撞机制与地幔柱作用提供热动力的两种地球动力学机制并存的构造背景,为大规模壳幔混合(染)岩浆作用和成矿爆发提供了可能。古特提斯洋是古亚洲洋在晚古生代的发展和继承,东昆仑夏日哈木超大型铜镍矿床的产生是冈瓦纳大陆北侧志留纪末破裂三叉裂谷开启大洋的开始,塔里木和华北等泛华夏陆块群构成了古特提斯洋北岸陆缘,石炭纪大洋形成,西昆仑玛尔坎苏大型优质锰矿可能就形成于大洋北侧被动大陆边缘的浅海或陆表海,成矿物质则很可能来自于同时代的大洋中脊。德尔尼大型铜钴矿为晚石炭世大洋中脊塞浦路斯型块状硫化物矿床。而铜峪沟大型铜矿和大场大型金矿等则分别为古特提斯洋消减俯冲岛弧岩浆作用矽卡岩-斑岩矿床和浅成低温热液矿床。中三叠世末古特提斯洋闭合。     

中国大陆地壳“镶嵌与叠覆”的结构特征及其演化

初步探讨了中国大陆地壳“块带镶嵌多层叠覆”的结构特征和多阶段的构造演化过程。中国大陆地壳新元古代中期以来的一级构造单元有中朝、塔里木、扬子、敦煌4个陆块和中央、西北、东北、西南、东南5个造山区(带)。中朝陆块的形成源于古元古代期间发生的古大陆裂解;扬子、塔里木和敦煌陆块的形成源于新元古代早期发生的古大陆裂解。西北造山区的形成源于古生代晚期洋盆关闭、大陆碰撞并叠加新生代陆内再造山;东北造山带的形成过程包括古生代碰撞造山及中生代增生、碰撞造山;中央造山带至三叠纪大陆碰撞才最后形成并叠加有新生代再造山;东南造山带的形成经历了古生代至新生代的多次造山作用;西南造山带主要是中—新生代造山作用的产物。这些单元都具有“块带镶嵌多层叠覆”的结构特征和多阶段构造演化的特点。中国大陆地壳的形成与演化可以划分为太古宙—古元古代、中元古代—新元古代早期、新元古代中期—古新世和始新世以来4个构造阶段,每个阶段都对应不同的超大陆裂解-聚合旋回。其中新元古代中期以来的地壳形成演化与全球洋陆格局中的古亚洲洋、古特提斯洋、古太平洋、特提斯洋和太平洋5个动力学体制有关,相应地可以归结为古亚洲、古特提斯、古太平洋、特提斯和太平洋5个造山域。正是这些多阶段的超大     

中国大陆地壳“镶嵌与叠覆“的结构特征及其演化

初步探讨了中国大陆地壳“块带镶嵌多层叠覆“的结构特征和多阶段的构造演化过程.中国大陆地壳新元古代中期以来的一级构造单元有中朝、塔里木、扬子、敦煌4个陆块和中央、西北、东北、西南、东南5个造山区(带).中朝陆块的形成源于古元古代期间发生的古大陆裂解;扬子、塔里木和敦煌陆块的形成源于新元古代早期发生的古大陆裂解.西北造山区的形成源于古生代晚期洋盆关闭、大陆碰撞并叠加新生代陆内再造山;东北造山带的形成过程包括古生代碰撞造山及中生代增生、碰撞造山;中央造山带至三叠纪大陆碰撞才最后形成并叠加有新生代再造山;东南造山带的形成经历了古生代至新生代的多次造山作用;西南造山带主要是中-新生代造山作用的产物.这些单元都具有“块带镶嵌多层叠覆“的结构特征和多阶段构造演化的特点.中国大陆地壳的形成与演化可以划分为太古宙-古元古代、中元古代-新元古代早期、新元古代中期-古新世和始新世以来4个构造阶段,每个阶段都对应不同的超大陆裂解-聚合旋回.其中新元古代中期以来的地壳形成演化与全球洋陆格局中的古亚洲洋、古特提斯洋、古太平洋、特提斯洋和太平洋5个动力学体制有关,相应地可以归结为古亚洲、古特提斯、古太平洋、特提斯和太平洋5个造山域.正是这些多阶段的超大陆裂解-聚合旋回及多个构造体制的叠加,形成了中国大陆地壳“块带镶嵌多层叠覆“的结构特征.     

