PHSC 3033: Meteorology Stability

Transcription

1 PHSC 3033: Meteorology Stability

2 Equilibrium and Stability Equilibrium s 2 States: Stable Unstable Perturbed from its initial state, an object can either tend to return to equilibrium (A. stable) or deviate away (B. unstable).

3 Environmental Lapse Rate (ELR) Γ = - T/ z Measured change in Temperature with Altitude Radiosondes yield information about the environmental lapse rate. It is what it is on average ~ 6.5 o C/1000m. This lapse rate can be equal to, less than, or greater than either the dry adiabatic lapse rate or moist adiabatic lapse rate. Determining stability involves asking what happens to a parcel of air if there is a small perturbation (vertical motion). What is its equilibrium like, stable or unstable?

4 Figure 6.4

5 Figure 6.3

6 Rising and Sinking Air Rising air expands and cools. Sinking air contracts and warms.

7 Adiabatic Process Expansion and cooling or compression and heating without any thermal exchange with the environment is an adiabatic process. Adiabatic Lapse Rates Γ Dry = - T/ z = -g/c p { ~10 o C/1000m } = -9.8 m/s J/kg/K Γ Wet = - T/ z { ~ 6 o C/1000m }

8 Eureka! In air, scale reads the weight W = T 1. Immersed in water, the additional buoyant force reduces the objects weight T 2 = W-F b Displaced fluid weight = ρ f V o g = F b (Archimedes Principle) F b T 1 T 2 W W

9 Buoyancy Archimedes Principle: The buoyancy force is equal to the weight of the volume of fluid displaced. Weight of the volume of fluid* displaced ρ f V o g Weight of the object ρ o V o g The net force on an object is its weight minus the buoyancy F = ρ o V o g - ρ f V o g *The environmental air is treated as a fluid in which a parcel of air is immersed.

10 Buoyancy and Acceleration Acceleration = Force/mass Acceleration = g(ρ o V o - ρ f V o )/m = g(ρ o - ρ f )/ρ o F = Weight - F b F = ρ o V o g - ρ f V o g Replacing densities using the ideal gas law P = ρ k T, yields an equation for the acceleration of the air parcel, given the temperature of the parcel (T o ) and the environment (T f ). Acceleration = g(τ o - Τ f )/Τ o Large temperature differences favor acceleration. a ~ T

11 Environmental lapse Rate (ELR) is black unsaturated adiabatic parcel path (blue) saturated parcel path (red)

12 A) unstable parcel in unsaturated environ B) stable parcel in unsaturated environ C) unstable parcel in saturated environ D) stable parcel in saturated environ

13 Summary of categories of atmospheric layer stability Environmental lapse rate ( Γ = ELR) Stability Γ = ELR > 10 C/km Unstable Dry Adiabat Wet Adiabat

14 Summary of categories of atmospheric layer stability Environmental lapse rate ( Γ = ELR) Stability Γ = ELR > 10 C/km 6 C/km < ELR < 10 C/km ELR < 6 C/km ELR = 10 C/km ELR = 6 C/km Unstable Conditionally unstable (Unstable if saturated, stable if unsaturated) Stable Neutral if unsaturated, unstable if saturated Neutral if saturated, stable if unsaturated

15 An atmosphere with an environmental lapse rate (ELR) will be... Stability Conditions Always Stable if ELR < Γ Dry ELR < Γ Wet Always Unstable if ELR > Γ Dry ELR > Γ Wet

16 Absolute Stability (Dry) The parcel of air is cooler and heavier than the surrounding air around it at all levels. Γ < Γ dry When perturbed it will tend to return to its original position.

17 Absolute Stability (Wet) The atmosphere is always stable when the environmental lapse rate is less than the moist adiabatic rate. Γ < Γ wet

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19 Convective Uplift Vertical Motion via Convection: exchange of thermal energy by mass motion. Hot air rises because it is less dense. Lifting a parcel of air to a height where condensation occurs, releases the latent heat stored in the water vapor as clouds form.

20 Lifting Mechanisms in the Atmosphere

21 Frontal Uplift Vertical Motion via Frontal Uplift: a cold air mass encounters warm air or a warm air mass encounters cooler air. Since colder air is more dense, it displaces the warm air upward in a cold front or a warm front along the air masses boundary.

22 Orographic Uplift Vertical Motion via Orographic Uplift: air that encounters steep topography is forced to rise.

23 Convergence Uplift Vertical Motion via Convergence: advection winds that encounter each other force rising motion away from the surface. Air rises because there is nowhere else to go.

24 Absolute Stability

25 A Stable Atmosphere Stability favors a small environmental lapse rate. Ways to make the lapse rate small. Warm the air aloft (Inversions) warm advection (warm front) slowly sinking air (high pressure) Cool the air near the ground (Fogs) calm night radiative cooling cold advection (cold front) air moving over a cold surface

26 Absolutely Unstable (Dry) The atmosphere is always unstable when the environmental lapse rate is greater than the dry adiabatic rate. Γ > Γ Dry > Γ Wet

27 Absolutely Unstable (Wet) The parcel of air is warmer and lighter than the surrounding air around it at all levels. When perturbed it will tend to accelerate away from its original position.

