设为首页
加入收藏
The Tropical Atmospheric Intra-seasonal Oscillation with Different Reanalysis Data
-
摘要: 利用NCEP/NCAR, NCEP/DOE和ERA40 3套再分析资料的逐日200 hPa纬向风数据，选取1961—1990年、1971—2000年和1981—2010年3种不同气候态，对比分析了3种气候态下热带大气季节内振荡 (ISO) 的基本气候特征及其在不同再分析资料中的异同。研究表明：1981—2010年气候态下，热带大气ISO冬春强、夏秋弱的年循环特征更加明显，东传短波能量增强，起始北传时间偏晚。NCEP/NCAR与NCEP/DOE资料所表征的热带大气ISO在空间分布、强度和能量传播方面的一致性较好。NCEP/NCAR资料反映的热带大气ISO强度在热带印度洋和热带西太平洋地区较ERA40资料偏弱，在赤道东太平洋地区较ERA40资料偏强；ERA40资料反映的热带大气ISO强度在12月—次年3月中旬较NCEP/NCAR资料偏强，而在3月中旬—11月偏弱；ERA40资料反映的热带大气ISO振荡位相较NCEP/NCAR资料超前10 d左右；NCEP/NCAR资料反映的东传谱能量弱于ERA40资料，西传能量强于ERA40资料；7月中旬，NCEP/NCAR资料反映的东亚地区大气ISO经向北传较ERA40资料偏晚。Abstract: Characteristics of the tropical intra-seasonal oscillation are analyzed using three kinds of data (NCEP/NCAR reanalysis data, NCEP/DOE reanalysis data and ECMWF/ERA40 reanalysis data) in three climate states of 1961—1991, 1971—2000 and 1981—2010. There is a significant 30—60 d oscillation period of 200 hPa zonal wind in different climate states of different reanalysis data. Different intra-seasonal oscillation characteristics can be found in different data and in different climate states. It is found that in 1981—2010 climate state compared with the other two climate states (1971—2000 and 1981—2010), annual cycle characteristics of the tropical intra-seasonal oscillation are more pronounced, strong in winter-spring and weak in summer-autumn. The tropical intra-seasonal oscillation is stronger in the tropical Indian Ocean and the tropical western Pacific Ocean, also its active areas extend eastwards and become larger. The eastward propagating energy of the tropical intra-seasonal oscillation centers more in 1—3 waves, while the westward propagating energy becomes weaker. The tropical intra-seasonal oscillation starts northward propagating later. It propagates southward strongly which spreads to the Southern Hemisphere in the beginning of May. NCEP/NCAR reanalysis data and NCEP/DOE reanalysis data match well in the annual cycle characteristics of tropical intra-seasonal oscillation, intensity and energy propagation. While NCEP/NCAR reanalysis data and ERA40 reanalysis data have some distinctions: The tropical intra-seasonal oscillation periods center in 20—100 d and its peak value is 55 d of NCEP/NCAR reanalysis data, while its oscillation periods are 20—60 d and its peak value is 50 d of ERA40 reanalysis data. As to the periods of 80—100 d, the oscillation pattern of ERA40 reanalysis data is stronger than that of NCEP/DOE reanalysis data. The tropical intra-seasonal oscillation variance contribution proportion of NCEP/NCAR reanalysis data is a little less than that of ERA40 reanalysis data in the tropical Indian Ocean and the tropical western Pacific Ocean, while stronger than that of ERA40 reanalysis data in the Eastern Equatorial Pacific Ocean. From December to the middle of March, the tropical intra-seasonal oscillation intensity of ECMWF data is stronger than that of NCEP/NCAR reanalysis data. While from the middle of March to November, the tropical intra-seasonal oscillation intensity of ERA40 reanalysis data is weaker than that of NCEP/NCAR reanalysis data; the tropical intra-seasonal oscillation phase of ERA40 reanalysis data is about 10 days ahead of NCEP/NCAR reanalysis data. The eastward propagating energy of the tropical intra-seasonal oscillation of NCEP/NCAR reanalysis data is weaker than that of ERA40 reanalysis data, while the westward propagating energy is stronger than that of ERA40 reanalysis data. In the middle of July, the northward propagating of NCEP/NCAR data is weaker than that of ERA40 reanalysis data.
