Download
slide1 n.
Skip this Video
Loading SlideShow in 5 Seconds..
Shallow Moist Convection PowerPoint Presentation
Download Presentation
Shallow Moist Convection

Shallow Moist Convection

206 Views Download Presentation
Download Presentation

Shallow Moist Convection

- - - - - - - - - - - - - - - - - - - - - - - - - - - E N D - - - - - - - - - - - - - - - - - - - - - - - - - - -
Presentation Transcript

  1. Shallow Moist Convection • Basic Moist Thermodynamics • Remarkable Features of Moist Convection • Shallow Cumulus • (Stratocumulus) Courtesy: Dave Stevens

  2. Basic Moist Thermodynamics

  3. Large scale advection Large scale subsidence Vertical turbulent transport Net Condensation Rate Grid Averaged Budget Equations

  4. Schematically: • Objectives • Understand Moist Convection…. • Design Models….. • But ultimately design parameterizations of:

  5. Moist Conserved Variables qv:Specific Humidity (g/kg) Condensation occurs if qvexceeds the saturation value qs(T,p) Usually through rising motion ql:Liquid Water (g/kg) qt = qv + ql :Total water specific humidity (Conserved for phase changes!!)

  6. Used Temperature Variables • Potential Temperature • Conserved for dry adiabatic changes • Liquid Water Potential Temperature • Conserved for moist adiabatic changes Energy equivalent: • Liquid Water Static Energy • Virtual Potential Temperature • Directly proportional to the density • Measure for buoyancy

  7. Grid averaged equations for moist conserved variables: Parametrization issue reduced to a convective mixing problem!

  8. A Unique Feature of Moist Convection

  9. z z T(K) A saturated ascending parcel will conserve hl : Moist Adiabatic Lapse Rate Leads to a moist adiabatic lapse rate : Remarks: • Example: T=290K,p=1000mb • Temperature decrease less than for dry parcels • Difference between and becomes progressively smaller for lower temperatures Q (K)

  10. sounding z zo Tv(K) Absolute Instability • Lift a (un)saturated parcel from a sounding at z0 by dz • Check on buoyancy with respect to a mean profile: Example 1: Unstable for saturated and unsaturated parcels Absolute Unstable

  11. sounding zo Tv(K) Absolute Stability • Lift a (un)saturated parcel from a sounding at z0 by dz • Check on buoyancy with respect to the sounding: Example 2: Stable for saturated and unsaturated parcels Absolute stable

  12. sounding z zo Tv(K) Conditional Instability • Lift a (un)saturated parcel from a sounding at z0 by dz • Check on buoyancy with respect to the sounding: Example 2: Stable for unsaturated parcels Unstable for saturated parcels Conditionally Unstable!!!

  13. Mean profile “Level of zero kinetic energy” Inversion Level of neutral buoyancy (LNB) conditionally unstable layer height Level of free convection (LFC) Lifting condensation level (LCL) well mixed layer The Miraculous Consequences of conditional Instability or: the “Cinderalla Effect” (Bjorn Stevens)

  14. CIN Non-local integrated stability funcions: CAPE, CIN Define a work function: LNB CAPE Positive part: CAPE = Convective Available Potential Energy. z1 Negative part: z0 CIN = Convection Inhibition CIN allows the accumulation of CAPE

  15. CAPE and CIN: An Analogue with Chemistry • 1) Large Scale Forcing: • Horizontal Advection • Vertical Advection (subs) • Radiation Activation (triggering) LS-forcing Surf Flux CIN 2) Large Scale Forcing: slowly builds up CAPE CAPE Free Energy • 3) CAPE • Consumed by moist convection • Transformed in Kinetic Energy • Heating due to latent heat release (as measured by the precipitation) • Fast Process!! RAD LS-forcing Mixed Layer LFC LNB Parcel Height Free after Brian Mapes

  16. Quasi-Equilibrium LS-Forcing that slowly builds up slowly The convective process that stabilizes environment Quasi-equilibrium: near-balance is maintained even when F is varying with time, i.e. cloud ensemble follows the Forcing. Forfilled if : tadj << tF Used convection closure (explicit or implicit) JMb ~ CAPE/ tadj tadj : hours to a day. wu au Mb=au wur :Amount of convective vertical motion at cloud base (in an ensemble sense)

  17. Quasi-Equilibrium: An Earthly Analogue Free after Dave Randall: • Think of CAPE as the length of the grass • Forcing as an irrigation system • Convective clouds as sheep • Quasi-equilibrium: Sheep eat grass no matter how quickly it grows, so the grass is allways short. • Precipitation………..

