Tempestites and storm deposites in the Lower Cretaceous from Lingshan Island, Qingdao
Zhong Jianhua1, Ni Liangtian1, Shao Zhufu2, Li Yong1, Liu Xuan3, Mao Cui4, Liu Shengxin1, Sun Ningliang1, Chen Bin1, Wang Kai1, Luo Ke1, Wang Shaojie1, Liu Chuang1, Liu Bao1, Xiong Zhiqiang1
1 School of Geosciences,China University of Petroleum(East China),Qingdao 266580,Shandong; 2 Key Laboratory of Marine Hydrocarbon Resources and Environmental Geology,Ministry of Land and Resources of China,Qingdao 266071,Shandong; 3 Research Institute of Petroleum Exploration &Development,SINOPEC, Beijing 100083; 4 School of Geosciences,Northeast Petroleum University,Daqing 163318,Heilongjiang;
Abstract：The typical tempestites and storm deposites developed well in detritus rocks in the Lower Cretaceous of Lingshan Island,Qingdao,Shandong Province. The features are as follows: (1)Hummocky or swaley structures and hummocky or swaley cross-stratification often occur and the hummocky cross-stratification is symmetrical or nearly symmetrical,commonly developed in thin-bedded sand and mud rocks that form in delta foresets. The thin layers are 1-2,cm in thickness and sometimes thicker. The parallel bedding or lower dipping angle cross bedding commonly occurs in the sandstones and sometimes hummocky cross-stratification and hummocky structure can also been observed. The laminea of hummocky cross-stratification is relatively thick,commonly between 1-2,cm,even 3-4,cm. Swaley cross-stratification relatively seldom occurs and commonly not perfect. Nevertheless,the swale structure is relatively common observed. (2)The swashing-eroding surface is considerably developed well and displace wavy ups and downs or is uneven with 20-30,cm height differences or even larger. The inner swashing-eroding surface commonly is not continuous and the bottom swashing-eroding surface is continuous very well. (3)The swashing-eroding surface developing in the medium and thick sandstone can be divided into several sub-layer,and because of discontinuity they combined together. (4)The sandstone contains commonly mudstone intraclast,most of them are dark mudstone with the diameters from 1-2,cm to 10,cm and the shape is polytropic. The long axis of mudstone gravels distributes mostly along the bedding plane. (5)The tempestites and storm deposites are fine to medium sandstones and not true conglomerate. (6)Intergrowth with a lot of multiple-scale and multiple-type soft sidement deformation structures. (7)Sometimes containing a bit of carbonized detritus of mm-scale. The discovery of tempestites and storm deposites reveals that the stratum is formed in relatively shallow water environment,not deep water environment like the sea and ocean. Otherwise,the storm makes the sandstone being sorted better and moves to the lower position of the foresets,resulting in being contacted with hydrocarbon rock and optimize its combination with sandstone reservoir,benefiting to formation of oil and gas trap.
Zhong Jianhua,Ni Liangtian,Shao Zhufu et al. Tempestites and storm deposites in the Lower Cretaceous from Lingshan Island, Qingdao[J]. JOPC, 2016, 18(3): 381-398.
