松辽盆地东缘岳王城剖面嫩江组二段生物地层及其对湖侵事件的响应
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摘要
松辽盆地嫩江组二段下部沉积期发生了大规模的湖侵事件,在整个盆地范围形成一套黑色泥页岩夹油页岩。然而,前人对嫩江组二段的地层及相关地质事件的研究主要基于井下岩心,地表露头不多见。通过调查,在松辽盆地东缘农安县青山口第二松花江沿岸发现一新的剖面——岳王城剖面,出露连续的嫩江组一段顶部—二段下部地层。通过对该套地层进行厘米级的描述和详细的分层,将该剖面地层划分为24层,累计厚度31.54m。第1层为嫩江组一段顶部,为青灰色砂质泥岩,含少量介形类化石;第2~24层为嫩江组二段下部,主体为暗色泥页岩夹油页岩、泥灰岩等,含丰富的介形类、叶肢介、鱼类,少量有孔虫及其他生物。此外,在嫩江组底部还发现一层火山灰和一层磷块岩。对其中的介形类化石进行初步研究,识别出11属18种。通过介形虫古生态和沉积学研究,并结合其他手段,初步探讨了该沉积期的湖泊环境,认为嫩二段下部沉积期经历了一次大规模湖侵,从一段顶部的滨浅湖过渡为二段下部的深湖环境,之后湖平面在波动中逐渐下降。
Large-scale lake transgressions occurred in the lower part of the 2~(nd) Member of the Nenjiang Formation in the Songliao Basin, which deposited a set of dark mudstone and black shale with intercalation of oil shale throughout the basin. However, previous researches on strata and related geological events in the 2~(nd) Member of the Nenjiang Formation were mainly based on the cores, with very insufficient attention paid to outcrops. A new section called Yuewangcheng section was found along the Di'er Songhua River in Qingshankou, Nong'an County, eastern margin of Songliao Basin, which successively exposes the top of the 1 stMember to the lower parts of the 2~(nd) Member of the Nenjiang Formation. In this study, the strata were described in centimeter-level and divided in detail into 24 layers with a cumulative thickness of 31.54 m. The first layer is the top of the 1 stMember of the Nenjiang Formation,which deposited bluish gray sandy mudstone with a small quantity of ostracods. 2~(nd) -24 thlayers constitute the lower part of the 2~(nd) Member of Nenjiang Formation, which is composed of dark shale with oil shale and marl, characterized by rich ostracods, phyllodes and fish,with a small amount of foraminifera and other organisms. In addition, a layer of volcanic ash and phosphorite was found at the bottom of Nenjiang Formation. 18 species of 11 genera of ostracods were preliminarily identified. On the basis of sedimentology and ostracod palaeoecology combined with other evidence, the lake environment is preliminarily discussed. It is suggested that a large-scale lake transgression occurred in the lower part of the 2~(nd) Member of Nenjiang Formation. The shore-shallow lake environment at the top turned to a deep lake environment at the bottom, and then the lake level was gradually declined in fluctuation.
Large-scale lake transgressions occurred in the lower part of the 2~(nd) Member of the Nenjiang Formation in the Songliao Basin, which deposited a set of dark mudstone and black shale with intercalation of oil shale throughout the basin. However, previous researches on strata and related geological events in the 2~(nd) Member of the Nenjiang Formation were mainly based on the cores, with very insufficient attention paid to outcrops. A new section called Yuewangcheng section was found along the Di'er Songhua River in Qingshankou, Nong'an County, eastern margin of Songliao Basin, which successively exposes the top of the 1 stMember to the lower parts of the 2~(nd) Member of the Nenjiang Formation. In this study, the strata were described in centimeter-level and divided in detail into 24 layers with a cumulative thickness of 31.54 m. The first layer is the top of the 1 stMember of the Nenjiang Formation,which deposited bluish gray sandy mudstone with a small quantity of ostracods. 2~(nd) -24 thlayers constitute the lower part of the 2~(nd) Member of Nenjiang Formation, which is composed of dark shale with oil shale and marl, characterized by rich ostracods, phyllodes and fish,with a small amount of foraminifera and other organisms. In addition, a layer of volcanic ash and phosphorite was found at the bottom of Nenjiang Formation. 18 species of 11 genera of ostracods were preliminarily identified. On the basis of sedimentology and ostracod palaeoecology combined with other evidence, the lake environment is preliminarily discussed. It is suggested that a large-scale lake transgression occurred in the lower part of the 2~(nd) Member of Nenjiang Formation. The shore-shallow lake environment at the top turned to a deep lake environment at the bottom, and then the lake level was gradually declined in fluctuation.
引文
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[24]刘招君,王东坡,刘立,等.松辽盆地白垩纪沉积特征[J].地质学报, 1992,(4):327-338.
