MIXING AND ENTRAINMENT AT STRATOCUMULUS TOP
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1 MIXING AND ENTRAINMENT AT STRATOCUMULUS TOP Szymon P. Malinowski with contributions from: Sławomir Błoński, Patrick Chuang, Krzysztof E. Haman, Hermann Gerber, Anna Górska, Wojciech W. Grabowski, Djamal Khelif, Marta Kopeć, Piotr Korczyk, Tomasz A. Kowalewski, Wojciech Kumala, Marcin Kurowski, Katarzyna Nurowska Multiphase Turbulent Flows in the Atmosphere and Ocean Workshop, Geophysical Turbulence Program National Cenetr for Atmospheric Research Boulder, CO, USA August 13-17, 2012
2 Cloud stew: slowly cooked from below, cooled from above Stevens, Annu.Rev Earth Planet. Sci Notice strong inversion, almost a rigid lid!!!
3 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY
4 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY
5 Rigid lid from above Photos courtesy Gabor Vali
6 Aircraft penetration of the upper part of marine Sc cloud. Stevens et al., BAMS, 2003, Gerber et al., JAS, 2005
7 High-resolution measurements inside cloud hole : LWC and water vapor mixing ratio (upper panel), temperature and droplet density (middle panel), droplet diameter (lower panel) The red line helps to visualize effects of different location of the sensors and various response. Haman et al., QJRMS, 2007
8 Cloud (filament?) edges in 1000 Hz temperature (thin line) and LWC (thick line) records. Sharp jumps in LWC and temperature at distances of the order of 10 cm (data resolution) can be seen. Notice shifts between the temperature and LWC records resulting from the 6 m separation between the instruments.
9 From the top to the bottom: successive blow ups of 10 khz temperature records showing selfsimilar structures filaments of significantly different temperatures separated by narrow interfaces. The bottom panel presents the evidence for filaments of thickness of the order of 10 cm as well as for the steep gradients of temperature.
10 Cloud holes regions of depleted LWC during DYCOMS occurred to be negatively buoyant convective plumes. Gerber et al., JAS 2005
11 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY
12 LES with EULAG. DX=DY=35m DZ=5m Mean profiles of: total water content (left) virtual potential temperature (middle) enstrophy (right) after 3,4 and 5 hours of simulations. Kurowski et al., 2009
13 Passive scalar was added above inversion after 3 hours of simulation. Passive scalar concentration χ (left, cloud water contours shown by white lines) and enstrophy (right), at 6 hours of simulations.
14 Mixing across the inversion: Dynamic stability (in terms of Richardson number Ri) and intensity of turbulence (in terms of enstrophy) on the inversion layer (TS) and top of the cloud (QS).
15 Mixing diagram showing buoyancy (density temperature) of mixture of cloud and free-tropospheric air (upper lines) and cloud and EIL air (lower lines).
16 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY LESSONS LEARNT 1. Cloud top is located below the inversion and below the level of maximum temperature gradient. 2. Entrainment events are initiated in regions where local shear is strong enough to destabilize the flow despite the strong static stability. 3. In cloud holes the negatively buoyant mixture of cloudy and free troposphere air descends down into the boundary layer. 4. We do not have good data on turbulence, high-resolution sensors must be collocated.
17 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY
18 POST proposal Hermann Gerber, 2007
19 POST (Physics of Stratocumulus Top) - aircraft field study off the California Coast in A single aircraft was used to primarily investigate unbroken stratocumulus clouds (Sc) near cloud top. The aircraft was instrumented with a full suite of probes for measuring state parameters of the atmosphere, drop spectra, CCN, irradiances, wind velocity and turbulence. microphysics FAST: aerosol (CCN) Turbulence Humidity LWC Temperature droplet counting
20 Data from POST available at
21 Ultra Fast Thermometer UFTM amplifiers (shown on the vane) protecting rod sensing wires 1 and 2 Kumala et al., 2010,2012
22 In turbulent temperature fluctuations In relatively calm, thermally uniform, free troposphere
23 Measurement strategy NexSat image (courtesy Naval Research Laboratory, Monterey) of CA and the Pacific Ocean showing the typical horizontal flight track used for each quasi Lagrangian Twin Otter flight. The red star indicates the Marina airport near Monterey Bay. Typical vertical flight pattern of the Twin Otter during POST flights. Porpoising through cloud top is the dominant feature. Notice that cloud deck does not have to be stable in course of flight.
