atmospheric radiation gcc summer school montreal - august 7, 2003 glen lesins department of physics...
TRANSCRIPT
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Atmospheric Radiation
GCC Summer SchoolMontreal - August 7, 2003
Glen LesinsDepartment of Physics and Atmospheric Science
Dalhousie UniversityHalifax
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Outline
Introductory concepts Radiation and Climate Radiative Transfer Theory Remote Sensing
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Credits
K.N. Liou, An Introduction to Atmospheric Radiation, 2nd Ed., 2002
Web Lecture Notes by Prof. Irina Sokolik, http://irina.colorado.edu/teaching.htm
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Kiehl and Trenberth (1997); IPCC (2001)
Global Annual Energy Balance
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What is the Solar Constant?
• 1366 W m-2
• How constant?– Earth’s orbit and tilt (annual)– Sunspot cycle (11 years)– Longer time variations
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Solar Irradiance Variation from ACRIM
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http://science.nasa.gov/headlines/images/sunbathing/sunspectrum.htm
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Solar vs. Terrestrial Radiation
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Absorption of Radiation by Gases
1. Ionization/Dissociation - UV
2. Electronic Transition - UV
3. Vibrational/Rotational Transition -Visible/IR
4. Pure Rotational - IR
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Transmission through the Atmosphere
Solar Terrestrial
IR Window
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Radiative Interactions - Dipole Transitions
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Vibrational Modes
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Electrostatic potential
map shows both end
oxygens are equivalent
with respect to negative
charge. Middle atom
is positive.
Ozone (O3)
OO OO
••••OO••••
••••••••••••••••––++
OO OOOO••••
••••••••••••••••
–– ++
••••
www.facstaff.oglethorpe.edu/mwolf/PowerPoint/ CareyOrgPP/sections1st/Chapter%201bx.ppt
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Absorption by Gases
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SolarIrradiance
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Scattering of Radiation
Particle Size
WavelengthSize Parameter,
r
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http://hyperphysics.phy-astr.gsu.edu/hbase/atmos/blusky.html#c2
Rayleigh Scattering
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Mie Theory for mr=1.5
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NormalizedPhaseFunctionsFromMie Theory
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Kiehl and Trenberth (1997); IPCC (2001)
Global Annual Energy Balance
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Zonal Average Irradiance
Solar
Terrestrial
Net
MeridionalTransport
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Cloud Radiative Forcing from ERBE
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Radiative Equilibrium & Role of Convection
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Solar Heating Rates from Model
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Zonal Annual Average from Satellite
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Results from SOCRATES (2-D Radiative-Chemical)
http://acd.ucar.edu/models/SOCRATES/socrates/socrates1.html
http://acd.ucar.edu/models/SOCRATES/socrates/socrates1.html
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Annual Mean Net Radiation Flux from SurfaceBased Measurements
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Terrestrial IR Spectra
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Modelled IR Fluxes
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High
Level of Scientific Understanding
1
2
3
0
-1
-2
Medium Medium Low Very
Low
Very
Low
Very
Low
Very
Low
Very
Low
Very
Low
Very
Low
Very
Low
Halocarbons
N2
O
CH4
CO2
Aerosols
Aviation-inducedTropospheric
ozone
Stratospheric
ozone
Black
carbon from
fossil fuel
burning
Organic
carbon
from
fossil
fuel
burning
Aerosol
indirect
effect
Biomass
burning
Land-use
(albedo)
only
Mineral
dust
Sulphate
Contrails Cirrus
Solar
Global mean radiative forcing of the climate
system for the year 2000, relative to 1750R
adia
tive
forc
ing
(W
m-2)
Wa
rmin
gC
oo
lin
g
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Kiehl and Trenberth (1997); IPCC (2001)
Global Annual Energy Balance
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Radiative Transfer Equation
Source FunctionOptical Depth
Cosine of solar zenith angle
Radiance
Azimuthal Angle
Beer’s Law
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Plane Parallel Radiances
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Solution to the Radiative Transfer Equation
UpwardRadiance
DownwardRadiance
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SUN
Source Function Multiple Scattering Term
Single Scattering Term
Single & Multiple Scattering Source
