Characteristics of Tropical Convection Intraseasonal Oscillation Anomaly and Their Relationship with Sea Surface Temperature

Li Liping; Wang Panxing; Guan Zhaoyong; Yang Song

Vol.19, NO.2, 2008

Article Contents

Article Navigation > Journal of Applied Meteorological Science > 2008 > 19(2): 145-152

Li Liping, Wang Panxing, Guan Zhaoyong, et al. Characteristics of tropical convection intraseasonal oscillation anomaly and their relationship with sea surface temperature. J Appl Meteor Sci, 2008, 19(2): 145-152.

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Characteristics of Tropical Convection Intraseasonal Oscillation Anomaly and Their Relationship with Sea Surface Temperature

1.
Nanjing University of Information Science & Technology, Nanjing 210044
2.
George Mason University, Fairfax, VA, USA

Received Date: 2007-01-09
Rev Recd Date: 2007-07-25
Publish Date: 2008-04-30

Abstract

Abstract

The seasonal and interannual variability of intraseasonal oscillation (ISO) intensity of tropical convection is investigated by using NCAR/NOAA outgoing longwave radiation (OLR) data, along with the relationship with sea surface temperature (SST). It shows that there are two strongest ISO areas, namely, tropical Indian Ocean and tropical western Pacific Ocean, companied with large SST zonal deviation in climatological fields for any seasons. There are three noticeable areas of interannual anomaly of OLR ISO intensity, i.e., tropical middle and eastern Pacific (TMEP), tropical northwest Pacific (TNP) and tropical southwest Pacific (TSP). In these areas, there are noticeably positive correlation relationships between anomalies of OLR ISO intensity and SST interannually, along with the circulation anomaly convergence (divergence) in the low (high) level at the same time, which is also closely related to El Niño (La Nina) events according to the time coefficient series. In addition, the ISO enhances and moves eastward gradually before El Niño event takes place, and weakens later in the tropical Indian Ocean and tropical west Pacific, which links up with the areas of OLR ISO interannual anomaly intrinsically, because OLR ISO weakens in TNP and TSP and enhances in TMEP after the El Niño event occurs. In the climatological fields, OLR ISO is weak in TMEP, TNP and TSP, whereas the SST interannual anomaly is notable in these areas. It shows that SST interannual anomaly is very important for that of OLR intensity and an even crucial factor. It is well known that ENSO is the strongest interannul signal of SST, which is most notable in the winter and spring, so it is easy to understand that there is a close relationship between the above local relations of ISO intensity and SST interannual anomaly with ENSO. SST interannual anomaly is too weak to produce the marked ISO anomaly in the western Pacific, so there is weak relation between ISO intensity and SST interannual anomaly. Comparing the seasonal with interannual variation of OLR intensity, it is found that SST is a key factor to determine the seasonal and interannual variations of OLR intraseasonal oscillation intensity.
- intraseasonal oscillation;
- seasonal and interannual variability;
- tropical convection;
- sea surface temperature

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References(41)

Figures and Tables

图 1 OLR ISO能量季节平均分布图 (单位:W²/m⁴)(a)12月—次年2月, (b)6—8月

Fig. 1 Seasonal mean OLR ISO energy (unit:W²/m⁴)(a) from Dec to next Feb, (b) from Jun to Aug

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图 2 850 hPa辐散风 (矢量, 单位:m/s)、SST的纬向偏差 (阴影, 单位:℃)、OLR的ISO能量 (粗实线包围的区域, 单位:W ²/m⁴)

(a)12月—次年2月, (b)6—8月

Fig. 2 850 hPa divergence wind (vector, unit:m/s), SST zonal departure (shaded, unit:℃), OLR ISO energy (circled by thick line, unit:W²/m⁴)

(a) from Dec to next Feb, (b) from Jun to Aug

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图 3 同图 2, 但为200 hPa辐散风场

Fig. 3 Same as in Fig.2, but for 200 hPa divergence wind

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图 4 冬季SVD第一奇异向量（阴影区为′_OLR，单位：W²/m⁴；断线为T’_ss，单位：℃；矢量为V′_d，单位：m/s）

（a）′_OLR~T′_ss，（b）′_OLR~V′_d200，（c）E′_OLR~V′_d850

Fig. 4 SVD first eigenvectors in the boreal winter (_OLR:shaded, unit:W²/m⁴; T'_ss; long dashed line, unit:℃; V'_d:vector, unit:m/s)

(a)_OLR~T'_ss, (b)_OLR~V'_d200, (c) E_OLR~V'_d850

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图 5 冬季SVD第一奇异向量（实线为′_OLR×10^-2，虚线为T′_ss，V′_d；●对应El Niño年，○对应La Niña年）

（a）′_OLR~T′_ss，（b）E′_OLR~V′_d200，（c）E′_OLR~V′_d850

Fig. 5 SVD first time coefficients in the boreal winter (solid line:'_OLR×10^-2; dashed line:T′_ss, V′_d; ● for El Niño events; ○ for La Niña events)

(a) ′_OLR~T′_ss, (b) ′_OLR~V′_d200, (c) ′_OLR~V′_d850

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图 6 同图 4，但为夏季SVD第一奇异向量

Fig. 6 Same as in Fig.4, but for the boreal summer

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图 7 同图 5, 但为夏季SVD第一时间系数

Fig. 7 Same as in Fig.5, but for the boreal summer

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表 1 SVD第一模态的ρ₁(单位:%)、相关系数r₁

Table 1 ρ₁ of the SVD first mode (unit:%) and correlation coefficient r₁

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