青藏高原未来气候变化预估:CMIP5模式结果

胡芩; 姜大膀; 范广洲

doi:10.3878/j.issn.1006-9895.1406.13325

青藏高原未来气候变化预估:CMIP5模式结果

doi: 10.3878/j.issn.1006-9895.1406.13325

1.
中国科学院大气物理研究所竺可桢—南森国际研究中心, 北京100029;成都信息工程学院, 成都610225
2.
中国科学院大气物理研究所竺可桢—南森国际研究中心, 北京100029;中国科学院气候变化研究中心, 北京100029
3.
成都信息工程学院, 成都610225

基金项目: 中国科学院战略性先导科技专项——青藏高原圈层相互作用及其资源环境效应项目XDB03020602, 国家重点基础研究发展计划(973计划)项目2012CB955401, 国家自然科学基金项目41375084、41175072

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出版历程
- 收稿日期: 2013-12-06
- 修回日期: 2014-08-25

Climate Change Projection on the Tibetan Plateau:Results of CMIP5 Models

1.
Nansen-Zhu International Research Centre, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029;Chengdu University of Information Technology, Chengdu 610225
2.
Nansen-Zhu International Research Centre, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029;Climate Change Research Center, Chinese Academy of Sciences, Beijing 100029
3.
Chengdu University of Information Technology, Chengdu 610225

摘要

摘要: 本文使用国际耦合模式比较计划第5阶段(CMIP5)中对青藏高原气候模拟较优的气候模式, 在RCP4.5中等偏低辐射强迫情景下对青藏高原未来气候变化进行了预估研究。结果表明, 青藏高原年均地表气温在2006~2100年的线性趋势平均为0.26℃/10a, 增暖幅度与海拔高度大体成正比;相比于1986~2005年参考时段, 2090年代平均升温2.7℃, 21世纪末期增温幅度明显高于早期和中期;在早、中和末期, 年均增温分别为0.8~1.3℃、1.6~2.5℃和2.1~3.1℃;各季节也均为变暖趋势, 其中冬季增温最大。对于年均降水来说, 未来百年将小幅增加, 集合平均趋势为1.15%/10a, 2090年代较参考时段增加10.4%;在早、中和末期的变化范围分别为-1.8%至15.2%、-0.9%至17.8%和1.4%至21.3%;季节降水也呈增加趋势, 夏季增幅明显高于其余三个季节且在21世纪末期较大, 青藏高原未来年均降水增加主要来自于夏季。需要指出的是, 上述预估结果在气候模式间存在着一定的差异, 未来气候变化的不确定性范围较大, 地表气温的可信度相对较高, 而降水的则偏低。
- CMIP5模式 /
- 青藏高原 /
- 气候变化 /
- 预估
Abstract: Climate change for the 21st century over the Tibetan Plateau (TP) is projected using multiple climate models within the phase five of the Coupled Model Intercomparison Project under the Representative Concentration Pathway 4.5 (RCP4.5) scenario.These models have a demonstrated ability to simulate modern climatology.The results show an annual warming trend of 0.26℃ per decade, which correlates positively with the topographical height in 2006-2100.With respect to the reference period 1986-2005, the TP annual temperature increases 2.7℃ in the 2090s, which is stronger than the warming in the early and middle 21st century.In the early, middle, and end periods, annual warming is 0.8-1.3℃, 1.6-2.5℃, and 2.1-3.1℃, respectively.Temperature increases are seen in all seasons, with the strongest warming occurring in winter.On the contrary, overall annual precipitation increases slightly on the TP, with a trend of 1.15% per decade during 2006-2100 and an increase of 10.4% in the 2090s relative to the reference period.Annual precipitation ranges from -1.8% to 15.2% in the early period, from -0.9% to 17.8% in the middle period, and from 1.4% to 21.3% in the end period.Precipitation generally increases in all seasons; the summer increase is larger compared with other seasons, particularly for the end of the 21st century.The annual precipitation increase occurs mainly in summer.It is noted that the above results differ somewhat among models, which indicates a relatively large level of uncertainty and a relatively high (low) reliability of temperature (precipitation) projection.
- CMIP5 models /
- Tibetan Plateau /
- Climate change /
- Projection

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参考文献(31)

