四川盆地中—新生代盆—山结构与油气分布
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摘要
盆-山结构及其动力学过程是21世纪大陆动力学研究重要的基本内容之一，也是中生代以来中国西部大陆构造的基本格局。四川盆地地处青藏高原东缘特提斯-喜马拉雅构造域和滨西太平洋构造域的交接转换部位。它既是沉积盆地和构造盆地，又是地貌盆地，盆地与周缘造山带构成一个典型的复合盆-山结构体系。本论文运用构造地质学、低温热年代学、地球化学等理论和技术方法，以“结构-构造-油气分布”为主线，将盆-山结构、构造演化与周缘板块围限多动力背景结合起来，分析中-新生代四川盆地沉积充填、抬升剥蚀与周缘造山带构造演化、扩展变形等关系，建立四川盆地多盆-山体系结构-构造格架，探讨不同盆-山结构与盆内浅部地表过程（如：构造变形、隆升剥露、沉积充填、流体活动等）差异性，揭示盆-山结构与油气分布关系。论文取得了如下主要成果与认识：
（1）基于四川盆地及周缘造山带不同地质结构、构造和热隆升-沉降过程等，将其分为板缘（龙门山、米仓山和大巴山）突变型盆-山结构和板内（齐岳山、大娄山和大凉山）渐变型盆-山结构两类。
板缘突变型盆-山结构具有显著深部结构差异性，浅部构造形成典型的冲断带（山）和前陆盆地（盆）二元结构；结构-构造上具明显的倾向上分带、走向上分段及垂向上分层性，构造演化上具倾向上前展性（和/或走向上扩展性）、造山带隆升剥蚀和盆内坳陷沉降-沉积具典型耦合特征；现今山-盆地貌反差大、地形坡度陡、盆-山边界明晰。板缘突变型盆-山耦合关系主要受控于差异性深部结构及其造山带的形成演化过程。如：龙门山-川西前陆突变型盆-山结构带晚三叠世-早侏罗世沉积中心沿走向迁移与砾岩展布特征、不整合界面走向迁移等具有明显的等时性和一致性，揭示出盆-山结构带倾向上前展式扩展和走向上分段式递进性（或序次性）的三维盆山耦合空间演化趋势。
板内渐变型盆-山结构具相似的深部结构特征和挤压-坳陷结构的浅部构造特征，不发育冲断推覆和前陆盆地；结构和构造上分带性、分段性不明显，不存在典型而明显的边界控制断裂（系），具有相似弥散式挤压褶皱变形特征，盆缘造山带隆升剥蚀和盆内坳陷沉降-沉积不具耦合特征；现今山-盆地貌反差小、盆-山边界不清、盆-山为渐变过渡关系。板内渐变型盆-山结构主要受控于（盆缘或盆外）邻区构造扩展变形过程和盆内沉积盖层多层次滑脱变形过程。如：大娄山渐变型盆山结构带不具明显的东、西分段和倾向分带性特征，多期叠加构造特征揭示受雪峰陆内造山系统控制。
（2）长波长、低起伏度渐变型盆-山地貌地区构造变形与浅表等温面挠曲具多种端元模型，基于单一结构上多系统低温热年代学特征揭示隆升剥露过程和褶皱变形相关事件。大凉山渐变型盆-山结构带单一背斜结构上（或典型花岗岩体）锆石和磷灰石(U-Th)/He年龄、磷灰石裂变径迹年龄与重建结构深度关系图（或海拔高程）关系研究表明，川西南地区主体构造格架变形事件发生于古新世末期-始新世早期（~40Ma），随后区域发生持续的抬升剥蚀作用。四川盆地东南缘及南缘地区~10Ma以前经历长时间的缓慢抬升冷却过程，速率大致为~0.15mm/yr，随后发生加速抬升冷却事件，其剥露速率为~0.3-0.8mm/yr。现今大凉山地区地表抬升剥蚀量约为~3-5km，四川盆地西南地区地表抬升剥蚀量约为~1-2km。它们共同揭示出晚新生代青藏高原沿鲜水河-小江断裂系走滑边界的东向扩展变形作用最终决定着大凉山渐变型盆-山结构区的快速隆升剥露过程。
（3）利用钻井和地表样品低温热年代学手段（AFT、(U-Th)/He）和数字热模型等手段，揭示四川盆地区域晚中、新生代阶段性构造抬升剥露过程及刚性基底结构与盆-山结构对其抬升剥蚀过程的复合-联合控制作用。
盆地区域（尤其是盆内华蓥山和川西前陆地区）的磷灰石裂变径迹（AFT）研究揭示，四川盆地区域具有阶段性沉降-隆升剥露过程，即早期沉积后沉降埋深阶段（~80Ma以前）、中期缓慢抬升冷却（80~20Ma）和晚期快速抬升剥露阶段（~20Ma-现今）。盆地中心及西北部地区（华蓥山断裂带北西）具显著的磷灰石裂变径迹年龄环带中心，体现出盆地中心（原地隆起区）及盆地西北地区（川北突变型盆-山结构区）较低的抬升剥蚀作用，它与区域空间上较弱的构造变形作用具有明显的耦合关系。
AFT热模型及连续井剖面镜质体特征揭示盆地晚中-新生代地表抬升剥蚀总厚度普遍大于~2000-3000m，新近纪快速抬升剥蚀幅度普遍大于~1000m。晚中-新生代隆升剥蚀总幅度体现出板缘突变型盆-山结构区最低、盆地腹地次之、板内渐变型盆-山结构区最大的特征。同时，盆地空间上由北东向南西具AFT年龄逐渐变小、径迹长度逐渐增大、新生代平均剥露速率逐渐增大的趋势。它们共同揭示盆地基底结构与盆缘造山带对盆地抬升剥蚀过程的复合-联合控制作用。
（4）根据四川盆地与环盆造山带的不同盆-山结构、构造变形及其建造定型过程等主要控制因素，将四川盆地复合盆-山体系划分为五大盆-山结构分区：Ⅰ区-川北突变型盆山结构区（秦岭构造控制域）、Ⅱ区-川西突变型盆山结构区（青藏构造控制域）、Ⅲ区-川东渐变盆山结构区（雪峰构造控制域）、Ⅳ区-川西南渐变型盆山结构区（雪峰-青藏-基底构造联合控制域）和Ⅴ区-川中原地隆起-盆地区（基底构造控制域）。受不同构造变形域控制，环四川盆地各盆-山结构区构造格架定型期总体体现出北西、北和北东边界早、东边界较晚、西南边界最晚（川北突变型盆-山结构区→川东渐变型盆-山结构区→川西南渐变型盆-山结构区）。四川盆地浅部地貌和结构-构造变形及其演化特征等主要受控于盆缘不同盆-山结构与盆地基底结构的联合-复合控制作用。
