本文選題：構(gòu)造控礦 + 構(gòu)造演化�。� 參考：《成都理工大學(xué)》2017年碩士論文

【摘要】：研究區(qū)大地構(gòu)造位置位于揚(yáng)子地臺(tái)西南緣,木里—錦屏山弧形推覆構(gòu)造帶北西側(cè)。區(qū)域構(gòu)造運(yùn)動(dòng)強(qiáng)烈,成礦條件優(yōu)越,礦產(chǎn)資源豐富,礦區(qū)成礦與構(gòu)造關(guān)系密切。通過對(duì)研究區(qū)構(gòu)造類型和構(gòu)造控礦特征的研究,結(jié)合區(qū)域地質(zhì)背景,探討其構(gòu)造變形特征和構(gòu)造控礦規(guī)律。(1)研究區(qū)地層主要為早元古界里伍巖群的云母片巖、云母石英片巖、云母石英巖、石英巖。區(qū)內(nèi)構(gòu)造變形強(qiáng)烈,礦區(qū)地層經(jīng)歷多期變質(zhì)變形作用,發(fā)育三期以上構(gòu)造面理,宏觀面理構(gòu)造置換現(xiàn)象明顯,S2面理為里伍巖群主期構(gòu)造面理,構(gòu)造變形以韌性、脆-韌性變形為主。(2)研究區(qū)主要有面理構(gòu)造、斷裂構(gòu)造、褶皺構(gòu)造三種構(gòu)造控礦類型。面理主要為含礦溶體提供通道和容礦空間。斷裂構(gòu)造是成礦過程中的巖漿和熱液的通道,但往往只是在斷裂的某些有利部位才有礦田及礦床的產(chǎn)出。褶皺構(gòu)造常控制著礦田及礦床的分布,無論是背斜軸部、向斜軸部還是褶皺冀部都可有礦床的產(chǎn)出。(3)礦區(qū)主要經(jīng)歷了四級(jí)構(gòu)造變形應(yīng)力作用。第一級(jí)為海西期WE向的伸展作用,區(qū)內(nèi)形成緊閉褶皺、石香腸構(gòu)造、順層韌性剪切帶等水平剪切構(gòu)造;第二級(jí)為印支期WE向和SN向的雙向擠壓作用,區(qū)內(nèi)形成不對(duì)稱褶皺、平臥褶皺、逆沖推覆構(gòu)造等;第三級(jí)為燕山期NNW-SSE向的擠壓作用,區(qū)內(nèi)構(gòu)造表現(xiàn)形式以層間斷裂和層間滑動(dòng)為主;第四級(jí)為喜山期WE向的擠壓作用,區(qū)域內(nèi)主要形成逆沖推覆構(gòu)造、高角度逆斷層和表層脆性變形等變形。(4)礦床的最終形成于燕山期—喜瑪拉雅期的造山碰撞階段,區(qū)域內(nèi)發(fā)生多層次的伸展剝離,結(jié)合礦區(qū)構(gòu)造控礦特征,成礦物質(zhì)來源,認(rèn)為礦區(qū)成礦作用受晉寧晚期—澄江期區(qū)內(nèi)發(fā)生強(qiáng)烈的造山褶皺作用和碰撞型巖漿活動(dòng)的影響,導(dǎo)致地殼部分重熔,地幔巖漿大量上涌將成礦物質(zhì)帶到地表或淺地表。在燕山期—喜瑪拉雅期的造山運(yùn)碰撞運(yùn)動(dòng),使地層中成礦物質(zhì)重新活化,以巖漿一熱液方式運(yùn)移,在構(gòu)造驅(qū)動(dòng)下運(yùn)移到有利賦存空間成礦。
[Abstract]:The tectonic location of the study area is located in the southwest margin of the Yangtze platform and the western side of the arc nappe belt in Muli-Jinpingshan. The regional tectonic movement is strong, the ore-forming conditions are superior, the mineral resources are rich, and the ore-forming is closely related to the tectonics. Based on the study of structural types and structural ore-controlling characteristics in the study area and in combination with the regional geological background, the structural deformation characteristics and tectonic ore-controlling regularity of the studied area are discussed. The strata in the study area are mainly mica schist and mica quartz schist of the early Proterozoic Liwu Group. Mica quartzite The tectonic deformation in the area is very strong, the strata in the mining area undergo multi-stage metamorphism and deformation, and there are more than three stages of tectonic facets developed, and the phenomenon of structural replacement of macroscopic facets is obvious that the S 2 plane is the main tectonic plane of the Liwu Group, and the structural deformation is tenacity. There are three types of ore-controlling structures in the study area, I. e., plain structure, fault structure and fold structure. The surface texture mainly provides the passage and the ore-bearing space for the ore-bearing solution. Fault structure is the channel of magma and hydrothermal fluid in the metallogenic process, but it is only in some favorable parts of the fault that ore fields and deposits are produced. Fold structure usually controls the distribution of ore fields and deposits. The ore deposits can be produced in the back inclined axis, the inclined axis or the fold Hebei part. The ore area mainly experienced the four grade tectonic deformation stress. The first stage is the extension of the Hercynian period we direction, the area forms the closed fold, the stone sausage structure, the bedding ductile shear zone and so on horizontal shear structure, the second stage is the Indosinian period we and SN direction bidirectional compressions, the area forms the asymmetry fold, The third stage is the compression of NNW-SSE direction in Yanshanian period, the main form of structure in this area is interlayer fault and interlayer slip, the fourth stage is the compressional action of we direction in Xishan period, the third stage is the compression of NNW-SSE direction in Yanshanian period, and the main structural form in this area is interlayer fault and interlayer slip. The thrust-nappe tectonics, high-angle thrust faults and brittle deformation of the surface layer, etc., were formed in the Orogen collision stage of the Yanshanian to Himalayan epoch, and the multi-level extension and stripping occurred in the area. Based on the ore-controlling characteristics and the source of ore-forming materials, it is considered that the ore-forming process is influenced by the intense orogenic fold and collisional magmatic activity in the late Jinning and Chengjiang period, which leads to the partial remelting of the crust. Massive upwelling of mantle magma brings ore-forming materials to the surface or shallow surface. During the Yanshanian to Himalayan orogenic collision movement, the ore-forming materials in the strata were reactivated and transported in magmatic hydrothermal mode, which were driven by tectonics and migrated to favorable ore-forming space.
【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】：2017
【分類號(hào)】：P618.2

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