# Clouds. Ulrike Lohmann Department of Physics and Atmospheric Science, Dalhousie University, Halifax, N. S., Canada

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1 Clouds Ulrike Lohmann Department of Physics and Atmospheric Science, Dalhousie University, Halifax, N. S., Canada

2 Outline of this Lecture Overview of clouds Warm cloud formation Precipitation formation in warm clouds Ice cloud formation Summary of cloud microphysical processes

3 Basic 10 Cloud Types in 4 Families Cumulus : vertical development Stratus : layered cloud Cirrus : ice clouds Low Base with vertical extent : Cu, Cb, Ns Low Base and layered : (0-2 km) : St, Sc Middle Altitude : (2-7 km) : As, Ac High Altitude (Ice clouds) (5-13 km) : Ci, Cs, Cc

4 Fog, Stratus, Stratocumulus, Nimbostratus ington.edu/gcg/atlas/

5 Convective Clouds [http://www.atmos.washington.edu/gcg/atlas]

6 Middle Clouds [http://www.atmos.washington.edu/gcg/atlas] Subtype of Ac: Castellanus

7 High Clouds (Ice) [http://www.atmos.washington.edu/gcg/atlas]

8 Orographic Clouds [http://www.atmos.washington.edu /gcg/atlas]

9 Clausius-Clapeyron Equation de s /dt = L e s2 /(R v T 2 ) R v = gas constant of water vapor e s = saturation vapor pressure over water/ice L = latent heat of vaporization/sublimation T = temperature

10 Köhler Curve consists of Raoult s law and Kelvin equation: e s (r)/ e s ( ) = exp ({2 σ}/{ρ w R v T r}) = exp (a/r) r = droplet radius e s (r) = saturation vapor pressure of droplet of size r e s ( ) = saturation vapor pressure over a bulk surface of water σ = surface tension = water density ρ w Saturation ratio Critical radius Number of molecules µm 2.5 x µm 2.8 x nm nm 20

11 Köhler Curve (2) Raoult s law: For a plane water surface the reduction in vapour pressure due to the presence of a non-volatile solute may be expressed: e* ( )/e s ( ) = 1 (3 ν m M w )/(4 π M s ρ w r 3 ) = 1 - b/r 3 e s * ( ) = saturation vapor pressure of bulk solution = molecular weight of the solute, M s m s ν = mass of the solute, = degree of dissociation.

12 Köhler Curve (3) Combination of Kelvin and Raoults equation (evaluated for e*(r)/e s (r)) gives the Koehler curve: e*(r)/e s ( ) = (1 - b/r 3 ) * exp(a/r) ~ 1 + a/r - b/r 3 1. term: surface molecules possess extra energy 2. term: solute molecules displacing surface water molecules a ~ /T [m] b ~ i M s /m s [m 3 /mol] M s = mass of salt [kg] m s = molecular mass of salt [kg/mol] The critical radius r c and critical supersaturation S c are given by: r c = (3b/a) 1/2, S c = (4 a 3 /[27 b]) 1/2

13 r c, S c

14 Cloud Droplet Formation r c, S c

15 Observed Cloud Droplet Spectra

16 Cloud Properties in a Developing Cloud

17 Droplet Sizes [Rogers and Yau, 1989]

18 Droplet Growth Equation Before and after the droplet reaches the critical size, it grows by diffusion of water molecules from the vapor onto its surface. r dr / dt = ( S 1 ) / [ F k + F d ] S = ambient saturation ratio F k = heat conduction term ~ L 2 ρ w / R v KT 2 F d = vapor diffusion term = ρ w R v T / D e s D = diffusion of water vapor in air K = thermal conductivity of air

19 Droplet Growth Equation (2)

20 Evolution of Droplet Population [Rogers and Yau, 1989]

21 How Does Warm Rain Form? Cloud droplets initially grow by condensation, then through collision-coalescence (sticking together). Coalescence is not efficient when droplets < 14 µm Problems in explaining observed droplet growth: e.g., growth rate to a 14 µm droplet by condensation ~10-20 min growth by collision-coalescence from 20 µm to 100 µm ~1 hour i.e., the combined growth time is longer than the lifetime of small, precipitating cumulus clouds

22 Cloud Spectrum Widening Need to overcome an effective radius of 14 µm before the collision-coalescence process becomes effective How? Turbulence or giant CCN Turbulence may help by providing overlapping eddies, different drop inertias, effects of shear

23 Giant Cloud Condensation Nuclei [Feingold et al. 1999]

24 Can Sea Salt Cleanse Air Pollution over Oceans? [Rosenfeld et al. 2002]

25 Can Sea Salt Cleanse Air Pollution over Oceans? [Rosenfeld et al. 2002]

26 Collision-Coalescence Coalescence Process

27 Collision efficiencies of water droplets of different size by gravitational settling Warm Rain Formation [Pruppacher and Klett, 1997]

28 Turbulent Collision Efficiencies [Charmaine Franklin et al. 2003] Separation distance = 0.04 cm E(gravitational) = 0.08 (theoretical values ) Collision Efficiency Collision Kernel x Collision Efficiency 2.3 x g 7.4 x g 1.7 x g 1.8 x g gravity R λ R λ

29 Rain Drop Spectra [Willis, 1984]

30 Warm Cloud Growth Regimes [Cotton, personal notes]

31 Different Ice Nucleation Mechanisms Contact Freezing T Warmer Immersion/Condensation Deposition Colder

32 Different Ice Nucleation Mechanisms

33 Requirements for Ice Nuclei (IN) Insolubility: so that IN do not disintegrate under action of water (mineral dust, black carbon) Size: IN must be larger than > 0.1 µm, a critical ice embryo (mineral dust) Chemical bonds: complex organic molecules (aerobic bacteria) have hydrogen bonding groups similar to ice (cholesterol) Crystallographic resemblance to ice (silver iodide AgI) Active Sites: need pits and steps on ice nuclei (dirty AgI works better for cloud seeding than clean AgI)

34 Ice Nuclei Concentration vs. Temperature

35 Ice Nuclei Concentration vs. Size

36 Clausius-Clapeyron Equation de s /dt = L e s2 /(R v T 2 ) R v = gas constant of water vapor e s = saturation vapor pressure over water/ice L = latent heat of vaporization/sublimation T = temperature

37 Bergeron-Findeisen Process

38 Seeder-Feeder Process

39 Mixed Phase Cloud

40 Summary of Cloud Microphysical Processes [Encyclopedia of Atmospheric Sciences]

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