（5）基于不同盆-山结构变形作用、差异抬升剥蚀过程等与流体活动特性研究，揭示四川盆地盆-山结构通过褶皱冲断变形和稳态抬升剥蚀作用的复合-联合作用过程控制着流体活动特性及其保存条件，从而控制和制约着盆地现今油气分布。
不同构造变形、抬升剥蚀作用等特征的盆山结构区（古）流体活动特征研究表明，板缘突变型盆-山结构带体现出强冲断作用与浅部流体垂向跨层和深部流体侧向运移活动的特性；渐变型盆-山结构带具与多层次滑脱褶皱变形相关的贯通裂缝系统渗流生长形成与流体垂向跨层运移特征。强构造变形区域，受控于盆缘造山带向盆地的扩展变形过程，以褶皱冲断构造变形为主控制和影响流体活动特性；受盆地刚性基底结构控制的盆内弱构造变形带以稳态抬升剥蚀作用为主控制和影响流体活动特性。由于地表浅部Brown-Hoek应力模式和/或构造变形作用影响，强、弱隆升剥蚀作用过程对区内流体和油气具有明显不同的能量场和再运聚影响。强隆升剥蚀作用过程中，不同岩石破裂行为特征的非连续性结构叠加改造，导致大规模流体幕式跨层流动和降温-降压的流体沸腾作用，油气保存条件破坏。弱隆升剥蚀作用过程中（贯通）裂缝系统的发育对流体活动性、连通性和油气调整聚集成藏具至关重要的作用，因而次生油气藏普遍体现出与裂缝系统具有较高的关联性。
盆-山结构主要通过构造变形强度、地表抬升剥蚀作用和陆相地层展布因素控制和影响盆地现今区域保存条件。四川盆地晚三叠世以来（残存）陆相碎屑岩较厚沉积地区（大于~3000m）主要分布在盆地西北及北部突变型盆-山结构区，（残存）陆相沉积厚度与晚三叠世以来的不同时期沉积中心相叠置，受控于环盆地不同突变型盆-山结构带中-新生代差异构造变形活动，具有较低的构造变形作用强度和晚-中新生代抬升剥蚀总厚度。因此，四川盆地现今（残存）大中型油气藏(田)和天然气的大部分主要分布于板缘突变型盆-山结构区(尤其是秦岭构造控制域)和川中原地隆起-盆地区（基底构造控制域）。
The basin-mountain systems and its geodynamics is one of the importantcomponents of the continential dynamics and was subject of tectonic studies inwestern China. The Sichuan basin located the eastern margin of the Tibetan Plateau ata transfer zone between the Tethys-Himalaya domain and the western Pacific domainis a complex sedimentary, tectonic and topographic basin. The basin and its peripheralmountains comprise composite basin-mountain system. This study uses structures,lower-temperature thermochronology, geochemistry etc., to document the relationshipbetween the basin-mountain system and the oil/gas distribution in the Sichuan basin.
(1) The composite basin-mountain system in the Sichuan basin and its peripheralmountains can be divided into two types-margin-plate systems and interior-platesystems.
The margin-plate basin-mountain systems include the Sichuan basin and itssurrounding Longmen Mountains, Micang Mountains and Daba Mountains. All ofthose are located at the western and northern marginal area of the Sichuan basin,representing the western margin of the Yangtze plate (South China Block). Themargin-plate basin-mountain systems，with binary units of large-scale thrust belts andforeland basins, have different deep lithospheric structures, abrupt boundaries andlarge contrast in today’s geomorphology. The coupling of the foreland