Discovery of Hyperpycnal Flow Deposits in the Late Triassic Lacustrine Ordos Basin

YANG RenChao; JIN ZhiJun; SUN DongSheng; FAN AiPing

doi:10.14027/j.cnki.cjxb.2015.01.002

Volume 33 Issue 1

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YANG RenChao, JIN ZhiJun, SUN DongSheng, FAN AiPing. Discovery of Hyperpycnal Flow Deposits in the Late Triassic Lacustrine Ordos Basin[J]. Acta Sedimentologica Sinica, 2015, 33(1): 10-20. doi: 10.14027/j.cnki.cjxb.2015.01.002

Citation:

YANG RenChao, JIN ZhiJun, SUN DongSheng, FAN AiPing. Discovery of Hyperpycnal Flow Deposits in the Late Triassic Lacustrine Ordos Basin[J]. Acta Sedimentologica Sinica, 2015, 33(1): 10-20. doi: 10.14027/j.cnki.cjxb.2015.01.002

Discovery of Hyperpycnal Flow Deposits in the Late Triassic Lacustrine Ordos Basin

doi: 10.14027/j.cnki.cjxb.2015.01.002

1.
Shandong Provincial Key Laboratay of Depositional Mineralization & Sedimentary Minerals, College of Earth Science and Engineering, Shandong University of Science and Technology, Qingdao, Shandong 266590;
2.
Petroleum Exploration and Production Research Institute, SINOPEC, Beijing 100083

Received Date: 2013-11-08
Rev Recd Date: 2014-04-15
Publish Date: 2015-02-10

Abstract

As a major focus of both academic and industrial circles, deep-water sandy sedimentation is not only a record of gravity flows transporting a great deal of continental sediments into basin, but also important reservoir of oil and gas with great economic value. Subaqueous sediment density flows are one of the most important processes for moving sediments from provenance to depositional basins, but people still know little about these subaqueous gravity flows such as slump, sandy debris flow, muddy debris flow, granular flow, fluidized flow, turbidite current, and so on. What is more, they are extremely difficult to monitor directly. A new kind of gravity flow sandstone deposits diferent to sandy debris flow and slumping turbidity current was discovered in the sixth and seventh member of Yanchang Formation (for short, YC6 and YC7 members) in the southern part of the deep lacustrine Ordos Basin. Characteristics of the gravity flow deposits dominated by: ① a series of upward coarsening interval (inverse grading) and upward fining interval (normal grading) always exist in pairs; ② changes of relative high clay content (high-low-high) consistent with that of granularity (fine-coarse-fine) in each size-graded couplet; ③ inner micro-erosion surface sometimes separated a couplet of an upper, upward fining interval and a lower, upward-coarsening interval; ④ sandstone interbedded with dark mudstone and grey siltstone; and ⑤ granularity changes in silty mudstone is similar to that of sandstone. It was considered as flood-generated hyperpycnal flow deposit in the late Triassic deep lacustrine Ordos Basin, based on drill core observation and slice identification. A hyperpycnal flow is a kind of sustainable turbidity current occurring at a flooding river mouth when the concentration of suspended sediment is so large that the density of the river water is greater than that of lake (sea) water. It is turbid river plume that can plunge to form turbidity current where it enters a water body with lesser density and flow at basin floor. Associated with high-suspended concentration, hyperpycnal flow can transport considerable volume of sediment to lacustrine basins. Mapping of individual flow deposits (beds) emphasizes how a single event can contain several flow types, with transformations between flow types. Flow transformation may be from dilute to dense flow, as well as from dense to dilute flow. Turbid river flow must move through transfer belt of a backwater zone, depth-limited plume, and plunging zone before becoming a turbidity current. The transfer belt can extend tens of kilometers offshore and significantly affect the transfer of momentum from river to turbidity current. Sedimentary architecture of deep lacustrine gravity flows in the southern part of the late Triassic Ordos bain consist of sandy debris flow deposits, turbidites and hyperpycnites, interbedded with fine-grained deposits (thin turbidites, hyperpycnites, and deep lacustrine mudstones). Sand and mud rich turbidite systems fed by mountainous “dirty” rivers and slumps at deep angle deltas front. Storm-influenced, hyperpycnal flows generated subaqueous channelized forms at the mouth of the river deltas, which later filled with sand. The typical deposit of hyperpycnal flow in the YC6 and YC7 members in the southern part of the deep lacustrine Ordos Basin is a compound of a basal coarsening-up unit, deposited during the waxing period of discharge, and a top fining-up unit formed during the waning period of discharge. Hyperpycnites differ from other turbidites because of their well-developed inversely graded intervals and intrasequence erosional contacts. Deposits of hyperpycnal flow, hyperpycnite is different to others turbidite as for well developed upward-coarsening interval and inner micro-erosion surface in size-graded couplets. The lower, upward-coarsening interval represents deposition of waxing hyperpycnal flow. The upper, upward-fining interval was generated from waning hyperpycnal flow. The two parts of the size-graded couplet of upward-coarsening interval and upward-fining interval in pairs represent a cycle of event sedimentary of flood-generated hyperpycnal flow. The micro-erosion surface that sometimes divides the two parts of the size-graded couplet resulted from waxing flows of sufficiently high velocity to erode the sediment previously deposited by the same flow. Some bed forms and sediment grading patterns in hyperpycnal- flow deposits can record multiple flow accelerations and decelerations even during a simple single-peaked flood. Because hyperpycnal flow provides one of the most direct connections between terrestrial sediment sources and lacustrine depositional basin, its deposits might preserve an important record across a variety of climatic and tectonic settings. Depositional processes in the late Triassic deep lacustrine in the studied area were dominated by sediment gravity flows originating from gravity induced slumps and mountainous “dirty” river discharged hyperpycnal flow. Gravity flows deposits in the YC6 and YC7 members in the southern part of the deep lacustrine Ordos Basin appear to be primarily controlled by the strong climatic and tectonic forcing parameters. The basin also must be deep enough, in some cases greater than tens of meters, in order for the plume to collapse and form a turbidity current. All in all, controlling factors of hyperpycnal flow include seasonal flood river, deep angle depositional slope, enough water depth and large density difference between basinal water mass and discharged flood river. The discovery of hyperpycnite in Yanchang Formation in the Ordos Basin can not only provide an example to probe hyperpycnal flow deposits in continental lacustrine environment, but also has theoretical and realistic significances to study on genesis of deep water sandbodies, to reservoir forecasting and oil-gas exploration.
- hyperpycnal flow,
- hyperpycnite,
- gravity flow deposits,
- Ordos Basin,
- Yanchang Formation

