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1/29 Parametrization of the planetary boundary layer (PBL) Irina Sandu & Anton Beljaars Introduction Irina Surface layer and surface fluxes Anton Outer.

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Presentation on theme: "1/29 Parametrization of the planetary boundary layer (PBL) Irina Sandu & Anton Beljaars Introduction Irina Surface layer and surface fluxes Anton Outer."— Presentation transcript:

1 1/29 Parametrization of the planetary boundary layer (PBL) Irina Sandu & Anton Beljaars Introduction Irina Surface layer and surface fluxes Anton Outer layerIrina Stratocumulus Irina PBL evaluation Maike ExercisesIrina & Maike

2 2/29 Why studying the Planetary Boundary Layer ? Natural environment for human activities Understanding and predicting its structure Agriculture, aeronautics, telecommunications, Earth energetic budget Weather forecast, pollutants dispersion, climate prediction

3 3/29 Outline Definition Turbulence Stability Classification Clear convective boundary layers Cloudy boundary layers (stratocumulus and cumulus) Summary

4 4/29 PBL: Definitions The layer where the flow is turbulent. The fluxes of momentum, heat or matter are carried by turbulent motions on a scale of the order of the depth of the boundary layer or less. The surface effects (friction, cooling, heating or moistening) are felt on times scales < 1 day. Free troposphere 50 m km Mixed layer surface layer Composition atmospheric gases (N 2, O 2, water vapor, …) aerosol particles clouds (condensed water) qvqv The PBL is the layer close to the surface within which vertical transports by turbulence play dominant roles in the momentum, heat and moisture budgets.

5 5/29 PBL: Turbulence Characteristics of the flow Rapid variation in time Irregularity Randomness Properties Diffusive Dissipative Irregular (butterfly effect) Origin: Hydrodynamic instability (wind shear) Reynolds number Thermal instability Rayleigh number Chaotic flow U

6 6/29 heat (first principle of thermodynamics) PBL: Governing equations for the mean state Reynolds averaging gas law (equation of state) momentum (Navier Stokes) total water continuity eq. (conservation of mass) Simplifications Boussinesq approximation (density fluctuations non-negligible only in buoyancy terms) Hydrostatic approximation (balance of pressure gradient and gravity forces) Incompressibility approximation (changes in density are negligible) Averaging (overbar) is over grid box, i.e. sub-grid turbulent motion is averaged out.

7 7/29 PBL: Governing equations for the mean state Reynolds averaging gas law virtual temperature

8 8/29 PBL: Governing equations for the mean state Reynolds averaging gas law virtual temperature mean advection gravity momentum Coriolis Pressure gradient Viscous stress Turbulent transport 2 nd order Need to be parameterized !

9 9/29 PBL: Governing equations for the mean state Reynolds averaging gas law virtual temperature mean advection gravity momentum Coriolis Pressure gradient Viscous stress Turbulent transport continuity eq. 2 nd order

10 10/29 radiation turbulent transport mean advection heat PBL: Governing equations for the mean state Reynolds averaging gas law virtual temperature Latent heat release mean advection gravity momentum Coriolis Pressure gradient Viscous stress Turbulent transport continuity eq. 2 nd order

11 11/29 radiation turbulent transport mean advection heat PBL: Governing equations for the mean state precipitation turbulent transport mean advection Total water Reynolds averaging gas law virtual temperature Latent heat release mean advection gravity momentum Coriolis Pressure gradient Viscous stress Turbulent transport precipitation turbulent transport mean advection total water continuity eq. 2 nd order

12 12/29 TKE: a measure of the intensity of turbulent mixing turbulent transport pressure transport buoyancy production mechanical shear dissipation PBL: Turbulent kinetic energy equation An example : v 0, w > 0 w v > 0 source v 0 or v > 0, w < 0 w v < 0 sink v q v q l virtual potential temperature

13 13/29 PBL: Stability (I) Traditionally stability is defined using the temperature gradient v gradient (local definition): stable layer unstable layer neutral layer How to determine the stability of the PBL taken as a whole ? In a mixed layer the gradient of temperature is practically zero Either v or w v profiles are needed to determine the PBL stability state stableunstable zz v v

14 14/29 PBL: Stability (II) Stable Unstable (Stull, 1988)

15 15/29 PBL: Other ways to determine stability (III) Bouyancy flux at the surface: unstable PBL (convective) stable PBL Or dynamic production of TKE integrated over the PBL depth stronger than thermal production neutral PBL Monin-Obukhov length: m L –100m unstable PBL -100m < L < 0 strongly unstable PBL 0 < L < 10 strongly stable PBL 10m L 10 5 m stable PBL |L| > 10 5 m neutral PBL Richardson flux number Rf < 0 statically unstable flow Rf > 0 statically stable flow Rf < 1 dynamically unstable flow Rf > 1 dynamically stable flow

