Influence of modeling conditions on the estimation of the dry deposition velocity of aerosols on highly inhomogeneous surfaces

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An approach to estimating the dry deposition velocity of aerosol particles on the surfaces of Arctic regions, where snow-covered surfaces, open water surface, tundra and coniferous forest predominate, is proposed and numerically investigated. Optimal modeling conditions are proposed, taking into account the characteristic sizes and densities of aerosol particles involved in transport in the planetary boundary layer, and the interaction of air flows with the surface through the parameter u*, calculated using the WRF-ARW model. The proposed approach is compared with other known models and experimental data. The dependence of the dry deposition velocity obtained by the proposed approach on the diameter, density of aerosol particles and dynamic velocity u* for the surfaces in the Far North is estimated.

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作者简介

D. Pripachkin

IBRAE RAS; NRNU “MEPhI“

编辑信件的主要联系方式.
Email: dmrwer@mail.ru
俄罗斯联邦, 115191, Moscow, Bolshaya Tulskaya str., 52; 115409, Moscow, Kashirskoe Highway, 31

V. Vysotsky

IBRAE RAS

Email: dmrwer@mail.ru
俄罗斯联邦, 115191, Moscow, Bolshaya Tulskaya str., 52

A. Budyka

NRNU “MEPhI“

Email: dmrwer@mail.ru
俄罗斯联邦, 115409, Moscow, Kashirskoe Highway, 31

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2. Fig. 1. The distance X traveled by aerosol particles before they are completely deposited on the surface at wind speeds of 1 m/s, particle density of 2.5 g/cm3 (— 1) and 5 g/cm3 (---2) and 5 m/s, particle density of 2.5 g/cm3 (— 3) and 5 g/cm3 (---4).

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3. Fig. 2. Dependence of the dynamic velocity u* on the roughness parameter z0 in the WRF-ARW model (calculation results (X) and approximation (···) according to formula (2).

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4. Fig. 3. Results of estimating the dry deposition rate Vd of aerosol particles on water (a) and snow-covered surfaces (b), obtained under the following conditions: 2, 4 – calculation using formula (7), 1, 3 – data from [Giardina et al., 2018] at u* = 0.10 and 0.14 m/s, respectively.

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5. Fig. 4. Results of estimating the dry deposition rate Vd of aerosol particles on surfaces covered with vegetation: tundra (a) and coniferous forest (b). 2, 4 – calculation using formula (7); 1, 3 – data from [Giardina et al., 2018] at u* = 0.5 and 1.5 m/s, respectively.

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6. Fig. 5. Dry sedimentation velocity Vd from particle diameter d with changing u* (a) and ρp (b) for a water surface (1, 2 – u* = 0.03 and 0.25 m/s for ρp = 2.5 g/cm3; 3, 4, 5 – ρp = 1, 2.5, 5 g/cm3 for u* = 0.1 m/s).

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7. Fig. 6. Dry deposition velocity Vd from particle diameter d with changing u* (a) and ρp (b) for a surface covered with snow (1, 2 – u* = 0.5 and 0.8 m/s for ρp = 2.5 g/cm3; 3, 4, 5 – ρp = 1, 2.5, 5 g/cm3 for u* = 0.5 m/s).

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8. Fig. 7. Dry sedimentation velocity Vd from particle diameter d with changing u* (a) and ρp (b) for tundra (1, 2 – u* = 0.5 and 1 m/s for ρp = 2.5 g/cm3; 3, 4, 5 – ρp = 1, 2.5, 5 g/cm3 for u* = 0.75 m/s).

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9. Fig. 8. Dry sedimentation velocity Vd from particle diameter d with changing u* (a) and ρp (b) for coniferous forest (1, 2 – u* = 0.8 and 1.5 m/s for ρp = 2.5 g/cm3; 3, 4, 5 – ρp = 1, 2.5, 5 g/cm3 for u* = 1 m/s).

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