新疆克孜勒塔格东北一带地层特征及地质演化
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摘要
本文研究区位于新疆克孜勒塔格东北一带,属于北山裂谷构造带西段。北山裂谷构造带是在塔里木原始陆核基础上发展起来的,北邻那拉提—红柳河缝合带,南接敦煌地块。构造带内断裂发育,岩浆活动强烈,地层包括了早元古代变质结晶基底、中元古代沉积盖层、晚古生代裂谷沉积盖层。
变质结晶基底—北山岩群是早元古代围绕陆核和陆核间出现的浅海环境下沉积的一套以火山岩为主夹少量成熟度低的碎屑岩经多期变质作用而成的成层无序地层。北山岩群主期变质作用是兴地期(1800Ma)中压角闪岩相变质作用,变质温度580-650℃、压力0.58-0.69GPa;主期褪变质作用是阿尔金期(1400Ma)绿帘角闪岩相变质作用,变质温度350-550℃、压力0.4-0.6Gpa,500℃左右温度可能是其主褪变质作用发生的主要温度。到了晚古生代,北山裂谷再次开始了拉张—闭合的演化,并伴随了大规模的火山喷发和岩浆侵位,使北山裂谷构造带内的地温梯度升高,在靠近侵入体的位置发生了接触变质作用,接触变质作用产生了排列不定向的片状黑云母。裂谷闭合收缩挤压和印支—喜山期动力作用及后期剪切作用影响使得北山岩群中的各期侵入岩体发生了碎裂岩化和糜棱岩化。
中元古代沉积盖层—古硐井岩群是浅海—滨海环境沉积的一套以沉积岩为主夹有少量凝灰岩的经变质作用而形成的一套成层无序的地层,其变质作用是北山岩群发生主褪变质作用的阿尔金期变质作用,温度压力要稍低于北山岩群。
晚古生代裂谷沉积地层有下石炭统红柳园组、上石炭统石板山组和胜利泉组、干泉组及中二叠统骆驼沟组,其中红柳园组、石板山组、胜利泉组、干泉组为北山裂谷构造带在晚古生代早石炭世第一次拉张—晚石炭世闭合期间所沉积,骆驼沟组为中二叠世第二次收缩闭合期间所沉积。
The area be studied in this dissertation located at the northeast of Keziletage in XinJiang,it is a part of the west Beishan rift valley structure belt .Beishan rift valley structure belt developed in Talimu land core, it’s north neighbour is Nalati-Hongliuhe suture belt and the south one is Dunhuang landmass. Here are a lot of ruptures and magma rocks in the belt.The stratum includes early proterozoic era metamorphic crystal basement、middle proterozoic era sedimented cover layer and later Paleozoic era rift valley sediment.
Metamorphic crystal basement-Beishan rock group are stratified but out of order layers, which lava and few juvenility clastic rock were sedimented in shallow sea around or between the early proterozoic era landmass. Main period metamorphism of Beishan rock group is Xingdi period(1800Ma) middle press hornblende facies , the temperature of this facies is 580-680℃,and press is 0.58-0.69GPa. Main period of fade metamorphism is Aerjin period ,its temperature is 350-550℃and press 0.4-0.6Gpa. Nearby 500℃maybe the mostly temperature of Main period of fade metamorphism . In later Paleozoic era , Beishan valley developed from craze to lose , at the same time , lots of volcanoes broken forth and lava up invaded , what makes ground temperature grads hoist, rocks nearby lava occurred contact metamorphic, which produced nondirective biotite . The close of rift valley and Indo-China -The Himalayas period drive effect made intrusive rock to be cataclastic or mylonite.
Middle proterozoic era sedimented cover layer-Gudongjing rock group are stratified but out of order layers, which juvenility clastic rock and few lava were sedimented in shallow sea ,its Main period metamorphism is the main period of fade metamorphism of Beishan rock group ,however the temperature and press are a little lower than that of Beishan rock group .
There are below Carboniferous system Hongliuyuan group、up Carboniferous system Shibanshan group、Shengli spring group、Ganquan group and middle Permian Luotuogou group sedimented in later Paleozoic era , Hongliuyuan group、Shibanshan group、Shengli spring group、Ganquan group were sedimented when the rift valley drawing opening period for the first time ,and Luotuogou group was sedimented in the second shrinking closing period .