basins andadjacent mountains is chiefly controlled by the diversity in the lithospheric structure.Sedimentary data from field and borehole investigations allow reconstruction of thesouthwesterly variations in proximal sedimentary processes along the Longmenshanthrust belt during Late Triassic and Early Jurassic and their relation to thedevelopment of a transpression basin.
In contrast, the interior-plate basin-mountain systems represented by the Sichuan basin and its adjacent interior-plate Qiyue Mountains, Dalou Mountains and DaliangMountains; located within the Yangtze plate, represent the eastern and southernmarginal area of the Sichuan basin. Due to gradual boundaries in shallow structureand similar deep lithospheric structure, the interior-plate basin-mountain systems lackof large-scale thrust belts and thrust-loaded foreland basins. The coupling of the basin(Sichuan basin) and the interior-plate mountains largely depends on the degree ofdeformation of the interior-plate mountains and multi-layer detachments in thesedimentary cover of the basin. For example, the superimposed structures indicate thatthe Daloushan basin-mountain system has experienced multistage build-up episodesunder the control of Xuefeng intercontinental orogen, accompanied by the northwardpartition of the Paleo-Yangtze basin.
(2) Due to different models between folding and deflected isotherm withinlow-relief and long-wavelength topography in the interior-plate basin-mountainsystems, it could unravel the processes of uplift/exhumation and folding deformationby multi-system lower-temperature thermochronology at a fold or anticline.
New apatite and zircon (U-Th)/He thermochronometry results using the age vs.elevation/structural depth relationship in the Daliang Mountains, support that,(1)cooling and exhumation with apparent rates of~0.15mm/yr from~30to~10Ma, waspervasive across the region after the build-up time of the orogen,(2) a differentexhumation occurred at the Daliang Mountains and southwestern part of the Sichuanbasin; the former has~3-5km exhumation magnitude while the latter~1-2kmexhumation, and (3) Late Cenozoic eastward growth of the Tibetan Plateau controlledthe rapid post~10Ma cooling and denudation, with rates of~0.4-0.8mm/yr in theDaliang Mountains.
