Atmospheric radiation and radiative transfer · 2019-09-10 · Radiation in the atmosphere...
Transcript of Atmospheric radiation and radiative transfer · 2019-09-10 · Radiation in the atmosphere...
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Atmospheric radiation andradiative transferAndré ButzInstitute of Environmental PhysicsUniversity of Heidelberg
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Radiation in the atmosphere
[IPCC, AR5, 2013]
Radiative energy fluxesrun planetary climate.
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Radiation in the atmosphere
Meridionally unbalancedincoming and outgoingradiative fluxes drivelarge scale atmosphereand ocean dynamics.
[Marshall and Plumb, 2008]
Zonal mean radiative cooling and heating: radiation surplus in the tropics, radiationdeficit at the poles: poleward transport ofheat required.
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Radiation in the atmosphere
Radiation drivesatmosphericphotochemistry: ozone layer, airpollution, …
[http://www.ccpo.odu.edu/SEES/ozone/class]
Production of ozone via the Chapman cycle in thestratosphere - initiatedby UV radiation thatsplits oxygen and ozonemolecules
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Radiation in the atmosphere
Radiation measurements are a key tool forunderstanding theEarth system … and other planets, stars, the universe.
[https://sites.physics.utoronto.ca/bit]
Measuring radiation enables remote sensing ofplanetary properties such as thermodynamic state, atmospheric composition, surface types, etc.
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Electromagnetic waves
Usually, we are interested in the electromagnetic energyflux in a certain direction:Poynting vector.
[Petty, 2006]
Ԧ𝑆 =1
𝜇𝐸 × 𝐵
W
m2
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Ԧ𝑆 =1
𝜇𝐸 × 𝐵
Electromagnetic waves
Usually, we are interested in the electromagnetic energyflux in a certain direction:Poynting vector.
[Petty, 2006]
W
m2
Usually, we do not care abouttimescales on theorder of em-waveoscillations: time averaging.
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Ԧ𝑆 =1
𝜇𝐸 × 𝐵
Electromagnetic waves
Usually, we are interested in the electromagnetic energyflux in a certain direction:Poynting vector.
[Petty, 2006]
W
m2
Usually, we do not care abouttimescales on theorder of em-waveoscillations: time averaging.
Usually, dealing withindividual waves (ofdifferent directions, different wavelengths, different shapes) isuntreatable.
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Ԧ𝑆 =1
𝜇𝐸 × 𝐵
Electromagnetic waves
Usually, we are interested in the electromagnetic energyflux in a certain direction:Poynting vector.
[Petty, 2006]
W
m2
Usually, we do not care abouttimescales on theorder of em-waveoscillations: time averaging.
Usually, dealing withindividual waves (ofdifferent directions, different wavelengths, different shapes) isuntreatable.
So, we need a „continuum“ quantitythat is something like the sum of all time-averaged Poynting vectorcontributions in a certain direction at a certain place: radiance.
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Radiometric quantities
