Why 1986 El Niño and 2005 La Niña evolved different from a typical El Niño and La Niña

Chen, Mingcheng; Li, Tim

doi:10.1007/s00382-017-3852-1

Cited by 17 publications

(9 citation statements)

References 52 publications

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“…In the following summer, a negative SSTA of less than −0.5°C is confined to a limited region over the equatorial CP, but re‐intensifies in following autumn. The SSTA evolution in this type is consistent with that of a typical La Niña (Chen and Li, ). Among the 18 La Niña events, 5 can be classified as R‐type.…”

Section: Three Types Of La Niña Decaysupporting

confidence: 84%

“…La Niña completely ends in the following summer, and there is no SSTA in the equatorial Pacific after the summer (Figure a). In fact, after the mature phase, a typical La Niña event usually decay slowly in the succeeding spring and summer, and then redevelops into a La Niña event in winter (Chen and Li, ). However, this does not materialize in the evolution of the composite SSTA of all La Niña events as shown in Figure , suggesting that each La Niña might evolve in a quite different manner, or even in an opposite way during the decaying phase.…”

Section: Three Types Of La Niña Decaymentioning

confidence: 99%

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The diversity of La Niña decay and the corresponding spring and summer precipitation anomalies over eastern China

Chen

Zhu

et al. 2019

Intl Journal of Climatology

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The present study investigates the diversity of the La Niña decaying phase and the corresponding spring and summer precipitation anomalies over the eastern China. Based on the differences in sea surface temperature anomaly (SSTA) evolution during the La Niña decaying phase, 18 La Niña events in the period 1961–2016 are classified into three types—namely, the “persistent type” (P‐type), the “re‐intensified type” (R‐type), and the “fast‐decay type” (F‐type). Precipitation responses over eastern China during the decaying spring and summer of the three types of La Niña present significant differences. For the R‐type La Niña decaying spring, the enhanced precipitation appears over northeastern China but significant suppressed precipitation anomalies are observed elsewhere, particularly in Yellow River basin, the Yangtze River basin, and southeastern China. Significant negative precipitation anomaly appears over northeastern China in both P‐type and F‐type La Niña decaying spring. In the decaying summer, for P‐type La Niña, dry anomalies are apparent in southern and northern China. For R‐type La Niña, negative rainfall anomalies are notable in northeastern China, the Hetao region, and the middle reaches of the Yangtze River basin. For F‐type La Niña, significant negative rainfall anomalies are found over the Yangtze River basin and parts of northern China. The responses of the large‐scale circulation anomalies to the distinct SSTA patterns of the different types of La Niña are responsible for the diversity of rainfall anomalies over eastern China. The precipitation anomaly pattern in eastern China is closely associated with the different types of La Niña decay, and it is seasonal‐dependent. These two aspects should be taken into account when conducting seasonal predictions of spring and summer rainfall anomalies over eastern China using El Niño–Southern Oscillation as a predictor.

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Section: Three Types Of La Niña Decaysupporting

confidence: 84%

Section: Three Types Of La Niña Decaymentioning

confidence: 99%

The diversity of La Niña decay and the corresponding spring and summer precipitation anomalies over eastern China

Chen

Zhu

et al. 2019

Intl Journal of Climatology

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“…During the months of October of the examined years, strong anomalous anticyclonic circulations were generated (positive stream function anomalies) in the Northern Indian Ocean, and strong suppressed convection activities (negative precipitation anomalies) were observed to have existed on the eastern sides of the anticyclonic circulations. Over time, the anomalous anticyclone and negative convection center had gradually moved eastward to the Northwestern Pacific Ocean region and had then merged with the local suppressed phase‐convection activities (Chen and Li, ). Therefore, during the winter periods of the El Niño years, the Northwestern Pacific Ocean region was dominated by negative precipitation anomalies and anticyclonic circulation activities (Figure j).…”

Section: Resultsmentioning

confidence: 99%

“…It has been well documented that the anomalous warming of the tropical Pacific SST during El Niño events has a significant teleconnection effect on the climate variabilities of the Indian and Atlantic Oceans (Enfield and Mayer, 1997;Chang et al, 2000;Alexander and Scott, 2002;Chiang and Sobel, 2002;Kug and Kang, 2006;Chowdary and Gnanaseelan, 2007;Xie et al, 2009;Sayantani et al, 2014). However, a growing number of related research results have also shown that SST anomalies in the tropical Indian and Atlantic Ocean regions also have remote influences on the variabilities of the ENSO events (Xie et al, 2002;Annamalai et al, 2005;Schott et al, 2009;Luo et al, 2012;Ham et al, 2013;McGregor et al, 2014;Sasaki et al, 2014;Chen and Li, 2017;Saji et al, 2018). It was observed in this study that the link between the SST anomalies and the ENSO events in the Southwestern Indian Ocean has so far received less attention from meteorologists.…”

