Condensation in aerosol dynamics
Condensation can be summarized as a phase transition from a gas to a liquid as vapor condenses on a pre-existing surface, the exact opposite of the transition from liquid to vapor which occurs in
evaporation. Both condensation and evaporation are happening all the time; atmospheric conditions determine which of them dominates. When the vapor is condensing, the particles on which the vapor condenses will grow bigger, in the same way when vapor evaporates from a particle, it will shrink. This can be seen in the size distribution of aerosol. When the vapor is condensing, then the size distribution moves to bigger sizes: on the contrary, when the vapor is evaporating it moves towards smaller sizes. As the size distribution grows towards bigger or smaller sizes, the airborne mass concentration increases or decreases respectively. In the atmosphere, condensation by for example H2SO4 and organic compounds is the main growth mechanism.
The conditions such as
vapor pressureand temperaturearound the particle determine the dominant process (condensation or evaporation). Following the Kelvineffect (based on the curvature of liquid droplets) smaller particles need a higher ambient relative humidityto maintain equilibrium than bigger ones would. Relative humidity(%) for equilibrium can be determined from the following formula: where "p"s is the saturation vapor pressureabove a particle at equilibrium (around a curved liquid droplet), "p"0 is the saturation vapor pressure (flat surface of the same liquid) and S is the saturation ratio. Kelvin equationfor saturation vapor pressure above a curved surface is: where "p"0 is saturation vapor pressure above a flat surface, "r"p droplet radius, "σ" surface tension of droplet, "ρ" density of liquid, "M" molar mass, "T" temperature, and "R" molar gas constant.
There are three regimes in the aerosol range. The first regime is called the free molecular regime, it contains aerosols with "d"p < 10 nm or "Kn" >> 1. Free molecular regime is characterized by very small particles that has a similar
mean free paththan the surrounding gas and there is a lot of space to travel before colliding to another particle. The mass flux equation in the free molecular regime is: where "a" is the particle radius, "P" are the pressures for from the droplet and at the surface of the droplet respectively, "k"b is the Boltzmann constant, "T" is the temperature, "C"A is mean thermal velocity and "α" is mass accommodation coefficient. It is assumed in the derivation of this equation that the pressure and the diffusion coefficient are constant.
The continuum regime is for bigger particles with "d"p > 200 nm or "Kn" << 1. In this regime, the particles are big enough to "see" their environment as a continuum. The molecular flux in this regime is: where "a" is the radius of the particle A, "M"A is the molecular mass of the particle A, "D"AB is the diffusion coefficient between particles A and B, "R" is the ideal gas constant, "T" is the temperature in kelvins and "P" are the pressures at infinite and at the surface respectively.
The transition regime contains all the particles in between the two preceding regimes (10 nm < "d"p < 200 nm) or "Kn" ≈ 1. The transition regime is situated in between the free molecular and the continuum regime. The semi-empirical equation describing mass flux is: where "I"cont is the mass flux in the continuum regime and "Kn" is the
Knudsen number. This formula is called the Fuchs-Sutugin interpolation formula.
These equations don’t take into account the heat release effect.
Deposition (Aerosol physics)
last = Pruppacher
first = H. R.
coauthors = J. D. Klett
title = Microphysics of Clouds and Precipitation
edition = Second Edition
publisher = Springer
pages = 976
id = ISBN 0-7923-4409-X
last = Seinfeld
first = John
coauthors = Spyros Pandis
title = Atmospheric Chemistry and Physics: From Air Pollution to Climate Change
edition = Second Edition
publisher = John Wiley & Sons, Inc.
date = 2006
location = Hoboken, New Jersey
pages = 1203
id = ISBN 0-471-72018-6
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