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Robert F. Rogers, Jun A. Zhang, Jonathan Zawislak, Haiyan Jiang, George R. Alvey III, Edward J. Zipser, and Stephanie N. Stevenson

. Efforts to reconcile these apparently different conclusions are ongoing. In terms of deep convection, a preferred radial and azimuthal distribution in the inner core has been identified as more favorable for intensification. For the radial distribution, a preponderance of deep convection inside the radius of maximum winds (RMWs) is favorable for intensification, since diabatic heating in the region of high inertial stability and upper-level subsidence around the periphery of the convective outflow

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Jonathan Zawislak, Haiyan Jiang, George R. Alvey III, Edward J. Zipser, Robert F. Rogers, Jun A. Zhang, and Stephanie N. Stevenson

symmetric and asymmetric components. The symmetric processes focus on the cooperative interaction between the primary and secondary circulations, and the impact of symmetric diabatic heating on this interaction ( Ooyama 1969 , 1982 ; Schubert and Hack 1982 ; Nolan and Grasso 2003 ; Nolan et al. 2007 ). Asymmetric mechanisms can assume a variety of scales and causal factors. These factors include environmental vertical wind shear (e.g., Reasor et al. 2009 ; Molinari and Vollaro 2010 ; Reasor and

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E. P. Nowottnick, P. R. Colarco, S. A. Braun, D. O. Barahona, A. da Silva, D. L. Hlavka, M. J. McGill, and J. R. Spackman

. (2007) showed that dust acting as CCN can reduce mean cloud droplet diameter, impacting storm diabatic heating, thermodynamic structure, and intensity. On the other hand, Jenkins et al. (2008) and Jenkins and Pratt (2008) found observational evidence that Saharan dust can invigorate precipitation by serving as CCN and INP, suggesting that dust entrainment serves as a mechanism for enhancing tropical convection. In this study, we investigate aerosol–radiation and aerosol–cloud interaction

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Alan Brammer, Chris D. Thorncroft, and Jason P. Dunion

. 12 . Vortex stretching through diabatic heating is likely the primary method for vorticity generation throughout this time; therefore, understanding the influences on the short-term precipitation forecasts is crucial to understanding the later evolution of the vortex. These figures highlight that after a certain lead time, hours 24–48 for these forecasts, the evolution of the vortex becomes largely dependent on its the strength and convective activity at earlier lead times. Members that continue

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William A. Komaromi and James D. Doyle

of a synoptic-scale anticyclone that exists above the level of maximum outflow, a decrease in height of the level of maximum radial outflow with time resulting in a “remnant” diabatically generated remnant upper-level anticyclone as the outflow descends, or some other process. Composites of V r , inertial stability, and Γ in radius–pressure coordinates for all intensifying ( Figs. 8a,b ) and nonintensifying and weakening ( Figs. 8c,d ) TCs are also examined. The level of maximum is fairly

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