[25]侯启军,赵志魁,王立武,等.松辽盆地深层天然气富集条件的特殊性[J].大庆石油学报, 2009, 33(2):31-35.
[26]高有峰,王成善,王璞珺,等.松科1井北孔选址、岩心剖面特征与特殊岩性层的分布[J].地学前缘, 2009, 16(6):104-112.
[27]高有峰,王璞珺,程日辉,等.松辽盆地松科1井上白垩统嫩江组一、二段沉积序列厘米级精细刻画:岩性·岩相·旋回[J].地学前缘, 2011, 18(6):195-217.
[28]Yu Z Q, He H Y, Deng C L, et al. New geochronologIcal constraints on the Nenjiang Formation in the Songliao Basin, NE China[J]. Cretaceous Research, 2019, doi:10.1016/j.cretres.
[29]张弥曼,周家健.我国东部中、新生代含油地层中的鱼化石及有关沉积环境的讨论[J].古脊椎动物学报, 1978, 16(4):19-27, 87.
[30]顾知微,黄宝玉,陈楚震,等.中国的瓣鳃类化石[M].北京:科学出版社, 1976.
[31]Xi D P, Cao W X, Huang Q H, et al. Late Cretaceous marine fossils and seawater incursion events in the Songliao Basin, NE China[J]. Cretaceous Research, 2016, 62:172-182.
[32]张智礼,蔡习尧,张铭,等.松辽盆地晚白垩世青山口组—嫩江组一段介形类壳饰,壳形类型与环境关系分析[J].中国地质,2014, 41(1):135-147.
[33]童晓宁,胡建芳,祝孟博,等.分子标志物揭示的松辽盆地晚三冬期气候环境[J].地学前缘, 2017, 24(1):154-165.
[34]祝孟博,宋建中,童晓宁,等.松辽盆地晚三冬期的黑碳记录及其古环境意义[J].地学前缘, 2017, 24(1):166-173.
[35]He H Y, Deng C L, Wang P J, et al. Toward age determination of the termination of the Cretaceous Normal Superchron[J].Geochemistry Geophysics Geosystems, 2012, 13:Q02002
[36]Haq B U. Cretaceous eustasy revisited[J]. Global&Planetary Change, 2014, 113(2):44-58.
[37]张智礼,蔡习尧,张莹,等.松辽盆地晚白垩世介形类古生态学[J].微体古生物学报, 2013(2):132-144.
[38]李军,余俊清.湖相介形虫古生态学在环境变化研究中的应用[J].盐湖研究, 2002, 10(1):66-71.
[2]Hu X M, Jansa L, Wang C S, et al. Upper Cretaceous oceanic red beds(CORBs)in the Tethys:occurrences, lithofacies, age, and environments[J]. Cretaceous Research, 2005, 26(1):3-20.
[3]Schlanger S O, Jenkyns H C. Cretaceous Oceanic Anoxic Events:Causes and consequences[J]. Geologie En Mijnbouw, 1976, 55(3/4):179-184.
[4]席党鹏,万晓樵,李国彪,等.中国白垩纪综合地层和时间框架[J].中国科学:地球科学, 2019, 49(1):261-292.
[5]Williams D F, Liu T S. The study of lake sediments for global change research[J]. Earth Science Frontiers, 1997, 4(1/2):34-42.
[6]Park L E, Cohen A S, Martens K, et al. The impact of taphonomic processes on interpreting paleoecologic changes in large lake ecosystems:ostracodes in Lakes Tanganyika and Malawi[J]. Journal of Paleolimnology, 2003, 30(2):127-138.
[7]杨万里,高瑞祺,郭庆福,等.松辽盆地陆相油气生成、运移和聚集[M].哈尔滨:黑龙江科学技术出版社, 1985.
[8]Wan X Q, Zhao J, Scott R W, et al. Late Cretaceous stratigraphy,Songliao Basin, NE China:SK1 cores[J]. Palaeogeography,Palaeoclimatology, Palaeoecology, 2013, 385:31-43.
[9]Wang P J, Mattern F, Didenko N A, et al. Tectonics and cycle system of the Cretaceous Songliao Basin:An inverted active continental margin basin[J]. Earth-Science Reviews, 2016, 159:82-102.
[10]黄清华,郑玉龙,杨明杰,等.松辽盆地白垩纪古气候研究[J].微体古生物学报, 1999, 16(1):95-103.
[11]万晓樵,吴怀春,席党鹏,等.中国东北地区白垩纪温室时期陆相生物群与气候环境演化[J].地学前缘, 2017, 24(1):18-31.
[12]刘招君,柳蓉.中国油页岩特征及开发利用前景分析[J].地学前缘, 2005, 12(3):315-323.