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25 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY
26 Many POST flights show different structure of SC top than DYCOMS! Gerber et al., 2010, 2012
27 Classical TO10, 2008/08/04 17:15 22:15 UTC (daytime: local time = UTC -8)
28 TO10 typical sounding: a remarkable inversion (10K). Notice a shear layer just above the cloud top -no shear in DYCOMS!!! Malinowski et al., 2011, 2012
29 FT TIL CTML EIL CTL
30 TO10: LWC on ~1.2m long samples (40Hz): maximum on the top, gradual decrease down except on dilution in mixing events
31 TOF 10: PDF's of LWC and droplet concentrations (courtesy Partick Chuang)
32 wind shear temperature gradient Turbulent Kinetic Energy TKE [m2/s2] TO10
33 Non classical TO13, 2008/08/09 00:52 06:00 UTC (evening)
34 Non classical flight TO13: weak inversion, wind shear in the cloud top layer, high humidity above.
35 FT TIL EIL CTML CTL
36 Notice steep temperature jumps: sharp edges of filaments...
37 TO13: LWC on ~1.2m long samples (40Hz): Clou top diluted, no gradual increase of LWC towards the top.
38 TOF 13: PDF's of LWC and droplet concentrations (courtesy Partick Chuang)
39 wind shear temperature gradient Turbulent Kinetic Energy TKE [m2/s2]
40 FT - free troposphere, TIL, TISL - turbulent inversion sublayer, CTML,CTMSL - cloud top mixing sublayer, EIL - entrainment interfacial layer, RMSV - root mean square velocity in m/s, Ri - bulk Richardson number, Lc/Lo - ratio of Corrsin and Ozmidov scales S - shear, N Brunt-Vaisala frequency
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42 TOF13: 100Hz (55cm resolution) temperature and LWC on horizontal leg inside cloud deck Upper panel: 100S/s records of LWC and T and covariances LWC' T' on a horizontal leg inside the cloud at the altitude of 550m. Right panel: histograms of LWC' T' at altitudes of 550m and 504m. Positive buoyancy in cloud holes!!!???
43 Histograms of LWC' T' in horizontal legs inside the Stratocumulus deck (inside CTL and CL). LWC'<0 T'<0 - depleted LWC - temperature deficit TO10 left negative buoyancy in cloud holes TO13 right positive buoyancy in cloud holes??? on some legs
44 Histograms of LWC' T' W' in horizontal legs inside the Stratocumulus deck. TO10 left TO13 right W' <0 downdraft How important are tails of the distribution? Do they really represent entrainment events?
45 TOF 10 TOF 13 For TOF10 mixtures of air from the cloud top and above EIL of fraction χ <0.12 of clear air are negatively buoyant, only those of fraction χ <0.11 are saturated after mixing. It means, that cloudy parcels of reduced LWC are likely to be removed down by negative buoyancy. TOF13 mixing across inversion cannot not result in negative buoyancy! Latent heat effects affect buoyancy marginally, mixtures of as high fraction of clear air as χ<0.7 are still cloudy. This means that most of mixed parcels maintain cloud water and they remain on the level where mixing occurred, if not affected by other dynamical effects. This explains observed differences in LWC profiles and in LWC' T' correlations!!!!
46 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY
47 Estimates of TKE dissipation rates in consecutive layers of stratocumulus top for all three velocity components No of cases No of cases No of cases
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49
50 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY MAIN FINDINGS: 1. Inversion is turbulent. 2. EIL is marginally unstable. This marginal dynamic instability governs EIL thickness and (probably) mass exchange. 3. Cloud holes do not have to be negatively buoyant. 4. Structure of the cloud top depends on CTEI ability to remove mixed air from the cloud top down due to negatively buoyant mixed parcels.
51 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY
52 Turbulent cloud chamber The set-up of the experiments is designed to mimic basic aspects of small-scale turbulent mixing of a cloudy air with unsaturated environment. new setup old setup
53 Turbulent cloud chamber in the lab:
54 A negatively buoyant cloud pumped into cloud chamber by a tube in the bottom chimney
55 Gentle filling of the cloud chamber with a negatively buoyant cloudy air through a chimney allows to obtain a layer of cloud capped by an inversion and create in this way a laboratory analogue of stratocumulus cloud. Evaporative cooling stabilizes the cloud top.
56 34*43cm 9*13cm Laser sheet photographs of the weak updraft diverging below inversion.
57 PIV Particle Imaging Velocimetry Principle: two consecutive frames compared; displacement of patterns allows to determine two components of the velocity. Special algorithms: iterative (with the increasing resolution) correlation of patterns; mean motion removal; iterative deformation of patterns; median filtering. Result: benchmark scenes show the average accuracy of the displacement detection =0.3 pixel size. Korczyk et al. 2006, 2012.
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59 Laser sheet photographs of vigorous negatively buoyant starting plume penetrating the inversion.