超大陆和超大陆旋回、冈瓦纳组成及特提斯演化

本文对超大陆、超大陆旋回、冈瓦纳及特提斯问题进行了论述，认为陆块是不断组合、拼接与裂解和扩散的，也就是超大陆演化．这种演化过程与威尔逊旋回相关．冈瓦纳大陆在元古宙并未构成统一的大陆体．而是在元古宙末一古生代初才拼合成统一的冈瓦纳大陆．特提斯洋的发生、发展和消亡都与中国大陆各块体的发展与演化有着密切的关系．     

中国大陆地壳"镶嵌与叠覆"的结构特征及其演化

初步探讨了中国大陆地壳“块带镶嵌多层叠覆”的结构特征和多阶段的构造演化过程。中国大陆地壳新元古代中期以来的一级构造单元有中朝、塔里木、扬子、敦煌4个陆块和中央、西北、东北、西南、东南5个造山区(带)。中朝陆块的形成源于古元古代期间发生的古大陆裂解；扬子、塔里木和敦煌陆块的形成源于新元古代早期发生的古大陆裂解。西北造山区的形成源于古生代晚期洋盆关闭、大陆碰撞并叠加新生代陆内再造山；东北造山带的形成过程包括古生代碰撞造山及中生代增生、碰撞造山；中央造山带至三叠纪大陆碰撞才最后形成并叠加有新生代再造山；东南造山带的形成经历了古生代至新生代的多次造山作用；西南造山带主要是中-新生代造山作用的产物。这些单元都具有“块带镶嵌多层叠覆”的结构特征和多阶段构造演化的特点。中国大陆地壳的形成与演化可以划分为太古宙-古元古代、中元古代-新元古代早期、新元古代中期-古新世和始新世以来4个构造阶段，每个阶段都对应不同的超大陆裂解-聚合旋回。其中新元古代中期以来的地壳形成演化与全球洋陆格局中的古亚洲洋、古特提斯洋、古太平洋、特提斯洋和太平洋5个动力学体制有关，相应地可以归结为古亚洲、古特提斯、古太平洋、特提斯和太平洋5个造山域。正是这些多阶段的超大陆裂解-聚合旋回及多个构造体制的叠加，形成了中国大陆地壳“块带镶嵌多层叠覆”的结构特征。     

全球早古生代造山带(Ⅳ):板块重建与Carolina超大陆

古元古代与显生宙的板块构造特征和旋回演化过程具有明显区别,反映出地质记录为两种不同的板块构造体制。早古生代为这两个时期的过渡阶段,其构造过程研究与板块重建是地球板块构造旋回机制和周期分析的关键。本文采用综合集成的方法,在总结对比罗迪尼亚超大陆裂解以来全球早古生代主要碰撞造山带的地质事件基础上,分析早古生代碰撞造山带的演化特征,总结出与冈瓦纳大陆拼合、劳俄大陆拼合、古中华陆块群增生相关的7期碰撞-增生造山事件群:Brasiliano、东非、Kuunga、东亚与原特提斯洋和古亚洲洋演化相关的的加里东期造山事件、经典加里东造山、中欧加里东造山、Appalachian造山。再在这7期造山事件群基础上,结合古地磁、古生物、古地理等资料,重建了新元古代-早古生代末全球板块的拼合过程:罗迪尼亚超大陆从新元古代的~950 Ma开始经历了3个阶段裂解,此时存在泛大洋、莫桑比克洋和古太平洋3个大洋,随后615~560 Ma Iapetus洋打开,~560 Ma波罗的陆块与西冈瓦纳裂离导致狭窄的Ran洋打开;~540 Ma南半球Brasiliano、东非和Kuunga造山运动导致冈瓦纳大陆分阶段最终完成拼贴;~500 Ma冈瓦纳大陆北缘西段的微陆块群局部向北裂离,导致Rheic洋和Tornquist洋打开,并于~420 Ma随经典加里东造山带和中欧缝合带形成导致Iapetus洋闭合,此时斯瓦尔巴特和英国可能位于格陵兰地盾东南缘,同时冈瓦纳大陆北缘东段华北为代表的微陆块基本拼合在冈瓦纳大陆北缘;此外,虽然425 Ma西伯利亚板块有远离聚合了的劳俄大陆的趋势,但晚奥陶世-早泥盆世南美和北美板块靠近,北美板块与环冈瓦纳北缘西段的地体拼合碰撞。在大约400 Ma时,南、北美洲的混合生物群和古地理重建显示两者非常接近,因此,推测此时存在一个初始的逐步稳定的超大陆的可能,本文称为Carolina超大陆,因为Carolina造山带是这个超大陆最终拼合的地带。并据此判断超大陆旋回为7亿年。     