Section: Introductionmentioning

confidence: 99%

The negative feedback effects of sea surface temperatures on El Niño Events in the West Indian Ocean

Zhang

Liu

et al. 2019

Atmospheric Science Letters

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In this study, multiple sets of atmospheric and oceanic observational data were used in combination with composite analysis and correlation analysis methods, in order to analyze the anomalous eastward spread phenomena of the equatorial Indian Ocean during the autumn and winter seasons when El Niño events have previously occurred. The analysis results showed that anomalous increases in the SSTs (sea surface temperatures) in the West Indian Ocean during the early autumn seasons had triggered the responses of anomalous easterlies. Meanwhile, anomalous anticyclonic circulation was observed to have existed on the north side of the easterlies. It was found that with the maximum center of the specific humidity retreating toward the vicinity of the equator during the processes of the seasonal conversion, the asymmetry of moisture advection on the eastern and western sides of the anomalous anticyclonic circulations tended to lead to the circulation systems to move in an eastward direction until reaching the Northwest Pacific region. During the winter seasons with peak periods of El Niño events, the easterly anomalies in the equatorial West Pacific Ocean were found to stimulate the upturning Kelvin fluctuations in the ocean. This resulted in eastward spreading actions which eventually helped the El Niño events to transform into La Niña events.

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“…A number of previous studies have devoted great efforts into investigating the cloud-radiative feedbacks in climate system (Ramanthan et al 1989;Cess et al 1990;Sun and Held 1996;Soden 1997;Schneider et al 1999;Soden and Held 2006;Sun et al 2003Sun et al , 2006Sun et al , 2009Zhu et al 2007;Zhang and Sun 2008;Wu et al 2011;Zheng et al 2014;Li et al 2014Li et al , 2015. As El Niño-Southern Oscillation (ENSO) is the greatest natural climate variability on interannual timescale and exerts profound impacts on the global climate and weather (Philander 1990;Chen 2016, 2017a, b;Yang et al 2018), a frequently used method to quantify the cloud-radiative feedbacks is to calculate the response of cloud-radiative forcing to the sea surface temperature (SST) changes on the time scale of ENSO (Sun and Held 1996;Soden 1997;Sun et al 2003Sun et al , 2006Sun et al , 2009Chen et al 2013Chen et al , 2015Chen et al , 2017Hu et al 2017). For example, through calculating the response of cloud-radiative forcing to El Niño (hereinafter EN) warming, some previous studies evaluated the cloud-radiative feedbacks in the ENSO cycle in coupled model simulations (e.g., Sun and Held 1996;Soden 1997;Sun et al 2006;Sun et al 2009;Chen et al 2013Chen et al , 2016a.…”

Section: Introductionmentioning

confidence: 99%

Contrasting Cloud Radiative Feedbacks during Warm Pool and Cold Tongue El Niños

Chen

Wang

et al. 2018

SOLA

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The study presents the contrasting characteristics of cloudradiative feedbacks to the cold tongue (CT) and warm pool (WP) El Niño (EN). The maximum sea surface temperature anomalies (SSTA) of the CT-EN are located in the far-eastern Pacific. However, the maximum responses of the shortwave-and longwavecloud-radiative forcing (SWCRF and LWCRF) to the CT-EN warming are centered near the dateline, showing 70° westward shift relative to the maximum SSTA center of CT-WN. In contrast, the maximum responses of the SWCRF and LWCRF to the WP-EN warming show only slight westward shift relative to the maximum SSTA center. The contrasting cloud-radiative feedbacks to the two types of ENs can be traced back to the contrasting precipitation feedbacks, which is associated with the convection threshold. When the warm SSTA of CT-EN occurs in the relatively cold eastern Pacific, the total SST in-situ may not exceed the convection threshold. Therefore, the induced precipitation anomaly would occur towards the warm western Pacific, and the corresponding cloud cover and cloud-radiative feedbacks would exhibit an apparent westward shift. As the warm SSTA of WP-EN occurs in the relatively warm central Pacific, the corresponding responses of the anomalous fields to the WP-EN show only slight westward displacement.

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Why 1986 El Niño and 2005 La Niña evolved different from a typical El Niño and La Niña

Cited by 17 publications

References 52 publications

The diversity of La Niña decay and the corresponding spring and summer precipitation anomalies over eastern China

The diversity of La Niña decay and the corresponding spring and summer precipitation anomalies over eastern China

The negative feedback effects of sea surface temperatures on El Niño Events in the West Indian Ocean

Contrasting Cloud Radiative Feedbacks during Warm Pool and Cold Tongue El Niños

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