本文選題：成都凹陷 + 沙溪廟組��； 參考：《長江大學》2015年碩士論文

【摘要】：成都凹陷位于四川盆地西部,龍門山系中南段與龍泉山、總崗山之間的平原地區(qū),面積約為5000km2；凹陷以北為北東東向隆起的新場構造帶,以西為北東-南西向展布的大邑-安縣構造帶(龍門山前構造帶),以東為南北向展布的知新場構造帶；行政區(qū)屬于成都市、崇州市、彭州市、都江堰市、德陽市、廣漢市和什邡市。研究區(qū)屬于構造弱變形區(qū),目前研究區(qū)的沙溪廟組主要勘探開發(fā)的區(qū)塊有區(qū)域東北部的彭縣-德陽大型向斜區(qū),北部的孝-新-合構造帶區(qū)域,以及南部的新都-成都斜坡平緩構造帶區(qū)域。成都凹陷經(jīng)歷了印支、燕山、喜山等多期構造運動,在晚三疊世,溫江、馬井地區(qū)開始形成構造雛形,而新都-洛帶地區(qū)的構造還未形成；早侏羅世,溫江、馬井、新都-洛帶地區(qū)的構造都開始逐步形成,德陽-廣漢一帶的向斜也隨著正向構造的形成,相切的幅度也不斷增大；晚侏羅世,溫江構造體現(xiàn)出隆起的繼承性,閉合面積和幅度都在逐漸減��；一直到早白堊世末,沙溪廟組地層才持續(xù)隆起,新都-洛帶地區(qū)隨著構造運動的擠壓,以及龍泉山斷裂的發(fā)展,形成背斜；在喜山運動的影響下,馬井背斜南東方向伴生的馬井斷裂發(fā)育,活動貫穿了馬井背斜形成的整個時期；在喜山運動晚期,新都-洛帶地區(qū)的背斜在構造運動的擠壓下,形成了現(xiàn)今的新都鼻狀構造以及洛帶的背斜構造。下沙溪廟組與下伏千佛崖組在剖面上表現(xiàn)為下沙溪廟組底部的“關口砂巖”對不整合界面的漸進超覆不整合接觸；上、下沙溪廟組之間以“葉肢介頁巖”作為識別界面的標志,但不是所有不整合界面上都有該標志；遂寧組與上沙溪廟組之間在盆地內部表現(xiàn)為相關整合面,垂向上表現(xiàn)為由粗轉細的相轉換界面。將沙溪廟組劃分為3個段：分別是下沙溪廟組、上沙溪廟組下段和上沙溪廟組下段。并可進一步將沙溪廟組劃分為J2S33、J2S32、J2S34、J2S24、J2S23、J2S22、J2S24、J2S44、 J2S43、J2S42、J2S44,一共11個砂組。通過砂巖巖屑類型分布分析、重礦物組合(ZTR指數(shù))特征分析、輕碎屑組分分析等,結合成都凹陷周圍古地貌的特征,確定成都凹陷主要物源方向有兩個：一是盆地北緣的米倉山-大巴山,二是西北緣的龍門山。其中成都凹陷西部的崇州-郫縣-彭州地區(qū)主要收到西部龍門山物源的影響；東部的德陽-金堂-洛帶地區(qū)主要受到東北部米倉山-大巴山物源的影響；中部馬井、新繁地區(qū)顯示明顯多物源的特征,除了受到東北、北部遠物源影響外,還受到西北部龍門山近物源的影響。前人對成都凹陷侏羅系沙溪廟組沉積相進行過-些研究,本文通過巖心觀察、描述,以及測錄井資料、分析化驗資料等的分析,認為成都凹陷侏羅系沙溪廟組主要存在兩大沉積體系：近源的辮狀河三角洲沉積體系(短軸)以及遠源的曲流河三角洲沉積體系(長軸)。凹陷西部以龍門山中段物源為主,主要為北西-南東向短軸辮狀河三角洲沉積,砂體呈片狀分布；凹陷中部、東部以龍門山北段、米倉山物源為主,主要為北東-南西向長軸曲流河三角洲沉積,河道砂體發(fā)育,砂體主要呈條帶狀分布。三角洲平原、三角洲前緣及前三角洲亞相均有發(fā)育,沉積微相包括分流河道、水下分流河道、分流間灣、河口壩、遠砂壩微相等。在研究區(qū)內,辮狀河三角洲沉積與曲流河三角洲沉積的不同體現(xiàn)在：一是沉積物平均粒度大小上,辮狀河三角洲與與之對應的曲流河三角洲沉積微相的沉積粒度相比較大；二是辮狀河三角洲沉積體系中不發(fā)育或者發(fā)育較少的遠砂壩微相。本文通過選取研究區(qū)內由不用物源主導的單井,對比了兩種三角洲沉積之間的差異。研究區(qū)重點砂組在下沙溪廟組有J2S33、J2S31,上沙溪廟組下段全部砂組均為重點砂組,上沙溪廟組上段有J2S14、J2S14。各砂組的砂體分布特征均有不同,本次就不同重點砂組砂體分布特征的不同進行了描述,為勘探開發(fā)的下一步工作打好了基礎。沙溪廟組形成時期總體顯示為湖平面不斷上升的過程,雖其內部也出現(xiàn)多次小幅度湖平面上升、下降的反復。在下沙溪廟組沉積時期,成都凹陷砂體發(fā)育,砂體厚度較大,主要為三角洲前緣亞相沉積；在上沙溪廟組下亞段沉積時期,與下沙溪廟組不同,成都凹陷內馬井-什邡、崇州-郫縣地區(qū)為三角洲前緣-平原亞相沉積,廣漢-金堂、新都-洛帶地區(qū)為三角洲前緣亞相沉積；在上沙溪廟組上亞段沉積時期,基本延續(xù)上沙溪廟組下亞段沉積格局,三角洲前緣面積有所減小。沉積過程的動態(tài)演化顯示不同沉積體系在不同時期的展布范圍具有繼承性,卻又存在一定的差異。剖面顯示,沙溪廟組沉積期間,湖盆水體的升降較為頻繁,并且整個沙溪廟組在縱向上各砂組的砂體發(fā)育程度是不同的,主要取決于其所處的基準面旋回的部位。本區(qū)的砂體主要集中發(fā)育在中期旋回的上升基準面早期,其次是下降基準面晚期,不同時期形成的砂體相互疊置拼接,使得研究區(qū)砂體在垂向上總體厚度較大,并且在平面分布上連續(xù)性較好,是油氣聚集及儲存的有利部位。
[Abstract]:The Chengdu sag is located in the west of the Sichuan basin, the plain area between the middle and southern section of the Longmen mountain system and the Longquan mountain and the general Gang mountain, with an area of about 5000km2, the North East to the East and the new field tectonic belt in the north of the sag, the Dayi an County tectonic belt (the front of the Longmen mountain tectonic belt) to the West and the east to the north and the north. The district belongs to Chengdu, Chongzhou, Pengzhou, Dujiangyan, Deyang, Guanghan and Shifang. The research area belongs to the structural weak deformation zone. The main exploration and development area of the Shaxi Temple group in the study area is the Peng County Deyang large Syncline area in the northeast of the region, the northern part of the filial and new combined tectonic zone, and the Southern new capital. The Chengdu sag has experienced many tectonic movements, such as Indo, Yanshan, Himalayan and other tectonic movements. In the late three fold, Wenjiang and Ma well began to form a structural prototype, while the structure of the new Du Luodai region had not been formed; the structures of the early