-
图 1 3种气候态下10°S~10°N平均200 hPa纬向风的功率谱值和0.05显著性水平检验曲线
Fig. 1 Power spectrum (solid line) of 200 hPa zonal wind averaged between 10°S-10°N and test line of 0.05 level (dashed line) in three different climate states
图 2 3种气候态下200 hPa纬向风20~100 d周期变化方差解释总方差的百分比
(单位：%；阴影区为方差百分比不小于40%的区域)
Fig. 2 Explained variance percentages of 200 hPa zonal wind by 20—100 d filtered in three different climate states
(unit:%; explained variance percentages of shaded areas are not less than 40%)
图 3 1961—1990年NCEPI与ERA40资料200 hPa纬向风20~100 d周期变化方差解释总方差的百分比差值
(单位：%; 阴影区为偏差绝对值不小于2%的区域)
Fig. 3 The difference of explained variance percentages of 200 hPa zonal wind by 20—100 d filtered between NCEPI and ERA40 data in 1961—1990
(unit:%; the difference of shaded areas is not less than 2%)
图 4 1981—2010年NCEPI资料200 hPa纬向风20~100 d周期变化方差解释总方差的百分比与1961—1990年的差值
(单位：%; 阴影区为偏差绝对值不小于4%的区域)
Fig. 4 The difference of explained variance of 200 hPa zonal wind by 20—100 d filtered between NCEPI data in 1981—2010 and 1961—1990
(unit:%; the difference of shaded areas is not less than 4%)
图 6 同图 2，但为200 hPa纬向风的空间-时间功率谱
(横坐标表示向东为正值，向西为负值的波频率；纵坐标表示空间纬向波数；阴影区为功率谱能量不小于0.04 m2·s-2的区域)
Fig. 6 The same as in Fig. 2, but for spatial-temporal spectrum of 200 hPa zonal wind
(the horizontal axis represents wave frequency, positive value represents eastward propagation, negative value represents westward propagation; the vertical axis represents wave number, the spectrum of shaded areas is no less than 0.04 m2·s-2)
-
[1] Slingo J M, Rowell D P, Sperber K R.On the predictability of interannual behavior of the Madden-Julian oscillation and its relationship with El Nino.Q J Roy Meteor Soc, 1999, 125:583-609. https://www.osti.gov/scitech/biblio/289673 [2] Salby M L, Hendon L H.Intraseasonal behavior of clouds, temperature and motion in the tropics.J Atmos Sci, 1994, 51(15):2207-2225. doi: 10.1175/1520-0469(1994)051<2207:IBOCTA>2.0.CO;2 [3] 智协飞, 朱乾根.北半球平流层低层大气季节内振荡特征.应用气象学报, 1995, 6(4):492-495. http://qikan.camscma.cn/jams/ch/reader/view_abstract.aspx?file_no=19950475&flag=1 [4] Madden R A, Julian P R.Description of a 40—50 day oscillation in the zonal wind in the tropical Pacific.J Atmos Sci, 1971, 28(5):702-708. doi: 10.1175/1520-0469(1971)028<0702:DOADOI>2.0.CO;2 [5] Madden R A, Julian P R.Description of global scale circulation cells in the tropics with a 40—50 day period.J Atmos Sci, 1972, 29(6):1109-1123. doi: 10.1175/1520-0469(1972)029<1109:DOGSCC>2.0.CO;2 [6] Madden R A.Seasonal variations of the 40—50 day oscillation in the tropics.J Atmos Sci, 1986, 43(24):3138-3145. doi: 10.1175/1520-0469(1986)043<3138:SVOTDO>2.0.CO;2 [7] Madden R A, Julian P R.Observations of the 40—50 day tropical oscillation—A review.Mon Wea Rev, 1994, 122(5):814-837. doi: 10.1175/1520-0493(1994)122<0814:OOTDTO>2.0.CO;2 [8] 林爱兰, 梁建因, 谷德军.热带大气季节内振荡对东亚季风区的影响及不同时间尺度变化研究进展.热带气象学学报, 2008, 24(1):11-19. http://www.cnki.com.cn/Article/CJFDTOTAL-RDQX200801003.htm [9] 李崇银.大气低频振荡.北京:气象出版社, 1993. http://www.cnki.com.cn/Article/CJFDTOTAL-SYQY201603027.htm [10] 王遵娅, 丁一汇.夏季长江中下游旱涝年季节内振荡气候特征.应用气象学报, 2008, 19(6):710-715. doi: 10.11898/1001-7313.20080610 [11] 林爱兰, Li Tim, 李春晖.热带夏季风场与对流场季节内振荡传播模比较.应用气象学报, 2010, 21(5):545-557. doi: 10.11898/1001-7313.20100504 [12] 李崇银, 周亚平.热带大气季节内振荡和ENSO的相互关系.