滇西哀牢山斷裂帶構(gòu)造巖塊變質(zhì)變形特征及其演化
發(fā)布時(shí)間：2018-07-25 15:20
【摘要】：云南省三江地區(qū)一直以來(lái)都是地學(xué)界各個(gè)領(lǐng)域?qū)＜已芯康臒狳c(diǎn)地區(qū),其中哀牢山斷裂帶是青藏高原東南緣的一條重要線性構(gòu)造。因其獨(dú)特的線形延伸,復(fù)雜而多期的構(gòu)造演化,以及構(gòu)造帶東西兩側(cè)地質(zhì)演化明顯差異,再加上新生代以來(lái)作為印度板塊-歐亞板塊碰撞調(diào)節(jié)及復(fù)合的重要場(chǎng)所,使該構(gòu)造帶成為長(zhǎng)期以來(lái)被地質(zhì)學(xué)界廣泛關(guān)注和研究的構(gòu)造帶之一。哀牢山斷裂帶位處特提斯三江造山帶東南緣處于板塊構(gòu)造結(jié)合部,構(gòu)造背景復(fù)雜,多級(jí)別、多期次的構(gòu)造形跡發(fā)育。研究區(qū)位于哀牢山斷裂帶北段,構(gòu)造帶總體上呈北北西-南南東展布,為一條北西段和南東段側(cè)較寬,中段相對(duì)較窄的狹長(zhǎng)構(gòu)造變形帶。哀牢山斷裂帶分布于南澗圖幅的馬鞍山-洪水井-梅子箐-阿扎魯小村-團(tuán)田山一帶,是揚(yáng)子板塊楚雄盆地與蘭坪-思茅盆地的分界線。它與東西兩側(cè)之中生界地層均為斷層接觸,其上僅有零星新近系地層不整合覆蓋。由三條斷裂和兩個(gè)變質(zhì)帶組成。三條斷裂從北東至南西斷裂分別為紅河斷裂、哀牢山斷裂和阿墨江斷裂。兩個(gè)變質(zhì)帶為深變質(zhì)帶和淺變質(zhì)帶,深變質(zhì)帶被紅河斷裂和哀牢山斷裂所夾持,淺變質(zhì)帶位于哀牢山斷裂和阿墨江斷裂間。前人將處于哀牢山北段的哀牢山巖群由東向西依次劃分為阿龍巖組、清水河巖組和小羊街巖組,將哀牢山南段的哀牢山巖群劃分為烏都坑組、鳳港組、阿龍組、小羊街組。該構(gòu)造域經(jīng)歷了前古特提斯階段、古特提斯階、新特提斯階段及陸內(nèi)演化階段。尤其是古生代-新生代時(shí)期,揚(yáng)子陸塊西緣的離解、碰撞拼貼及陸內(nèi)會(huì)聚作用,包括巖石圈伸展作用、收縮作用、推覆作用和分層撤離作用,其地質(zhì)構(gòu)造演化歷史漫長(zhǎng)而復(fù)雜。哀牢山巖群的變形-變質(zhì)作用十分強(qiáng)烈,尤以韌性變形表現(xiàn)顯著,巖石糜棱巖化現(xiàn)象普遍。巖群中早期形成的結(jié)晶片理、片麻理已經(jīng)全面取代原生層理,且多期次變形現(xiàn)象明顯,因此,目前所見(jiàn)到的“層狀”構(gòu)造已不能代表原巖建造特征。因而,哀牢山巖群已無(wú)層序可言。大河邊巖組經(jīng)歷了澄江運(yùn)動(dòng)、海西-印支運(yùn)動(dòng)、喜馬拉雅運(yùn)動(dòng)的構(gòu)造變形、變質(zhì)作用及改造,巖石中早期平臥褶皺發(fā)生再褶現(xiàn)象,形成直立或斜歪褶皺,并伴生軸面劈理,置換早期的面理構(gòu)造。中二疊世至晚二疊世時(shí),沉積了中二疊統(tǒng)壩溜組碳酸鹽巖(P2b)和上二疊統(tǒng)羊八寨組(P3y)三角洲相含煤建造。隨著洋殼的向西推擠以及弧后盆地的擴(kuò)張,盆地內(nèi)的古生界地層均遭受了變形變質(zhì)作用。產(chǎn)生了程度不等的低綠片巖相區(qū)域低溫動(dòng)力變質(zhì)。在伸展構(gòu)造背景下,形成了區(qū)域性透入面理以及片理面上出現(xiàn)拉伸線理,面理中發(fā)育平臥褶皺及斜臥褶皺,它們是形成于中淺部構(gòu)造層次,熱流的上涌使巖石發(fā)生明顯的熱變質(zhì)作用。根據(jù)研究區(qū)的地質(zhì)概況并結(jié)合區(qū)域地質(zhì)資料進(jìn)行綜合分析,大致可以將研究區(qū)構(gòu)造演化分為三個(gè)階段,即洋盆形成,洋盆閉合,陸陸碰撞。洋盆形成時(shí)間為晚泥盆世-早二疊世。洋盆閉合時(shí)間為晚早二疊世晚期-中三疊世晚期,包括兩個(gè)階段:俯沖消減,弧后盆地的形成階段;洋殼閉合,弧后前陸盆地的形成階段。陸陸碰撞時(shí)間為晚三疊世至古近紀(jì)。
[Abstract]:The Sanjiang area of Yunnan province has always been a hot area of expert research in various fields of the geosciences. The Ailaoshan fault zone is an important linear structure in the southeastern margin of the Qinghai Tibet Plateau. Because of its unique linear extension, complex and multi phase tectonic evolution, and the obvious difference in geological evolution between the two sides of the tectonic belt and the Cenozoic era, it is added to the Cenozoic era. As an important place for the collision regulation and recombination of the India plate Eurasia plate, the tectonic belt has been one of the tectonic belts which have been widely concerned and studied by the geologists for a long time. The southeastern edge of the Sanjiang orogenic belt at the Ailao Mountain fault zone is in the plate tectonic junction, and the structure of the tectonic back is complex, multilevel and multistage. The study area is located in the northern section of the Ailao Mountain fault zone. The tectonic belt is generally north north west to South East. It is a narrow and narrow structural deformation zone with a wide side in the North West and the South East section and relatively narrow in the middle section. The Ailao Mountain fault zone is located in the Ma'anshan flood well of Nanjian - Maizi - Al - Al - Al - Al - Tsau small village - tutian area, and the Yangtze plate Chuxiong The dividing line between the basin and the Lanping Simao basin, which is in contact with the Mesozoic strata on both