Recognition and Correlation of Supersequences in Lhasa Block, Southern Tibet

LI XiangHui; WANG ChengShan; WU RuiZhong

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Article Navigation > Acta Sedimentologica Sinica > 2002 > 20(2): 179-187

LI XiangHui, WANG ChengShan, WU RuiZhong. Recognition and Correlation of Supersequences in Lhasa Block, Southern Tibet[J]. Acta Sedimentologica Sinica, 2002, 20(2): 179-187.

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LI XiangHui, WANG ChengShan, WU RuiZhong. Recognition and Correlation of Supersequences in Lhasa Block, Southern Tibet[J]. Acta Sedimentologica Sinica, 2002, 20(2): 179-187.

Recognition and Correlation of Supersequences in Lhasa Block, Southern Tibet

Chengdu University of Technology,Chengdu 610059

Received Date: 2001-06-24
Rev Recd Date: 2001-08-30
Publish Date: 2002-04-10

Abstract

Eleven sedimentary supersequences CQ ₁_～₁₁ of marine Paleozoic and Mesozoic sediments are recognized in the Coqen basin, Lhasa Block. Detailed characteristics of sedimentation, age range, number, and T-R tecture are described in the paper, and correlations and discussions of supersequence between Tethys Himalaya and Lhasa Block are made. CQ 1 is temporally thought to be the Cambrian supersequence due to crystallinely metamorphic rocks. CQ 2 of the Ordovician supersequence is dominated by black shale and limestone, in which only regressive part is exposed and the transgressive sediment is not. CQ 3 within duration of ca. 39 Ma of the Silurian supersequence is characterized by a texture of depositional sequence sets from transgressive shalely and limy rocks to medium-thicked wackstone and packstone, within which abundant grapitutid and little thinned shelly brachiopod became shallower sea coral and conodent. The boundary between the CQ 2 and CQ 3 is placed at the Lower Ashgill of Upper Ordovician. As the Devonian supersequence in range of ca. 48 Ma, CQ4 can be broadly recognized in the Coqen basin, which is composed of transgrassive and regreassive sets. Thinned marlstone with the mixture of shale, siltstone, and sandstone and benthos associated with planktons comprises the former, and the later is of property of shallow sea dolomitized and crystalline limestone. This supersequence is separated the CQ 3 away by terrigenous sediment at the base of Devonian. CQ 5 is limited in Lower Carboniferous with an interval of ca. 33 Ma. It starts by the wormkalk at the bottom of Carboniferous and continues by bioclastic and intraclastic limestone, for which the transgrassive and regreassive depositional sets are vague to distinguish. CQ 6 ranges from upper Lower Carboniferous to lower Lower Permian with a total age of ca. 55 Ma. It is characterized by glaciomarine shale with lens of limestone and cool fauna fossils, and the boundary between CQ 6 and CQ 5 is located at the sharp contact of terrigenous rocks onto carbonate rocks. CQ 7 is the latest supersequence in Paleozoic, which has duration of age time ca. 30 Ma in most of Permian. The transgressive depositional sequence set is similar as the set in the CQ 6 and became the shallower carbonate sediments of regressive set. CQ 8 and CQ 7 are separated by disconformable and erosional surface at the base of the Triassic Quehala group. The age range of the supersequence is estimated 37 Ma. The transgressive set is not exposed, and the regression is consitituent of terrigenous turbidite of inner fan with little volcanic and carbonate rock. There is a nonconformity contact between the CQ 9 and CQ 8, above which the transgressive depositional sequence set is superposed by flysch middle and outer turbidite fan, and follows by changeable and complicated system sediment. It is ranges ca. 63 Ma and is separated over CQ 10 away by a regional unconformity. Supersequence CQ 10 is composed of kinds of limestone and clastic rocks in shallow sea environment deposited in Lower Cretaceous (50 Ma). The transgressive set is combined by hybrid sediments of shallow and volcanic rock, and the regressive by predominant carbonate rocks. The Upper Cretaceous supersequence CQ 11 is the only one superposed by much continental delta and shore facies. In general, the T-R sets are not readily differentiated either in filed or in room. Of them, three supersequencesCQ ₁_～₃ are classified in Early Paleozoic; four CQ ₄_～₇ and four CQ ₈_～₁₁ are in Late Paleozoic and Mesozoic respectively. The sedimentation, age range, number, and T-R texture of the super sequences CQ ₁_～₃ are similar, but different are in the CQ ₄_～₇ and CQ ₈_～₁₁ of Upper Paleozoic and Mesozoic. We suppose that the turnover of supersequence from Early to Late Paleozoic could be caused by the changes of tectonic and types of sedimentary basin, but not by second-order sea-level change, because there should be a same / similar sedimentary response to eustatic change for sedimentary basins
- supersequence,
- Cimmerian Subcontinent,
- Indian Subcontinent,
- Gondwanal,
- and Paleozoic,
- Mesozoic,
- Lhasa Block