变质结晶基底—北山岩群是早元古代围绕陆核和陆核间出现的浅海环境下沉积的一套以火山岩为主夹少量成熟度低的碎屑岩经多期变质作用而成的成层无序地层。北山岩群主期变质作用是兴地期(1800Ma)中压角闪岩相变质作用,变质温度580-650℃、压力0.58-0.69GPa;主期褪变质作用是阿尔金期(1400Ma)绿帘角闪岩相变质作用,变质温度350-550℃、压力0.4-0.6Gpa,500℃左右温度可能是其主褪变质作用发生的主要温度。到了晚古生代,北山裂谷再次开始了拉张—闭合的演化,并伴随了大规模的火山喷发和岩浆侵位,使北山裂谷构造带内的地温梯度升高,在靠近侵入体的位置发生了接触变质作用,接触变质作用产生了排列不定向的片状黑云母。裂谷闭合收缩挤压和印支—喜山期动力作用及后期剪切作用影响使得北山岩群中的各期侵入岩体发生了碎裂岩化和糜棱岩化。
中元古代沉积盖层—古硐井岩群是浅海—滨海环境沉积的一套以沉积岩为主夹有少量凝灰岩的经变质作用而形成的一套成层无序的地层,其变质作用是北山岩群发生主褪变质作用的阿尔金期变质作用,温度压力要稍低于北山岩群。
晚古生代裂谷沉积地层有下石炭统红柳园组、上石炭统石板山组和胜利泉组、干泉组及中二叠统骆驼沟组,其中红柳园组、石板山组、胜利泉组、干泉组为北山裂谷构造带在晚古生代早石炭世第一次拉张—晚石炭世闭合期间所沉积,骆驼沟组为中二叠世第二次收缩闭合期间所沉积。
The area be studied in this dissertation located at the northeast of Keziletage in XinJiang,it is a part of the west Beishan rift valley structure belt .Beishan rift valley structure belt developed in Talimu land core, it’s north neighbour is Nalati-Hongliuhe suture belt and the south one is Dunhuang landmass. Here are a lot of ruptures and magma rocks in the belt.The stratum includes early proterozoic era metamorphic crystal basement、middle proterozoic era sedimented cover layer and later Paleozoic era rift valley sediment.
Metamorphic crystal basement-Beishan rock group are stratified but out of order layers, which lava and few juvenility clastic rock were sedimented in shallow sea around or between the early proterozoic era landmass. Main period metamorphism of Beishan rock group is Xingdi period(1800Ma) middle press hornblende facies , the temperature of this facies is 580-680℃,and press is 0.58-0.69GPa. Main period of fade metamorphism is Aerjin period ,its temperature is 350-550℃and press 0.4-0.6Gpa. Nearby 500℃maybe the mostly temperature of Main period of fade metamorphism . In later Paleozoic era , Beishan valley developed from craze to lose , at the same time , lots of volcanoes broken forth and lava up invaded , what makes ground temperature grads hoist, rocks nearby lava occurred contact metamorphic, which produced nondirective biotite . The close of rift valley and Indo-China -The Himalayas period drive effect made intrusive rock to be cataclastic or mylonite.
Middle proterozoic era sedimented cover layer-Gudongjing rock group are stratified but out of order layers, which juvenility clastic rock and few lava were sedimented in shallow sea ,its Main period metamorphism is the main period of fade metamorphism of Beishan rock group ,however the temperature and press are a little lower than that of Beishan rock group .
There are below Carboniferous system Hongliuyuan group、up Carboniferous system Shibanshan group、Shengli spring group、Ganquan group and middle Permian Luotuogou group sedimented in later Paleozoic era , Hongliuyuan group、Shibanshan group、Shengli spring group、Ganquan group were sedimented when the rift valley drawing opening period for the first time ,and Luotuogou group was sedimented in the second shrinking closing period .
引文
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[2] Boynton W V. Geochemistry of the rare earth elements: meteorite studies [C]/ /Henderson P (ed). Rare Earth Element Geochemistry. Elsevier, Amsterdam., 1984: 63- 114.Sugisaki R, Yamamoto K, Adachi M. Triassic bedded cherts in central Japan are not pelagic.Nature,1982,298(5875):644～647
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[9] Le Bas M J, Le Maitre R W, Streckeisen A, et al. A chemical classification of volcanic rocks based on the total alkali– silica diagram [J]. Journal of Petrology., 1986, 27: 745- 750
[10] Pearce J A, Norry M J. Petrogenetic implications of Ti, Zr, Y and Nb variations in volcanic rocks[J]. Contrib. Mineral. Petrol., 1979,69: 33- 47
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[13] Rona P A. Criteria for recognition of hydrothermal mineral deposits in ocean crust [J ] . Econ Geol ,1978 ,73 :135– 160.
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[15] Sun S S, Nesbitt R W. Geochemical characteristics of mid- ocean ridge basalts[J]. Earth Planet. Sci. Lett., 1979,44: 119- 138
[16] Yamamoto K. Geochemical characteristics and depositional enviroment of cherts and associated rocks in the Franciscan and Shiment terranes[J ] . Sediment Geol ,1987 ,52 :65– 108
[17]白君武.新疆大阪城西南硅质岩成因及其成矿意义[D].中国地质大学,2006
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