06-Thermal-Processes.ppt
- 1. Thermal Processes ENVI 1400 : Lecture 6
- 2. ENVI 1400 : Meteorology and Forecasting 2 Radiation Processes Incoming solar radiation 342 W m2 Reflected by clouds, aerosol & atmosphere 77 168 30 Reflected by surface Absorbed by surface Absorbed by atmosphere 67 thermals 24 24 Evapo- transpiration 78 78 390 324 324 350 40 40 30 Surface radiation Absorbed by surface reflected solar radiation 107 W m2 back radiation emitted by atmosphere 165 Outgoing longwave radiation 235 W m2
- 3. ENVI 1400 : Meteorology and Forecasting 3 Adiabatic Processes • An adiabatic process is one in which no energy enters or leaves the system. • Many atmospheric processes are adiabatic (or nearly so) – particularly those involving the vertical movement of air. – Air is a poor thermal conductor, and mixing often slow enough for a body of air to retain its identity distinct from the surrounding air during ascent. • Near-surface processes are frequently non-adiabatic. Adiabatic Processes: – Ascent of convective plumes – Large scale lifting/subsidence – Condensation/evaporation within an airmass Non-Adiabatic Processes: – Radiative heating/cooling – Surface heating/cooling – Loss of water through precipitation – Addition of water from evaporation of precipitation falling from above
- 4. ENVI 1400 : Meteorology and Forecasting 4 Lapse Rate • Lapse Rate is the term given to the vertical gradient of temperature. • The fall in temperature with altitude of dry air that results from the decrease in pressure is called the Dry Adiabatic Lapse Rate = -9.8°C/km. 1km 9.8°C Temperature Altitude Dry Adiabatic Lapse Rate
- 5. ENVI 1400 : Meteorology and Forecasting 5 • Condensation releases latent heat, thus saturated air cools less with altitude than dry air. • There is no single value for the saturated adiabatic lapse rate. It increases as temperature decreases, from as low as 4°C/km for very warm, tropical air, up to 9°C/km at -40°C. Temperature Altitude Saturated Adiabatic Lapse Rate Dry Adiabatic Lapse Rate
- 6. ENVI 1400 : Meteorology and Forecasting 6 Pressure & Temperature • A column of air has pressure levels P1, P2, etc. • If the column is warmed, the air will expand and it’s density at any given level decrease. • The vertical interval between pressure levels increases, so that at any given altitude the pressure in the warmer column is greater than in the cooler. • N.B. since the total mass of air in the column is constant, the pressure at the surface does not change P0 P1 P2 P3 P4 P5 z cool P0 P1 P2 P3 P4 P5 warm
- 7. ENVI 1400 : Meteorology and Forecasting 7 H L cool warm warm cold-core High weakens with height, may form a low aloft H H Warm-core High intensifies with height cool cool warm L L Cold-core Low intensifies with height cool warm warm L H cool cool warm Warm-core Low weakens with height, may form a high aloft
- 8. ENVI 1400 : Meteorology and Forecasting 8 • Mid-latitude low-pressure cells have colder air to the rear. • As a result, the axis of the low slopes towards the colder air L Sea-level isobars 500 mb contours Cold low Warm high
- 9. ENVI 1400 : Meteorology and Forecasting 9 • High pressure cells slope towards the warmest air aloft. • The centre of the cell at 3000m may be displaced 10-15° towards the equator. Sea-level isobars 500 mb contours Warm high H Cold low
- 10. ENVI 1400 : Meteorology and Forecasting 10 The Thermal Low • Thermal lows result from the strong contrast in surface heating between land and sea • Land heats up (solar radiation) and cools down (infra-red radiation) much more rapidly than ocean large diurnal cycle cross-coast temperature gradient • N.B. A thermal low results from fine, clear, warm weather, and thus differs from the depressions associated with cloud and bad weather.
