大同新生代断陷盆地形成与演化

发布时间：2018-05-09 00:35

本文选题：大同 + 新生代　；参考：《太原理工大学》2015年硕士论文

【摘要】：大同新生代断陷盆地位于山西地堑系北部，是一个经历多期构造运动并于晚新生代开始发育的断陷盆地。作者以沉积学、构造地质学为理论指导，通过对大同新生代断陷盆地周边山体古-中生代地层分布、沉积特征及构造作用特征的研究，探讨了大同新生代断陷盆地周边山体隆升过程，分析了大同断陷盆地的沉积演化特征，主要取得以下几个方面的认识： 1.大同断陷盆地周邻山区下古生界地层包括寒武系、奥陶系，，总体上为一套稳定的陆表海碳酸盐岩建造。主要分布于盆地东侧浑源、恒山北东部三条岭、悬空寺和盆地西侧鹅毛口—神头一带及西南角宁武向斜北东扬起端牛食窑一带，在盆地东南侧恒山杂岩高山上有零星残余。上古生界包括石炭-二叠系地层，主要分布于盆地西侧怀仁县鹅毛口—楼子沟—山阴县后石门—玉井一线以西，浑源县北山及官王铺、刘官庄一带、西南角牛食窑、东北部的恒山等地有零星残存，总体为一套海陆交互环境三角洲相—大陆环境河流（湖）相沉积。盆地周边山区不同地区古生界地层可以对比，说明大同断陷盆地所在地和周边山区在古生代均接受了寒武-奥陶系和石炭-二叠系沉积。盆地周边及所在地无三叠系沉积，侏罗系和白垩系仅局部分布。 2.大同断陷盆地周边山区古生代处于相对的构造平稳期，中生代进入了强烈构造活动阶段。晚侏罗世在北西-南东向的挤压应力场中，大同新生代断陷盆地周邻山区发生大规模的逆冲推覆、北东向的逆断层、北西向正断层为主的构造作用。新生代大同新生代断陷盆地总体是在拉张构造环境下，以继承性断裂活动为主，以中生代燕山期断裂的复活与反向发展为特征。控盆边界断裂均转化成为呈阶梯状向盆地方向滑落的张性正断层。拉张应力控制的正断层作用导致断块陷落，形成北东-南西向展布的大同断陷盆地。盆缘主控断裂与盆内断裂一起控制形成以大同-怀仁凹陷、黄花梁陷隆和后所凹陷为主要次级单元组成的不对称箕状断陷盆地，并控制着盆地新生代沉积，形成怀仁和后所两个沉积中心，最大沉积厚度分别为1500m和3500m。 3.大同新生代断陷盆地新生代沉积相的展布受构造运动的影响，横向上从黄土丘陵边山与盆地间呈侧向消长关系,具明显的同时异相特征。在纵向上呈有规律的阶段性变迁,自上新世以来盆地内自下而上的沉积相演化为上新世以湖泊相为主-上新世晚期的冲积扇及扇前倾斜平原相-早更新世早期的湖泊相及扇三角洲相-早更新世晚期至中更新世的浅湖相及扇三角洲相-晚更新世及全新世时期的冲积扇相和河流相，大同断陷盆地自上新世以来经历了水退-水进-水退的湖盆发育过程。 4.大同新生代断陷盆地受新生代构造活动的影响，其形成及演化呈现出振荡式升降过程。盆地形成前为隆起剥蚀区，受喜山运动影响，古近纪始新世-渐新世开始裂陷，中新世大同新生代断陷盆地雏形形成，为大同断陷盆地的初始裂陷阶段。上新世以来盆地周缘主控断裂开始发生强烈差异运动，大同断陷盆地进入裂陷发展成熟阶段，盆地内沉积主要是上新世的填平补平，第四纪的披盖式沉积。 5.大同断陷盆地周边山体的隆升经历了如下3个阶段：①三叠纪时期的整体隆升阶段（250-205Ma）②侏罗纪-白垩纪陆内造山作用阶段（205-65Ma）③新生代盆地周边山体强烈隆升作用阶段（65Ma-至今）。 6.大同新生代断陷盆地朔州断阶新生界基底地层保留了二叠系、石炭系、奥陶系、寒武系，大同-浑源一线北东地区新生界基底地层可能保留有侏罗系和下白垩系地层。在黄花梁隆起地区胡家岭地段新生界基底地层为繁峙玄武岩下伏有上白垩统地层，部分地段为太古代繁峙玄武岩，其他地段繁峙玄武岩下伏地层可能有中-古生代地层。对于盆地内断陷较深钻未钻穿新生代，其基底地层可能有中-古生代地层
[Abstract]:The Datong Cenozoic fault basin is located in the northern part of the Shanxi graben system. It is a faulted basin that has experienced multiple tectonic movements and began to develop in the late Cenozoic. The author, guided by the theory of sedimentology and tectonic geology, has studied the distribution, sedimentary and tectonic characteristics of the Paleozoic Mesozoic strata in the surrounding mountains of the Datong Cenozoic fault basin. The process of the uplift of the surrounding mountains of the Datong Cenozoic fault basin is discussed, and the characteristics of the sedimentary evolution of the Datong fault basin are analyzed, and the following aspects are mainly obtained.
The lower Paleozoic strata in the vicinity of the 1. Datong fault basin, including the Cambrian and Ordovician, are generally a set of stable continental carbonate formations, mainly located in the eastern side of the basin, three mountains in the eastern part of the Mt. Hengshan, the goose head of the Hanging Temple and the west side of the basin and the north east of the Jiao Ningwu syncline, and the basin of the north east of the Jiao Ningwu syncline. There are sporadic remnants in the Mt. Hengshan complex on the south side of the East and the south of the earth. The upper Paleozoic consists of Carboniferous Permian strata, mainly distributed in the west of the goosemouth of the Huairen County in the west of the basin, the west of the first line of the Shimen jade well after Shanyin County, and the north and Guan Wang Pak of Hunyuan County, the Liu Guanzhuang area, the southwest corner ox food kiln and the Mt. Hengshan in the northeast, and the total fragmentary remnants of the Mt. Hengshan and other places in the northeast. The Paleozoic strata in different regions around the basin can be compared to a set of marine and continental environmental delta facies - Continental environmental River (Lake) facies. It is indicated that the Cambrian Ordovician and Carboniferous Permian sediments were deposited in the Datong fault basin and the surrounding mountainous areas. Only locally distributed in the Cretaceous system.
