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东亚季风湿润区水分收支的气候特征
Climate Characteristics of Moisture Budget in Humid Region Affected by East Asian Monsoon
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摘要: 采用1958—2007年NCEP/NCAR月平均再分析资料，分别从水汽通量、水汽通量散度以及区域内降水量与蒸发量差计算东亚季风湿润区的水分收支，分析其差异特征，结果表明：用不同方法计算的水分收支距平年际变化的相关系数分别为0.91，0.71和0.81，误差ε百分率分别为17.4%，44.1%和44%，其中利用水汽通量和散度计算得到的季风湿润区水分收支结果很接近。总体上看，整个区域全年表现为水分收入，春季和夏季的水分收入贡献最大，秋季和冬季贡献较小。在水汽经向输送中，南边界为主要的水汽输入区。从水汽输送计算的水分收支垂直分布来看，多年平均气候态下整个区域除850 hPa存在水分支出外，其余各层均为水分收入，3种方法计算的水分收支在4个季节的年际变化明显。Abstract: Based on 1958—2007 NCEP/NCAR reanalysis data, the characteristics of moisture budget in humid region affected by East Asian Monsoon are calculated by moisture transport, moisture flux divergence and P-E methods. The correlation coefficients of climatological variability calculated by these methods are 0.91, 0.71, 0.81, and the percentage of ε are 17.4%, 44.1% and 44%. The results calculated by moisture transport and moisture flux divergence methods are nearly the same. The results reveal net income of moisture budget thoughout the year especially in spring and summer, while in winter and autumn it's relatively weaker. Using moisture flux divergence and P-E methods, the absolute errors in summer are larger than in other seasons. In spring and summer, water transport and moisture flux divergence are both stronger than those in autumn and winter. For the meridional moisture transport, moisture enters this area mainly from south boundary. For the zonal moisture transport, moisture enters through west boundary and departs from east boundary all the year. Overall, the period of positive moisture budget is from February to October calculated by moisture transport method, and from February to September by the other two methods. Vertical distribution of moisture budget is calculated by moisture transport method and moisture flux divergence method. It shows that the anomaly transport between 800—500 hPa is positive during 1960s and early 1970s and negative after that. Below 800 hPa, the values manifest negative before 1960s, and then turn to positive. There is net income of moisture at the whole layer except for the 850 hPa. By moisture flux divergence method, the calculated moisture convergence is positive above 450 hPa, and negative below. The interannual moisture budget variability of four seasons is quite obvious.
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图 2 1958-2007年东亚季风湿润区多年平均的年水汽输送的气候分布 (单位:kg·s-1·m-1，阴影区为水汽输送通量大于100kg·s-1·m-1的区域)
Fig. 2 Climatic distribution of the annual average moisture transport in humid region affected by East Asian Monsoon from 1958 to 2007(unit: kg • s-1 • m-1, the value of moisture transport flux in shadow area exceeds 100 kg • s-1 • m-1)
图 3 1958-2007年东亚季风湿润区多年平均纬向及平均经向水分收支的年循环
(a) 西边界，(b) 东边界，(c) 纬向水分收支距平，(d) 南边界，(e) 北边界，(f) 经向水分收支距平
Fig. 3 The climatological average zonal and meridional cycle of moisture budget in humid region affected by East Asian Monsoon from 1958 to 2007
(a) from the west boundary, (b) from the east boundary, (c) the zonal net budget anomaly, (d) from the south boundary, (e) from the north boundary, (f) the meridional net budget anomal
图 4 用水汽输送、水汽通量散度及P-E方法计算的1958-2007年平均东亚季风湿润区水分收支距平年循环
Fig. 4 The climatological cycle of the moisture budget anomaly calculated by the moisture transport, moisture llux divergence and P-E motheds in humid region affected by East Asian Monsoon averaged from 1958 to 2007