References

[1]	Etienne S, Mulder T, Bez M, et al. Multiple scale characterization of sand-rich distal lobe deposit variability: Examples from the Annot Sandstones Formation, Eocene-Oligocene, SE France [J]. Sedimentary Geology, 2012, 273-274: 1-18.
[2]	Valle G D, Gamberi F. Erosional sculpting of the Caprera confined deep-sea fan as a result of distal basin-spilling processes (eastern Sardinian margin, Tyrrhenian Sea) [J]. Marine Geology, 2010, 268(1/2/3/4): 55-66.
[3]	Di Celma C. Sedimentology, architecture, and depositional evolution of a coarse-grained submarine canyon fill from the Gelasian (early Pleistocene) of the Peri-Adriatic basin, Offida, central Italy [J]. Sedimentary Geology, 2011, 238(3/4): 233-253.
[4]	Talling P J, Masson D G, Sumner E J, et al. Subaqueous sediment density flows: depositional processes and deposit types [J]. Sedimentology, 2012, 59(7): 1937-2003.
[5]	何起祥. 沉积动力学若干问题的讨论[J]. 海洋地质与第四纪地质,2010,30(4):1-10.[He Qixiang. A discussion on sediment dynamics[J]. Marine Geology & Quaternary Geology, 2010, 30(4): 1-10.]
[6]	Shanmugam G. High-density turbidity currents:are they sandy debris flows?[J]. Journal of Sedimentary Research, 1996, 66(1): 2-10.
[7]	Mulder T, Syvitski J P M. Turbidity currents generated at river mouths during exceptional discharges to the world oceans[J].The Journal of Geology, 1995, 103(3): 285-299.
[8]	Mulder T, Migeon S, Savoye B, et al.Inversely graded turbidite sequences in the deep Mediterranean: A record of deposits from flood-generated turbidity currents? [J]. Geo-Marine Letters, 2001, 21(2): 86-93.
[9]	Yoshida M, Yoshiuchi Y, Hoyanagi K. Occurrence conditions of hyperpycnal flows, and their significance for organic-matter sedimentation in a Holocene estuary, Niigata Plain, Central Japan [J]. Island Arc, 2009,18(2): 320-332.
[10]	Bourget J, Zaragosi S, Mulder T, et al. Hyperpycnal-fed turbidite lobe architecture and recent sedimentary processes: A case study from the Al Batha turbidite system, Oman margin [J]. Sedimentary Geology, 2010, 229(3): 144-159.
[11]	Bates C C. Rational theory of delta formation [J]. AAPG Bulletin, 1953, 37(9): 2119-2162.
[12]	Shanmugam G. Discussion on Mulder et al. (2001, Geo-Marine Letters 21: 86-93)Inversely graded turbidite sequences in the deep Mediterranean. A record of deposits from flood-generated turbidity currents? [J]. Geo-Marine Letters, 2002, 22(2): 108-111.
[13]	Mulder T, Syvitski J P M, Migeon S, et al. Marine hyperpycnal flows: initiation, behavior and related deposits. A review[J]. Marine & Petroleum Geology, 2003, 20(6/7/8): 861-882.
[14]	Khripounoff A, Vangriesheim A, Crassous P, et al. High frequency of sediment gravity flow events in the Var submarine canyon (Mediterranean Sea) [J]. Marine Geology, 2009, 263(1/2/3/4): 1-6.
[15]	McConnico T S, Bassett K N. Gravelly Gilbert-type fan delta on the Conway Coast, New Zealand: Foreset depositional processes and clast imbrications [J]. Sedimentary Geology, 2007, 198(3/4): 147-166.
[16]	Migeon S, Mulder T, Savoye B, et al. Hydrodynamic processes, velocity structure and stratification in natural turbidity currents: Results inferred from field data in the Var Turbidite System [J]. Sedimentary Geology, 2012, 245-246: 48-62.
[17]	Zavala C, Ponce J J, Arcuri M, et al. Ancient lacustrine hyperpycnites: a depositional model from a case study in the Rayoso Formation (Cretaceous) of west-central Argentina [J]. Journal of Sedimentary Research, 2006, 76(1): 41-59.
[18]	Mulder T, Zaragosi S, Jouanneau J M, et al. Deposits related to the failure of the Malpasset Dam in 1959: An analogue for hyperpycnal deposits from jökulhlaups [J]. Marine Geology, 2009, 260(1/2/3/4): 81-89.
[19]	Shirai M, Omura A, Wakabayashi T, et al. Depositional age and triggering event of turbidites in the western Kumano Trough, central Japan during the last ca. 100 years [J]. Marine Geology, 2010, 271(3/4): 225-235.
[20]	St-Onge G, Chapron E, Mulsow S, et al. Comparison of earthquake-triggered turbidites from the Saguenay (Eastern Canada) and Reloncavi (Chilean margin) Fjords: Implications for paleoseismicity and sedimentology[J]. Sedimentary Geology, 2012, 243-244: 89-107.
[21]	余斌. 泥石流异重流入海的研究[J]. 沉积学报,2002,20(3):382-386. [Yu Bin. Research on debris flow into the sea as a density flow[J]. Acta Sedimentologica Sinica, 2002, 20(3): 382-386.]
[22]	Addington L D, Kuehl S A, McNinch J E. Contrasting modes of shelf sediment dispersal off a high-yield river:Waiapu River, New Zealand [J]. Marine Geology, 2007, 243(1/2/3/4): 18-30.
[23]	Soyinka O A, Slatt R M. Identification and micro-stratigraphy of hyperpycnites and turbidites in Cretaceous Lewis Shale,Wyoming[J]. Sedimentology, 2008, 55(5): 1117-1133.
[24]	Mutti E, Bernoulli D, Ricci L F, et al. Turbidites and turbidity currents from Alpine 'flysch' to the exploration of continental margins[J]. Sedimentology, 2009, 56(1): 267-318.
[25]	Lamb M P, Mohrig D. Do hyperpycnal-flow deposits record river-flood dynamics? [J]. Geology, 2009, 37(12): 1067-1070.