东亚原特提斯洋(Ⅱ):早古生代微陆块亲缘性与聚合

原特提斯洋内存在塔里木、中祁连、柴达木、扬子、华夏、印支、兰坪-思茅等诸多陆块/微陆块,多数陆块之间在早古生代晚期发育有蛇绿岩带或高压-超高压带。原特提斯域形成于从Rodinia裂解到Pangea超大陆集结期间,存在复杂的洋-陆格局和聚散过程。原特提斯洋不同陆块/微陆块属性和关系及其拼合过程是恢复重建Pangea超大陆聚合前构造背景的关键,但对其认识迄今还存在争论。因此,本文采用综合对比方法,以期建立原特提斯洋陆块/微陆块的亲缘性和海-陆格局,厘定原特提斯微陆块拼合时序与方式。结果表明,早古生代早期除华北陆块不具有亲冈瓦纳大陆的特征外,扬子、华夏、塔里木、柴达木、阿拉善、北秦岭-中祁连-中阿尔金、欧龙布鲁克、北羌塘、南羌塘、拉萨、兰坪-思茅、印支等陆块/微陆块都具有亲冈瓦纳的特征。在450~400Ma左右这一系列陆块/微陆块都向南俯冲-增生,并逐步拼合于冈瓦纳大陆北缘东段,原特提斯洋关闭,并形成了原潘吉亚(Proto-Pangea)超大陆;原潘吉亚于380Ma以后裂离出塔里木-华北陆块和大华南陆块,分别出现勉略洋和古特提斯洋,直到240~220Ma逐步向北聚合,形成最终的劳亚古陆,此时才形成潘吉亚超大陆。     

Petroliferous basins at continental margins of paleozoic paleoseas: Communication 2. Petroliferous basins at continental margins in the Rheic, Uralian, and Central Asian paleoseas

The continental block of the Earth’s crust was separated in the Paleozoic into two unequal parts: (i) huge supercontinent Gondwana located at high latitudes of the Southern Hemisphere and (ii) several small continents (Laurentia, Baltica, Siberia, Kazakhstan, South Chinese block, and North Chinese blocks) located at low latitudes south and north of the equator. Morphology of the Paleozoic seas between these blocks was subjected to changes (expansion and contraction) with time. Their closure was provoked by several orogenic (Taconian, Caledonian, Acadian, and Hercynian) phases. At present, relicts of these ancient orogenic structures extend as belts along the boundaries of many petroliferous basins and record the position of past seas. One of the oldest oil-and-gas deposition belts, which appeared in southern Iapetus in the Precambrian/Phanerozoic, was confined to a passive margin of Gondwana. In the Early Paleozoic, small blocks of the continental crust (Avalonia, Armorica, Perunica, Iberica, and others) were successively detached from the passive margin. This process was accompanied by the opening of a new deep basin (Rheic Sea or Paleotethys). The Uralian and Central Asian paleoseas were formed approximately at the same time. Many petroliferous basins existing now were located in the Paleozoic at the margins of these paleoseas.     

