Seasonal Variation and Physical Properties of the Cloud System over Southeastern China Derived from CloudSat Products

GUO Zhunand ZHOU Tianjun

1State Key Laboratory of Numerical Modeling for Atmospheric Sciences and Geophysical Fluid Dynamics,

Institute of Atmospheric Physics,Chinese Academy of Sciences,Beijing100029

2Climate Change Research Center,Chinese Academy of Sciences,Beijing100029

3Joint Center for Global Change Studies,Beijing100875

Seasonal Variation and Physical Properties of the Cloud System over Southeastern China Derived from CloudSat Products

GUO Zhun1,2and ZHOU Tianjun?1,3

1State Key Laboratory of Numerical Modeling for Atmospheric Sciences and Geophysical Fluid Dynamics,

Institute of Atmospheric Physics,Chinese Academy of Sciences,Beijing100029

2Climate Change Research Center,Chinese Academy of Sciences,Beijing100029

3Joint Center for Global Change Studies,Beijing100875

Based on the National Centers for Environmental Prediction(NCEP)and Climate Prediction Center(CPC)Merged Analysis of Precipitation(CMAP)data and CloudSat products,the seasonal variations of the cloud properties,vertical occurrence frequency,and ice water content of clouds over southeastern China were investigated in this study.In the CloudSat data,a signi fi cant alternation in high or low cloud patterns was observed from winter to summer over southeastern China.It was found that the East Asian Summer Monsoon(EASM)circulation and its transport of moisture leads to a conditional instability,which bene fi ts the local upward motion in summer,and thereby results in an increased amount of high cloud.The deep convective cloud centers were found to coincide well with the northward march of the EASM,while cirrus lagged slightly behind the convection center and coincided well with the out fl ow and meridional wind divergence of the EASM.Analysis of the radiative heating rates revealed that both the plentiful summer moisture and higher clouds are effective in destabilizing the atmosphere.Moreover,clouds heat the mid-troposphere and the cloud radiative heating is balanced by adiabatic cooling through upward motion,which causes meridional wind by the Sverdrup balance.The cloud heating–forced circulation was observed to coincide well with the EASM circulation,serving as a positive effect on EASM circulation.

East Asian summer monsoon,seasonal cycle,CloudSat,cloud

1. Introduction

Clouds play a vital role in the earth’s climate system because of their in fl uence on radiative heating.The distribution of clouds has a profound impact on radiative energy balance, which is the main driver for atmospheric circulations and climate systems(Hartmann et al.,1992).Therefore,studies on the changes in cloud distributions,radiative effect,and their formation mechanisms are of essential importance to our understanding of climate changes.

The formation mechanism of cloud types is associated with the dynamic and thermal conditions(Houze,1994).The radiative effects and feedback of clouds depend on their properties(Arking,1991;Hartmann et al.,1992).Low stratiform cloud,such as marine boundary layer cloud,corresponds to lower troposphere static stability and has a strong net radiative cooling effect on the atmosphere(Klein and Hartmann, 1993;Lin et al.,2009).Some studies have demonstrated that there is positive feedback between SST and stratiform cloud over the northern Paci fi c and the oceans of the eastern tropics(Norris and Leovy,1994;Huang and Hu,2007).On the contrary,high clouds,such as deep convective and cirrus clouds, have a cancellation effect on long-and short-wave cloud radiative forcing(CRF),regulating the SST of the western Paci fi c warm pool(Ramanathan and Collins,1991),except in El Ni?no years(Cess et al.,2001).

Southeastern China is covered by a large amount of cloud (Wang et al.,2004),and is also one of the most signi fi cant stratiform cloud regions(Klein and Hartmann,1993).Therefore,this region has a strong net radiative cooling effect(Rajeevan and Sriviasan,2000;Wang et al.,2004).Moreover, this region also has a signi fi cant annual cycle in cloud cover that the high-and low-cloud alternates with each other(Yu et al.,2001;Luo et al.,2009).However,because of the limitation of conventional cloud data and the complexity of cloud physics,knowledge about the formation mechanisms and climate effects of cloud in this region is still limited.Only a limited number of studies exist that have focused on the effects of total cloud amounts on the East Asian summer monsoon (EASM).

The climate of southeastern China is dominated by the activity of the EASM(Wang et al.,2004;Ding and Chan, 2005;Zhou et al.,2009a),whose onset is a key indicatorcharacterizing the abrupt transition from the dry to the rainy season and the subsequent seasonal march(Ding and Chan, 2005).Therefore,both the onset and march of the EASM further in fl uence the properties of clouds by changing the atmospheric conditions.Recently,the availability of CloudSat(a new satellite-based cloud experiment;Stephens et al.,2002), for which the satellite was launched in 2006 as part of National Aeronautics and Space Administration(NASA)’s ATrain constellation of satellites(L’Ecuyer and Jiang,2010), has provided us with an opportunity to reveal verticallyresolved cloud properties and formation mechanisms.