References

[1]

1. Gaetani M & Garzanti E.Multicyclic history of the northern India continental margin （northwestern Himalaya） [J]. AAPG Bull.,1991, 75（9）: 1 427～1 446

2. 李祥辉，王成善。特提斯喜马拉雅显生宙的超层序[J].特提斯地质。1997,（21）: 8～30 [Li Xianghui,Wang Chengshan.Supersequences of the Phanerozoic in the Tethys Himalayas [J].Tethys Geology,1997,（21）:8～30]

3. Wang C S ,Li X H.Supersequences of the Phanerozoic in the Tethys Himalayas [A].In: Liu B J and Li S T,eds.,Basin analysis,global sedimentary geology and sedimentology [C].Proceedings of the 30th IGC,1997,8: 275～293

4. 西藏区调队。西藏地矿局。中华人民共和国区域地质调查报告1:1000000,拉萨幅H-46 [M].北京: 地质出版社，1979[Tibet Survey of Tibet Bureau of Geology and Mineral Resources.Caption of Geology Map:1∶1000000,Lhasa H-46,P.R.China [M].Beijing:Geological Publishing House,1979]

5. 西藏地质局综合普查大队。西藏申扎地区古生代地层的新发现[J].地质论评，1980,26（2）: 162,151[Reconnaissance Survey Team of Tibet Geology Bureau.New discovery of Paleozoic strata in Shenzha area,Tibet[J].Geological Review,1980,26（2）:162,151]

6. 喻洪津。藏北申扎地区中-晚志留世牙形剌生物地层[A].青藏高原地质文集（16）[C].北京: 地质出版社，1985.15～34[Yu Hongjin.Middle-Late conodont biostratigraphy in Shenzha area,northern Tibet[A].Contributions to Qinghai-Xizang Plateau Geology （16）[C].Beijing:Geological Publishing House,1985.15～34]

7. 西藏区调队。西藏地矿局。中华人民共和国区域地质调查报告1:1000000,日喀则幅H-45、亚东幅G-45[M].北京: 地质出版社，1983[Tibet Survey of Tibet Bureau of Geology and Mineral Resources.Caption of Geology Map:1∶1000000,Xigaze H-46,Yadong G-45,P.R.China[M].Beijing:Geological Phblishing House,1983]

8. 陈清华，王建平，王绍兰，吴孔友。西藏措勤盆地上二叠统的发现及其地质意义[J].科学通报，1998,43（19）:2 111～2 114[Chen Qinghua,Wang Jianping,Wang Shaolan,Wu Kongyou.The discovery of Upper Permianin the Cuoqen basin of Tibet and its significances[J].Chinese Science Bulletin,1998,43（19）:2 111～2 114]

9. Marcoux J,Girardeau J,Fourcade E,et al.Geology and biostratigraphy of the Jurassic and Lower Cretaceous series to the north of the Lhasa Block （Tibet,China）[J].Geodinamica Acta （Paris），1987,1（4/5）: 313～326

10. 王冠民。西藏措勤盆地下白垩统多巴组沉积环境分析[J].沉积学报，2000,18（3）: 349～354[Wang Guanmin.Sedimentary environment analysis of the Duoba Formation of Lower Cretaceous in the Cuoqen basin of Tibet[J].Acta Sedimentaologica Sinica,2000,18（3）:349～354]

11. Vail P R,Mitchum R M,Todd R G,et al.Seismic stratigraphy and global changes of sea level [A].In: Payton C E,ed.Seismic Stratigraphy-Applications to Hydrocarbon Exploration [C].AAPG Mem.,1977,26: 49～212

12. 刘训，傅德荣，姚培毅等。青藏高原不同地体的地层、生物区系及沉积构造演化史[M].北京: 地质出版社，1992.169[Liu Xun,Fu Derong,Yao Peiyi,et al.Tectonic evolution of terranes on strata,biota and sediment in the Qinghai-Xizang Plateau [M].Beijing:Geological Phblishing House,1992.169]