Spectral radiance 𝐼𝜆 (or 𝐿𝜆): 𝐼𝜆 = 𝐼𝜆 𝑡; 𝑥, 𝑦, 𝑧; 𝛺 =𝑑𝐸𝑛𝑒𝑟𝑔𝑦
𝑑𝑡 𝑑𝜆 𝑑𝛺 𝑐𝑜𝑠𝜃 𝑑𝐴
W
m2 nm sr
„Radiant power in wavelength element 𝑑𝜆 transported
through cross-sectional area 𝑐𝑜𝑠𝜃 𝑑𝐴 into/from
direction element 𝑑𝛺 (defined via solid angle
[steradian]).“
= strength of pencil beam of radiation / ray of light
[Petty, 2006]
dW
W
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Radiometric quantities
Spectral radiance 𝐼𝜆 (or 𝐿𝜆): 𝐼𝜆 = 𝐼𝜆 𝑡; 𝑥, 𝑦, 𝑧; 𝛺 =𝑑𝐸𝑛𝑒𝑟𝑔𝑦
𝑑𝑡 𝑑𝜆 𝑑𝛺 𝑐𝑜𝑠𝜃 𝑑𝐴
W
m2 nm sr
„Radiant power in wavelength element 𝑑𝜆 transported
through cross-sectional area 𝑐𝑜𝑠𝜃 𝑑𝐴 into/from
direction element 𝑑𝛺 (defined via solid angle
[steradian]).“
= strength of pencil beam of radiation / ray of light
𝐼𝜆 𝑡; 𝑥, 𝑦, 𝑧; 𝛺
dW
W
dl
dA
[http://www.oceanopticsbook.info]
[Petty, 2006]
dW
W
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Spectral irradiance 𝐹𝜆:
Radiometric quantities
„Radiant power in
wavelength element 𝑑𝜆transported through
surface area 𝑑𝐴.“
= „radiant energy flux
through surface.“
𝐹𝜆 = 𝐹𝜆 𝑡; 𝑥, 𝑦, 𝑧 =𝑑𝐸𝑛𝑒𝑟𝑔𝑦
𝑑𝑡 𝑑𝜆 𝑑𝐴=
= 2𝜋 𝐼𝜆 cos 𝜃 𝑑𝛺
W
m2 nm
[Petty, 2006]
dW
W
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Spectral irradiance 𝐹𝜆:
Radiometric quantities
„Radiant power in
wavelength element 𝑑𝜆transported through
surface area 𝑑𝐴.“
= „radiant energy flux
through surface.“
𝐹𝜆 = 𝐹𝜆 𝑡; 𝑥, 𝑦, 𝑧 =𝑑𝐸𝑛𝑒𝑟𝑔𝑦
𝑑𝑡 𝑑𝜆 𝑑𝐴=
= 2𝜋 𝐼𝜆 cos 𝜃 𝑑𝛺
W
m2 nm
𝐹𝜆 𝑡; 𝑥, 𝑦, 𝑧
dA
W in 2p
[http://www.oceanopticsbook.info]
[Petty, 2006]
dW
W
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Spectral actinic flux 𝐴𝜆:
Radiometric quantities
Photons
s m2 nm
𝐴𝜆 = 𝐴𝜆 𝑡; 𝑥, 𝑦, 𝑧 = න4𝜋
𝐼𝜆 𝑑𝛺
„Radiant power / Number of
photons in wavelength
element 𝑑𝜆 hitting surface 𝑑𝐴.“
= „Radiant energy available for
chemical reactions.“
𝐴𝜆,𝑝ℎ = 𝐴𝜆,𝑝ℎ 𝑡; 𝑥, 𝑦, 𝑧 = න4𝜋
𝐼𝜆/ℎ𝑐
𝜆𝑑𝛺
W
m2 nm
[Petty, 2006]
dW
W
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Spectral actinic flux 𝐴𝜆:
Radiometric quantities
Photons
s m2 nm
𝐴𝜆 = 𝐴𝜆 𝑡; 𝑥, 𝑦, 𝑧 = න4𝜋
𝐼𝜆 𝑑𝛺
„Radiant power / Number of
photons in wavelength
element 𝑑𝜆 hitting surface 𝑑𝐴.“
= „Radiant energy available for
chemical reactions.“
𝐴𝜆,𝑝ℎ = 𝐴𝜆,𝑝ℎ 𝑡; 𝑥, 𝑦, 𝑧 = න4𝜋
𝐼𝜆/ℎ𝑐
𝜆𝑑𝛺
W
m2 nm
W in 4p
𝐴𝜆 𝑡; 𝑥, 𝑦, 𝑧
[http://www.oceanopticsbook.info]
[Petty, 2006]
dW
W
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Radiation in the middle atmosphere
Actinic flux 𝑨𝝀: Driver for photochemistry.
Irradiance 𝑭𝝀: Energy balance, heating and cooling rates.
Radiance 𝑰𝝀: Remote sensing of composition.
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Planetary radiation sources
Collimated radiance beam from sun
[Thomas and Stamnes, 1999]
𝐵𝜆 𝑇 =2ℎ𝑐2
𝜆5 expℎ𝑐𝜆𝑘𝑇
− 1
Planck’s law of black body radiation:
For the sun: 𝑇 ≈ 5800 𝐾 (photosphere)
+ Fraunhofer lines (absorption in the solar atmosphere)
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Planetary radiation sources
Collimated radiance beam from sun
[Thomas and Stamnes, 1999]
𝐵𝜆 𝑇 =2ℎ𝑐2
𝜆5 expℎ𝑐𝜆𝑘𝑇
− 1
Planck’s law of black body radiation:
For the sun: 𝑇 ≈ 5800 𝐾 (photosphere)
+ Fraunhofer lines (absorption in the solar atmosphere)
In the deep UV, solar radiation stems from the dilute and hot solar atmosphere.
