Relationship Between Rossby Wave Propagation in Southern Branch of Westerlies and the Formation of the Southern Branch Trough in Wintertime

Suo Miaoqing; Ding Yihui; Wang Zunya

Vol.19, NO.6, 2008

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Article Navigation > Journal of Applied Meteorological Science > 2008 > 19(6): 731-740

Suo Miaoqing, Ding Yihui, Wang Zunya. Relationship between Rossby wave propagation in southern branch of westerlies and the formation of the southern branch trough in wintertime. J Appl Meteor Sci, 2008, 19(6): 731-740.

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Relationship Between Rossby Wave Propagation in Southern Branch of Westerlies and the Formation of the Southern Branch Trough in Wintertime

1.
Chinese Academy of Meteorological Sciences, Beijing 100081
2.
Nanjing University of Information Science & Technology, Nanjing 210044
3.
Yunnan Provincial Meteorological Observatory, Kunming 650034
4.
National Climate Center, Beijing 100081

Received Date: 2008-02-18
Rev Recd Date: 2008-08-22
Publish Date: 2008-12-31

Abstract

Abstract

Based on the calculation of wave number of Rossby wave and flux of wave activity, the characteristics of Rossby wave propagation in southern branch of westerlies are analyzed, and the relationship between Rossby wave propagation in westerly jet stream and the formation mechanism of the wintertime southern branch trough in the subtropical westerlies is also investigated by using 58-year monthly and daily NCEP/ NCAR reanalysis data with the aid of one point correlation, EOF, harmonic and composition analysis.Results show that the reare three westerly disturbances under the subtropical westerly jet stream in Arabian Sea, the Bay of Bengal, and South China of Northern Hemisphere during the winter half year. Southern branch trough over the Bay of Bengal is a semi-permanent trough due to the smallest variability. A teleconnection wave train with negative, positive and negative centers, migrating from North Africa to the Bay of Bengal via Arabian Sea, suggests that southern branch trough is positively related with the trough over North Africa.In the propagation process from North Africa to the Bay of Bengal, the westerly disturbances usually pause or strengthen in the Arabian Sea.The propagation from west to east takes about 20 days, appearing remarkable quasi-biweekly oscillation.There are waveguide regions of wave number 6—8 along the subtropical westerly jet stream in the half year of winter.Because jet stream waveguide is the strongest and the stationary Rossby wave energy in the lower troposphere coming from North Africa is transported to the Bay of Bengal, southern branch trough becomes deepest in February.Bay of Bengal is also a main source place of southern branch trough in the winter half year, and the development of trough over South China mainly connects with the eastern propagation of southern branch trough.Moreover, the activity of the cold air along the eastern and western sides of the the Plateau plays an important role in the formation of southern branch trough.After the breaking down of cold air, it first arrives at Bay of Bengal along the southern sides of the Plateau and then departs from the western sides of the Tibetan Plateau, and makes the southern branch trough gradually deepened.The eastern cold air of the Tibetan Plateau breaks down in the wake of cold surge breaking down in East Asia.Cold air at surface layer from north-east to south-west disperses to the region of India and Burma, which is another important factor of development of southern branch trough.
- Rossby wave;
- SBT;
- propagate and developed mechanism

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References(17)

Figures and Tables

图 1 1948-2005年多年平均冬半年 (10月-次年5月)700 hPa位势高度 (实线, 单位:gpm) 及其标准差 (虚线, 单位:gpm) 和200 hPa西风急流 (阴影表示u≥30 m · s^-1)

(点划线表示3000 m地形, 粗实线为槽线)

Fig. 1 Climatology of the geopotential height (solid contours, unit :gpm) and corresponding standard deviation (dashed lines, unit :gpm) at 700 hPa and the westerly jet stream (shaded area means the high speed of jet stream u≥30 m · s^-1) at 200 hPa in winter (October to next May) averaged from 1948-2005(dot-dashed line indicates 3000 m topography, thick solid line indicates trough-line)

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图 2 1948-2005年多年平均冬半年高度距平一点相关图 (基点:57.5°N, 0°)

(a)200 hPa, (b)700 hPa (图b中阴影表示3000 m地形)

Fig. 2 One-point correlation map between the base-point (57.5°N, 0°) and winter time geopotential height anomalies averaged from 1948-2005 at 200 hPa (a) and 700 hPa (b)(shadow in Fig.b is for the 3000 m topography)

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图 3 1948-2005年200 hPa高度距平标准化EOF第二模态

(a) 冬季 (11月-次年2月), (b) 春季 (3-5月)

Fig. 3 The second EOF modes based on the normalized geopotantial height anomalies at 200 hPa in winter (NDJF)(a) and spring (MAM)(b) from 1948 to 2005

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图 4 1948-2005年多年平均1月1日-2月28日位势高度距平经向-时间剖面

(a)200 hPa (沿20°~35°N), (b)700 hPa (沿20°~27.5°N)

Fig. 4 The meridion-time cross-section of the geopotential height anomalies from January 1 to February 28 averaged from 1948-2005 at 200 hPa along 20°-27.5°N (a), 700 hPa along 20°-35°N (b)

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图 5 1948-2005年多年平均200 hPa局地定常Rossby波波数

(a)10月, (b)11月, (c)12月, (d)1月, (e)2月, (f)3月, (g)4月, (h)5月

Fig. 5 Distribution of the stationary Rossby wave number at 200 hPa for the period of 1948-2005 in Oct (a), Nov (b), Dec (c), Jan (d), Feb (e), Mar (f), Apr (g) and May (h)

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图 6 1948-2005年多年平均700 hPa水平波作用矢量 (箭矢, 单位:m² · s^-2) 及其散度(阴影表示绝对值≥10 m · s^-2的散度, 单位:m · s^-2) 和位势高度纬向偏差 (等值线, 单位:gpm)

(a)10月, (b)11月, (c)12月, (d)1月, (e)2月, (f)3月, (g)4月, (h)5月 (点划线表示3000 m地形; “ +”表示源, “-”表示汇)

Fig. 6 Distribution of the horizontal components of stationary Rossby wave activity flux (arrowheads, unit :m ² · s^-2) with its diver gence (shadows, divergence with its absolute value≥10 m · s^-2 omitted, unit :m · s^-2) and geopotential height anomalies (isolines, unit :gpm) in Oct (a), Nov (b), Dec (c), Jan (d), Feb (e), Mar (f), Apr (g) and May (h) averaged from 1948-2005 (dot-dashed line indicates the 3000 m topog raphy; " +" indicates sources and"-" indicates sinks)

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图 7 用傅利叶谐波分析滤除前2波后的冬半年南支槽指数标准化时间序列

Fig. 7 Time series of normalized winter time SBT index with the first two wave removed by Fourier harmonic analysis

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图 8 700hPA南支槽最强日及前4天至后2天位势高度距平（等值线，单位：gpm）、复变温（阴影）和风场距平（箭矢，单位：s·m^-1）分布

Fig. 8 Distribution of geopotential height anomaly (isolines, unit:gpm), negative anomaly of temperature (shadows) and wind anomaly (arrowheads, unit:m·^-1) at 700hPa from leading 4 days to lag 2 days of the deepest SBT day

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表 1 南支槽个例最强日前4天至后2天日期

Table 1 Appearing date of the deepest IBT from leading 4 days to lag 2 days

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