Jurassic, Wenjiang, Ma well and the Xindu Luodai region began to form gradually, and the Deyang - Guanghan area was gradually formed. The syncline is also formed with the formation of the positive structure, and the amplitude of the tangent is also increasing; the late Jurassic, the Wenjiang structure embodies the inheritance of the uplift, and the closed area and amplitude are gradually decreasing; from the end of the early Cretaceous to the end of the early Cretaceous, the Shaxi Temple formation continues to rise, the new Du Luodai region is extruded with the tectonic movement and the Longquan mountain fracture. Under the influence of the Himalayan movement, the well developed in the south east direction of the Ma well anticline is developed, and the activity runs through the whole period of the formation of the horse well anticline. In the late Xi Shan movement, the anticline in the Xindu Luodai area was squeezed by the tectonic movement, forming the present new metropolitan structure and the Luodai anticline structure. The Xi Miao formation and the lower Qian Buddha cliff formation show the progressive overlying unconformity contact of the "Guan Kou sandstone" on the unconformable interface at the bottom of the lower Shaxi Temple formation, and the "leaf limb mesoporous shale" between the Xiashi Temple group as a symbol of the recognition interface, but not all the unconformities on the interface, and the Suining group and the upper Shaxi Temple group. The Shaxi Temple group is divided into 3 sections: Xiashan Temple group, upper Shaxi Temple formation lower section and upper Shaxi Temple group lower section, respectively. The Shaxi Temple group can be further divided into J2S33, J2S32, J2S34, J2S24, J2S23, J2S22, J2S24, J2S44, J2S43, J2S42. J2S44, a total of 11 sand groups. Through the analysis of the type distribution of sandstone debris, the analysis of the combination of heavy minerals (ZTR index), the analysis of the light detrital component, and the characteristics of the paleogomorphology around the Chengdu depression, there are two main source directions of the Chengdu sag: one is the rice Cangshan Daba Mountain in the northern margin of the basin, and the two of the Longmen mountain in the northwest margin. Chengdu is the Longmen mountain in the northwest margin. The Chongzhou Pixian Pengzhou region in the west of the depression is mainly affected by the source of the western Longmen mountain, and the Deyang Jintang Luodai area in the East is mainly influenced by the source of the north northeast m Cangshan Daba Mountain. The central well and the new propagation area show the characteristics of the obvious multiple source. Besides the influence of the East North and the northern far source, the northwest part is also subject to the northwest. The influence of the near source of the Longmen mountain. The predecessors have studied the sedimentary facies of the Jurassic Shaxi Temple formation in the Chengdu depression. Through the analysis of the core observation, description, logging data and analysis of the laboratory data, it is believed that there are two major sedimentation systems in the Shaxi Temple formation of the Jurassic in the Chengdu depression: the braid delta depositional system of the near source (short) In the west of the depression, the main source is the source of the middle Longmen mountain, mainly from the North West to the short axis Braided