(3) Based on the lower-temperature thermochronology and thermal models, it issuggested that there were different uplift and exhumation processes across theSichuan basin, controlled by a coupling between basement and compositebasin-mountain systems.
Modeled temperature-time histories and the Boomerang plot of AFT datasetacross the Sichuan basin suggest two-stage cooling and exhumation processes. Afterreaching their maximum burial depth during120~80Ma, it was followed significantacceleration in cooling rate during last20~10Ma. In particular, nested old-age centerseparated by Huayun Mts. was found in the center-to-northwest part of the Sichuanbasin, coupled with the low-grade deformation in the basin center. It indicatessignificant change in exhumation (at least~2000m) across the Huayun Mts.
The magnitude of exhumation across the Sichuan basin was more than~2000-3000m since the Late Cretaceous, while more than1000m in the Neogene. Ingeneral, the lowest exhumation area is located at the margin-plate basin-mountainsystems, while the largest exhumation area is at the interior-plate basin-mountainsystems. The exhumation in the basin center have magnitude averaging betweent thethe latter two. A simplified one-dimensional, steady-state solution model wasdeveloped to calculate the mean exhumation rate, which is0.05~0.2mm/yr in mostof the basin. It suggests slow uplift and exhumation across much of the basin. Theregional pattern of AFT age, length and erosion rate support a progressive changefrom the nested old-age center towards the southwest. This pattern supports theprolonged, steady-state uplift and exhumation across the basin, controlled by cratonicbasin structure. The eastern growth of the Tibetan Plateau has exerted significantcontrol on the rapid exhumation of the southwestern part of the Sichuan basin, but noton all of the basin during the Late Cenozoic.
(4) Considering the different features such as structure, deformation, evolutionand dynamics etc., the Sichuan basin can be subdivided into five units.
Unit I-North Sichuan margin-plate basin-mountain system (under the control ofQinling orogen), Unit II-West Sichuan margin-plate basin-mountain system (underthe control of Tibetan Plateau), Unit III-East Sichuan interior-plate basin-mountainsystem (under the control of Xuefeng orogen), Unit IV-SW Sichuan interior-platebasin-mountain system (under a composite control of Xuefeng orogen, TibetanPlateau and basement structures), Unit V-Central Sichuan interior-plate uplift (underthe control of basement structures). Due to different dynamics, these five units havedifferent build-up time; the Unit I has been formed during the Late Yanshanian, theUnit II and III during the Himalayan period, and the Unit IV during Late Cenozoic.Thus, the evolution of the basin and its topography are controlled by couplingprocesses between basement structures and composite basin-mountain systems of theSichuan basin.
(5) The basin-mountain systems in the Sichuan basin exert major control ontoday’s oil/gas distribution across the basin chiefly by their controlling influence onthe fluid flow and petroleum reservoirs preservation. It is controlled by the couplingprocesses between the steady-state uplift and exhumation and the thrusting andfolding deformation.
The margin-plate basin-mountain system with strong thrusting deformation, ischaracteristic by vertically throughgoing fluid flow in shallow system, and lateral fluid flow in the deep system. Whilest the interior-plate basin-mountain system ischaracteristic by throughgoing fluid flow closely correlated with a percolating clustermodel of veins. In general, the fluid flow is controlled by the thrusting and folding.However, the fluid flow shows a close correlationship with the steady state uplift andexhumation in the basin center under control of a basement.
The strong uplift and exhumation with a magnitude larger than~3000-4000m,exerts major control on the energy change and accumulation of fluid and oil/gas.During the progressive uplift and exhumation, the shallow strata attained differenttypes of fractures and joints, etc. that formed under different stress-strain regimewithin shallow and/or deep depth. The connection among different types of fractureand joint resulted in multistage fluid flow with boiling features, and finally in adestraction of petroleum reservoirs. Presence of fractures and joints have significantinfluence on the fluid flow, its connectivity and accumulation. There is a goodcorrelation betweent the gas field and fractures in the Sichuan basin, with fieldspreferentially located in an areas of a weak uplift and low exhumation.
