Simple model for estimating dry deposition velocity of ozone and its destruction in a polluted nocturnal boundary layer

2010 ◽  
Vol 44 (35) ◽  
pp. 4364-4371 ◽  
Author(s):  
Ching-Ho Lin ◽  
Chin-Hsing Lai ◽  
Yee-Lin Wu ◽  
Ming-Jen Chen
Keyword(s):  
Boundary Layer ◽  
Simple Model ◽  
Dry Deposition ◽  
Deposition Velocity ◽  
Nocturnal Boundary Layer ◽  
Dry Deposition Velocity

Determining PM2.5 dry deposition velocity on plant leaves: An indirect experimental method

2019 ◽  
Vol 46 ◽  
pp. 126467 ◽  
Author(s):  
Shan Yin ◽  
Xuyi Zhang ◽  
Annie Yu ◽  
Ningxiao Sun ◽  
Junyao Lyu ◽  
...  
Keyword(s):  
Experimental Method ◽  
Dry Deposition ◽  
Deposition Velocity ◽  
Plant Leaves ◽  
Dry Deposition Velocity

scholarly journals Aerosol dry deposition measured with eddy-covariance technique at Wasa and Aboa, DronningMaud Land, Antarctica

2002 ◽  
Vol 35 ◽  
pp. 355-361 ◽  
Author(s):  
Anna Grönlund ◽  
Douglas Nilsson ◽  
Ismo K. Koponen ◽  
Aki Virkkula ◽  
Margareta E. Hansson
Keyword(s):  
Eddy Covariance ◽  
Dry Deposition ◽  
Transfer Functions ◽  
Deposition Velocity ◽  
Ice Core ◽  
Brownian Diffusion ◽  
Wind Component ◽  
Surface Boundary ◽  
Surface Boundary Layer ◽  
Dry Deposition Velocity

AbstractInterpretation of ice-core records in terms of changes in atmospheric concentrations requires understanding of the various parameters within air–snow transfer functions. the dry-deposition velocity is one of these parameters, dependent on local meteorological conditions and thereby also affected by climate changes. We have determined aerosol dry-deposition velocities by measurements of aerosol particle-number concentration and the vertical wind component with an eddy-covariance system close to the Swedish and Finnish research stations Wasa and Aboa in Dronning Maud Land, Antarctica. Measurements were performed over a smooth, snow-covered area and over moderately rough, rocky ground during 4 and 19 days, respectively, in January 2000. the median dry-deposition velocity determined 5.25 mabove the surface was 0.33 and 0.80 cm s–1, respectively. the large difference between the two sites was mainly due to the stratification of the surface boundary layer, the surface albedo and the surface roughness height. the dry-deposition number fluxes were dominated by the particle-size modes defined as ultrafine and Aitken, withmean diameters around 14 and 42 nm, respectively. A larger dry-deposition velocity, owing to stronger Brownian diffusion, for the smaller ultrafine mode was verified by the measurements.

scholarly journals Chemistry, transport and dry deposition of trace gases in the boundary layer over the tropical Atlantic Ocean and the Guyanas during the GABRIEL field campaign

2007 ◽  
Vol 7 (14) ◽  
pp. 3933-3956 ◽  
Author(s):  
A. Stickler ◽  
H. Fischer ◽  
H. Bozem ◽  
C. Gurk ◽  
C. Schiller ◽  
...  
Keyword(s):  
Boundary Layer ◽  
Atlantic Ocean ◽  
Dry Deposition ◽  
Deposition Velocity ◽  
Ozone Production ◽  
Organic Peroxides ◽  
Tropical Atlantic ◽  
Model Calculations ◽  
Tropical Atlantic Ocean ◽  
Positive Tendency