图 5 1958-2007年多年平均的东亚季风湿润区水汽输送的时间-纬向分布和时间-经向分布
(阴影区的值大于100kg·s-1·m-1)(a) B边界，(b) D边界，(c) F边界，(d) A边界，(e) C边界，(f) E边界
Fig. 5 The time-zone distribution and time-meridian distribution of moisture transport under the climatic mean state in humid region affected by East Asian
Monsoon from 1958 to 2007 (the value of shadow area exceeds 100kg·s-1·m-1) (a) B boundary, (b) D boundary, (c) F boundary, (d) A boundary, (e) C boundary, (f) E boundary
图 6 1958-2007年利用水汽输送方法计算的东亚季风湿润区水分收支距平垂直分布的年际变化 (单位:104 m3·s-1)(深色阴影区值大于1×104 m3·s-1，浅色阴影区值小于-1×104 m3·s-1)
Fig. 6 The interannual change of the vertical distribution of moisture budget anomaly calculated by moisture transport method in humid region affected by East Asian Monsoon from 1958 to 2007(unit:104 m3·s-1) (the value of heavy shadow area exceeds1×104 m3·s-1, the light shadow area is below-1×104 m3·s-1)
图 7 1958-2007年利用水汽输送方法计算的多年平均的东亚季风湿润区水分收支垂直分布
Fig. 7 The vertical distribution of climatological mean moisture budgetcalculated by moisture transport method under the climatic mean state inhumid region affected by East Asian Monsoon from 1958 to 2007
图 8 1958-2007年东亚季风湿润区利用水汽输送、水汽通量散度及P-E方法计算的水分收支距平年际变化 (a) 全年，(b) 春季，(c) 夏季，(d) 秋季，(e) 冬季
Fig. 8 The interannual changes of moisture budget anomaly calculated by the moisture transport, moisture flux divergence and P~E methods in humid region affected by East Asian Monsoon from 1958 to 2007 (a) annual budget, (b) spring, (c) summer, (d) autumn, (d) winter
表 1 1958-2007年用水汽输送方法计算得到的东亚季风湿润区水分收支季节变化
Table 1 The seasonal variability of moisture budget calculated by moisture transport in humid region affected by East Asian Monsoon from 1958
表 2 1958-2007年用
Table 2 The seasonal variability and absolute error of themoisture budget calculated by
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[1] 高由禧, 徐淑英.关于东亚季风区域的气候的研究.气象学报, 1959, 30(3):258-262. http://www.cnki.com.cn/Article/CJFDTOTAL-QXXB195903011.htm [2] HoL, Wang B.The time space structure of the Asian-Pacific summer monsoon:A fast annual cycle view.J Climate, 2002, 15(15):2001-2019. doi: 10.1175/1520-0442(2002)015<2001:TTSSOT>2.0.CO;2 [3] 孙林海, 赵振国, 许力, 等.中国东部季风区夏季雨型的划分及其环流成因分析.应用气象学报, 2005, 16(3):56-62. http://www.cnki.com.cn/Article/CJFDTOTAL-YYQX2005S1006.htm [4] 赵平, 周秀骥.近40年我国东部降水持续时间和雨带移动的年代际变化.应用气象学报, 2006, 17(5):548-556. http://qikan.camscma.cn/jams/ch/reader/view_abstract.aspx?file_no=20060594&flag=1 [5] 陈隆勋.东亚季风.北京:气象出版社, 1991. [6] 王劲松, 陈发虎, 靳立亚, 等.亚洲中部干旱区在20世纪两次暖期的表现.冰川冻土, 2008, 30(2):224-233. http://www.cnki.com.cn/Article/CJFDTOTAL-BCDT200802007.htm [7] Rasmusson E M.Atmospheric water vapor transport and the water balance of North America.Part I:Characteristics of the water vapor flux field.Mon Wea Rev, 1967, 95:403-426. doi: 10.1175/1520-0493(1967)095<0403:AWVTAT>2.3.CO;2 [8] Rasmusson E M, Mo K C.Large-scale atmospheric moisture cycling as evaluated from NMC global analysis and forecast products.J Climate, 1996, 9:3276-3297. doi: 10.1175/1520-0442(1996)009<3276:LSAMCA>2.0.CO;2 [9] Roads JO, Chen S C, Guetter A K, et al.Large-scale aspects of the United States hydrological cycle.Bull Amer Meteor Soc, 1994, 75:1589-1610. doi: 10.1175/1520-0477(1994)075<1589:LSAOTU>2.0.CO;2 [10] Schmitz J T, Mullen S L.Water vapor transport associated with summertime North American monsoon as depicted by ECWMF analyses.J Climate, 1996, 9:1621-1634. doi: 10.1175/1520-0442(1996)009<1621:WVTAWT>2.0.CO;2 [11] Trenberth K E, Guillemot C J.Evaluation of the atmospheric