River Delta, and the sand body is flaky, in the middle of the depression, in the eastern part of the Longmen mountain, the main source of the rice in the rice of the North East and the South West to the long axis of the River Delta. The channel sand body is developed and the sand body is mainly banded distribution. Delta plain, delta front and anterior delta subfacies are developed, sedimentary microfacies include distributary channel, underwater distributary channel, distributary Bay, estuarine dam, and far sand dam. In the average grain size of the sediments, the braided river delta is larger than the sedimentary granularity of the sedimentary microfacies of the corresponding Meandering River Delta, and the two is the micro facies of the long sand dams that are not developed or developed in the braided river delta depositional system. In this paper, two kinds of triangles are compared by selecting a single well dominated by unused source in the study area. The main sand groups in the Xiasha Temple formation in Xiasha Temple group are J2S33, J2S31, and upper Shaxi Temple formation in the lower Shaxi Temple formation, the key sand groups in the lower Sha Xi Temple formation are the key sand groups, and the upper part of the upper Shaxi Temple Group has J2S14, and the sand body distribution characteristics of the J2S14. sand groups are different, this time the different sand body distribution characteristics of different key sand groups were described, for exploration and development. In the formation period of the Shaxi Temple formation, the formation period of the Temple group was generally shown as the rising process of the lake level. Although there were several small amplitude lake levels rising and decreasing, the sand body of the Chengdu sag developed and the sand body was thick, mainly the delta front subfacies, and the upper Shaxi temple in the Xiashan Temple formation. The lower subsection sedimentary period is different from the lower Shaxi Temple group. The Chengdu sag Nei Ma Jing - Shifang, Chongzhou - Pixian area is delta front plain subfacies deposit, Guanghan Jintang and Xindu Luodai area is delta front subfacies deposit. In the upper subsection of upper Shaxi Temple formation, the lower subsection of Shaxi Temple subsection was basically extended. The area of the front edge of the continent decreases. The dynamic evolution of the deposition process shows that the distribution range of the different depositional systems is inheriting, but there is a certain difference. The section shows that during the period of the Shaxi Temple formation, the water body of the lake basin is more frequent, and the development degree of the sand body in the longitudinal sand groups in the whole Shaxi Temple group is not. The same is mainly determined by the position of the base level cycle. The sand bodies in this area are mainly concentrated in the early stage of the rising datum of the mid-term cycle, followed by the late descent datum, and the sand bodies formed in different periods are stacked and spliced each other, making the sand body in the vertical upper body thick and continuous in the plane distribution. Well, it is a favorable place for oil and gas accumulation and storage.
【學位授予單位】：長江大學
【學位級別】：碩士
【學位授予年份】：2015
【分類號】：P618.13

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相關期刊論文 前7條

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本文編號：1922269