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Section 04 Adiabatic Processes and Stability

Section 04 Adiabatic Processes and Stability. Lessons 12 & 13. Adiabatic Process. An adiabatic process is one which involves no transfer of heat or mass across an imaginary boundary. An air parcel is said to cool or warm adiabatically under these conditions.

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Section 04 Adiabatic Processes and Stability

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  1. Section 04Adiabatic Processes and Stability Lessons 12 & 13

  2. Adiabatic Process • An adiabatic process is one which involves no transfer of heat or mass across an imaginary boundary. • An air parcel is said to cool or warm adiabatically under these conditions.

  3. Dry Adiabatic Lapse Rate3.0°C/1000 ft - 1.0°C/100m 15C

  4. Saturated Adiabatic Lapse Rate1.5°C/1000 in Lower Atmosphere - 0.3°C/100m 5C

  5. Dew Point Lapse Rate • The Dew Point Lapse Rate (DPLR) is the rate at which the dew point inside a rising air parcel decreases due to the decreasing atmospheric pressure. • It has a value of 0.5°C/1000 feet – 0.13 °C/100m

  6. Dew Point Lapse Rate 0.5°C/1000 ft– 0.13 °C/100m

  7. Upper Air Sounding

  8. SIMPLIFIED ADIABATIC DIAGRAM DP 15°C OAT 20°C

  9. Föhn Effect SALR DALR DPLR DALR DPLR DP 12°C OAT 20°C

  10. Atmospheric Stability/Instability • Stability discourages vertical motion. • Instability encourages vertical motion; • The degree of stability/instability depends on the environmental lapse rate (ELR) and moisture content.

  11. Atmospheric Stability/Instability • Stability/Instability of air determines the weather • Unstable air gives: • Cumuliform cloud • Rain showers and good visibility • Stable air gives: • Fine hazy weather, moderate to poor visibility or • Layer cloud or fog

  12. -15°C -5°C 0°C -9°C -1°C 3°C -3°C 3°C 6°C 3°C 7°C 9°C 9°C 11°C 12°C 15°C 15°C 15°C Conditional Instability Atmospheric Stability 10000 ft. ELR>SALR & ELR<DALR 8000 ft. 3°C/1000’ 1.5°C/1000’ 6000 ft. Rising air COOLER than environment -STABLE Rising air WARMER than environment -UNSTABLE ENVIRONMENT 4000 ft. 2000 ft. Surface Dry Adiabatic Lapse Rate (DALR) Environmental lapse Rate 2°C/1000’ (ELR) Saturated Adiabatic Lapse Rate (SALR

  13. -5°C 5°C 0°C 0°C -15°C -1°C 7°C -9°C 3°C 3°C 1.5°C/1000’ 3°C 9°C 6°C 6°C -3°C 1°C 7°C 11°C 3°C 9°C 9°C 13°C 11°C 8°C 9°C 12°C 12°C 15°C 15°C 15°C 15°C 15°C 15°C Saturated Adiabatic Lapse Rate (SALR Environmental lapse Rate 1°C/1000’ (ELR) Dry Adiabatic Lapse Rate (DALR) ELR<SALR Absolute Stability 10000 ft. 8000 ft. 3°C/1000’ 6000 ft. 4000 ft. 2000 ft. Surface

  14. -20°C -15°C -20°C 0°C 0°C -13°C -9°C -13°C 3°C 3°C 3°C/1000’ 1.5°C/1000’ -6°C 6°C 6°C -3°C 1°C 1°C 3°C 9°C 9°C 8°C 8°C 9°C 12°C 12°C 15°C 15°C 15°C 15°C 15°C Environmental lapse Rate 3.5°C/1000’ (ELR) Dry Adiabatic Lapse Rate (DALR) Saturated Adiabatic Lapse Rate (SALR ELR>DALR Absolute Instability 10000 ft. 8000 ft. 6000 ft. 4000 ft. 2000 ft. Surface

  15. Lapse Rates • The Environmental Lapse Rate (ELR) is the rate at which the unlifted surrounding air layers cool. • The Dry Adiabatic Lapse Rate (DALR) is the rate at which a parcel of dry or unsaturated air cools as it rises or warms as it sinks. • The Saturated Adiabatic Lapse Rate (SALR) is the rate at which a parcel of saturated air cools as it rises. • The DALR is modified to this value by the release of Latent Heat of Condensation in the rising air parcel.