Neoproterozoic evolution of Rodinia: constraints from new paleomagnetic data on the western margin of the Siberian craton

The paper summarizes paleomagnetic results obtained from the Neoproterozoic rocks of the western margin of the Siberian craton. On the basis of the obtained paleomagnetic poles and available paleomagnetic data for the Precambrian of Siberia, a new version of the Neoproterozoic segment of the apparent polar wandering path (APWP) is proposed for the craton and is compared with the Laurentian APWP. The superposition of these paths suggests that in the Neoproterozoic the southern margin of the Siberian craton (in modern coordinates) faced the Canadian margin of Laurentia. Most likely, in the end of the Mesoproterozoic and during the Neoproterozoic the Siberian craton and Laurentia were connected to form the supercontinent Rodinia. At 1 Ga the western margin of the Siberian craton was a northern (in modern coordinates) continuation of the western margin of Laurentia. The available paleomagnetic data on Laurentia and continental blocks of Eastern Gondwana (Australia, Antarctica, India, South China) and the proposed APWP trend allowed a new model for the breakup of this segment of Rodinia. Analysis of a total of the data available suggests that strike-slip movements on the background of the progressive opening of the oceanic basin between Siberia and Laurentia were predominant in the south of the Siberian craton during the Neoproterozoic. Similar kinematics is typical of the western margin of Laurentia, where strike-slip motions are probably associated with the progressive opening of the ocean basin between Laurentia and eastern Gondwana.     

Paleozoic terranes of eastern Australia and the drift history of Gondwana

Critical assessment of Paleozoic paleomagnetic results from Australia shows that paleopoles from locations on the main craton and in the various terranes of the Tasman Fold Belt of eastern Australia follow the same path since 400 Ma for the Lachlan and Thomson superterranes, but not until 250 Ma or younger for the New England superterrane. Most of the paleopoles from the Tasman Fold Belt are derived from the Lolworth-Ravenswood terrane of the Thomson superterrane and the Molong-Monaro terrane of the Lachlan superterrane. Consideration of the paleomagnetic data and geological constraints suggests that these terranes were amalgamated with cratonic Australia by the late Early Devonian. The Lolworth-Ravenswood terrane is interpreted to have undergone a 90° clockwise rotation between 425 and 380 Ma. Although the Tamworth terrane of the western New England superterrane is thought to have amalgamated with the Lachlan superterrane by the Late Carboniferous, geological syntheses suggest that movements between these regions may have persisted until the Middle Triassic. This view is supported by the available paleomagnetic data. With these constraints, an apparent polar wander path for Gondwana during the Paleozoic has been constructed after review of the Gondwana paleomagnetic data. The drift history of Gondwana with respect to Laurentia and Baltica during the Paleozoic is shown in a series of paleogeographic maps.     

http://www.sciencedirect.com/science/article/pii/S1674987111001113

The Rheic Ocean was one of the most important oceans of the Paleozoic Era.It lay between Laurentia and Gondwana from the Early Ordovician and closed to produce the vast Ouachita-Alleghanian -Variscan orogen during the assembly of Pangea.Rifting began in the Cambrian as a continuation of Neoproterozoic orogenic activity and the ocean opened in the Early Ordovician with the separation of several Neoproterozoic arc terranes from the continental margin of northern Gondwana along the line of a former suture.The rapid rate of ocean opening suggests it was driven by slab pull in the outboard lapetus Ocean.The ocean reached its greatest width with the closure of lapetus and the accretion of the periGondwanan arc terranes to Laurentia in the Silurian.Ocean closure began in the Devonian and continued through the Mississippian as Gondwana sutured to Laurussia to form Pangea.The ocean consequently plays a dominant role in the Appalachian-Ouachita orogeny of North America,in the basement geology of southern Europe,and in the Paleozoic sedimentary,structural and tectonothermal record from Middle America to the Middle East.Its closure brought the Paleozoic Era to an end.     