[26]	Dadson S J, Hovius N, Chen H, et al. Earthquake-triggered increase in sediment delivery from an active mountain belt [J]. Geology, 2004, 32(8): 733-736.
[27]	Milliman J D, Kao S J. Hyperpycnal discharge of fluvial sediment to the ocean: impact of super-typhoon Herb (1996) on Taiwanese Rivers [J].The Journal of Geology, 2005, 113(5): 503-516.
[28]	Johnson K S, Paull C K, Barry J P. A decal record of underflows from a coastal river into the deep sea[J]. Geology, 2001, 29(11): 1019-1022.
[29]	Shanmugam G. 50 years of the turbidite paradigm(1950-1990 s):deep-water processes and facies models-a critical perspective[J].Marine and Petroleum Geology, 2000, 17(2): 285-342.
[30]	Sáez A, Anadón P, Herrero M J, et al. Variable style of transition between Palaeogene fluvial fan and lacustrine systems, southern Pyrenean foreland, NE Spain [J]. Sedimentology, 2007, 54(2): 367-390.
[31]	Pouderoux H, Proust J N, Lamarche G, et al. Postglacial (after 18ka) deep-sea sedimentation along the Hikurangi subduction margin (New Zealand): Characterisation, timing and origin of turbidites [J]. Marine Geology, 2012, 295-298: 51-76.
[32]	Eilertsen R S, Corner G D, Aasheim O, et al. Facies characteristics and architecture related to palaeodepth of Holocene fjord-delta sediments [J]. Sedimentology, 2011, 58(7): 1784-1809.
[33]	Ça?atay M N, Erel L, Bellucci L G, et al. Sedimentary earthquake records in the īzmit Gulf, Sea of Marmara, Turkey [J]. Sedimentary Geology, 2012, 282: 347-359.
[34]	McHugh C M, Seeber L, Braudy N, et al. Offshore sedimentary effects of the 12 January 2010 Haiti earthquake [J]. Geology, 2011, 39(8): 723-724.
[35]	Eri? K K, Ça?atay N, Beck C, et al. Late-Pleistocene to Holocene sedimentary fills of the Çinarcik Basin of the Sea of Marmara [J]. Sedimentary Geology, 2012, 281: 151-165.
[36]	You Y, Flemings P, Mohrig D. Dynamics of dilative slope failure [J]. Geology, 2012, 40(7): 663-666.
[37]	JacksonC A L, Johnson H D. Sustained turbidity currents and their interaction with debrite-related topography:Labuan Island, offshore NW Borneo, Malaysia [J]. Sedimentary Geology, 2009, 219(1/2/3/4): 77-96.
[38]	Talling P J, Wynn R B, Masson D G, et al. Onset of submarine debris flow deposition far from original giant landslide[J]. Nature, 2007, 450(7169): 541-544.
[39]	Haughton P D W, Davis C, McCaffrey W, et al. Hybrid sediment gravity flow deposits -classification, origin and significance[J]. Marine and Petroleum Geology, 2009, 26(10): 1900-1918.
[40]	Sumner E J, Talling P J, Amy L A, et al. Facies architecture of individual basin-plain turbidites: Comparison with existing models and implications for flow processes[J]. Sedimentology, 2012, 59(6): 1850- 1887.
[41]	李文厚,邵磊,魏红红,等. 西北地区湖相浊流沉积[J]. 西北大学学报:自然科学版,2001,31(1):57-62.[Li Wenhou, Shao Lei, Wei Honghong, et al. Turbidity current deposits of lake facies in northwestern China[J]. Journal of Northwest University: Natural Science Edition, 2001, 31(1): 57-62. ]
[42]	王起琮,李文厚,赵虹,等. 鄂尔多斯盆地东南部三叠系延长组一段湖相浊积岩特征及意义[J]. 地质科学,2006,41(1):54-63.[Wang Qizong, Li Wenhou, Zhao Hong, et al. Characteristics and significance of lacustrine turbidites in the member 1 of Yanchang Formation, Upper Triassic in the southeastern Ordos Basin [J]. Chinese Journal of Geology, 2006, 41(1): 54-63.]
[43]	郑荣才,文华国,韩永林,等. 鄂尔多斯盆地白豹地区长6油层组湖底滑塌浊积扇沉积特征及其研究意义[J]. 成都理工大学学报:自然科学版,2006,33(6):566-575.[Zheng Rongcai, Wen Huaguo, Han Yonglin, et al. Discovery and significance of sublacustrine slump turbidite fans in Chang 6 oil-bearing formation of Baibao region in Ordos Basin, China [J]. Journal of Chengdu University of Technology: Science & Technology Edition, 2006, 33(6): 566-575.]
[44]	傅强,吕苗苗,刘永斗. 鄂尔多斯盆地晚三叠世湖盆浊积岩发育特征及地质意义[J]. 沉积学报,2008,26(2):186-192.[Fu Qiang, Lü Miaomiao, Liu Yongdou. Developmental characteristics of Turbidite and its implication on petroleum geology in Late-Triassic Ordos Basin [J]. Acta Sedimentologica Sinica, 2008, 26(2): 186-192.]
[45]	夏青松,田景春. 鄂尔多斯盆地西南部上三叠统长6油层组湖底扇特征[J]. 古地理学报,2007,9(1):33-43.[Xia Qingsong, Tian Jingchun. Sedimentary characteristics of sublacustrine fan of the Interval 6 of Yanchang Formation of Upper Triassic in southwestern Ordos Basin [J]. Journal of Palaeogeography, 2007, 9(1): 33-43.]
[46]	Chen Quanhong, Li Wenhou, Gao Yongxiang, et al. The deep-lake deposit in the Upper Triassic Yanchang Formation in Ordos Basin, China and its significance for oil-gas accumulation[J]. Science China: Earth Sciences,2007, 50(S2): 47-58.
[47]	邹才能,赵文智,张兴阳,等. 大型敞流坳陷湖盆浅水三角洲与湖盆中心砂体的形成与分布[J]. 地质学报,2008,82(6):815-825.[Zou Caineng, Zhao Wenzhi, Zhang Xingyang, et al. Formation and distribution of shallow-water deltas and central-basin sandbodies in large open depression lake basins [J]. Acta Geologica Sinica, 2008, 82(6): 815-825.]
[48]	邹才能,赵政璋,杨华,等. 陆相湖盆深水砂质碎屑流成因机制与分布特征——以鄂尔多斯盆地为例[J]. 沉积学报,2009,27(6):1065-1075.[Zou Caineng, Zhao Zhengzhang, Yang Hua, et al. Genetic mechanism and distribution of sandy debris flows in terrestrial lacustrine basin [J]. Acta Sedimentologica Sinica, 2009, 27(6): 1065-1075.]