  16. ELR<SALR (or SALR>ELR)

  17. Absolute Stability • The ELR is less than the SALR (ELR<SALR); • A rising saturated air parcel would cool at 1.5°C/1000 feet (SALR); • It would be cooler than it’s surroundings and sink back • A dry or unsaturated air parcel would cool at 3°C/1000 feet (DALR); • It would still be cooler than it’s surroundings and sink back. • The ELR is therefore described as as absolutely stable. • It can also be described as a shallow lapse rate.

  18. ELR > DALR (or DALR < ELR)

  19. Absolute Instability • If the ELR is greater than 3°C/1000 feet (ELR >DALR); • Rising saturated air will cool at 1.5°C/1000 ft (SALR); • It will be warmer than it’s surroundings at all levels and keep rising. • Rising dry or unsaturated air will cool at 3°C/1000 ft (DALR); • It will be warmer at all levels than it’s surroundings and keep rising. • Such an ELR is described as absolutely unstable. • Such “steep” ELR’s occur very rarely.

  20. ELR > SALR And ELR < DALR

  21. Conditional Instability • Conditional Instability • Is the most usual state of the atmosphere. • If the rising air parcel is dry or unsaturated, it cools at the DALR of 3°C/1000 feet if forced to rise. • At all altitudes it is cooler than it’s surroundings and would sink back. • If the parcel is saturated, however, it would cool at the SALR of 1.5°C/1000 feet if forced to rise. • At all altitudes it is warmer than it’s surroundings and would keep rising

  22. Conditional Instability (Cont.) • ELRs lying between the DALR and the SALR are therefore generally described as being conditionally unstable; • The condition for instability being that: • the air is saturated, or will become saturated through cooling by lifting at some low level. • If the air parcel is initially dry or unsaturated it is stable. • If it is initially saturated it will be unstable.

  23. Effect of Inversion on Cloud Development • Inversion arrests the vertical development Insolation

  24. Subsidence Inversion • Subsiding air compresses and warms, • Spreads out at low level causing the inversion WARM

  25. Cooling at SALR Warming at DALR FÖHN/CHINOOK WIND Wet windward slope Rain shadow, hot,dry air Warm moist air

  26. Chinook Wind Effect 20C +13 C +12 C 10C 10:30 05:00 0C 09:40 10:45 -10C -12 C -20C -20 C Rapid City - South Dakota January 22nd 1943

  27. Effect on Stability of Cold/Warm Advection • Advection of warm air over a cold surface: • Cooled in the boundary layer. • The boundary layer mixing also modifies the lapse rate and produces an inversion at the top of the mixing layer. • This will further stabilise the air in addition to the cooling caused by the cold surface.

  28. Advection of cold air aloft over warm air at the surface: • This will steepen the lapse rate considerably aloft causing extreme instability and severe thunderstorms. • A classic example of this is warm tropical maritime air moving north over the central plains of the USA. If cold dry air from the NW advects aloft over the warm air it will produce the extreme unstable conditions for supercell thunderstorms.

  29. Advection of cold air over a warm surface: • Warmer surface will steepen the lapse rate in the lower layers due to the turbulent mixing and thermal activity and increase the instability.

  30. Advection of warmer air aloft: • Generally increases stability due to the formation of an inversion at the interface between the cold and the warm air. • However the degree of instability will ultimately depend on the environmental lapse rate in the air aloft.

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