[13]高瑞祺.松辽盆地白垩纪陆相沉积特征[J].地质学报, 1980, 54(1):9-26.
[14]刘招君,孙平昌,贾建亮,等.陆相深水环境层序识别标志及成因解释:以松辽盆地青山口组为例[J].地学前缘, 2011, 18(4):171-180.
[15]Xi D P, Wan X Q, Feng Z Q, et al. Discovery of Late Cretaceous foraminifera in the Songliao Basin:Evidence from SK-1 and implications for identifying seawater incursions[J]. Chinese Science Bulletin, 2011, 56(3):253-256.
[16]Hu J F, Peng P A, Liu M Y, et al. Seawater incursion events in a Cretaceous paleo-lake revealed by specific marine biological markers[J]. Scientific reports, 2015, 5:9508.
[17]Huber B T, Norris R D, MacLeod K G. Deep-sea paleotemperature record of extreme warmth during the Cretaceous[J].Geology, 2002, 30(2):123-126.
[18]O'Brien C L, Robinson S A, Pancost R D, et al. Cretaceous seasurface temperature evolution:Constraints from TEX86 and planktonic foraminiferal oxygen isotopes[J]. Earth-Science Reviews, 2017, 172:224-247.
[19]侯贺晟,王成善,张交东,等.松辽盆地大陆深部科学钻探地球科学研究进展[J].中国地质, 2018, 45(4):641-657.
[20]闫晶晶,席党鹏,于涛,等.松辽盆地青山口地区嫩江组下部生物地层及环境变化[J].地层学杂志, 2007, 31(3):296-302.
[21]席党鹏,李罡,万晓樵,等.松辽盆地东南区姚家组-嫩江组-段地层特征与湖泊演变[J].古生物学报, 2009, 48(3):556-568.
[22]叶得泉,黄清华,张莹.松辽盆地白垩纪介形类生物地层学[M].北京:石油工业出版社, 2002.
[23]胡望水,吕炳全,张文军,等松辽盆地构造演化及成盆动力学探讨[J].地质科学, 2005, 40(1):16-31.
[24]刘招君,王东坡,刘立,等.松辽盆地白垩纪沉积特征[J].地质学报, 1992,(4):327-338.
[25]侯启军,赵志魁,王立武,等.松辽盆地深层天然气富集条件的特殊性[J].大庆石油学报, 2009, 33(2):31-35.
[26]高有峰,王成善,王璞珺,等.松科1井北孔选址、岩心剖面特征与特殊岩性层的分布[J].地学前缘, 2009, 16(6):104-112.
[27]高有峰,王璞珺,程日辉,等.松辽盆地松科1井上白垩统嫩江组一、二段沉积序列厘米级精细刻画:岩性·岩相·旋回[J].地学前缘, 2011, 18(6):195-217.
[28]Yu Z Q, He H Y, Deng C L, et al. New geochronologIcal constraints on the Nenjiang Formation in the Songliao Basin, NE China[J]. Cretaceous Research, 2019, doi:10.1016/j.cretres.
[29]张弥曼,周家健.我国东部中、新生代含油地层中的鱼化石及有关沉积环境的讨论[J].古脊椎动物学报, 1978, 16(4):19-27, 87.
[30]顾知微,黄宝玉,陈楚震,等.中国的瓣鳃类化石[M].北京:科学出版社, 1976.
[31]Xi D P, Cao W X, Huang Q H, et al. Late Cretaceous marine fossils and seawater incursion events in the Songliao Basin, NE China[J]. Cretaceous Research, 2016, 62:172-182.
[32]张智礼,蔡习尧,张铭,等.松辽盆地晚白垩世青山口组—嫩江组一段介形类壳饰,壳形类型与环境关系分析[J].中国地质,2014, 41(1):135-147.
[33]童晓宁,胡建芳,祝孟博,等.分子标志物揭示的松辽盆地晚三冬期气候环境[J].地学前缘, 2017, 24(1):154-165.
[34]祝孟博,宋建中,童晓宁,等.松辽盆地晚三冬期的黑碳记录及其古环境意义[J].地学前缘, 2017, 24(1):166-173.
[35]He H Y, Deng C L, Wang P J, et al. Toward age determination of the termination of the Cretaceous Normal Superchron[J].Geochemistry Geophysics Geosystems, 2012, 13:Q02002
[36]Haq B U. Cretaceous eustasy revisited[J]. Global&Planetary Change, 2014, 113(2):44-58.
[37]张智礼,蔡习尧,张莹,等.松辽盆地晚白垩世介形类古生态学[J].微体古生物学报, 2013(2):132-144.
[38]李军,余俊清.湖相介形虫古生态学在环境变化研究中的应用[J].盐湖研究, 2002, 10(1):66-71.
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