# 全球变暖下热带降水变化研究回顾与挑战*

1.中国科学院大气物理研究所,季风系统研究中心, 北京 100190
2.中国科学院大气物理研究所,大气科学和地球流体力学数值模拟国家重点实验室, 北京 100029
3. 全球变化与可持续发展协同创新中心, 北京 100875
4.中国科学院大学, 北京 100049

# Advances and Challenges in the Study on the Tropical Rainfall Changes Under Global Warming*

Huang Ping123, Zhou Shijie24

1.Center for Monsoon System Research, Institute of Atmospheric Physics, Chinese Academy of Sciences,Beijing 100190,China
2.State Key Laboratory of Numerical Modeling for Atmospheric Sciences and Geophysical Fluid Dynamics,Institute of Atmospheric Physics, Chinese Academy of Sciences,Beijing 100029, China
3.Joint Center for Global Change Studies (JCGCS), Beijing 100875, China
4.University of Chinese Academy of Sciences, Beijing 100049, China

First author:Huang Ping (1982-), male, Zizhong County, Sichuan Province, Professor. Research areas include tropical air-sea interaction and climate change. E-mail: huangping@mail.iap.ac.cn

Abstract

Since tropical rainfall is important in the global energy and hydrologic cycle, the tropical rainfall changes under global warming have attracted extensive attention around the world in recent decades. The advances in the observational studies and model projection for the tropical rainfall changes under global warming were reviewed here. The frontiers in the mechanism of regional tropical rainfall changes and the approaches of rainfall change research are summarized. The large intermodel spread in the multi-model projections, the sources of uncertainty and the methods to reduce the uncertainty were also introduced. Finally, the challenges about the tropical rainfall changes were discussed.

Keywords： Tropical rainfall ; Global warming ; Climate change projection ; Moisture budget ; Model comparison.

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Huang Ping, Zhou Shijie. Advances and Challenges in the Study on the Tropical Rainfall Changes Under Global Warming*[J]. Advances in Earth Science, 2018, 33(11): 1181-1192 https://doi.org/10.11867/j.issn.1001-8166.2018.11.1181.

## 2 观测研究

(a)温度与水汽的关系;(b)温度与降水的关系;(c)地表净向下辐射与降水的关系;(d)大气净辐射冷却与降水的关系

Fig.1   The relationship between projected changes and projected temperature and rainfall changes simulated in the CMIP3 models under global warming[23]
(a) Temperature change vs. column-integrated water vapor change; (b)Temperature change vs. precipitation change;(c)Precipitation change vs. net downward radiation change at the surface; (d) Precipitation change vs. net radiative cooling change of the atmosphere

## 3 水汽增加对降水的作用和整体降水变化的能量约束

$ΔRsfc+ΔRatm=LΔP,(1)$

## 4 区域降水变化的水汽通量展开及变化机制

$ΔPC=1ρwg-∫0psω20∂Δq∂p-∫0psΔω∂q20∂p-Δ(∫0psu·∇q)+ΔE+residual,(2)ΔPS=1ρwg(-∫0ps∇·(u20Δq)dp-∫0ps∇·[q20Δu)dp]+ΔE+residual。$(3)

Huang等[10]在热带降水变化的研究中,使用一种更简洁的水汽收支方程。该简化方法考虑将大气层分为2层的简化模型,上层为自由大气,下层为边界层,主要保留了热力项与动力项。简化过的水汽收支方程可由方程(2)推导而来:

$ΔP≈-1ρwg(Δq·ω+q·Δω),(4)$

(a)500 hPa垂直速度变化;(b)动力项;(c)热力项;(d)两者之和[10]

Fig.2   Seasonal cycle of circulation change and decomposition of precipitation change under global warming
(a) Circulation change at 500 hPa; (b) Dynamic component;(c) Thermodynamic component;(d) The sum of dynamic and thermodynamic components [10]

(a)动力项;(b)热力项;(c)两者的总和;(a)绿色曲线为热力项的-3×10-3 Pa/(s·102)等值线;(c)红色曲线为降水变化0.4 mm/d等值线[8]

Fig.3   The decomposition of annual-mean rainfall changes under global warming
(a)The dynamic component; (b) Thermodynamic components; (c) The sum of dynamic and thermodynamic components. In (a), the green curves are the -3×10-3 Pa/(s·102) contour of thermodynamic component; In (c), the red curves are the 0.4 mm/d contour of rainfall change[8]

## 5 目前热带降水变化研究的前沿方向

### 5.1 热带降水变率的年际变化

$ΔP'=1ρwg(-∫0ps∇·(uΔq')dp-∫0ps∇·(qΔu')dp)+ΔE'+residual,(4)ΔP'≈-1ρwg[Δq·ω'+q·(Δω'a+Δω's1+Δω's2)],$(5)

Fig.4   Diagram illustrating the formation mechanisms of the changes in ENSO-driven rainfall variability

### 5.3 模式预估不确定性及偏差校订

Huang等[76]针对热带海温、降水等空间非均一的气候变化预估,扩展了最初针对区域平均的“观测约束”思想和方法,提出一个“空间分布型多模式回归校订”的思路和方法(Ensemble Pattern Regression, EPR)。利用此方法Huang等[76]校订了多模式预估的热带太平洋海温增暖型和热带太平洋降水(图5)。对海温,模式中普遍存在冷舌过强、东南太平洋暖偏差、暖池较窄等系统性误差(图5a),“观测约束”校订指出这些偏差将在全球变暖背景下导致模式模拟出类似于拉尼娜型的海温增暖偏差,当把这种偏差去除之后,未来热带太平洋地区的海温增暖型将呈现为更典型的类厄尔尼诺型分布(图5c)。背景态海温的系统性误差将导致未来中东太平洋降水偏低而西太平洋降水偏高。在多模式集合的预估结果中除去这些共性偏差后,中东太平洋的降水显著增强而西太平洋降水减弱,表现为更明显的“湿更湿”的降水变化分布型,与校订后的海温变化空间分布型相匹配。

(a)模式预估的未来降水(填色),1 000 hPa风和相对海温的变化;(b)利用EPR方法估计的预估的未来降水(填色),风和相对海温变化的共同偏差;(c)经过校订之后的降水(填色),1 000 hPa风和相对海温的变化[76]

Fig.5   The comparison between the corrected and original precipitation change
(a) Projected changes in precipitation (shaded), 1 000 hPa wind and relative SST; (b) Estimated change biases in precipitation (shaded) and 1 000 hPa wind; (c) Corrected changes in precipitation (shaded), 1 000 hPa wind (vectors), and relative SST[76]

## 6 结语及展望

The authors have declared that no competing interests exist.