The tectonics, terrestrial strata distribution and the late Mesozoic-Cenozoic upliftaccompanied by denudation, control the regional conditions for natural gas reservoirpreservation in the Sichuan basin. The foreland basins of the margin-platebasin-mountain systems contain (more than3000m) thick T3—K terrestrialsedimentary strata, controlled by tectonics and formation of the basin-mountainsystems. These strata were subjected only to a low degree of uplift and denudationand to weak tectonic deformation, which resulted in good preservation of oil/gasreservoirs. Therefore, today’s natural gas proven reserves and medium-large sizenatural gas fields in Sichuan basin are mainly located within the foreland basins at themargin-plate basin-mountain systems.
（1）基于四川盆地及周缘造山带不同地质结构、构造和热隆升-沉降过程等，将其分为板缘（龙门山、米仓山和大巴山）突变型盆-山结构和板内（齐岳山、大娄山和大凉山）渐变型盆-山结构两类。
板缘突变型盆-山结构具有显著深部结构差异性，浅部构造形成典型的冲断带（山）和前陆盆地（盆）二元结构；结构-构造上具明显的倾向上分带、走向上分段及垂向上分层性，构造演化上具倾向上前展性（和/或走向上扩展性）、造山带隆升剥蚀和盆内坳陷沉降-沉积具典型耦合特征；现今山-盆地貌反差大、地形坡度陡、盆-山边界明晰。板缘突变型盆-山耦合关系主要受控于差异性深部结构及其造山带的形成演化过程。如：龙门山-川西前陆突变型盆-山结构带晚三叠世-早侏罗世沉积中心沿走向迁移与砾岩展布特征、不整合界面走向迁移等具有明显的等时性和一致性，揭示出盆-山结构带倾向上前展式扩展和走向上分段式递进性（或序次性）的三维盆山耦合空间演化趋势。
板内渐变型盆-山结构具相似的深部结构特征和挤压-坳陷结构的浅部构造特征，不发育冲断推覆和前陆盆地；结构和构造上分带性、分段性不明显，不存在典型而明显的边界控制断裂（系），具有相似弥散式挤压褶皱变形特征，盆缘造山带隆升剥蚀和盆内坳陷沉降-沉积不具耦合特征；现今山-盆地貌反差小、盆-山边界不清、盆-山为渐变过渡关系。板内渐变型盆-山结构主要受控于（盆缘或盆外）邻区构造扩展变形过程和盆内沉积盖层多层次滑脱变形过程。如：大娄山渐变型盆山结构带不具明显的东、西分段和倾向分带性特征，多期叠加构造特征揭示受雪峰陆内造山系统控制。
（2）长波长、低起伏度渐变型盆-山地貌地区构造变形与浅表等温面挠曲具多种端元模型，基于单一结构上多系统低温热年代学特征揭示隆升剥露过程和褶皱变形相关事件。大凉山渐变型盆-山结构带单一背斜结构上（或典型花岗岩体）锆石和磷灰石(U-Th)/He年龄、磷灰石裂变径迹年龄与重建结构深度关系图（或海拔高程）关系研究表明，川西南地区主体构造格架变形事件发生于古新世末期-始新世早期（~40Ma），随后区域发生持续的抬升剥蚀作用。四川盆地东南缘及南缘地区~10Ma以前经历长时间的缓慢抬升冷却过程，速率大致为~0.15mm/yr，随后发生加速抬升冷却事件，其剥露速率为~0.3-0.8mm/yr。现今大凉山地区地表抬升剥蚀量约为~3-5km，四川盆地西南地区地表抬升剥蚀量约为~1-2km。它们共同揭示出晚新生代青藏高原沿鲜水河-小江断裂系走滑边界的东向扩展变形作用最终决定着大凉山渐变型盆-山结构区的快速隆升剥露过程。
（3）利用钻井和地表样品低温热年代学手段（AFT、(U-Th)/He）和数字热模型等手段，揭示四川盆地区域晚中、新生代阶段性构造抬升剥露过程及刚性基底结构与盆-山结构对其抬升剥蚀过程的复合-联合控制作用。
盆地区域（尤其是盆内华蓥山和川西前陆地区）的磷灰石裂变径迹（AFT）研究揭示，四川盆地区域具有阶段性沉降-隆升剥露过程，即早期沉积后沉降埋深阶段（~80Ma以前）、中期缓慢抬升冷却（80~20Ma）和晚期快速抬升剥露阶段（~20Ma-现今）。盆地中心及西北部地区（华蓥山断裂带北西）具显著的磷灰石裂变径迹年龄环带中心，体现出盆地中心（原地隆起区）及盆地西北地区（川北突变型盆-山结构区）较低的抬升剥蚀作用，它与区域空间上较弱的构造变形作用具有明显的耦合关系。