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[Petty, 2006]
Planetary radiation sources
Isotropic thermal emission by the Earth’s surface and atmosphere
𝐵𝜆 𝑇 =2ℎ𝑐2
𝜆5 expℎ𝑐𝜆𝑘𝑇
− 1
Planck’s law of black body radiation:
For the Earth: 𝑇 ≈180…320 𝐾
Wavelength / micron
𝜆𝑚𝑎𝑥 =2898 𝜇𝑚
𝑇
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Planetary radiation sources
In the shortwave (< 4 micron) solar radiation dominates, in the longwave (> 4 micron) telluric radiation dominates
… unless one looks directly into the sun or into mirror-like reflections of the sun – then the sun dominates at all wavelengths.
Comparison of isotropically reflected solar and emitted telluric radiation (under conceptual Planck’s law assumption).
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Radiative transfer equation
𝑑𝐼𝜆𝑑𝑠
=
−𝐼𝜆 ⋅ 𝑘𝑎,𝜆
−𝐼𝜆 ⋅ 𝑘𝑠,𝜆
+𝐵𝜆 ⋅ 𝑘𝑎,𝜆
+𝑘𝑠,𝜆4𝜋
න0
2𝜋
න0
𝜋
𝐼𝜆 Ω′ ⋅ 𝑝 Ω′ → Ω 𝑑Ω′
𝐼𝜆 𝑥, 𝑦, 𝑧; 𝛺
𝐼𝜆 𝑥′, 𝑦′, 𝑧′; 𝛺
𝑑𝑠
𝑑𝑧
[http://www.oceanopticsbook.info]
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Radiative transfer equation
𝑑𝐼𝜆𝑑𝑠
=
−𝐼𝜆 ⋅ 𝑘𝑎,𝜆
−𝐼𝜆 ⋅ 𝑘𝑠,𝜆
+𝐵𝜆 ⋅ 𝑘𝑎,𝜆
+𝑘𝑠,𝜆4𝜋
න0
2𝜋
න0
𝜋
𝐼𝜆 Ω′ ⋅ 𝑝 Ω′ → Ω 𝑑Ω′
𝐼𝜆 𝑥, 𝑦, 𝑧; 𝛺
𝐼𝜆 𝑥′, 𝑦′, 𝑧′; 𝛺
𝑑𝑠
𝑑𝑧
[http://www.oceanopticsbook.info]
Absorption coefficient (n, p, T,…)
Scattering coefficient
Scattering phase function
Properties of the medium
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Examples: Direct-sun
Direct sun:
• neglect telluric emission (𝑇𝐸𝑎𝑟𝑡ℎ ≪ 𝑇𝑆𝑢𝑛)
• neglect scattering gain (number of scattered photons ≪ direct photons)
𝑑𝐼𝜆𝑑𝑠
≈ −(𝑘𝑎,𝜆 + 𝑘𝑠,𝜆)𝐼𝜆
(Beer Lambert‘s law)
𝐼𝜆 = 𝐼𝜆,𝑠𝑢𝑛𝑒− 𝑠𝑢𝑛
𝑠𝑒𝑛𝑠𝑜𝑟𝑘𝑎,𝜆+𝑘𝑠,𝜆 𝑑𝑠
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Examples: Direct-sun
Direct sun:
• neglect telluric emission (𝑇𝐸𝑎𝑟𝑡ℎ ≪ 𝑇𝑆𝑢𝑛)
• neglect scattering gain (number of scattered photons ≪ direct photons)
𝑑𝐼𝜆𝑑𝑠
≈ −(𝑘𝑎,𝜆 + 𝑘𝑠,𝜆)𝐼𝜆
(Beer Lambert‘s law)
𝐼𝜆 = 𝐼𝜆,𝑠𝑢𝑛𝑒− 𝑠𝑢𝑛
𝑠𝑒𝑛𝑠𝑜𝑟𝑘𝑎,𝜆+𝑘𝑠,𝜆 𝑑𝑠
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Examples: Direct-sun
Direct sun:
• neglect telluric emission (𝑇𝐸𝑎𝑟𝑡ℎ ≪ 𝑇𝑆𝑢𝑛)
• neglect scattering gain (number of scattered photons ≪ direct photons)
𝑑𝐼𝜆𝑑𝑠
≈ −(𝑘𝑎,𝜆 + 𝑘𝑠,𝜆)𝐼𝜆
(Beer Lambert‘s law)
𝐼𝜆 = 𝐼𝜆,𝑠𝑢𝑛𝑒− 𝑠𝑢𝑛
𝑠𝑒𝑛𝑠𝑜𝑟𝑘𝑎,𝜆+𝑘𝑠,𝜆 𝑑𝑠
𝑘𝑎,𝜆: here - rotational-vibrational absorption by CO2
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Examples: Solar occultation sounding
Solar occultation from stratospheric balloons –composition profiling
Combine a series of direct sun radiance measurements during sunset / sunrise to infer the concentration profiles of substances in the middle atmosphere.
