Partitioning between the inorganic chlorine reservoirs HCl and ClONO&amp;lt;sub&amp;gt;2&amp;lt;/sub&amp;gt; during the Arctic winter 2005 from the ACE-FTS

Dufour, G.; Nassar, Ray; Boone, C. D.; Skelton, R.; Walker, Kaley A.; Bernath, P. F.; Rinsland, C. P.; Semeniuk, K.; Jin, J. J.; McConnell, J. C.; Manney, G. L.

doi:10.5194/acp-6-2355-2006

Cited by 28 publications

(13 citation statements)

References 36 publications

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“…This winter was chosen, because it was characterized by an unusually large catalytic ozone loss as documented in numerous studies (e.g., Dufour et al, 2006;Grooß and Müller, 2007;Singleton et al, 2007Singleton et al, , 2005Rösevall et al, 2008;Rex et al, 2006). Comparison with previous studies for the other winters will be described later in this section.…”

Section: Arctic Wintersmentioning

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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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: Arctic Wintersmentioning

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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“…Hence, by the end of Arctic winter, high values of more than 2 ppbv ClONO 2 have been measured (see, e.g., Dufour et al, 2006;Höpfner et al, 2007;Wetzel et al, 2010).…”

Section: G Wetzel Et Al: Diurnal Variations Of Reactive Chlorine Anmentioning

confidence: 99%

“…8. ClONO 2 values of up to 1.5 ppbv, which are not unusual for mid-winter conditions (Dufour et al, 2006), were measured at 27 km. However, below 25 km ClONO 2 mixing ratios fall to values below 0.1 ppbv, coincident with the region of high ClO x amounts.…”

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confidence: 99%

Diurnal variations of reactive chlorine and nitrogen oxides observed by MIPAS-B inside the January 2010 Arctic vortex

et al. 2012

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Abstract. The winter 2009/2010 was characterized by a strong Arctic vortex with extremely cold mid-winter temperatures in the lower stratosphere associated with an intense activation of reactive chlorine compounds (ClO x ) from reservoir species. Stratospheric limb emission spectra were recorded during a flight of the balloon version of the Michelson Interferometer for Passive Atmospheric Sounding (MIPAS-B) from Kiruna (Sweden) on 24 January 2010 inside the Arctic vortex. Several fast limb sequences of spectra (in time steps of about 10 min) were measured from nighttime photochemical equilibrium to local noon allowing the retrieval of chlorine-and nitrogen-containing species which change rapidly their concentration around the terminator between night and day. Mixing ratios of species like ClO, NO 2 , and N 2 O 5 show significant changes around sunrise, which are temporally delayed due to polar stratospheric clouds reducing the direct radiative flux from the sun. ClO variations were derived for the first time from MIPAS-B spectra. Daytime ClO values of up to 1.6 ppbv are visible in a broad chlorine activated layer below 26 km correlated with low values (below 0.1 ppbv) of the chlorine reservoir species ClONO 2 . Observations are compared and discussed with calculations performed with the 3-dimensional Chemistry Climate Model EMAC (ECHAM5/MESSy Atmospheric Chemistry). Mixing ratios of the species ClO, NO 2 , and N 2 O 5 are well reproduced by the model during night and noon. However, the onset of ClO production and NO 2 loss around the terminator in the model is not consistent with the measurements. The MIPAS-B observations along with Tropospheric UltravioletVisible (TUV) radiation model calculations suggest that polar stratospheric clouds lead to a delayed start followed by a faster increase of the photodissoziation of ClOOCl and NO 2 near the morning terminator since stratospheric clouds alter the direct and the diffuse flux of solar radiation. These effects are not considered in the EMAC model simulations which assume a cloudless atmosphere.

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“…The fitting error of the ClONO 2 data is below 10 % at 20-30 km and increases to 40 % at 14 km . Dufour et al (2006) have provided an error budget for a single occultation: the total errors for HCl and ClONO 2 are, respectively, estimated to be 4-7 % and 10-19 % between 16.5 km and 28.5 km. et al, 2009, 2013).…”

Section: Ace-ftsmentioning

confidence: 99%

“…An aircraft mission was performed in the 1999/2000 Arctic winter; the time evolution of the Cl y species has been investigated (e.g., Wilmouth et al, 2006). Dufour et al (2006) also showed an evolution of the Cl y partitioning in the 2004/2005 Arctic winter from the Atmospheric Chemistry Experiment-Fourier Transform Spectrometer (ACE-FTS) measurements. However, the HCl value or HCl / Cl y ratio in the Arctic was lower than those in the Antarctic (e.g., Santee et al, 2008b;Manney et al, 2011;Wegner et al, 2012), even with severe ozone loss in the 2010/2011 Arctic winter (e.g., Manney et al, 2011).…”

Section: Introductionmentioning

confidence: 99%

HCl and ClO profiles inside the Antarctic vortex as observed by SMILES in November 2009: comparisons with MLS and ACE-FTS instruments

et al. 2013

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Abstract. We present vertical profiles of hydrogen chloride (HCl) and chlorine monoxide (ClO) as observed by the Superconducting Submillimeter-Wave Limb-Emission Sounder (SMILES) on the International Space Station (ISS) inside the Antarctic vortex on 19-24 November 2009. The SMILES HCl value reveals 2.8-3.1 ppbv between 450 K and 500 K levels in potential temperature (PT). The high value of HCl is highlighted since it is suggested that HCl is a main component of the total inorganic chlorine (Cl y ), defined as Cl y HCl + ClO + chlorine nitrate (ClONO 2 ), inside the Antarctic vortex in spring, owing to low ozone values. To confirm the quality of two SMILES level 2 (L2) data products provided by the Japan Aerospace Exploration Agency (JAXA) and Japan's National Institute of Information and Communications Technology (NICT), vis-à-vis the partitioning of Cl y , comparisons are made using other satellite data from the Aura Microwave Limb Sounder (MLS) and Atmospheric Chemistry Experiment Fourier Transform Spectrometer (ACE-FTS). HCl values from the SMILES NICT L2 product agree to within 10 % (0.3 ppbv) with the MLS HCl data between 450 and 575 K levels in PT and with the ACE-FTS HCl data between 425 and 575 K. The SMILES JAXA L2 product is 10 to 20 % (0.2-0.5 ppbv) lower than that from MLS between 400 and 700 K and from ACE-FTS between 500 and 700 K. For ClO in daytime, the difference between SMILES (JAXA and NICT) and MLS is less than ±0.05 ppbv (100 %) between 500 K and 650 K with the ClO values less than 0.2 ppbv. ClONO 2 values as measured by ACE-FTS also reveal 0.2 ppbv at 475-500 K level, resulting in the HCl / Cl y ratios of 0.91-0.95. The HCl / Cl y ratios derived from each retrieval agree to within −5 to 8 % with regard to their averages. The high HCl values and HCl / Cl y ratios observed by the three instruments in the lower stratospheric Antarctic vortex are consistent with previous observations in late Austral spring.

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Partitioning between the inorganic chlorine reservoirs HCl and ClONO<sub>2</sub> during the Arctic winter 2005 from the ACE-FTS

Cited by 28 publications

References 36 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

Diurnal variations of reactive chlorine and nitrogen oxides observed by MIPAS-B inside the January 2010 Arctic vortex

HCl and ClO profiles inside the Antarctic vortex as observed by SMILES in November 2009: comparisons with MLS and ACE-FTS instruments

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