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Jake P. Mulholland, Stephen W. Nesbitt, Robert J. Trapp, and John M. Peters

simulation and line along which the west-to-east-oriented vertical cross sections of terrain are shown in (c) (red dashed line), and (c) west-to-east-oriented vertical cross sections of terrain height taken through the peak of the terrain for each simulation [km; see red dashed line in (b)]. Radiation and surface fluxes of heat, moisture, and momentum were included to allow for the development of realistic slope flows and natural DCI without prescribing a warm/cold “bubble” in proximity to the heated

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Hernán Bechis, Paola Salio, and Juan José Ruiz

mechanisms have been proposed to explain the strength of the low-level moisture gradient leading to the formation of drylines. Frontogenesis caused by shearing deformation and confluence acting over the moisture fields is one of them ( Anthes et al. 1982 ; Ziegler et al. 1995 ). Drylines can also appear as a consequence of inhomogeneities in land cover type or soil conditions. For example, strong differences in soil moisture can lead to horizontal gradients in surface moisture fluxes which can directly

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Sujan Pal, Francina Dominguez, María Eugenia Dillon, Javier Alvarez, Carlos Marcelo Garcia, Stephen W. Nesbitt, and David Gochis

the warm air advection at ~30°S at the lower level. To understand the role of lower-level moisture advection during this event we plot a Hovmöller diagram of meridional wind ( V wind; Fig. 8a ) and moisture flux due to meridional wind ( Vq ; Fig. 8b ). It is clear that prior to the event ~0000 UTC 27 November, there is a strengthening of northerly SALLJ (deep purple shading) at ~850 mb carrying moisture southward. We see a reversal of lower-level wind direction after the event ~0000 UTC 28

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