AFT热模型及连续井剖面镜质体特征揭示盆地晚中-新生代地表抬升剥蚀总厚度普遍大于~2000-3000m，新近纪快速抬升剥蚀幅度普遍大于~1000m。晚中-新生代隆升剥蚀总幅度体现出板缘突变型盆-山结构区最低、盆地腹地次之、板内渐变型盆-山结构区最大的特征。同时，盆地空间上由北东向南西具AFT年龄逐渐变小、径迹长度逐渐增大、新生代平均剥露速率逐渐增大的趋势。它们共同揭示盆地基底结构与盆缘造山带对盆地抬升剥蚀过程的复合-联合控制作用。
（4）根据四川盆地与环盆造山带的不同盆-山结构、构造变形及其建造定型过程等主要控制因素，将四川盆地复合盆-山体系划分为五大盆-山结构分区：Ⅰ区-川北突变型盆山结构区（秦岭构造控制域）、Ⅱ区-川西突变型盆山结构区（青藏构造控制域）、Ⅲ区-川东渐变盆山结构区（雪峰构造控制域）、Ⅳ区-川西南渐变型盆山结构区（雪峰-青藏-基底构造联合控制域）和Ⅴ区-川中原地隆起-盆地区（基底构造控制域）。受不同构造变形域控制，环四川盆地各盆-山结构区构造格架定型期总体体现出北西、北和北东边界早、东边界较晚、西南边界最晚（川北突变型盆-山结构区→川东渐变型盆-山结构区→川西南渐变型盆-山结构区）。四川盆地浅部地貌和结构-构造变形及其演化特征等主要受控于盆缘不同盆-山结构与盆地基底结构的联合-复合控制作用。
（5）基于不同盆-山结构变形作用、差异抬升剥蚀过程等与流体活动特性研究，揭示四川盆地盆-山结构通过褶皱冲断变形和稳态抬升剥蚀作用的复合-联合作用过程控制着流体活动特性及其保存条件，从而控制和制约着盆地现今油气分布。
不同构造变形、抬升剥蚀作用等特征的盆山结构区（古）流体活动特征研究表明，板缘突变型盆-山结构带体现出强冲断作用与浅部流体垂向跨层和深部流体侧向运移活动的特性；渐变型盆-山结构带具与多层次滑脱褶皱变形相关的贯通裂缝系统渗流生长形成与流体垂向跨层运移特征。强构造变形区域，受控于盆缘造山带向盆地的扩展变形过程，以褶皱冲断构造变形为主控制和影响流体活动特性；受盆地刚性基底结构控制的盆内弱构造变形带以稳态抬升剥蚀作用为主控制和影响流体活动特性。由于地表浅部Brown-Hoek应力模式和/或构造变形作用影响，强、弱隆升剥蚀作用过程对区内流体和油气具有明显不同的能量场和再运聚影响。强隆升剥蚀作用过程中，不同岩石破裂行为特征的非连续性结构叠加改造，导致大规模流体幕式跨层流动和降温-降压的流体沸腾作用，油气保存条件破坏。弱隆升剥蚀作用过程中（贯通）裂缝系统的发育对流体活动性、连通性和油气调整聚集成藏具至关重要的作用，因而次生油气藏普遍体现出与裂缝系统具有较高的关联性。
盆-山结构主要通过构造变形强度、地表抬升剥蚀作用和陆相地层展布因素控制和影响盆地现今区域保存条件。四川盆地晚三叠世以来（残存）陆相碎屑岩较厚沉积地区（大于~3000m）主要分布在盆地西北及北部突变型盆-山结构区，（残存）陆相沉积厚度与晚三叠世以来的不同时期沉积中心相叠置，受控于环盆地不同突变型盆-山结构带中-新生代差异构造变形活动，具有较低的构造变形作用强度和晚-中新生代抬升剥蚀总厚度。因此，四川盆地现今（残存）大中型油气藏(田)和天然气的大部分主要分布于板缘突变型盆-山结构区(尤其是秦岭构造控制域)和川中原地隆起-盆地区（基底构造控制域）。
The basin-mountain systems and its geodynamics is one of the importantcomponents of the continential dynamics and was subject of tectonic studies inwestern China. The Sichuan basin located the eastern margin of the Tibetan Plateau ata transfer zone between the Tethys-Himalaya domain and the western Pacific domainis a complex sedimentary, tectonic and topographic basin. The basin and its peripheralmountains comprise composite basin-mountain system. This study uses structures,lower-temperature thermochronology, geochemistry etc., to document the relationshipbetween the basin-mountain system and the oil/gas distribution in the Sichuan basin.