Abstract. We present a comparison of different Lagrangian and chemical box model calculations with measurement data obtained during the GABRIEL campaign over the tropical Atlantic Ocean and the Amazon rainforest in the Guyanas, October 2005. Lagrangian modelling of boundary layer (BL) air constrained by measurements is used to derive a horizontal gradient (≈5.6 pmol/mol km−1) of CO from the ocean to the rainforest (east to west). This is significantly smaller than that derived from the measurements (16–48 pmol/mol km−1), indicating that photochemical production from organic precursors alone cannot explain the observed strong gradient. It appears that HCHO is overestimated by the Lagrangian and chemical box models, which include dry deposition but not exchange with the free troposphere (FT). The relatively short lifetime of HCHO implies substantial BL-FT exchange. The mixing-in of FT air affected by African and South American biomass burning at an estimated rate of 0.12 h−1 increases the CO and decreases the HCHO mixing ratios, improving agreement with measurements. A mean deposition velocity of 1.35 cm/s for H2O2 over the ocean as well as over the rainforest is deduced assuming BL-FT exchange adequate to the results for CO. The measured increase of the organic peroxides from the ocean to the rainforest (≈0.66 nmol/mol d−1) is significantly overestimated by the Lagrangian model, even when using high values for the deposition velocity and the entrainment rate. Our results point at either heterogeneous loss of organic peroxides and/or their radical precursors, underestimated photodissociation or missing reaction paths of peroxy radicals not forming peroxides in isoprene chemistry. We calculate a mean integrated daytime net ozone production (NOP) in the BL of (0.2±5.9) nmol/mol (ocean) and (2.4±2.1) nmol/mol (rainforest). The NOP strongly correlates with NO and has a positive tendency in the boundary layer over the rainforest.

scholarly journals Chemistry, transport and dry deposition of trace gases in the boundary layer over the tropical Atlantic Ocean and the Guyanas during the GABRIEL field campaign

2007 ◽  
Vol 7 (2) ◽  
pp. 4781-4855 ◽  
Author(s):  
A. Stickler ◽  
H. Fischer ◽  
H. Bozem ◽  
C. Gurk ◽  
C. Schiller ◽  
...  
Keyword(s):  
Boundary Layer ◽  
Steady State ◽  
Atlantic Ocean ◽  
Dry Deposition ◽  
Trace Gases ◽  
Deposition Velocity ◽  
Organic Peroxides ◽  
Tropical Atlantic ◽  
Tropical Atlantic Ocean ◽  
Positive Tendency

Abstract. We present a comparison of different Lagrangian and steady state box model runs with measurement data obtained during the GABRIEL campaign over the tropical Atlantic Ocean and the rainforest in the Guyanas, October 2005. Lagrangian modelling of boundary layer (BL) CO constrained by measurements of reactive trace gases and radiation is used to derive a horizontal gradient (≈5.6 pmol/mol km−1) of this compound from the ocean to the rainforest (east to west). This is significantly smaller than that derived from the measurements (16–48 pmol/mol km−1), indicating that photochemical production from organic precursors alone cannot explain the observed strong gradient. It appears that HCHO is overestimated by the Lagrangian and "steady state" models, which include dry deposition but not exchange with the free troposphere (FT). The relatively short lifetime of HCHO (50–100 min) implies substantial BL-FT exchange. The mixing-in of FT air affected by African and South American biomass burning at an estimated rate of 0.12 h−1 increases the CO and lowers the HCHO mixing ratios, leading to a better agreement with measurements. A 24 h mean deposition velocity of 1.35 cm/s for H2O2 over the ocean as well as over the rainforest is deduced assuming BL-FT exchange adequate to the results for CO. The measured increase of the organic peroxides from the ocean to the rainforest (≈0.66 nmol/mol d−1) is significantly overestimated by the Lagrangian model, even when using high values for the deposition velocity and the entrainment rate. Our results point at either heterogeneous loss of organic peroxides and/or their radical precursors or a missing reaction path of peroxy radicals not forming peroxides in isoprene chemistry. We calculate a mean integrated daytime net ozone production (NOP) in the BL of (0.2±5.9) nmol/mol (ocean) and (2.4±2.1) nmol/mol (rainforest). The NOP strongly correlates with NO and shows a positive tendency in the boundary layer over the rainforest.

Sign in / Sign up

Export Citation Format

Share Document