multiwavelength aerosol lidar and vertical-wind lidar observations during cops
DESCRIPTION
Multiwavelength aerosol lidar and vertical-wind lidar observations during COPS Dietrich Althausen, Detlef Müller, Ronny Engelmann, Matthias Tesche, Patric Seifert, Julia Fruntke, Christina Herold, Luise Hentschel, (Albert Ansmann) - PowerPoint PPT PresentationTRANSCRIPT
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Multiwavelength aerosol lidar and vertical-wind lidar observations during COPS
Dietrich Althausen, Detlef Müller, Ronny Engelmann, Matthias Tesche, Patric Seifert, Julia Fruntke, Christina Herold, Luise Hentschel, (Albert Ansmann)
Leibniz Institute for Tropospheric Research, Leipzig, Germany
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Aerosol and vertical–velocity profiling and cloud glaciation observations during COPSApplicant: Albert Ansmann
Contribution to ACM and SPP 1167 (2 year period)
• Aerosol characterization • Obtaining geometrical, optical, and microphysical properties of aerosols and clouds Derivation of microphysical properties such as aerosol number
concentration
• Vertical Wind in the upper PBL (at cloud base)
• Studies of heterogeneous ice formation • Investigating the effect of aerosol particles and meteorological conditions on cloud glaciation Many Saharan dust cases and forest fire cases observed
DFG
pro
posa
l
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3 months of data, 400-500 hours
Backscatter Extinction lidar-Ratio Temperature Humditiy profiling Apparatus
Wind Lidar
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0
1000
2000
3000
4000
0 2 4 6 8 10
355 nm 400 nm 532 nm 710 nm 800 nm 1064 nm
BACKSC. COEF. (Mm-1 sr-1)
HEI
GH
T (m
)
0 200 400 600 800
25 MARCH 1999: Optical Parameters mean of 3600 s, 1330 - 1500 UTC
EXTINCTION COEF. (Mm-1)
355 nm 532 nm
INDOEX,Maldives1999-2000
SAMUM I, Morocco, May-Jun 2006COPS, Black F., Jun-Aug 2007SAMUM II, Cape Verde, Jan/Feb+May/Jun 2008
6 x beta 2 x sigma
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Inversion algorithm
Input: – 6 backscatter coefficients – 2 extinction coefficients
Output:– volume size distribution– effective radius– total volume concentration– total surface-area concentration– mean complex refractive index– single-scattering albedo
COPS: β(532nm) ~ n (particle number conc.)
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VALIDATION OF INVERSION RESULTS WITH AIRBORNE IN-SITU MEASUREMENTS
LACE 98: Biomass Burning From NW CanadaMeasurement : 9 August 1998
3500-4000 m 3400-3900 m inversion in-situ
IfT IMP (r > 50 nm)
eff. radius ( m )
v ( m /cm ) 3 3
s ( m /cm ) 2 3
n (1/cm ) 3
real part
imag.
single-scat.albedo (532nm)
part
0.27
13
142
295
1 .62
0.047
0.81
0.04
2
7
64
0.08
0.013
0.03
0.24
11
136
506
1.66
0 .79
0 .053
0 .01
1
5
131
0 .02
0 .01
0.004
0.25 0 .07
8 5
95 55
271 74
(1.56)
(0 .07)
0.79 0.02
9 August 1998, 2200-2400 U TC
COPS: we may only get the order of magnitude of the particle number conc. (100 cm-3, 1000 cm-3, 10000 cm-3)
DLR Falcon
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Aerosol type: finger prints
Aerosol type Lidar ratio (sr) Depol. ratio (%) Maritime S355=S532 (low) <5% (low)
Urban S355>=S532 (high) <5% (low) Forest fire smoke S355<S532 (high) <10-15% (med) Desert Dust S355>=S532 (high) 25-35% (high)
355 nm versus 532 nm
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COPS: Some measurement examples
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PBL+CU
Vertical wind
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P B L d e v e l o p m e n t
in terms of vertical wind
profile of horiz. wind speed and direction
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Deep cumulus tower
Spectacular event
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Heterogenous ice formation
melting layer
uncalibrated depol. ratio (710nm)
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AC
ICE
terminal velocities
CI
Bertha + Wili
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Topic 1 Topic 2PBL heterog. ice form.
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Influence of Saharan dust and biomass burning smoke on cloud glaciationover the northern tropical Atlantic Ocean (Cape Verde) during SAMUM II
Published February 2008
SAMUM II: 15 Jan – 14 Feb 2008, Praia, Cabo Verde (15oN, 23.5oW)
Our work on heterogenous ice formation
…upcoming
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Next future (beginning in March 2008):
Diploma student working on WiLi data (wind fields)
Diploma student working on Raman lidar data(water vapor and temperature)
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BERTHA, Heselbach, 532nm backscatter signal
PBL, sunny day dust
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BERTHA, water vapor Raman lidar, Heselbach
SONDE
LIDAR, 20 min, 60m smoothing LIDAR, 1 min, 240 m smoothing
LIDAR
LIDAR
532 nm backscatter signal
g/kg
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COPS:
Bertha(Raman lidar)
water vapor
nighttime,
1 min res.,60 m height res.