  18. Typical Tradewind Cumulus Strong horizontal variability !

  19. Horizontal Variability and Correlation Mean profile height

  20. Schematic picture of cumulus moist convection: • Cumulus convection: • more intermittant • more organized • than • Dry Convection.

  21. a a a Mass flux concept: tomorrow more!! wc

  22. Shallow Cumulus Convection Photo courtesy Bjorn Stevens

  23. Observational Characteristics : Trade wind shallow Cu non well-mixed cloud layer Surface heat-flux: ~10W/m^2 Surface Latent heat flux : 150~200W/m^2

  24. adiabat Mixing between Clouds and Environment (SCMS Florida 1995) Due to entraiment! Data provided by: S. Rodts, Delft University, thesis available from:http://www.phys.uu.nl/~www.imau/ShalCumDyn/Rodts.html

  25. adiabat Liquid water potential temperature Total water (ql+qv) • Entrainment Influences: • Vertical transport • Cloud top height

  26. The simplest Cloud Mixing Model

  27. hc 4.1 lateral mixing bulkmodel Fractional entrainment rate

  28. Diagnose through conditional sampling: Typical Tradewind Cumulus Case (BOMEX) Data from LES: Pseudo Observations

  29. Trade wind cumulus: BOMEX LES Observations Cumulus over Florida: SCMS Siebesma JAS 2003

  30. Adopted in cloud parameterizations: Lateral mixing Horizontal or vertical mixing? Cloud-top mixing Observations (e.g. Jensen 1985) However: cloud top mixing needs substantial adiabatic cores within the clouds.

  31. adiabat (SCMS Florida 1995) No substantial adiabatic cores (>100m) found during SCMS except near cloud base. (Gerber) Does not completely justify the entraining plume model but……… It does disqualify a substantial number of other cloud mixing models.

  32. Cloudtop Cloudtop entrainment Entrance level Lateral entrainment Inflow from subcloud Measurement level Cloudbase Cloudtop Backtracing particles in LES: where does the air in the cloud come from? Courtesy Thijs Heus

  33. Height vs. Source level Virtually all cloudy air comes from below the observational level!!

  34. 5.Dynamics, Fluxes and other stuff that can’t be measured accurately

  35. No observations of turbulent fluxes. • Use Large Eddy Simulation (LES) • based on observations BOMEX ship array (1969) observed observed To be modeled by LES

  36. 10 different LES models • Initial profiles • Large scale forcings prescribed • 6 hours of simulation Is LES capable of reproducing the steady state?

  37. Large Scale Forcings

  38. Mean profiles after 6 hours • Use the last 4 simulation hours for analysis of …….

  39. To do analyses of the dynamics using the LES results

  40. How is the steady state achieved? forcing forcing rad turb turb c-e c-e

  41. How is the steady state achieved?

  42. Cloud cover

  43. Turbulent Fluxes of and Subcloud layer looks similar than dry PBL!!

  44. Turbulent Fluxes of the conserved variables qt and ql Cloud layer looks like a enormous entrainment layer!!

  45. Vertical Velocity in the cloud and the total vertical velocity variance Dry PBL velocity variance profile

  46. Conditional Sampling of: • Total water qt • Liquid water potential temperature ql

  47. Virtual potential temperature:qv

  48. Cloud Liquid water

  49. Bjorn Stevens accepted for JAS Non-precipating cumulus Shallow Cumulus Growth, (an idealized view) Extension from the dry PBL growth, but now….. Adding Moisture dry cloudy

  50. Temporal Evolution