粤北丹霞盆地晚白垩世丹霞组锦石岩段钙质泥岩 C-O同位素特征及其环境意义
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摘要
丹霞山是"中国丹霞"世界自然遗产的典型代表,目前对成景地层-上白垩统丹霞组沉积环境的研究程度不高,尤其对丹霞组锦石岩段沉积环境还存在争议。文中利用沉积学和稳定同位素地球化学方法,对丹霞山丹霞组锦石岩段钙质泥岩进行研究,分析该套泥岩沉积时期的古环境和古气候。粤北丹霞盆地丹霞组锦石岩寺段钙质泥岩的δ~(13)C_(PDB)值在-3.34‰～-2.0‰之间,平均值为-2.49‰,δ~(18)O_(PDB)值在-8.9‰～-5.7‰之间,平均值为-7.28‰。盐度值Z平均为119,在中国典型湖相碳酸盐岩碳氧同位素分布图中,样品主要投点于四川盆地侏罗系大安寨段和青藏高原北部的湖相碳酸盐岩中,预示着其可能形成于咸水-半咸水的陆相湖泊体系中。其古水温为19～34℃,平均为26℃之间。在75Ma,丹霞盆地大气CO_2浓度为1009～1436ppmv,平均为1282ppmv。丹霞盆地晚白垩世锦石岩寺段时期,具有干燥的地表沉积环境,可能与晚白垩世中期Campanian期东亚中纬度地区的干旱古气候条件相关。
Danxiashan is a typical representative of the world's natural heritage-"China Danxia". The study on the sedimentary environment of the Upper Cretaceous Danxia formation is not deep, especially for Jinshiyansi section of Danxia formation. In this research, the calcareous mudstone in Jinshiyan section of Danxia formation was studied by means of sedimentology and stable isotope geochemistry. The value of δ~(13)C_(PDB) of the calcareous mudstone in the Jinshiyansi section is between-3.34‰ and-2.0‰, with an average value of -2.49‰; the value of δ~(18)O_(PDB) is between-8.9‰ and -5.7‰, with an average value of -7.28‰. The salinity value Z is 119 on average. In the carbon and oxygen isotope distribution map of typical lacustrine carbonate rocks in China, the samples are mainly taken in the range of the lacustrine carbonate rocks in the Jurassic Daanzhai section in Sichuan basin and the northern part of Qinghai-tibet plateau, indicating that they developed in the saltwater or semi-saltwater lake system. The ancient water temperature is between 19 and 34℃, with an average of 26℃. At 75 Ma, the atmospheric concentration of CO_2 in Danxia basin was 1009～1436 ppmv, with an average of 1282 ppmv. In the Jinshiyansi period of the late Cretaceous, Danxia basin had a dry surface sedimentary environment which may be related to the arid paleoclimate conditions in the middle latitude region of East Asia in Campanian period.
Danxiashan is a typical representative of the world's natural heritage-"China Danxia". The study on the sedimentary environment of the Upper Cretaceous Danxia formation is not deep, especially for Jinshiyansi section of Danxia formation. In this research, the calcareous mudstone in Jinshiyan section of Danxia formation was studied by means of sedimentology and stable isotope geochemistry. The value of δ~(13)C_(PDB) of the calcareous mudstone in the Jinshiyansi section is between-3.34‰ and-2.0‰, with an average value of -2.49‰; the value of δ~(18)O_(PDB) is between-8.9‰ and -5.7‰, with an average value of -7.28‰. The salinity value Z is 119 on average. In the carbon and oxygen isotope distribution map of typical lacustrine carbonate rocks in China, the samples are mainly taken in the range of the lacustrine carbonate rocks in the Jurassic Daanzhai section in Sichuan basin and the northern part of Qinghai-tibet plateau, indicating that they developed in the saltwater or semi-saltwater lake system. The ancient water temperature is between 19 and 34℃, with an average of 26℃. At 75 Ma, the atmospheric concentration of CO_2 in Danxia basin was 1009～1436 ppmv, with an average of 1282 ppmv. In the Jinshiyansi period of the late Cretaceous, Danxia basin had a dry surface sedimentary environment which may be related to the arid paleoclimate conditions in the middle latitude region of East Asia in Campanian period.
引文
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[35]曹珂.胶莱盆地晚白垩世辛格庄组钙质结核的碳、氧同位素特征[J].矿物岩石,2014,34(2):85-90.
[36]Hong S K,Lee Y I.Evaluation of atmospheric carbon dioxide concentrations during the Cretaceous[J].Earth and Planetary Science Letters,2002,327-328:33-38.
[2]Wu C,Liu C,Shen L,Wang J,et al.A cretaceous desert-playa sedimentary system controlled the potash formation in the Simao basin[J].Acta Geologica Sinica( Eenglish Edition),2017,91(3):1143-1144.
[3]Hasegawa H,Tada R,Jiang X,et al.Drastic shrinking of the Hadley circulation during the mid-cretaceous super-greenhouse[J].Climate of the Past Discussion,2012,7(1):119-151.
[4]陈丕基.晚白垩世中国东南沿岸山系与中南地区的沙漠和盐湖化[J].地层学杂志,1997,21(3):203-213.
[5]徐行,葛同明,肖晖.丹霞盆地红层时代的初探-古地磁研究的新证据[J].成都地质学院学报,1990,17(2):79-86.
[6]张显球,林小燕.粤北丹霞盆地白垩系长坝组的介形类动物群[J].微体古生物学报,2013,30(1):58-86.