## 参考文献 原文顺序 文献年度倒序 文中引用次数倒序 被引期刊影响因子

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As climate warms, features of the changes in both the atmospheric and ocean circulation over the tropical Pacific Ocean resemble "El Nio-like" conditions; however, the mechanisms are shown to be distinct from those of El Nio and are reproduced in both mixed-layer and full ocean dynamics coupled climate models. Even though the mechanisms and structure differ from El Nio, aspects of climate teleconnections resemble those associated with El Nio. Changes seen in the consensus of models presented here are also consistent with recently detected changes in the tropical circulation during the 20^t^h Century. [24] Greve P,Orlowsky B,Mueller B, et al. Global assessment of trends in wetting and drying over land[J]. Nature Geoscience, 2014, 7(10): 716-721. Changes in the hydrological conditions of the land surface have substantial impacts on society1, 2. Yet assessments of observed continental dryness trends yield contradicting results3, 4, 5, 6, 7. The concept that dry regions dry out further, whereas wet regions become wetter as the climate warms has been proposed as a simplified summary of expected8, 9, 10 as well as observed10, 11, 12, 13, 14 changes over land, although this concept is mostly based on oceanic data8, 10. Here we present an analysis of more than 300 combinations of various hydrological data sets of historical land dryness changes covering the period from 1948 to 2005. Each combination of data sets is benchmarked against an empirical relationship between evaporation, precipitation and aridity. Those combinations that perform well are used for trend analysis. We find that over about three-quarters of the global land area, robust dryness changes cannot be detected. Only 10.8% of the global land area shows a robustry gets drier, wet gets wetter pattern, compared to 9.5% of global land area with the opposite pattern, that is, dry gets wetter, and wet gets drier. We conclude that aridity changes over land, where the potential for direct socio-economic consequences is highest, have not followed a simple intensification of existing patterns. [25] Hegerl G C,Black E,Allan R P, et al. Challenges in quantifying changes in the global water cycle[J]. Bulletin of the American Meteorological Society, 2015, 96(7): 1 097-1 115. [26] Neelin J D,Münnich M,Su H, et al. Tropical drying trends in global warming models and observations[J]. Proceedings of the National Academy of Sciences, 2006, 103(16): 6 110-6 115. Anthropogenic changes in tropical rainfall are evaluated in a multimodel ensemble of global warming simulations. Major discrepancies on the spatial distribution of these precipitation changes remain in the latest-generation models analyzed here. Despite this uncertainty, we find a number of measures, both global and local, on which reasonable agreement is obtained, notably for the regions of drying trend (negative precipitation anomalies). Models agree on the overall amplitude of the precipitation decreases that occur at the margins of the convective zones, with percent error bars of magnitude similar to those for the tropical warming. Similar agreement is found on a precipitation climate sensitivity defined here and on differential moisture increase inside and outside convection zones, a step in a hypothesized causal path leading to precipitation changes. A measure of local intermodel agreement on significant trends indicates consistent predictions for particular regions. Observed rainfall trends in several data sets show a significant summer drying trend in a main region of intermodel agreement: the Caribbean/Central-American region. [27] Chadwick R, Good P, Martin G, et al. Large rainfall changes consistently projected over substantial areas of tropical land[J]. Nature Climate Change, 2015, 6(2): 177-181. Many tropical countries are exceptionally vulnerable to changes in rainfall patterns, with floods or droughts often severely affecting human life and health, food and water supplies, ecosystems and infrastructure. There is widespread disagreement among climate model projections of how and where rainfall will change over tropical land at the regional scales relevant to impacts, with different models predicting the position of current tropical wet and dry regions to shift in different ways. Here we show that despite uncertainty in the location of future rainfall shifts, climate models consistently project that large rainfall changes will occur for a considerable proportion of tropical land over the twenty-first century. The area of semi-arid land affected by large changes under a higher emissions scenario is likely to be greater than during even the most extreme regional wet or dry periods of the twentieth century, such as the Sahel drought of the late 1960s to 1990s. Substantial changes are projected to occur by mid-century--earlier than previously expected--and to intensify in line with global temperature rise. Therefore, current climate projections contain quantitative, decision-relevant information on future regional rainfall changes, particularly with regard to climate change mitigation policy. [28] Zhang X, Zwiers F W, Hegerl G C, et al. Detection of human influence on twentieth-century precipitation trends[J]. Nature, 2007, 448(7 152): 461-465. Abstract Human influence on climate has been detected in surface air temperature, sea level pressure, free atmospheric temperature, tropopause height and ocean heat content. Human-induced changes have not, however, previously been detected in precipitation at the global scale, partly because changes in precipitation in different regions cancel each other out and thereby reduce the strength of the global average signal. Models suggest that anthropogenic forcing should have caused a small increase in global mean precipitation and a latitudinal redistribution of precipitation, increasing precipitation at high latitudes, decreasing precipitation at sub-tropical latitudes, and possibly changing the distribution of precipitation within the tropics by shifting the position of the Intertropical Convergence Zone. Here we compare observed changes in land precipitation during the twentieth century averaged over latitudinal bands with changes simulated by fourteen climate models. We show that anthropogenic forcing has had a detectable influence on observed changes in average precipitation within latitudinal bands, and that these changes cannot be explained by internal climate variability or natural forcing. We estimate that anthropogenic forcing contributed significantly to observed increases in precipitation in the Northern Hemisphere mid-latitudes, drying in the Northern Hemisphere subtropics and tropics, and moistening in the Southern Hemisphere subtropics and deep tropics. The observed changes, which are larger than estimated from model simulations, may have already had significant effects on ecosystems, agriculture and human health in regions that are sensitive to changes in precipitation, such as the Sahel. [29] Ma J, Xie S P.Regional patterns of sea surface temperature change: A source of uncertainty in future projections of precipitation and atmospheric circulation[J]. Journal of Climate, 2013, 26(8): 2 482-2 501. [30] Ma J,Chadwick R,Seo K H, et al. Responses of the tropical atmospheric circulation to climate change and connection to the hydrological cycle[J]. Annual Review of Earth and Planetary Sciences, 2018, 46(1): 549-580. Projected changes in regional seasonal precipitation due to climate change are highly uncertain, with model disagreement on even the sign of change in many regions. Using a 20-member CMIP5 ensemble under the RCP8.5 scenario, the intermodel uncertainty of the spatial patterns of projected end-of-twenty-first-century change in precipitation is found not to be strongly influenced by uncertainty... [Show full abstract] [31] Allan R P, Soden B J.Atmospheric warming and the amplification of precipitation extremes[J]. Science, 2008, 321(5 895): 1 481-1 484. Climate models suggest that extreme precipitation events will become more common in an anthropogenically warmed climate. However, observational limitations have hindered a direct evaluation of model-projected changes in extreme precipitation. We used satellite observations and model simulations to examine the response of tropical precipitation events to naturally driven changes in surface temperature and atmospheric moisture content. These observations reveal a distinct link between rainfall extremes and temperature, with heavy rain events increasing during warm periods and decreasing during cold periods. Furthermore, the observed amplification of rainfall extremes is found to be larger than that predicted by models, implying that projections of future changes in rainfall extremes in response to anthropogenic global warming may be underestimated. [32] Lenderink G, Van Meijgaard E.Increase in hourly precipitation extremes beyond expectations from temperature changes[J]. Nature Geoscience, 2008, 1(8): 511-514. Changes in precipitation extremes under greenhouse warming are commonly assumed to be constrained by changes in the amounts of precipitable water in the atmosphere. Global climate models generally predict only marginal changes in relative humidity, implying that the actual amount of atmospheric precipitable water scales with the water vapour content of saturation, which is governed by the Clausius-Clapeyron relation. Indeed, changes in daily precipitation extremes in global climate models seem to be consistent with the 7% increase per degree of warming given by the Clausius-Clapeyron relation, but it is uncertain how general this scaling behaviour is across timescales. Here, we analyse a 99-year record of hourly precipitation observations from De Bilt, the Netherlands, and find that one-hour precipitation extremes increase twice as fast with rising temperatures as expected from the Clausius-Clapeyron relation when daily mean temperatures exceed 12C. In addition, simulations with a high-resolution regional climate model show that one-hour precipitation extremes increase at a rate close to 14% per degree of warming in large parts of Europe. Our results demonstrate that changes in short-duration precipitation extremes may well exceed expectations from the Clausius-Clapeyron relation. These short-duration extreme events can have significant impacts, such as local flooding, erosion and water damage. [33] Trenberth