Aerosol

Not to be confused withaerosil.

This article is about a suspension of particulates in a gas. For details on atmospheric particulate matter, seeparticulates.

For the spray can, seeAerosol spray dispenser.

Mistandfogare aerosols

Anaerosolis asuspensionof finesolidparticlesorliquiddropletsinairor anothergas.Aerosols can be generated from natural orhuman causes.The termaerosolcommonly refers to the mixture ofparticulatesin air, and not to the particulate matter alone.Examples of natural aerosols arefog,mistordust.Examples of human caused aerosols includeparticulateair pollutants,mist from the discharge athydroelectric dams,irrigation mist,perfume from atomizers,smoke,dust,sprayed pesticides,and medical treatments for respiratory illnesses.

Several types of atmospheric aerosol have a significant effect on Earth's climate: volcanic, desert dust, sea-salt, that originating from biogenic sources and human-made. Volcanic aerosol forms in the stratosphere after an eruption as droplets ofsulfuric acidthat can prevail for up to two years, and reflect sunlight, lowering temperature. Desert dust, mineral particles blown to high altitudes, absorb heat and may be responsible for inhibiting storm cloud formation. Human-madesulfate aerosols,primarily from burning oil and coal, affect the behavior of clouds.When aerosols absorb pollutants, it facilitates the deposition of pollutants to the surface of the earth as well as to bodies of water.This has the potential to be damaging to both the environment and human health.

Ship tracksarecloudsthat form around theexhaustreleased by ships into the still ocean air. Watermoleculescollect around the tiny particles (aerosols) from exhaust to form acloud seed.More and more water accumulates on the seed until a visible cloud is formed. In the case of ship tracks, the cloud seeds are stretched over a long narrow path where the wind has blown the ship's exhaust, so the resulting clouds resemble long strings over the ocean.

The warming caused by human-produced greenhouse gases has been somewhat offset by the cooling effect of human-produced aerosols. In 2020, regulations on fuel significantly cut sulfur dioxide emissions from international shipping by approximately 80%, leading to an unexpected global geoengineering termination shock.

The liquid or solid particles in an aerosol have diameters typically less than1 μm.Larger particles with a significant settling speed make the mixture asuspension,but the distinction is not clear. In everyday language,aerosoloften refers to adispensing systemthat delivers a consumer product from aspray can.

Diseases can spreadby means of small droplets in thebreath,sometimes calledbioaerosols.

Definitions

See also:Particulates

Photomicrographmade with a Scanning Electron Microscope (SEM):Fly ashparticles at 2,000× magnification. Most of the particles in this aerosol are nearly spherical.

Aerosol spray can

Aerosol is defined as a suspension system of solid or liquid particles in a gas. An aerosol includes both the particles and the suspending gas, which is usually air.Meteorologists usually refer to them as particle matter - PM2.5 or PM10, depending on their size.Frederick G. Donnanpresumably first used the termaerosolduringWorld War Ito describe an aero-solution,clouds of microscopic particles in air. This term developed analogously to the termhydrosol,acolloidsystem with water as the dispersed medium.Primary aerosolscontain particles introduced directly into the gas;secondary aerosolsform through gas-to-particle conversion.

Key aerosol groups include sulfates, organic carbon, black carbon, nitrates, mineral dust, and sea salt, they usually clump together to form a complex mixture.Various types of aerosol, classified according to physical form and how they were generated, include dust, fume, mist, smoke and fog.

There are several measures of aerosol concentration.Environmental scienceandenvironmental healthoften use themass concentration(M), defined as the mass of particulate matter per unit volume, in units such as μg/m³.Also commonly used is thenumber concentration(N), the number of particles per unit volume, in units such as number per m³or number per cm³.

Particle size has a major influence on particle properties, and the aerosol particle radius or diameter (d_p) is a key property used to characterise aerosols.

Aerosols vary in theirdispersity.Amonodisperseaerosol, producible in the laboratory, contains particles of uniform size. Most aerosols, however, aspolydispersecolloidal systems, exhibit a range of particle sizes.Liquid droplets are almost always nearly spherical, but scientists use anequivalent diameterto characterize the properties of various shapes of solid particles, some very irregular. The equivalent diameter is the diameter of a spherical particle with the same value of some physical property as the irregular particle.Theequivalent volume diameter(d_e) is defined as the diameter of a sphere of the same volume as that of the irregular particle.Also commonly used is theaerodynamic diameter,d_a.