The primary purpose of this study is to investigate the relationship between the variations of cloud properties and EASM circulation over southeastern China.In addition,we alsowantto addressthefollowing questions:(1)What arethe seasonal variations of cloud properties derived from Cloud-Sat data?(2)What is the in fl uence of EASM circulation on the vertical structure of cloud properties?(3)What kind of interaction occurs between cloud(their heating effects)and EASM circulation?

The remainder of the paper is organized as follows.The data and methodology are described in section 2.The seasonal variation of the cloud properties over southeastern China and the large-scale triggers for the prevailing cloud types are analyzed in section 3.The seasonal meridional migration of the cloud system and its vertical structures associated with the advance and retreat of the EASM are analyzed in section 4.Section 5 presents an analysis of the radiative heating rates of the clouds.The major fi ndings are summarized in section 6.

2. Data and methods

2.1.Satellite data

To analyze the cloud pro fi les over southeastern China, fi ve standard data products from CloudSat version 4, namely 2B-GEOPROF,2B-GEOPROF-lidar,2B-CWC-RO, 2B-CLDCLASS and 2B-FLXHR,were used(http://www. cloudsat.cira.colostate.edu/dataSpecs.php).The CloudSat is an active remote sensor,which is useful for the observation of the vertical locations of hydrometeor layers(Mace,2007). The Cloud Pro fi ling Radar(CPR)mounted on the CloudSat satellite identi fi es the radar echoes from hydrometeors and produces an estimate of the radar re fl ectivity factor for each volume deemed to contain signi fi cant echo(Stephens et al., 2002).

The 2B-GEOPROF product determines the existence of clouds by examining the CloudSat CPR radar echo,and then compares with the Moderate Resolution Imaging Spectroradiometer(MODIS)cloud mask spectral tests.Finally,the geometrical pro fi le of clouds is obtained,which includes cloud mask,cloud fraction,radar re fl ectivity,and gaseous attenuation(Mace et al.,2007).

The 2B-GEOPROF-lidar data is the product of a combination of both CPR and CALIPSO(the Cloud-Aerosol Lidar and Infrared Path fi nder Satellite Observation)Cloud-Aerosol Lidar with Orthogonal Polarization(CALIOP).The CPR can probe optically thick large particle layers,while CALIOP can probe optically thin layers and tenuous cloud tops.An ef ficient cooperation of the two instruments can provide more reliable and accurate geometrical pro fi les of cloud(Mace, 2007).

The 2B-CLASS product classi fi es the clouds into eight types by examining the maximum effective radar re fl ectivity,precipitation,temperature,and vertical scale of hydrometeors.It includes cirrus,altostratus,altocumulus,stratus, stratocumulus,cumulus,nimbostratus,and deep convection clouds(Wang and Sassen,2007).

The 2B-FLXHR product uses the liquid and ice water content estimated from the CPR and European Centre for Medium-Range Weather Forecasts(ECWMF)reanalysis to produce the estimates of broadband fl uxes and heating rates for each radar pro fi le(L’Ecuyer et al.,2008).

In this study,all the CloudSat datasets span from June 2006 to June 2010.The data are interpolated onto a grid with 1°×1°resolution.The products(i.e.cloud properties)are derived from satellite tracks.There are about 14 tracks in a day and about 420 tracks in a month.The frequency and corresponding satellite products are counted when the satellite fl ies over an assumed grid box.And then,for each grid and each month,such a treatment allows suf fi cient sampling for meaningful use.There are at least 4000 valid samples in each grid and each month.The monthly averaged products are the average of all those 4000 samples.

Similar to Xi et al.(2010),the occurrence frequency of cloud is de fi ned by using cloud mask derived from 2BGEOPROF.Thecloudmaskis0forclearskyand100%when cloud mask is lager than 20.When cloud mask is less than 20,the cloud occurrence frequency is set to the cloud fraction,which is derived from 2B-GEOPROF-lidar.Therefore, the cloud occurrence frequency is a ratio of the number of times when the cloud mask is larger than 20 to the total number of satellite observations.

2.2.Reanalysis data and precipitation data

The atmospheric general circulation data are from the National Centers for Environmental Prediction(NCEP)Department of Energy(DOE)Atmospheric Model Intercomparison Project(AMIP)reanalysis(hereafter NCEP2)(Kanamitsu et al.,2002).In addition,Climate Prediction Center(CPC) Merged Analysis of Precipitation(CMAP)precipitation data are also used to describe the monsoon rain band(Xie and Arkin,1996).Corresponding to the CloudSat data,the time periods of NCEP2 and CMAP also range from June 2006 to June 2010.