[1] 陈辉,田景春,蒋裕强,游李伟,张翔,康建威. 2008. 川中地区须二、四段湖相风暴岩沉积特征及其意义. 新疆石油地质,29(5):581-584. [Chen H,Tian J C,Jiang Y Q,You L W,Zhang X,Kang J W. 2008. Sedimentary characteristics and significance of the storm deposits in the two and four stages of the Sichuan basin. Xinjiang Petroleum Geology,29(5):581-584] [2] 董晓朋,吕洪波,张星,张海春,王俊,张素菁. 2013. 山东灵山岛早白垩世复理石软沉积变形期次解析. 地质论评,59(6):1061-1066. [Dong X P,Lü H B,Zhang X,Zhang H C,Wang J,Zhang S J. 2013. Shandong Lingshan Island Early Cretaceous flysch soft sedimentary deformation stages. Geological Review,59(6):1061-1066] [3] 董晓朋,吕洪波,张星,张海春,王俊,张素菁. 2014. 灵山岛北端早白垩世复理石中的滑塌断崖. 地质论评,60(4):771-779. [Dong X P,Lü H B,Zhang X,Zhang H C,Wang J,Zhang S J. 2014. North Lingshan Island Early Cretaceous flysch in the stone cliff collapse. Geological Review,60(4):771-779] [4] 方少仙,侯方浩,杨西燕,何江,沈昭国,乔琳,阎荣辉. 2011. 鄂尔多斯盆地内部中二叠统石盒子组盒8下亚段砂岩中的风暴岩. 沉积学报,29(1):23-30. [Fang S X,Hou F H,Yang X Y,He J,Shen Z G,Qiao L,Yan R H. 2011. The storm rocks in the two lower sub section of the Middle Triassic in the Ordos basin. Acta Sedimentologica Sinica,29(1):23-30] [5] 冯兴雷,马立祥,邓宏文,林会喜. 2011. 大王北洼陷湖相滩坝砂体风暴沉积特征. 新疆地质,29(1):80-85. [Feng X L,Ma L X,Deng H W,Lin H X. 2011. Dawangbei subsag of lacustrine sedimentary characteristics of beach bar sand storm. Xinjiang Geology,29(1):80-85] [6] 郭峰,郭岭. 2011. 柴达木盆地西部古近系湖相风暴岩. 新疆地质,29(2):125-129. [Guo F,Guo L. 2011. Lacustrine facies storm rocks in the western Qaidam basin. Xinjiang Geology,29(2):125-129] [7] 姜在兴,赵澄林,刘孟慧,袁政文. 1990. 东濮凹陷西部湖相风暴沉积的初步研究. 沉积学报,8(1):107-114. [Jiang Z X,Zhao C L,Liu M H,Yuan Z W. 1990. A preliminary study on the east sag web lacustrine storm deposits. Acta Sedimentologica Sinica,8(1):107-114] [8] 吕洪波,王俊,张海春. 2011. 山东灵山岛晚中生代滑塌沉积层的发现及区域构造意义初探. 地质学报, 85(6):938-946. [Lü H B,Wang J,Zhang H C. 2011. Shandong Lingshan Island late Mesozoic tectonic significance of the sliding layer and collapse area. Acta Geologica Sinica,85(6):938-946] [9] 吕洪波,张海春,王俊,张素菁,董晓朋,张星. 2013. 灵山岛早白垩世复理石不是陆内三角洲沉积:答钟建华教授. 地质论评,59(1):11-14. [Lü H B,Zhang H C,Wang J,Zhang S J,Dong X P,Zhang X. 2013. Lingshan Island Early Cretaceous flysch not intracontinental Delta:A reply to Professor Zhong Jianhua. Geological Review,59(1):11-14] [10] 孙钰,钟建华,姜在兴,饶孟余. 2006. 松辽盆地南部青山口组湖相风暴沉积. 煤田地质与勘探,34(1):12-15. [Sun Y,Zhong J H,Jiang Z X,Rao M Y. 2006. Lake facies storm deposits in the southern part of the Songliao basin. Coal Geology and Exploration,34(1):12-15] [11] 王安东,周瑶琪,闫华,王瑞,张振凯,王子阳. 2013. 山东省灵山岛早白垩世软沉积物变形构造特征. 古地理学报,15(5):718-728. [Wang A D,Zhou Y Q,Yan H,Wang R,Zhang Z K,Wang Z Y. 2013. Shandong Province Lingshan Island Early Cretaceous tectonic deformation characteristics of soft sediments. Journal of Palaeogeography(Chinese Edition),15(5):718-728] [12] 王安东,周瑶琪,张振凯,于姗姗,王子阳. 2014. 山东灵山岛莱阳群水下非构造裂缝特征及意义. 地球学报,35(3):321-328. [Wang A D,Zhou Y Q,Zhang Z K,Yu S S,Wang Z Y. 2014. Non fracture characteristics and significance of structure of Shandong Lingshan island Laiyang group under the water. Acta Geoscientia Sinica,35(3):321-328] [13] 阳伟,田景春,朱迎堂,王峰. 2009. 河南登封地区上二叠统石千峰组风暴沉积特征. 沉积与特提斯地质,29(1):65-70. [Yang W,Tian J C,Zhu Y T,Wang F. 2009. Two characteristics of Permian Shiqianfeng Formation in Dengfeng area of Henan storm deposits. Sedimentary Geology and Tethyan Geology,29(1):65-70] [14] 袁静. 2006. 山东惠民凹陷古近系风暴岩沉积特征及沉积模式. 