Generation and applications

People generate aerosols for various purposes, including:

• as test aerosols forcalibratinginstruments, performing research, and testing sampling equipment and air filters;
• to deliverdeodorants,paints,and other consumer products in sprays;
• for dispersal and agricultural application
• for medical treatment ofrespiratory disease;and
• infuel injectionsystems and othercombustiontechnology.

Some devices for generating aerosols are:

• Aerosol spray
• Atomizer nozzleornebulizer
• Electrospray
• Electronic cigarette
• Vibrating orifice aerosol generator (VOAG)

In the atmosphere

Aerosol pollution over northernIndiaandBangladesh

Overview of large clouds of aerosols around Earth (green: smoke, blue: salt, yellow: dust, white: sulfuric)

Main article:Particulates

Several types of atmospheric aerosol have a significant effect on Earth's climate: volcanic, desert dust, sea-salt, that originating from biogenic sources and human-made. Volcanic aerosol forms in the stratosphere after an eruption as droplets ofsulfuric acidthat can prevail for up to two years, and reflect sunlight, lowering temperature. Desert dust, mineral particles blown to high altitudes, absorb heat and may be responsible for inhibiting storm cloud formation. Human-madesulfate aerosols,primarily from burning oil and coal, affect the behavior of clouds.

Although allhydrometeors,solid and liquid, can be described as aerosols, a distinction is commonly made between such dispersions (i.e. clouds) containing activated drops and crystals, and aerosol particles. Theatmosphere of Earthcontains aerosols of various types and concentrations, including quantities of:

• naturalinorganicmaterials: fine dust, sea salt, or water droplets
• naturalorganicmaterials: smoke,pollen,spores,orbacteria
• anthropogenicproducts of combustion such as: smoke,ashesor dusts

Aerosols can be found in urbanecosystemsin various forms, for example:

• Dust
• Cigarette smoke
• Mist fromaerosol spraycans
• Sootor fumes in car exhaust

The presence of aerosols in the Earth's atmosphere can influence its climate, as well as human health.

Effects

See also:Particulates § Climate effects

Aerosols have a cooling effect that is small compared to the radiative forcing (warming effect) of greenhouse gases.

Volcanic eruptions release large amounts ofsulphuric acid,hydrogen sulfideandhydrochloric acidinto the atmosphere. These gases represent aerosols and eventually return to earth asacid rain,having a number ofadverse effectson the environment and human life.

When aerosols absorb pollutants, it facilitates the deposition of pollutants to the surface of the earth as well as to bodies of water.This has the potential to be damaging to both the environment and human health.

Aerosols interact with theEarth's energy budgetin two ways, directly and indirectly.

• E.g., adirecteffect is that aerosols scatter and absorb incoming solar radiation.This will mainly lead to a cooling of the surface (solar radiation is scattered back to space) but may also contribute to a warming of the surface (caused by the absorption of incoming solar energy).This will be an additional element to thegreenhouse effectand therefore contributing to the global climate change.
• Theindirecteffects refer to the aerosol interfering with formations that interact directly with radiation. For example, they are able to modify the size of the cloud particles in the lower atmosphere, thereby changing the way clouds reflect and absorb light and therefore modifying the Earth's energy budget.
• There is evidence to suggest that anthropogenic aerosols actually offset the effects of greenhouse gases in some areas, which is why the Northern Hemisphere shows slower surface warming than the Southern Hemisphere, although that just means that the Northern Hemisphere will absorb the heat later through ocean currents bringing warmer waters from the South.On a global scale however, aerosol cooling decreases greenhouse-gases-induced heating without offsetting it completely.

Ship tracksarecloudsthat form around theexhaustreleased by ships into the still ocean air. Watermoleculescollect around the tiny particles (aerosols) from exhaust to form acloud seed.More and more water accumulates on the seed until a visible cloud is formed. In the case of ship tracks, the cloud seeds are stretched over a long narrow path where the wind has blown the ship's exhaust, so the resulting clouds resemble long strings over the ocean.

The warming caused by human-produced greenhouse gases has been somewhat offset by the cooling effect of human-produced aerosols. In 2020, regulations on fuel significantly cut sulfur dioxide emissions from international shipping by approximately 80%, leading to an unexpected global geoengineering termination shock.

