Carbon and oxygen isotope stratigraphy of the oxfordian carbonate rocks in Amu Darya basin
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- 作者：Rongcai Zheng (1315)
Yanghui Pan (1315) (2315)
Can Zhao (1315)
Lei Wu (3315)
Renjin Chen (3315)
Rui Yang (3315) - 关键词：carbon and oxygen stable isotope ; geochemistry ; isotope stratigraphic curve ; depositional environment ; diagenetic information ; Oxfordian ; Amu Darya Basin
- 刊名：Journal of Earth Science
- 出版年：2013
- 出版时间：February 2013
- 年：2013
- 卷：24
- 期：1
- 页码：42-56
- 全文大小：921KB
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Yanghui Pan (1315) (2315)
Can Zhao (1315)
Lei Wu (3315)
Renjin Chen (3315)
Rui Yang (3315)
1315. State Key Laboratory of Oil and Gas Reservoir Geology and Exploitation, Chengdu University of Technology, Chengdu, 610059, China
2315. Sichuan Nuclear Geology Institute, Chengdu, 610061, China
3315. CNPC International (Turkmenistan), Ashgabat, 744020, Turkmenistan - ISSN：1867-111X
文摘
Based on the detailed research on petrologic and geochemical characteristics of deposition and diagenesis of Oxfordian carbonate rocks in Amu Darya Basin, Turkmenistan, carbon and oxygen isotopes were analyzed. The results show that the paleoenvironmental evolution reflected by the samples with well-preserved original carbon isotopes coincides with the carbon-isotope stratigraphic curve and is almost consistent with the global sea-level curve, the Mid-Oxfordian wide transgression, and the positive carbon-isotope excursion event. The Mid-Oxfordian continuing transgression not only laid the foundation for the development of the Oxfordian reef and shoal reservoirs in Amu Darya Basin but also provided an example for the Oxfordian global transgression and the resulting development of reefs and banks and high-speed organic carbon burial events. The response of oxygen isotopes in diagenetic environment showed that micrite limestones and granular limestones underwent weak diagenetic alteration, and the samples largely retained the original seawater features. Dolomitization and the precipitation of hydrothermal calcites filling solution vugs and fractures before hydrocarbon accumulation occurred in a closed diagenetic environment where the main controlling factor is the temperature, and the diagenetic fluids were from the deep hot brine. The chalkification of the limestones after hydrocarbon accumulation occurred in the oilfield water systems.