- 11. ENVI 1400 : Meteorology and Forecasting 11 1. Start with a horizontally uniform pressure distribution. Solar radiation starts to warm land. Air near surface is warmed by land, convection mixes warm air upwards and whole boundary layer warms. 2. Air over land warms and expands. Can’t expand sideways, so column expand upwards produces high pressure aloft. N.B. Surface pressure remains constant at this stage. warm cool cool H
- 12. ENVI 1400 : Meteorology and Forecasting 12 3. Horizontal pressure gradient aloft drives a flow from over land to over ocean. warm cool cool H 4. Mass of air in column over land is reduced surface pressure falls to produce a surface low. High pressure aloft weakens, but is maintained by continued heating at surface. Surface pressure gradient drives flow from sea to land: the sea breeze. warm cool cool H L
- 13. ENVI 1400 : Meteorology and Forecasting 13 H L 5. When solar heating stops, pressure driven flows act to equalize pressure, restoring conditions to the initial uniform pressure field. If land cools sufficiently at night, the reverse situation can be established. Over large land masses there may be insufficient time over night for the sea breeze to reach regions far from the coast, and a weak surface low is maintained over night. This then deepens during the following days, and a heat low may be maintained for days or weeks, until synoptic conditions change. warm cool H L warm
- 14. ENVI 1400 : Meteorology and Forecasting 14 Sea Breeze • Formation of local thermal low over land, results in the formation of a sea-breeze • In-flowing cool air from sea forms a sea-breeze front – a miniature cold front • Air ahead of the front is forced upward, contributing to the formation of cumulus. 1000 mb 975 mb 950 mb 25C 15C
- 15. ENVI 1400 : Meteorology and Forecasting 15 Pressure as an indicator of temperature Because the depth of a layer of air increases as its temperature increases, we can use the difference in altitude between two constant pressure levels as an indicator of the mean temperature of the layer. Charts are usually produced of the depth of the layer between 1000 and 500 mb. The layer depth is usually quoted in deca-metres (10s of metres) A useful rule of thumb is that for 1000-500 mb layer depths less than 528 dm (5280 m) any precipitation will fall as snow rather than rain.
- 16. ENVI 1400 : Meteorology and Forecasting 16 SLP (mb) & 1000-500 thickness : 48hr forecast valid 0000 040922
- 17. ENVI 1400 : Meteorology and Forecasting 17
- 18. ENVI 1400 : Meteorology and Forecasting 18 SLP (mb) & 1000-500 thickness (dm) : 36hr forecast valid 0000 040930
- 19. ENVI 1400 : Meteorology and Forecasting 19 SLP (mb) & 1000-500 thickness (dm) : analysis valid 0000 040930
- 20. ENVI 1400 : Meteorology and Forecasting 20 12°C 2°C 850 mb Temperature (2°C contours), RH (%), wind (m s-1) : analysis valid 0000 040930
- 21. ENVI 1400 : Meteorology and Forecasting 21 Surface temperature (2°C contours) and SLP (mb)(5mb contours) : analysis valid 0600 040930
- 22. ENVI 1400 : Meteorology and Forecasting 22 The Thermal Wind • It is commonly observed that clouds at different altitudes move in different directions winds are in different directions. • The gradient of wind velocity (speed & direction) is called the (vertical) wind shear. • In the free air, away from surface (where friction effects complicate matters), the wind shear depends upon the temperature structure of the air. • The thermal wind is a theoretical wind component equal to the difference between the actual wind at two different altitudes. • Any two levels can be used, but unless otherwise stated the altitudes of the 1000mb and 500mb levels are usually used. • Note that the 1000mb level might be below sea level, and is usually within the boundary layer and thus influenced by friction effects at the surface.
- 23. ENVI 1400 : Meteorology and Forecasting 23 1000mb 996 1004 1008 HIGH LOW Vg(1000) warm cold 500mb LOW HIGH
- 24. ENVI 1400 : Meteorology and Forecasting 24 60 0 120 180 HIGH LOW 5760 5820 5700 5640 VG500 VT LOW HIGH VG1000 5700 5640 5580 500-1000 mb thickness Contours of 1000 mb surface Contours of 500 mb surface
- 25. ENVI 1400 : Meteorology and Forecasting 25 • Note that cold air is to the left of the thermal wind vector (looking along wind) in the northern hemisphere, to the right in the southern hemisphere. • The decrease in temperature towards the poles results in a westerly thermal wind in the upper atmosphere in both hemispheres. • The largest meridional temperature gradient occurs in mid-latitudes across the polar front. • The thermal wind makes up a significant component of the jet-stream, located over the upper part of the polar front.