Aerosols in the 20 μm range show a particularly long persistence time in air conditioned rooms due to their "jet rider" behaviour (move with air jets, gravitationally fall out in slowly moving air);as this aerosol size is most effectively adsorbed in the human nose,the primordial infection site inCOVID-19,such aerosols may contribute to the pandemic.

Aerosol particles with an effective diameter smaller than 10 μm can enter the bronchi, while the ones with an effective diameter smaller than 2.5 μm can enter as far as the gas exchange region in the lungs,which can be hazardous to human health.

Size distribution

See also:Particulates § Size, shape, and solubility matter

The same hypothetical log-normal aerosol distribution plotted, from top to bottom, as a number vs. diameter distribution, a surface area vs. diameter distribution, and a volume vs. diameter distribution. Typical mode names are shown at the top. Each distribution is normalized so that the total area is 1000.

For a monodisperse aerosol, a single number—the particle diameter—suffices to describe the size of the particles. However, more complicatedparticle-size distributionsdescribe the sizes of the particles in a polydisperse aerosol. This distribution defines the relative amounts of particles, sorted according to size.One approach to defining the particle size distribution uses a list of the sizes of every particle in a sample. However, this approach proves tedious to ascertain in aerosols with millions of particles and awkward to use. Another approach splits the size range into intervals and finds the number (or proportion) of particles in each interval. These data can be presented in ahistogramwith the area of each bar representing the proportion of particles in that size bin, usually normalised by dividing the number of particles in a bin by the width of the interval so that the area of each bar is proportionate to the number of particles in the size range that it represents.If the width of the binstends to zero,the frequency function is:

$\mathrm {d} f=f(d_{p})\,\mathrm {d} d_{p}$

where

$d_{p}$is the diameter of the particles

$\,\mathrm {d} f$is the fraction of particles having diameters between$d_{p}$and$d_{p}$+$\mathrm {d} d_{p}$

$f(d_{p})$is the frequency function

Therefore, the area under the frequency curve between two sizes a andbrepresents the total fraction of the particles in that size range:

$f_{ab}=\int _{a}^{b}f(d_{p})\,\mathrm {d} d_{p}$

It can also be formulated in terms of the total number densityN:

$dN=N(d_{p})\,\mathrm {d} d_{p}$

Assuming spherical aerosol particles, the aerosol surface area per unit volume (S) is given by the secondmoment:

$S=\pi /2\int _{0}^{\infty }N(d_{p})d_{p}^{2}\,\mathrm {d} d_{p}$

And the third moment gives the total volume concentration (V) of the particles:

$V=\pi /6\int _{0}^{\infty }N(d_{p})d_{p}^{3}\,\mathrm {d} d_{p}$

The particle size distribution can be approximated. Thenormal distributionusually does not suitably describe particle size distributions in aerosols because of theskewnessassociated with along tailof larger particles. Also for a quantity that varies over a large range, as many aerosol sizes do, the width of the distribution implies negative particles sizes, which is not physically realistic. However, the normal distribution can be suitable for some aerosols, such as test aerosols, certainpollengrains andspores.

A more widely chosenlog-normal distributiongives the number frequency as:

$\mathrm {d} f={\frac {1}{d_{p}\sigma {\sqrt {2\pi }}}}e^{-{\frac {(ln(d_{p})-{\bar {d_{p}}})^{2}}{2\sigma ^{2}}}}\mathrm {d} d_{p}$

where:

$\sigma$is thestandard deviationof the size distribution and

${\bar {d_{p}}}$is thearithmetic meandiameter.

The log-normal distribution has no negative values, can cover a wide range of values, and fits many observed size distributions reasonably well.

Other distributions sometimes used to characterise particle size include: theRosin-Rammler distribution,applied to coarsely dispersed dusts and sprays; the Nukiyama–Tanasawa distribution, for sprays of extremely broad size ranges; thepower function distribution,occasionally applied to atmospheric aerosols; theexponential distribution,applied to powdered materials; and for cloud droplets, the Khrgian–Mazin distribution.

Physics

Terminal velocity of a particle in a fluid

For low values of theReynolds number(<1), true for most aerosol motion,Stokes' lawdescribes the force of resistance on a solid spherical particle in a fluid. However, Stokes' law is only valid when the velocity of the gas at the surface of the particle is zero. For small particles (< 1 μm) that characterize aerosols, however, this assumption fails. To account for this failure, one can introduce theCunningham correction factor,always greater than 1. Including this factor, one finds the relation between the resisting force on a particle and its velocity:

$F_{D}={\frac {3\pi \eta Vd}{C_{c}}}$

where

$F_{D}$is the resisting force on a spherical particle

$\eta$is the dynamicviscosityof the gas

$V$is the particle velocity

$C_{c}$is the Cunningham correction factor.