3. The seasonal variation of cloud properties over southeastern China

3.1.The seasonal variation of cloud properties derived from CloudSat data

To demonstrate the seasonal cycle of cloud properties, the occurrence frequencies of fi ve cloud types derived fromCloudSat data are presented in Fig.1.It can be observed that there are more stratiform clouds,especially stratocumulus,in winter than in summer.In contrast,high clouds are prevalent in summer,especially cirrus and deep convective clouds.The cloud properties derived from CloudSat data are slightly different from those derived from the International Satellite Cloud Climatology Project(ISCCP D2).The dominant cloud type over southeastern China is noted to be nimbostratus in ISCCP-D2 data(Yu et al.,2004),but stratocumulus in CloudSat data(Fig.1).This difference is due to the different methods of categorizing cloud types in the ISCCP and CloudSat datasets.The categories of clouds in Cloud-Sat are de fi ned by their horizontal and vertical cloud dimensions,base height,precipitation,and water path(Sassen and Wang,2008);however,in ISCCP,the categories are just defi ned by visible spectrometry(or infrared)cloud-top pressure and optical depth data(Rossow and Schiffer,1991;Wang and Sassen,2001;Sassen and Wang,2008).Although the prevalent winter cloud types derived from the two datasets are different,they are highly consistent in measuring the seasonal variation of cirrus;both reach their maximum values in summer.

3.2.Large-scale circulation triggers for the seasonal change of prevailing cloud types over southeastern China

The mean vertical pro fi les of horizontal divergence and vertical velocity are shown in Fig.2.The wintertime lowlevel convergence and mid-level divergence prohibit deep convection,and thus high clouds cannot form.As a result, the wintertime upward motion is shallow and peaks at around 2 km(Fig.2b).Such a kind of vertical pro fi le of horizontal divergence is caused by the blocking and frictional effects of the Tibetan Plateau(Yu et al.,2004).

In boreal summer,the low-level convergence is still evident,but the mid-level divergence is replaced by a convergence,along with a high-level divergence(Fig.2a),indicating the impact of the EASM.A deep convection peaking at 6 km is also evident.The strong upward motion enhances the updraft of mass fl ux,which is in favor of the increase in the occurrence frequency of high clouds,such as deep convective and cirrus clouds(Fig.1).

To gain further information on the general circulation, the potential and equivalent potential temperature(θandθe) averaged over southeastern China are calculated using the NCEP2 data(Fig.3a).Lower troposphere stability(LTS), which is de fi ned asθ700hPa-θ1000hPa,is correlated with the occurrence frequency of stratiform clouds,both seasonally and geographically(Klein and Hartmann,1993).Over southeastern China,the season with the maximum stratiform cloud is associated with the largest LTS.In boreal winter,this region is highly stable,having an LTS value of 18.6 K(Fig. 3b).Owing to the dynamic effects of the Tibetan Plateau(Yu et al.,2004),the convections are restricted to the lower troposphere,which is in favor of the formation of a large amount of stratiform clouds in winter.

In boreal summer,the LTS falls to its minimum value (14.0 K),which is associated with a weaker inversion.This tends to result in a poorly-mixed,strong entraining boundary layer,where there is ef fi cient turbulent decoupling of the cloud layer with the sub-cloud layer,and the surface moisture supply is cut off.Following the strong solar radiation input in summer,the entrainment at the stratiform cloud-top is enhanced.Associated with the strong evaporation caused by a warm cloud-base,the occurrence frequency of stratiform clouds sharply decreases in summer.

The seasonal cycle of total cloud is different from that of stratiform cloud.The high cloud occurrence frequency reaches its peak in boreal summer over southeastern China due to the contribution of increased high clouds.Figure 3 shows that the summertime equivalent potential temperature decreases vertically with height from 0 to 4 km,but increases with height from 4 km up to the TOA.Furthermore,a strong negative correlation between high cloudiness andlower-troposphereconditionalstabilityisfound(Fig.3b). These features re fl ect the impact of EASM moisture transports,when the summer monsoon circulation replaces the Hadley cell over southeastern China(Ye and Yang,1979; Zhou and Li,2002;Chen et al.,2010).The strong upwardmotion determines the height and occurrence frequency of the high cloud,as well as plays a critical role in the vertical transport of water vapor.

4. Advance and retreat of the EASM cloud system and its vertical structures

The above discussion already shows that the EASM plays an essential role in the seasonal variation of the vertical structure of clouds by changing the atmospheric circulations over southeastern China.The seasonal variations of the vertical structure of clouds also re fl ects the advance and retreat of the EASM.The seasonal movement of the rain belt is the most signi fi cant indicator of monsoon advance and retreat(Zhou and Li,2002;Ding and Chan,2005;Chen et al.,2010).In the following discussion,we depict the seasonal march of the monsoon by the maximum value of mean precipitation over southeastern China(105°–120°E).

