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Aaron Johnson, Xuguang Wang, Kevin R. Haghi, and David B. Parsons

1989 ; their Eqs. (2.4)–(2.6)]: Here, h 1 is the depth of the stable layer after bore passage, C is the bore speed, g ′ is reduced gravity, and u 1 is the bore-relative flow (different from the density current relative flow U ). It has been shown ( Klemp et al. 1997 ; Kingsmill and Crook 2003 ) that the following equation improves upon the derivation for C in Eq. (3) and Rottman and Simpson (1989) by including the effects of energy dissipation by undulations and turbulence and the

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Aaron Johnson and Xuguang Wang

-allowing and convection-parameterizing ensemble forecasts of a mesoscale convective vortex and associated severe weather environment . Wea. Forecasting , 25 , 1052 – 1081 , . 10.1175/2010WAF2222390.1 Coleman , T. A. , and K. R. Knupp , 2011 : Radiometer and profiler analysis of the effects of a bore and a solitary wave on the stability of the nocturnal boundary layer . Mon. Wea. Rev. , 139 , 211 – 223 , . 10

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Samuel K. Degelia, Xuguang Wang, and David J. Stensrud

near the ongoing surface-based convection, convective-scale regions along the borders of the storms are moistened by the final assimilation cycle ( Figs. 17b,h ). This moisture impact is maximized at 600 hPa ( Fig. 18 ). Assimilating wind profilers and rawinsonde observations produces similar effects near the ongoing convection ( Figs. 17d,f ), though additional moisture is already present due to the effects discussed previously. The additional moisture from assimilating Doppler lidar and surface

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Manda B. Chasteen, Steven E. Koch, and David B. Parsons

and surface-based CAPE ( Figs. 10h,i ). To our knowledge, no prior studies have examined the influence that such prominent moisture plumes have on nocturnal convection within central Texas. The effects of baroclinicity on the LLJ structure are more pronounced within regions of strongly sloped terrain, which were spatially varying owing to the complex topography of west Texas. Using the inference that spatial gradients in buoyancy generate horizontal vorticity, Gebauer et al. (2018) explained

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Samuel K. Degelia, Xuguang Wang, David J. Stensrud, and Aaron Johnson

the thermodynamic profile. A sounding valid 45 min before CI that has been modified for the two profiles of vertical velocity is shown in Fig. 14 . The one-dimensional model to modify a sounding is taken from Stensrud and Maddox (1988) and only considers the effects of vertical velocity and latent heating. The governing equations are where is designed to maintain saturation and is defined as Other terms include as the latent heat of condensation, as the specific heat at constant pressure

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Tammy M. Weckwerth and Ulrike Romatschke

was used to distinguish between hydrometeor types at each radar gate ( Vivekanandan et al. 1999 ). A beam blockage algorithm was used to account for the propagation effects and the convolution of the beam pattern with the terrain features. Prior validation with rain gauges showed a high correlation coefficient of 0.834, providing confidence in this enhanced QPE algorithm ( Dixon et al. 2015 ). Fig . 1. Precipitation (mm) shown for 11 Jun 2015 at (a) 0000, (b) 0100, (c) 0200, and (d) 0300 UTC

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Dylan W. Reif and Howard B. Bluestein

effects of sea/land breezes. The warm season, defined here as April–July, was chosen because much of the nocturnal convection over the Great Plains occurs during that time period ( Wallace 1975 , Fritsch et al. 1986 ). To identify the CI events, 2 radar composite data were examined from the UCAR MMM radar composite archive (available online at ). The radar data are available in 30-min intervals for most days and only the central and southern Great Plains were

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