[49]	李相博,付金华,陈启林,等. 砂质碎屑流概念及其在鄂尔多斯盆地延长组深水沉积研究中的应用[J]. 地球科学进展,2011,26(3):286-294.[Li Xiangbo, Fu Jinhua, Chen Qilin, et al. The concept of sandy debris flow and its application in the Yanchang Formation deep water sedimentation of the Ordos Basin [J]. Advances in Earth Science, 2011, 26(3): 286-294.]
[50]	李相博,刘化清,完颜容,等. 鄂尔多斯盆地三叠系延长组砂质碎屑流储集体的首次发现[J]. 岩性油气藏,2009,21(4):19-21.[Li Xiangbo, Liu Huaqing, Wanyan Rong, et al. First discovery of the sandy debris flow from the Triassic Yanchang Formation, Ordos Basin [J]. Lithologic Reservoirs, 2009, 21(4):19-21.]
[51]	付锁堂,邓秀芹,庞锦莲. 晚三叠世鄂尔多斯盆地湖盆沉积中心厚层砂体特征及形成机制分析[J]. 沉积学报,2010,28(6):1081-1089.[Fu Suotang, Deng Xiuqin, Pang Jinlian. Characteristics and mechanism of thick sandbody of Yanchang Formation at the centre of Ordos Basin[J]. Acta Sedimentologica Sinica, 2010, 26(6): 1081-1089.]
[52]	刘池洋,赵红格,桂小军,等. 鄂尔多斯盆地演化—改造的时空坐标及其成藏(矿)响应[J]. 地质学报,2006,80(5):617-638.[Liu Chiyang, Zhao Hongge, Gui Xiaojun, et al. Space-time coordinate of the evolution and reformation and mineralization response in Ordos Basin [J]. Acta Geologica Sinica, 2006, 80(5): 617-638.]
[53]	付国民,赵俊兴,张志升,等. 鄂尔多斯盆地东南缘三叠系延长组物源及沉积体系特征[J]. 矿物岩石,2010,30(1):99-105. [Fu Guomin, Zhao Junxing, Zhang Zhisheng, et al. The provenance and features of depositional system in the Yanchang Formation of Triassic in southeast area of Ordos Basin[J]. Journal of Mineralogy and Petrology, 2010, 30(1): 99-105.]
[54]	李涛,谈广鸣,张俊华,等. 水库异重流研究进展[J]. 中国农村水利水电,2006(9):21-24.[Li Tao, Tan Guangming, Zhang Junhua, et al. Research advances in reservoir hyperpycnal flow [J].China Rural Water and Hydropower, 2006(9): 21-24.]J]. 成都理工大学学报: 自然科学版,2006,33(6): 566-575.[Zheng Rongcai, Wen Huaguo, Han Yonglin, et al. Discovery and significance of sublacustrine slump turbidite fans in Chang 6 oil-bearing formation of Baibao region in Ordos Basin, China [J]. Journal of Chengdu University of Technology: Science & Technology Edition, 2006, 33(6): 566-575.]
[55]	傅强,吕苗苗,刘永斗. 鄂尔多斯盆地晚三叠世湖盆浊积岩发育特征及地质意义[J]. 沉积学报,2008,26(2): 186-192.[Fu Qiang, Lü Miaomiao, Liu Yongdou. Developmental characteristics of Turbidite and its implication on petroleum geology in late-Triassic Ordos Basin [J]. Acta Sedimentologica Sinica, 2008, 26(2): 186-192.]
[56]	夏青松,田景春. 鄂尔多斯盆地西南部上三叠统长6油层组湖底扇特征[J]. 古地理学报,2007,9(1): 33-43.[Xia Qingsong, Tian Jingchun. Sedimentary characteristics of sublacustrine fan of the Interval 6 of Yanchang Formation of Upper Triassic in southwestern Ordos Basin [J]. Journal of Palaeogeography, 2007, 9(1): 33-43.]
[57]	Chen Quanhong, Li Wenhou, Gao Yongxiang, et al. The deep-lake deposit in the Upper Triassic Yanchang Formation in Ordos Basin, China and its significance for oil-gas accumulation[J]. Science China: Earth Sciences,2007, 50(S2): 47-58.
[58]	邹才能,赵文智,张兴阳,等. 大型敞流坳陷湖盆浅水三角洲与湖盆中心砂体的形成与分布[J]. 地质学报,2008,82(6): 815-825.[Zou Caineng, Zhao Wenzhi, Zhang Xingyang, et al. Formation and distribution of shallow-water deltas and central-basin sandbodies in large open depression lake basins [J]. Acta Geologica Sinica, 2008, 82(6): 815-825.]
[59]	邹才能,赵政璋,杨华,等. 陆相湖盆深水砂质碎屑流成因机制与分布特征——以鄂尔多斯盆地为例[J]. 沉积学报,2009,27(6): 1067-1074.[Zou Caineng, Zhao Zhengzhang, Yang Hua, et al. Genetic mechanism and distribution of sandy debris flows in terrestrial lacustrine basin [J]. Acta Sedimentologica Sinica, 2009, 27(6): 1065-1076.]
[60]	李相博,付金华,陈启林,等. 砂质碎屑流概念及其在鄂尔多斯盆地延长组深水沉积研究中的应用[J]. 地球科学进展,2011,26(3): 286-294.[Li Xiangbo, Fu Jinhua, Chen Qilin, et al. The concept of sandy debris flow and its application in the Yanchang Formation deep water sedimentation of the Ordos Basin [J]. Advances in Earth Science, 2011, 26(3): 286-294.]
[61]	李相博,刘化清,完颜容,等. 鄂尔多斯盆地三叠系延长组砂质碎屑流储集体的首次发现[J]. 岩性油气藏,2009,21(4): 19-21.[Li Xiangbo, Liu Huaqing, Wanyan Rong, et al. First discovery of the sandy debris flow from the Triassic Yanchang Formation, Ordos Basin [J]. Lithologic Reservoirs, 2009, 21(4):19-21.]
[62]	付锁堂,邓秀芹,庞锦莲. 晚三叠世鄂尔多斯盆地湖盆沉积中心厚层砂体特征及形成机制分析[J]. 沉积学报,2010,28(6): 1081-1089.[Fu Suotang, Deng Xiuqin, Pang Jinlian. Characteristics and mechanism of thick sandbody of Yanchang Formation at the centre of Ordos Basin[J]. Acta Sedimentologica Sinica, 2010, 26(6): 1081-1089.]
[63]	刘池洋,赵红格,桂小军,等. 鄂尔多斯盆地演化—改造的时空坐标及其成藏(矿)响应[J]. 地质学报,2006,80(5): 617-638.[Liu Chiyang, Zhao Hongge, Gui Xiaojun, et al. Space-time coordinate of the evolution and reformation and mineralization response in Ordos Basin [J]. Acta Geologica Sinica, 2006, 80(5): 617-638.]
[64]	付国民,赵俊兴,张志升,等. 鄂尔多斯盆地东南缘三叠系延长组物源及沉积体系特征[J]. 矿物岩石,2010,30(1): 99-105. [Fu Guomin, Zhao Junxing, Zhang Zhisheng, et al. The provenance and features of depositional system in the Yanchang Formation of Triassic in southeast area of Ordos Basin[J]. Journal of Mineralogy and Petrology, 2010, 30(1): 99-105.]
[65]	李涛,谈广鸣,张俊华,等. 水库异重流研究进展[J]. 中国农村水利水电,2006(9): 21-24.[Li Tao, Tan Guangming, Zhang Junhua, et al. Research advances in reservoir hyperpycnal flow [J].China Rural Water and Hydropower, 2006(9): 21-24.]