60 Velocity retrievals of the starting plume.
61 Negatively buoyant evaporating plume penetrating capping inversion HORIZONTAL STRUCTURES -EFFCT OF STATIC STABILITY AND DECELERATION (CONVERGENCE IN VERTICAL) VERTICAL STRUCTURES - EFFECT OF EVAPORATIVE COOLING AND ACCELERATION (DIVERGENCE IN VERTICAL)
62 Summary temperature inversion of thickness 20 cm capping stratocumulus top can be produced in the chamber velocity fields in high- and low- resolution images agree qualitatively estimated values of TKE in high- and low- resolution images are in a reasonable agreement ε values are of order of these observed in stratocumulus, Rλ~40 low resolution images do not allow to properly resolve small scale features of flow, which affects estimates of ε and Ω
63 Overview: DYCOMS high resolution measurements DYCOMS numerical modeling of entrainment POST high resolution measurements POST entrainment and mixing at Sc top POST turbulence LAB analogue of Sc cloud first results SUMMARY 1. Mixing across inversion capping SC top is due to shear (local resulting from divergence of updrafts, or nonlocal) which allows to destabilize the flow despite the high static stability. 2. Structure of the cloud top (dilution of LWC, nature of cloud holes) is governed by buoyancy of mixed parcels. For CTEI conditions classical Sc, for NON-CTEI conditions non-classical Sc. 3. In the lab we may produce analog of Sc cloud capped by inversion in order to study updrafts diverging under inversion.
64 References: Gerber, H., G. Frick, S.P. Malinowski, J-L. Brenguier and F. Burnet, 2005: Holes and Entrainment in Stratocumulus, J. Atmos. Sci., 62, ; doi: /JAS Gerber, H., G. Frick, S. P. Malinowski, W. Kumala, S. Krueger, 2010: POST - A New Look at Stratocumulus. 13th AMS Conference on Cloud Physics 28 June 2 July 2010, Portland, OR, Gerber, H., G. Frick, S. P. Malinowski, H. Jonsson, D. Khelif, S. Krueger, 2012: Entrainment in unbroken stratocumulus. J.Geophys.Res., submitted. Korczyk, P.M., S.P. Malinowski and T.A. Kowalewski, 2006: Mixing of cloud and clear air in centimeter scales observed in laboratory by means of particle image velocimetry, Atmos. Res., 82, ; doi: /j.atmosres Korczyk, P.M., T.A. Kowalewski and S.P. Malinowski, 2012: Turbulent mixing of clouds with the environment: Small scale two phase evaporating flow investigated in a laboratory by particle image velocimetry. Physica D, 243, , doi: /j.physd Kumala, W., K.E. Haman, M.K. Kopec, D. Khelif and S.P.. Malinowski, 2012: Modified Ultrafast Thermometer UFT-M and temperature measurements during Physics of Stratocumulus Top (POST). Atmos. Meas.Tech., submitted Kurowski M., S. P. Malinowski and W.W. Grabowski, 2009: Numerical investigation of entrainment and transport within stratocumulus-topped boundary layer. Q. J. Roy. Meteorol. Soc., 135, 77-92; doi: /qj.354 Malinowski, S.P., M. Andrejczuk, Wojciech W. Grabowski, P. Korczyk, Tomasz A. Kowalewski and P.K. Smolarkiewicz, 2008: Laboratory and modeling studies of cloud-clear air interfacial mixing: anisotropy of small-scale turbulence due to evaporative cooling, New Journal of Physics, 10, , doi: / /10/7/ Malinowski, S.P., A. Górska, T. A. Kowalewski, P. Korczyk, S. Błoński, and W. Kumala, 2010: Small-scale mixing at cloud top observed in a laboratory cloud chamber preliminary results. 13th AMS Conference on Cloud Physics 28 June 2 July 2010, Portland, OR, Malinowski S.P., K.E. Haman, M.K. Kopec, W. Kumala and H. Gerber, 2011: Small-scale turbulent mixing at stratocumulus top observed by means of high resolution airborne temperature and LWC measurements. J. Phys.: Conf. Ser. 318, , doi: / /318/7/ Malinowski, S.P., M. K. Kopec, W. Kumala, K. Nurowska, K. E. Haman, H. Gerber, P. Y. Chuang, J. Jonsson, D. Khelif, S. K. Krueger, 2012: Physics of Stratocumulus Top (POST): turbulent mixing across inversion. In preparation to Atmos. Chem.Phys. Stevens, B., Lenschow, D.H., Vali, G., Gerber, H., Bandy, A., Blomquist, B., Brenguier, J.-L., Bretherton, C. S., Burnet, F., Campos, T., Chai, S., Faloona, I., Friesen, D., Haimov, S., Laursen, K., Lilly, D. K., Loehrer, S. M., Malinowski, S.P., Morley, B., Petters, M. D., Rogers, D. C., Russell, L., Savic-Jovcic, V., Snider, J. R., Straub, D., Szumowski, Marcin J., Takagi, H., Thornton, D. C., Tschudi, M., Twohy, C., Wetzel, M., van Zanten, M. C., 2003: Dynamics and chemistry of marine stratocumulus Dycoms-II; Bull. Amer. Meteorol. Soc., 84, ; doi: /BAMS Stevens, B., 2005: Atmospheric moist convection. Annu. Rev. Earth Planet. Sci. 33, , doi: /annurev.earth
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