The distribution of ozone on Mars as measured by the NOMAD-UVIS spectrometer in Mars year 34.
Authors: Mason Jon , Patel Manish , Holmes James , Streeter Paul , Brown Megan , Sellers Graham , Marriner Charlotte , Lewis Stephen , Wolff Michael , Willame Yannick , Depiesse Cedric , Ristic Bojan , Thomas Ian , Daerden Frank , Vandaele Ann-Carine , López Moreno José Juan , Bellucci Giancarlo 
Published: July 2021

Introduction: The spatial and temporal variation of ozone (O3) is key to understanding ongoing atmospheric processes and transport in the martian atmosphere[1]. As a photochemically active species, O3 has been used to validate the photochemistry of short lived species and, by extension, the water vapour cycle [2,3,4,5] and as a tracer to track the global circulation[6].The Ultraviolet and Visible Spectrometer (UVIS) instrument[7], a channel of the NOMAD spectrometer suite[8], has been in orbit around Mars for over two years with near continuous nadir observations through the latter half of Mars Year(MY) 34 through to MY36. The UVIS observations provide high resolution spatial and temporal maps of O3 column abundance and provides observations at different local times.A retrieval procedure was developed, using spectral measurements over the Hartley band to obtain the O3 column abundances. The radiative transfer simulation is performed using the discrete ordinates DISORT package[9] and we employ the &#8216;front-end&#8217; routines (DISORT_MULTI) developed by Mike Wolff, for studies of the martian atmosphere [1,10,11]Results: In this work we present the geographic and seasonal distribution of O3 in the martian atmosphere as measured by UVIS between LS = 148 and 360&#176; in Mars Year 34 (April 2018 to March 2019). Seasonally the O3 distribution is consistent, with low O3 abundances in equatorial regions and higher O3 abundances at higher latitudes in the winter season. As the martian atmosphere cools through northern spring between Ls&#160;=&#160;350&#176;(MY34) and Ls&#160;=&#160;90&#176;(MY35), due to the reduced solar insolation, we observed a steady increase in equatorial O3, coinciding with the onset of the aphelion cloud belt. The equatorial O3 peaks near the northern winter solstice Ls&#160;=&#160;90&#176;, associated with the cooler and dryer atmosphere of the martian aphelion season before reducing again as the atmosphere warms and more water vapour enters the atmosphere.Ozone entrapment[1] is observed in large impact basins, such as the Hellas Basin and to a lesser extent Argyre Planitia. Ozone abundances measured within Hellas can be an order of magnitude higher than the surrounding regions with abundances of 20 &#181;m-atm observed within Hellas compared to 2-5&#160;&#181;m-atm in the surrounding area at aphelion. Ozone entrapment is still observed during the perihelion season, with abundances within Hellas being 5-10&#160;&#181;m-atm.The UVIS dataset provides comprehensive seasonal coverage between latitudes ~74&#176;&#160;N and 74&#176;&#160;S and samples multiple local times at a giving location enabling unprecedented detail in the O3 diurnal cycle.References:[1] Clancy, R. T, et al. Icarus 266 (2016). [2] Lef&#232;vre, F, et al. Nature 454.7207 (2008). [3] Montmessin, F and Lef&#232;vre, F. Nature Geoscience 6.11 (2013). [4] Holmes, J,A. et al. Icarus 302 (2018). [5] Daerden, F., et al. Icarus 326 (2019). [6] Holmes, J,A. et al. Icarus 282 (2017). [7] Patel, M, R., et al. &#160;Applied Optics 56.10 (2017). [8] Neefs, Eddy, et al. Applied Optics 54.28 (2015). [9] Stamnes, Knut, et al. Applied Optics 27.12 (1988). [10] Wolff, M, J., et al. Icarus 208.1 (2010). [11] Wolff, M, J., et al. &#160;Icarus 332 (2019).