16 16/29 PBL: Classification and scaling Neutral PBL : turbulence scale l ~ 0.07 H, H being the PBL depth Quasi-isotropic turbulence Scaling - adimensional parameters : z 0, H, u * Stable PBL: l << H (stability embeds turbulent motion) Turbulence is local (no influence from surface), stronger on horizontal Scaling :,, H Unstable (convective) PBL l ~ H (large eddies) Turbulence associated mostly to thermal production Turbulence is non-homogeneous and asymmetric (top-down, bottom-up) Scaling: H,

17 17/29 PBL: Diurnal variation Clear convective PBL Cloudy convective PBL

18 18/29 q l = q t -q sat q sat q sat Cloud base qtqt l qvqv l = PBL: State variables Clear PBLCloudy PBL T p p 0 R d /c p Potential temperature l - L v c p q l Specific humidity Liquid water potential temperature Total water content Evaporation temperature Conserved variables

19 19/29 Clear Convective PBL qtqt q sat v Stephan de Roode, Ph.D thesis Free atmosphere Inversion layer mixed layer surface layer

20 20/29 Clear Convective PBL Buoyantly-driven from surface 0.7 H inversion level of neutral buoyancy Main source of TKE production Turbulent transport and pressure term turbulent fluxes : a function of convective scaling variables: PBL height: Entrainment rate: (a possible parameterization ) Fluxes at PBL top: Key parameters:

21 21/29 Clouds effects on climate warming Greenhouse effect Infrared radiation Solar radiation Umbrella effect cooling Boundary layer clouds

22 22/29 Cloudy marine boundary layers Stratocumulus capped boundary layers Fair weather cumuli Trade wind cumuli

23 23/29 Cloudy boundary layers Stratocumulus topped PBL Cumulus PBL qtqt q sat v qtqt v Stephan de Roode, Ph.D thesis Free atmosphere Inversion layer mixed layer surface layer Free atmosphere Inversion layer Conditionally unstable cloud layer surface layer Subcloud mixed Dry-adiabatic lapse rate wet-adiabatic lapse rate

24 24/29 Cloudy boundary layers Stratocumulus topped PBL Cumulus PBL qtqt q sat v qtqt v Stephan de Roode, Ph.D thesis Free atmosphere Inversion layer mixed layer surface layer Free atmosphere Inversion layer Conditionally unstable cloud layer surface layer Subcloud mixed Dry-adiabatic lapse rate wet-adiabatic lapse rate

25 25/29 Stratocumulus topped boundary layer Complicated turbulence structure Cloud top entrainment condensation Long-wave cooling Long-wave warming Buoyantly driven by radiative cooling at cloud top Surface latent and heat flux play an important role Cloud top entrainment an order of magnitude stronger than in clear PBL Solar radiation transfer essential for the cloud evolution Key parameters:

26 26/29 Longwave radiative transfer in stratocumulus cooling warming At cloud top

27 27/29 Cumulus capped boundary layers Buoyancy is the main mechanism that forces cloud to rise Active cloud CAPE

28 28/29 Cumulus capped boundary layers Buoyancy is the main mechanism that forces cloud to rise Represented by mass flux convective schemes Decomposition: cloud + environment Lateral entrainment/detrainment rates prescribed Key parameters:

29 29/29 PBL: Summary Characteristics : several thousands of meters – 2-3 km above the surface turbulence, mixed layer convection Reynolds framework Classification: neutral (extremely rare) stable (nocturnal) convective (mostly diurnal) Clear convective Cloudy (stratocumulus or cumulus) Importance of boundary layer clouds (Earth radiative budget) Small liquid water contents, difficult to measure

30 30/29 Bibliography Deardorff, J.W. (1973) Three-dimensional numerical modeling of the planetary boundary layer, In Workshop on Micrometeorology, D.A. Haugen (Ed.), American Meteorological Society, Boston, P. Bougeault, V. Masson, Processus dynamiques aux interfaces sol- atmosphere et ocean-atmosphere, cours ENM Nieuwstad, F.T.M., Atmospheric boundary-layer processes and influence of inhomogeneos terrain. In Diffusion and transport of pollutants in atmospheric mesoscale flow fields (ed. by Gyr, A. and F.S. Rys), Kluwer Academic Publishers, Dordrecht, The Netherlands, , Stull, R. B. (1988) An introduction to boundary layer meteorology, Kluwer Academic Publisher, Dordrecht, The Netherlands. S. de Roode (1999), Cloudy Boundary Layers: Observations and Mass-Flux Parameterizations, Ph.D. Thesis Wyngaard, J.C. (1992) Atmospheric turbulence, Annu. Rev. Fluid Mech. 24,


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