Presentation is loading. Please wait.

Presentation is loading. Please wait.

1 Atmospheric profiling to better understand fog and low level cloud life cycle ARM/EU workshop on algorithms, 13-14 May 2013 J. Delanoe (LATMOS), JC.

Published byArchibald Lane Modified over 8 years ago

Similar presentations

Presentation on theme: "1 Atmospheric profiling to better understand fog and low level cloud life cycle ARM/EU workshop on algorithms, 13-14 May 2013 J. Delanoe (LATMOS), JC."— Presentation transcript:

1 1 Atmospheric profiling to better understand fog and low level cloud life cycle ARM/EU workshop on algorithms, 13-14 May 2013 J. Delanoe (LATMOS), JC. Dupont (IPSL), M. Haeffelin (IPSL)

2 22 Aerosol profilingT/RH profilingWater profilingWind profiling Backscatter signal CL31 ceilometer ALS450 lidar Aerosol optical properties DF20, DF20 + diffusometer Nephelometer Aerosol size distribution SMPS, CPC, Welas Brightness temperature Hatpro MWR T/RH in-situ measurement Tethered balloon (0-300m) Mast sensors (0-30m) Radiosounding (0 -25km) Reflectivity & Dop. velocity BASTA cloud radar Dropplet size distribution FM100 Liquid water content PVM 3D wind speed Sodar PA2, Doppler lidar WLS7 & WLS70, UHF radar 3D wind speed Cup anemometer Sonic anemometer Radiosounding + Extinction closure combining size distribution and visibility + CL31 backscattering versus visibility and LOAC on tethered balloon + Evaluation of MWR retrieval with tethered balloon + Analysis of T/RH profile variability for F and QF + Estimation of LW vertical profile combining in-situ and BASTA data + Comparisons between FM100 and PVM + Evaluation of sodar, WLS and UHF radar versus in-situ sensors + Effect of mast on in-situ measurement JC Dupont (IPSL), J. Delanoe (LATMOS) JC. Dupont(IPSL), L. Musson-Genon (CEREA) E. Dupont (CEREA) JC Dupont (IPSL), D. Legain (CNRM) S. Pal (LMD), T. Elias (HYGEOS), M. Haeffelin (IPSL), JB. Renard (LPC2E) Atmospheric profiling to better understand fog and low level cloud life cycle Red : Remote sensing Blue : in-situ RETRIEVAL

3 3 CASE 1 Stratus Lowering without fog. Why ? Ceilometer Cloud radar BASTA doppler velocity Cloud radar BASTA reflectivity 1st case study: 5 January 2013 High pressure system (1033 hPa), very low stratus cloud Advection: 10m/s at 400m Case of stratus lowering due to advection of moisture + lifting due to precipitation

4 4 Stratus appears for Z >-35dBZ (after 7UTC) Drizzle below the cloud base Cloud top is constant CL31: backscatter signal  Wet air advection after 5 UTC (9 to 17 mm) Leading to stratus lowering with bigger LWP Downward flux + Visibilimeter : surface visibility BASTA : cloud reflectivity Stratus cloud lowering, 400m to 70m between 6 and 14 UTC Sonic anemometer : vertical wind speed at 10m HATPRO MWR : Integrated water vapor HATPRO MWR : Liquid Water Path CASE 1 The stratus lowering phase…1/2

5 5 SODAR: North-West advection W: Heating by the surface, cooling by the top CT 2 : high level of turbulence at cloud top when stratus lowering period SODAR CASE 1 The stratus lowering phase…2/2

6 6 Z =0 dBZ at 14 UTC Cloud top is max (670m) at 14 UTC Cloud base is min (60m) at 14 UTC Visibilimeter : surface visibility BASTA : cloud reflectivity MAST : T  until and after 11UTC T  and RH reaches saturation at 14 at 30m CASE 1 The developed stratus phase… HATPRO MWR : Liquid Water Path Hotplate TPS3100 : low precipitation level Precipitation rate is 0.005mm/hr after 14UTC Linked with max value of Z Drizzle droplet fall on the ground Fog-Monitor 100 : Droplet number and size distribution Very low droplet concentration, <6 particles / cm 3 Saturation of LWP around 300g/m² Biggest droplets fall on the ground Surface Total column

7 7 Cloud base lifting at 17 UTC  Z after 17 UTC and  of cloud top Visibilimeter : surface visibility BASTA : cloud reflectivity Sodar : wind speed (clear air) CASE 1 The stratus lifting phase… HATPRO MWR : Liquid Water Path Cup anemometer : wind speed at 10m No dynamics at 19UTC, WS~m/s Fog-Monitor 100 : Droplet number and size distribution No drizzle after 18 UTC No droplet Downward flux stops after 16UTC, no wet air entrainment and so LWP  Surface Total column  wind speed along the vertical after 17 UTC Low wind shear Low vertical mixing

8 8 Vertical profile of particle size distribution between 0.5 and 150µm. With LOAC (Light Optical Aerosol Counter) Developped in LPC2E French Lab. at 08 UTC. Z ~ -35dBZ Small Aerosols Drop Droplet Cloud base Size Altitude (m) Concentration (#/cm 3 ) CASE 1 Vertical profiles of ASD and DSD

9 9 Aérosols hydratés …. activation Peak of droplet size Ceilometer BASTA cloud radar doppler velocity CASE 2 A radiative fog event BASTA cloud radar doppler reflectivity Peak of droplet vertical velocity

10 10 CASE 2 Liquid water closure ? 1 2 3 123 Liquid water path Surface liquid water content Surface droplet concentration Basta reflectivity 3 1 2 3 3

11 11 Strong wind shear : 12 m/s at 350m agl Updraft air due to solar heating :+0.5m/s Important turbulent flux at fog top SODAR CASE 2 Role of wind shear …

12 12 Updraft Droplet vertical velocity around -0.4m/s LIDAR DOPPLER Clear air Cloudy air CASE 2 Role of droplet vertical velocity

Download ppt "1 Atmospheric profiling to better understand fog and low level cloud life cycle ARM/EU workshop on algorithms, 13-14 May 2013 J. Delanoe (LATMOS), JC."