The monthly evolution of vertical–latitude pro fi les of cloud occurrence frequency zonally averaged between 105°E and 120°E is shown in Fig.4(upper colored part of each panel).To clearly describe the relationship between cloud system formations and monsoon circulation movement,the corresponding meridional and vertical winds are also shown, and the precipitation averaged over the same longitudes at each month are displayed in the lower part of each panel.It is clear that the frequent cloud occurrence is well synchronized with the rain belts,as well as the EASM upwelling(Fig.4).It can be observed that a front-like cloud structure,whose base coincides well with the rain belts,tilts northward with altitude(Figs.4a and b).Following the seasonal march of the summer monsoon circulation,the frequent cloud occurrence indicated by the front-like cloud structure and rain belt move northward consistently.

From Figs.5a and b it can be seen that,before the summer monsoon season,the precipitation center is located in South China around 25°N.The front-like cloud structure, withitsbaselocatedat25°N,wherethenorthwardwarmerair encounters the southward colder air,is attributed to the quasistationary fronts that prevail in spring and winter.Above 11 km,there is no cloud from 20°N to higher latitudes.Following the seasonal progression of the EASM,the tropical convective systems gradually expand northward.

In June,the vertical monsoon circulation establishes over southeastern China and the center of high clouds over the SouthChinaSeaextendsnorthwardtothecontinent(Fig.4c). The occurrence frequency of high clouds over southeastern China increases in magnitude and the dip of the frequent belt moves upward to a higher level.An increase is also seen in the amount of precipitation.As will be shown later,a predominantincreaseinthecloudoccurrencefrequencyofcirrus and deep convective clouds is observed,with the latter being associated with precipitation.

Following the consecutive northward advance of summer monsoon in July,both the rain belt and frequent cloud center under 11 km arrive at their northernmost position, and the high-level frequent cloud center above 11 km expands northward(Fig.4d).It is clear that when the monsoon circulation is fully established,the maximum cloud occurrence frequency below 11 km coincides well with the vertical monsoon circulation.In the meantime,the high-level cloud center above 10 km lags behind the upwelling monsoon circulation,indicating that the out fl ow of convection is accompanied by frequent convective anvil clouds and divergence (Figs.4c and d).

From April to July,although the northward movement of the cloud system is consistent with the northward progress of monsoon circulation,the maximum cloud occurrence frequency below 11 km is found to lead the monsoon rain belt slightly(Figs.4a–d).

After August,following the southward retreat of the summer monsoon,both the cloud system and rain belt withdraw southward abruptly.The upper-level occurrence frequency center above 11 km almost disappears,and the front-like cloud system dominates South China again(Figs.4e and f).

Following the northward movement of the monsoon circulation and associated cloud system,the cloud ice water content(IWC)is observed to show a similar seasonal march (Fig.6).The consistent northward movement of the frontlike cloud system and the out fl ow of convection are also evident in the structures of IWC.

The increase in IWC following the monsoon’s progress is found to be consistent with the uplift of the cloud-top caused by an enhanced upwelling of monsoon circulation.Owing to the latitude-dependence of the tropopause,the altitude of IWC is observed to decrease with latitude(Fig.5).

The above evidence shows that the seasonal advance of the monsoon circulation determines the seasonal cycle of the cloud properties over southeastern China.The cloud system as a whole may contain several types of clouds.To demonstrate this,we analyze the occurrence frequency of deep convective clouds,altostratus,and cirrus.All of them show signi fi cant seasonal variations with their peaks in boreal summer.

Themaximumfrequencyofdeepconvectivecloudspartly represents the strength of deep convective systems,because its seasonal cycle agrees well with that of the upward motion and precipitation(Fig.6).Both the frequency and horizontal span of deep convective clouds are determined by the monsoon circulation.In boreal summer,the contribution of deep convective clouds to total cloud occurrence frequency has been found to exceed 50%in the lower and middle troposphere.Following the advance and retreat of monsoon circulation,the center of deep convective clouds has also been observed to exhibit a similar meridional movement.In addition,following the dominance of upward monsoon circulation over southeastern China in June,the frequency of convective cloud has also been noted to reach its peak(Fig.6c). InJuly,thecenterofconvectivecloudhasbeenfoundtoreach its northernmost latitude,35°N(Fig.6d).

Cirrus is also evident over southeastern China.Figure 7 displays the occurrence frequency of cirrus.In the ice cloud layer above 10 km,cirrus dominates the total cloud.The occurrence frequency of cirrus is generally higher than deep convection clouds.The center of the cirrus cloud slightly lags behind the deep convective systems,as evidenced by the center of the deep convective cloud and the rain belt.Unlike cirrus,the altostratus is located in front of deep convections in the mid-level(5–10 km).Above the convective clouds,the occurrence frequency of altostratus is extremely low( fi gure omitted).