[1]	Chen B, Chao W C, Liu X.2003.Enhanced climatic warming in the Tibetan Plateau due to doubling CO₂:A model study[J].Climate Dyn., 20 (4):401-413.
[2]	Chen H P, Sun J Q.2013.Projected change in East Asian summer monsoon precipitation under RCP scenario[J].Meteor.Atmos.Phys., 121 (1-2):55-77.
[3]	Duan A M, Wu G X, Zhang Q, et al.2006.New proofs of the recent climate warming over the Tibetan Plateau as a result of the increasing greenhouse gases emissions[J].Chinese Science Bulletin, 51 (11):1396-1400.
[4]	Ding Y H, Ren G Y, Zhao Z C, et al.2007.Detection, causes and projection of climate change over China:An overview of recent progress[J].Advances in Atmospheric Sciences, 24 (6):954-971.
[5]	高学杰, 李栋梁, 赵宗慈, 等.2003.温室效应对我国青藏高原及青藏铁路沿线气候影响的数值模拟[J].高原气象, 22 (5):458-463.Gao Xuejie, Li Dongliang, Zhao Zongci, et al.2003.Numerical simulation for influence of greenhouse effects on climatic change of Qinghai-Xizang Plateau along Qinghai-Xizang railway[J].Plateau Meteorology (in Chinese), 22 (5):458-463.
[6]	Gao X J, Shi Y, Zhang D F, et al.2012a.Climate change in China in the 21st century as simulated by a high resolution regional climate model[J].Chinese Science Bulletin, 57 (10):1188-1195.
[7]	Gao X J, Shi Y, Zhang D F, et al.2012b.Uncertainties in monsoon precipitation projections over China:Results from two high resolution RCM simulations[J].Climate Research, 52:213-226.
[8]	Gao X J, Wang M L, Giorgi F.2013.Climate change over China in the 21st century as simulated by BCC_CSM1.1-RegCM4.0[J].Atmospheric and Oceanic Science Letters, 6 (5):381-386.
[9]	Giorgi F, Hurrell J W, Marinucci M R, et al.1997.Elevation dependency of the surface climate change signal:A model study[J].J.Climate, 10 (2):288-296.
[10]	胡芩, 姜大膀, 范广洲.2014.CMIP5全球气候模式对青藏高原地区气候模拟能力评估[J].大气科学, 38 (5):924-938.Hu Qin, Jiang Dabang, Fan Guangzhou.2014.Evaluation of CMIP5 models over the Qinghai- Tibetan Plateau[J].Chinese Journal of Atmospheric Sciences (in Chinese), 38 (5):924-938.
[11]	IPCC.2013.Summary for Policymakers[M]// Stocker T F, Qin D, Plattner G K, et al.Climate Change 2013:The Physical Science Basis.Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change.Cambridge, United Kingdom and New York, NY, USA:Cambridge University Press, 1-27.
[12]	Jiang D B, Tian Z P.2013.East Asian monsoon change for the 21st century:Results of CMIP3 and CMIP5 models[J].Chinese Science Bulletin, 58 (12):1427-1435.
[13]	Jiang D B, Wang H J, Lang X M.2005.Evaluation of East Asian climatology as simulated by seven coupled models[J].Advances in Atmospheric Sciences, 22 (4):479-495.
[14]	Jiang D B, Zhang Y, Sun J Q.2009.Ensemble projection of 1-3℃ warming in China[J].Chinese Science Bulletin, 54 (18):3326-3334.
[15]	Lang X M, Sui Y.2013.Changes in mean and extreme climates over China with a 2℃ global warming[J].Chinese Science Bulletin, 58 (12):1453- 1461.
[16]	Li J F, Zhang Q, Chen Y Q, et al.2013.GCMs-based spatiotemporal evolution of climate extremes during the 21st century in China[J].Journal of Geophysical Research:Atmospheres, 118 (19):11017-11035.
[17]	Liu X D, Cheng Z G, Yan L B, et al.2009.Elevation dependency of recent and future minimum surface air temperature trends in the Tibetan Plateau and its surroundings[J].Global and Planetary Change, 68 (3):164-174.