Gondwana dispersion and Asian accretion: Tectonic and palaeogeographic evolution of eastern Tethys

Present-day Asia comprises a heterogeneous collage of continental blocks, derived from the Indian–west Australian margin of eastern Gondwana, and subduction related volcanic arcs assembled by the closure of multiple Tethyan and back-arc ocean basins now represented by suture zones containing ophiolites, accretionary complexes and remnants of ocean island arcs. The Phanerozoic evolution of the region is the result of more than 400 million years of continental dispersion from Gondwana and plate tectonic convergence, collision and accretion. This involved successive dispersion of continental blocks, the northwards translation of these, and their amalgamation and accretion to form present-day Asia. Separation and northwards migration of the various continental terranes/blocks from Gondwana occurred in three phases linked with the successive opening and closure of three intervening Tethyan oceans, the Palaeo-Tethys (Devonian–Triassic), Meso-Tethys (late Early Permian–Late Cretaceous) and Ceno-Tethys (Late Triassic–Late Cretaceous). The first group of continental blocks dispersed from Gondwana in the Devonian, opening the Palaeo-Tethys behind them, and included the North China, Tarim, South China and Indochina blocks (including West Sumatra and West Burma). Remnants of the main Palaeo-Tethys ocean are now preserved within the Longmu Co-Shuanghu, Changning–Menglian, Chiang Mai/Inthanon and Bentong–Raub Suture Zones. During northwards subduction of the Palaeo-Tethys, the Sukhothai Arc was constructed on the margin of South China–Indochina and separated from those terranes by a short-lived back-arc basin now represented by the Jinghong, Nan–Uttaradit and Sra Kaeo Sutures. Concurrently, a second continental sliver or collage of blocks (Cimmerian continent) rifted and separated from northern Gondwana and the Meso-Tethys opened in the late Early Permian between these separating blocks and Gondwana. The eastern Cimmerian continent, including the South Qiangtang block and Sibumasu Terrane (including the Baoshan and Tengchong blocks of Yunnan) collided with the Sukhothai Arc and South China/Indochina in the Triassic, closing the Palaeo-Tethys. A third collage of continental blocks, including the Lhasa block, South West Borneo and East Java–West Sulawesi (now identified as the missing “Banda” and “Argoland” blocks) separated from NW Australia in the Late Triassic–Late Jurassic by opening of the Ceno-Tethys and accreted to SE Sundaland by subduction of the Meso-Tethys in the Cretaceous.     

Black shales and other sediments with high organic matter contents in Phanerozoic climatic cycles: Communication 2. Black shales during the Pangea existence

According to recent concepts, the Earth surface was permanently transformed during its geological history. Some stages of its evolution were marked by the convergence of separate continental blocks to result in the formation of supercontinents, which resisted successfully centrifugal processes. Other stages were characterized by the opposite tendency: after their long existence, the supercontinents became disintegrated into several large and small blacks, the motion of which was accompanied by opening of new sea basins and closure of former basins with the oceanic crust. The second half of the Paleozoic was marked by amalgamation of large continental blocks. In the Devonian, collision between Laurentia and Baltica culminated in the formation of the Euroamerica continent. After the closure of the Ural paleocean in the terminal Carboniferous–initial Permian, it was united with the Siberian and Kazakhstan continental blocks. These events provided the prerequisites for the formation of a new supercontinent (Pangea), which acquired its final configuration at the end of the Permian. One of its segments located mainly south of the equator included Gondwana. Another segment located northward included Euroamerica, Kazakhstan, Siberian, and two China continental blocks. During its geological history, Pangea suffered many dramatic events including several extinctions of organisms. The most significant event took place in the terminal Permian–initial Triassic and at the transition between the Triassic and Jurassic periods.     

