北京下苇甸剖面张夏组鲕粒特征及其白云化机制
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摘要
北京下苇甸剖面张夏组作为华北寒武系的标准剖面之一,鲜有人对其中的鲕粒类型及其成岩作用进行细致研究。在充分调研前人研究的基础上,通过野外观察、实测,并结合室内薄片鉴定、XRD测试等技术,对下苇甸剖面张夏组的鲕粒类型进行总结,并对鲕粒白云化机制进行分析。结果显示:(1)下苇甸张夏组鲕粒类型主要为放射鲕、同心放射鲕及单晶鲕/多晶鲕,还有少量同心鲕、复鲕及藻鲕;(2)鲕粒发生白云化,填隙物未见白云化,且放射圈层白云化程度高于同心圈层,并且放射圈层白云石颗粒围绕核心呈放射状分布,同心圈层围绕核心呈同心状分布;(3)鲕粒内部白云石颗粒多为中细晶,自形-半自形,回流渗透白云化是造成鲕粒白云化的主要成因,因此造成亮晶鲕粒石灰岩白云化程度高于灰泥鲕粒石灰岩。
The Xiaweidian outcrop in Beijing is a typical Cambrian stratigraphic profile in North China. Previous studies focused mainly on the depositional environment of the Zhangxia Formation,whereas the oolitic types and their diagenesis of the formation are poorly understood. In this paper,field geological and microscopic petrographic observations and XRD analysis were conducted to identify the oolitic types and elucidate the mechanism of oolitic dolomitization. It comes to a conclusion as follows:( 1) Major oolitic types include radial ooids,concentric-radial ooids and monocrystalline/polycrystalline ooids,and minor concentric ooids,compound ooids and algae ooids.( 2) Oolites are dolomitized whereas the interstitials are not,and the degree of dolomitization in the radial layer is higher than that in the concentric layer. Dolomite particles in the radial layer are radially distributed around the core,and the concentric rings occur around the core.( 3) Dolomite grains in the oolites are mostly mesocrystalline or fine-grained,euhedral to subhedral,and returning infiltration of dolomitization was likely the main cause of the oolitic dolomitization,which resulted in a higher degree of dolomitization of the luminescent oolite limestone than the stucco oolite limestone.
The Xiaweidian outcrop in Beijing is a typical Cambrian stratigraphic profile in North China. Previous studies focused mainly on the depositional environment of the Zhangxia Formation,whereas the oolitic types and their diagenesis of the formation are poorly understood. In this paper,field geological and microscopic petrographic observations and XRD analysis were conducted to identify the oolitic types and elucidate the mechanism of oolitic dolomitization. It comes to a conclusion as follows:( 1) Major oolitic types include radial ooids,concentric-radial ooids and monocrystalline/polycrystalline ooids,and minor concentric ooids,compound ooids and algae ooids.( 2) Oolites are dolomitized whereas the interstitials are not,and the degree of dolomitization in the radial layer is higher than that in the concentric layer. Dolomite particles in the radial layer are radially distributed around the core,and the concentric rings occur around the core.( 3) Dolomite grains in the oolites are mostly mesocrystalline or fine-grained,euhedral to subhedral,and returning infiltration of dolomitization was likely the main cause of the oolitic dolomitization,which resulted in a higher degree of dolomitization of the luminescent oolite limestone than the stucco oolite limestone.
引文
[1]DUGUID S M A,KYSER T K,JAMES N P,et al.Microbes and ooids[J].Journal of Sedimentary Research,2010,80(3/4):236-251.
[2]KRUMBEIN W E.Biomicrospheres generate ooids in the laboratory[J].Geomicrobiology Journal,2006,23(7):545-550.
[3]PLEE K,ARIZTEGUI D,MARTINI R,et al.Unravelling the microbial role in ooid formation:results of an in situ experiment in modern freshwater Lake Geneva in Switzerland[J].Geobiology,2010,6(4):341-350.
[4]李飞,武思琴,刘柯.鲕粒原生矿物识别及对海水化学成分变化的指示意义[J].沉积学报,2015,33(3):500-511.
[5]梅冥相.鲕粒成因研究的新进展[J].沉积学报,2012,30(1):20-32.
[6]周瑶琪,张晗,张振凯.海相碳酸盐鲕粒形成过程的模拟实验研究[J].中国石油大学学报(自然科学版),2017,41(3):23-30.
[7]王英华,杨承运,张秀莲.鲕粒的结构变化与成岩作用性质和强度的关系[J].沉积学报,1983,1(2):77-87.
[8]张秀莲.鲕粒在成岩作用中的次生变化及其意义[J].大庆石油地质与开发,1984(4):5-16.
[9]蒋小琼,管宏林,郑和荣,等.四川盆地普光气田飞仙关组白云岩储层成因探讨[J].石油实验地质,2014,36(3):332-336.
[10]苏立萍,罗平,胡社荣,等.川东北罗家寨气田下三叠统飞仙关组鲕粒滩成岩作用[J].古地理学报,2004,6(2):182-190.
[11]王恕一,蒋小琼,管宏林,等.川东北普光气田鲕粒白云岩储层粒内溶孔的成因[J].沉积学报,2010,28(1):10-16.
