南海北部陆坡海底火山活动对天然气水合物成藏的影响
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摘要
南海北部陆坡发育海底火山。海底火山的发育是否有利于天然气水合物的成藏是该区进行水合物勘探首先要考虑的一个关键问题。通过地震剖面解释、建立地质模型,并通过模型温度场计算,认为发生岩浆底侵时,高温岩浆使水合物稳定域的厚度变薄。随着热量的散失,水合物稳定域的厚度逐渐恢复。底侵的深度较浅时,水合物稳定域减薄的幅度增大,恢复周期变短。对海底火山喷发的情况,水合物稳定域将完全不存在,但其恢复的时间更短。岩浆底侵深度为6 km时,其对水合物稳定域的影响周期为1 Ma左右。南海北部东沙运动和流花运动都伴随着规模性的火山活动,两次构造运动期间岩浆侵入、侵出引起的热效应到目前为止已对该区水合物稳定域的发育没有影响,但海底火山活动对增大地层的孔隙与通道,从而对甲烷气体的运聚和水合物的成藏都能起到积极的作用。火山活动引起的高地温梯度,对生物甲烷的产生也将起到一定的帮助,从而有利于水合物的形成。南海北部陆坡火山区仍是天然气水合物勘探的有利靶区。
There are volcanoes developed on the northern South China Sea slope.The influence on gas hydrates formation produced by those volcanic activities is the key problem which should be considered first before field exploration conducted.Based on seismic line interpretation and geological thermal model calculation,this paper concluded that the thickness of gas hydrates stability zone would be influenced by magma intrusion.The shallower the magma intrusion depth is,the bigger the influence to the thickness of the gas hydrates stability zone is,but the shorter the thickness of gas hydrates stability zone recover period time is.When volcanic eruption occurred on the seafloor,the gas hydrate stability zone would be destroyed totally at first,however,it would also recovered after a shortest period of time as comparing to the case of magma intrusion.As to the case of magma intrusion depth of 6 km,the total recover time for the gas hydrates stability zone is about 1Ma.There had been volcanic activities during both Dongsha movement and Liuhua movement.Up to now the influences on gas hydrates stability zone produced by those volcanic activities during those two tectonic movements have been disappeared.Finer sediment grain and lower porosity usually developed on slope area are unfavorable factors for the formation of gas hydrates.As the volcanic activity can both enlarge the sediment porosity and accelerate the migration and accumulation of methane in the slope environment,it can help for the formation of gas hydrates on the slope environment.On the other hand,the higher temperature introduced by magma intrusion will help for the formation of gas hydrates by stimulating the activity of methanogens and producing more methane.The volcanic mountain area of northern South China Sea slope is the favorable target area for gas hydrates exploration.
There are volcanoes developed on the northern South China Sea slope.The influence on gas hydrates formation produced by those volcanic activities is the key problem which should be considered first before field exploration conducted.Based on seismic line interpretation and geological thermal model calculation,this paper concluded that the thickness of gas hydrates stability zone would be influenced by magma intrusion.The shallower the magma intrusion depth is,the bigger the influence to the thickness of the gas hydrates stability zone is,but the shorter the thickness of gas hydrates stability zone recover period time is.When volcanic eruption occurred on the seafloor,the gas hydrate stability zone would be destroyed totally at first,however,it would also recovered after a shortest period of time as comparing to the case of magma intrusion.As to the case of magma intrusion depth of 6 km,the total recover time for the gas hydrates stability zone is about 1Ma.There had been volcanic activities during both Dongsha movement and Liuhua movement.Up to now the influences on gas hydrates stability zone produced by those volcanic activities during those two tectonic movements have been disappeared.Finer sediment grain and lower porosity usually developed on slope area are unfavorable factors for the formation of gas hydrates.As the volcanic activity can both enlarge the sediment porosity and accelerate the migration and accumulation of methane in the slope environment,it can help for the formation of gas hydrates on the slope environment.On the other hand,the higher temperature introduced by magma intrusion will help for the formation of gas hydrates by stimulating the activity of methanogens and producing more methane.The volcanic mountain area of northern South China Sea slope is the favorable target area for gas hydrates exploration.