Chinese Continental Blocks in Global Paleocontinental Reconstruction during Paleozoic and Mesozoic

The Cambrian to Cretaceous paleomagnetic data from Chinese continental and adjacent blocks were collected using principles to obtain reliable and high-precision paleomagnetic data and to pay attention to the similarity of paleobiogeography and the coordination of tectonic evolution. The Chinese continental blocks were laid up on the reconstruction of proposed global paleocontinents with almost the same scale. Thus, it can be clearly recognized that the global continents, including Chinese continental blocks, range along latitudes on the southern side of the equator during the Early Paleozoic. In the Paleozoic, Chinese continental blocks were still located among the Laurentia, Siberia and Gondwana plates, following the fast moving of the Siberia Plate northwards, the amalgamation in a north-south direction at the western parts of the Laurentia and Gondwana plates, and the Iapetus and Rheic Oceans were subducted, eventually to form a uniform Pangea in the Late Paleozoic. The Australian and Indian plates of Eastern Gondwana moved and dispersed gradually southwards, continued to extend the Paleo-Tethys Ocean. The Chinese continental and adjacent blocks were still located in the Paleo-Tethys Ocean, preserved the status of dispersion, gradually moving northwards, showing characteristics of ranging along a north–south orientation until the Permian. In addition, a series of local collisions happened during the Triassic, and consequently most of the Chinese continental blocks were amalgamated into the Pangea, except for the Gangdise and Himalayan blocks. There was a counter-clockwise rotation of the Eastern Asian continent in the Jurassic and northwards migration of the Chinese continent in varying degrees during the Cretaceous, but the Himalayan and Indian plates did not collide into the Chinese continent during this period.     

特提斯地球动力学

特提斯是地球显生宙期间位于北方劳亚大陆和南方冈瓦纳大陆之间的巨型海洋,它在新生代期间的闭合形成现今东西向展布的欧洲阿尔卑斯山、土耳其-伊朗高原、喜马拉雅山和青藏高原。根据演化历史,特提斯可划分为原特提斯、古特提斯和新特提斯三个阶段,分别代表早古生代、晚古生代和中生代期间的大洋。大约在500Ma左右,冈瓦纳大陆北缘发生张裂,裂解的块体向北漂移,并使其与塔里木-华北之间的原特提斯洋在420～440Ma左右关闭,产生原特提斯造山作用,与北美-西欧地区Avalonia地体与劳伦大陆之间的阿巴拉契亚-加里东造山作用基本相当。原特提斯造山带之南、早古生代即已存在的龙木错-双湖-昌宁-孟连古特提斯洋在380Ma向北俯冲,使早期闭合的康西瓦-阿尼玛卿洋重新张开,并由于弧后扩张形成金沙江-哀牢山洋。330～360Ma左右,特提斯西部大洋由于南侧非洲板块和北侧欧洲板块的碰撞而关闭,形成欧洲华力西造山带。而特提斯东段的上述三条古特提斯洋在250Ma左右基本同时关闭,华北、华南、印支等块体聚合形成华夏大陆。该大陆与冈瓦纳大陆、劳亚大陆和华力西造山带一起围限形成封闭的古特提斯残留洋,并一直到晚三叠世-早侏罗世海水才全部退出。此后,南侧冈瓦纳大陆在三叠纪晚期重新裂解形成新特提斯洋,该洋盆在新生代初期由于印度和亚洲的碰撞而关闭。原、古、新特提斯三次造山作用基本代表了中国大陆显生宙期间的地质演化历史,并在此过程中形成了特色的特提斯域金属成矿作用。广布的被动陆缘和赤道附近的古地理位置,以及后期的造山作用同时也成就了特提斯域内巨量油气资源的形成;塑就的地貌与海陆分布格局,也对当时的古气候与古环境产生了重要影响。特别是,与原、古、新特提斯洋消亡相关的三次弧岩浆活动与显生宙地球历史上三次温室地球向冰室地球的转变,在时间上高度吻合。上述演化历史同时还表明,特提斯地质演化以南侧冈瓦纳大陆不断裂解、块体向北漂移并与劳亚大陆持续聚合为特征,其动力机制主要来自俯冲板片的拖拽力,而地幔柱是否对大陆的裂解与漂移有所贡献,则有待进一步评价。