This allows us to calculate theterminal velocityof a particle undergoing gravitational settling in still air. Neglectingbuoyancyeffects, we find:

$V_{TS}={\frac {\rho _{p}d^{2}gC_{c}}{18\eta }}$

where

$V_{TS}$is the terminal settling velocity of the particle.

The terminal velocity can also be derived for other kinds of forces. If Stokes' law holds, then the resistance to motion is directly proportional to speed. The constant of proportionality is the mechanical mobility (B) of a particle:

$B={\frac {V}{F_{D}}}={\frac {C_{c}}{3\pi \eta d}}$

A particle traveling at any reasonable initial velocity approaches its terminal velocityexponentiallywith ane-folding time equal to the relaxation time:

$V(t)=V_{f}-(V_{f}-V_{0})e^{-{\frac {t}{\tau }}}$

where:

$V(t)$is the particle speed at time t

$V_{f}$is the final particle speed

$V_{0}$is the initial particle speed

To account for the effect of the shape of non-spherical particles, a correction factor known as thedynamic shape factoris applied to Stokes' law. It is defined as the ratio of the resistive force of the irregular particle to that of a spherical particle with the same volume and velocity:

$\chi ={\frac {F_{D}}{3\pi \eta Vd_{e}}}$

where:

$\chi$is the dynamic shape factor

Aerodynamic diameter

The aerodynamic diameter of an irregular particle is defined as the diameter of the spherical particle with a density of 1000 kg/m³and the same settling velocity as the irregular particle.

Neglecting the slip correction, the particle settles at the terminal velocity proportional to the square of theaerodynamicdiameter,d_a:

$V_{TS}={\frac {\rho _{0}d_{a}^{2}g}{18\eta }}$

where

$\ \rho _{0}$= standard particle density (1000 kg/m³).

This equation gives the aerodynamic diameter:

$d_{a}=d_{e}\left({\frac {\rho _{p}}{\rho _{0}\chi }}\right)^{\frac {1}{2}}$

One can apply the aerodynamic diameter to particulate pollutants or to inhaled drugs to predict where in the respiratory tract such particles deposit. Pharmaceutical companies typically use aerodynamic diameter, not geometric diameter, to characterize particles in inhalable drugs.

Dynamics

The previous discussion focused on single aerosol particles. In contrast,aerosol dynamicsexplains the evolution of complete aerosol populations. The concentrations of particles will change over time as a result of many processes. External processes that move particles outside a volume of gas under study includediffusion,gravitational settling, andelectric chargesand other external forces that cause particle migration. A second set of processes internal to a given volume of gas include particle formation (nucleation), evaporation, chemical reaction, and coagulation.

Adifferential equationcalled theAerosol General Dynamic Equation(GDE) characterizes the evolution of the number density of particles in an aerosol due to these processes.

${\frac {\partial {n_{i}}}{\partial {t}}}=-\nabla \cdot n_{i}\mathbf {q} +\nabla \cdot D_{p}\nabla _{i}n_{i}+\left({\frac {\partial {n_{i}}}{\partial {t}}}\right)_{\mathrm {growth} }+\left({\frac {\partial {n_{i}}}{\partial {t}}}\right)_{\mathrm {coag} }-\nabla \cdot \mathbf {q} _{F}n_{i}$

Change in time = Convective transport +brownian diffusion+ gas-particle interactions + coagulation + migration by external forces

Where:

$n_{i}$is number density of particles of size category$i$

$\mathbf {q}$is the particle velocity

$D_{p}$is the particleStokes-Einsteindiffusivity

$\mathbf {q} _{F}$is the particle velocity associated with an external force

Coagulation

As particles and droplets in an aerosol collide with one another, they may undergo coalescence or aggregation. This process leads to a change in the aerosol particle-size distribution, with the mode increasing in diameter as total number of particles decreases.On occasion, particles may shatter apart into numerous smaller particles; however, this process usually occurs primarily in particles too large for consideration as aerosols.

