Detection and mapping of polar stratospheric clouds using limb scattering observations

Savigny, Christian von; Ulasi, E. P.; Eichmann, Kai‐Uwe; Bovensmann, H.; Burrows, John P.

doi:10.5194/acp-5-3071-2005

Cited by 42 publications

(36 citation statements)

References 24 publications

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“…PSC results will be presented as PSC occurrence rate, which is a dimensionless quantity and is defined as the ratio of the number of observations with PSC detections and the total number of SCIAMACHY limb measurements -in a given latitude/longitude bin of 5 • × 5 • . As demonstrated in von Savigny et al (2005b) the detections are robust with very few PSC detections at temperatures exceeding 200 K. Unfortunately, H 2 SO 4 and HNO 3 have no strong spectral signatures in the spectral range covered by SCIA-MACHY. Therefore, the identification of different PSC types (in particular the distinction between type Ia and Ib) is challenging.…”

Section: Detection Of Polar Stratospheric Cloudsmentioning

confidence: 80%

“…Polar stratospheric clouds (PSCs) are also detected using SCIAMACHY limb-scatter observations with a colour-index approach employing two weakly absorbing wavelengths in the near IR (750 nm and 1090 nm) as described in von Savigny et al (2005b). PSC results will be presented as PSC occurrence rate, which is a dimensionless quantity and is defined as the ratio of the number of observations with PSC detections and the total number of SCIAMACHY limb measurements -in a given latitude/longitude bin of 5 • × 5 • .…”

Section: Detection Of Polar Stratospheric Cloudsmentioning

confidence: 99%

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Chemical ozone losses in Arctic and Antarctic polar winter/spring season derived from SCIAMACHY limb measurements 2002–2009

et al. 2013

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Abstract. Stratospheric ozone profiles are retrieved for the period 2002–2009 from SCIAMACHY measurements of limb-scattered solar radiation in the Hartley and Chappuis absorption bands of ozone. This data set is used to determine the chemical ozone losses in both the Arctic and Antarctic polar vortices by averaging the ozone in the vortex at a given potential temperature. The chemical ozone losses at isentropic levels between 450 K and 600 K are derived from the difference between observed ozone abundances and the ozone modelled taking diabatic cooling into account, but no chemical ozone loss. Chemical ozone losses of up to 30–40% between mid-January and the end of March inside the Arctic polar vortex are reported. Strong inter-annual variability of the Arctic ozone loss is observed, with the cold winters 2004/2005 and 2006/2007 showing chemical ozone losses inside the polar vortex at 475 K, where 1.7 ppmv and 1.4 ppmv of ozone were removed, respectively, over the period from 22 January to beginning of April and 0.9 ppmv and 1.2 ppmv, respectively, during February. For the winters of 2007/2008 and 2002/2003, ozone losses of about 0.8 ppmv and 0.4 ppmv, respectively are estimated at the 475 K isentropic level for the period from 22 January to beginning of April. Essentially no ozone losses were diagnosed for the relatively warm winters of 2003/2004 and 2005/2006. The maximum ozone loss in the SCIAMACHY data set was found in 2007 at the 600 K level and amounted to about 2.1 ppmv for the period between 22 January and the end of April. Enhanced losses close to this altitude were found in all investigated Arctic springs, in contrast to Antarctic spring. The inter-annual variability of ozone losses and PSC occurrence rates observed during Arctic spring is consistent with the known QBO effects on the Arctic polar vortex, with exception of the unusual Arctic winter 2008/2009. The maximum total ozone mass loss of about 25 million tons was found in the cold Arctic winter of 2004/2005 inside the polar vortex between the 450 K and 600 K isentropic levels from mid-January until the middle of March. The Antarctic vortex averaged ozone loss as well as the size of the polar vortex do not vary much from year to year. The total ozone mass loss inside the Antarctic polar vortex between the 450 K and 600 K isentropic levels is about 50–60 million tons and the vortex volume for this altitude range varies between about 150 and 300 km3 for the period between mid-August and mid-November of every year studied, except for 2002. In 2002 a mid-winter major stratospheric warming occurred in the second half of September and the ozone mass loss was only about half of the value in the other years. However, inside the polar vortex we find chemical ozone losses at the 475 K isentropic level that are similar to those in all other years studied. At this isentropic level ozone losses of 70–90% between mid-August and mid-November or about 2.5 ppmv are observed every year. At isentropic levels above 500 K the chemical ozone losses were found to be larger in 2002 than in all other years studied. Comparisons of the vertical variation of ozone losses derived from SCIAMACHY observations with several independent techniques for the Arctic winter 2004/2005 show that the SCIAMACHY results fall in the middle of the range of previously published results for this winter. For other winters in both hemispheres – for which comparisons with other studies were possible – the SCIAMACHY results are consistent with the range of previously published results.