moisture and hydrological cycle in the NCEP/NCAR reanalyses.Climate Dynamics, 1998, 14:213-231. doi: 10.1007/s003820050219 [12] Bisslink B, Dolman A J.Precipitation recycling:Moisture sources over Europe using ERA-40 data.Journal of H ydrometeorology, 2008, 9(10):1073-1083. [13] Serreze M C, Roger G.Atmospheric water vapor characteris-tics at 70°N.J Climate, 1995, 8(4):719-731. doi: 10.1175/1520-0442(1995)008<0719:AWVCA>2.0.CO;2 [14] Zangvil A, Portis D H, Lamb P J.Investigation of the large-scale atmospheric moisture field over the Midwestern United States in relation to summer precipitation.Part I:Relation-ships between moisture budget components on different time scales.J Climate, 2000, 14:582-597. [15] Simmonds I, Bi D H, Hope P.Atmospheric water vapor flux and it sassociation with rainfall over China in summer.J Climate, 1999, 12(5):1353-1367. doi: 10.1175/1520-0442(1999)012<1353:AWVFAI>2.0.CO;2 [16] Ninimiya K.Moisture balance over China and the South China Sea during the summer monsoon in relation to the intense rainfalls over China.J Meteor Soc Japan, 1999, 77(3): 737-751. [17] Knippert z P, Wernli H.A Lagrangian climatology of tropical moisture exports to the Northern Hemispheric extratropics. J Climate, 2010, 23(2):987-1003. http://www.academia.edu/13574968/A_Lagrangian_Climatology_of_Tropical_Moisture_Exports_to_the_Northern_Hemispheric_Extratropics [18] 周天军, 张学洪, 王绍武.全球水循环的海洋分量研究.气象学报, 1999, 57(3):264-282. http://www.cnki.com.cn/Article/CJFDTOTAL-QXXB903.001.htm [19] 黄荣辉, 张振洲, 黄刚, 等.夏季东亚季风区水汽输送特征及其与南亚季风区水气输送的差别.大气科学, 1998, 22 (4):460-469. http://www.cnki.com.cn/Article/CJFDTOTAL-DQXK804.007.htm [20] 范广洲, 吕世华, 程国栋.华北地区夏季水量丰、枯年大气水分收支对比分析.兰州大学学报 (自然科学版), 2001, 37 (3):134-141. [21] 苗秋菊, 徐祥德, 张胜军.长江流域水汽收支与高原水汽输送分量"转换"特征.气象学报, 2005, 63(1):93-99. [22] 赵瑞霞, 吴国雄, 张宏.夏季风期间长江流域的水汽输送状态及其年际变化.地球物理学报, 2008, 51(6):1670-1681. http://www.cnki.com.cn/Article/CJFDTOTAL-DQWX200806008.htm [23] 赵瑞霞, 吴国雄.黄河流域中上游水分收支以及再分析资料可用性分析.自然科学进展, 2006, 16(3):316-324. http://www.cnki.com.cn/Article/CJFDTOTAL-ZKJZ200603012.htm [24] 赵瑞霞, 吴国雄.长江流域水分收支以及再分析资料可用性分析.气象学报, 2007, 65(3):416-427. http://www.cnki.com.cn/Article/CJFDTOTAL-QXXB200703009.htm [25] 张文君, 周天军, 宇如聪.中国东部水分收支的初步分析.大气科学, 2007, 31(2):329-345. http://www.cnki.com.cn/Article/CJFDTOTAL-DQXK200702014.htm [26] 张洁, 周天军, 宇如聪, 等.中国春季典型降水异常及相联系的大气水汽输送.大气科学, 2009, 33(1):121-134. http://www.cnki.com.cn/Article/CJFDTOTAL-DQXK200901010.htm [27] 谢安, 毛江玉, 宋焱云, 等.长江中下游地区水汽输送的气候特征.应用气象学报, 2002, 13(1):67-77. http://qikan.camscma.cn/jams/ch/reader/view_abstract.aspx?file_no=20020108&flag=1 [28] 施小英, 施晓晖.夏季青藏高原东南部水汽收支气候特征及其影响.应用气象学报, 2008, 19(1):41-46. http://qikan.camscma.cn/jams/ch/reader/view_abstract.aspx?file_no=20080108&flag=1 [29] Yanai M, Esbensen S, ChuJ H.Determination of average bulk properties of tropical cloud clusters from largerscale heat and moisture budgets.Journal of Atmospheric Science, 1973, 30 (4):611-627. doi: 10.1175/1520-0469(1973)030<0611:DOBPOT>2.0.CO;2 [30] Rasmusson E M.Atmospheric water vapor transport and the water balance of North America.Part II:Large-scale water balance investigations.Mon Wea Rev, 1968, 96:720-724. doi: 10.1175/1520-0493(1968)096<0720:AWVTAT>2.0.CO;2 [31] Barry R G.Variations in the content and flux of water vapor over north-eastern North America during two winter seasons. Quarterly Journal of the Royal Meteorological Society, 1967, 93:535-543. doi: 10.1002/(ISSN)1477-870X -
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