沉积学报, 24(1):43-49. [Yuan J. 2006. Sedimentary characteristics and depositional model of the ancient near system of the Shandong depression. Acta Sedimentologica Sinica,24(1):43-49] [15] 张金亮,寿建峰,赵澄林,袁政文. 1988. 东濮凹陷沙三段的风暴沉积. 沉积学报,6(1):50-57. [Zhang J L,Shou J F,Zhao C L,Yuan Z W. 1988. The storm deposits in Dongpu sag sand three section. Acta Sedimentologica Sinica,6(1):50-57] [16] 郑宁,姜在兴,李廷栋,耿树方,游国庆,何幼斌. 2010. 渤海湾盆地孤南洼陷沙三中亚段风暴沉积基本特征及其地质意义. 中国地质,37(4):1191-1198. [Zheng N,Jiang Z X,Li T D,Geng S F, You G Q,He Y B. 2010. The basic characteristics of sediments in Bohai Bay Basin in Gunan sag storm and its geological significance. Geology in China,37(4):1191-1198] [17] 钟建华. 2012. 灵山岛中生代沉积岩是深水远源浊积岩还是陆内三角洲沉积?与吕洪波教授商榷. 地质论评,58(6):1180-1182. [Zhong J H. 2012. Lingshan Island Mesozoic sedimentary rocks in deep water far source turbidite or continental delta deposits?A discussion with Professor Lü Hongbo. Geological Review,58(6):1180-1182] [18] Allen P A. 1982. Physical oceanography of continental shelves. Reviews of Geophysics and Space Physics,21:1149-1181. [19] Aigner T A. 1980. Storm deposits as a tool in facies analysis. International Association of Sedimentologists 1st European Meeting. Abstracts:44-46. [20] Aigner T A. 1985. Storm Depositional Systems. Springer Verlag,Berlin:119. [21] Aigner T A. 1985. Storm depositional systems:Dynamic stratigraphy in modern and ancient shallow-marine sequences:Berlin,Springer-Verlag,Lecture Notes in Earth Sciences,3:174. [22] Aigner T A,Reineck H E. 1982. Proximality trends in modern storm sands from the Helgoland Bight(North Sea)and their implications for basin analysis. Senckenbergiana Marítima,14:83-215. [23] Dott R H,Bourgeois J. 1982. Hummocky stratification:Significance of its variable bedding sequences. Geology. Society of America Bulletin,93:663-680. [24] Einsele G,Seilacher A. 1991. Distinction of Tempestites and turbidites. In: Einsele G,Ricken,Myrow P M,Southard J B (eds). Tempestite deposition. Journal of Sedimentary Research:875-887. [25] Gillbert G K. 1899. Ripple-marks and cross-bedding. Geology Society of America Bulletin, 10:135-140. [26] Immenhauser A. 2009. Estimating palaeo-water depth from the physical rock record. Earth-Science Review,96:107-139. [27] Kelling G,Mullin P R. 1975. Graded limestones and limestone-quartzite couplets:Possible storm-deposits from the Moroccan Carboniferous. Sedimentary Geology,13:161-190. [28] Klein G D,Marsaglia K M. 1987. Discussion of “Hummocky cross-stratification,tropical hurricanes,and intense winter storms”:Sedimentology,34:333-337. [29] Liu X,Zhong J H,Grapes R,Bian S H,Liang C. 2012. Late Cretaceous tempestite in northern Songliao Basin,China. Journal of Asian Earth Sciences,56:33-41. [30] Mohseni H,Al-Aasm I S. 2004. Tempestite deposits on a storm-influenced carbonate ramp:An example from the pabdeh formation(paleogene),Zagros basin,SW Iran. Journal of Petroleum Geology,27(2):163-178. [31] Molina1 J M,Alfaro P,Moretti M,Soria J M. 1998. Soft-sediment deformation structures induced by cyclic stress of storm waves in tempestites(Miocene,Guadalquivir Basin,Spain). Terra Nova,10(3):145-150. [32] Osamu F,Takanobu K. 2007. Identification of trunami deposits considering the trunami waveform:An example of suaqueous trunami deposits in Holocene shallow bay on southern Boso Peninsula,Central Japan. Sedimentary Geology,200:295-313. [33] Paul M. M,John B. S. 1996. Tempestite deposition. Journal of Sedimentary Research,66(5):875-887.