13. 陈挺恩。西藏南部奥陶纪头足类动物群特征及奥陶系的再划分[J].古生物学报，1984,23（4）: 452～471[Chen Ting-en.Ordovician cephalopod fauna and Ordovician reclassification in southern Tiber[J].Acta Palaeotologica Sinica,1984,23（4）:452～471]

14. 李祥辉，吴铬，王成善等。西藏措勤盆地古生界-中生界岩相古地理演化[J].成都理工学院学报，2001,28（3）: 1～10[Li Xianghui,Wu Ge,Wang Chengshan,et al.Paleozoic to Mesozoic changes of lithofacies and paleogeography of the Cuoqen Basin,central Tibet[J].Journal of Chengdu University of Technology,28（4）:331～339]

15. Sengr A M C.The Cimmeride orogenic system and the tectonics of Eurasia [M].Spec.Pap.GSA,1984,195: 7～82

Sengr A M C.The story of Tethys: How many views did Okeanos have? [J] Episode,1985,8: 3～12

16. 徐仁。藏南舌羊齿植物群的发现和其在地质学和古地理学上的意义[J].地质科学，1976,10（4）: 323～332[Xu Ren.The Discovery of Glossoperis flora in southern Tibet and its significances on geology and paleogeography [J].Scientia Geologica Sinica,1976,10（4）:323～332]

17. 林宝玉。西藏中南部雅鲁藏布江两侧早二叠世地层和珊瑚动物学[A].中法喜马拉雅考察报告（1980）[C].北京: 地质出版社，1984.63～84[Lin Baoyu,Early Permian and coral invertebrate along both northern and southern sides of Yarlung Zangbo[A].In:Report to the Himalaya Geological Investigation of Sino-France united team （1980）[C].Beijing:Geological Publishing House,1984.63～84]

18. 杨式溥，范影年。西藏石炭纪腕足类动物群及其古动物地理区系特征[A].青藏高原地质文集（11）[C],1983.265～289[Yang Shipu,Fan Yingnian.Carboniferous brachiopod fauna and their biota feature in Tibet[A].Contributions to Qinghai-Xizang Plateau Geology（11）[C].Beijing:Geological Publishing House,1983.265～289]

19. 范影年。中国西藏石炭-二叠纪皱纹珊瑚的地理区系[A].青藏高原地质文集（16）[C],1985.87～106[Fan Yingnian.Rogusa biota of Carboniferous and Permian in Tibet of China[A].Contributions to Qinghai-Xizang Plateau Geology （16）[C].1985.87～106]

20. 范影年。西藏石炭系[M].重庆: 重庆出版社，1988.128[Fan Yingnian.Carboniferous in Tibet[M].Chongqing:Chongqing Press,1988.128]

21. 王连城，郭师曾。西藏的含砾板岩[A].西藏南部的沉积岩[C].北京: 科学出版社，1981.73～86[Wang Liancheng,Guo Shizeng.Diamictites in Tibet[A].In:Sedimentary Rocks in Southern Tibet[C].Beijing:Science Press,1981.73～86]

22. 韩同林，王乃文。西藏北部石炭纪冰川-海洋相地层的发现[J].中国地质科学院院报，1983,7: 41～56[Han Tonglin and Wang Naiwen.Discovery of Carboniferous glacial-type marine strata [J].Journal of Chinese Geology Academy,1983,7:41～56]

23. 陈炳蔚。西藏八宿来姑中、上石炭统似冰碛岩的发现及其意义[J].地质论评，1982,28（2）: 148～151[Chen Bingwei.Discovery of middle-Upper Carboniferous para-tillite at Laigu of Basu,Tibet and its significances[J].Geological Review,1982,28（2）:148～151]

24. 尹集祥，闻传芬。西藏石炭系和下二叠统杂砾岩及其地层特征和成因讨论[A].地质研究所集刊[C],1988,3: 26～54[Yin Jixiang,Wen Chuanfen.Carboniferous and Lower Permian diamictites within stratigraphical controls and causes discussion in Tibet [A].In:Treatise of Geology Institute of Chinese Academy[C].1988,3:26～54]

25. Yin J X.Characteristics of diamictites from the Late Carbonaiferous Pondo Group in Lhasa terrane,Xizang （Tibet） of China and discussion on the origin [A].In: Onzieme Congress Inter.De Stratigr.et de Geologie du Carbonifere [C].Beijing,Compte Rendu,Tom.4,Nanjing University Press,1989.96～105

26. Leeder M R,Smith A B,Yin J X.Sedimentology,palaeoecology and palaeoenvironmental evolution of the 1985 Lhasa to Gulmod geotraverse [A].In Geological Evolution of Tibet [C].Phil.Trans.R.Soc.Lond.,1988,A327; 107～144

