东印度洋中部缺氧区的季节变化特征
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摘要
依据2013春、2016夏、2016秋三季在东印度洋中部开展的水体综合调查资料,研究东印度洋中部缺氧区(ρ_(DO)<2mg/L)的季节变化。结果表明:垂向分布上,缺氧区上边界一般位于水深100～150 m,厚度春季最厚、秋季次之、夏季最薄。平面分布上,春季缺氧区范围最大,主要位于89°00′E以东海区,其南端越过赤道向南扩展至1°12′S;夏季缺氧区的南端退缩至赤道以北海域,且分布面积最小;秋季缺氧区东西向的位置与春季相反,主要位于赤道91°00′E以西海域,其南向扩展范围可达赤道附近。从氧跃层强度来看,赤道附近氧跃层强度最强,由此向南、向北氧跃层强度逐渐减弱,与温跃层变化一致。研究表明,东印度洋中部缺氧区源于孟加拉湾缺氧区的南扩,季风性环流变化是缺氧区扩展范围季节变化的主要控制因素,有机碎屑的分解耗氧和高强度的水柱层化是缺氧区得以形成和维持的重要保障。
Based on the comprehensive survey data in spring,summer and autumn in 2013 and 2016,the seasonal variation of the hypoxic zone(ρ_(DO)<2 mg/L)in the central East Indian Ocean is investigated.The results show that in the vertical profile,the upper of boundary the hypoxic zone is generally located between depth of 100～150 m,it is the thickest in spring,followed by the autumn,and the thinnest in summer.In the horizontal distribution,the area of hypoxic zone in spring is the largest,mainly located in the east of 89°E,and its southern boundary extends southward across the equator to 1.2°S.However,in summer,the boundary of hypoxic zone contracts to the north of the equator,with the smallest distribution area.The position of hypoxic zone is mainly located in the west of 91°E in autumn,which is just opposite to that in spring,and its southern boundary extends southward near the equator.The most intense oxycline is found near the equator,but it gradually weakens toward the north and the south,being consistent with that of the thermocline.The hypoxic zone in the central East Indian Ocean is derived from the southward extension of the hypoxic zone in the Bay of Bengal.The change of the monsoon circulation is the main driving force for the seasonal variation of the hypoxic zone,and the oxygen consumption of organic debris together with the intensive water column stratification are the important guarantee for the formation and maintenance of the hypoxic zone.
Based on the comprehensive survey data in spring,summer and autumn in 2013 and 2016,the seasonal variation of the hypoxic zone(ρ_(DO)<2 mg/L)in the central East Indian Ocean is investigated.The results show that in the vertical profile,the upper of boundary the hypoxic zone is generally located between depth of 100～150 m,it is the thickest in spring,followed by the autumn,and the thinnest in summer.In the horizontal distribution,the area of hypoxic zone in spring is the largest,mainly located in the east of 89°E,and its southern boundary extends southward across the equator to 1.2°S.However,in summer,the boundary of hypoxic zone contracts to the north of the equator,with the smallest distribution area.The position of hypoxic zone is mainly located in the west of 91°E in autumn,which is just opposite to that in spring,and its southern boundary extends southward near the equator.The most intense oxycline is found near the equator,but it gradually weakens toward the north and the south,being consistent with that of the thermocline.The hypoxic zone in the central East Indian Ocean is derived from the southward extension of the hypoxic zone in the Bay of Bengal.The change of the monsoon circulation is the main driving force for the seasonal variation of the hypoxic zone,and the oxygen consumption of organic debris together with the intensive water column stratification are the important guarantee for the formation and maintenance of the hypoxic zone.
引文
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[2]PAULMIER A,RUIZ-PINO D.Oxygen minimum zones(OMZs)in the modern ocean[J].Progress in Oceanography,2009,80(3):113-128.
[3]MCCREARY J P,YU Z,HOOD R R,et al.Dynamics of the Indian-Ocean oxygen minimum zones[J].Progress in Oceanography,2013,112-113(2):15-37.
[4]BOYER T P,LEVITUS S,ANTONOY J I,et al.Coauthors,2006:World Ocean Database 2005[J].NOAA Atlas NESDIS,2006,60:190.
[5]WYRTKI K.The oxygen minima in relation to ocean circulation[C]∥Deep Sea Research and Oceanographic Abstracts.Cambridge,USA:Cambridge University Press,1962,9(1-2):11-23.
[6]WYRTKI K.Physical oceanography of the Indian Ocean[M]∥The biology of the Indian Ocean.Germany:Springer Berlin,Heidelberg,1973:18-36.
[7]KAMYKOWSKI D,ZENTARA,S J.Hypoxia in the world ocean as recorded in the historical data set[J].Deep-Sea Research,1990,37:1861-1874.