(1) The composite basin-mountain system in the Sichuan basin and its peripheralmountains can be divided into two types-margin-plate systems and interior-platesystems.
The margin-plate basin-mountain systems include the Sichuan basin and itssurrounding Longmen Mountains, Micang Mountains and Daba Mountains. All ofthose are located at the western and northern marginal area of the Sichuan basin,representing the western margin of the Yangtze plate (South China Block). Themargin-plate basin-mountain systems，with binary units of large-scale thrust belts andforeland basins, have different deep lithospheric structures, abrupt boundaries andlarge contrast in today’s geomorphology. The coupling of the foreland basins andadjacent mountains is chiefly controlled by the diversity in the lithospheric structure.Sedimentary data from field and borehole investigations allow reconstruction of thesouthwesterly variations in proximal sedimentary processes along the Longmenshanthrust belt during Late Triassic and Early Jurassic and their relation to thedevelopment of a transpression basin.
In contrast, the interior-plate basin-mountain systems represented by the Sichuan basin and its adjacent interior-plate Qiyue Mountains, Dalou Mountains and DaliangMountains; located within the Yangtze plate, represent the eastern and southernmarginal area of the Sichuan basin. Due to gradual boundaries in shallow structureand similar deep lithospheric structure, the interior-plate basin-mountain systems lackof large-scale thrust belts and thrust-loaded foreland basins. The coupling of the basin(Sichuan basin) and the interior-plate mountains largely depends on the degree ofdeformation of the interior-plate mountains and multi-layer detachments in thesedimentary cover of the basin. For example, the superimposed structures indicate thatthe Daloushan basin-mountain system has experienced multistage build-up episodesunder the control of Xuefeng intercontinental orogen, accompanied by the northwardpartition of the Paleo-Yangtze basin.
(2) Due to different models between folding and deflected isotherm withinlow-relief and long-wavelength topography in the interior-plate basin-mountainsystems, it could unravel the processes of uplift/exhumation and folding deformationby multi-system lower-temperature thermochronology at a fold or anticline.
New apatite and zircon (U-Th)/He thermochronometry results using the age vs.elevation/structural depth relationship in the Daliang Mountains, support that,(1)cooling and exhumation with apparent rates of~0.15mm/yr from~30to~10Ma, waspervasive across the region after the build-up time of the orogen,(2) a differentexhumation occurred at the Daliang Mountains and southwestern part of the Sichuanbasin; the former has~3-5km exhumation magnitude while the latter~1-2kmexhumation, and (3) Late Cenozoic eastward growth of the Tibetan Plateau controlledthe rapid post~10Ma cooling and denudation, with rates of~0.4-0.8mm/yr in theDaliang Mountains.
(3) Based on the lower-temperature thermochronology and thermal models, it issuggested that there were different uplift and exhumation processes across theSichuan basin, controlled by a coupling between basement and compositebasin-mountain systems.
Modeled temperature-time histories and the Boomerang plot of AFT datasetacross the Sichuan basin suggest two-stage cooling and exhumation processes. Afterreaching their maximum burial depth during120~80Ma, it was followed significantacceleration in cooling rate during last20~10Ma. In particular, nested old-age centerseparated by Huayun Mts. was found in the center-to-northwest part of the Sichuanbasin, coupled with the low-grade deformation in the basin center. It indicatessignificant change in exhumation (at least~2000m) across the Huayun Mts.