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Discovery of Hyperpycnal Flow Deposits in the Late Triassic Lacustrine Ordos Basin

1. Shandong Provincial Key Laboratay of Depositional Mineralization & Sedimentary Minerals, College of Earth Science and Engineering, Shandong University of Science and Technology, Qingdao, Shandong 266590;

2. Petroleum Exploration and Production Research Institute, SINOPEC, Beijing 100083

Received Date: 2013-11-08

Rev Recd Date: 2014-04-15

Publish Date: 2015-02-10

Key words:

Abstract: As a major focus of both academic and industrial circles, deep-water sandy sedimentation is not only a record of gravity flows transporting a great deal of continental sediments into basin, but also important reservoir of oil and gas with great economic value. Subaqueous sediment density flows are one of the most important processes for moving sediments from provenance to depositional basins, but people still know little about these subaqueous gravity flows such as slump, sandy debris flow, muddy debris flow, granular flow, fluidized flow, turbidite current, and so on. What is more, they are extremely difficult to monitor directly. A new kind of gravity flow sandstone deposits diferent to sandy debris flow and slumping turbidity current was discovered in the sixth and seventh member of Yanchang Formation (for short, YC6 and YC7 members) in the southern part of the deep lacustrine Ordos Basin. Characteristics of the gravity flow deposits dominated by: ① a series of upward coarsening interval (inverse grading) and upward fining interval (normal grading) always exist in pairs; ② changes of relative high clay content (high-low-high) consistent with that of granularity (fine-coarse-fine) in each size-graded couplet; ③ inner micro-erosion surface sometimes separated a couplet of an upper, upward fining interval and a lower, upward-coarsening interval; ④ sandstone interbedded with dark mudstone and grey siltstone; and ⑤ granularity changes in silty mudstone is similar to that of sandstone. It was considered as flood-generated hyperpycnal flow deposit in the late Triassic deep lacustrine Ordos Basin, based on drill core observation and slice identification. A hyperpycnal flow is a kind of sustainable turbidity current occurring at a flooding river mouth when the concentration of suspended sediment is so large that the density of the river water is greater than that of lake (sea) water. It is turbid river plume that can plunge to form turbidity current where it enters a water body with lesser density and flow at basin floor. Associated with high-suspended concentration, hyperpycnal flow can transport considerable volume of sediment to lacustrine basins. Mapping of individual flow deposits (beds) emphasizes how a single event can contain several flow types, with transformations between flow types. Flow transformation may be from dilute to dense flow, as well as from dense to dilute flow. Turbid river flow must move through transfer belt of a backwater zone, depth-limited plume, and plunging zone before becoming a turbidity current. The transfer belt can extend tens of kilometers offshore and significantly affect the transfer of momentum from river to turbidity current. Sedimentary architecture of deep lacustrine gravity flows in the southern part of the late Triassic Ordos bain consist of sandy debris flow deposits, turbidites and hyperpycnites, interbedded with fine-grained deposits (thin turbidites, hyperpycnites, and deep lacustrine mudstones). Sand and mud rich turbidite systems fed by mountainous “dirty” rivers and slumps at deep angle deltas front. Storm-influenced, hyperpycnal flows generated subaqueous channelized forms at the mouth of the river deltas, which later filled with sand. The typical deposit of hyperpycnal flow in the YC6 and YC7 members in the southern part of the deep lacustrine Ordos Basin is a compound of a basal coarsening-up unit, deposited during the waxing period of discharge, and a top fining-up unit formed during the waning period of discharge. Hyperpycnites differ from other turbidites because of their well-developed inversely graded intervals and intrasequence erosional contacts. Deposits of hyperpycnal flow, hyperpycnite is different to others turbidite as for well developed upward-coarsening interval and inner micro-erosion surface in size-graded couplets. The lower, upward-coarsening interval represents deposition of waxing hyperpycnal flow. The upper, upward-fining interval was generated from waning hyperpycnal flow. The two parts of the size-graded couplet of upward-coarsening interval and upward-fining interval in pairs represent a cycle of event sedimentary of flood-generated hyperpycnal flow. The micro-erosion surface that sometimes divides the two parts of the size-graded couplet resulted from waxing flows of sufficiently high velocity to erode the sediment previously deposited by the same flow. Some bed forms and sediment grading patterns in hyperpycnal- flow deposits can record multiple flow accelerations and decelerations even during a simple single-peaked flood. Because hyperpycnal flow provides one of the most direct connections between terrestrial sediment sources and lacustrine depositional basin, its deposits might preserve an important record across a variety of climatic and tectonic settings. Depositional processes in the late Triassic deep lacustrine in the studied area were dominated by sediment gravity flows originating from gravity induced slumps and mountainous “dirty” river discharged hyperpycnal flow. Gravity flows deposits in the YC6 and YC7 members in the southern part of the deep lacustrine Ordos Basin appear to be primarily controlled by the strong climatic and tectonic forcing parameters. The basin also must be deep enough, in some cases greater than tens of meters, in order for the plume to collapse and form a turbidity current. All in all, controlling factors of hyperpycnal flow include seasonal flood river, deep angle depositional slope, enough water depth and large density difference between basinal water mass and discharged flood river. The discovery of hyperpycnite in Yanchang Formation in the Ordos Basin can not only provide an example to probe hyperpycnal flow deposits in continental lacustrine environment, but also has theoretical and realistic significances to study on genesis of deep water sandbodies, to reservoir forecasting and oil-gas exploration.