K E.Atmospheric moisture residence times and cycling: Implications for rainfall rates and climate change[J]. Climatic Change, 1998, 39(4): 667-694. New estimates of the moistening of the atmosphere through evaporation at the surface and of the drying through precipitation are computed. Overall, the e-folding residence time of atmospheric moisture is just over 8 days. New estimates are also made of how much moisture that precipitates out comes from horizontal transport versus local evaporation, referred to as ecycling. The results depend greatly on the scale of the domain under consideration and global maps of the recycling for annual means are produced for 500 km scales for which global recycling is 9.6%, consisting of 8.9% over land and 9.9% over the oceans. Even for 1000 km scales, less than 20% of the annual precipitation typically comes from evaporation within the domain. While average overall atmospheric moisture depletion and restoration must balance, precipitation falls only a small fraction of the time. Thus precipitation rates are also examined. Over the United States, one hour intervals with 0.1 mm or more are used to show that the frequency of precipitation ranges from over 30% in the Northwest, to about 20% in the Southeast and less than 4% just east of the continental divide in winter, and from less than 2% in California to over 20% in the Southeast in summer. In midlatitudes precipitation typically falls about 10% of the time, and so rainfall rates, conditional on when rain is falling, are much larger than evaporation rates. The mismatches in the rates of rainfall versus evaporation imply that precipitating systems of all kinds feed mostly on the moisture already in the atmosphere. Over North America, much of the precipitation originates from moisture advected from the Gulf of Mexico and subtropical Atlantic or Pacific a day or so earlier. Increases in greenhouse gases in the atmosphere produce global warming through an increase in downwelling infrared radiation, and thus not only increase surface temperatures but also enhance the hydrological cycle, as much of the heating at the surface goes into evaporating surface moisture. Global temperature increases signify that the water-holding capacity of the atmosphere increases and, together with enhanced evaporation, this means that the actual atmospheric moisture should increase. It follows that naturally-occurring droughts are likely to be exacerbated by enhanced potential evapotranspiration. Further, globally there must be an increase in precipitation to balance the enhanced evaporation but the processes by which precipitation is altered locally are not well understood. Observations confirm that atmospheric moisture is increasing in many places, for example at a rate of about 5% per decade over the United States. Based on the above results, we argue that increased moisture content of the atmosphere therefore favors stronger rainfall or snowfall events, thus increasing risk of flooding, which is a pattern observed to be happening in many parts of the world. Moreover, because there is a disparity between the rates of increase of atmospheric moisture and precipitation, there are implied changes in the frequency of precipitation and/or efficiency of precipitation (related to how much moisture is left behind in a storm). However, an analysis of linear trends in the frequency of precipitation events for the United States corresponding to thresholds of 0.1 and 1 mm/h shows that the most notable statistically significant trends are for increases in the southern United States in winter and decreases in the Pacific Northwest from November through January, which may be related to changes in atmospheric circulation and storm tracks associated with El Nio outhern Oscillation trends. It is suggested that as the physical constraints on precipitation apply only globally, more attention should be paid to rates in both observations and models as well as the frequency of occurrence. [34] Boer G J.Climate change and the regulation of the surface moisture and energy budgets[J]. Climate Dynamics, 1993, 8(5): 225-239. The increase in the vigor of the hydrological cycle simulated in a 2 CO 2 experiment with the Canadian Climate Centre general circulation model is smaller than that obtained by other models which have similar increases in mean surface temperature. The surface energy budget, which encompasses also the moisture budget for the oceans, is analyzed. Changes in the net radiative input to and sensible heat flux from the surface act to warm it. This is balanced, at the new equilibrium, by a change in the latent heat flux which acts to cool it. Although this same general behavior is seen in other models, the increase in radiative input to the surface in the CCC GCM is smaller than in other models while the change in the sensible heat flux is of similar size. As a consequence, the latent heat flux required for balance is smaller. The comparatively small increase in the net radiative input at the surface occurs because of a decrease in the solar component. On average the decrease in solar input in the tropical region outweighs the higher latitude increase associated with the snow/ice albedo feedback. The notable tropical decrease in solar input occurs because the albedo of the clouds increase enough in this region to outweigh a small decrease in cloud amount. The increase in cloud albedo in the warmer and moister tropical atmosphere is a consequence of the parameterized cloud optical properties in the model which play an important role in the regulation of the surface energy and moisture budgets. The results demonstrate some of the consequences of the negative feedback mechanism associated with increasing cloud albedo in the model. They also suggest that the simulated change in the vigor of the hydrological cycle is not a simple function of the average increase in surface temperature but is a consequence of all of the processes in the model which control the available energy at the surface as a function of latitude. [35] Allen M R,Ingram W J.Constraints on future changes in climate and the hydrologic cycle[J]. Nature, 2002, 419(6 903): 224-232. Abstract What can we say about changes in the hydrologic cycle on 50-year timescales when we cannot predict rainfall next week? Eventually, perhaps, a great deal: the overall climate response to increasing atmospheric concentrations of greenhouse gases may prove much simpler and more predictable than the chaos of short-term weather. Quantifying the diversity of possible responses is essential for any objective, probability-based climate forecast, and this task will require a new generation of climate modelling experiments, systematically exploring the range of model behaviour that is consistent with observations. It will be substantially harder to quantify the range of possible changes in the hydrologic cycle than in global-mean temperature, both because the observations are less complete and because the physical constraints are weaker. [36] Stephens G L,Ellis T D.Controls of global-mean precipitation increases in global warming gcm experiments[J]. Journal of Climate, 2008, 21(23): 6 141-6 155. The main findings of this paper are threefold. First, increases in the global precipitation track increase atmospheric radiative energy loss and the ratio of precipitation sensitivity to water vapor sensitivity is primarily determined by changes to this atmospheric column energy loss. A reference limit to this ratio is introduced as the rate at which the emission of radiation from the clear-sky atmosphere increases as water vapor increases. It is shown that the derived efficiency based on the simple ratio of precipitation to water vapor sensitivities of models in fact closely matches the sensitivity derived from simple energy balance arguments involving changes to water vapor emission alone. Second, although the rate of increase of clear-sky emission is the dominant factor in the change to the energy balance of the atmosphere, there are two important and offsetting processes that contribute to in the model simulations studied: One involves a negative feedback through cloud radiative heating that acts to reduce the efficiency; the other is the global reduction in sensible heating that counteracts the effects of the cloud feedback and increases the efficiency. These counteracting feedbacks only apply on the global scale. Third, the negative cloud radiative heating feedback occurs through reductions of cloud amount in the middle troposphere, defined as the layer between 680 and 440 hPa, and by slight global cloud decreases in the lower troposphere. These changes act in a manner to expose the warmer atmosphere below to high clouds, thus resulting in a net warming of the atmospheric column by clouds and a negative feedback on the precipitation. [37] Stephens G L,Li J,Wild M, et al. An update on Earth's energy balance in light of the latest global observations[J]. Nature Geoscience, 2012, 5(10): 691-696. Climate change is governed by changes to the global energy balance. At the top of the atmosphere, this balance is monitored globally by satellite sensors that provide measurements of energy flowing to and from Earth. By contrast, observations at the surface are limited mostly to land areas. As a result, the global balance of energy fluxes within the atmosphere or at Earth's surface cannot be derived directly from measured fluxes, and is therefore uncertain. This lack of precise knowledge of surface energy fluxes profoundly affects our ability to understand how Earth's climate responds to increasing concentrations of greenhouse gases. In light of compilations of up-to-date surface and satellite data, the surface energy balance needs to be revised. Specifically, the longwave radiation received at the surface is estimated to be significantly larger, by between 10 and 17 Wm612, than earlier model-based estimates. Moreover, the latest satellite observations of global precipitation indicate that more precipitation is generated than previously thought. This additional precipitation is sustained by more energy leaving the surface by evaporation — that is, in the form of latent heat flux — and thereby offsets much of the increase in longwave flux to the surface. [38] Richter I,Xie S P.Muted precipitation increase in global warming simulations: A surface evaporation perspective[J]. Journal of Geophysical Research, 2008, 