The Palaeozoic area around the 2. Datong fault basin was in a relatively stable period of tectonic stability, and the Mesozoic era entered a strong tectonic activity stage. In the late Jurassic, in the compression stress field of North West to South East, large scale thrust nappe, north-east reverse fault and North West to normal fault occurred in the adjacent mountainous area of the Datong Cenozoic fault basin. The Cenozoic fault basin of the Cenozoic Datong new generation is mainly in the tension structure environment, mainly with the succession fault activity, characterized by the resurrection and reverse development of the Mesozoic Yanshan fault. The basin boundary faults are all transformed into the tensional positive faults that slide in the direction of the basin to the direction of the basin. The positive fault of La Zhang Yingli control leads to the fault block subsidence. The basin margin is controlled by the main secondary unit of the Datong Huairen sag, the Huanghua beam trapping and the post depression, and the Cenozoic sedimentary basin is controlled to form the two sedimentary centers in Huairen and the post basin. The thickness of the product is 1500m and 3500m., respectively.
The distribution of the Cenozoic sedimentary facies in the 3. Datong Cenozoic fault basin is influenced by the tectonic movement, laterally extending from the Loess Hilly side mountain to the basin, with obvious simultaneous heterogenous characteristics. In the longitudinal direction, there is a regular phase change. Since the Pliocene, the sedimentary facies from the bottom to the upper part of the Pliocene have evolved into a lake in the Pliocene. The facies are the alluvial fan in the late Pliocene and the early Pleistocene lacustrine facies and fan delta facies, the shallow lacustrine facies of the late Pleistocene to the Middle Pleistocene and fan delta facies, the alluvial fan and the river facies in the late Pleistocene and Holocene epoch, and the Datong fault basin has experienced water retreat water regression and water retreat since the Pliocene. The development process of the lake basin.
The formation and evolution of the 4. Datong Cenozoic fault basin, influenced by the Cenozoic tectonic movement, showed an oscillatory rise and fall process. Before the formation of the basin, the basin was a uplift denudation area, affected by the Himalayan movement, the Paleogene Eocene Oligocene began to crack, and the early Miocene Datong Cenozoic fault basin was formed, which was the initial rift order of the Datong fault basin. Since the Pliocene, the main control faults of the basin around the basin began to have a strong difference movement, and the Datong fault basin entered the mature stage of the rifting, and the deposit in the basin was mainly the Pliocene filling and leveling, and the cover type deposition in the Quaternary period.
The uplifting of the surrounding mountains in the 5. Datong fault basin experienced the following 3 stages: (1) the overall uplift stage (250-205Ma) of the Triassic period (2) the Jurassic Cretaceous orogenic stage (205-65Ma) (3) the strong uplift stage of the mountains surrounding the Cenozoic basins (65Ma-).
The Cenozoic basement strata of the Shuozhou fault step of the 6. Datong Cenozoic fault basin retained Permian, Carboniferous, Ordovician, Cambrian, and the Cenozoic basement strata in the north east area of Datong Hunyuan, which may retain Jurassic and lower Cretaceous strata. In the Huanghua beam uplift area, the basal strata of the Hu Jialing section of the Hu Jialing area are under the basalts of Fanshi basalt. The Cretaceous strata are part of the Archean Fanshi basalt, and the lower Fanshi basaltic strata may have middle Paleozoic strata in other sections. For the deep drilling in the basin, the deep drilling has not been drilled in the Cenozoic, and the basement strata may have middle Paleozoic strata.

【学位授予单位】：太原理工大学
【学位级别】：硕士
【学位授予年份】：2015
【分类号】：P548

【参考文献】