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Surface Reflectance
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Bi-directional ReflectanceDistribution Function (BRDF)
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Surface Albedo
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Remote Sensing of Clouds
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Effect of Clouds from Radiative-ConvectiveModel
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Solar Albedo of Clouds - Theory
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Indirect Aerosol Effect - ShiptracksIndirect Aerosol Effect - ShiptracksL1B true color RGB composite (25 April 2001)L1B true color RGB composite (25 April 2001)
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60
0
30
15
45
re (µ
m)
Effective radius retrieval(using 2.1 µm band, all phases)
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Shiptracks from MODISIndirect Aerosol Effect
July 1, 2003
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Kiehl and Trenberth (1997); IPCC (2001)
Global Annual Energy Balance
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IR Brightness Temperature from ER-2 (Clear)
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BrightnessTemperaturesFrom ER-2(Various Clouds)
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Polarization of Sunlight Reflected by Venus
Points=Obs
Lines=Theory
Hansen and Hovenier, 1974
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POLDER – Polarization for Ice Habits
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Ice Crystal Phase Functions
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http://isccp.giss.nasa.gov
Cloud Fraction from Satellites
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TERRA - Launched Dec. 18, 1999(MODIS, ASTER, MISR, CERES, MOPITT)
• MODIS– 1-2 day global coverage in 36 wavelengths from 250 m to
1 km resolution• MISR
– Stereo images at 9 look angles• ASTER
– Hi-resolution, multi-spectral images from 15 m to 90 m resolution, plus stereo
• MOPITT
– Global measures of CH4 & CO
• CERES– Measures Earth’s shortwave, longwave, – net radiant energy budget
http://modis-atmos.gsfc.nasa.gov/reference.html
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MODIS Atmospheric Products
• Pixel-level (level-2) products– Cloud mask for distinguishing clear sky from clouds– Cloud radiative and microphysical properties
• Cloud top pressure, temperature, and effective emissivity• Cloud optical thickness, thermodynamic phase, and effective
radius• Thin cirrus reflectance in the visible
– Aerosol optical properties• Optical thickness over the land and ocean• Size distribution (parameters) over the ocean
– Atmospheric moisture and temperature gradients– Column water vapor amount
• Gridded time-averaged (level-3) atmosphere product– Daily, 8-day, and monthly products– 1° x 1° equal angle grid– Mean, standard deviation, marginal probability density function,
joint probability density functions
• modis-atmos.gsfc.nasa.gov
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MODIS - TERRATrue colour image
Dust over theMediterranianMarch 12, 2003
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CO2 Slicing Method
• CO2 slicing method
– ratio of cloud forcing at two near-by wavelengths
– assumes the emissivity at each wavelength is same, and cancels out in ratio of two bands
• The more absorbing the band, the more sensitive it is to high clouds– technique the most accurate for
high and middle clouds
• MODIS is the first sensor to have CO2 slicing bands at high spatial resolution (1 km)– technique has been applied to HIRS
data for ~20 years– retrieved for every 5 x 5 box of 1
km FOVs, when at least 5 FOVs are cloudy, day & night
1000
100
10
0.0 0.2 0.4 0.6 0.8 1.0
Pres
sure
(mb)
Weighting Function dt(,p)/d ln p
Channel 32 33 34 35 36
Central Wavelength (µm)
12.020 13.335 13.635 13.935 14.235
36
1.2
35
34
33
32
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Brightness Temperature in 15 m CO2 band
Arrows atWavelengthsMeasured byVTPR
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Retrieval of Cloud Optical Depth and Effective Radius
• The reflection function of a nonabsorbing band (e.g., 0.86 µm) is primarily a function of optical thickness
• The reflection function of a near-infrared absorbing band (e.g., 2.14 µm) is primarily a function of effective radius– clouds with small drops (or
ice crystals) reflect more than those with large particles
• For optically thick clouds, there is a near orthogonality in the retrieval of c and re using a visible and near-infrared band
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Cloud Optical DepthApril 2001
20
0
10
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Cloud Effective Particle RadiusApril 2001
4 m
22
40
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Remote Sensing of Aerosols
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Kiehl and Trenberth (1997); IPCC (2001)
Global Annual Energy Balance
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Global Aerosol Emissions
