【摘要】：萬合永火山盆地位于大興安嶺南段最南端,華北北緣增生帶北側(cè),緊鄰西拉沐倫斷裂帶。盆地基底受古生代近東西向古亞洲洋構(gòu)造域控制明顯,蓋層受晚中生代北東向環(huán)太平洋構(gòu)造域影響,因此在其構(gòu)造活動史上必然受古亞洲構(gòu)造域和太平洋構(gòu)造域的雙重影響。盆地區(qū)內(nèi)廣泛發(fā)育晚中生代火山巖,以出露過鋁質(zhì)高鉀鈣堿性流紋巖組合為特征,呈北東向展布。本文在充分收集整理前人資料的基礎(chǔ)上,主要以萬合永火山盆地下馬架-劉家營子流紋巖為研究對象,利用SHRIMP鋯石U-Pb同位素測年技術(shù)確定流紋巖的形成時代;通過實(shí)測野外地質(zhì)剖面,查明了巖石組合特征,確定了流紋巖的地層時代歸屬;最后通過巖石學(xué)、巖石地球化學(xué)分析,并結(jié)合已有區(qū)域資料,討論了流紋巖的巖石成因、物質(zhì)來源與其形成的構(gòu)造背景。研究區(qū)內(nèi)主要出露一套中酸性火山巖、火山碎屑巖組合,以盆地內(nèi)出露的一套紫紅色的碎屑巖組合為標(biāo)志,同時結(jié)合下馬架-劉家營子流紋巖的年齡數(shù)據(jù),將盆地內(nèi)原屬于滿克頭鄂博組火山巖中的這套紫紅色碎屑巖組合劃歸為土城子組,將其之下的一套中酸性火山巖組合劃歸入新民組,將其之下的中酸性火山巖組合劃歸入興安群。下馬架-劉家營子流紋巖SHRIMP鋯石U-Pb年齡顯示為159.6±1.5Ma,表明晚中生代時期研究區(qū)內(nèi)存在火山-巖漿事件,巖漿活動時間為晚侏羅世。巖石地球化學(xué)資料顯示,萬合永火山盆地鈣堿性流紋巖以高硅高鉀、貧鈣鎂為特征,在火山巖TAS圖解,流紋巖顯示為亞堿性系列。流紋巖分異指數(shù)DI值介于89.83~96.32之間,表明在其巖漿演化過程中經(jīng)歷了較高程度的分離結(jié)晶作用。稀土元素總量較高,ΣREE值為264.44×10-6~540.98×10-6,輕、重稀土元素分餾較為明顯,(La/Yb)N值為5.34~14.46,輕稀土元素明顯富集,ΣLREE/ΣHRE值為7.83~10.33,重稀土較為平坦,稀土元素球粒隕石標(biāo)準(zhǔn)化配分模式圖顯示為典型的輕稀土右傾型,具有強(qiáng)烈的負(fù)Eu異常,正Ce異常不明顯。微量元素分析顯示,流紋巖明顯的富集Rb、Zr、Th、Ga、Y等而虧損Ba、Sr、Ti、P等元素,與大興安嶺地區(qū)低Ba-Sr流紋巖地球化學(xué)特征一致。下馬架-劉家營子流紋巖在K2O+Na2O、K2O/Mg O、Zr、Nb-10000Ga/Al以及Fe OT/Mg O、(K2O+Na2O)/Ca O-Zr+Nb+Ce+Y圖解上,全部落入到A型花崗巖區(qū)域。其Rb/Sr、Ti/Zr、Ti/Y與Th/La比值分別為1.52~10.00、0.01~0.03、0.28~0.39、0.18~1.45,都在殼源巖漿范圍內(nèi);在Ce/Nb-Th/Nb圖解上,樣品落入大陸地殼范圍內(nèi),說明其物質(zhì)來源與地殼物質(zhì)相關(guān)。在R1-R2以及Nb-Y-3Ga、Nb-Y-Ce圖解上,樣品落入到后造山花崗巖區(qū)域;在Y-Nb與(Y+Nb)-Rb圖解上,樣品全部落入到板內(nèi)花崗巖區(qū),表明其應(yīng)該形成于板塊內(nèi)部造山后的伸展拉張構(gòu)造環(huán)境。綜上所述,下馬架-劉家營子流紋巖應(yīng)歸屬于新民組,形成于晚侏羅世,其物質(zhì)來源為地殼物質(zhì)的部分熔融,應(yīng)該形成于板塊內(nèi)部造山后伸展拉張的構(gòu)造環(huán)境,可能與蒙古-鄂霍茨克洋的演化有關(guān)。
[Abstract]:The Wanheyong volcanic basin is located at the southernmost end of the southern part of the Daxinganling Mountains, north of the North China North margin accretive belt, adjacent to the Xilamulun fault zone. The basement of the basin is obviously controlled by the Paleozoic near east-west direction paleo-ocean tectonic domain, and the cover is influenced by the late Mesozoic north-east circumferential Pacific tectonic domain. Therefore, the tectonic activity of the basin is bound to be influenced by the paleo-Asian tectonic domain and the Pacific tectonic domain in the history of its tectonic activity. The late Mesozoic volcanic rocks are widely developed in the basin area, characterized by the outcropping of aluminous high-potassium calc-alkaline rhyolite assemblages, which are distributed in the north to east direction. On the basis of collecting and sorting out the previous data, this paper mainly takes the Xiamajiayingzi rhyolite in the Wanheyong volcanic basin as the research object, and uses the SHRIMP zircon U-Pb isotope dating technique to determine the age of the rhyolite formation. The characteristics of rock assemblage and stratigraphic age of rhyolite are determined by field geological profile. Finally, the petrogenesis, material source and tectonic setting of rhyolite are discussed through petrology, petrogeochemical analysis and regional data. In the study area, a set of intermediate-acid volcanic rocks and volcanic clastic assemblages, marked