sides of the East and West, has only the unconformable cover of the sporadic Neogene strata. It consists of three faults and two metamorphic belts. The three faults are Honghe fault, Ailaoshan fault, and a Mojiang fault, respectively, from the North East to the South West fault. Two metamorphic belts are deep. The metamorphic belt and the epic metamorphic belt are held by the Honghe fault and Ailao Mountain fault. The epic metamorphic belt is located between the Ailao Mountain Fault and the Mojiang fault. The Ailao Mountain groups in the northern section of the Ailao Mountain are divided from east to west to the Longyan formation, the Qingshui River rock group and the Xiao Yang Street rock group, and the Ailao Mountain groups in the southern section of Ailao Mountain are divided into a group of Ailao Mountains. The tectonic domain experienced the former Gut Tis stage, the ancient Tethys stage, the new Tethys stage and the intracontinental evolution stage, especially in the Paleozoic and Cenozoic era, especially in the western margin of the Yangtze block, the collision collage and the intracontinental convergence, including lithospheric extension, contraction and nappe. The evolution history of the geological structure is long and complicated. The deformation and metamorphism of the Ailao rock group is very strong, especially the ductile deformation is remarkable, and the rock mylonitization is common. The early formation of the crystalline schism in the group of rock groups has completely replaced the primary bedding, and the multistage deformation phenomenon is obvious, therefore, at present, The "lamellar" structure can not represent the characteristics of the original rock formation. Therefore, the Ailaoshan rock group has no sequence. The Dahe edge rock group experienced the Chengjiang movement, the Hercynian Indo branch movement, the tectonic deformation, metamorphism and transformation of the Himalaya movement, and the early pleat of the flat pleat in the rocks, forming erect or oblique folds, accompanied by the formation of the crease. During the Middle Permian to late Permian, the Middle Permian carbonate rock (P2b) and the upper two stack of sheep eight village (P3y) Delta were deposited in the Middle Permian to the Late Permian, and the Paleozoic strata in the basin were deformable and metamorphosed as the oceanic crust pushed westward and the back arc basin expanded. Under the background of extensional tectonics, there is a regional penetration surface and a stretch line on the surface, and the horizontal folds and slumping folds are developed in the surface. They are formed in the middle and shallow structures, and the upwelling of heat flow causes the rock to have obvious thermal metamorphism. The geological survey and comprehensive analysis of the regional geological data can be divided into three stages, namely the formation of the oceanic basin, the closure of the ocean basin and the continental collision. The formation time of the oceanic basin is late Devonian Early Permian. The closing time of the oceanic basin is late Early Permian to the late middle three fold period, including two stages: subduction. Subduction, the formation stage of the back arc basin, the closure of oceanic crust and the formation stage of the back arc foreland basin. The land collision time is from late three to Paleogene.