[7]陈方举.贝尔凹陷南屯组钙质泥岩地质成因及其石油地质意义[J].东北石油大学学报,2015,39(2):42-50.
[8]Coplen T B,Kendall C,Hopple J.Comparison of stable isotope reference samples[J].Nature,1983,302:236-238.
[9]李儒峰,刘本培.碳氧同位素与碳酸盐岩层序地层学关系研究-以黔南马平组为例[J].地球科学,1996,31(3):261-266.
[10]曲长胜,邱隆伟,杨勇强,等.吉木萨尔凹陷芦草沟组碳酸盐岩碳氧同位素特征及其古湖泊学意义[J].地质学报,2017,91(3):605-616.
[11]王英华,周书欣,张秀莲.中国湖相碳酸盐岩[M].北京:中国矿业大学出版社,1993.
[12]刘传联,赵泉鸿,汪品先.湖相碳酸盐氧碳同位素的相关性与生油古湖泊类型[J].地球化学,2001,30(4):363-367.
[13]柳益群,周鼎武,焦鑫,等.一类新型沉积岩:地幔热液喷积岩-以中国新疆三塘湖地区为例[J].沉积学报,2013,31(5):773-781.
[14]Keith A L,Weber J N.Carbon and oxygen isotopic composition of selected limestone and fossils[J].Geochimica et Cosmochimica Acta,1964,18(10-11):1787-1816.
[15]Yu H Y,Li W,Qin X Y,et al.Gas and water distribution of Ordovician Majiagou Formation in northwest of Ordos Basin,NW China[J].Petroleum Exploration and Development,2016,43(3):435-442.
[16]罗顺社,吕奇奇,席明利,等.湘北九溪、沅古坪下奥陶统等深岩类型、碳氧同位素特征及沉积环境[J].石油与天然气地质,2015,36(5):745-755.
[17]苏玲,朱如凯,崔景伟,等.中国湖相碳酸盐岩时空分布与碳氧同位素特征[J].古地理学报,2017,19(6):1063-1074.
[18]张秀莲.碳酸盐岩中氧、碳稳定同位素与古盐度、古水温的关[J].沉积学报,1985,3(4):17-29.
[19]赵艳军,刘成林,张华,等.古盐湖卤水温度对钾盐沉积的控制作用探讨[J].岩石学报,2015,31(9):2751-2756.
[20]宋立军,刘池阳,赵红格,等.鄂尔多斯西南部待建纪黄旗口期和王全口期原盆面貌及其成因机制分析[J].地学前缘,2016,23(5):221-234.
[21]Coplen T.Stable isotope hydrology,deuterium and oxygen-18 in the water cycle[J].Eos Transactions American Geophysical Union,2013,63(45):861-862.
[22]郑淑蕙.稳定同位素地球化学分析[M].北京:北京大学出版社,1986.
[23]邵龙义.碳酸盐岩氧、碳同位素与古温度等的关系[J].中国矿业大学学报,1994,23(1):39-45.
[24]陈军明,赵平,王成善,等.晚白垩世(80Ma)东亚气候的数值模拟[J].地学前缘,2009,16(6):226-238.
[25]杨卫东,陈南生,倪师,等.白垩纪红层碳酸盐岩和恐龙蛋壳碳氧同位素组成及环境意义[J].科学通报,1993,38(23):2161-2163.
[26]Médard T,Simon-Coin.Palaeoweathering,palaeosurfaces and related continental deposits[J].Geobios,2000,33(2):232.
[27]Ekart D D,Cerling T E,Montoez I P,et al.A 400 million year carbon isotope record of pedogenic carbonate:implications for paleoatmospheric carbon dioxide[J].American Journal of Science,1999,299(10):805-827.
[28]Arens N C,Jahren A H,Amundson R.Can C3 plants faithfully record the carbon isotopic composition of atmospheric carbon dioxide?[J].Paleobiology,2000,26(1):137-164.
[29]Breecker D O,Sharp Z D,McFadden L D.Seasonal bias in the formation and stable isotopic composition of pedogenic carbonate in modern soils from central New Mexico,USA[J].Geological Society of America Bulletin,2009,121(3-4):630-640.
[30]Quan C,Sun C L,Sun Y W,et al.High resolution estimates of paleo-CO2 levels through the Campanian( Late Cretaceous) based on Ginkgo cutide[J].Cretaceous Research,2009,30(2):424-428.
[31]Berner R A.GEOCARB II:A revised model of atmospheric CO2 over phanerozoic time[J].American Journal of Science,1994,294(2):56-91.
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[33]刘立新,周凌晞,张晓春,等.我国4个国家级本底站大气CO2浓度变化特征[J].中国科学(D辑:地球科学),2009,39(2):222-228.
[34]Li X H,Xu W L,Liu W H,et al.Climatic and environmental indications of carbon and oxygen isotopes from the Lower Cretaceous calcrete and lacustrine carbonates in Southeast and Northwest China[J].Palaeogeography Palaeoclimatology Palaeoecology,2013,385:171-189.
[35]曹珂.胶莱盆地晚白垩世辛格庄组钙质结核的碳、氧同位素特征[J].矿物岩石,2014,34(2):85-90.
[36]Hong S K,Lee Y I.Evaluation of atmospheric carbon dioxide concentrations during the Cretaceous[J].Earth and Planetary Science Letters,2002,327-328:33-38.
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