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[1]	Etienne S, Mulder T, Bez M, et al. Multiple scale characterization of sand-rich distal lobe deposit variability: Examples from the Annot Sandstones Formation, Eocene-Oligocene, SE France [J]. Sedimentary Geology, 2012, 273-274: 1-18.
[2]	Valle G D, Gamberi F. Erosional sculpting of the Caprera confined deep-sea fan as a result of distal basin-spilling processes (eastern Sardinian margin, Tyrrhenian Sea) [J]. Marine Geology, 2010, 268(1/2/3/4): 55-66.
[3]	Di Celma C. Sedimentology, architecture, and depositional evolution of a coarse-grained submarine canyon fill from the Gelasian (early Pleistocene) of the Peri-Adriatic basin, Offida, central Italy [J]. Sedimentary Geology, 2011, 238(3/4): 233-253.
[4]	Talling P J, Masson D G, Sumner E J, et al. Subaqueous sediment density flows: depositional processes and deposit types [J]. Sedimentology, 2012, 59(7): 1937-2003.
[5]	何起祥. 沉积动力学若干问题的讨论[J]. 海洋地质与第四纪地质,2010,30(4):1-10.[He Qixiang. A discussion on sediment dynamics[J]. Marine Geology & Quaternary Geology, 2010, 30(4): 1-10.]
[6]	Shanmugam G. High-density turbidity currents:are they sandy debris flows?[J]. Journal of Sedimentary Research, 1996, 66(1): 2-10.
[7]	Mulder T, Syvitski J P M. Turbidity currents generated at river mouths during exceptional discharges to the world oceans[J].The Journal of Geology, 1995, 103(3): 285-299.
[8]	Mulder T, Migeon S, Savoye B, et al.Inversely graded turbidite sequences in the deep Mediterranean: A record of deposits from flood-generated turbidity currents? [J]. Geo-Marine Letters, 2001, 21(2): 86-93.
[9]	Yoshida M, Yoshiuchi Y, Hoyanagi K. Occurrence conditions of hyperpycnal flows, and their significance for organic-matter sedimentation in a Holocene estuary, Niigata Plain, Central Japan [J]. Island Arc, 2009,18(2): 320-332.
[10]	Bourget J, Zaragosi S, Mulder T, et al. Hyperpycnal-fed turbidite lobe architecture and recent sedimentary processes: A case study from the Al Batha turbidite system, Oman margin [J]. Sedimentary Geology, 2010, 229(3): 144-159.
[11]	Bates C C. Rational theory of delta formation [J]. AAPG Bulletin, 1953, 37(9): 2119-2162.
[12]	Shanmugam G. Discussion on Mulder et al. (2001, Geo-Marine Letters 21: 86-93)Inversely graded turbidite sequences in the deep Mediterranean. A record of deposits from flood-generated turbidity currents? [J]. Geo-Marine Letters, 2002, 22(2): 108-111.
[13]	Mulder T, Syvitski J P M, Migeon S, et al. Marine hyperpycnal flows: initiation, behavior and related deposits. A review[J]. Marine & Petroleum Geology, 2003, 20(6/7/8): 861-882.
[14]	Khripounoff A, Vangriesheim A, Crassous P, et al. High frequency of sediment gravity flow events in the Var submarine canyon (Mediterranean Sea) [J]. Marine Geology, 2009, 263(1/2/3/4): 1-6.
[15]	McConnico T S, Bassett K N. Gravelly Gilbert-type fan delta on the Conway Coast, New Zealand: Foreset depositional processes and clast imbrications [J]. Sedimentary Geology, 2007, 198(3/4): 147-166.
[16]	Migeon S, Mulder T, Savoye B, et al. Hydrodynamic processes, velocity structure and stratification in natural turbidity currents: Results inferred from field data in the Var Turbidite System [J]. Sedimentary Geology, 2012, 245-246: 48-62.
[17]	Zavala C, Ponce J J, Arcuri M, et al. Ancient lacustrine hyperpycnites: a depositional model from a case study in the Rayoso Formation (Cretaceous) of west-central Argentina [J]. Journal of Sedimentary Research, 2006, 76(1): 41-59.
[18]	Mulder T, Zaragosi S, Jouanneau J M, et al. Deposits related to the failure of the Malpasset Dam in 1959: An analogue for hyperpycnal deposits from jökulhlaups [J]. Marine Geology, 2009, 260(1/2/3/4): 81-89.
[19]	Shirai M, Omura A, Wakabayashi T, et al. Depositional age and triggering event of turbidites in the western Kumano Trough, central Japan during the last ca. 100 years [J]. Marine Geology, 2010, 271(3/4): 225-235.
[20]	St-Onge G, Chapron E, Mulsow S, et al. Comparison of earthquake-triggered turbidites from the Saguenay (Eastern Canada) and Reloncavi (Chilean margin) Fjords: Implications for paleoseismicity and sedimentology[J]. Sedimentary Geology, 2012, 243-244: 89-107.
[21]	余斌. 泥石流异重流入海的研究[J]. 沉积学报,2002,20(3):382-386. [Yu Bin. Research on debris flow into the sea as a density flow[J]. Acta Sedimentologica Sinica, 2002, 20(3): 382-386.]
[22]	Addington L D, Kuehl S A, McNinch J E. Contrasting modes of shelf sediment dispersal off a high-yield river:Waiapu River, New Zealand [J]. Marine Geology, 2007, 243(1/2/3/4): 18-30.
[23]	Soyinka O A, Slatt R M. Identification and micro-stratigraphy of hyperpycnites and turbidites in Cretaceous Lewis Shale,Wyoming[J]. Sedimentology, 2008, 55(5): 1117-1133.
[24]	Mutti E, Bernoulli D, Ricci L F, et al. Turbidites and turbidity currents from Alpine 'flysch' to the exploration of continental margins[J]. Sedimentology, 2009, 56(1): 267-318.
[25]	Lamb M P, Mohrig D. Do hyperpycnal-flow deposits record river-flood dynamics? [J]. Geology, 2009, 37(12): 1067-1070.