Dynamics regimes

TheKnudsen numberof the particle define three different dynamical regimes that govern the behaviour of an aerosol:

$K_{n}={\frac {2\lambda }{d}}$

where$\lambda$is themean free pathof the suspending gas and$d$is the diameter of the particle.For particles in thefree molecular regime,K_n>> 1; particles small compared to the mean free path of the suspending gas.In this regime, particles interact with the suspending gas through a series of "ballistic" collisions with gas molecules. As such, they behave similarly to gas molecules, tending to follow streamlines and diffusing rapidly through Brownian motion. The mass flux equation in the free molecular regime is:

$I={\frac {\pi a^{2}}{k_{b}}}\left({\frac {P_{\infty }}{T_{\infty }}}-{\frac {P_{A}}{T_{A}}}\right)\cdot C_{A}\ Alpha$

whereais the particle radius,P_∞andP_Aare the pressures far from the droplet and at the surface of the droplet respectively,k_bis the Boltzmann constant,Tis the temperature,C_Ais mean thermal velocity andαis mass accommodation coefficient.The derivation of this equation assumes constant pressure and constant diffusion coefficient.

Particles are in thecontinuum regimewhen K_n<< 1.In this regime, the particles are big compared to the mean free path of the suspending gas, meaning that the suspending gas acts as a continuous fluid flowing round the particle.The molecular flux in this regime is:

$I_{cont}\sim {\frac {4\pi aM_{A}D_{AB}}{RT}}\left(P_{A\infty }-P_{AS}\right)$

whereais the radius of the particleA,M_Ais the molecular mass of the particleA,D_ABis the diffusion coefficient between particlesAandB,Ris the ideal gas constant,Tis the temperature (in absolute units like kelvin), andP_A∞andP_ASare the pressures at infinite and at the surface respectively.

Thetransition regimecontains all the particles in between the free molecular and continuum regimes orK_n≈ 1. The forces experienced by a particle are a complex combination of interactions with individual gas molecules and macroscopic interactions. The semi-empirical equation describing mass flux is:

$I=I_{cont}\cdot {\frac {1+K_{n}}{1+1.71K_{n}+1.33{K_{n}}^{2}}}$

whereI_contis the mass flux in the continuum regime.This formula is called the Fuchs-Sutugin interpolation formula. These equations do not take into account the heat release effect.

Partitioning

Condensation and evaporation

Aerosol partitioning theory governscondensationon andevaporationfrom an aerosol surface, respectively. Condensation of mass causes the mode of the particle-size distributions of the aerosol to increase; conversely, evaporation causes the mode to decrease. Nucleation is the process of forming aerosol mass from the condensation of a gaseous precursor, specifically avapor.Net condensation of the vapor requires supersaturation, apartial pressuregreater than itsvapor pressure.This can happen for three reasons:

1. Lowering the temperature of the system lowers the vapor pressure.
2. Chemical reactions may increase the partial pressure of a gas or lower its vapor pressure.
3. The addition of additional vapor to the system may lower the equilibrium vapor pressure according toRaoult's law.

There are two types of nucleation processes. Gases preferentially condense onto surfaces of pre-existing aerosol particles, known asheterogeneous nucleation.This process causes the diameter at the mode of particle-size distribution to increase with constant number concentration.With sufficiently high supersaturation and no suitable surfaces, particles may condense in the absence of a pre-existing surface, known ashomogeneous nucleation.This results in the addition of very small, rapidly growing particles to the particle-size distribution.

Activation

Water coats particles in aerosols, making themactivated,usually in the context of forming a cloud droplet (such as natural cloud seeding by aerosols from trees in a forest).Following theKelvin equation(based on the curvature of liquid droplets), smaller particles need a higher ambientrelative humidityto maintain equilibrium than larger particles do. The following formula givesrelative humidityat equilibrium:

$RH={\frac {p_{s}}{p_{0}}}\times 100\%=S\times 100\%$

where$p_{s}$is thesaturation vapor pressureabove a particle at equilibrium (around a curved liquid droplet),p₀is the saturation vapor pressure (flat surface of the same liquid) andSis the saturation ratio.

Kelvin equationfor saturation vapor pressure above a curved surface is:

$\ln {p_{s} \over p_{0}}={\frac {2\sigma M}{RT\rho \cdot r_{p}}}$

wherer_pdroplet radius,σsurface tension of droplet,ρdensity of liquid,Mmolar mass,Ttemperature, andRmolar gas constant.