by a set of purplish red clastic assemblages from the basin, and age data of Xiamaka-Liujiayingzi rhyolite, The fuchsia clastic rock assemblage, which belongs to the volcanic rocks of the Mankitou Obo formation in the basin, is classified as Tuchengzi formation, and a set of intermediate-acid volcanic rock assemblages under the assemblage are classified into the Xinmin formation. The intermediate-acid volcanic rock assemblage under it is classified into the Xingan Group. The SHRIMP zircon U-Pb age of Xiamajiayingzi rhyolite is 159.6 鹵1.5 Ma, indicating that there were volcanic-magmatic events in the study area during the late Mesozoic, and the magmatic activity occurred in the late Jurassic. The petrogeochemical data show that the calc-alkaline rhyolite in Wanheyong volcanic basin is characterized by high silicon and high potassium and poor calcium and magnesium. In the TAS diagram of volcanic rocks the rhyolite is subalkaline series. The DI value of the rhyolite differentiation index is between 89.83 and 96.32, which indicates that the rhyolite experienced a high degree of separation and crystallization in the process of magmatic evolution. The total amount of rare earth elements is relatively high, 危 REE value is 264.44 脳 10-6, 540.98 脳 10-6, light, heavy rare earth element fractionation is obvious, (La/Yb) N value is 5.34 ~ 14.46, light rare earth element is obviously enriched, 危 LREE/ 危 HRE value is 7.83 ~ 10.33, The normalized partition pattern of chondrites of rare earth elements shows a typical light rare earth right-dip type with strong negative Eu anomalies and no significant positive Ce anomalies. Trace element analysis shows that rhyolite is obviously enriched in Rb,Zr,Th,Ga,Y and depleted in elements such as Ba,Sr,Ti,P, which is consistent with the geochemical characteristics of low Ba-Sr rhyolite in Daxinganling area. The Liujiayingzi rhyolite all fell into the A-type granite area on the K _ 2O Na2O,K2O/Mg, ZrNb-10000Ga / Al and Fe OT/Mg O, (K _ 2O Na2O) / Ca O-Zr Nb Ce Y diagrams. The ratio of Rb/Sr,Ti/Zr,Ti/Y to Th/La is 1.52U 10.00 0. 01 ~ 0. 03U 0.28 ~ 0. 39 ~ 0. 18 ~ 1. 45, which are within the range of crust-derived magma. In the Ce/Nb-Th/Nb diagram, the samples fall into the continental crust, indicating that the source of the material is related to the crustal material. In the R1-R2 and Nb-Y-3Ga,Nb-Y-Ce diagrams, the samples fall into the post-orogenic granite area. On the Y-Nb and (Y Nb) Rb diagrams, all samples fall into the intraplate granite area, indicating that they should be formed in the extensional and extensional tectonic environment after orogeny within the plate. In conclusion, the rhyolite belongs to the Xinmin formation, formed in the late Jurassic, and originated from the partial melting of the crustal material, and should be formed in the tectonic environment of extension and extension after orogeny within the plate. It may be related to the evolution of Mongol-Okhotsk Ocean.
【學(xué)位授予單位】：東華理工大學(xué)
【學(xué)位級別】：碩士
【學(xué)位授予年份】：2015
【分類號】：P588.141

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