Lecture Ch. 6 Condensed (Liquid) Water

• Saturation of moist air • Ch. 4: Will H2O condense? • Relationship between and dewpoint – Clausius-Clapeyron describes esat(T) – Clausius-Clapeyron equation • Ch. 5: What will H2O condense on? • Dewpoint – Kohler describes droplet formation – • Ch. 6: How much H2O will condense? – Depression – Dew point temperature provides metric • Isobaric cooling • Ch. 7: How does condensed H2O affect stability? • Moist adiabatic ascent of air – Conditional stability is affected by moist adiabats • Equivalent temperature • Ch. 8: What happens to condensed H2O? • Aerological diagrams – processes Curry and Webster, Ch. 6

Cloud in a Jar Demonstration How does saturation occur?

• By increasing – of water at surface – Evaporation of falling rain http://www.youtube.com/ • By cooling watch?v=XH_M4jItiKw – Isobaric – Radiative cooling of rising air • By mixing of two unsaturated air parcels

http://groups.physics.umn.edu/demo/old_page/demo_gifs/4B70_20.GIF Curry and Webster, Ch. 6

Saturation of Moist Air Saturation of Moist Air

• Dew point temperature • Clausius-Clapeyron equation at dew point

R T v = v v p

dp L = lv dT p R T 2 € v Llv dln p = 2 dT RvT dln p L = lv dT R T 2 Curry and Webster, Ch. 6 v

€

1 Clausius Clapeyron Dewpoint and Humidity

• Recall by integration between two • Integrating from ambient to saturation we had

• (T-TD)

1.0

T=2C INCORRECT! T=24C Figure is wrong. T=46C 0.8

0.6

0.4 Relative Humidity Relative

0.2

0.0 0 5 10 15 20

Dewpoint Depression (T-Td)

Start with measured Equivalent T and Td with altitude, then overlay

ws(T).

2 Equivalent Potential Temperature Temperature Metrics

• : The temperature air would have at the given • Accounts for liquid water heating and density if there were no water vapor in it • Potential Temperature: The temperature a parcel would have if it were brought adiabatically and reversibly to p0 (usually 1 atm) • Virtual Potential Temperature: The temperature a parcel would have if there were no water vapor in it (only condensed water) and if it were

brought adiabatically and reversibly to p0 (usually 1 atm) • Equivalent Temperature: The temperature that an air parcel would have if all of the water vapor were to condense in an adiabatic isobaric process Although approximate, (6.48) retains the of water • Equivalent Potential Temperature: The temperature a parcel would vapor provides energy to the moist air and increases its temperature have if all of the water were condensed in an adiabatic isobaric process relative to what the temperature would have been in dry adiabatic and if it were brought adiabatically and reversibly to p0 (usually 1 atm) ascent.

T vs. ln(p) Emagram (T is vertical; thetas slant left) {1884}

Stuve diagram (T is vertical) Tephigram (T slants right; thetas slants left) {1927} {1915}

areas contained by the curves have equal energies for equal areas, leading to better comparisons of CAPE and hence convective systems

3 Skew-T Log P (T slants right) {1947} Dew • All temperatures are point: equal at the horizontal 1000 mb e=es(TD) level near the How to find dew bottom. point and frost – red lines are isotherms, ws~4 g/kg wv=w-ws=11 g/kg point? – dashed green lines are the equivalent Cool isobarically potential temperature; until reaching – solid green lines are the T saturation. potential d temperature • Blue lines are the isobars (scale on the Frost left side) • Dashed purple lines point: are the saturated e=e (T ) humidity mixing Then follow theta-e s F ratio (ws(T), i.e. adiabat to 400hPa nearly parallel to T) Follow theta to 1000hPa saturation (T=Td=30C)

Td=20C wv~15 g/kg T=30C

Enthalpy Change for Parcel 1 Mixing Line Phase+Temperature Change (subsaturated)

Clausius-Clapeyron (with exagerated curvature) Parcel 2 (subsaturated)

N.B. For mixture to be supersaturated, need two parcels very close to saturation at two somewhat different temperatures.

Enthalpy Change for Wet-Bulb Temperature Phase+Temperature Change

4 Radiation Transport in the Atmosphere

Latent Heat accounts for 78 W/m2!

What did we learn in Ch. 6?

• formation – what causes saturation?

– Cooling to decrease es(T) – Increasing water vapor to increase e – Mixing of two nearly-saturated parcels

• Enthalpy balance: How much H2O will condense? – from evaporation causes cooling – Latent heat from condensation causes warming

• Dew point (TD) and frost point (TF) temperatures – Cool isobarically until saturation is reached

– RH scales with dewpoint depression (T-TD) • Llv affects energy balance (Kiehl+Trenberth, 1997)

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