In summary,when the summer monsoon circulation is fully established over southeastern China,the deep convective cloud is collocated with the upwelling circulation,whose central position is the same as the maximum cloudy-sky radiative heating(Fig.8).Both the cloud anvil and cirrus are coupled with the convective detrainment and divergent outfl ow of monsoon circulation in upper levels.They also spread outwardfromthecenterofconvections.Owingtotheshallowuplifts over the fronts,a large number of altostratus is found in front of the deep convective system.Following the northward march of deep convections in July,both the convective clouds and altostratus decrease sharply,but this kind of sharp transitionisnotevidentintheamountofcirrus.Thus,theseasonal variation of cloud properties over southeastern China to a large extent re fl ects the seasonal march of monsoon circulation and the corresponding cloud system.

5. The radiative heating rates of clouds over southeastern China

The EASM is one of the most important triggers for the seasonal variation of general circulation and cloud types over southeastern China.Clouds can also in fl uence the circulation through their radiative effects.To obtain information on cloud heating over southeastern China,the radiative heating rates(including longwave,shortwave,and net heating)for clear-skyandall-skyconditions areexaminedusingCloudSat FLXHR data(Fig.8).It should be noted that the clear-sky conditions are de fi ned as the cloud mask value(GEOPROF product)equal to 0(Mace,2007).The vertical pro fi le of radiative heating rates largely depends on the vertical distributions of absorbers or re fl ectors(e.g.moisture,clouds).In the following sub-sections,we discuss the clear-sky radiative heating rates and cloud effects over southeastern China.

5.1.Clear-sky radiative heating rates

The pro fi le of longwave(LW)clear-sky cooling re fl ects the impact of water vapor and other greenhouse gases.In bo-real winter(Fig.8a),the maximum LW cooling is located around 4–7 km,which corresponds to the maximum vertical gradient of moisture(Zhang and Chou,1999).Because of the greenhouse effects of moisture,the boundary layer is usually opaque to LW fl ux.Thus,the LW cooling near the surface is small and increases with height up to 3 km,indicating a well-mixed boundary layer and a gradual reduction of moisture with altitude.The clear-sky LW cooling,which peaks at 4 km,tends to have a stabilizing effect on the high-level troposphere and thus restrains the vertical penetration of deep convections.

Over southeastern China,the wintertime SW clear-sky heating rate pro fi les show heating throughout the troposphere (Fig.8b).Its distribution largely depends on the absorption of moisture and ozone(McFarlane et al.,2007).The vertical structure of SW heating reaches its maximum value at around 3–4 km,and then decreases with altitude.The magnitude of SW heating is smaller than that of LW.Thus,the net heating rate has a cooling effect in the troposphere,but turns to a heating effect above 15 km(Fig.8c).

In summer,the moisture transport due to the monsoon results in a moist atmosphere,especially in the middle troposphere.Thus,the altitude of the maximum clear-sky LW cooling uplifts to 10 km,and then decreases sharply with height(Fig.8d).They can also be found in the pro fi les of SW (Fig.8e)and net heating(Fig.8f).As the saturation vapor pressure is low at the high-level troposphere,the rapid decrease near 12 km might re fl ect CO2emissions and reduced water vapor emissions(Hartmann et al.,2001;Hartmann and Larson,2002).The destabilizing effect of LW cooling extends to the mid-level,which is favorable for the occurrence of upward motion.Another extreme LW cooling(or SW heating)occurs near the surface(Fig.5d–e),which might indicate a poorly-mixed boundary layer and is associated with decreased stratiform cloud.

The above evidence indicates that we can assume a positive feedback process between upward motion and the vertical pro fi le of moisture.Following a strong deep convection, the vertical transport of moisture also increases,which favors the extension of LW cooling and enhances its destabilizing effect,reinforcing the uplifts,and fi nally leads to a moister upper troposphere.

5.2.Cloud effects on radiative heating rates and its contribution to monsoon circulation

Both the increase in high-cloud amounts and the height of clouds in summer are resulted from the deep convection associated with the development of the summer monsoon.The changed cloud properties can also in fl uence the EASM circulation by changing the vertical pro fi les of radiative heating rates.The cloud radiative heating rates are generally de fi ned as the difference between all-sky and clear-sky radiative heating rates(McFarlane et al.,2007;Mather et al.,2007).Figure 8 clearly reveals the seasonal difference in the vertical profi les of cloud radiative heating rates.The cloud warms the atmosphere by its greenhouse effect,and thus the atmosphere below the cloud layer is warmer than that of the clear sky (Fig.8g).The cloud also in fl uences the albedo and cools the atmosphere below the cloud.At the same time,the cloud absorbs solar radiative fl uxes and heats the cloud top(Fig. 8h).In summer,following the increase in high clouds,the cloud LW heating also becomes stronger and the maximum value is evident at around 6–7 km,which is higher than in winter.Thus,the summertime high cloud serves as an additional heating source relative to the conditions of clear sky. It increases the vertical temperature gradient,which helps to maintain or even enhance the local atmospheric instability for upward motion.

