本文選題：吉林省 + 通化　； 參考：《吉林大學》2015年碩士論文

【摘要】：二密銅礦位于吉林省通化市境內(nèi)，大地構造位置上位于華北地臺北緣東段的三源浦火山盆地內(nèi)，是一個具有悠久開采歷史的老礦山。礦區(qū)內(nèi)出露的地層主要為晚侏羅世-白堊紀陸相火山巖-火山碎屑巖地層，局部有太古宙基底和元古宙地層出露；巖漿活動強烈，早白堊世火山作用主要可以分為三個噴發(fā)旋回（果松期、林子頭期和三棵榆樹期），晚期松頂山巖體沿火山通道侵入；礦區(qū)構造主要為三源浦復式火山機構，主要為東西向、南北向、北西向和北東向的斷裂。 礦體主要分布于松頂山巖體的東南部，以及與火山巖地層的內(nèi)外接觸帶中，可分為東區(qū)、東南區(qū)、南區(qū)、四道洋岔、四方頂子區(qū)及小橫道河子等幾個礦區(qū)，礦體主要以三種形式產(chǎn)出：（1）脈狀礦體主要分布在石英閃長巖和花崗斑巖內(nèi)外接觸帶中緩傾斜的張性斷裂中，自北東向南西，礦帶的傾向也從北東向逐漸變?yōu)槟衔飨�，是該礦區(qū)主要的工業(yè)礦體；此外，在南部安山巖地層中發(fā)育北西向陡傾斜和東西的緩傾斜的細脈浸染狀礦體；（2）浸染狀礦體主要分布在花崗斑巖和石英閃長巖體內(nèi)；（3）在花崗斑巖體頂部的角礫巖內(nèi)發(fā)育塊狀的富礦體以及水晶礦產(chǎn)；礦石礦物主要為毒砂、磁黃鐵礦、黃銅礦和黃鐵礦等，其次為輝鉬礦、閃鋅礦等；脈石礦物主要由石英、絹云母、綠泥石、方解石等組成；圍巖蝕變主要為硅化、絹云母化、青磐巖化、碳酸鹽化和高嶺土化等。 二密銅礦的成礦作用與松頂山巖體密切相關，巖體的主體巖性為石英閃長巖、石英二長閃長巖、花崗閃長巖、斑狀花崗閃長巖和花崗斑巖等。LA-ICP-MS鋯石U-Pb精確測年獲得花崗閃長巖、石英閃長巖和斑狀花崗閃長巖的結晶年齡分別為94.2±1.7Ma（N=15，MSWD=0.53）、94.3±1.2Ma（N=17，MSWD=0.30）和93.9±1.2Ma（N=19，MSWD=0.22）。元素地球化學特征顯示，松頂山巖體為中酸性侵入巖，SiO2=56.76~72.69%， Na2O=3.64~6.44%， K2O=1.88~3.87%， CaO=1.86~6.41%，A/CNK=0.86~0.97，A/NK=1.29~2.05，屬于亞堿性高鉀鈣堿性系列，具有低的Mg#（0.28~0.38）；稀土元素配分圖解呈右傾斜模式（LREE/HREE=5.75~9.84;（La/Yb）N=5.27~10.36），δEu=0.71~1.12；微量元素以富集Rb、Ba、Th、U、K和LREE等大離子親石元素（LILEs）和虧損Nb、Ta、P、Ti和HREE等高場強元素（HFSEs）為特征；（87Sr/86Sr）i比值和εNd（t）值分別為0.70765~0.70829和-13.8~-10.8，Nd模式年齡TDM為1.68~2..05Ga，與該區(qū)早白堊世火山巖Sr-Nd同位素比值相似，表明它們的源區(qū)由太古宙下地殼和底侵的玄武巖兩個端元組成，原始巖漿起源于受板塊流體交代的地幔楔。結合前人的研究，本文認為二密銅礦的成巖成礦作用發(fā)生在晚白堊世，形成于太平洋俯沖作用背景下的伸展環(huán)境下。 礦床地質特征、室內(nèi)礦相學研究表明成礦過程包括石英-黃鐵礦階段、石英-輝鉬礦-黃鐵礦-黃銅礦階段、石英-黃銅礦-多金屬成礦階段、灰白色石英-綠泥石化-黃鐵礦-塊狀黃銅礦階段、石英-碳酸鹽階段五個階段。流體包裹體研究表明流體包裹體類型主要為富液相包裹體和含子晶三相包裹體，還含有少量富氣相包裹體；流體包裹體的均一溫度為149.9~450℃，鹽度為3.85~52.42wt%，可劃分為445~450℃、330.5~419℃、260~328.9℃、204~258.4℃和149.9~180.3℃五個階段；其中，富液相包裹體均一溫度為149.9~450℃，鹽度為3.85~12.65，密度為0.584~0.970g/cm3；含子晶三相包裹體均一溫度為265~419℃，，鹽度為34.72~38.57wt%，密度為1.107~1.110g/cm3；富氣相包裹體均一溫度為358~362℃，鹽度為3.85~9.65wt%，密度為0.63~0.72g/cm3。激光拉曼成分分析顯示，富液相體包裹體成分主要為H2O和CH4，含子晶三相包裹體成分主要為H2O，富氣相包裹體成分主要為CO2和CH4；流體沸騰和溫度降低是二密銅礦重要的成礦機制。
[Abstract]:The two dense copper mine is located in the Tonghua city of Jilin province. The tectonic position is located in the Sanyuan basin volcanic basin in the eastern part of the Taipei edge of North China. It is an old mine with a long history of mining. The exposed strata in the mining area are mainly late Jurassic Cretaceous volcanic clastic rocks in the Cretaceous and volcanic clastic rocks, and some Archean basement and Proterozoic era. The volcanic activity of the early Cretaceous can be divided into three eruptive cycles (fruit pine period, forest head stage and three elm period), and the late pine roof rock mass is intruded along the volcanic passage, and the main structure of the mining area is the Sanyuan PU compound volcano, which is mainly east west, North and south, northwestern and northward.
The ore bodies are mainly distributed in the southeastern part of the pantinshan rock mass and in the inner and outer contact zones of the volcanic rocks, which can be divided into eastern, Southeast, southern, four Dao Yang, Sifang and Xiao Heng River, and the ore bodies are mainly produced in three forms: (1) the veins are mainly distributed inside and outside the quartz diorite and granite porphyry. In the gently inclined tensional fracture of the belt, the tendency of the ore belt from the North East to the South West, and from the North East to the South West, is the main industrial ore body in the mining area. In addition, in the southern andesite, the North West to steeply inclined and gently inclined fine vein disseminated orebodies are developed, and (2) the disseminated orebodies are mainly distributed in granite porphyry and stone. (3) the massive ore bodies and crystal minerals are developed in the breccia at the top of the granitoid rock mass; ore minerals are mainly arsenopyrite, pyrrhotite, chalcopyrite and pyrite, followed by molybdenite, sphalerite, etc.; the gangue minerals are mainly composed of quartz, sericite, chlorite, calcite, etc.; the alteration of the surrounding rock is mainly caused by the alteration of the surrounding rock. Silicification, sericite, dolomitization, carbonation and KAOLINIZATION.