[8]YIN L.On the India Ocean development strategy and regional non-traditional security issues cooperation mechanism of China[J].Academic Exploration,2015(5):31-35.尹仑.21世纪海上丝绸之路与“环印度洋战略”研究[J].学术探索,2015(5):31-35.
[9]FENG C L.The logic behind China's westward strategy in the Indian Ocean[J].Pacific Journal,2016,24(3):76-84.冯传禄.中国“西进”印度洋的战略逻辑[J].太平洋学报,2016,24(3):76-84.
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[11]LI H L,CHEN J F,LU Y,et al.Seasonal variation of DO and formation mechanism of bottom water hypoxia of Changjiang River Estuary[J].Journal of Marine Sciences,2011,29(3):78-87.李宏亮,陈建芳,卢勇,等.长江口水体溶解氧的季节变化及底层低氧成因分析[J].海洋学研究,2011,29(3):78-87.
[12]WEI Q S,WEI X H,XIE L P,et al.Features of dissolved oxygen distribution and its effective factors in the southern Yellow Sea in Spring,2007[J].Advances in Marine Science,2010,28(2):179-185.韦钦胜,魏修华,谢琳萍,等.2007年春季南黄海溶解氧的分布特征及影响因素[J].海洋科学进展,2010,28(2):179-185.
[13]WEI Q S,WANG B D,CHEN J F,et al.Recognition on the forming-vanishing process and underlying mechanisms of the hypoxia off the Yangtze River estuary[J].Scientia Sinica Terra,2015,58(4):628-648.韦钦胜,王保栋,陈建芳,等.长江口外缺氧区生消过程和机制的再认知[J].中国科学:地球科学,2015,58(4):628-648.
[14]ZHANG Z,ZHANG Z F,HAN G C,et al.Spatio-temporal variation,formation and transformation of the hypoxia area off the Yangtze River Estuary[J].Marine Environmental Science,2012,4(3):469-473.张哲,张志锋,韩庚辰,等.长江口外低氧区时空变化特征及形成、变化机制初步探究[J].海洋环境科学,2012,4(3):469-473.
[15]XUAN L L,QIU Y,XU J D,et al.Seasonal variation of surface-layer circulation in the eastern tropical Indian Ocean[J].Journal of Tropical Oceanography,2014,33(1):26-35.宣莉莉,邱云,许金电,等.热带东印度洋表层环流季节变化特征研究[J].热带海洋学报,2014,33(1):26-35.
[16]QIAO B,LIU Z Z,ZHANG S Y,et al.Equatorial current system structure and hydrologic characteristics in monsoonal wind transition period[J].Advances in Marine Science,2014,32(3):301-305.乔彬,刘子洲,张书颖,等.季风转换期东印度洋的赤道流系结构和水文特征[J].海洋科学进展,2014,32(3):301-305.
[17]ZAHNG W Q.Spatial Distributions of biogenic elements and their influencing factors in the East Indian Ocean in Spring[D].Qingdao:The First Institute of Oceanography,SOA,2016.张文全.春季东印度洋生源要素的分布特征及其影响因素[D].青岛:国家海洋局第一海洋研究所,2016.
[18]XUAN L L,QIU Y,XU J D,et al.Seasonal variation of the water exchange between the Bay of Bengal and the equatorial eastern Indian Ocean[J].Journal of Tropical Oceanography,2015,34(6):26-34.宣莉莉,邱云,许金电,等.孟加拉湾与赤道东印度洋水交换的季节变化特征[J].热带海洋学报,2015,34(6):26-34.
[19]WYRTKI K.An equatorial jet in the Indian Ocean[J].Science,1973,181(4096):262-264.
[20]LIN L,GAO L B.Vertical structure of the low level atmosphere around the southeast Indian Ocean Fronts[J].Chinese Journal of Polar Research,2012,24(2):136-142.刘琳,高立宝.东南印度洋海洋锋面处低空大气的垂向分布结构[J].极地研究,2012,24(2):136-142.
[21]YUAN C.Characteristics of chlorophyll a,primary productivity and photosynthetic fluorescence in the East Tropical Indian Ocean during the boreal spring inter-mosoon[D].Qingdao:The First Institute of Oceanography,SOA,2015.袁超.春季季风间期热带东印度洋叶绿素a、初级生产力与光合荧光特征[D].青岛:国家海洋局第一海洋研究所,2015.
[22]REDFIED A C.The influence of organisms on the composition of seawater[J].The Sea,1963,2:26-77.
[23]ZHAI W D,ZHAO H D,ZHENG N,et al.Coastal acidification in summer bottom oxygen-depleted waters in northwestern-northern Bohai Sea from June to August in 2011[J].Chinese Science Bulletin,2012,57(9):753-758.翟惟东,赵化德,郑楠.2011年夏季渤海西北部、北部近岸海域的底层耗氧与酸化[J].科学通报,2012,57(9):753-758.