113(D24). DOI:10.1029/2008JD010561. [1] Atmospheric moisture content is expected to rise in response to global warming, but climate models predict a much slower rate of precipitation increase. This muted response of the hydrological cycle is investigated from a surface evaporation perspective, using a multimodel ensemble of simulations under the A1B forcing scenario. A 90-year analysis of surface evaporation based on a standard bulk formula reveals that the following atmospheric changes act to slow down the increase in surface evaporation over ice-free oceans: surface relative humidity increases by 1.0%, surface stability, as measured by air-sea temperature difference, increases by 0.2 K, and surface wind speed decreases by 0.02 m/s. As a result of these changes, surface evaporation increases by only 2% per Kelvin of surface warming, rather than the 7%/K rate simulated for atmospheric moisture. The increased surface stability and relative humidity are robust across models. The former is nearly uniform over ice-free oceans while the latter features a subtropical peak on either side of the equator. While relative humidity changes are positive almost everywhere in a thin surface layer, changes aloft show positive trends in the deep tropics and negative ones in the subtropics. The surface-trapped structure suggests the following mechanism: owing to its thermal inertia, the ocean lags behind the atmospheric warming, and this retarding effect causes an increase in surface stability and relative humidity, analogously to advection fog. Our results call for observational efforts to monitor and detect changes in surface relative humidity and stability over the world ocean. [39] Vecchi G A,Soden B J,Wittenberg A T, et al. Weakening of tropical Pacific atmospheric circulation due to anthropogenic forcing[J]. Nature, 2006, 441(7 089): 73-76. Abstract Since the mid-nineteenth century the Earth's surface has warmed, and models indicate that human activities have caused part of the warming by altering the radiative balance of the atmosphere. Simple theories suggest that global warming will reduce the strength of the mean tropical atmospheric circulation. An important aspect of this tropical circulation is a large-scale zonal (east-west) overturning of air across the equatorial Pacific Ocean--driven by convection to the west and subsidence to the east--known as the Walker circulation. Here we explore changes in tropical Pacific circulation since the mid-nineteenth century using observations and a suite of global climate model experiments. Observed Indo-Pacific sea level pressure reveals a weakening of the Walker circulation. The size of this trend is consistent with theoretical predictions, is accurately reproduced by climate model simulations and, within the climate models, is largely due to anthropogenic forcing. The climate model indicates that the weakened surface winds have altered the thermal structure and circulation of the tropical Pacific Ocean. These results support model projections of further weakening of tropical atmospheric circulation during the twenty-first century. [40] Chou C,Neelin J D.Mechanisms of global warming impacts on regional tropical precipitation[J]. Journal of Climate, 2004, 17: 2 688-2 701. Mechanisms that determine the tropical precipitation anomalies under global warming are examined in an intermediate atmospheric model coupled with a simple land surface and a mixed layer ocean. To compensate for the warm tropospheric temperature, atmospheric boundary layer (ABL) moisture must increase to maintain positive convective available potential energy (CAPE) in convective regions. In nonconvective regions, ABL moisture is controlled by different balances and does not increase as much, creating a spatial gradient of ABL moisture anomalies. Associated with this spatial pattern of the ABL moisture anomalies are two main mechanisms responsible for the anomalous tropical precipitation. In the “upped-ante mechanism,” increases in ABL moisture are opposed by imported dry air wherever inflow from nonconvective regions over margins of convective regions occurs. The ABL moisture is not enough to meet the higher “convective ante” induced by the warmer tropospheric temperature, so precipitation is decreased. In the “anomalous gross moist stability mechanism,” gross moist stability is reduced due to increased ABL moisture. As a result, convection is enhanced and precipitation becomes heavier over convective regions. While the upped-ante mechanism induces negative precipitation anomalies over the margins of convective regions, the anomalous gross moist stability mechanism induces positive precipitation anomalies within convective regions. The importance of variation in gross moist stability, which is likely to differ among climate models, is suggested as a potential factor causing discrepancies in the predicted regional tropical precipitation changes.
[41] Seager R, Naik N, Vecchi G A.Thermodynamic and dynamic mechanisms for large-scale changes in the hydrological cycle in response to global warming[J]. Journal of Climate, 2010, 23(17): 4 651-4 668. The mechanisms of changes in the large-scale hydrological cycle projected by 15 models participating in the Coupled Model Intercomparison Project phase 3 and used for the Intergovernmental Panel on Climate Change0964s Fourth Assessment Report are analyzed by computing differences between 2046 and 2065 and 1961 and 2000. The contributions to changes in precipitation minus evaporation, P 0903’ E, caused thermodynamically by changes in specific humidity, dynamically by changes in circulation, and by changes in moisture transports by transient eddies are evaluated. The thermodynamic and dynamic contributions are further separated into advective and divergent components. The nonthermodynamic contributions are then related to changes in the mean and transient circulation. The projected change in P 0903’ E involves an intensification of the existing pattern of P 0903’ E with wet areas [the intertropical convergence zone (ITCZ) and mid- to high latitudes] getting wetter and arid and semiarid regions of the subtropics getting drier. In addition, the subtropical dry zones expand poleward. The accentuation of the twentieth-century pattern of P 0903’ E is in part explained by increases in specific humidity via both advection and divergence terms. Weakening of the tropical divergent circulation partially opposes the thermodynamic contribution by creating a tendency to decreased P 0903’ E in the ITCZ and to increased P 0903’ E in the descending branches of the Walker and Hadley cells. The changing mean circulation also causes decreased P 0903’ E on the poleward flanks of the subtropics because the descending branch of the Hadley Cell expands and the midlatitude meridional circulation cell shifts poleward. Subtropical drying and poleward moistening are also contributed to by an increase in poleward moisture transport by transient eddies. The thermodynamic contribution to changing P 0903’ E, arising from increased specific humidity, is almost entirely accounted for by atmospheric warming under fixed relative humidity. [42] Long S M, Xie S P.Intermodel variations in projected precipitation change over the North Atlantic: Sea surface temperature effect[J]. Geophysical Research Letters, 2015, 42(10): 4 158-4 165. Abstract Intermodel variations in future precipitation projection in the North Atlantic are studied using 23 state-of-art models from Phase 5 of the Coupled Model Intercomparison Project. Model uncertainty in annual mean rainfall change is locally enhanced along the Gulf Stream. The moisture budget analysis reveals that much of the model uncertainty in rainfall change can be traced back to the discrepancies in surface evaporation change and transient eddy effect among models. Results of the intermodel Singular Value Decomposition (SVD) analysis show that intermodel variations in local sea surface temperature (SST) pattern exert a strong control over the spread of rainfall projection among models through the modulation of evaporation change. The first three SVD modes explain more than 60% of the intermodel variance of rainfall projection and show distinct SST patterns with mode water-induced banded structures, reduced subpolar warming due to ocean dynamical cooling, and the Gulf Stream shift, respectively. [43] Neelin J D,Battisti D S,Hirst A C, et al. ENSO theory[J]. Journal of Geophysical Research, 1998, 103(C7): 14 261-14 290. [44] Alexander M A, Blade I, Newman M, et al. The atmospheric bridge: The influence of ENSO teleconnections on air-sea interaction over the global oceans[J]. Journal of Climate, 2002, 15(16): 2 205-2 231. During El Nio-Southern Oscillation (ENSO) events, the atmospheric response to sea surface temperature (SST) anomalies in the equatorial Pacific influences ocean conditions over the remainder of the globe. This connection between ocean basins via the `atmospheric bridge' is reviewed through an examination of previous work augmented by analyses of 50 years of data from the National Centers for Environmental Prediction-National Center for Atmospheric Research (NCEP-NCAR) reanalysis project and coupled atmospheric general circulation (AGCM)-mixed layer ocean model experiments. Observational and modeling studies have now established a clear link between SST anomalies in the equatorial Pacific with those in the North Pacific, north tropical Atlantic, and Indian Oceans in boreal winter and spring. ENSO-related SST anomalies also appear to be robust in the western North Pacific during summer and in the Indian Ocean during fall. While surface heat fluxes are the key component of the atmospheric bridge driving SST anomalies, Ekman transport also creates SST anomalies in the central North Pacific although the full extent of its impact requires further study. The atmospheric bridge not only influences SSTs on interannual timescales but also affects mixed layer depth (MLD), salinity, the seasonal evolution of upper-ocean temperatures, and North Pacific SST variability at lower frequencies. The model results indicate that a significant fraction of the dominant pattern of low-frequency (>10 yr) SST variability in the North Pacific is associated with tropical forcing. AGCM experiments suggest that the oceanic feedback on the extratropical response to ENSO is complex, but of modest amplitude. Atmosphere-ocean coupling outside of the tropical Pacific slightly modifies the atmospheric circulation