【學(xué)位授予單位】：成都理工大學(xué)
【學(xué)位級(jí)別】：碩士
【學(xué)位授予年份】：2015
【分類(lèi)號(hào)】：P542
本文編號(hào)：2144228
[Abstract]:The Sanjiang area of Yunnan province has always been a hot area of expert research in various fields of the geosciences. The Ailaoshan fault zone is an important linear structure in the southeastern margin of the Qinghai Tibet Plateau. Because of its unique linear extension, complex and multi phase tectonic evolution, and the obvious difference in geological evolution between the two sides of the tectonic belt and the Cenozoic era, it is added to the Cenozoic era. As an important place for the collision regulation and recombination of the India plate Eurasia plate, the tectonic belt has been one of the tectonic belts which have been widely concerned and studied by the geologists for a long time. The southeastern edge of the Sanjiang orogenic belt at the Ailao Mountain fault zone is in the plate tectonic junction, and the structure of the tectonic back is complex, multilevel and multistage. The study area is located in the northern section of the Ailao Mountain fault zone. The tectonic belt is generally north north west to South East. It is a narrow and narrow structural deformation zone with a wide side in the North West and the South East section and relatively narrow in the middle section. The Ailao Mountain fault zone is located in the Ma'anshan flood well of Nanjian - Maizi - Al - Al - Al - Al - Tsau small village - tutian area, and the Yangtze plate Chuxiong The dividing line between the basin and the Lanping Simao basin, which is in contact with the Mesozoic strata on both sides of the East and West, has only the unconformable cover of the sporadic Neogene strata. It consists of three faults and two metamorphic belts. The three faults are Honghe fault, Ailaoshan fault, and a Mojiang fault, respectively, from the North East to the South West fault. Two metamorphic belts are deep. The metamorphic belt and the epic metamorphic belt are held by the Honghe fault and Ailao Mountain fault. The epic metamorphic belt is located between the Ailao Mountain Fault and the Mojiang fault. The Ailao Mountain groups in the northern section of the Ailao Mountain are divided from east to west to the Longyan formation, the Qingshui River rock group and the Xiao Yang Street rock group, and the Ailao Mountain groups in the southern section of Ailao Mountain are divided into a group of Ailao Mountains. The tectonic domain experienced the former Gut Tis stage, the ancient Tethys stage, the new Tethys stage and the intracontinental evolution stage, especially in the Paleozoic and Cenozoic era, especially in the western margin of the Yangtze block, the collision collage and the intracontinental convergence, including lithospheric extension, contraction and nappe. The evolution history of the geological structure is long and complicated. The deformation and metamorphism of the Ailao rock group is very strong, especially the ductile deformation is remarkable, and the rock mylonitization is common. The early formation of the crystalline schism in the group of rock groups has completely replaced the primary bedding, and the multistage deformation phenomenon is obvious, therefore, at present, The "lamellar" structure can not represent the characteristics of the original rock formation. Therefore, the Ailaoshan rock group has no sequence. The Dahe edge rock group experienced the Chengjiang movement, the Hercynian Indo branch movement, the tectonic deformation, metamorphism and transformation of the Himalaya movement, and the early pleat of the flat pleat in the rocks, forming erect or oblique folds, accompanied by the formation of the crease. During the Middle Permian to late Permian, the Middle Permian carbonate rock (P2b) and the upper two stack of sheep eight village (P3y) Delta were deposited in the Middle Permian to the Late Permian, and the Paleozoic strata in the basin were deformable and metamorphosed as the oceanic crust pushed westward and the back arc basin expanded. Under the background of extensional tectonics, there is a regional penetration surface and a stretch line on the surface, and the horizontal folds and slumping folds are developed in the surface. They are formed in the middle and shallow structures, and the upwelling of heat flow causes the rock to have obvious thermal metamorphism. The geological survey and comprehensive analysis of the regional geological data can be divided into three stages, namely the formation of the oceanic basin, the closure of the ocean basin and the continental collision. The formation time of the oceanic basin is late Devonian Early Permian. The closing time of the oceanic basin is late Early Permian to the late middle three fold period, including two stages: subduction. Subduction, the formation stage of the back arc basin, the closure of oceanic crust and the formation stage of the back arc foreland basin. The land collision time is from late three to Paleogene.
【學(xué)位授予單位】：成都理工大學(xué)
【學(xué)位級(jí)別】：碩士
【學(xué)位授予年份】：2015
【分類(lèi)號(hào)】：P542
【參考文獻(xiàn)】
相關(guān)期刊論文 前1條
1 張志斌,劉發(fā)剛,包佳鳳;哀牢山造山帶構(gòu)造演化[J];云南地質(zhì);2005年02期
，本文編號(hào)：2144228
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