[26]	Dadson S J, Hovius N, Chen H, et al. Earthquake-triggered increase in sediment delivery from an active mountain belt [J]. Geology, 2004, 32(8): 733-736.
[27]	Milliman J D, Kao S J. Hyperpycnal discharge of fluvial sediment to the ocean: impact of super-typhoon Herb (1996) on Taiwanese Rivers [J].The Journal of Geology, 2005, 113(5): 503-516.
[28]	Johnson K S, Paull C K, Barry J P. A decal record of underflows from a coastal river into the deep sea[J]. Geology, 2001, 29(11): 1019-1022.
[29]	Shanmugam G. 50 years of the turbidite paradigm(1950-1990 s):deep-water processes and facies models-a critical perspective[J].Marine and Petroleum Geology, 2000, 17(2): 285-342.
[30]	Sáez A, Anadón P, Herrero M J, et al. Variable style of transition between Palaeogene fluvial fan and lacustrine systems, southern Pyrenean foreland, NE Spain [J]. Sedimentology, 2007, 54(2): 367-390.
[31]	Pouderoux H, Proust J N, Lamarche G, et al. Postglacial (after 18ka) deep-sea sedimentation along the Hikurangi subduction margin (New Zealand): Characterisation, timing and origin of turbidites [J]. Marine Geology, 2012, 295-298: 51-76.
[32]	Eilertsen R S, Corner G D, Aasheim O, et al. Facies characteristics and architecture related to palaeodepth of Holocene fjord-delta sediments [J]. Sedimentology, 2011, 58(7): 1784-1809.
[33]	Ça?atay M N, Erel L, Bellucci L G, et al. Sedimentary earthquake records in the īzmit Gulf, Sea of Marmara, Turkey [J]. Sedimentary Geology, 2012, 282: 347-359.
[34]	McHugh C M, Seeber L, Braudy N, et al. Offshore sedimentary effects of the 12 January 2010 Haiti earthquake [J]. Geology, 2011, 39(8): 723-724.
[35]	Eri? K K, Ça?atay N, Beck C, et al. Late-Pleistocene to Holocene sedimentary fills of the Çinarcik Basin of the Sea of Marmara [J]. Sedimentary Geology, 2012, 281: 151-165.
[36]	You Y, Flemings P, Mohrig D. Dynamics of dilative slope failure [J]. Geology, 2012, 40(7): 663-666.
[37]	JacksonC A L, Johnson H D. Sustained turbidity currents and their interaction with debrite-related topography:Labuan Island, offshore NW Borneo, Malaysia [J]. Sedimentary Geology, 2009, 219(1/2/3/4): 77-96.
[38]	Talling P J, Wynn R B, Masson D G, et al. Onset of submarine debris flow deposition far from original giant landslide[J]. Nature, 2007, 450(7169): 541-544.
[39]	Haughton P D W, Davis C, McCaffrey W, et al. Hybrid sediment gravity flow deposits -classification, origin and significance[J]. Marine and Petroleum Geology, 2009, 26(10): 1900-1918.
[40]	Sumner E J, Talling P J, Amy L A, et al. Facies architecture of individual basin-plain turbidites: Comparison with existing models and implications for flow processes[J]. Sedimentology, 2012, 59(6): 1850- 1887.
[41]	李文厚,邵磊,魏红红,等. 西北地区湖相浊流沉积[J]. 西北大学学报:自然科学版,2001,31(1):57-62.[Li Wenhou, Shao Lei, Wei Honghong, et al. Turbidity current deposits of lake facies in northwestern China[J]. Journal of Northwest University: Natural Science Edition, 2001, 31(1): 57-62. ]
[42]	王起琮,李文厚,赵虹,等. 鄂尔多斯盆地东南部三叠系延长组一段湖相浊积岩特征及意义[J]. 地质科学,2006,41(1):54-63.[Wang Qizong, Li Wenhou, Zhao Hong, et al. Characteristics and significance of lacustrine turbidites in the member 1 of Yanchang Formation, Upper Triassic in the southeastern Ordos Basin [J]. Chinese Journal of Geology, 2006, 41(1): 54-63.]
[43]	郑荣才,文华国,韩永林,等. 鄂尔多斯盆地白豹地区长6油层组湖底滑塌浊积扇沉积特征及其研究意义[J]. 成都理工大学学报:自然科学版,2006,33(6):566-575.[Zheng Rongcai, Wen Huaguo, Han Yonglin, et al. Discovery and significance of sublacustrine slump turbidite fans in Chang 6 oil-bearing formation of Baibao region in Ordos Basin, China [J]. Journal of Chengdu University of Technology: Science & Technology Edition, 2006, 33(6): 566-575.]
[44]	傅强,吕苗苗,刘永斗. 鄂尔多斯盆地晚三叠世湖盆浊积岩发育特征及地质意义[J]. 沉积学报,2008,26(2):186-192.[Fu Qiang, Lü Miaomiao, Liu Yongdou. Developmental characteristics of Turbidite and its implication on petroleum geology in Late-Triassic Ordos Basin [J]. Acta Sedimentologica Sinica, 2008, 26(2): 186-192.]
[45]	夏青松,田景春. 鄂尔多斯盆地西南部上三叠统长6油层组湖底扇特征[J]. 古地理学报,2007,9(1):33-43.[Xia Qingsong, Tian Jingchun. Sedimentary characteristics of sublacustrine fan of the Interval 6 of Yanchang Formation of Upper Triassic in southwestern Ordos Basin [J]. Journal of Palaeogeography, 2007, 9(1): 33-43.]
[46]	Chen Quanhong, Li Wenhou, Gao Yongxiang, et al. The deep-lake deposit in the Upper Triassic Yanchang Formation in Ordos Basin, China and its significance for oil-gas accumulation[J]. Science China: Earth Sciences,2007, 50(S2): 47-58.
[47]	邹才能,赵文智,张兴阳,等. 大型敞流坳陷湖盆浅水三角洲与湖盆中心砂体的形成与分布[J]. 地质学报,2008,82(6):815-825.[Zou Caineng, Zhao Wenzhi, Zhang Xingyang, et al. Formation and distribution of shallow-water deltas and central-basin sandbodies in large open depression lake basins [J]. Acta Geologica Sinica, 2008, 82(6): 815-825.]
[48]	邹才能,赵政璋,杨华,等. 陆相湖盆深水砂质碎屑流成因机制与分布特征——以鄂尔多斯盆地为例[J]. 沉积学报,2009,27(6):1065-1075.[Zou Caineng, Zhao Zhengzhang, Yang Hua, et al. Genetic mechanism and distribution of sandy debris flows in terrestrial lacustrine basin [J]. Acta Sedimentologica Sinica, 2009, 27(6): 1065-1075.]