anomalies in the Pacific-North America (PNA) region but these modifications appear to depend on the seasonal cycle and air-sea interactions both within and beyond the North Pacific Ocean. [45] Deser C, Alexander M A, Xie S, et al. Sea surface temperature variability: Patterns and mechanisms[J]. Annual Review of Marine Science, 2010, 2(1): 115-143. Patterns of sea surface temperature (SST) variability on interannual and longer timescales result from a combination of atmospheric and oceanic processes. These SST anomaly patterns may be due to intrinsic modes of atmospheric circulation variability that imprint themselves upon the SST field mainly via Surface energy fluxes. Examples include SST fluctuations in the Southern Ocean associated with the Southern Annular Mode, a tripolar pattern of SST anomalies in the North Atlantic associated with the North Atlantic Oscillation, and a pan-Pacific mode known as the Pacific Decadal Oscillation (with additional contributions from oceanic processes). They may also result from coupled ocean-atmosphere interactions, such as the El Nino-Southern Oscillation phenomenon in the tropical Indo-Pacific, the tropical Atlantic Nino, and the cross-equatorial meridional modes ill the tropical Pacific and Atlantic. Finally, patterns of SST variability may arise from intrinsic oceanic modes, notably the Atlantic Multidecadal Oscillation. [46] Mcphaden M J, Zebiak S E, Glantz M H.ENSO as an integrating concept in earth science[J]. Science, 2006, 314(5 806): 1 740-1 745. [47] Power S, Delage F, Chung C, et al. Robust twenty-first-century projections of El Niño and related precipitation variability[J]. Nature, 2013, 502(7 472): 541-545. The El Nino-Southern Oscillation (ENSO) drives substantial variability in rainfall(1-3), severe weather(4,5), agricultural production(3,6), ecosystems(7) and disease(8) in many parts of the world. Given that further human-forced changes in the Earth's climate system seem inevitable(9,10), the possibility exists that the character of ENSO and its impacts might change over the coming century. Although this issue has been investigated many times during the past 20 years, there is very little consensus on future changes in ENSO, apart from an expectation that ENSO will continue to be a dominant source of year-to-year variability(9,11,12). Here we show that there are in fact robust projected changes in the spatial patterns of year-to-year ENSO-driven variability in both surface temperature and precipitation. These changes are evident in the two most recent generations of climate models(13,14), using four different scenarios for CO2 and other radiatively active gases(14-17). By the mid- to late twenty-first century, the projections include an intensification of both El-Nino-driven drying in the western Pacific Ocean and rainfall increases in the central and eastern equatorial Pacific. Experiments with an Atmospheric General Circulation Model reveal that robust projected changes in precipitation anomalies during El Nino years are primarily determined by a nonlinear response to surface global warming. Uncertain projected changes in the amplitude of ENSO-driven surface temperature variability have only a secondary role. Projected changes in key characteristics of ENSO are consequently much clearer than previously realized. [48] Chung C T Y,Power S B,Arblaster J M, et al. Nonlinear precipitation response to El Niño and global warming in the Indo-Pacific[J]. Climate Dynamics, 2013, 42(7/8): 1 837-1 856. [49] Seager R,Naik N,Vogel L.Does global warming cause intensified interannual hydroclimate variability?[J]. Journal of Climate, 2012, 25(9): 3 355-3 372. [50] Cai W,Borlace S, Lengaigne M, et al. Increasing frequency of extreme El Niño events due to greenhouse warming[J]. Nature Climate Change, 2014, 4(2): 111-116. El Nio events are a prominent feature of climate variability with global climatic impacts. The 1997/98 episode, often referred to as 'the climate event of the twentieth century', and the 1982/83 extreme El Nio, featured a pronounced eastward extension of the west Pacific warm pool and development of atmospheric convection, and hence a huge rainfall increase, in the usually cold and dry equatorial eastern Pacific. Such a massive reorganization of atmospheric convection, which we define as an extreme El Nio, severely disrupted global weather patterns, affecting ecosystems, agriculture, tropical cyclones, drought, bushfires, floods and other extreme weather events worldwide. Potential future changes in such extreme El Nio occurrences could have profound socio-economic consequences. Here we present climate modelling evidence for a doubling in the occurrences in the future in response to greenhouse warming. We estimate the change by aggregating results from climate models in the Coupled Model Intercomparison Project phases 3 (CMIP3; ref. ) and 5 (CMIP5; ref. ) multi-model databases, and a perturbed physics ensemble. The increased frequency arises from a projected surface warming over the eastern equatorial Pacific that occurs faster than in the surrounding ocean waters, facilitating more occurrences of atmospheric convection in the eastern equatorial region. [51] Zhou Z Q,Xie S P,Zheng X T, et al. Global warming-induced changes in El Niño teleconnections over the North Pacific and North America[J]. Journal of Climate, 2014, 27(24): 9 050-9 064. Abstract El Nio-Southern Oscillation (ENSO) induces climate anomalies around the globe. Atmospheric general circulation model simulations are used to investigate how ENSO-induced teleconnection patterns during boreal winter might change in response to global warming in the Pacific-North American sector. As models disagree on changes in the amplitude and spatial pattern of ENSO in response to global warming, for simplicity the same sea surface temperature (SST) pattern of ENSO is prescribed before and after the climate warming. In a warmer climate, precipitation anomalies intensify and move eastward over the equatorial Pacific during El Nio because the enhanced mean SST warming reduces the barrier to deep convection in the eastern basin. Associated with the eastward shift of tropical convective anomalies, the ENSO-forced Pacific-North American (PNA) teleconnection pattern moves eastward and intensifies under the climate warming. By contrast, the PNA mode of atmospheric internal variability remains largely unchanged in pattern, suggesting the importance of tropical convection in shifting atmospheric teleconnections. As the ENSO-induced PNA pattern shifts eastward, rainfall anomalies are expected to intensify on the west coast of North America, and the El Nio-induced surface warming to expand eastward and occupy all of northern North America. The spatial pattern of the mean SST warming affects changes in ENSO teleconnections. The teleconnection changes are larger with patterned mean warming than in an idealized case where the spatially uniform warming is prescribed in the mean state. The results herein suggest that the eastward-shifted PNA pattern is a robust change to be expected in the future, independent of the uncertainty in changes of ENSO itself. [52] Kug J S,An S I,Ham Y G, et al. Changes in El Niño and La Niña teleconnections over North Pacific-America in the global warming simulations[J]. Theoretical and Applied Climatology, 2009, 100(3/4): 275-282. The change in the teleconnections of both El Ni09o and La Ni09a over the North Pacific and American regions due to a future greenhouse warming has been analyzed herein by means of diagnostics of the Intergovernmental Panel on Climate Change-Fourth Assessment Report (IPCC-AR4) coupled general circulation models (CGCMs). Among the IPCC-AR4 CGCM simulations, the composites of the eight-member multimodel ensemble are analyzed. In most CGCMs, the tropical Pacific warming due to the increase of CO 2 concentration in the atmosphere promotes the main convection centers in the equatorial Pacific associated with both El Ni09o and La Ni09a to the east. The eastward shift of the convection center causes a systematic eastward shift of not only El Ni09o but also La Ni09a teleconnection patterns over the North Pacific and America, which is demonstrated in the composite maps of 50002hPa circulation, surface temperature, and the precipitation against El Ni09o and La Ni09a, as observed in a comparison between the pre-industrial and CO 2 doubling experiments. Thus, a systematic eastward migration of convection centers in the tropical Pacific associated with both El Ni09o and La Ni09a due to a future global warming commonly causes the eastward shift of the atmospheric teleconnection patterns over the Northern Hemisphere. [53] DiNezio P N,Clement A C,Vecchi G A, et al. Climate response of the equatorial Pacific to global warming[J]. Journal of Climate, 2009, 22(18): 4 873-4 892. The climate response of the equatorial Pacific to increased greenhouse gases is investigated using numerical experiments from 11 climate models participating in the Intergovernmental Panel on Climate Change0964s Fourth Assessment Report. Multimodel mean climate responses to CO2 doubling are identified and related to changes in the heat budget of the surface layer. Weaker ocean surface currents driven by a slowing down of the Walker circulation reduce ocean dynamical cooling throughout the equatorial Pacific. The combined anomalous ocean dynamical plus radiative heating from CO2 is balanced by different processes in the western and eastern basins: Cloud cover feedbacks and evaporation balance the heating over the warm pool, while increased cooling by ocean vertical heat transport balances the warming over the cold tongue. This increased cooling by vertical ocean heat transport arises from increased near-surface thermal stratification, despite a reduction in vertical velocity. The stratification response is found to be a permanent feature of the equilibrium climate potentially linked to both thermodynamical and dynamical changes within the equatorial Pacific. Briefly stated, ocean dynamical changes act to reduce (enhance) the net heating in the east (west). This explains why the models simulate enhanced equatorial warming, rather than El Ni01±o09“like warming, in response to a weaker Walker circulation. To conclude, the implications for detecting these signals in the modern observational record are discussed. [54] Kent C,Chadwick R,Rowell D P.Understanding uncertainties in future projections of seasonal tropical