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Examples: Solar heating
The absorbed radiative energy (difference between TOA and sea level) heats the atmosphere.
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Examples: Solar heating
Spectral heating rate 𝑯𝝀: 𝐻𝜆 = −1
𝜌 𝐶𝑝න4𝜋
𝛺 ∙ 𝛻𝐼𝜆 𝑑𝛺
„change (per pathlength) of radiance
along direction 𝛺” (= fancy variant of 𝑑𝐼𝜆
𝑑𝑠)
𝐾
𝑛𝑚 𝑠
𝜌(𝑧): air density
𝐶𝑝 : specific heat
capacity at constant p
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Examples: Solar heating
Spectral heating rate 𝑯𝝀: 𝐻𝜆 = −1
𝜌 𝐶𝑝න4𝜋
𝛺 ∙ 𝛻𝐼𝜆 𝑑𝛺𝐾
𝑛𝑚 𝑠
𝜌(𝑧): air density
𝐶𝑝 : specific heat
capacity at constant p
If one is interested onlyin vertically (z) layeredheating rates (plane parallel geometry): 𝐻𝜆 = −
1
𝜌 𝐶𝑝
𝑑𝐹𝜆𝑑𝑧
𝐹𝜆 𝑧 = 𝐹𝜆↑ 𝑧 − 𝐹𝜆
↓ 𝑧
𝐹𝜆 𝑧 + 𝑑𝑧 = 𝐹𝜆↑ 𝑧 + 𝑑𝑧 − 𝐹𝜆
↓ 𝑧 + 𝑑𝑧
𝑑𝑧
„change (per pathlength) of radiance
along direction 𝛺” (= fancy variant of 𝑑𝐼𝜆
𝑑𝑠)
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Examples: Solar heating
Spectral heating rate 𝑯𝝀: 𝐻𝜆 = −1
𝜌 𝐶𝑝න4𝜋
𝛺 ∙ 𝛻𝐼𝜆 𝑑𝛺𝐾
𝑛𝑚 𝑠
𝜌(𝑧): air density
𝐶𝑝 : specific heat
capacity at constant p
If one is interested onlyin vertically (z) layeredheating rates (plane parallel geometry): 𝐻𝜆 = −
1
𝜌 𝐶𝑝
𝑑𝐹𝜆𝑑𝑧
𝐹𝜆 𝑧 = 𝐹𝜆↑ 𝑧 − 𝐹𝜆
↓ 𝑧
𝐹𝜆 𝑧 + 𝑑𝑧 = 𝐹𝜆↑ 𝑧 + 𝑑𝑧 − 𝐹𝜆
↓ 𝑧 + 𝑑𝑧
𝑑𝑧
„change (per pathlength) of radiance
along direction 𝛺” (= fancy variant of 𝑑𝐼𝜆
𝑑𝑠)
Total heating rate 𝑯: 𝐻 = න0
∞
𝐻𝜆 𝑑𝜆
„given the rich spectral structureof atmospheric absorption, thespectral integral is a complexundertaking: band models“
𝐾
𝑠
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Examples: Solar heating
𝐻𝜆 = −1
𝜌 𝐶𝑝
𝑑𝐹𝜆𝑑𝑧
𝐹𝜆 𝑧 = 𝐹𝜆↑ 𝑧 − 𝐹𝜆
↓ 𝑧
𝐹𝜆 𝑧 + 𝑑𝑧 = 𝐹𝜆↑ 𝑧 + 𝑑𝑧 − 𝐹𝜆
↓ 𝑧 + 𝑑𝑧
𝑑𝑧
[Brasseur and Solomon, 2006]
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Examples: Telluric emission
Telluric emission:
• neglect scattering - operate sufficiently far in the infrared such that scattering is negligible (under cloudless conditions)
𝐼𝜆 𝑡; 𝑥, 𝑦, 𝑧; 𝛺
W=Wnadir
𝑑𝐼𝜆𝑑𝑠
= −𝑘𝑎,𝜆(𝐼𝜆 − 𝐵𝜆)
(Schwarzschild equation)Earth
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33
Examples: Telluric emission
Telluric emission:
• neglect scattering - operate sufficiently far in the infrared such that scattering is negligible (under cloudless conditions)
𝑑𝐼𝜆𝑑𝑠
= −𝑘𝑎,𝜆(𝐼𝜆 − 𝐵𝜆)
(Schwarzschild equation)
[Petty, 2006]
Upwelling longwave radiation: downward looking from satellite / or high-altitude balloon
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34
Examples: Telluric emission
Telluric emission:
• neglect scattering - operate sufficiently far in the infrared such that scattering is negligible (under cloudless conditions)
𝑑𝐼𝜆𝑑𝑠
= −𝑘𝑎,𝜆(𝐼𝜆 − 𝐵𝜆)
(Schwarzschild equation)
[Petty, 2006]
Upwelling longwave radiation: downward looking from satellite / or high-altitude balloon
Transparent wavelength(radiance emitted byground)
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35
Examples: Telluric emission
Telluric emission:
• neglect scattering - operate sufficiently far in the infrared such that scattering is negligible (under cloudless conditions)
𝑑𝐼𝜆𝑑𝑠
= −𝑘𝑎,𝜆(𝐼𝜆 − 𝐵𝜆)
(Schwarzschild equation)
[Petty, 2006]
Upwelling longwave radiation: downward looking from satellite / or high-altitude balloon
Transparent wavelength(radiance emitted byground)
Opaque wavelength(radiance emitted by
ground gets absorbedby molecules in the
atmosphere, atmosphere emits
upward and downward)
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Examples: Emission limb sounding
Emission limb sounding from stratospheric balloons –composition profiling.
Combine a series of tangential limb emission spectra at different tangent heights to infer the concentration profiles of substances in the middle atmosphere.
[https://www.imk-asf.kit.edu/english/319.php]
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Examples: Emission limb sounding
Emission limb sounding from stratospheric balloons –composition profiling.
Combine a series of tangential limb emission spectra at different tangent heights to infer the concentration profiles of substances in the middle atmosphere.
[https://www.imk-asf.kit.edu/english/319.php][courtesy by M. Höpfner, MIPAS-Balloon, KIT]
HNO3
CO2
O3O3
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Examples: Thermal cooling
Escape of thermal radiation into space cools the atmosphere and the surface.
(But absorption in the atmosphere hinders some of the radiation to escape / cooling less efficient than without atmosphere = greenhouse effect.)
Upwelling longwave radiation: downward looking from satellite / or high-altitude balloon
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Examples: Thermal cooling
𝐻𝜆 = −1
𝜌 𝐶𝑝
𝑑𝐹𝜆𝑑𝑧
𝐹𝜆 𝑧 = 𝐹𝜆↑ 𝑧 − 𝐹𝜆
↓ 𝑧
𝐹𝜆 𝑧 + 𝑑𝑧 = 𝐹𝜆↑ 𝑧 + 𝑑𝑧 − 𝐹𝜆
↓ 𝑧 + 𝑑𝑧
𝑑𝑧
[Brasseur and Solomon, 2006]
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Examples: Solar heating and thermal cooling
𝐻𝜆 = −1
𝜌 𝐶𝑝
𝑑𝐹𝜆𝑑𝑧
𝐹𝜆 𝑧 = 𝐹𝜆↑ 𝑧 − 𝐹𝜆
↓ 𝑧
𝐹𝜆 𝑧 + 𝑑𝑧 = 𝐹𝜆↑ 𝑧 + 𝑑𝑧 − 𝐹𝜆
↓ 𝑧 + 𝑑𝑧
𝑑𝑧
[Brasseur and Solomon, 2006]
In a steady state (T constant), net radiative heating/cooling would need to be balanced by dynamic heat transport.