[49]	李相博,付金华,陈启林,等. 砂质碎屑流概念及其在鄂尔多斯盆地延长组深水沉积研究中的应用[J]. 地球科学进展,2011,26(3):286-294.[Li Xiangbo, Fu Jinhua, Chen Qilin, et al. The concept of sandy debris flow and its application in the Yanchang Formation deep water sedimentation of the Ordos Basin [J]. Advances in Earth Science, 2011, 26(3): 286-294.]
[50]	李相博,刘化清,完颜容,等. 鄂尔多斯盆地三叠系延长组砂质碎屑流储集体的首次发现[J]. 岩性油气藏,2009,21(4):19-21.[Li Xiangbo, Liu Huaqing, Wanyan Rong, et al. First discovery of the sandy debris flow from the Triassic Yanchang Formation, Ordos Basin [J]. Lithologic Reservoirs, 2009, 21(4):19-21.]
[51]	付锁堂,邓秀芹,庞锦莲. 晚三叠世鄂尔多斯盆地湖盆沉积中心厚层砂体特征及形成机制分析[J]. 沉积学报,2010,28(6):1081-1089.[Fu Suotang, Deng Xiuqin, Pang Jinlian. Characteristics and mechanism of thick sandbody of Yanchang Formation at the centre of Ordos Basin[J]. Acta Sedimentologica Sinica, 2010, 26(6): 1081-1089.]
[52]	刘池洋,赵红格,桂小军,等. 鄂尔多斯盆地演化—改造的时空坐标及其成藏(矿)响应[J]. 地质学报,2006,80(5):617-638.[Liu Chiyang, Zhao Hongge, Gui Xiaojun, et al. Space-time coordinate of the evolution and reformation and mineralization response in Ordos Basin [J]. Acta Geologica Sinica, 2006, 80(5): 617-638.]
[53]	付国民,赵俊兴,张志升,等. 鄂尔多斯盆地东南缘三叠系延长组物源及沉积体系特征[J]. 矿物岩石,2010,30(1):99-105. [Fu Guomin, Zhao Junxing, Zhang Zhisheng, et al. The provenance and features of depositional system in the Yanchang Formation of Triassic in southeast area of Ordos Basin[J]. Journal of Mineralogy and Petrology, 2010, 30(1): 99-105.]
[54]	李涛,谈广鸣,张俊华,等. 水库异重流研究进展[J]. 中国农村水利水电,2006(9):21-24.[Li Tao, Tan Guangming, Zhang Junhua, et al. Research advances in reservoir hyperpycnal flow [J].China Rural Water and Hydropower, 2006(9): 21-24.]J]. 成都理工大学学报: 自然科学版,2006,33(6): 566-575.[Zheng Rongcai, Wen Huaguo, Han Yonglin, et al. Discovery and significance of sublacustrine slump turbidite fans in Chang 6 oil-bearing formation of Baibao region in Ordos Basin, China [J]. Journal of Chengdu University of Technology: Science & Technology Edition, 2006, 33(6): 566-575.]
[55]	傅强,吕苗苗,刘永斗. 鄂尔多斯盆地晚三叠世湖盆浊积岩发育特征及地质意义[J]. 沉积学报,2008,26(2): 186-192.[Fu Qiang, Lü Miaomiao, Liu Yongdou. Developmental characteristics of Turbidite and its implication on petroleum geology in late-Triassic Ordos Basin [J]. Acta Sedimentologica Sinica, 2008, 26(2): 186-192.]
[56]	夏青松,田景春. 鄂尔多斯盆地西南部上三叠统长6油层组湖底扇特征[J]. 古地理学报,2007,9(1): 33-43.[Xia Qingsong, Tian Jingchun. Sedimentary characteristics of sublacustrine fan of the Interval 6 of Yanchang Formation of Upper Triassic in southwestern Ordos Basin [J]. Journal of Palaeogeography, 2007, 9(1): 33-43.]
[57]	Chen Quanhong, Li Wenhou, Gao Yongxiang, et al. The deep-lake deposit in the Upper Triassic Yanchang Formation in Ordos Basin, China and its significance for oil-gas accumulation[J]. Science China: Earth Sciences,2007, 50(S2): 47-58.
[58]	邹才能,赵文智,张兴阳,等. 大型敞流坳陷湖盆浅水三角洲与湖盆中心砂体的形成与分布[J]. 地质学报,2008,82(6): 815-825.[Zou Caineng, Zhao Wenzhi, Zhang Xingyang, et al. Formation and distribution of shallow-water deltas and central-basin sandbodies in large open depression lake basins [J]. Acta Geologica Sinica, 2008, 82(6): 815-825.]
[59]	邹才能,赵政璋,杨华,等. 陆相湖盆深水砂质碎屑流成因机制与分布特征——以鄂尔多斯盆地为例[J]. 沉积学报,2009,27(6): 1067-1074.[Zou Caineng, Zhao Zhengzhang, Yang Hua, et al. Genetic mechanism and distribution of sandy debris flows in terrestrial lacustrine basin [J]. Acta Sedimentologica Sinica, 2009, 27(6): 1065-1076.]
[60]	李相博,付金华,陈启林,等. 砂质碎屑流概念及其在鄂尔多斯盆地延长组深水沉积研究中的应用[J]. 地球科学进展,2011,26(3): 286-294.[Li Xiangbo, Fu Jinhua, Chen Qilin, et al. The concept of sandy debris flow and its application in the Yanchang Formation deep water sedimentation of the Ordos Basin [J]. Advances in Earth Science, 2011, 26(3): 286-294.]
[61]	李相博,刘化清,完颜容,等. 鄂尔多斯盆地三叠系延长组砂质碎屑流储集体的首次发现[J]. 岩性油气藏,2009,21(4): 19-21.[Li Xiangbo, Liu Huaqing, Wanyan Rong, et al. First discovery of the sandy debris flow from the Triassic Yanchang Formation, Ordos Basin [J]. Lithologic Reservoirs, 2009, 21(4):19-21.]
[62]	付锁堂,邓秀芹,庞锦莲. 晚三叠世鄂尔多斯盆地湖盆沉积中心厚层砂体特征及形成机制分析[J]. 沉积学报,2010,28(6): 1081-1089.[Fu Suotang, Deng Xiuqin, Pang Jinlian. Characteristics and mechanism of thick sandbody of Yanchang Formation at the centre of Ordos Basin[J]. Acta Sedimentologica Sinica, 2010, 26(6): 1081-1089.]
[63]	刘池洋,赵红格,桂小军,等. 鄂尔多斯盆地演化—改造的时空坐标及其成藏(矿)响应[J]. 地质学报,2006,80(5): 617-638.[Liu Chiyang, Zhao Hongge, Gui Xiaojun, et al. Space-time coordinate of the evolution and reformation and mineralization response in Ordos Basin [J]. Acta Geologica Sinica, 2006, 80(5): 617-638.]
[64]	付国民,赵俊兴,张志升,等. 鄂尔多斯盆地东南缘三叠系延长组物源及沉积体系特征[J]. 矿物岩石,2010,30(1): 99-105. [Fu Guomin, Zhao Junxing, Zhang Zhisheng, et al. The provenance and features of depositional system in the Yanchang Formation of Triassic in southeast area of Ordos Basin[J]. Journal of Mineralogy and Petrology, 2010, 30(1): 99-105.]
[65]	李涛,谈广鸣,张俊华,等. 水库异重流研究进展[J]. 中国农村水利水电,2006(9): 21-24.[Li Tao, Tan Guangming, Zhang Junhua, et al. Research advances in reservoir hyperpycnal flow [J].China Rural Water and Hydropower, 2006(9): 21-24.]

Discovery of Hyperpycnal Flow Deposits in the Late Triassic Lacustrine Ordos Basin

doi: 10.14027/j.cnki.cjxb.2015.01.002

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