南黄海盆地碳酸盐岩碳氧同位素特征及意义

郑仰帝; 蔡进功

doi:10.11781/sysydz201303307

南黄海盆地碳酸盐岩碳氧同位素特征及意义

doi: 10.11781/sysydz201303307

郑仰帝,
蔡进功^,

同济大学海洋地质国家重点实验室, 上海 200092

基金项目: 中国自然科学基金(41072089);国家油气重大专项(2011ZX05023-003-003)资助.

详细信息

作者简介:
郑仰帝(1987- ),男,硕士研究生,石油地质学专业.E-mail:zhengyangdi1987@126.com.

通讯作者:
蔡进功(1961- ),男,教授,博士生导师,海洋沉积学和石油地质学专业.E-mail:jgcai@tongji.edu.cn.

中图分类号: TE122.1⁺13
计量
- 文章访问数: 1402
- HTML全文浏览量: 86
- PDF下载量: 634
- 被引次数: 0
出版历程
- 收稿日期: 2012-08-03
- 修回日期: 2013-04-17
- 刊出日期: 2013-05-28

Characteristics of carbon and oxygen isotopes of carbonate rocks in South Yellow Sea Basin and their implication

Zheng Yangdi,
Cai Jingong^,

State Key Laboratory of Marine Geology, Tongji University, Shanghai 200092, China

摘要

摘要: 对南黄海盆地碳酸盐岩烃源岩(P₁q-T₁q)进行了碳氧同位素测定及孢粉相等分析,研究海相碳酸盐岩有效烃源岩的形成和控制因素.通过对样品δ¹³C与δ¹⁸O相关性等的分析,发现碳氧同位素组成基本保留了原始海洋的同位素组成.栖霞组δ¹³C相对青龙组偏重,预示着较高的生物生产力,更有利于烃源岩的发育.栖霞组δ¹³C以均值为基准可以划分为3个演化阶段,并与孢粉相的变化相对应,表明不同层段烃源岩发育具有差异性.WX5-ST1井青龙组δ¹³C_PDB(均值3.83‰)明显比CZ24-1-1井(均值-1.34‰)的偏重,并与高无定形孢粉相相对应,表明同一层段不同区域烃源岩形成也具有差异性.对比碳氧同位素和孢粉相资料,发现生物生产力与保存条件有效的匹配是烃源岩发育的有利层段.
- 生物生产力 /
- 保存条件 /
- 孢粉相 /
- 碳氧同位素 /
- 烃源岩 /
- 碳酸盐岩 /
- 南黄海盆地
Abstract: Based on the analyses of carbon and oxygen isotope composition and palynofacies of carbonate source rocks (P₁q-T₁q) from the South Yellow Sea Basin,the formation and controlling factors of effective source rocks of marine facies were studied.The correlation between δ¹³C and δ¹⁸O indicated that the carbon and oxygen carbon isotope compositions were similar to those in original ocean.The δ¹³C_PDB values in P₁q were heavier than those in T₁q,indicating for higher biological productivity,which was favorable for source rock generation.Based on mean value,the δ¹³C_PDB values of P₁q were divided into 3 evolution stages corresponding to the changes of palynofacies,indicating that the formation of source rocks varied among different layers.The δ¹³C_PDB values in P₁q from well WX5-ST1 were 3.83‰ in average,obviously heavier than those from well CZ24-1-1 (-1.34‰ in average).It corresponded to the high content of amorphous organic matter,and proved the differences of source rock formation among different regions in the same layer.The comparison of carbon and oxygen isotopes and palynofacies showed that the effective matching of biological productivity and preservation condition was favorable for source rock formation.
- biological productivity /
- preservation condition /
- palynofacies /
- carbon and oxygen isotopes /
- source rock /
- carbonate rock /
- South Yellow Sea Basin

HTML全文

参考文献(25)