引文
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[17]苏新,陈芳,陆红锋,等.南海北部深海甲烷冷泉自生碳酸盐岩显微结构特征与流体活动的关系[J].现代地质,2008,22(3):376-381.
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[22]龚再升,李思田,谢泰俊,等.南海北部大陆架边缘盆地分析与油气聚集[M].北京:科学出版社,1997:510.
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[24]徐世浙.地球物理中的有限单元法[M].北京:科学出版社,1994:287-296.
[25]栾锡武,高德章,喻普之,等.我国东海陆架地区新生代地层的热导率[J].海洋与湖沼,2002,33(2):151-159.
[26]栾锡武,赵一阳,秦蕴珊,等.我国东海陆架区新生代地层岩石生热率研究[J].沉积学报,2003,21(4):152-159.
[27]王良书,施央申.油气盆地地热研究[M].南京:南京大学出版社,1989:1-105.
[28]周惠兰.地球内部物理[M].北京:地震出版社,1990:167-213.
[29]Hyndman R D,Spence G D,Chapman R,et al.Geophysicalstudies of marine gas hydrate in northern Cascadia,natural gashydrates:Occurrence,distribution,and detection[J].AGUMonograph,2001,124:273-295.
[30]Schutter S R.Occurrences of hydrocarbons in and around igneousrocks[J].Geological Society of London,Special Publications,2003,214:35-68.
[31]刘嘉麒,孟凡超.火山作用与油气成藏[J].天然气工业,2009,29(8):1-4.
[32]邹才能,赵文智,贾承造.中国沉积盆地火山岩油气藏形成与分布[J].石油勘探与开发,2008,35(3):257-271.
[33]栾锡武.天然气水合物的上界面——硫酸盐还原-甲烷厌氧氧化界面[J].海洋地质与第四纪地质,2009,29(2):91-102.
[34]李平鲁.珠江口盆地新生代构造运动[J].中国海上油气(地质),1993,7(6):11-17.
[35]曾麟.南海珠江口盆地上新世末至更新世的一次构造运动[J].南海研究与开发,1994(2):1-8.
[36]邹和平.南海北部—台湾海峡及邻区新生代火山活动时序与分布[J].华东地质学院学报,1993,16(1):24-31.
[2]Fraday M.On the condendation of several gases into liquids[J].Philosophical Transactions,1823,113:189-198.
[3]Kvenvolden K A.Gas hydrate-goelogical perspective and globalchange[J].Review of Geophysics,1993,31:173-187.
[4]MacDonald G T.The future of methane as an energy resource[J].Annual Review of Energy,1990,15:53-83.
[5]Milkov A V,Claypool G E,Lee Y J,et al.In situ methaneconcentrations at Hydrate Ridge Offshore Oregon:newconstraintson the global gas hydrate inventory from an active margin[J].Geology,2003,31:833-836.
[6]栾锡武,赵克斌,孙冬胜,等.鄂霍次克海天然气水合物成藏条件分析[J].海洋地质与第四纪地质,2006,26(6):91-100.
[7]Ludmann T,Wong H K.Characteristics of gas hydrate occur-rences associated with mud diapirism and gas escape structures inthe northwestern Sea of Okhotsk[J].Marine Geology,2003,201:269-286.
[8]Shakirov R,Obzhirov A,Suess E.Mud volcanoes and gas ventsin the Okhotsk Sea area[J].Geo-Marine Letters,2004,24:140-149.
[9]陈忠,颜文,陈木宏.南海北部大陆坡冷泉碳酸盐结核的发现:海底天然气渗漏活动的新证据[J].科学通报,2006,51(9):1065-1072.
[10]栾锡武,赵克斌,Obzhirov A,等.鄂霍次克海浅表层天然气水合物的勘查识别和基本特征[J].中国科学:D辑,2008,38(1):99-107.