[12]薛晶晶,孙靖,朱筱敏,等.准噶尔盆地二叠系风城组白云岩储层特征及成因机理分析[J].现代地质,2012,26(4):755-761.
[13]伊硕,黄文辉,金振奎,等.哈萨克斯坦Zanazor油田石炭系KT-Ⅱ碳酸盐岩层成岩作用与孔隙演化[J].现代地质,2017,31(4):791-801.
[14]陈荣坤.埋藏环境下碳酸盐岩建设性成岩作用类型、特征及其意义[J].现代地质,1993,7(1):40-49.
[15]姜楠,范凌霄,刘卉,等.普光气田滩相储层特征及白云化成因[J].天然气地球科学,2013,24(5):923-930.
[16]张欣国,饶丹,蔡立国.普光气藏储层中鲕粒白云岩孔隙成因分析[J].天然气技术与经济,2009(2):11-13.
[17]景宇轩,刘建波,闫振,等.利用风暴沉积类型恢复海平面变化:以北京西山下苇甸剖面寒武纪中晚期风暴沉积为例[J].古地理学报,2015,17(5):653-668.
[18]黄宝春,周烑秀,朱日祥.从古地磁研究看中国大陆形成与演化过程[J].地学前缘,2008,15(3):348-359.
[19]金振奎,石良,高白水,等.碳酸盐岩沉积相及相模式[J].沉积学报,2013,31(6):965-979.
[20]冯增昭,陈继新,吴胜和.华北地台早古生代岩相古地理[J].沉积学报,1989,7(4):15-55.
[21]康世龙,邵龙义,易琦,等.京西下苇甸地区寒武系岩石特征及沉积环境研究[J].中国煤炭地质,2016,28(6):1-8.
[22]马永生,梅冥相,周润轩,等.层序地层框架下的鲕粒滩形成样式:以北京西郊下苇甸剖面寒武系第三统为例[J].岩石学报,2017,33(4):1021-1036.
[23]梅冥相.华北寒武系二级海侵背景下的沉积趋势及层序地层序列:以北京西郊下苇甸剖面为例[J].中国地质,2011,38(2):317-337.
[24]王成述,范开强,尹占国.北京西山中寒武统张夏组鲕粒特征及其环境意义[M]//中国地质科学院地质研究所.中国地质科学院地质研究所文集.北京:中国地质科学院地质研究所,1990:17.
[25]张旭,张宁,杨振鸿,等.北京西山下苇甸中寒武统碳酸盐岩微相及沉积相研究[J].地质科技情报,2009,28(6):25-30.
[26]朱筱敏.沉积岩石学[M].北京:石油工业出版社,2008:1-20.
[27]TUCKER M E,BATHURST R G C.New Interpretations of Great Salt Lake Ooids and of Ancient Non-Skeletal Carbonate Mineralogy[M].London:Blackwell Publishing Ltd,2009:497-537.
[28]祝海华,钟大康.四川盆地龙岗气田三叠系飞仙关组储集层特征及成因机理[J].古地理学报,2013,15(2):275-282.
[29]魏国齐,杨威,张林,等.川东北飞仙关组鲕滩储层白云石化成因模式[J].天然气地球科学,2005,16(2):162-166.
[30]高白水,金振奎,朱小二,等.哈萨克斯坦扎纳诺尔油田石炭系碳酸盐岩浅滩沉积模式及诸层质量差异机理[J].石油学报,2016,37(7):867-877.
[31]金振奎,邹元荣,张响响,等.黄骅坳陷古近系沙河街组湖泊碳酸盐沉积相[J].古地理学报,2002,4(3):11-18.
[32]邢延路,冯李强.北京西山下苇甸剖面寒武系徐庄组鲕粒研究[J].古地理学报,2015,17(4):517-528.
[33]周书欣.碳酸盐鲕粒的成因与鉴别[J].地质地球化学,1982(1):18-21.
[34]袁鑫鹏,刘建波.回流渗透模式白云岩研究历史与进展[J].古地理学报,2012,14(2):219-228.
[35]黄思静.碳酸盐岩的成岩作用[M].北京:地质出版社,2010:1-20.
[36]王英华.碳酸盐岩成岩作用与孔隙演化[J].沉积学报,1992,10(3):85-95.
[2]KRUMBEIN W E.Biomicrospheres generate ooids in the laboratory[J].Geomicrobiology Journal,2006,23(7):545-550.
[3]PLEE K,ARIZTEGUI D,MARTINI R,et al.Unravelling the microbial role in ooid formation:results of an in situ experiment in modern freshwater Lake Geneva in Switzerland[J].Geobiology,2010,6(4):341-350.
[4]李飞,武思琴,刘柯.鲕粒原生矿物识别及对海水化学成分变化的指示意义[J].沉积学报,2015,33(3):500-511.
[5]梅冥相.鲕粒成因研究的新进展[J].沉积学报,2012,30(1):20-32.
[6]周瑶琪,张晗,张振凯.海相碳酸盐鲕粒形成过程的模拟实验研究[J].中国石油大学学报(自然科学版),2017,41(3):23-30.