Clouds also provide a stabilizing effect on the local atmosphere,as demonstrated by the SW heating rate(Fig.8h).In summer,the reinforced deep convections increase the thickness of the cloud layer and the albedo is increased,which refl ects more solar radiative fl ux and produces a cooling effect on the underlying cloud.The colder low-level atmosphere provides a stabilizing effect on the local atmosphere.

With regard to the climate mean conditions,the cloud heats the mid-troposphere over southeastern China in summer,as shown in Fig.8i.Owing to the balance between heating and adiabatic cooling through upward motion,the above-mentioned cloud radiative heating further causes upward motions over southeastern China.Such a mechanism can be explained by the thermodynamic energy equation,

This equation can be further simpli fi ed to

whereTis the temperature,Ris the gas constant,v/wis the horizontal/vertical velocity,His the scale height,andQare the heating rates.The Brunt–Vaisala frequency is de fi ned byN2=(g/θ)(?θ/?z).Over southeastern China,the vertically averaged heating rate due to clouds is approximately 0.5 K d-1in the troposphere.This indicates that the rate of ascentrequiredtobalancethisadditionalcloudradiativeheating is approximately-8 hPa d-1,with its peak appearing at around 6–8 km,where the maximum cloud heating occurs (Fig.9a).Actually,over southeastern China,the magnitude of summertime upward motion is about-20 hPa d-1in the troposphere,as shown in Fig.2.This indicates that the aggregate effect of cloud radiative heating has an important impact on local upward motion of the EASM circulation.

Such an additional rate of ascent associated with cloud radiative heating further affects the meridional wind by Sverdrup vorticity balances(Rodwell and Hoskins,2001;Zhou et al.,2009b):

wheref=2?sin?is the Coriolis parameter andβ= 2?cos?/ais its meridional gradient.Based on the Sverdrup vorticity balance,the meridional wind is proportional to the vertical velocity gradient?ω/?p(Fig.9b).Thus,northerly wind prevails over the maximum center of?ω/?pwhile southerly wind appears below the maximum center of?ω/?p(Fig.9c).

The cloud-forced upward motion and its resultant meridional wind constitute a meridional circulation(vectors in Fig. 10d)that coincides well with the EASM circulation(vectors in Fig.4d).This indicates that the cloud-forced circulation has an important impact on the EASM circulation;there is positiveinteractionbetweencloudandtheEASMcirculation.

The radiative cooling that occurs in clear–sky conditions balances the convective heating and constrains the upwelling motions through large-scale circulations(Hartmann and Larson,2002).Therefore,the vertical scale of the EASM circulation also depends on the local clear-sky radiative cooling pro fi les over southeastern China,although the cloud heating tends to enhance the EASM circulation.

The regional average of the clear-sky net radiative heating rate pro fi le is observed to show a cooling throughout the troposphere in both the seasons(Figs.8g–h).It is balanced by adiabatic heating through large-scale subsidence in clear–sky conditions and conforms to convective heating.Thus,maximum clear-sky radiative cooling occurs at altitudes with robust subsidence in clear-sky conditions and most convective clouds in cloudy conditions.Moreover,the strong decline in radiative cooling(both LW and net heating)with altitude is followed by strong convergence of mass at that level.The convergence is further balanced by the divergence of mass from convective regions.Thus,the high-frequency center of convective anvil or cirrus clouds occurs at this level,which is evident in Fig.4 and Fig.8,where large-scale meridional wind fi elds indicate a peak in convective detrainment and maximum divergence.Therefore,the altitude showing a strong decline in clear-sky net radiative cooling indicates the vertical scale of EASM upwelling or the top of convective cloud(Fig.4).

In the above analysis,the latent heating is neglected for the purpose of assessing the impact of clouds.However,we note that the latent heating should not be ignored,especiallyat the lower level.

6. Conclusions

In this study,seasonal variations of cloud properties,occurrence frequency,and IWC of clouds over southeastern China were analyzed using CloudSat data.The seasonal cycle of cloud proprieties was explained based on the changes in monsoon circulations.The energy balance due to cloud heating was also investigated.The major results can be summarized as follows:

(1)The CloudSat data reveal a signi fi cant seasonal variation in cloud properties over southeastern China.Similar to ISCCP,the high and low clouds alternately dominate in CloudSat.Different from ISCCP,the prevailing cloud in winter is stratocumulus.

(2)The EASM is one of the most important triggers for thevariationsofcloudpropertiesfromwintertosummer.The establishment of the EASM circulation and conditional instability caused by increased moisture result in frequent upward motions over southeastern China.Consequently,the high-cloud occurrence frequency increases sharply in summer.Moreover,the summertime weaker lower troposphere stability and stronger solar radiation reduce stratiform clouds in summer.