27. 尹集祥。青藏高原及邻区冈瓦纳相地层地质学[M].北京: 地质出版社，1997.206[Yin Jixiang.Gondwanaland stratigraphic geology in Tibet and surrounding areas[M].Beijing:Geological Publishing House,1997.206]

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Recognition and Correlation of Supersequences in Lhasa Block, Southern Tibet

Chengdu University of Technology,Chengdu 610059

Received Date: 2001-06-24

Rev Recd Date: 2001-08-30

Publish Date: 2002-04-10

Key words:

Abstract: Eleven sedimentary supersequences CQ ₁_～₁₁ of marine Paleozoic and Mesozoic sediments are recognized in the Coqen basin, Lhasa Block. Detailed characteristics of sedimentation, age range, number, and T-R tecture are described in the paper, and correlations and discussions of supersequence between Tethys Himalaya and Lhasa Block are made. CQ 1 is temporally thought to be the Cambrian supersequence due to crystallinely metamorphic rocks. CQ 2 of the Ordovician supersequence is dominated by black shale and limestone, in which only regressive part is exposed and the transgressive sediment is not. CQ 3 within duration of ca. 39 Ma of the Silurian supersequence is characterized by a texture of depositional sequence sets from transgressive shalely and limy rocks to medium-thicked wackstone and packstone, within which abundant grapitutid and little thinned shelly brachiopod became shallower sea coral and conodent. The boundary between the CQ 2 and CQ 3 is placed at the Lower Ashgill of Upper Ordovician. As the Devonian supersequence in range of ca. 48 Ma, CQ4 can be broadly recognized in the Coqen basin, which is composed of transgrassive and regreassive sets. Thinned marlstone with the mixture of shale, siltstone, and sandstone and benthos associated with planktons comprises the former, and the later is of property of shallow sea dolomitized and crystalline limestone. This supersequence is separated the CQ 3 away by terrigenous sediment at the base of Devonian. CQ 5 is limited in Lower Carboniferous with an interval of ca. 33 Ma. It starts by the wormkalk at the bottom of Carboniferous and continues by bioclastic and intraclastic limestone, for which the transgrassive and regreassive depositional sets are vague to distinguish. CQ 6 ranges from upper Lower Carboniferous to lower Lower Permian with a total age of ca. 55 Ma. It is characterized by glaciomarine shale with lens of limestone and cool fauna fossils, and the boundary between CQ 6 and CQ 5 is located at the sharp contact of terrigenous rocks onto carbonate rocks. CQ 7 is the latest supersequence in Paleozoic, which has duration of age time ca. 30 Ma in most of Permian. The transgressive depositional sequence set is similar as the set in the CQ 6 and became the shallower carbonate sediments of regressive set. CQ 8 and CQ 7 are separated by disconformable and erosional surface at the base of the Triassic Quehala group. The age range of the supersequence is estimated 37 Ma. The transgressive set is not exposed, and the regression is consitituent of terrigenous turbidite of inner fan with little volcanic and carbonate rock. There is a nonconformity contact between the CQ 9 and CQ 8, above which the transgressive depositional sequence set is superposed by flysch middle and outer turbidite fan, and follows by changeable and complicated system sediment. It is ranges ca. 63 Ma and is separated over CQ 10 away by a regional unconformity. Supersequence CQ 10 is composed of kinds of limestone and clastic rocks in shallow sea environment deposited in Lower Cretaceous (50 Ma). The transgressive set is combined by hybrid sediments of shallow and volcanic rock, and the regressive by predominant carbonate rocks. The Upper Cretaceous supersequence CQ 11 is the only one superposed by much continental delta and shore facies. In general, the T-R sets are not readily differentiated either in filed or in room. Of them, three supersequencesCQ ₁_～₃ are classified in Early Paleozoic; four CQ ₄_～₇ and four CQ ₈_～₁₁ are in Late Paleozoic and Mesozoic respectively. The sedimentation, age range, number, and T-R texture of the super sequences CQ ₁_～₃ are similar, but different are in the CQ ₄_～₇ and CQ ₈_～₁₁ of Upper Paleozoic and Mesozoic. We suppose that the turnover of supersequence from Early to Late Paleozoic could be caused by the changes of tectonic and types of sedimentary basin, but not by second-order sea-level change, because there should be a same / similar sedimentary response to eustatic change for sedimentary basins

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Recognition and Correlation of Supersequences in Lhasa Block, Southern Tibet

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