(Tg / yr)
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Annual Global Volcanic Aerosol Loading
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Aerosol Optical Weighting Functions
K(a)=a2Qen(a)~Qe/reff
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http://www.giss.nasa/gov/data
Model Aerosol Type Optical Thickness
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MODIS Aerosol Optical Properties
• Seven MODIS bands are utilized to derive aerosol properties– 0.47, 0.55, 0.65, 0.86, 1.24, 1.64, and 2.13 µm– Ocean
• reflectance contrast between cloud-free atmosphere and ocean reflectance (dark)
• aerosol optical thickness (0.55-2.13 µm)• size distribution characteristics (fraction of aerosol optical
thickness in the fine particle mode; effective radius)– Land
• dense dark vegetation and semi-arid regions determined where aerosol is most transparent (2.13 µm)
• contrast between Earth-atmosphere reflectance and that for dense dark vegetation surface (0.47 and 0.66 µm)
• enhanced reflectance and reduced contrast over bright surfaces (post-launch)
• aerosol optical thickness (0.47 and 0.66 µm)
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Gobi Desert Dust Storm - March 20, 2001 MODIS
a (0.55 µm)
0
2.0
1.0
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Aerosol Optical Thickness - MODISFine Particle Mode
a (0.55 µm)
0
0.8
0.4
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TOMS - Aerosol Index - Feb 26, 2000
http://toms.gsfc.nasa.gov/index.html
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LITE - Lidar In space Technology ExperimentSeptember 1994 - Space Shuttle
http://www-lite.larc.nasa.gov/
Deep Convection
Saharan Dust
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Cloud-Aerosol Lidar and Infrared Pathfinder Sate llite O bs ervations
EARLINET Sy mposium 11 February2003
· Orbit: 705 km, 98° inclination,in formation with Aqua,CloudSat and Parasol
· Launch end of 2004
· Mission duration: 3 years
· Three co-alignedinstruments:
• 3-channel lidar– 532 nm ||– 532 nm ^– 1064 nm
• Imaging IR radiometer
• Wide-fie ld camera
Mission Concept
Complementary Instruments
• CloudSat radar (cloud profiles)• Aqua CERES (top-of-the-atmosphere radiation)• Aqua AIRS / AMSU-A / HSB (atmospheric state)• Aqua MODIS (aerosol / cloud properties)• PARASOL (aerosol / cloud properties)• Aura OMI (aerosol absorption)
Aqua CALIPSOCloudSat
PARASOL
Aura
Vertical distribution ofaerosols and clouds
Aerosol / cloud properties
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Remote Sensing of Gases
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Radiative Forcing Between 1850 to 2000
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Kiehl and Trenberth (1997); IPCC (2001)
Global Annual Energy Balance
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Atmospheric Transmittances in the Microwave
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Microwave Emissivity of Ocean Surface
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Microwave Brightness Temperature
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Precipitable Water
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http://www.arm.gov/docs/instruments/static/rl.html
Source/Aerosol 355nmN2 387nmWater Vapour 408nm
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Raman Lidar to Measure Water Vapour Profile
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GPS Signals to Measure Water Vapour
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http://atmos.af.op.dlr.de/projects/scops/
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Normalised weighting functions for the High Resolution Infrared Sounder (HIRS) on NOAA satellites. Each function indicates the relative contribution of the atmosphere from a given level to the radiance observed at the satellite through the numbered channel.
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Satellite Limb Scanning
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Limb ScanningWeightingFunctions
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Kiehl and Trenberth (1997); IPCC (2001)
Global Annual Energy Balance
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Final Comments
Ultimately radiation drives all processes in the atmosphere
Remote sensing will continue to grow as a source of atmospheric measurements
New suite of satellites will require more atmospheric scientists in this area
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Solar Ultra-violet Spectrum
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Optical Properties for Typical Stratus and Cumulus
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Bidirectional Reflectance and Absorbanceof Cirrus Clouds
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LIDARS
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Brightness Temperature in 15 m CO2 band
Arrows atWavelengthsMeasured byVTPR
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IR Brightness Temperature from ER-2
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