2. Skew T Log P Diagram AOS 330 LAB 10

3. Outline Static (local) Stability Review Critical Levels on Thermodynamic Diagram Severe Weather and Thermodynamic Diagram

4. Static (local) Stability Static Stability: Stability of the atmospheric layer w.r.t. small vertical displacements of air parcel within the layer. Let’s consider an air parcel that has the same temperature as the environment and is at rest. Now, give it a slight push upward. As it moves upward, it adiabatically expands and cools. At the new level higher up, it could : 1) be denser than its surrounding, sink back down to its original position. (STABLE) 2) be less dense than its surrounding, continue to rise. (UNSTABLE) 3) have the same density as its surrounding, will continue to rise until it encounters enough friction to stop it. (neutral)

5. Absolutely Stable Parcel is unsaturated, it cools following dry adiabatic lapse rate. ΓdΓd ΓdΓd Γ As parcel rises(sinks), it is cooler(warmer) than its environment, it would want to move back to its original position. ΓmΓm

6. Absolutely Unstable Parcel is unsaturated, it cools following dry adiabatic lapse rate. ΓdΓd ΓdΓd Γ As parcel rises(sinks), it is warmer(cooler) than its environment, it would want to continue to rise(sinks). ΓmΓm Unstable for both saturated / unsaturated parcels.

7. Conditionally Unstable Parcel is unsaturated, it cools following dry adiabatic lapse rate. ΓdΓd ΓdΓd Γ ΓmΓm ΓmΓm Parcel is saturated, it cools following moist/pseudoadiabatic lapse rate. Stable when parcel is unsaturated. Unstable when parcel is saturated.

8. Neutral ΓmΓm Γ Saturated neutral Dry neutral Potentially Stable Potentially Unstable Stable Neutral Unstable

9. Atmospheric Soundings Plotted Thermodynamic Diagram To determine what atmospheric processes may undergo. Help us to identify clouds Allow us to identify stability of a layer Identify critical levels and to determine at which levels the parcel would be saturated and/or buoyant. The level at which the parcel is saturated depends on both its moisture content and the processes that an atmosphere is going though.

10. The information on diagrams will allow us to determine things such as: CAPE (Convective Available Potential Energy) CIN (Convective INhibition) DCAPE (Downdraft Convective Available Potential Energy) Maximum updraft speed in a thunderstorm Hail size Height of overshooting tops Layers at which clouds may form due to various processes, such as: – Lifting – Surface heating – Turbulent mixing

11. Critical Levels on Thermodynamic Diagram

12. The level at which a parcel lifted dry adiabatically will become saturated. Find the temperature and dewpoint of the parcel (at the same level, typically the surface). Follow the mixing ratio up from the dewpoint, and follow the dry adiabat from the temperature, where they intersect is the LCL. Lifting Condensation Level (LCL)

13. Finding the LCL

14. Level of Free Convection (LFC) The level above which a parcel will be able to freely convect without any other forcing. Find the LCL, then follow the moist adiabat until it crosses the temperature profile. At the LFC the parcel is neutrally buoyant.

15. Example of LFC

16. Equilibrium Level (EL) The level above the LFC at which a parcel will no longer be buoyant. (At this point the environment temperature and parcel temperature are the same.) It is a level of neutral buoyancy. Above this level the parcel is negatively buoyant. The parcel may still continue to rise due to accumulated kinetic energy of vertical motion. Find the LFC and continue following the moist adiabat until it crosses the temperature profile again.

17. Example of finding the EL

18. Convective Condensation Level (CCL) Level at which the base of convective clouds will begin. From the surface dew point temperature follow the mixing ratio until it crosses the temperature profile of sounding.

19. Convective Temperature (CT) The surface temperature that must be reached for purely convective clouds to develop. (If the CT is reached at the surface then convection will be deep enough to form clouds at the CCL.) Determine the CCL, then follow the dry adiabat down to the surface.

20. Finding the CCL and CT

21. Mixing Condensation Level (MCL) This represents the level at which clouds will form when a layer is sufficiently mixed mechanically. (i.e. due to turbulence) To find the MCL determine the average potential temperature (  ) and average mixing ratio (w) of the layer. Where the average  and average w intersect is the MCL.

22. Finding the MCL

23. Thermodynamic Diagrams and Severe Weather

24. What is Severe Thunderstorm? Tornado Wind Gust > 50 knots Hail > or = 3/4inch

25. Convective Available Potential Energy (CAPE) Remember: Area on a thermodynamic diagram is proportional to energy. CAPE on a thermodynamic diagram is the area between the parcel and the environment temperatures from the LFC to the EL CAPE is also called buoyant energy. CAPE is a measure of instability

26. CAPE

28. If we convert the potential energy of CAPE to a kinetic energy, we can get the maximum speed of any updraft that may develop. Maximum Updraft Speed

29. Convective Inhibition (CIN) CIN on a thermodynamic diagram is the area between the parcel and the environment temperatures from the surface to the LFC CIN is NOT negative CAPE!!!!!! – CAPE tells us the maximum amount of energy that may be released by the parcel through ascent. – CIN tells us how much energy must be used to lift a parcel from surface to LFC. (Energy barrier) CIN is a measure of stability Reported as an absolute value

30. CIN

31. Overcoming Convective Inhibition A convective outbreak rarely occurs from surface heating alone! Triggering Mechanisms for T-Storms – fronts – dry lines – sea-breeze fronts – gust fronts from other thunderstorms – atmospheric bouyancy waves – mountains

32. Cap Strength Very important for severe weather to develop Too little or no cap: happy little cumulus everywhere Too strong of a cap: nothing happens Just the right amount of a cap: Severe Weather

34. At the inversion * look at the temperature difference between the parcel and the environment.

35. References Petty, G (2008). A First Course in Atmospheric Thermodynamics, Sundog Publishing. Potter and Coleman, 2003a: Handbook of Weather, Climate and Water: Dynamics, Climate, Physical Meteorology, Weather Systems and Measurements, Wiley, 2003 Links: http://www.spc.noaa.gov/faq http://www.srh.noaa.gov/oun/severewx