precipitation[J]. Journal of Climate, 2015, 28(11): 4 390-4 413. ABSTRACT Projected changes in regional seasonal precipitation due to climate change are highly uncertain, with model disagreement on even the sign of change in many regions. Using a 20-member CMIP5 ensemble under the RCP8.5 scenario, the intermodel uncertainty of the spatial patterns of projected end-of-twenty-first-century change in precipitation is found not to be strongly influenced by uncertainty in global mean temperature change. In the tropics, both the ensemble mean and intermodel uncertainty of regional precipitation change are found to be predominantly related to spatial shifts in convection and convergence, associated with processes such as sea surface temperature (SST) pattern change and land-sea thermal contrast change. The authors hypothesize that the zonal-mean seasonal migration of these shifts is driven by 1) the nonlinear spatial response of convection to SST changes and 2) a general movement of convection from land to ocean in response to SST increases. Assessment of tropical precipitation model projections over East Africa highlights the complexity of regional rainfall changes. Thermodynamically driven moisture increases determine the magnitude of the long rains (March-May) ensemble mean precipitation change in this region, whereas model uncertainty in spatial shifts of convection accounts for almost all of the intermodel uncertainty. Moderate correlations are found across models between the long rains precipitation change and patterns of SST change in the Pacific and Indian Oceans. Further analysis of the capability of models to represent present-day SST-rainfall links, and any relationship with model projections, may contribute to constraining the uncertainty in projected East Africa long rains precipitation. [55] Shepherd T G.Atmospheric circulation as a source of uncertainty in climate change projections[J]. Nature Geoscience, 2014, 7(10): 703-708. The evidence for anthropogenic climate change continues to strengthen, and concerns about severe weather events are increasing. As a result, scientific interest is rapidly shifting from detection and attribution of global climate change to prediction of its impacts at the regional scale. However, nearly everything we have any confidence in when it comes to climate change is related to global patterns of surface temperature, which are primarily controlled by thermodynamics. In contrast, we have much less confidence in atmospheric circulation aspects of climate change, which are primarily controlled by dynamics and exert a strong control on regional climate. Model projections of circulation-related fields, including precipitation, show a wide range of possible outcomes, even on centennial timescales. Sources of uncertainty include low-frequency chaotic variability and the sensitivity to model error of the circulation response to climate forcing. As the circulation response to external forcing appears to project strongly onto existing patterns of variability, knowledge of errors in the dynamics of variability may provide some constraints on model projections. Nevertheless, higher scientific confidence in circulation-related aspects of climate change will be difficult to obtain. For effective decision-making, it is necessary to move to a more explicitly probabilistic, risk-based approach. [56] Bony S,Bellon G,Klocke D, et al. Robust direct effect of carbon dioxide on tropical circulation and regional precipitation[J]. Nature Geoscience, 2013, 6(6): 447-451. Predicting the response of tropical rainfall to climate change remains a challenge(1). Rising concentrations of carbon dioxide are expected to affect the hydrological cycle through increases in global mean temperature and the water vapour content of the atmosphere(2-4). However, regional precipitation changes also closely depend on the atmospheric circulation, which is expected to weaken in a warmer world(4-6). Here, we assess the effect of a rise in atmospheric carbon dioxide concentrations on tropical circulation and precipitation by analysing results from a suite of simulations from multiple state-of-the-art climate models, and an operational numerical weather prediction model. In a scenario in which humans continue to use fossil fuels unabated, about half the tropical circulation change projected by the end of the twenty-first century, and consequently a large fraction of the regional precipitation change, is independent of global surfacewarming. Instead, these robust circulation and precipitation changes are a consequence of the weaker net radiative cooling of the atmosphere associated with higher atmospheric carbon dioxide levels, which affects the strength of atmospheric vertical motions. This implies that geo-engineering schemes aimed at reducing global warming without removing carbon dioxide from the atmosphere would fail to fully mitigate precipitation changes in the tropics. Strategies that may help constrain rainfall projections are suggested. [57] Hawkins E,Sutton R.The potential to narrow uncertainty in projections of regional precipitation change[J]. Climate Dynamics, 2011, 37(1/2): 407-418. We separate and quantify the sources of uncertainty in projections of regional (2,500km) precipitation changes for the twenty-first century using the CMIP3 multi-model ensemble, allowing a direct comparison with a similar analysis for regional temperature changes. For decadal means of seasonal mean precipitation, internal variability is the dominant uncertainty for predictions of the first decade everywhere, and for many regions until the third decade ahead. Model uncertainty is generally the dominant source of uncertainty for longer lead times. Scenario uncertainty is found to be small or negligible for all regions and lead times, apart from close to the poles at the end of the century. For the global mean, model uncertainty dominates at all lead times. The signal-to-noise ratio (S/N) of the precipitation projections is highest at the poles but less than 1 almost everywhere else, and is far lower than for temperature projections. In particular, the tropics have the highest S/N for temperature, but the lowest for precipitation. We also estimate a otential S/N by assuming that model uncertainty could be reduced to zero, and show that, for regional precipitation, the gains in S/N are fairly modest, especially for predictions of the next few decades. This finding suggests that adaptation decisions will need to be made in the context of high uncertainty concerning regional changes in precipitation. The potential to narrow uncertainty in regional temperature projections is far greater. These conclusions on S/N are for the current generation of models; the real signal may be larger or smaller than the CMIP3 multi-model mean. Also note that the S/N for extreme precipitation, which is more relevant for many climate impacts, may be larger than for the seasonal mean precipitation considered here. [58] Lau W K M,Kim K M. Robust Hadley circulation changes and increasing global dryness due to CO2 warming from CMIP5 model projections[J]. Proceedings of the National Academy of Sciences, 2015, 112(12): 3 630-3 635. Erratum for Proc Natl Acad Sci U S A. 2013 Jul 2;110(27):E2518-27. doi: 10.1073/pnas.1306832110. Epub 2013 Jun 17.. [59] Tao L,Hu Y,Liu J.Anthropogenic forcing on the Hadley circulation in CMIP5 simulations[J]. Climate Dynamics, 2015, 46(9/10): 3 337-3 350. Poleward expansion of the Hadley circulation has been an important topic in climate change studies in the past few years, and one of the critically important issues is how it is related to anthropogenic forcings. Using simulations from the coupled model intercomparison projection phase 5 (CMIP5), we study influences of anthropogenic forcings on the width and strength of the Hadley circulation. It is found that significant poleward expansion of the Hadley circulation can be reproduced in CMIP5 historical all-forcing simulations although the magnitude of trends is much weaker than observations. Simulations with individual forcings demonstrate that among three major types of anthropogenic forcings, increasing greenhouse gases (GHGs) and stratospheric ozone depletion all cause poleward expansion of the Hadley circulation, whereas anthropogenic aerosols do not have significant influences on the Hadley circulation. Increasing GHGs cause significant poleward expansion in both hemispheres, with the largest widening of the northern cell in boreal autumn. Stratospheric ozone depletion forces significant poleward expansion of the Hadley circulation for the southern cell in austral spring and summer and for the northern cell in boreal spring. In CMIP5 projection simulations for the twenty-first century, the magnitude of poleward expansion of the Hadley circulation increases with GHG forcing. On the other hand, ozone recovery competes with increasing GHGs in determining the width of the Hadley circulation, especially in austral summer. In both historical and projection simulations, the strength of the Hadley circulation shows significant weakening in winter in both hemispheres. [60] Hu Y,Fu Q.Observed poleward expansion of the Hadley circulation since 1979[J]. Atmospheric Chemistry and Physics, 2007, 7(19): 5 229-5 236. [61] Fu Q,Johanson C M,Wallace J M, et al. Enhanced mid-latitude tropospheric warming in satellite measurements[J]. Science, 2006, 312(5 777): 1 179. [62] Schneider T,Bischoff T,Haug G H.Migrations and dynamics of the intertropical convergence zone[J]. Nature, 2014, 513(7 516): 45-53. Rainfall on Earth is most intense in the intertropical convergence zone (ITCZ), a narrow belt of clouds centred on average around six degrees north of the Equator. The mean position of the ITCZ north of the Equator arises primarily because the Atlantic Ocean transports energy northward across the Equator, rendering the Northern Hemisphere warmer than the Southern Hemisphere. On seasonal and longer timescales, the ITCZ migrates, typically towards a warming hemisphere but with exceptions, such as during El Nio events. An emerging framework links the ITCZ to the atmospheric energy balance and may account for ITCZ variations on timescales from years to geological epochs. [63] Hu Y,Li D,Liu J.Abrupt seasonal variation of the ITCZ and the Hadley circulation[J]. Geophysical Research Letters, 2007, 34(18): L18814. DOI: 10.1029/2007GL030950. Using Global Precipitation Climatology Project (GPCP) daily data, we