地球物理学报, 1994, 37(1):17-26. http://www.cnki.com.cn/Article/CJFDTOTAL-DQWX401.002.htm [13] Chen Longxun, Xie An.Westward propagation low-frequency oscillation and its teleconnection in the eastward hemisphere.Acta Meteor Sinica, 1998, 2(3):300-312. https://www.researchgate.net/publication/262419614_Predictability_of_the_quasi-biennial_oscillation_and_its_northern_winter_teleconnection_on_seasonal_to_decadal_timescales [14] Lau K M, Chan P H.The 40—50 day oscillation and the El Nino/Southern Oscillation:A new perspective.Bull Amer Meteor Soc, 1986, 67(5):533-534. doi: 10.1175/1520-0477(1986)067<0533:TDOATE>2.0.CO;2 [15] 李丽平, 王盘兴, 管兆勇, 等.热带对流季内振荡强度异常特征及其与海表温度的关系.应用气象学报, 2008, 19(2):145-152. doi: 10.11898/1001-7313.20080227 [16] 董敏, 吴统文, 王在志, 等. BCC_CSM1.0模式对20世纪降水及其变率的模拟.应用气象学报, 2013, 24(1):1-11. doi: 10.11898/1001-7313.20130101 [17] Kalnay E, Kanmitsu M, Kistler R, et al.The NCEP/NCAR 40-year reanalysis project.Bull Amer Meteor Soc, 1996, 77(3): 437-471. doi: 10.1175/1520-0477(1996)077<0437:TNYRP>2.0.CO;2 [18] Kanamitsu M, Ebisuzaki W, Woollen J, et al.NCEP-DOE AMIP-Ⅱ reanalysis (R-2).Bull Amer Meteor Soc, 2002, 83(11):1631-1643. doi: 10.1175/BAMS-83-11-1631 [19] GibsonJK, Kallberg P, Uppala S.The ECMWF ReAnalysis (ERA) Project.ECMWF Newsl, 1996, 73:7-17. https://en.wikipedia.org/wiki/ECMWF_re-analysis [20] Gibson J K, Kallberg P, Uppala S, et al.ECMWF ReAnalysis Project Rep Ser1.ECMWF, Shinfield Park, Reading, United Kingdom, 1997:1-72. http://www.ecmwf.int/ [21] Annamalai H, Slingo J M, Sperber K R.The mean evolution and variability of the Asian Summer Monsoon: Comparison of ECMWF and NCEP/NCAR Reanalysis.Mon Wea Rev, 1999, 127(6):1157-1186. doi: 10.1175/1520-0493(1999)127<1157:TMEAVO>2.0.CO;2 [22] Dell'Aquila A, Lucarini V, Ruti P M, et al.Hayashi spectra of the northern hemisphere mid-latitude atmospheric variability in the NCEP/NCAR and ECMWF reanalysis.Climate Dyn, 2005, 25(6):639-652. doi: 10.1007/s00382-005-0048-x [23] Pocard I, Janicot S, Camberlin P.Comparison of rainfall structures between NCEP/NCAR reanalysis and observed data over tropical Africa.Climate Dyn, 2000, 16(12):897-916. doi: 10.1007/s003820000087 [24] Inoue T, Matsumoto J.A comparison of summer sea level pressure over east Eurasiabetween NCEP-NCAR reanalysis and ERA-40 for the Period 1960-1999.J Meteor Soc Japan, 2004, 82(3):951-958. doi: 10.2151/jmsj.2004.951 [25] 宋超辉.长年代气候资料统计处理结果的质量保障.气象科技, 2000, 28(4):53-56. http://www.cnki.com.cn/Article/CJFDTOTAL-QXKJ200004009.htm [26] Slingo J M, and Coauthors.Intraseasonal oscillation in 15 atmospheric general circulation models:Results from an AMIP subject.Climate Dyn, 1996, 12:325-357. doi: 10.1007/BF00231106 [27] Hayashi Y.A method of analyzing transient waves by space-time cross spetra.J Appl Meteor, 1973, 12:404-408. doi: 10.1175/1520-0450(1973)012<0404:AMOATW>2.0.CO;2 [28] 黄嘉佑.气象中的谱分析.北京:气象出版社, 1984. http://www.cnki.com.cn/Article/CJFDTOTAL-SYQY201603027.htm [29] Butterworth S.On the theory of filter amplifiers.Experimental Wireless and the Wireless Engineer, 1930, 7:536-541. [30] Sperber K R.Madden-Julian variability in NCAR CAM2.0 and CCSM2.0.Climate Dyn, 2004, 23:259-278. [31] 刘芸芸, 俞永强, 何金海, 等.全球变暖背景下热带大气季节内振荡的变化特征及数值模拟.气象学报, 2006, 64(6):723-733. doi: 10.11676/qxxb2006.069 [32] Zhu Qiangen, He Jinhai, Wang Panxing.A study of circulation differences between East-Asian and Indian summer monsoon with their interaction.Adv Atmos Sci, 1986, 3(4):466-477. doi: 10.1007/BF02657936 [33] 何金海, 杨松.东亚地区低频振荡的经向传播及中纬度的低频波动.气象学报, 1992, 5, 50(2):190-198. doi: 10.11676/qxxb1992.021 -
下载:
计量
- 摘要浏览量: 2716
- HTML全文浏览量: 1121
- PDF下载量: 1101
- 被引次数: 0