28 Absolutely Unstable

29 Conditional Stability (Dry) In this example the dry air is cooler and heavier than the air around it at all levels. It is stable. The environmental lapse rate is less than the dry adiabatic lapse rate. But, Γ Dry > Γ > Γ Wet

30 Conditionally Unstable (Wet) A saturated parcel is warmer than the surrounding air at all levels. It is unstable. With an environmental lapse rate between the dry and moist adiabatic rates, stability depends upon whether the air is saturated or not.

31 Conditional Stability If air can be lifted to a level where it is saturated, instability would result.

32 Figure 6.7

33 Table 6.2 Table 6.2 Stability categories and likelihood of severe convective storms for various ranges of the Lifted Index (LI), Showalter Index (SI), Convective Available Potential Energy (CAPE), Total Totals (TT) index and SWEAT index. Stability LI SI CAPE TT SWEAT Very stable > +3 (no significant activity) Stable 0 to +3 > +2 < 0 (Showers possible; T showers unlikely) Marginally unstable 2 to 0 0 to (T showers possible) Moderately unstable 4 to 2 3 to (Thunderstorms possible) Very unstable 6 to 4 6 to (Severe T storms possible) Extremely unstable < 6 < 6 > 3500 > 400 (Severe T storms probable; tornadoes possible)

34 Figure 6B

35 Conditional Stability

36 Conditional Stability

37 Instability Causes Instability favors a large environmental lapse rate. Ways to increase the lapse rate large. Cool the air aloft cold advection (jet stream) radiative cooling (emitting IR to space) Warm the air near the ground warm advection daytime solar heating of the surface

38 Mixing Instability Mixing may occur via convection or turbulence.

39 Stratocumulus

40 Stratus Formation Mixing stable air close to saturation can cause stratus-type clouds. The upper layer cools and saturates while the lower layer warms and dries out, increasing the environmental lapse rate.

41 Rising Instability As a stable layer rises, the change in density spreads it out. If it remains unsaturated, the top cools faster than below.

42 Convective Instability An inversion layer with a saturated bottom and an unsaturated top. The top cools at Γ Dry while the bottom cools at Γ Wet because of latent heat release. This leads to absolute instability associated with severe storms.

43 Cumulus Convection A warm wet bottom and a cool dry top. Convection leads to large vertical development while the sinking air in between the clouds is clear.

44 Cumulus Conditions

45 Cumulus Development Instability may reach to the top of the troposphere where cumulonimbus clouds anvil out in response to the stable inversion layer of the stratosphere.

46 Mountain Rain Shadow Orographic lifting, adiabatic cooling, heating and loss of moisture content.

47 Adiabatic Chart (Rain Shadow Example)

48 Summary A parcel of air in stable/unstable equilibrium will return/depart its original position. A rising parcel of unsaturated air will cool at the dry adiabatic rate of (~ 10 o C/1000m); a descending unsaturated parcel warms at this rate. A rising parcel of saturated air will cool at the moist adiabatic rate of (~ 6 o C/1000m); a descending saturated parcel warms at this rate. The environmental lapse rate is the rate that the actual air temperature decreases with increasing altitude. Γ = - T/ z Absolute Stability: Air at surface is cooler than air aloft (inversion), or the environmental lapse rate is greater than the dry adiabatic rate. Instability can be initiated if surface air warms, air aloft cools, or vertical lifting occurs (convection, convergence, fronts, topography). Conditional Instability: Environmental lapse rate is between the moist and dry adiabatic rates. Unsaturated air is lifted to a point where condensation occurs and becomes warmer than the surrounding air.

49 Relative Humidity The relative humidity can be calculated from the vapor pressure (e) and saturation vapor pressure (e s ) and/or the mixing ratio (w) and saturation mixing ratio (w s ) RH % = 100 (e/e s ) = 100 (w/w s ) Vapor Pressure (mb) or Mixing Ratio (g/kg) (T,e s ) or (T,w s ) (T,e) or (T,w) Temperature

50 Dew Point The dew point temperature (T d ) can be taken from the temperature and saturation vapor pressure (e s ) and/or the saturation mixing ratio (w s ). RH % = 100 (e/e s ) = 100 (w/w s ) Vapor Pressure (mb) or Mixing Ratio (g/kg) (T,e) or (T,w) T d Temperature

51 Wet-Bulb Temperature At a given pressure level, do the following: From the temperature, proceed up along a dry adiabat. From the dew point proceed up along a mixing ratio line. At the intersection, proceed down the saturation adiabat to the original level. In this example, air at 850 mb with T = 20 C and T d = 0 C has a wet-bulb temperature of 10 C.

52 Lifting Condensation Level (LCL) The LCL is located on a sounding at the intersection of the saturation mixing-ratio line that passes through the surface dew point temperature with the dry adiabat that passes through the surface temperature. In this example, air at the surface with T=9 C and T d =0 C will become saturated if lifted dry adiabatically to 870 mb.

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