Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature
ABSTRACT Previous studies suggested that the variability of boreal spring Arctic Oscillation ( AO ) can exert a significant influence on the sea surface temperature ( SST ) anomalies in the Niño‐3.4 region during the following winter. This study further reveals that AO in November can have a pronoun...
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crwiley:10.1002/joc.4288 2024-06-23T07:50:08+00:00 Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature Chen, Shangfeng Wu, Renguang Chen, Wen Yu, Bin Chinese Academy of Sciences National Natural Science Foundation of China 2015 http://dx.doi.org/10.1002/joc.4288 https://api.wiley.com/onlinelibrary/tdm/v1/articles/10.1002%2Fjoc.4288 https://rmets.onlinelibrary.wiley.com/doi/pdf/10.1002/joc.4288 en eng Wiley http://onlinelibrary.wiley.com/termsAndConditions#vor International Journal of Climatology volume 35, issue 14, page 4307-4317 ISSN 0899-8418 1097-0088 journal-article 2015 crwiley https://doi.org/10.1002/joc.4288 2024-06-04T06:40:28Z ABSTRACT Previous studies suggested that the variability of boreal spring Arctic Oscillation ( AO ) can exert a significant influence on the sea surface temperature ( SST ) anomalies in the Niño‐3.4 region during the following winter. This study further reveals that AO in November can have a pronounced influence on the tropical central‐eastern Pacific SST anomalies during the following spring and summer. When the November AO is in its positive (negative) phase, SST anomalies tend to be positive (negative) during the following spring and summer in the tropical central‐eastern Pacific. The influence of the AO is accomplished by atmospheric circulation anomalies over the subtropical North Pacific through an interaction between the synoptic‐scale eddy and the low‐frequency mean flow. In the positive November AO years, pronounced cyclonic circulation and atmospheric heating anomalies are observed over the subtropical North Pacific. The atmospheric heating anomalies sustain westerly wind anomalies over the tropical western North Pacific through a Gill‐like atmospheric response. The westerly wind anomalies extend eastward subsequently through positive air–sea feedback mechanism, and result in SST warming during the following spring and summer in the tropical central‐eastern Pacific. Results of this study imply that the November AO index can be used as an effective predictor of SST anomalies in the Niño‐3.4 region during the following spring and summer. Article in Journal/Newspaper Arctic Wiley Online Library Arctic Pacific International Journal of Climatology 35 14 4307 4317 |
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Open Polar |
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Wiley Online Library |
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crwiley |
language |
English |
description |
ABSTRACT Previous studies suggested that the variability of boreal spring Arctic Oscillation ( AO ) can exert a significant influence on the sea surface temperature ( SST ) anomalies in the Niño‐3.4 region during the following winter. This study further reveals that AO in November can have a pronounced influence on the tropical central‐eastern Pacific SST anomalies during the following spring and summer. When the November AO is in its positive (negative) phase, SST anomalies tend to be positive (negative) during the following spring and summer in the tropical central‐eastern Pacific. The influence of the AO is accomplished by atmospheric circulation anomalies over the subtropical North Pacific through an interaction between the synoptic‐scale eddy and the low‐frequency mean flow. In the positive November AO years, pronounced cyclonic circulation and atmospheric heating anomalies are observed over the subtropical North Pacific. The atmospheric heating anomalies sustain westerly wind anomalies over the tropical western North Pacific through a Gill‐like atmospheric response. The westerly wind anomalies extend eastward subsequently through positive air–sea feedback mechanism, and result in SST warming during the following spring and summer in the tropical central‐eastern Pacific. Results of this study imply that the November AO index can be used as an effective predictor of SST anomalies in the Niño‐3.4 region during the following spring and summer. |
author2 |
Chinese Academy of Sciences National Natural Science Foundation of China |
format |
Article in Journal/Newspaper |
author |
Chen, Shangfeng Wu, Renguang Chen, Wen Yu, Bin |
spellingShingle |
Chen, Shangfeng Wu, Renguang Chen, Wen Yu, Bin Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature |
author_facet |
Chen, Shangfeng Wu, Renguang Chen, Wen Yu, Bin |
author_sort |
Chen, Shangfeng |
title |
Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature |
title_short |
Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature |
title_full |
Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature |
title_fullStr |
Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature |
title_full_unstemmed |
Influence of the November Arctic Oscillation on the subsequent tropical Pacific sea surface temperature |
title_sort |
influence of the november arctic oscillation on the subsequent tropical pacific sea surface temperature |
publisher |
Wiley |
publishDate |
2015 |
url |
http://dx.doi.org/10.1002/joc.4288 https://api.wiley.com/onlinelibrary/tdm/v1/articles/10.1002%2Fjoc.4288 https://rmets.onlinelibrary.wiley.com/doi/pdf/10.1002/joc.4288 |
geographic |
Arctic Pacific |
geographic_facet |
Arctic Pacific |
genre |
Arctic |
genre_facet |
Arctic |
op_source |
International Journal of Climatology volume 35, issue 14, page 4307-4317 ISSN 0899-8418 1097-0088 |
op_rights |
http://onlinelibrary.wiley.com/termsAndConditions#vor |
op_doi |
https://doi.org/10.1002/joc.4288 |
container_title |
International Journal of Climatology |
container_volume |
35 |
container_issue |
14 |
container_start_page |
4307 |
op_container_end_page |
4317 |
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1802641009202429952 |