Similar presentations

Ewan OConnor, Robin Hogan, Anthony Illingworth Drizzle comparisons.

Ewan OConnor, Robin Hogan, Anthony Illingworth Drizzle comparisons.
Radar/lidar observations of boundary layer clouds

Radar/lidar observations of boundary layer clouds
Integrated Profiling at the AMF

Integrated Profiling at the AMF
Matthew Shupe Ola Persson Paul Johnston Cassie Wheeler Michael Tjernstrom Surface-Based Remote-Sensing of Clouds during ASCOS Univ of Colorado, NOAA and.

Matthew Shupe Ola Persson Paul Johnston Cassie Wheeler Michael Tjernstrom Surface-Based Remote-Sensing of Clouds during ASCOS Univ of Colorado, NOAA and.
CEREA – Group « Meteorological Measurements » 15 September 2006 1 METEOROLOGICAL MEASUREMENTS IN THE ATMOSPHERIC BOUNDARY LAYER E. Dupont – D. Demengel.

CEREA – Group « Meteorological Measurements » 15 September METEOROLOGICAL MEASUREMENTS IN THE ATMOSPHERIC BOUNDARY LAYER E. Dupont – D. Demengel.
Atmospheric Analysis Lecture 3.

Atmospheric Analysis Lecture 3.
Radiative Properties of Clouds SOEE3410 Ken Carslaw Lecture 3 of a series of 5 on clouds and climate Properties and distribution of clouds Cloud microphysics.

Radiative Properties of Clouds SOEE3410 Ken Carslaw Lecture 3 of a series of 5 on clouds and climate Properties and distribution of clouds Cloud microphysics.
Atmospheric structure from lidar and radar Jens Bösenberg 1.Motivation 2.Layer structure 3.Water vapour profiling 4.Turbulence structure 5.Cloud profiling.

Atmospheric structure from lidar and radar Jens Bösenberg 1.Motivation 2.Layer structure 3.Water vapour profiling 4.Turbulence structure 5.Cloud profiling.
Remote sensing of Stratocumulus using radar/lidar synergy Ewan O’Connor, Anthony Illingworth & Robin Hogan University of Reading.

Remote sensing of Stratocumulus using radar/lidar synergy Ewan O’Connor, Anthony Illingworth & Robin Hogan University of Reading.
METR215- Cloud Droplet Formation

METR215- Cloud Droplet Formation
Radiative Properties of Clouds ENVI3410 : Lecture 9 Ken Carslaw Lecture 3 of a series of 5 on clouds and climate Properties and distribution of clouds.

Radiative Properties of Clouds ENVI3410 : Lecture 9 Ken Carslaw Lecture 3 of a series of 5 on clouds and climate Properties and distribution of clouds.
TReSS (Transportable Remote Sensing Station) in Tamanrasset Overview of TReSS Status of implementation on April 1 st 2006 Operations in the framework of.

TReSS (Transportable Remote Sensing Station) in Tamanrasset Overview of TReSS Status of implementation on April 1 st 2006 Operations in the framework of.
Balloon-Borne Sounding System (BBSS) Used for atmospheric profiling Measures P, T, RH, wind speed and direction Uncertainties arise from incorrect surface.

Balloon-Borne Sounding System (BBSS) Used for atmospheric profiling Measures P, T, RH, wind speed and direction Uncertainties arise from incorrect surface.
Warm Up 3/18/08 The wet adiabatic rate of cooling is less than the dry rate because ____. a. of the dew point b. of the release of latent heat c. wet air.

Warm Up 3/18/08 The wet adiabatic rate of cooling is less than the dry rate because ____. a. of the dew point b. of the release of latent heat c. wet air.
Dew, Frost and Fog. RECAP Hydrological cycle: transport of water and energy. Humidity: absolute humidity, specific humidity, water mixing ratio, relative.

Dew, Frost and Fog. RECAP Hydrological cycle: transport of water and energy. Humidity: absolute humidity, specific humidity, water mixing ratio, relative.
Remote-sensing of the environment (RSE) ATMOS Analysis of the Composition of Clouds with Extended Polarization Techniques L. Pfitzenmaier, H. Russchenbergs.

Remote-sensing of the environment (RSE) ATMOS Analysis of the Composition of Clouds with Extended Polarization Techniques L. Pfitzenmaier, H. Russchenbergs.
Precipitation.

Precipitation.
Chapter 4 Moisture in the Atmosphere Chapter 4 Moisture in the Atmosphere Water on the Earth has three common states solid, liquid, and vapor Each with.

Chapter 4 Moisture in the Atmosphere Chapter 4 Moisture in the Atmosphere Water on the Earth has three common states solid, liquid, and vapor Each with.
Ship-based measurements of cloud microphysics and PBL properties in precipitating trade cumulus clouds during RICO Allen White and Jeff Hare, University.

Ship-based measurements of cloud microphysics and PBL properties in precipitating trade cumulus clouds during RICO Allen White and Jeff Hare, University.
Characterization of Arctic Mixed-Phase Cloudy Boundary Layers with the Adiabatic Assumption Paquita Zuidema*, Janet Intrieri, Sergey Matrosov, Matthew.

Characterization of Arctic Mixed-Phase Cloudy Boundary Layers with the Adiabatic Assumption Paquita Zuidema*, Janet Intrieri, Sergey Matrosov, Matthew.

Similar presentations

Ads by Google