LIMBTRAN: A pseudo three‐dimensional radiative transfer model for the limb‐viewing imager OSIRIS on the ODIN satellite

Griffioen, E.; Oikarinen, Liisa

doi:10.1029/2000jd900566

Cited by 48 publications

(48 citation statements)

References 27 publications

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“…Therefore, radiative transfer calculations can be used as a guide to find an optimum threshold for PSC detection. In order to estimate the range of color index ratios (TH) occurring in a PSC-free stratosphere -only due to Rayleigh scattering and stratospheric sulphate aerosol -we performed simulations with the RT model LIMBTRAN (Griffioen and Oikarinen., 2000) for the following scenarios: (a) a pure Rayleigh atmosphere without aerosols, (b) stratospheric background aerosol conditions, (c) moderate volcanic and (d) high volcanic aerosol conditions and for the solar zenith angle (SZA) range from 30 • to 90 • , and the solar azimuth angle (SAA) range from 20 • (forward scattering) to 160 • (backward scattering). These SZA and SAA ranges include all possible SCIAMACHY limb viewing geometries.…”

Section: Methodsmentioning

confidence: 99%

Detection and mapping of polar stratospheric clouds using limb scattering observations

et al. 2005

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Abstract. Satellite-based measurements of Visible/NIR limb-scattered solar radiation are well suited for the detection and mapping of polar stratospheric clouds (PSCs). This publication describes a method to detect PCSs from limb scattering observations with the Scanning Imaging Absorption spectroMeter for Atmospheric CartograpHY (SCIA-MACHY) on the European Space Agency's Envisat spacecraft. The method is based on a color-index approach and requires a priori knowledge of the stratospheric background aerosol loading in order to avoid false PSC identifications by stratospheric background aerosol. The method is applied to a sample data set including the 2003 PSC season in the Southern Hemisphere. The PSCs are correlated with coincident UKMO model temperature data, and with very few exceptions, the detected PSCs occur at temperatures below 195-198 K. Monthly averaged PSC descent rates are about 1.5 km/month for the −50 • S to −75 • S latitude range and assume a maximum between August and September with a value of about 2.5 km/month. The main cause of the PSC descent is the slow descent of the lower stratospheric temperature minimum.

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Section: Methodsmentioning

confidence: 99%

Detection and mapping of polar stratospheric clouds using limb scattering observations

et al. 2005

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“…[40] The pseudo-spherical multiple scattering radiative transfer model LIMBTRAN [Griffoen and Oikarinen, 2000] is used to invert ECD as a function of tangent height to number density as a function of height. Temperature and pressure information used in LIMBTRAN is from the European Centre for Medium-Range Weather Forecasts (ECMWF) analysis fields.…”

Section: Forward Modelmentioning

confidence: 99%

Validation of Odin/OSIRIS stratospheric NO₂ profiles

Brohede¹,

Haley²,

McLinden³

et al. 2007

J. Geophys. Res.

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[1] This paper presents the validation study of stratospheric NO 2 profiles retrieved from Odin/OSIRIS measurements of limb-scattered sunlight (version 2.4). The Optical Spectrograph and Infrared Imager System (OSIRIS) NO 2 data set is compared to coincident solar occultation measurements by the Halogen Occultation Experiment (HALOE), Stratospheric Aerosol and Gas Experiment (SAGE) II, SAGE III, and Polar Ozone and Aerosol Measurement (POAM) III during the 2002-2004 period. Comparisons with seven Systeme d'Analyse par Observation Zenithal (SAOZ) balloon measurements are also presented. All comparisons show good agreement, with differences, both random and systematic, of less than 20% between 25 km and 35 km. Inconsistencies with SAGE III below 25 km are found to be caused primarily by diurnal effects from varying NO 2 concentrations along the SAGE III line-of-sight. On the basis of the differences, the OSIRIS random uncertainty is estimated to be 16% between 15 km and 25 km, 6% between 25 km and 35 km, and 9% between 35 km and 40 km. The estimated systematic uncertainty is about 22% between 15 and 25 km, 11-21% between 25 km and 35 km, and 11-31% between 35 km and 40 km. The uncertainties for AM (sunrise) profiles are generally largest and systematic deviations are found to be larger at equatorial latitudes. The results of this validation study show that the OSIRIS NO 2 profiles are well behaved, with reasonable uncertainty estimates between 15 km and 40 km. This unique NO 2 data set, with more than hemispheric coverage and high vertical resolution will be of particular interest for studies of nitrogen chemistry in the middle atmosphere, which is closely linked to ozone depletion.

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“…The first step is the spectral analysis of the OS measurements to calculate the OClO ECD profiles by applying the DOAS technique. The second step is the inversion of these ECD profiles to obtain the number density profiles using a nonlinear iterative version of the MAP estimator coupled with the LIMBTRAN (Griffioen and Oikarinen, 2000) radiative transfer model. Table 1 summarizes the specifications of the spectral window used to retrieve OClO in this work.…”

Section: Methodsmentioning

confidence: 99%

“…Simulated optical depths are then calculated and subjected to a DOAS analysis. The resulting effective column densities constitute the forward model F. In a trade-off between computational efficiency and accuracy, the pseudo-spherical multiple scattering radiative transfer model LIMBTRAN (Griffioen and Oikarinen, 2000) is applied in the inversion procedure. Temperature and pressure are taken from the ECMWF analysis fields.…”

Section: The Forward Modelmentioning

confidence: 99%

Retrieving the vertical distribution of stratospheric OClO from Odin/OSIRIS limb-scattered sunlight measurements

Krecl

Haley²,

Stegman³

et al. 2006

Atmos. Chem. Phys.

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Abstract. The first vertical profiles of stratospheric OClO retrieved from Odin/OSIRIS limb-scattered sunlight radiances are presented. The retrieval method is based on a two-step approach, using differential optical absorption spectroscopy combined with the maximum a posteriori estimator. The details of the spectral window selection, spectral corrections and inversion technique are discussed. The results show that OClO can be detected inside the South polar vortex region between about 14 and 22 km altitude with a 2-5 km height resolution and an estimated retrieval error better than 50% at the peak. OClO concentrations show the expected relation to the atmospheric conditions in the lower stratosphere in the austral spring 2002. This unique data set of OClO profiles is very promising to study the stratospheric chlorine activation in both polar regions.

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LIMBTRAN: A pseudo three‐dimensional radiative transfer model for the limb‐viewing imager OSIRIS on the ODIN satellite

Abstract: Abstract.A

Cited by 48 publications

References 27 publications

Detection and mapping of polar stratospheric clouds using limb scattering observations

Detection and mapping of polar stratospheric clouds using limb scattering observations

Validation of Odin/OSIRIS stratospheric NO₂ profiles

Retrieving the vertical distribution of stratospheric OClO from Odin/OSIRIS limb-scattered sunlight measurements

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LIMBTRAN: A pseudo three‐dimensional radiative transfer model for the limb‐viewing imager OSIRIS on the ODIN satellite

Abstract: Abstract.A

Cited by 48 publications

References 27 publications

Detection and mapping of polar stratospheric clouds using limb scattering observations

Detection and mapping of polar stratospheric clouds using limb scattering observations

Validation of Odin/OSIRIS stratospheric NO2 profiles

Retrieving the vertical distribution of stratospheric OClO from Odin/OSIRIS limb-scattered sunlight measurements

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Validation of Odin/OSIRIS stratospheric NO₂ profiles