(3)Following the seasonal advance of the EASM circulation,the seasonal variations of deep convective clouds coincide well with those of the strongest upward motion and rain belt.The cirrus cloud always spreads outward from the convective systems,lags behind the rain belt,and coincides well with convective detrainment and maximum largescalemeridionalwinddivergence.Thepositionofaltostratus, which is caused by the front and uplifts fl ow,generally leads to the center of deep convective clouds.

(4)The vertical pro fi les of radiative heating rates show that both the moisture and clouds tend to destabilize the middle and lower troposphere,which is bene fi cial to the local upwelling.Clouds heat the underlying air by LW fl uxes and their upper part by SW fl uxes.Such a cloud radiative heating is required to be balanced by the rate of ascent,which further in fl uences meridional wind through the Sverdrup vorticity balance.Circulation forced by cloud radiative heating coincides well with the EASM circulation,and is comparable to the EASM circulation in magnitude.Therefore,there is positive interaction between clouds and the EASM circulation because large-scale circulations connect clear-sky radiative cooling and cloudy-sky heating.The cloud distribution and vertical scale of the EASM circulation are also consistent with the pro fi les of clear-sky radiative heating.The strong decline in radiative cooling with altitude in clear-sky conditionsisbalancedbyastrongdivergenceofmasswithfrequent convective anvil clouds,and the peak of clear-sky cooling is coupled with the convective cloud center.

Acknowledgements.This work was supported by the National Science Fund for Distinguished Young Scholars(41125017)and National Natural Science Funds of China(41405103).

REFERENCES

Arking,A.,1991:The radiative effects of clouds and their impact on climate.Bull.Amer.Meteor.Soc.,72,795–813.

Cess,R.D.,M.Zhang,B.A.Wielicki,D.F.Young,X.-L.Zhou, and Y.Nikitenko,2001:The in fl uence of 1998 El Ni?no upon cloud-radiative forcing over the Paci fi c warm pool.J.Climate,14,2129–2137.

Chen,H.,T.Zhou,R.B.Neale,X.Wu,and G.J.Zhang,2010: Performance of the new NCAR CAM3.5 in East Asian summer monsoon simulations:Sensitivity to modi fi cations of the convection scheme.J.Climate,23,3657–3675.

Ding,Y.,and J.C.L.Chan,2005:The East Asian summer monsoon:An overview.Meteor.Atmos.Phys.,89,117–142.

Hartmann,D.L.,and K.Larson,2002:An important constraint on tropical cloud–climate feedback.Geophys.Res.Lett.,29,doi: 10.1029/2002GL015835.

Hartmann,D.L.,M.E.Ockert-Bell,and M.L.Michelsen,1992: The effect of cloud type on Earth’s energy balance:Global analysis.J.Climate,5,1281–1304.

Hartmann,D.L.,J.R.Holton,and Q.Fu,2001:The heat balance of the tropical tropopause,cirrus,and stratospheric dehydration.Geophys.Res.Lett.,28,1969–1972.

Houze,R.A.,1994:Cloud Dynamics.2nd ed,Academic Press, San Diego,573 pp.

Huang,B.,and Z.-Z.Hu.,2007:Cloud–SST feedback in southeastern tropical Atlantic anomalous events.J.Geophys.Res., 112,doi:10.1029/2006JC003626.

Kanamitsu,M.,W.Ebisuzaki,J.Woollen,S.-K.Yang,J.J.Hnilo, M.Fiorino,and G.L.Potter,2002:NCEP–DOE AMIP-II reanalysis(R-2).Bull.Amer.Meteor.Soc.,83,1631–1643.

Klein,S.A.,and D.L.Hartmann,1993:The seasonal cycle of low stratiform clouds.J.Climate,6,1587–1606.

L’Ecuyer,T.S.,and J.H.Jiang,2010:Touring the atmosphere aboard the A-Train.Physics Today,63(7),36–41,doi: 10.1063/1.3463626.

L’Ecuyer,T.S.,N.B.Wood,T.Haladay,G.L.Stephens,and P.W. Stackhouse Jr.,2008:Impact of clouds on atmospheric heating based on the R04 CloudSat fl uxes and heating rates data set.J.Geophys.Res.,113,doi:10.1029/2008JD009951.

Lin,W.,M.Zhang,and N.G.Loeb,2009:Seasonal variation of the physical properties of marine boundary layer clouds off the California coast.J.Climate,22,2624–2638.

Luo,Y.,R.Zhang,and H.Wang,2009:Comparing occurrences and vertical structures of hydrometeors between eastern China and the Indian monsoon region usingCloudSat/ CALIPSO data.J.Climate,22,1052–1064.

Mace,G.,2007:Level 2GEOPROF product process description and interface control document algorithm version 5.3.[Available online at http://www.cloudsat.cira.colostate.edu.]

Mace,G.,and Coauthors,2007:Level 2 Radar-Lidar GEOPROF Product Version 1.0 Process Description and Interface Control Document.JPL,Pasadena,USA,1-20.

