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ATMOSPHERIC STABILITY INDICIES
Lifted Index (LI) This is an index used to determine the stability of the lower half of the troposphere. An air parcel is lifted from the surface with temperature and mixing ratios representative of the mean layer values of the lowest 100 mb of the atmosphere. This is done in order to capture low level boundary layer temperature and moisture conditions while reducing diurnal effects. This hypothetical parcel is then lifted dry adiabatically to the LCL and pseudoadiabatically to 500 mb. The value of this index is the temperature of the environment subtracted from the temperature of the parcel at 500 mb. The risk of thunderstorms and severe weather activity is defined as follows: LI > 2 No significant activity
0 < LI < 2 Showers/thunderstorms possible with other source of lift 2 < LI < 0 Thunderstorms possible 4 < LI < 2 Thunderstorms more probable, but few, if any severe LI < 4 Severe thunderstorms possible Showalter Index (SI) This is an index used to determine the stability of the lower half of the troposphere. An air parcel is lifted from an initial position at 850 mb where localized low level influences are greatly reduced. It is lifted dry adiabatically to its LCL and then pseudoadiabatically to 500 mb. The environmental temperature is then subtracted from the parcel temperature to obtain the value of the Showalter index. The risk of severe weather activity is defined as follows: SI > 3 No significant activity
1 < SI < 3 Showers possible with other source of lift 2 < SI < 1 Thunderstorms possible (generally weak) 3 < SI < 2 Thunderstorms more probable (possibly strong) 6 < SI < 4 Strong or severe thunderstorms possible SI < 6 Any thunderstorms likely to be strong or severe Total Totals Index (TT) The Total Totals index is a simple index derived from the temperature lapse rate between 850 mb and 500 mb and moisture content at 850 mpse rate between 850 mb and 500 mb and moisture content at 850 mb. It is defined as follows: TT = T850 + Td850  2T500 The risk of severe weather activity is defined as follows: 4445 Isolated moderate thunderstorms
4647 Scattered moderate / few heavy thunderstorms 4849 Scattered moderate / few heavy / isolated severe thunderstorms 5051 Scattered heavy / few severe thunderstorms and isolated tornadoes 5255 Scattered to numerous heavy / few to scattered severe thunderstorm / few tornadoes > 55 Numerous heavy / scattered severe thunderstorms and scattered tornadoes K Index (KI) The K index is similar to Total Totals index except that it takes into account moist air at 700 mb contributing to air mass thunderstorm development. The K index is defined as follows: K = T850  T500 + Td850  (T700  Td700) The risk of air mass thunderstorms is defined as follows: K < 15 near 0% Air mass thunderstorm probability
1520 <20% Air mass thunderstorm probability 2125 2040% Air mass thunderstorm probability 2630 4060% Air mass thunderstorm probability 3135 6080% Air mass thunderstorm probability 3640 8090% Air mass thunderstorm probability K > 40 >90% Air mass thunderstorm probability SWEAT ( Severe Weather thrEAT ) Index This is an United States Air Force index that takes into account thermal instability, low level moisture content, vertical wind shear and horizontal wind speeds. The risk of severe weather activity is defined as follows: SW < 300 No severe storms expected
300 < SW < 400 Possible severe thunderstorms SW > 400 Severe thunderstorms likely and possible tornadoes Bulk Richardson Number (BRN) Ratio between the CAPE and the wind shear vector difference. A valuable tool in determining if potential storms will be supercells. MUST be used with other thunderstorm parameters when making thunderstorm decisions. BRN < 10 Probably too much shear for thunderstorms
BRN > 10 < 45 Supercells possible BRN > 45 Storms more likely to be multicells rather than supercells Convective Available Potential Energy (CAPE): CAPE + represents the vertically integrated positive buoyancy of an adiabatically rising parcel. Proportional to the amount of kinetic energy that a parcel gains while it is warmer than the surrounding environment. Parcel ascent is enhanced by this instability. CAPE represents the cumulative effect of atmospheric layers that are warmer than the parcel moving vertically along an adiabat. These stable layers often inhibit lowlevel parcel ascent. CAPE < 1000 instability is WEAK
CAPE > 1000 < 2500 MODERATE instability CAPE > 2500 STRONG instability