[18]	Moss R H, Edmonds J A, Hibbard K A, et al.2010.The next generation of scenarios for climate change research and assessment[J].Nature, 463 (7282):747-756.
[19]	Qin J, Yang K, Liang S L, et al.2009.The altitudinal dependence of recent rapid warming over the Tibetan Plateau[J].Climatic Change, 97 (1-2):321-327.
[20]	Su F G, Duan X L, Chen D L, et al.2013.Evaluation of the global climate models in the CMIP5 over the Tibetan Plateau[J].J.Climate, 26 (10):3187-3208.
[21]	Sui Y, Jiang D B, Tian Z P.2013.Latest update of the climatology and changes in the seasonal distribution of precipitation over China[J].Theor.Appl.Climatol., 113 (3-4):599-610.
[22]	Sun J Q, Ao J.2013.Changes in precipitation and extreme precipitation in a warming environment in China[J].Chinese Science Bulletin, 58 (12):1395-1401.
[23]	Sun Y, Ding Y H.2010.A projection of future changes in summer precipitation and monsoon in East Asia[J].Science in China Series D:Earth Sciences, 53 (2):284-300.
[24]	Taylor K E, Stouffer B J, Meehl G A.2012.An o湶来??どづ???癦愠汃畍慉瑐椵漠湡?潤映?灨牥攠捥楸灰楥瑲慩瑭楥潮湴?獤楥浳畩汧慮瑛楊潝渮?極湬??慁獭瑥??獍楥慴湥?浲漮湓獯潣漮測?愹爳攠愨猴?戺礴?挵漭甴瀹永攮搼?潲挾敶慡湮?慖瑵浵潲獥灮栠敄爠敐?朠故湤敭牯慮汤?挠楊爬挠畋污慩瑮極潭湡?浍漬搠敥汴猠孡?崮??栱椱渮敔獨敥??潥異牲湥慳汥?潴晡??瑶浥漠獣灯桮散牥楮捴?卡捴楩敯湮挠数獡??楷湡??栺楁湮攠獯敶??????????至????????扃牨?婮桧潥甬?吱‰???失甭′利???社????呲眾敗湡瑮楧攠瑈栠?挬攠湚瑥畮牧礠?猠畃爬映慚捨敡?慧椠牘?瑈攮洱瀹改爳愮瑔畨牥攠?潵癭敥牲??桡楬渠慳?慭湵摬?瑴桩敯?朠汯潦戠整?獥椠浣畬汩慭瑡整摩?戠祣?捡潮畧灥氠散摡?捳汥楤洠慢瑹攠?浏漼摳敵汢猾嬲?崯????氠楤浯慵瑢敬??????金??????????????扮牡?婓桥潲畩?塳????婨桥慭潩?側???栠攳渶??????攵琱?愴氶?金?ぢ???淑灜愬挠璊玆?漲昰‰琴栮攵爪海演搦礈渡意洡槟挜?瀺狟演挙旽玛玄攝獥?澐癛敊牝?琔栙攎?咃椔扶攬琠愹渠?倲氩愺琲攴愰甭′漵渰?瑗桡敮?丠潓牨瑵桹敵爬渠??敯浮楧猠灚桨敥爮椲挰‰挴氮楔浨慥琠数孲?嵬?卭捩楮敡湲捹攠?楮湡??桳楩湳愠?卦攠爵椠散獯????慤爠瑯档?卡据椭敡湴捭敯獳???????????????????? models simulation of regional climate in Asia[J].Climatic and Environmental Research (in Chinese), 9 (2):240-250.
[25]	吴国雄, 刘屹岷, 刘新, 等.2005.青藏高原加热如何影响亚洲夏季的气候格局[J].大气科学, 29 (1):47-56.Wu Guoxiong, Liu Yimin, Liu Xin, et al.2005.How the heating over the Tibetan Plateau affects the Asian climate in summer[J].Chinese Journal of Atmospheric Sciences (in Chinese), 29 (1):47-56.
[26]	许崇海, 沈新勇, 徐影.2007.IPCC AR4模式对东亚地区气候模拟能力的分析[J].气候变化研究进展, 3 (5):287-292.Xu Chonghai, Shen Xinyong, Xu Ying.2007.An analysis of climate change in East Asia by using the IPCC AR4 simulations[J].Advances in Climate Change Research (in Chinese), 3 (5):287-292.
[27]	徐影, 丁一汇, 李栋梁.2003.青藏地区未来百年气候变化[J].高原气象, 22 (5):451-457.Xu Ying, Ding Yihui, Li Dongliang.2003.Climatic change over Qinghai and Xizang in 21st century[J].Plateau Meteorology (in Chinese), 22 (5):451-457.
[28]	Xu C H, Xu Y.2012.The projection of temperature and precipitation over China under RCP scenarios using a CMIP5 multi-model ensemble[J].Atmospheric and Oceanic Science Letters, 5 (6):527-533.
[29]	Xu Y, Xu C H, Gao X J, et al.2009.Projected changes in temperature and precipitation extremes over the Yangtze River basin of China in the 21st century[J].Quaternary International, 208 (1-2):44-52.
[30]	Yu Y Q, Zhi H, Wang B, et al.2008.Coupled model simulations of climate changes in the 20th century and beyond[J].Advances in Atmospheric Sciences, 25 (4):641-654.
[31]	张莉, 丁一汇, 孙颖.2008.全球海气耦合模式对东亚季风降水模拟的检验[J].大气科学, 32 (2):261-276.Zhang Li, Ding Yihui, Sun Yi