显生宙罕见的巨鲕及其鲕粒形态多样性的意义:以湖北利川下三叠统大冶组为例
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摘要
上扬子区早三叠世印度期的地层,从西向东由滨岸相砂泥岩(飞仙关组)到台地碳酸盐岩(大冶组),代表了一个二叠纪与三叠纪之交的大规模碳酸盐台地淹没事件之后、三叠纪早期缓坡型台地的生长发育过程。受制于三叠纪早期的两个海侵—海退旋回,早三叠世印度期大冶组中的鲕粒滩相灰岩经历了自西向东的进积作用。上述沉积作用过程的结果,在湖北利川的三叠系大冶组顶部发育厚层块状鲕粒滩相灰岩;该鲕粒灰岩,较大的粒径以及多样的宏观形态,成为一个窥视鲕粒成因的典型地点。这些主要由碳酸盐泥晶粘聚而成的粒径多超过2 mm的鲕粒,包括同心鲕粒、椭圆鲕粒、复合鲕粒、不规则鲕粒、核心不太清楚的鲕粒等多种类型。这些粒径超过2 mm的巨鲕,不但代表了显生宙较为罕见的沉积学现象,而且有可能代表了二叠纪末期生物大灭绝之后荒凉海底环境的沉积响应,为进一步了解成因还未完全明了的鲕粒所代表的碳酸盐世界提供了一个有意义的实例。
Strata of the Triassic Induan in the Upper-Yangtze region,i.e.the littoral-facies sandstones and mudstones of the Feixianguan Formation in the western part and the ramp carbonates of the Daye Formation in the eastern part,represent a developing process of a ramp carbonate platform.Controlled by the two transgressive-regressive processes in the Induan age of the Early Triassic,the oolitic-bank limestones within the Daye Formation in the Upper-Yangtze region have been undergone the obvious progradation from the west to the east.Resulting from this sedimentary process,a set of oolitic-bank limestones with the thickness of more than 40 meters is developed in the top part of the Triassic Daye Formation at the Lichuan section.For this set of oolitic-bank limestones,the larger grain size and the diversity of morphology make it become a useful example to understand the origin of oolites.Further,the diverse configurations including the circular,the sub-circular,the irregular and the composite shapes of oolites in the top part of the Triassic Daye Formation at the Lichuan section,especially for the development of the giant oolites that are unusual in the Phanerozoic,provide an important clue for the understanding of both the sedimentary response to the mass extinction at the turn from the Permian to the Triassic and the evolving carbonate world that is reflected by the oolite whose origin remains uncertain.
Strata of the Triassic Induan in the Upper-Yangtze region,i.e.the littoral-facies sandstones and mudstones of the Feixianguan Formation in the western part and the ramp carbonates of the Daye Formation in the eastern part,represent a developing process of a ramp carbonate platform.Controlled by the two transgressive-regressive processes in the Induan age of the Early Triassic,the oolitic-bank limestones within the Daye Formation in the Upper-Yangtze region have been undergone the obvious progradation from the west to the east.Resulting from this sedimentary process,a set of oolitic-bank limestones with the thickness of more than 40 meters is developed in the top part of the Triassic Daye Formation at the Lichuan section.For this set of oolitic-bank limestones,the larger grain size and the diversity of morphology make it become a useful example to understand the origin of oolites.Further,the diverse configurations including the circular,the sub-circular,the irregular and the composite shapes of oolites in the top part of the Triassic Daye Formation at the Lichuan section,especially for the development of the giant oolites that are unusual in the Phanerozoic,provide an important clue for the understanding of both the sedimentary response to the mass extinction at the turn from the Permian to the Triassic and the evolving carbonate world that is reflected by the oolite whose origin remains uncertain.
引文
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[20]吴应林,朱洪发,朱忠发,等.中国南方三叠纪岩相古地理与成矿作用[M].北京:地质出版社,1994.
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[22]梅冥相,李仲远.滇黔桂地区晚古生代至三叠纪层序地层序列及沉积盆地演化[J].现代地质,2004,18(4):555-563.
[23]梅冥相,马永生,郑宽兵,等.加里东运动构造古地理及滇黔桂盆地的形成———兼论滇黔桂盆地深层油气勘探潜力[J].地学前缘,2005,12(3):227-236.
[24]梅冥相,马永生,邓军,等.滇黔桂盆地及其邻区二叠系乐平统层序地层格架及其古地理背景[J].中国科学:D辑,2007,37(5):605-617.