Mather,J.H.,S.A.McFarlane,M.A.Miller,and K.L.Johnson,2007:Cloud properties and associated radiative heating rates in the tropical western Paci fi c.J.Geophys.Res.,112, doi:10.1029/2006JD007555.

McFarlane,S.A.,J.H.Mather,and T.P.Ackerman,2007:Analysis of tropical radiative heating pro fi les:A comparison ofmodels and observations.J.Geophys.Res.,112(D14),doi: 10.1029/2006JD008290.

Norris,J.R.,and C.B.Leovy,1994:Interannual variability in stratiformcloudinessandseasurfacetemperature.J.Climate., 7(12),1915–1925.

Rajeevan,M.,and J.Sriviasan,2000:Net cloud radiative forcing at the top of the atmosphere in the Asian monsoon region.J. Climate,13,650–657.

Ramanathan,V.,and W.Collins,1991:Thermodynamic regulation ofoceanwarmingbycirruscloudsdeducedfromobservations of the 1987 El Ni?no.Nature,315,27–32.

Rodwell,M.J.,and B.J.Hoskins,2001:Subtropical anticyclones and summer monsoons.J.Climate,14,3192–3211.

Rossow,W.B.and R.A.Schiffer,1991:ISCCP Cloud Data Products.Bull.Amer.Meteor.Soc.,72,2–20.

Sassen,K.,and Z.Wang,2008:Classifying clouds around the globe with the CloudSat radar:1-year of results,Geophys. Res.Lett.,35,L04805,doi:10.1029/2007GL032591.

Stephens,G.L.,and Coauthors,2002:The CloudSat mission and the A-train.Bull.Amer.Meteor.Soc.,83,1771–1790.

Wang,B.,I.-S.Kang,and J.-Y.Lee,2004:Ensemble simulations of Asian–Australian monsoon variability by 11 AGCMs.J. Climate,15,803–818.

Wang,W.-C.,W.Gong,W.-S.Kau,C.-T.Chen,H.-H.Hsu,and C.-H.Tu,2004:Characteristics of cloud radiation forcing over East China.J.Climate,17,845–853.

Wang,Z.,and K.Sassen,2001:Cloud type and macrophysical property retrieval using multiple remote sensors.J.Appl.Me-teor.,40,1665–1682.

Wang,Z.,and K.Sassen,cited 2007:Level 2 cloud scenario classifi cation product process description and interface control document,version 5.0.[Available online at http://www.cloudsat. cira.colostate.edu.]

Xi,B.,X.Dong,P.Minnis,and M.M.Khaiyer,2010:A 10 year climatology of cloud cover and vertical distribution derivedfrombothsurfaceandGOESobservationsovertheDOE ARM SGP site.J.Geophys.Res.,115(D12),doi:10.1029/ 2009JD012800.

Xie,P.,and P.A.Arkin,1996:Analyses of global monthly precipitation using gauge observations,satellite estimates,and numerical model predictions.J.Climate,9,840–858.

Ye,D.Z.,and G.Yang,1979:Mean meridional circulations over East Asia and the Paci fi c Ocean.I:Summer;II:Winter.Sci. Atmos.Sinica,3,299–305.(in Chinese)

Yu,R.,Y.Yu,and M.Zhang,2001:Comparing cloud radiative properties between the eastern China and the Indian monsoon region.Adv.Atmos.Sci.,18,1090–1102,doi:10.1007/ soo376-001-0025-1.

Yu,R.,B.Wang,and T.Zhou,2004:Climate effects of the deep continental stratus clouds generated by the Tibetan Plateau.J. Climate.,17(13),2702–2713.

Zhang,C.,and M.-D.Chou,1999:Variability of water vapor,infrared radiative cooling,and atmospheric instability for deep convection in the equatorial western Paci fi c.J.Atmos.Sci., 56,711–723.

Zhou,T.,and Z.Li,2002:Simulation of the East Asian summer monsoon using a variable resolution atmospheric GCM.Climate Dyn.,19(2),167–180.

Zhou,T.,B.Wu,and B.Wang,2009a:How well do atmospheric general circulation models capture the leading modes of the interannual variability of the Asian–Australian monsoon?J. Climate,22,1159–1173.

Zhou,T.,and Coauthors,2009b:Why the western Paci fi c subtropical high has extended westward since the late 1970s.J. Climate,22,2199–2215.

:Guo,Z.,and T.J.Zhou,2015:Seasonal variation and physical properties of the cloud system over southeastern China derived from CloudSat products.Adv.Atmos.Sci.,32(5),659–670,

10.1007/s00376-014-4070-y.

(Received 2 April 2014;revised 9 August 2014;accepted 15 September 2014)

?Corresponding author:ZHOU Tianjun

Email:zhoutj@lasg.iap.ac.cn