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frontogenesis or a strengthening temperature gradient over time. In contrast, cold fronts in which the wind shifts are not coincident with the temperature gradient imply frontolysis or a weakening temperature gradient over time as dissipative processes (e.g., mixing) dominate. Second, in some cases, the prefrontal wind shift or trough may develop a temperature gradient and thus become frontogenetical, eventually leading to clouds and precipitation. Third, given the right environmental conditions, convective
frontogenesis or a strengthening temperature gradient over time. In contrast, cold fronts in which the wind shifts are not coincident with the temperature gradient imply frontolysis or a weakening temperature gradient over time as dissipative processes (e.g., mixing) dominate. Second, in some cases, the prefrontal wind shift or trough may develop a temperature gradient and thus become frontogenetical, eventually leading to clouds and precipitation. Third, given the right environmental conditions, convective
corresponds tothe warm boundary of the frontal zone (not shown).This orientation of maximum vertical motions relativeto the midtropospheric frontal zone is consistent withparcel frontogenesis and frontolysis in the frontal entrance and exit, respectively, as described previouslyin the discussion of Fig. 30. Vertical cross sections of the total (geostrophic plusageostrophic) transverse flow for the inflection in theflow coinciding with the frontal entrance region (Fig.32) exhibit subsidence along a
corresponds tothe warm boundary of the frontal zone (not shown).This orientation of maximum vertical motions relativeto the midtropospheric frontal zone is consistent withparcel frontogenesis and frontolysis in the frontal entrance and exit, respectively, as described previouslyin the discussion of Fig. 30. Vertical cross sections of the total (geostrophic plusageostrophic) transverse flow for the inflection in theflow coinciding with the frontal entrance region (Fig.32) exhibit subsidence along a