Solution to the general dynamic equation

There are no generalsolutionsto the general dynamic equation (GDE);common methods used to solve the general dynamic equation include:

• Moment method
• Modal/sectional method,and
• Quadrature method of moments/Taylor-series expansion method of moments,and
• Monte Carlo method.

Detection

Aerosol can either be measuredin-situor withremote sensingtechniques.

In situobservations

Some available in situ measurement techniques include:

• Aerosol mass spectrometer(AMS)
• Differential mobility analyzer(DMA)
• Electrical aerosol spectrometer(EAS)
• Aerodynamic particle sizer(APS)
• Aerodynamic aerosol classifier(AAC)
• Wide range particle spectrometer(WPS)
• Micro-Orifice Uniform Deposit Impactor(MOUDI)
• Condensation particle counter(CPC)
• Epiphaniometer
• Electrical low pressure impactor(ELPI)
• Aerosol particle mass-analyser(APM)
• Centrifugal Particle Mass Analyser(CPMA)

Remote sensing approach

Remote sensing approaches include:

• Sun photometer
• Lidar
• Imaging spectroscopy

Size selective sampling

Particles can deposit in thenose,mouth,pharynxandlarynx(the head airways region), deeper within the respiratory tract (from thetracheato theterminal bronchioles), or in thealveolar region.The location of deposition of aerosol particles within the respiratory system strongly determines the health effects of exposure to such aerosols.This phenomenon led people to invent aerosol samplers that select a subset of the aerosol particles that reach certain parts of the respiratory system.

Examples of these subsets of the particle-size distribution of an aerosol, important in occupational health, include the inhalable, thoracic, and respirable fractions. The fraction that can enter each part of the respiratory system depends on the deposition of particles in the upper parts of the airway.The inhalable fraction of particles, defined as the proportion of particles originally in the air that can enter the nose or mouth, depends on external wind speed and direction and on the particle-size distribution by aerodynamic diameter.The thoracic fraction is the proportion of the particles in ambient aerosol that can reach the thorax or chest region.The respirable fraction is the proportion of particles in the air that can reach the alveolar region.To measure the respirable fraction of particles in air, a pre-collector is used with a sampling filter. The pre-collector excludes particles as the airways remove particles from inhaled air. The sampling filter collects the particles for measurement. It is common to usecyclonic separationfor the pre-collector, but other techniques include impactors, horizontalelutriators,and large poremembrane filters.

Two alternative size-selective criteria, often used in atmospheric monitoring, are PM₁₀and PM_2.5.PM₁₀is defined byISOasparticles which pass through a size-selective inlet with a 50% efficiency cut-off at 10 μm aerodynamic diameterand PM_2.5asparticles which pass through a size-selective inlet with a 50% efficiency cut-off at 2.5 μm aerodynamic diameter.PM₁₀corresponds to the "thoracic convention" as defined in ISO 7708:1995, Clause 6; PM_2.5corresponds to the "high-risk respirable convention" as defined in ISO 7708:1995, 7.1.TheUnited States Environmental Protection Agencyreplaced the older standards for particulate matter based on Total Suspended Particulate with another standard based on PM₁₀in 1987and then introduced standards for PM_2.5(also known as fine particulate matter) in 1997.

See also

• Aerogel
• Aeroplankton
• Aerosol transmission
• Bioaerosol
• Deposition (Aerosol physics)
• Global dimming
• Nebulizer
• Monoterpene
• Stratospheric aerosol injection

References

Sources

• Colbeck, Ian; Lazaridis, Mihalis, eds. (2014).Aerosol Science: Technology and Applications.John Wiley & Sons - Science.ISBN978-1-119-97792-6.
• Friedlander, S. K. (2000).Smoke, Dust and Haze: Fundamentals of Aerosol Behavior(2nd ed.). New York: Oxford University Press.ISBN0-19-512999-7.
• Hinds, William C. (1999).Aerosol Technology(2nd ed.). Wiley - Interscience.ISBN978-0-471-19410-1.
• Hidy, George M. (1984).Aerosols, An Industrial and Environmental Science.Academic Press, Inc.ISBN978-0-12-412336-6.

External links

• International Aerosol Research AssemblyArchived2020-01-21 at theWayback Machine
• American Association for Aerosol Research
• NIOSH Manual of Analytical Methods(see chapters on aerosol sampling)