[25]颜佳新,伍明.显生宙海水成分、碳酸盐沉积和生物演化系统研究进展[J].地质科技情报,2006,25(3):1-7.
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[27]Wright V P,Burgess P M.The carbonate factory continuum,fa-cies mosaics and microfacies:an appraisal of some of the keyconcepts underpinning carbonate sedimentology[J].Facies,2005,51:17-23.
[28]Pomer L,Hallock P.Carbonate factories:a conundrum in sedi-mentary geology[J].Earth-Science Reviews,2008,87:134-169.
[29]Schlager W.Secular oscillations in the stratigraphic record:anacute debate[J].Facies,2005,51:12-16.
[30]Gmez J J,Fernndez-Lpez S.Condensed processes in shallowplatform[J].Sedimentary Geology,1994,92:147-159.
[31]Hallam A,Wignall P G.Mass extinction and sea-level changes[J].Earth-Science Reviews,1999,48:217-250.
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[33]Stanley S M.Earth System History[M].NewYork:W HFree-man and Company,1999:399-434.
[34]Enos P,Wei Jiayong,Lehrmann D J.Death in Guizhou—LateTriassic drowning of the Yangtze carbonate platform[J].Sedi-mentary Geology,1998,118:55-76.
[35]Goldhammer R K,Dunn P A,Hardie L A.Depositional cycles,composite sea-level changes,cycle stacking patterns,and the hi-erarchy of stratigraphic forcing:example from Alpine Triassicplatform carbonates[J].Geological Society of American Bulle-tin,1990,102:535-562.
[36]Vail P R,Mitchum R M,Thompson S.Seismic stratigraphy andglobal changes of sea level,part3 and part4[J].American As-sociation of Petroleum Geologist Memoir 26,1977:63-98.
[37]Read J F,Goldhammer R K.Use of Fischer plots to define third-order sea-level curves in Ordovician peritidal cyclic carbonates,Appalachians[J].Geology,1988,16:895-899.
[38]Hunt D,Tucker ME.Stranded parasequences and forced regres-sive wedge system tract:deposition during base-level fall[J].Sedimentary Geology,1992,81:1-9.
[39]Walker R G,James N P.Facies Models:Response to Sea-LevelChange[M].Ontario:Geological Association of Canada,1992.
[40]Reading H G.Sedimentary Environment:Processes,Facies andStratigraphy[M].Oxford:Blackwell Scientific Publication,1996.
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[42]Swett K,Knoll AH.Marine pisolites from Upper Proterozoic car-bonates of East Greenland and Spitzbergen[J].Sedimentology,1989,36:75-93.
[43]Knoll AH,Swett K.Carbonate deposition during the later Proter-ozoic Era:an example from Spitzbergen[J].American Journalof Science,1990,290(A):104-132.
[44]Wignall P B,Twitchett R J.Unusual intraclastic limestones inlower Triassic carbonates and their bearing on the aftermath of theend-Permian mass extinction[J].Sedimentology,1999,46:303-316.
[45]Schubert J K,Bottjier D J.Early Triassic stromatolites as post-mass-extinction disaster forms[J].Geology,1992,20:883-886.
[46]Hips K,Hass J.Calcimicrobial stromatolites at the Permian-Tri-assic boundary in a western Tethyan section,Bukk Mountains,Hungary[J].Sedimentary Geology,2006,185:239-253.
[47]Pruss S,Fraiser M,Bottjer D J.Proliferation of early Triassicwrinkle structures:implications for environmental stress followingthe end-Permian mass extinction[J].Geology,2004,32:461-464.
[48]刘建波,江崎洋一,杨守仁,等.贵州罗甸二叠纪末生物大灭绝事件后沉积的微生物岩的时代和沉积学特征[J].古地理学报,2007,9(5):473-486.
[49]Riding R.Microbial carbonates:the geological record of calcifiedbacterial-algal mats and biofilms[J].Sedimentology,2000,47(1):179-214.
[50]Riding R.Microbial carbonate abundance compared with fluctua-tions in metazoan diversity over geological time[J].SedimentaryGeology,2006,185:229-238.
[51]梅冥相.微生物碳酸盐岩分类体系的修订:对灰岩成因-结构分类体系的补充[J].地学前缘,2007,14(5):597-614.
[52]Perri E,Tucker ME.Bacterial fossils and microbial dolomite inTriassic stromatolites[J].Geology,2007,35:207-210.
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