[1]	刘峰,蔡进功,吕炳全,等.巢湖地区栖霞组碳酸盐烃源岩的形成及影响因素[J].中国科学:地球科学,2011,41(6):873-886.
[2]	张水昌,张宝民,边立曾,等.中国海相烃源岩发育控制因素[J].地学前缘,2005,12(3):39-48.
[3]	Hatch J R,Jacobson S R,Witzke B J,et al.Possible late Middle Ordovician organic carbon isotope excursion:Evidence from Ordovician oils and hydrocarbon source rocks,Mid-Continent and east-central United States[J].AAPG Bulletin,1987,71(11):1342-1354.
[4]	Wang K,Chatterton B D E,Wang Y.An organic carbon isotope record of Late Ordovician to Early Silurian marine sedimentary rocks,Yangtze Sea,South China:Implications for CO₂ changes during the Hirnantian glaciation[J].Palaeogeography,Palaeoclimatology,Palaeoecology,1997,132(2):147-158.
[5]	王大锐,冯晓杰.渤海湾地区下古生界碳氧同位素地球化学研究[J].地质学报,2002,76(3):400-408.
[6]	腾格尔,刘文汇,徐永昌,等.海相地层无机参数与烃源岩发育环境的相关研究:以鄂尔多斯盆地为例[J].石油与天然气地质,2005,26(4):411-421.
[7]	胡芬.南黄海盆地海相中、古生界油气资源潜力研究[J].海洋石油,2010,30(3):1-8.
[8]	范小林.南黄海盆地海相领域油气勘探战略思考[J].海洋油气地质,2001,6(4):35-40.
[9]	左景勋,童金南,邱海鸥,等.下扬子地区早三叠世碳酸盐岩碳同位素组成的演化特征[J].中国科学:地球科学,2006,36(2):109-122.
[10]	Qing Hairong,Veizer J.Oxygen and carbon isotopic composition of Ordovician brachiopods:implications for coeval seawater[J].Geochimica et Cosmochimica Acta,1994,58(20):4429-4442.
[11]	Derry L A,Kaufman A J,Jacobsen S B.Sedimentary cycling and environmental change in the Late Proterozoic:evidence from stable and radiogenic isotopes[J].Geochimica et Cosmochimica Acta,1992,56:1317-1329.
[12]	Kaufman A J,Jacobsen S R,Knoll A H.The Vendian record of Sr and C isotopic variations in seawater:implications for tecto-nics and paleoclimate[J].Earth and Planetary Science Letters,1993,120:409-430.
[13]	Derry L A,Brasier M D,Corfield R M,et al.Sr and C isotopic in Lower Cambrian carbonates from the Siberian Craton:a paleoenvironmental record during the Cambrian explosion[J].Earth and Planetary Science Letters,1994,128:671-681.
[14]	Kaufman A J,Knoll A H,Narbonne G M.Isotopes,ice ages and terminal Proterozoic earth history[J].Preceedings of the National Academy of Sciences of the United States of America,1997,94(3):6600-6605.
[15]	Keith M L,Weber J N.Carbon and oxygen isotopic composition of selected limestones and fossils[J].Geochimica et Cosmochimica Acta,1964,28(10/11):1787-1816.
[16]	张水昌,WANG R L,金之钧,等.塔里木盆地寒武纪—奥陶纪优质烃源岩沉积与古环境变化的关系:碳氧同位素新证据[J].地质学报,2006,80(3):459-466.
[17]	Demaison G J,Moore G T.Anoxic environments and oil source bed genesis[J].AAPG Bulletin,1980,64:1179-1209.
[18]	Tyson R V.The genesis and palynofacies characteristics of marine petroleum source rocks[M]//Fleeta J.Marine petroleum source rocks.Oxford:Geological Society Special Publication,1987:47-67.
[19]	Lynne E,Ibach J.Relationship between sedimentation rate and total organic carbon content in ancient marine sediments[J].AAPG Bulletin,1982,66:170-188.
[20]	陈践发,张水昌,孙省利,等.海相碳酸盐岩优质烃源岩发育的主要影响因素[J].地质学报,2006,80 (3):467-472.
[21]	Vanaover C L,Humphris S E,Fornari D,et al.Biogeography and ecological setting of Indian Ocean hydrothermal vents[J].Science,2001,294:818-823.
[22]	Huc A Y.Paleogeography,Paleoclimate and Source Rocks[M].Tulsa,USA:AAPG,1995.
[23]	Müller P J,Suess E.Productivity sedimentation rate and sedimentary organic matter in the oceans-I.Organic carbon preservation//Deep Sea Research Part A.Oceanographic Research Papers.:Elsevier,1979:1347-1362.
[24]	Clavert S E.Oceangraphic controls on the accumulation of organic matter in marine sediments//Brook J,Fleet A J,eds.Marine Petroleum Source Rock.London:Blackwell Scientific,1987:137-151.
[25]	Pedersen T F,Calvert S E.Anoxia vs productivity:what controls the formation of organic-carbon-rich sediments and sedimentary rock?[J].AAPG Bulletin,1990,74:454-466.