[11]栾锡武,岳保静,Obzhirov A.浅表层天然气水合物区的海底地形特征——以鄂霍次克海为例[J].现代地质,2008,22(3):420-429.
[12]姚伯初,万玲,曾维军.中国南海海域岩石圈结构及演化[M].北京:地质出版社,2006:223.
[13]黄永样,Suess E,吴能友.南海北部陆坡甲烷和天然气水合物地质——中德合作SO-177航次成果专报[M].北京:地质出版社,2008:197.
[14]陈忠,杨华平,黄奇瑜,等.南海东沙西南海域冷泉碳酸盐特征及意义[J].现代地质,2008,22(3):382-389.
[15]祝有海,吴必豪,罗续荣,等.南海沉积物中烃类气体(酸解烃)特征及其成因来源[J].现代地质,2008,22(3):407-414.
[16]陆敬安,杨胜雄,吴能友,等.南海神狐海域天然气水合物地球物理测井评价[J].现代地质,2008,22(3):447-451.
[17]苏新,陈芳,陆红锋,等.南海北部深海甲烷冷泉自生碳酸盐岩显微结构特征与流体活动的关系[J].现代地质,2008,22(3):376-381.
[18]栾锡武,彭学超,邱燕.南海北部陆坡高速堆积体的构造成因[J].现代地质,2009,23(2):183-199.
[19]庞雄,陈长民,彭大钧,等.南海珠江深水扇系统及油气[M].北京:科学出版社,2007:361.
[20]朱伟林,张功成,杨少坤,等.南海北部大陆边缘盆地天然气地质[M].北京:石油工业出版社,2007:391.
[21]何家雄,刘海龄,姚永坚,等.南海北部边缘盆地油气地质及资源前景[M].北京:石油工业出版社,2008:185.
[22]龚再升,李思田,谢泰俊,等.南海北部大陆架边缘盆地分析与油气聚集[M].北京:科学出版社,1997:510.
[23]Wang P X,Prell W L,Blum P,et al.Proceedings of the OceanDrilling Program,Initial Reports of South China Sea[M].Col-lege Station,TX:Ocean Drilling Program,2000,184:18-20.
[24]徐世浙.地球物理中的有限单元法[M].北京:科学出版社,1994:287-296.
[25]栾锡武,高德章,喻普之,等.我国东海陆架地区新生代地层的热导率[J].海洋与湖沼,2002,33(2):151-159.
[26]栾锡武,赵一阳,秦蕴珊,等.我国东海陆架区新生代地层岩石生热率研究[J].沉积学报,2003,21(4):152-159.
[27]王良书,施央申.油气盆地地热研究[M].南京:南京大学出版社,1989:1-105.
[28]周惠兰.地球内部物理[M].北京:地震出版社,1990:167-213.
[29]Hyndman R D,Spence G D,Chapman R,et al.Geophysicalstudies of marine gas hydrate in northern Cascadia,natural gashydrates:Occurrence,distribution,and detection[J].AGUMonograph,2001,124:273-295.
[30]Schutter S R.Occurrences of hydrocarbons in and around igneousrocks[J].Geological Society of London,Special Publications,2003,214:35-68.
[31]刘嘉麒,孟凡超.火山作用与油气成藏[J].天然气工业,2009,29(8):1-4.
[32]邹才能,赵文智,贾承造.中国沉积盆地火山岩油气藏形成与分布[J].石油勘探与开发,2008,35(3):257-271.
[33]栾锡武.天然气水合物的上界面——硫酸盐还原-甲烷厌氧氧化界面[J].海洋地质与第四纪地质,2009,29(2):91-102.
[34]李平鲁.珠江口盆地新生代构造运动[J].中国海上油气(地质),1993,7(6):11-17.
[35]曾麟.南海珠江口盆地上新世末至更新世的一次构造运动[J].南海研究与开发,1994(2):1-8.
[36]邹和平.南海北部—台湾海峡及邻区新生代火山活动时序与分布[J].华东地质学院学报,1993,16(1):24-31.
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