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Volume 18, issue 3
Atmos. Chem. Phys., 18, 1507–1534, 2018
https://doi.org/10.5194/acp-18-1507-2018
© Author(s) 2018. This work is distributed under
the Creative Commons Attribution 3.0 License.
Atmos. Chem. Phys., 18, 1507–1534, 2018
https://doi.org/10.5194/acp-18-1507-2018
© Author(s) 2018. This work is distributed under
the Creative Commons Attribution 3.0 License.

Research article 02 Feb 2018

Research article | 02 Feb 2018

Modelling the physical multiphase interactions of HNO3 between snow and air on the Antarctic Plateau (Dome C) and coast (Halley)

Hoi Ga Chan1,2, Markus M. Frey1, and Martin D. King2 Hoi Ga Chan et al.
  • 1British Antarctic Survey, Natural Environment Research Council, Cambridge, CB3 0ET, UK
  • 2Department of Earth Sciences, Royal Holloway University of London, Egham, Surrey, TW20 0EX, UK

Abstract. Emissions of nitrogen oxide (NOx  =  NO + NO2) from the photolysis of nitrate (NO3) in snow affect the oxidising capacity of the lower troposphere especially in remote regions of high latitudes with little pollution. Current air–snow exchange models are limited by poor understanding of processes and often require unphysical tuning parameters. Here, two multiphase models were developed from physically based parameterisations to describe the interaction of nitrate between the surface layer of the snowpack and the overlying atmosphere. The first model is similar to previous approaches and assumes that below a threshold temperature, To, the air–snow grain interface is pure ice and above To a disordered interface (DI) emerges covering the entire grain surface. The second model assumes that air–ice interactions dominate over all temperatures below melting of ice and that any liquid present above the eutectic temperature is concentrated in micropockets. The models are used to predict the nitrate in surface snow constrained by year-round observations of mixing ratios of nitric acid in air at a cold site on the Antarctic Plateau (Dome C; 75°06′ S, 123°33′ E; 3233 m a.s.l.) and at a relatively warm site on the Antarctic coast (Halley; 75°35′ S, 26°39′ E; 35 m a.s.l). The first model agrees reasonably well with observations at Dome C (Cv(RMSE)  =  1.34) but performs poorly at Halley (Cv(RMSE)  =  89.28) while the second model reproduces with good agreement observations at both sites (Cv(RMSE)  =  0.84 at both sites). It is therefore suggested that in winter air–snow interactions of nitrate are determined by non-equilibrium surface adsorption and co-condensation on ice coupled with solid-state diffusion inside the grain, similar to Bock et al. (2016). In summer, however, the air–snow exchange of nitrate is mainly driven by solvation into liquid micropockets following Henry's law with contributions to total surface snow NO3 concentrations of 75 and 80 % at Dome C and Halley, respectively. It is also found that the liquid volume of the snow grain and air–micropocket partitioning of HNO3 are sensitive to both the total solute concentration of mineral ions within the snow and pH of the snow. The second model provides an alternative method to predict nitrate concentration in the surface snow layer which is applicable over the entire range of environmental conditions typical for Antarctica and forms a basis for a future full 1-D snowpack model as well as parameterisations in regional or global atmospheric chemistry models.

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Emissions of reactive nitrogen from snowpacks influence remote air quality. Two physical air–snow models for nitrate were developed. One assumes that below a threshold temperature the air–snow grain interface is pure ice and above it a disordered interface emerges. The other assumes an air–ice interface below melting and that any liquid present is concentrated in micropockets. Only the latter matches observations at two Antarctic lcoations covering a wide range of environmental conditions.
Emissions of reactive nitrogen from snowpacks influence remote air quality. Two physical...
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