The mineralization of the two dense copper mine is closely related to the pinzidan rock mass. The main lithology of the rock mass is quartz diorite, quartz two diorite, granodiorite, porphyritic granodiorite and granite porphyry to obtain granodiorite, and the crystalline age of quartz diorite and porphyritic diorite is 94.2 + 1, respectively, with.LA-ICP-MS zircon. .7Ma (N=15, MSWD=0.53), 94.3 + 1.2Ma (N=17, MSWD=0.30) and 93.9 + 1.2Ma (N=19, MSWD=0.22). The elemental geochemical characteristics show that the pine roof rock is a medium acid intrusive rock, SiO2=56.76~72.69%, Na2O=3.64~6.44%, K2O=1.88~3.87%, and belongs to the subalkaline high potassium calc alkaline series with low (0) .28~0.38); the distribution of rare earth elements is in the right tilt mode (LREE/HREE=5.75~9.84; (La/Yb) N=5.27~10.36) and delta Eu=0.71~1.12, and the trace elements are characterized by the enrichment of large ionic stone elements such as Rb, Ba, Th, U, K and LREE. The 829 and -13.8~-10.8, Nd mode age TDM is 1.68~2..05Ga, similar to the Sr-Nd isotope ratio of the early Cretaceous volcanic rocks in this area, indicating that their source region is composed of two endpoints of the Archean Lower Crust and the basalt in the bottom, and the original magma originated from the mantle wedge with the metasomatism of the plate fluid. Rock mineralization occurred in the late Cretaceous, and was formed in the extensional environment of Pacific subduction.
The geological characteristics of the deposit and the study of indoor mineralogy indicate that the mineralization process includes quartz - pyrite stage, quartz - molybdenite - pyrite - chalcopyrite stage, quartz - chalcopyrite - polymetallic phase, gray - white quartz - greenstone - pyrite - block chalcopyrite stage and five stages of quartz - carbonate phase. Fluid inclusion studies show that fluid The inclusions are mainly rich liquid inclusions and three phase inclusions containing seed crystals, and contain a small amount of rich gas inclusions. The homogenization temperature of the fluid inclusions is 149.9~450 C, and the salinity is 3.85~52.42wt%, which can be divided into five stages, 445~450, 330.5~419, 260~328.9, 204~258.4 and 149.9~180.3; among them, the rich liquid inclusions are homogeneous. The temperature is 149.9~450 C, the salinity is 3.85~12.65, the density is 0.584~0.970g/cm3, the homogeneous temperature of the three phase inclusions is 265~419 C, the salinity is 34.72~38.57wt%, the density is 1.107~1.110g/cm3, the homogeneous temperature of the rich gas phase inclusions is 358~362 C, the salinity is 3.85~9.65wt%, the density of the 0.63~0.72g/cm3. laser Raman analysis shows that the rich liquid is rich. The main components of the phase inclusions are H2O and CH4, and the composition of the three phase inclusions is mainly H2O, and the composition of the rich gas inclusions is mainly CO2 and CH4, and the fluid boiling and the temperature decrease are the important metallogenic mechanism of the two dense copper deposit.
【學位授予單位】：吉林大學
【學位級別】：碩士
【學位授予年份】：2015
【分類號】：P618.41