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Examples: Scattered sunlight
Scattered sunlight (typically considered at short wavelengths < 4 micron):
• neglect telluric emission𝑑𝐼𝜆𝑑𝑠
= −(𝑘𝑎,𝜆 + 𝑘𝑠,𝜆)𝐼𝜆
+𝑘𝑠,𝜆4𝜋
න0
2𝜋
න0
𝜋
𝐼𝜆 Ω′ ⋅ 𝑝 Ω′ → Ω 𝑑Ω′
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Skylight limb sounding from stratospheric balloons –composition profiling.
Combine a series of scattered sunlight spectra at different tangent heights to infer the concentration profiles of substances in the middle atmosphere.
Examples: Skylight limb sounding
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Skylight limb sounding from stratospheric balloons –composition profiling.
Combine a series of scattered sunlight spectra at different tangent heights to infer the concentration profiles of substances in the middle atmosphere.
Examples: Skylight limb sounding
[Petty, 2006]
Atmospheric scattering properties depend heavily on size/wavelength, particle phase/shape
(liquid, ice): x =2𝜋𝑟
𝜆
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Skylight limb sounding from stratospheric balloons –composition profiling.
Combine a series of scattered sunlight spectra at different tangent heights to infer the concentration profiles of substances in the middle atmosphere.
Examples: Skylight limb sounding
Atmospheric scattering properties depend heavily on size/wavelength, particle phase/shape
(liquid, ice): x =2𝜋𝑟
𝜆
Scattering phase function
x ≪ 1 (molecules)
[Petty, 2006]
Cirrus 22°halo
x > 1 (liquid)
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Examples: Cloud radiative effects
[Corti and Peter, ACP, 2009]
Shortwave
clear-sky cloudy
Longwave
clear-sky cloudy
Clouds backscattersolar shortwaveradiation and traplongwave telluricradiation.
Schematic radiative effects of cloudy vs. clearsky conditions in the shortwave and longwave regimes
[Corti and Peter, ACP, 2009]
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Examples: Cloud radiative effects
[Meerkötter et al., 1999]
Clouds backscattersolar shortwaveradiation and traplongwave telluricradiation.
Net radiative flux (𝐹) changes (referenced to clear-sky) for a cirrus at roughly 11 km altitude
coo
ling
he
atin
g For high altitude clouds, the longwave trappingeffect typically outweighsthe shortwavebackscattering effect such that the cloud is a netheating of the belowatmosphere and surface.
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Examples: Cloud radiative effects
Clouds backscattersolar shortwaveradiation and traplongwave telluricradiation.
Net radiative flux (𝐹) changes (contours) as function of cloud optical thickness and clout top height.
cooling heating
For the shortwave effect, it does not really matter at what height the cloudis, cloud thickness is important. The thicker, the „brighter“ the cloud. (However, high ice clouds are often thin.)
For the longwave effect, cloud height is important (in particular for opaqueclouds) since higher clouds at lower T radiate less to space.
LWSW
[Corti and Peter, ACP, 2009]
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Examples: Cloud radiative effects
Clouds backscattersolar shortwaveradiation and traplongwave telluricradiation.
Net radiative flux (𝐹) changes (contours) as function of cloud optical thickness and clout top height.
cooling heating
For the shortwave effect, it does not really matter at what height the cloudis, cloud thickness is important. The thicker, the „brighter“ the cloud. (However, high ice clouds are often thin.)
For the longwave effect, cloud height is important (in particular for opaqueclouds) since higher clouds at lower T radiate less to space.
LWSW
cooling
cooling
heating
NET„High, thin clouds heatthe Earth; low, thickclouds cool the Earth.“
[Corti and Peter, ACP, 2009]
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Summary
Stratospheric ballooningprovides a great way toexperience the manifoldways of how radiationshapes our environment:
climate physics,atmospheric photochemistry, atmospheric dynamics, balloon thermodynamics, Earth observation, solar physics, astronomy, …
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Examples: Cloud radiative effects
[Meerkötter et al., 1999]
Clouds backscattersolar shortwaveradiation and traplongwave telluricradiation.
Net radiative flux (𝐹) changes (referenced to clear-sky) and heating rate for a thin cirrus (optical thickness 0.5 in the visible) at roughly 11 km altitude.
Cirrus