show that the seasonal migration of the global zonal-mean intertropical convergence zone (ITCZ) is not smooth, but jumps from the winter hemisphere to the summer hemisphere. The abrupt migration is within 10 days. Detailed analyses reveal that the phenomenon of the abrupt seasonal migration of the ITCZ mainly exists over particular tropical domains, such as Indian Ocean, western and central Pacific, and South America, which gives the rise of the jump of the global zonal-mean ITCZ. Because the ITCZ constitutes the ascending branch of the Hadley circulation, we also examine whether there exists such an abrupt seasonal change in the Hadley circulation. It is found that the intensity of the Hadley cells evolves smoothly with time. However, the horizontal scales of the Hadley cells demonstrate abrupt seasonal changes, corresponding to the abrupt seasonal migration of the global ITCZ. The winter cell extends rapidly across the equator, while the summer cell rapidly narrows. This suggests that the solsticial cell is the dominant component of the Hadley circulation, and that the equinoctial symmetric pattern is ephemeral. [64] Chadwick R,Boutle I,Martin G.Spatial patterns of precipitation change in CMIP5: Why the rich do not get richer in the tropics[J]. Journal of Climate, 2013, 26(11): 3 803-3 822. [65] Su H, Jiang J H,Zhai C, et al. Weakening and strengthening structures in the Hadley circulation change under global warming and implications for cloud response and climate sensitivity[J]. Journal of Geophysical Research: Atmospheres, 2014, 119(10): 5 787-5 805. AbstractIt has long been recognized that differences in climate model-simulated cloud feedbacks are a primary source of uncertainties for the model-predicted surface temperature change induced by increasing greenhouse gases such as CO2. Large-scale circulation broadly determines when and where clouds form and how they evolve. However, the linkage between large-scale circulation change and cloud radiative effect (CRE) change under global warming has not been thoroughly studied. By analyzing 15 climate models, we show that the change of the Hadley Circulation exhibits meridionally varying weakening and strengthening structures, physically consistent with the cloud changes in distinct cloud regimes. The regions that experience a weakening (strengthening) of the zonal-mean circulation account for 54% (46%) of the multimodel-mean top-of-atmosphere (TOA) CRE change integrated over 45°S–40°N. The simulated Hadley Circulation structure changes per degree of surface warming differ greatly between the models, and the intermodel spread in the Hadley Circulation change is well correlated with the intermodel spread in the TOA CRE change. This correlation underscores the close interactions between large-scale circulation and clouds and suggests that the uncertainties of cloud feedbacks and climate sensitivity reside in the intimate coupling between large-scale circulation and clouds. New model performance metrics proposed in this work, which emphasize how models reproduce satellite-observed spatial variations of zonal-mean cloud fraction and relative humidity associated with the Hadley Circulation, indicate that the models closer to the satellite observations tend to have equilibrium climate sensitivity higher than the multimodel mean. [66] Lin J L.The double-ITCZ problem in IPCC AR4 coupled GCMs: Ocean-atmosphere feedback analysis[J]. Journal of Climate, 2007, 20(18): 4 497-4 525. [67] Bayr T,Dommenget D.The tropospheric land-sea warming contrast as the driver of tropical sea level pressure changes[J]. Journal of Climate, 2013, 26(4): 1 387-1 402. This article addresses the causes of the large-scale tropical sea level pressure (SLP) changes during climate change. The analysis presented here is based on model simulations, observed trends, and the seasonal cycle. In all three cases the regional changes of tropospheric temperature (T-tropos) and SLP are strongly related to each other [considerably more strongly than (sea) surface temperature and SLP]. This relationship basically follows the Bjerknes circulation theorem, with relatively low regional SLP where there is relatively high T-tropos and vice versa. A simple physical model suggests a tropical SLP response to horizontally inhomogeneous warming in the tropical T-tropos, with a sensitivity coefficient of about-1.7 hPa K-1. This relationship explains a large fraction of observed and predicted changes in the tropical SLP.It is shown that in climate change model simulations the tropospheric land-sea warming contrast is the most significant structure in the regional T-tropos changes relative to the tropical mean changes. Since the land-sea warming contrast exists in the absence of any atmospheric circulation changes, it can be argued that the large-scale response of tropical SLP changes is to first order a response to the tropical land-sea warming contrast. Furthermore, as the land-sea warming contrast is mostly moisture dependent, the models predict a stronger warming and decreasing SLP in the drier regions from South America to Africa and a weaker warming and increasing SLP over the wetter Indo-Pacific warm pool region. This suggests an increase in the potential for deep convection conditions over the Atlantic sector and a decrease over the Indo-Pacific warm pool region in the future. [68] Xie S P,Deser C,Vecchi G A, et al. Towards predictive understanding of regional climate change[J]. Nature Climate Change, 2015, 5(10): 921-930. This Review considers recent advances in our understanding of regional climate change, critically discusses outstanding issues, and recommends targets for future research. [69] IPCC. Climate Change 2013: The Physical Science Basis[M]. Cambridge, United Kingdom and New York, NY, USA: Cambridge University Press,2013. [70] Goddard L M,Kumar A,Solomon A, et al. A verification framework for interannual-to-decadal predictions experiments[J]. Climate Dynamics, 2013, 40(1): 245-272. Decadal predictions have a high profile in the climate science community and beyond, yet very little is known about their skill. Nor is there any agreed protocol for estimating their skill. This paper proposes a sound and coordinated framework for verification of decadal hindcast experiments. The framework is illustrated for decadal hindcasts tailored to meet the requirements and specifications of CMIP5 (Coupled Model Intercomparison Project phase 5). The chosen metrics address key questions about the information content in initialized decadal hindcasts. These questions are: (1) Do the initial conditions in the hindcasts lead to more accurate predictions of the climate, compared to un-initialized climate change projections? and (2) Is the prediction model ensemble spread an appropriate representation of forecast uncertainty on average? The first question is addressed through deterministic metrics that compare the initialized and uninitialized hindcasts. The second question is addressed through a probabilistic metric applied to the initialized hindcasts and comparing different ways to ascribe forecast uncertainty. Verification is advocated at smoothed regional scales that can illuminate broad areas of predictability, as well as at the grid scale, since many users of the decadal prediction experiments who feed the climate data into applications or decision models will use the data at grid scale, or downscale it to even higher resolution. An overall statement on skill of CMIP5 decadal hindcasts is not the aim of this paper. The results presented are only illustrative of the framework, which would enable such studies. However, broad conclusions that are beginning to emerge from the CMIP5 results include (1) Most predictability at the interannual-to-decadal scale, relative to climatological averages, comes from external forcing, particularly for temperature; (2) though moderate, additional skill is added by the initial conditions over what is imparted by external forcing alone; however, the impact of initialization may result in overall worse predictions in some regions than provided by uninitialized climate change projections; (3) limited hindcast records and the dearth of climate-quality observational data impede our ability to quantify expected skill as well as model biases; and (4) as is common to seasonal-to-interannual model predictions, the spread of the ensemble members is not necessarily a good representation of forecast uncertainty. The authors recommend that this framework be adopted to serve as a starting point to compare prediction quality across prediction systems. The framework can provide a baseline against which future improvements can be quantified. The framework also provides guidance on the use of these model predictions, which differ in fundamental ways from the climate change projections that much of the community has become familiar with, including adjustment of mean and conditional biases, and consideration of how to best approach forecast uncertainty. [71] Deser C,Phillips A S,Alexander M A.Twentieth century tropical sea surface temperature trends revisited[J]. Geophysical Research Letters, 2010, 37(10). DOI:10.1029/2010GL043321. This study compares the global distribution of 20th century SST and marine air temperature trends from a wide variety of data sets including un-interpolated archives as well as globally-complete reconstructions. Apart from the eastern equatorial Pacific, all datasets show consistency in their statistically significant trends, with warming everywhere except the far northwestern Atlantic; the largest warming trends are found in the middle latitudes of both hemispheres. Two of the SST reconstructions exhibit statistically significant cooling trends over the eastern equatorial Pacific, in disagreement with the un-interpolated SST and marine air temperature datasets which show statistically significant warming in this region. Twentieth century trends in tropical marine cloudiness, precipitation and SLP from independent data sets provide physically consistent evidence for a reduction in the strength of the atmospheric Walker Circulation accompanied by an eastward shift of deep convection from the western to the central equatorial Pacific. [72] Brown J N,Sen Gupta A,Brown J R, et al. Implications of CMIP3 model biases and uncertainties for climate projections in the western tropical Pacific[J]. Climatic Change, 2013, 119(1): 147-161. Regional climate projections in the Pacific region