Modeling sea‐salt aerosols in the atmosphere: 1. Model development

Gong, Sunling; Barrie, L. A.; Blanchet, Jean‐Pierre

doi:10.1029/96jd02953

Cited by 456 publications

(323 citation statements)

References 48 publications

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“…[31] In large-scale models, MH86 has been extrapolated beyond its range of validity [e.g., Gong et al, 1997;Lohmann et al, 2000]. Figure 11 shows that the extrapolated MH86 flux increases monotonously with decreasing D p below 0.9 mm, and as expected, the size spectra observed in the laboratory study as well in the field measurements (compare Figure 4) are not reproduced.…”

Section: Comparison With Field Measurements and Other Flux Parameterimentioning

confidence: 70%

Laboratory simulations and parameterization of the primary marine aerosol production

et al. 2003

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[1] A major source of the primary marine aerosol is the bursting of air bubbles produced by breaking waves. Several source parameterizations are available from the literature, usually limited to particles with a dry diameter D p > 1 mm. The objective of this work is to extend the current knowledge to submicrometer particles. Bubbles were generated in synthetic seawater using a sintered glass filter, with a size spectra that are only partly the same spectra as measured in the field. Bubble spectra, and size distributions of the resulting aerosol (0.020-20.0 mm D p ) of the resulting aerosol, were measured for different salinity, water temperature (T w ), and bubble flux. The spectra show a minimum at $1 mm D p , which separates two modes, one at $0.1 mm, with the largest number of particles, and one at 2.5 mm D p . The modes show different behavior with the variation of salinity and water temperature. When the water temperature increases, the number concentration N p decreases for D p < 0.07 mm, whereas for D p > 0.35 mm, N p increases. The salinity effect suggests different droplet formation processes for droplets smaller and larger than 0.2 mm D p . The number of particles produced per size increment, time unit, and whitecap surface (È) is described as a linear function of T w and a polynomial function of D p . Combining È with the whitecap coverage fraction W (in percent), an expression results for the primary marine aerosol source flux dF 0 /dlogD p = W È (m À2 s À1 ). The results are compared with other commonly used formulations as well as with recent field observations. Implications for aerosol-induced effects on climate are discussed.

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Section: Comparison With Field Measurements and Other Flux Parameterimentioning

confidence: 70%

Laboratory simulations and parameterization of the primary marine aerosol production

et al. 2003

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“…Many current global climate models do not yet have this capability. A second advantage of our approach is that small changes to ice number concentrations and to radiative forcing are not subject to variations associated with weather variations as would occur if the changes Gong et al (1997) to ice number concentrations were allowed to change the cloud fields through changes in ice sedimentation rates and other processes. Thus, the difference in forcing associated with different aerosol emissions are all statistically significant, even if the calculations are only carried out for a single year.…”

Section: Methodsmentioning

confidence: 99%

“…The first simulation uses pre-industrial (≈1870) emissions of aerosol particles and aerosol precursors. These include natural (Kettle and Andreae, 2000; Andres and Kasgnoc, 1998) and anthropogenic (Smith, et al, 2001(Smith, et al, , 2004 emissions of sulfur and soot from surface sources of biomass burning and fossil fuels (Ito and Penner, 2005), natural organic matter emissions based on a 9% conversion rate of the terpene carbon emissions from Guenther et al (2001) to organic matter (Penner et al, 2001), dust particles for the year 2000 (P. Ginoux, personal communication, 2004) generated using the algorithm of Ginoux et al (2001), and sea salt emissions generated internally in the model using the method of Gong et al (1997). The second uses natural and anthropogenic particle and precursor emissions for the present day (≈2000) for anthropogenic sulfur, anthropogenic soot from surface sources, and aircraft-generated soot.…”

Section: Methodsmentioning

confidence: 99%

Possible influence of anthropogenic aerosols on cirrus clouds and anthropogenic forcing

et al. 2009

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Abstract. Cirrus clouds have a net warming effect on the atmosphere and cover about 30% of the Earth's area. Aerosol particles initiate ice formation in the upper troposphere through modes of action that include homogeneous freezing of solution droplets, heterogeneous nucleation on solid particles immersed in a solution, and deposition nucleation of vapor onto solid particles. Here, we examine the possible change in ice number concentration from anthropogenic soot originating from surface sources of fossil fuel and biomass burning, from anthropogenic sulfate aerosols, and from aircraft that deposit their aerosols directly in the upper troposphere. We use a version of the aerosol model that predicts sulfate number and mass concentrations in 3-modes and includes the formation of sulfate aerosol through homogeneous binary nucleation as well as a version that only predicts sulfate mass. The 3-mode version best represents the Aitken aerosol nuclei number concentrations in the upper troposphere which dominated ice crystal residues in the upper troposphere. Fossil fuel and biomass burning soot aerosols with this version exert a radiative forcing of −0.3 to −0.4 Wm −2 while anthropogenic sulfate aerosols and aircraft aerosols exert a forcing of −0.01 to 0.04 Wm −2 and −0.16 to −0.12 Wm −2 , respectively, where the range represents the forcing from two parameterizations for ice nucleation. The sign of the forcing in the mass-only version of the model depends on which ice nucleation parameterization is used and can be either positive or negative. The magnitude of Correspondence to: J. E. Penner (penner@umich.edu) the forcing in cirrus clouds can be comparable to the forcing exerted by anthropogenic aerosols on warm clouds, but this forcing has not been included in past assessments of the total anthropogenic radiative forcing of climate.

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“…Gong et al, 1997;Grini et al, 2002;Pryor and Sorensen, 2000) used the parameterization that was developed by Monahan et al (1986). This parameterization is based on laboratory measurements and is generally limited to particles with radius bigger than 0.8 µm at a relative humidity of 80%.…”

Section: Sea Salt Aerosol Productionmentioning

confidence: 99%

Modelling sea salt aerosol and its direct and indirect effects on climate

Salzen

2008

Atmos. Chem. Phys.

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Abstract.A size-dependent sea salt aerosol parameterization was developed based on the piecewise log-normal approximation (PLA) for aerosol size distributions. Results of this parameterization from simulations with a global climate model produce good agreement with observations at the surface and for vertically-integrated volume size distributions. The global and annual mean of the sea salt burden is 10.1 mg m −2 . The direct radiative forcing is calculated to be −1.52 and −0.60 W m −2 for clear sky and all sky, respectively. The first indirect radiative forcing is about twice as large as the direct forcing for all-sky (−1.34 W m −2 ). The results also show that the total indirect forcing of sea salt is −2.9 W m −2 if climatic feedbacks are taken into account. The sensitivity of the forcings to changes in the burdens and sizes of sea salt particles was also investigated based on additional simulations with a different sea salt source function.

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Modeling sea‐salt aerosols in the atmosphere: 1. Model development

Abstract: Physical ModelThe fate of sea-salt aerosols, once they are injected into the atmosphere from the ocean source, is governed by a series of physical processes such as transport, coagulation, dry and wet removal, and chemical transformation. Transport of aerosols is 3805

Cited by 456 publications

References 48 publications

Laboratory simulations and parameterization of the primary marine aerosol production

Laboratory simulations and parameterization of the primary marine aerosol production

Possible influence of anthropogenic aerosols on cirrus clouds and anthropogenic forcing

Modelling sea salt aerosol and its direct and indirect effects on climate

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