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Section: Detection Of Polar Stratospheric Cloudsmentioning

confidence: 80%

Section: Detection Of Polar Stratospheric Cloudsmentioning

confidence: 99%

Chemical ozone losses in Arctic and Antarctic polar winter/spring season derived from SCIAMACHY limb measurements 2002–2009

et al. 2013

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“…Consequently, these datasets are restricted to local sites or are directly attached to the solar terminator and therefore do not allow measurements inside the cold and dark winter polar vortices. UV-vis limb scattering measurements can also measure PSC distributions (von Savigny et al, 2005) but currently do not allow PSC types to be discriminated and are restricted to daylight conditions. Stellar occultation mea-surements in the UV-vis wavelength region can partly compensate for the difficulty of adequate coverage of the polar night cap (e.g.…”

Section: Introductionmentioning

confidence: 99%

A climatology of polar stratospheric cloud composition between 2002 and 2012 based on MIPAS/Envisat observations

Spang¹,

Hoffmann²,

Müller³

et al. 2018

Atmos. Chem. Phys.

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Abstract. The Michelson Interferometer for Passive Atmospheric Sounding (MIPAS) instrument aboard the European Space Agency (ESA) Envisat satellite operated from July 2002 to April 2012. The infrared limb emission measurements provide a unique dataset of day and night observations of polar stratospheric clouds (PSCs) up to both poles. A recent classification method for PSC types in infrared (IR) limb spectra using spectral measurements in different atmospheric window regions has been applied to the complete mission period of MIPAS. The method uses a simple probabilistic classifier based on Bayes' theorem with a strong independence assumption on a combination of a well-established two-colour ratio method and multiple 2-D probability density functions of brightness temperature differences. The Bayesian classifier distinguishes between solid particles of ice, nitric acid trihydrate (NAT), and liquid droplets of supercooled ternary solution (STS), as well as mixed types.A climatology of MIPAS PSC occurrence and specific PSC classes has been compiled. Comparisons with results from the classification scheme of the spaceborne lidar CloudAerosol Lidar with Orthogonal Polarization (CALIOP) on the Cloud-Aerosol-Lidar and Infrared Pathfinder Satellite Observations (CALIPSO) satellite show excellent correspondence in the spatial and temporal evolution for the area of PSC coverage (A PSC ) even for each PSC class. Probability density functions of the PSC temperature, retrieved for each class with respect to equilibrium temperature of ice and based on coincident temperatures from meteorological reanalyses, are in accordance with the microphysical knowledge of the formation processes with respect to temperature for all three PSC types.This paper represents unprecedented pole-covering dayand nighttime climatology of the PSC distributions and their composition of different particle types. The dataset allows analyses on the temporal and spatial development of the PSC formation process over multiple winters. At first view, a more general comparison of A PSC and A ICE retrieved from the observations and from the existence temperature for NAT and ice particles based on the European Centre for MediumRange Weather Forecasts (ECMWF) reanalysis temperature data shows the high potential of the climatology for the validation and improvement of PSC schemes in chemical transport and chemistry-climate models.

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“…Consequently, these datasets are restricted to local sites or are directly attached to the solar terminator, and therefore do not allow measurements inside the cold and dark winter polar vortices. UV/vis limb scattering measurements can also measure PSC 90 distributions (von Savigny et al, 2005), but currently do not allow PSC types to be discriminated and are restricted to daylight Atmos. Chem.…”

mentioning

confidence: 99%

A climatology of polar stratospheric cloud composition between 2002 and 2012 based on MIPAS/Envisat observations

Spang¹,

Hoffmann²,

Müller³

et al. 2017

Preprint

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Detection and mapping of polar stratospheric clouds using limb scattering observations

Cited by 42 publications

References 24 publications

Chemical ozone losses in Arctic and Antarctic polar winter/spring season derived from SCIAMACHY limb measurements 2002–2009

Chemical ozone losses in Arctic and Antarctic polar winter/spring season derived from SCIAMACHY limb measurements 2002–2009

A climatology of polar stratospheric cloud composition between 2002 and 2012 based on MIPAS/Envisat observations

A climatology of polar stratospheric cloud composition between 2002 and 2012 based on MIPAS/Envisat observations

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