The magnitude of exhumation across the Sichuan basin was more than~2000-3000m since the Late Cretaceous, while more than1000m in the Neogene. Ingeneral, the lowest exhumation area is located at the margin-plate basin-mountainsystems, while the largest exhumation area is at the interior-plate basin-mountainsystems. The exhumation in the basin center have magnitude averaging betweent thethe latter two. A simplified one-dimensional, steady-state solution model wasdeveloped to calculate the mean exhumation rate, which is0.05~0.2mm/yr in mostof the basin. It suggests slow uplift and exhumation across much of the basin. Theregional pattern of AFT age, length and erosion rate support a progressive changefrom the nested old-age center towards the southwest. This pattern supports theprolonged, steady-state uplift and exhumation across the basin, controlled by cratonicbasin structure. The eastern growth of the Tibetan Plateau has exerted significantcontrol on the rapid exhumation of the southwestern part of the Sichuan basin, but noton all of the basin during the Late Cenozoic.
(4) Considering the different features such as structure, deformation, evolutionand dynamics etc., the Sichuan basin can be subdivided into five units.
Unit I-North Sichuan margin-plate basin-mountain system (under the control ofQinling orogen), Unit II-West Sichuan margin-plate basin-mountain system (underthe control of Tibetan Plateau), Unit III-East Sichuan interior-plate basin-mountainsystem (under the control of Xuefeng orogen), Unit IV-SW Sichuan interior-platebasin-mountain system (under a composite control of Xuefeng orogen, TibetanPlateau and basement structures), Unit V-Central Sichuan interior-plate uplift (underthe control of basement structures). Due to different dynamics, these five units havedifferent build-up time; the Unit I has been formed during the Late Yanshanian, theUnit II and III during the Himalayan period, and the Unit IV during Late Cenozoic.Thus, the evolution of the basin and its topography are controlled by couplingprocesses between basement structures and composite basin-mountain systems of theSichuan basin.
(5) The basin-mountain systems in the Sichuan basin exert major control ontoday’s oil/gas distribution across the basin chiefly by their controlling influence onthe fluid flow and petroleum reservoirs preservation. It is controlled by the couplingprocesses between the steady-state uplift and exhumation and the thrusting andfolding deformation.
The margin-plate basin-mountain system with strong thrusting deformation, ischaracteristic by vertically throughgoing fluid flow in shallow system, and lateral fluid flow in the deep system. Whilest the interior-plate basin-mountain system ischaracteristic by throughgoing fluid flow closely correlated with a percolating clustermodel of veins. In general, the fluid flow is controlled by the thrusting and folding.However, the fluid flow shows a close correlationship with the steady state uplift andexhumation in the basin center under control of a basement.
The strong uplift and exhumation with a magnitude larger than~3000-4000m,exerts major control on the energy change and accumulation of fluid and oil/gas.During the progressive uplift and exhumation, the shallow strata attained differenttypes of fractures and joints, etc. that formed under different stress-strain regimewithin shallow and/or deep depth. The connection among different types of fractureand joint resulted in multistage fluid flow with boiling features, and finally in adestraction of petroleum reservoirs. Presence of fractures and joints have significantinfluence on the fluid flow, its connectivity and accumulation. There is a goodcorrelation betweent the gas field and fractures in the Sichuan basin, with fieldspreferentially located in an areas of a weak uplift and low exhumation.
The tectonics, terrestrial strata distribution and the late Mesozoic-Cenozoic upliftaccompanied by denudation, control the regional conditions for natural gas reservoirpreservation in the Sichuan basin. The foreland basins of the margin-platebasin-mountain systems contain (more than3000m) thick T3—K terrestrialsedimentary strata, controlled by tectonics and formation of the basin-mountainsystems. These strata were subjected only to a low degree of uplift and denudationand to weak tectonic deformation, which resulted in good preservation of oil/gasreservoirs. Therefore, today’s natural gas proven reserves and medium-large sizenatural gas fields in Sichuan basin are mainly located within the foreland basins at themargin-plate basin-mountain systems.
引文
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