本文選題：大同 + 新生代��； 參考：《太原理工大學(xué)》2015年碩士論文

【摘要】：大同新生代斷陷盆地位于山西地塹系北部，是一個(gè)經(jīng)歷多期構(gòu)造運(yùn)動(dòng)并于晚新生代開始發(fā)育的斷陷盆地。作者以沉積學(xué)、構(gòu)造地質(zhì)學(xué)為理論指導(dǎo)，通過對大同新生代斷陷盆地周邊山體古-中生代地層分布、沉積特征及構(gòu)造作用特征的研究，探討了大同新生代斷陷盆地周邊山體隆升過程，分析了大同斷陷盆地的沉積演化特征，主要取得以下幾個(gè)方面的認(rèn)識： 1.大同斷陷盆地周鄰山區(qū)下古生界地層包括寒武系、奧陶系，，總體上為一套穩(wěn)定的陸表海碳酸鹽巖建造。主要分布于盆地東側(cè)渾源、恒山北東部三條嶺、懸空寺和盆地西側(cè)鵝毛口—神頭一帶及西南角寧武向斜北東揚(yáng)起端牛食窯一帶，在盆地東南側(cè)恒山雜巖高山上有零星殘余。上古生界包括石炭-二疊系地層，主要分布于盆地西側(cè)懷仁縣鵝毛口—樓子溝—山陰縣后石門—玉井一線以西，渾源縣北山及官王鋪、劉官莊一帶、西南角牛食窯、東北部的恒山等地有零星殘存，總體為一套海陸交互環(huán)境三角洲相—大陸環(huán)境河流（湖）相沉積。盆地周邊山區(qū)不同地區(qū)古生界地層可以對比，說明大同斷陷盆地所在地和周邊山區(qū)在古生代均接受了寒武-奧陶系和石炭-二疊系沉積。盆地周邊及所在地?zé)o三疊系沉積，侏羅系和白堊系僅局部分布。 2.大同斷陷盆地周邊山區(qū)古生代處于相對的構(gòu)造平穩(wěn)期，中生代進(jìn)入了強(qiáng)烈構(gòu)造活動(dòng)階段。晚侏羅世在北西-南東向的擠壓應(yīng)力場中，大同新生代斷陷盆地周鄰山區(qū)發(fā)生大規(guī)模的逆沖推覆、北東向的逆斷層、北西向正斷層為主的構(gòu)造作用。新生代大同新生代斷陷盆地總體是在拉張構(gòu)造環(huán)境下，以繼承性斷裂活動(dòng)為主，以中生代燕山期斷裂的復(fù)活與反向發(fā)展為特征�？嘏柽吔鐢嗔丫D(zhuǎn)化成為呈階梯狀向盆地方向滑落的張性正斷層。拉張應(yīng)力控制的正斷層作用導(dǎo)致斷塊陷落，形成北東-南西向展布的大同斷陷盆地。盆緣主控?cái)嗔雅c盆內(nèi)斷裂一起控制形成以大同-懷仁凹陷、黃花梁陷隆和后所凹陷為主要次級單元組成的不對稱箕狀斷陷盆地，并控制著盆地新生代沉積，形成懷仁和后所兩個(gè)沉積中心，最大沉積厚度分別為1500m和3500m。 3.大同新生代斷陷盆地新生代沉積相的展布受構(gòu)造運(yùn)動(dòng)的影響，橫向上從黃土丘陵邊山與盆地間呈側(cè)向消長關(guān)系,具明顯的同時(shí)異相特征。在縱向上呈有規(guī)律的階段性變遷,自上新世以來盆地內(nèi)自下而上的沉積相演化為上新世以湖泊相為主-上新世晚期的沖積扇及扇前傾斜平原相-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淺湖相及扇三角洲相-晚更新世及全新世時(shí)期的沖積扇相和河流相，大同斷陷盆地自上新世以來經(jīng)歷了水退-水進(jìn)-水退的湖盆發(fā)育過程。 4.大同新生代斷陷盆地受新生代構(gòu)造活動(dòng)的影響，其形成及演化呈現(xiàn)出振蕩式升降過程。盆地形成前為隆起剝蝕區(qū)，受喜山運(yùn)動(dòng)影響，古近紀(jì)始新世-漸新世開始裂陷，中新世大同新生代斷陷盆地雛形形成，為大同斷陷盆地的初始裂陷階段。上新世以來盆地周緣主控?cái)嗔验_始發(fā)生強(qiáng)烈差異運(yùn)動(dòng)，大同斷陷盆地進(jìn)入裂陷發(fā)展成熟階段，盆地內(nèi)沉積主要是上新世的填平補(bǔ)平，第四紀(jì)的披蓋式沉積。 5.大同斷陷盆地周邊山體的隆升經(jīng)歷了如下3個(gè)階段：①三疊紀(jì)時(shí)期的整體隆升階段（250-205Ma）②侏羅紀(jì)-白堊紀(jì)陸內(nèi)造山作用階段（205-65Ma）③新生代盆地周邊山體強(qiáng)烈隆升作用階段（65Ma-至今）。 6.大同新生代斷陷盆地朔州斷階新生界基底地層保留了二疊系、石炭系、奧陶系、寒武系，大同-渾源一線北東地區(qū)新生界基底地層可能保留有侏羅系和下白堊系地層。在黃花梁隆起地區(qū)胡家?guī)X地段新生界基底地層為繁峙玄武巖下伏有上白堊統(tǒng)地層，部分地段為太古代繁峙玄武巖，其他地段繁峙玄武巖下伏地層可能有中-古生代地層。對于盆地內(nèi)斷陷較深鉆未鉆穿新生代，其基底地層可能有中-古生代地層
[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.

【學(xué)位授予單位】：太原理工大學(xué)
【學(xué)位級別】：碩士
【學(xué)位授予年份】：2015
【分類號】：P548

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