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ENTRAINMENT and MICROPHYSICS in RICO Cu

ENTRAINMENT and MICROPHYSICS in RICO Cu. Hermann Gerber. NASA/GISS Workshop Sept. 2006. CLASSICAL ENTRAINMENT CONCEPT. Erosion (Detrainment). Rising Toroidal Thermal. Entrainment. X. Scorer, R.S., and F.H. Ludlam: 1953 : Bubble theory of penetrative

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ENTRAINMENT and MICROPHYSICS in RICO Cu

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  1. ENTRAINMENT and MICROPHYSICS in RICO Cu Hermann Gerber NASA/GISS Workshop Sept. 2006

  2. CLASSICAL ENTRAINMENT CONCEPT Erosion (Detrainment) Rising Toroidal Thermal Entrainment X Scorer, R.S., and F.H. Ludlam: 1953: Bubble theory of penetrative convection. Q.J. Roy. Meteor. Soc., 79, 317-341. (Blyth, A.M., et al., 1988: J. Atmos. Sci., 45, 3944-3964.) (Baker, B., A., 1992: J. Atmos. Sci., 49, 387-404.) (Damiani, et al, 2006: J. Atmos. Sci., 63, 1432-1450)

  3. MICROPHYSICS ISSUES 1. Homogenous or inhomogeneous mixing? 2. What about entrained CCN? 4.Super-AdiabaticDrops? 3. Entrainment scales?

  4. HOMOGENOUS MIXING INHOMOGENEOUS MIXING ADIABATIC PEAK SUPER ADIABATIC (Lasher-Trapp, S., W. Cooper, and A. Blyth, 2005: QJRMS, 195-220)

  5. RICO FLIGHTS

  6. CONDITIONAL SAMPLING FOR ACTIVE TURRETS VERTICAL VELOCITY IS POSITIVE (~80%) IN AREA WITHLWC TOP OF CLOUD IS VISIBLE IN FORWARD-LOOKING VIDEO CLOUD IS TRAVERSED NEAR CLOUD TOP A SINGLE TURRET IS TRAVERSED (Raga, G.B., et al, 1990: J. Atmos. Sci., 47, 338-355.)

  7. (m)

  8. PVM FSSP Fast FSSP

  9. PVM

  10. 10-cm RESOLUTION (1000 Hz) LWC DATA PVM

  11. INHOMOGENEOUS EXTREME HOMOGENEOUS c or (Brenguier, J.-L.,and F. Burnet, 1996: 12th Int. Conf. Clouds and Precip; Zurich; 67-70) (Gerber, H., et al, 2001: J. Atmos. Sci., 58, 497-503) (Burnet,F., and J.-L. Brenguier, 2006: J. Atmos. Sci., in print) (Schleuter, M.H., 2006: Master’s Thesis, U. of Utah)

  12. (Blyth A.M., and J. Latham, 1991: J.A.S., 48, 2367-2371) (Gerber, H., et al, 2000: 13th Int.Conf. Clouds and Precip., Reno, NV, 105-108)

  13. COMPOSITE OF 35 Cu IN

  14. COMPOSITE FRACTIONAL ENTRAINMENT RICO, RF12 .0062 djc /dz = -e (jc- je) e = fractional entrain. j = scalar = qT e =environment c = cloud

  15. COMPOSITE TKE DISSIPATION TKE (diss. rate) = [v’(rms)]3/L v’ = gust velocity L = penetration length = 40m TKE INHOMOGENEOUS

  16. CLOUD EDGE 1000 Hz -60 -50 -40 -30 -20 -10 0 10 20 (Brenguier, J.-L, 1993: J. Appl. Meteor., 32, 783-793)

  17. COMPOSITE OF ENTRAINED PARCEL LENGTH (Brenguier, J-L, and W.W. Grabowski, 1993: J. Atmos. Sci., 50, 120-136) (Kreuger, S.K., et al, 1997: J. Atmos. Sci., 54, 2697-2712)

  18. COMPOSITE OF ENTRAINED PARCEL PENETRATION

  19. ENTRAINMENT CONCEPT ENTRAINMENT SHEATH DILUTION DOMINATES RH HALO? VORTEX RINGS? NO HOLES SMALL PARCELS X SUPER-ADIABATIC DROPS? NEW CCN ACTIVATION

  20. TURRET SPECTRA

  21. THANK YOU hgerber6@comcast.net

  22. SPARE SLIDES FOLLOW

  23. Cu (Courtesy of Dr. Jim Hudson)

  24. RELAXATION TIME ANALYSIS tDrop(s)= 4r2 / [4x10-10 x (1-S)] tTurb.(s) = (D2 / TKEdiss.)1/3 D = entrained parcel width (m) r = droplet radius [10--5 (m)] tDrop(s) >> 1 R = HOMOGENEOUS MIXING tTurb.(s) tDrop(s) << 1 R = INHOMOGENEOUS MIXING tTurb.(s)

  25. RELAXATION TIME RATIO, R CLOUD #21 S .77 .99 tdrop(s) 5 100 D(m) 2 20 2 20 tturb(s) 8.5 40 8.5 40 R .59 .1212 2.5

  26. (Damiani, R., G. Vali, and S. Haimov, 2006: J.A.S., 1432-1450)

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