are potentially sensitive to a range of existing model biases. This study examines the implications of coupled model biases on regional climate projections in the tropical western Pacific. Model biases appear in the simulation of the El Nino Southern Oscillation, the location and movement of the South Pacific Convergence Zone, rainfall patterns, and the mean state of the ocean-atmosphere system including the cold tongue bias and erroneous location of the edge of the Western Pacific warm pool. These biases are examined in the CMIP3 20th century climate models and used to provide some context to the uncertainty in interpretations of regional-scale climate projections for the 21st century. To demonstrate, we provide examples for two island nations that are located in different climate zones and so are affected by different biases: Nauru and Palau. We discuss some of the common approaches to analyze climate projections and whether they are effective in reducing the effect of model biases. These approaches include model selection, calculating multi model means, downscaling and bias correcting. [73] Cox P M,Pearson D,Booth B B, et al. Sensitivity of tropical carbon to climate change constrained by carbon dioxide variability[J]. Nature, 2013, 494(7 437): 341-344. [74] Bracegirdle T J,Stephenson D B.On the robustness of emergent constraints used in multimodel climate change projections of Arctic warming[J]. Journal of Climate, 2013, 26(2): 669-678. Statistical relationships between future and historical model runs in multimodel ensembles (MMEs) are increasingly exploited to make more constrained projections of climate change. However, such emergent constraints may be spurious and can arise because of shared (common) errors in a particular MME or because of overly influential models. This study assesses the robustness of emergent constraints used for Arctic warming by comparison of such constraints in ensembles generated by the two most recent Coupled Model Intercomparison Project (CMIP) experiments: CMIP3 and CMIP5. An ensemble regression approach is used to estimate emergent constraints in Arctic wintertime surface air temperature change over the twenty-first century under the Special Report on Emission Scenarios (SRES) A1B scenario in CMIP3 and the Representative Concentration Pathway (RCP) 4.5 scenario in CMIP5. To take account of different scenarios, this study focuses on polar amplification by using temperature responses at each grid point that are scaled by the global mean temperature response for each climate model. In most locations, the estimated emergent constraints are reassuringly similar in CMIP3 and CMIP5 and differences could have easily arisen from sampling variation. However, there is some indication that the emergent constraint and polar amplification is substantially larger in CMIP5 over the Sea of Okhotsk and the Bering Sea. Residual diagnostics identify one climate model in CMIP5 that has a notable influence on estimated emergent constraints over the Bering Sea and one in CMIP3 that that has a notable influence more widely along the sea ice edge and into midlatitudes over the western North Atlantic. [75] Collins M,Chandler R E,Cox P M, et al. Quantifying future climate change[J]. Nature Climate Change, 2012, 2(6): 403-409. [76] Huang P,Ying J.A multimodel ensemble pattern regression method to correct the tropical Pacific SST change patterns under global warming[J]. Journal of Climate, 2015, 28(12): 4706-4 723. ABSTRACT This study develops a new observational constraint method, called multimodel ensemble pattern regression (EPR), to correct the projections of regional climate change by the conventional unweighted multimodel mean (MMM). The EPR method first extracts leading modes of historical bias using intermodel EOF analysis, then builds up the linear correlated modes between historical bias and change bias using multivariant linear regression, and finally estimates the common change bias induced by common historical bias. Along with correcting common change bias, the EPR method implicitly removes the intermodel uncertainty in the change projection deriving from the intermodel diversity in background simulation. The EPR method is applied to correct the patterns of tropical Pacific SST changes using the historical and representative concentration pathway 8.5 (RCP8.5) runs in 30 models from phase 5 of CMIP (CMIP5) and observed SSTs. The common bias patterns of the tropical Pacific SSTs in historical runs, including the excessive cold tongue, the southeastern warm bias, and the narrower warm pool, are estimated to induce La Ni09a–like change biases. After the estimated common change biases are removed, the corrected SST changes display a pronounced El Ni09o–like pattern and have much greater zonal gradients. The bias correction decreases by around half of the intermodel uncertainties in the MMM SST projections. The patterns of corrected tropical precipitation and circulation change are dominated by the enhanced SST change patterns, displaying a pro- nounced warmer-get-wetter pattern and a decreased Walker circulation with decreased uncertainties. [77] Hall A.Projecting regional change[J]. Science, 2014, 346(6216): 1 461-1 462. [78] Collins M,Minobe S,Barreiro M, et al. Challenges and opportunities for improved understanding of regional climate dynamics[J]. Nature Climate Change, 2018, 8(2): 101-108. Dynamical processes in the atmosphere and ocean are central to determining the large-scale drivers of regional climate change, yet their predictive understanding is poor. Here, we identify three frontline challenges in climate dynamics where significant progress can be made to inform adaptation: response of storms, blocks and jet streams to external forcing; basin-to-basin and tropical-extratropical teleconnections; and the development of non-linear predictive theory. We highlight opportunities and techniques for making immediate progress in these areas, which critically involve the development of high-resolution coupled model simulations, partial coupling or pacemaker experiments, as well as the development and use of dynamical metrics and exploitation of hierarchies of models. [79] Luan Yihua,Yu Yongqiang,Zheng Weipeng.Review of development and application of high resolution global climate system model[J]. Advances in Earth Science, 2016, 31(3): 258-268. [栾贻花, 俞永强, 郑伟鹏. 全球高分辨率气候系统模式研究进展[J]. 地球科学进展, 2016, 31(3): 258-268.] 气候模式是定量研究气候演变规律、预测或预估未来气候变化的重要工具。提高气候模式空间分辨率并改进相应的物理参数化过程,是改善模式性能的重要途径之一, 对于认识气候变化规律、提高气候预测能力具有重要作用。在阐述发展全球高分辨率气候系统模式重要性的基础上,对当今国内外高分辨率气候系统模式的研究进展进行总结,介绍全球高分辨率气候系统模式研发和评估的现状及其存在的问题,并着重讨论了制约当前高分辨率气候系统模式发展的关键科学问题和技术瓶颈,其中包括高分辨率海洋和大气模式动力框架的研制和大规模高性能并行计算、次网格物理参数化过程的改进,以及中尺度海气相互作用等。同时,还介绍了国际耦合模式比较计划第六阶段中的高分辨率模式比较子计划的科学目标及其试验设计方案。最后对未来我国全球高分辨率气候系统模式的发展和评估进行了展望。 [80] Ying J,Huang P.Cloud-radiation feedback as a leading source of uncertainty in the tropical Pacific SST warming pattern in CMIP5 models[J]. Journal of Climate, 2016, 29(10): 3 867-3 881. Abstract The role of the intermodel spread of cloud-radiation feedback in the uncertainty in the tropical Pacific SST warming (TPSW) pattern under global warming is investigated based on the historical and RCP8.5 runs from 32 models participating in CMIP5. The large intermodel discrepancies in cloud-radiation feedback contribute 24% of the intermodel uncertainty in the TPSW pattern over the central Pacific. The mechanism by which the cloud-radiation feedback influences the TPSW pattern is revealed based on an analysis of the surface heat budget. A relatively weak negative cloud-radiation feedback over the central Pacific cannot suppress the surface warming as greatly as in the multimodel ensemble and thus induces a warm SST deviation over the central Pacific, producing a low-level convergence that suppresses (enhances) the evaporative cooling and zonal cold advection in the western (eastern) Pacific. With these processes, the original positive SST deviation over the central Pacific will move westward to the western and central Pacific, with a negative SST deviation in the eastern Pacific. Compared with the observed cloud-radiation feedback from six sets of reanalysis and satellite-observed data, the negative cloud-radiation feedback in the models is underestimated in general. It implies that the TPSW pattern should be closer to an El Nino-like pattern based on the concept of observational constraint. However, the observed cloud-radiation feedback from the various datasets also demonstrates large discrepancies in magnitude. Therefore, the authors suggest that more effort should be made to improve the precision of shortwave radiation observations and the description of cloud-radiation feedback in models for a more reliable projection of the TPSW pattern in future. [81] Zhou Z,Xie S.Effects of climatological model biases on the projection of tropical climate change[J]. Journal of Climate, 2015, 28(24): 9 909-9 917. Climate models suffer from long-standing biases including the double intertropical convergence zone (ITCZ) problem and the excessive westward extension of the equatorial Pacific cold tongue. An atmospheric general circulation model is used to investigate how model biases in the mean state affect the projection of tropical climate change. The model is forced with a pattern of sea surface temperature (SST) increase derived from a coupled simulation of global warming but uses an SST climatology derived from either observations or a coupled historical simulation. The comparison of the experiments reveals that the climatological biases have important impacts on projected changes in the tropics. Specifically, during February-April when the climatological ITCZ displaces spuriously into the Southern Hemisphere, the model overestimates (underestimates) the projected rainfall increase in the warmer climate south (north) of the equator over the eastern Pacific. Furthermore, the global warming-induced Walker circulation slowdown is biased weak in the projection using coupled model climatology, suggesting that the projection of the reduced equatorial Pacific trades may also be under-estimated. This is related to the bias that the climatological Walker circulation is too weak in the model, which is in turn due to too weak mean SST gradient in the zonal direction. Our results highlight the importance of improving the climatological simulation for more reliable projections of regional climate change.

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