[7]王英华,杨承运,张秀莲.鲕粒的结构变化与成岩作用性质和强度的关系[J].沉积学报,1983,1(2):77-87.
[8]张秀莲.鲕粒在成岩作用中的次生变化及其意义[J].大庆石油地质与开发,1984(4):5-16.
[9]蒋小琼,管宏林,郑和荣,等.四川盆地普光气田飞仙关组白云岩储层成因探讨[J].石油实验地质,2014,36(3):332-336.
[10]苏立萍,罗平,胡社荣,等.川东北罗家寨气田下三叠统飞仙关组鲕粒滩成岩作用[J].古地理学报,2004,6(2):182-190.
[11]王恕一,蒋小琼,管宏林,等.川东北普光气田鲕粒白云岩储层粒内溶孔的成因[J].沉积学报,2010,28(1):10-16.
[12]薛晶晶,孙靖,朱筱敏,等.准噶尔盆地二叠系风城组白云岩储层特征及成因机理分析[J].现代地质,2012,26(4):755-761.
[13]伊硕,黄文辉,金振奎,等.哈萨克斯坦Zanazor油田石炭系KT-Ⅱ碳酸盐岩层成岩作用与孔隙演化[J].现代地质,2017,31(4):791-801.
[14]陈荣坤.埋藏环境下碳酸盐岩建设性成岩作用类型、特征及其意义[J].现代地质,1993,7(1):40-49.
[15]姜楠,范凌霄,刘卉,等.普光气田滩相储层特征及白云化成因[J].天然气地球科学,2013,24(5):923-930.
[16]张欣国,饶丹,蔡立国.普光气藏储层中鲕粒白云岩孔隙成因分析[J].天然气技术与经济,2009(2):11-13.
[17]景宇轩,刘建波,闫振,等.利用风暴沉积类型恢复海平面变化:以北京西山下苇甸剖面寒武纪中晚期风暴沉积为例[J].古地理学报,2015,17(5):653-668.
[18]黄宝春,周烑秀,朱日祥.从古地磁研究看中国大陆形成与演化过程[J].地学前缘,2008,15(3):348-359.
[19]金振奎,石良,高白水,等.碳酸盐岩沉积相及相模式[J].沉积学报,2013,31(6):965-979.
[20]冯增昭,陈继新,吴胜和.华北地台早古生代岩相古地理[J].沉积学报,1989,7(4):15-55.
[21]康世龙,邵龙义,易琦,等.京西下苇甸地区寒武系岩石特征及沉积环境研究[J].中国煤炭地质,2016,28(6):1-8.
[22]马永生,梅冥相,周润轩,等.层序地层框架下的鲕粒滩形成样式:以北京西郊下苇甸剖面寒武系第三统为例[J].岩石学报,2017,33(4):1021-1036.
[23]梅冥相.华北寒武系二级海侵背景下的沉积趋势及层序地层序列:以北京西郊下苇甸剖面为例[J].中国地质,2011,38(2):317-337.
[24]王成述,范开强,尹占国.北京西山中寒武统张夏组鲕粒特征及其环境意义[M]//中国地质科学院地质研究所.中国地质科学院地质研究所文集.北京:中国地质科学院地质研究所,1990:17.
[25]张旭,张宁,杨振鸿,等.北京西山下苇甸中寒武统碳酸盐岩微相及沉积相研究[J].地质科技情报,2009,28(6):25-30.
[26]朱筱敏.沉积岩石学[M].北京:石油工业出版社,2008:1-20.
[27]TUCKER M E,BATHURST R G C.New Interpretations of Great Salt Lake Ooids and of Ancient Non-Skeletal Carbonate Mineralogy[M].London:Blackwell Publishing Ltd,2009:497-537.
[28]祝海华,钟大康.四川盆地龙岗气田三叠系飞仙关组储集层特征及成因机理[J].古地理学报,2013,15(2):275-282.
[29]魏国齐,杨威,张林,等.川东北飞仙关组鲕滩储层白云石化成因模式[J].天然气地球科学,2005,16(2):162-166.
[30]高白水,金振奎,朱小二,等.哈萨克斯坦扎纳诺尔油田石炭系碳酸盐岩浅滩沉积模式及诸层质量差异机理[J].石油学报,2016,37(7):867-877.
[31]金振奎,邹元荣,张响响,等.黄骅坳陷古近系沙河街组湖泊碳酸盐沉积相[J].古地理学报,2002,4(3):11-18.
[32]邢延路,冯李强.北京西山下苇甸剖面寒武系徐庄组鲕粒研究[J].古地理学报,2015,17(4):517-528.
[33]周书欣.碳酸盐鲕粒的成因与鉴别[J].地质地球化学,1982(1):18-21.
[34]袁鑫鹏,刘建波.回流渗透模式白云岩研究历史与进展[J].古地理学报,2012,14(2):219-228.
[35]黄思静.碳酸盐岩的成岩作用[M].北京:地质出版社,2010:1-20.
[36]王英华.碳酸盐岩成岩作用与孔隙演化[J].沉积学报,1992,10(3):85-95.