【參考文獻】

相關期刊論文 前10條

1 孫德有,吳福元,張艷斌,高山;西拉木倫河-長春-延吉板塊縫合帶的最后閉合時間——來自吉林大玉山花崗巖體的證據(jù)[J];吉林大學學報(地球科學版);2004年02期

2 裴福萍;許文良;于洋;趙全國;楊德彬;;吉林南部晚三疊世螞蟻河巖體的成因:鋯石U-Pb年代學和地球化學證據(jù)[J];吉林大學學報(地球科學版);2008年03期

3 王建新;陳雪;趙利剛;臧興運;謝海東;劉強;;吉林二密復式火山機構及成礦控制作用[J];吉林大學學報(地球科學版);2008年04期

4 李碧樂,孫豐月,姚鳳良;中生代敦化—密山斷裂大規(guī)模左旋平移及其對金礦床形成的控制作用[J];大地構造與成礦學;2002年04期

5 侯增謙,曲曉明,黃衛(wèi),高永豐;岡底斯斑巖銅礦成礦帶有望成為西藏第二條“玉龍”銅礦帶[J];中國地質;2001年10期

6 陳衍景;肖文交;張進江;;成礦系統(tǒng):地球動力學的有效探針[J];中國地質;2008年06期

7 孫德有,鈴木和博,吳福元,路孝平;吉林省南部荒溝山地區(qū)中生代花崗巖CHIME定年[J];地球化學;2005年04期

8 王守旭;張興春;秦朝建;石少華;冷成彪;陳衍景;;滇西北中甸普朗斑巖銅礦流體包裹體初步研究[J];地球化學;2007年05期

9 張德會;流體的沸騰和混合在熱液成礦中的意義[J];地球科學進展;1997年06期

10 劉洪文,邢樹文,周永昶;吉南地區(qū)斑巖—熱液脈型金多金屬礦床成礦模式[J];地質與勘探;2002年02期

相關博士學位論文 前1條

1 白令安;大興安嶺中北部熱液銅礦床的成礦機制與資源預測[D];吉林大學;2013年

本文編號：2059805