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If a particle is climbing in an CSI zone, it will cool down and the water vapor will condense upon saturation, giving cloud and precipitation by oblique convection. For example, in front of a warm front, the air mass is stable because the mild air overcomes a cold mass. The geostrophic equilibrium brings back any particle moving perpendicularly from the center of the depression towards it. However, an upwardly oblique displacement by [[synoptic scale]] upward acceleration in an CSI layer produces parallel bands of heavy rainfall.<ref name="Schultz"/><ref>{{cite web | language = en | url= http://www.crh.noaa.gov/lmk/?n=paper-1/17/94 | title= Vertical Motion Forcing Mechanisms Responsable for the Production of a Mesoscale very heavy snow band across Northern Kentucky | publisher = [[National Weather Service]] | author= Theodore W. Funk | author2= James T. Moore}}</ref>
Conditional symmetric instability affects a layer that can be thin or very large in the vertical, similar to hydrostatic convection. The thickness of the layer determines the enhancement of convective [[precipitation]] within a region otherwise [[stratiform]] clouds <ref name=Schultz/>. As the motion is in an area near saturation, the particle remains very close to the [[Lapse rate#Moist adiabatic lapse rate|moist adiabatic lapse rate]] which gives it a limited [[Convective available potential energy]] (CAPE). The rate of climb in a slantwise convection zone ranges from a few tens of centimeters per second to a few meters per second.<ref name=Schultz/>. This is usually below the climbing speed limit in a [[cumulonimbus]], ie 5 m/s, which gives [[lightning]] and limit the
* The trailing precipitation region of [[mesoscale convective system]]s.
* Wintertime convection because
* In the [[Eye (cyclone)|eyewall]] during the deepening phase of mature hurricanes, although rarely as it is a region symmetrically neutral and is generally free of lightning activity.
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