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Wojciech W. Grabowski

others. However, in nature, convective clouds continuously interact with their surroundings through gravity waves and detrainment that modify their environment (e.g., Bretherton and Smolarkiewicz 1989 ). These interactions affect development of subsequent clouds. Thus, it is irrelevant what the first cloud does, but what matters is a response of an ensemble of clouds to realistic forcings averaged over many cloud realizations. (An exception to this argument might be when the first cloud causes a

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Peter J. Marinescu, Susan C. van den Heever, Max Heikenfeld, Andrew I. Barrett, Christian Barthlott, Corinna Hoose, Jiwen Fan, Ann M. Fridlind, Toshi Matsui, Annette K. Miltenberger, Philip Stier, Benoit Vie, Bethan A. White, and Yuwei Zhang

type of deep convective cloud system under consideration can alter the effect that aerosol particles have within deep convective updrafts (e.g., Seifert and Beheng 2006b ; Khain et al. 2008 ; van den Heever et al. 2011 ). Supercells that are primarily driven by dynamical forcings have been shown to have lesser impacts from varying CCN concentrations than other types of deep convection (e.g., Grant and van den Heever 2015 ). Another cause of complication stems from differences in studies that

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Jie Peng, Zhanqing Li, Hua Zhang, Jianjun Liu, and Maureen Cribb

, which would decrease maximum wind speeds. This was supported by observations of how variations in aerosols accounted for an 8% variation in the intensity of Atlantic hurricanes ( Rosenfeld et al. 2011 ). Wang et al. (2014) have also shown that both precipitation and net cloud radiative forcing (CRF) over the northwestern Pacific are enhanced by Asian pollution via the invigoration of winter cyclones. A review of aerosol effects on the intensity and microphysics of tropical cyclones has been given

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Jiwen Fan, Yuan Wang, Daniel Rosenfeld, and Xiaohong Liu

impacts on cloud radiative forcing from the meteorological effects in observations and poor parameterizations of convection and clouds in numerical simulations especially for large-scale models cause the largest uncertainty in current estimates of climate forcing, which resides in aerosol–cloud interactions (ACI) that are traditionally referred to as aerosol indirect effects ( IPCC 2013 ). How aerosols affect cloud properties and precipitation through ACI strongly varies among cloud types that are

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Yan Yang, Jiwen Fan, L. Ruby Leung, Chun Zhao, Zhanqing Li, and Daniel Rosenfeld

constitute the largest uncertainty in climate forcing and projection ( IPCC 2013 ). Through ARI, aerosol particles reduce the energy reaching the surface by scattering and absorbing solar radiation. Absorbing aerosols such as black carbon (BC) can also heat the lower-level atmosphere by absorbing sunlight, which may increase atmospheric stability locally and influence the large-scale circulation, convection, and precipitation (e.g., Fan et al. 2008 , 2015 ; Lau and Kim 2006 ; Zhang et al. 2009a

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Luke B. Hande, C. Hoose, and C. Barthlott

Brownian motion; is the sum of phoretic forces (kg m 3 s −2 ); and and are the thermophoretic force (kg m s −2 ) and diffusiophoretic force (kg m s −2 ), respectively. The governing equations presented above are also described in numerous other references ( Martin et al. 1980 ; Pruppacher et al. 1998 ; Ladino et al. 2011 ). In such a model, hydrodynamic effects are treated very simply compared to the trajectory model ( Grover et al. 1977 ), where the actual vapor density, temperature, and velocity

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Andrew R. Jongeward, Zhanqing Li, Hao He, and Xiaoxiong Xiong

other radiative forcing agent ( IPCC 2013 ). Further in-depth studies are needed to probe and assess any long-term changes in aerosol and its ensuing changes in clouds and other climate variables. Recent work has shown that aerosol loading is not constant on decadal time scales. For example, Mishchenko et al. (2007) show a globally decreasing trend in aerosol optical depth (AOD) over oceans beginning in the 1990s using observations from the Advanced Very High Resolution Radiometer (AVHRR), whereas

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Yun Lin, Yuan Wang, Bowen Pan, Jiaxi Hu, Yangang Liu, and Renyi Zhang

those of its individual cloud components, it is necessary to evaluate the long-term response of the various cloud types when assessing the aerosol direct and indirect radiative forcings. 4. Summary and conclusions The aerosol microphysical and radiative effects on an evolving continental cloud complex occurring from 25 May to 27 May 2009 during the DOE ARM RACORO field campaign are investigated. The TAMU-WRF model with a two-moment bulk microphysics by Li et al. (2008b) and a modified Goddard

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Tianmeng Chen, Jianping Guo, Zhanqing Li, Chuanfeng Zhao, Huan Liu, Maureen Cribb, Fu Wang, and Jing He

isolate the signal attributed to aerosol loading from that attributed to environmental forcing. The LTS is calculated as the difference between potential temperatures at 700 and 1000 hPa. The ω at the following pressure levels were chosen for investigation of the dependence of aerosol–cloud interaction on atmospheric environment: 825 hPa for shallow and deep Cu clouds, 600 hPa for Ns clouds, and 400 hPa for DCC. The roles of these environmental factors in the development of MCOG and CTH under clean

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Jianjun Liu, Zhanqing Li, and Maureen Cribb

indirect effect; Albrecht 1989 ). AIE are the dominant contributors to the overall aerosol radiative forcing in most climate models yet are poorly constrained and can vary by a factor of 5 across different models ( Quaas et al. 2009 ; Wood et al. 2015 ). Marine boundary layer (MBL) clouds are common over the subtropical and midlatitude oceans and are particularly susceptible to perturbations in aerosols ( Wood et al. 2015 ). These clouds strongly influence regional and global climate systems

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