Distribution of air pollution into Earth's atmosphere
The followingoutline is provided as an overview of and topical guide to air pollution dispersion:Inenvironmental science,air pollution dispersion is the distribution ofair pollution into theatmosphere.Air pollution is the introduction ofparticulates, biological molecules, or other harmful materials into Earth's atmosphere, causingdisease, death to humans, damage to other living organisms such as food crops, and thenatural orbuilt environment. Air pollution may come fromanthropogenic or natural sources.Dispersion refers to what happens to the pollution during and after its introduction; understanding this may help in identifying and controlling it.
Visualization of a buoyant Gaussian air pollutant dispersion plume
Air pollution emission plume – flow of pollutant in the form of vapor or smoke released into the air. Plumes are of considerable importance in the atmospheric dispersion modelling of air pollution. There are three primary types of air pollutionemissionplumes:
Buoyant plumes – Plumes which are lighter than air because they are at a highertemperature and lowerdensity than the ambient air which surrounds them, or because they are at about the same temperature as the ambient air but have a lowermolecular weight and hence lower density than the ambient air. For example, the emissions from theflue gas stacks of industrialfurnaces are buoyant because they are considerably warmer and less dense than the ambient air. As another example, an emission plume ofmethane gas at ambient air temperatures is buoyant because methane has a lower molecular weight than the ambient air.
Dense gas plumes – Plumes which are heavier than air because they have a higher density than the surrounding ambient air. A plume may have a higher density than air because it has a higher molecular weight than air (for example, a plume ofcarbon dioxide). A plume may also have a higher density than air if the plume is at a much lower temperature than the air. For example, a plume ofevaporated gaseous methane from an accidental release ofliquefied natural gas (LNG) may be as cold as −161 °C (−258 °F).
Passive or neutral plumes – Plumes which are neither lighter or heavier than air.
There are five types of air pollution dispersion models, as well as some hybrids of the five types:[1]
Box model – The box model is the simplest of the model types.[2] It assumes theairshed (i.e., a given volume ofatmospheric air in a geographical region) is in the shape of a box. It also assumes that the air pollutants inside the box are homogeneously distributed and uses that assumption to estimate the average pollutantconcentrations anywhere within the airshed. Although useful, this model is very limited in its ability to accurately predict dispersion of air pollutants over an airshed because the assumption of homogeneous pollutant distribution is much too simple.
Gaussian model – The Gaussian model is perhaps the oldest (circa 1936)[3] and perhaps the most commonly used model type. It assumes that the air pollutant dispersion has aGaussian distribution, meaning that the pollutant distribution has a normal probability distribution. Gaussian models are most often used for predicting the dispersion of continuous, buoyant air pollution plumes originating from ground-level or elevated sources. Gaussian models may also be used for predicting the dispersion of non-continuous air pollution plumes (calledpuff models). The primary algorithm used in Gaussian modeling is theGeneralized Dispersion Equation For A Continuous Point-Source Plume.[4][5]
Lagrangian model – a Lagrangian dispersion model mathematically follows pollution plume parcels (also called particles) as the parcels move in the atmosphere and they model the motion of the parcels as arandom walk process. The Lagrangian model then calculates the air pollution dispersion by computing the statistics of the trajectories of a large number of the pollution plume parcels. A Lagrangian model uses a movingframe of reference[6] as the parcels move from their initial location. It is said that an observer of a Lagrangian model follows along with the plume.
Eulerian model – an Eulerian dispersion model is similar to a Lagrangian model in that it also tracks the movement of a large number of pollution plume parcels as they move from their initial location. The most important difference between the two models is that the Eulerian model uses a fixed three-dimensionalCartesian grid[6] as a frame of reference rather than a moving frame of reference. It is said that an observer of an Eulerian model watches the plume go by.
Dense gas model – Dense gas models are models that simulate the dispersion of dense gas pollution plumes (i.e., pollution plumes that are heavier than air). The three most commonly used[citation needed][dubious –discuss] dense gas models are:
Types of air pollutant emission sources – named for their characteristics
Sources, by shape – there are four basic shapes which an emission source may have. They are:
Point source – single, identifiable source of air pollutant emissions (for example, the emissions from acombustion furnace flue gas stack). Point sources are also characterized as being either elevated or at ground-level. A point source has nogeometric dimensions.
Line source – one-dimensional source of air pollutant emissions (for example, the emissions from thevehicular traffic on a roadway).
Area source – two-dimensional source of diffuse air pollutant emissions (for example, the emissions from aforest fire, alandfill or the evaporated vapors from a large spill of volatile liquid).
Volume source – three-dimensional source of diffuse air pollutant emissions. Essentially, it is an area source with a third (height) dimension (for example, the fugitive gaseous emissions frompipingflanges,valves and other equipment at various heights within industrial facilities such asoil refineries andpetrochemical plants). Another example would be the emissions from an automobile paint shop with multiple roof vents or multiple open windows.
Mobile source –buses are examples of mobile sources
Sources, by urbanization level – whether the source is within a city or not is relevant in that urban areas constitute a so-calledheat island and the heat rising from an urban area causes the atmosphere above an urban area to be more turbulent than the atmosphere above a rural area
Urban source – emission is in an urban area
Rural source – emission is in a rural area
Sources, by elevation
Surface or ground-level source
Near surface source
Elevated source
Sources, by duration
Puff or intermittent source – short term sources (for example, manyaccidental emission releases are short term puffs)
Continuous source – long term source (for example, most flue gas stack emissions are continuous)
Effect ofturbulence on dispersion – turbulence increases theentrainment and mixing of unpolluted air into the plume and thereby acts to reduce the concentration of pollutants in the plume (i.e., enhances the plume dispersion). It is therefore important to categorize the amount of atmospheric turbulence present at any given time. This type of dispersion is scale dependent.[10] Such that, for flows where the cloud of pollutant is smaller than the largest eddies present, there will be mixing. There is no limit on the size on mixing motions in the atmosphere and therefore bigger clouds will experience larger and stronger mixing motions. And hence, this type of dispersion is scale dependent.
Pasquill atmospheric stability classes – oldest and, for a great many years, the most commonly used method of categorizing the amount of atmospheric turbulence present was the method developed byPasquill in 1961.[11] He categorized the atmospheric turbulence into sixstability classes named A, B, C, D, E and F with class A being the most unstable or most turbulent class, and class F the most stable or least turbulent class.
Table 1 lists the six classes
Table 2 provides the meteorological conditions that define each class. The stability classes demonstrate a few key ideas. Solar radiation increasesatmospheric instability through warming of the Earth's surface so that warm air is below cooler (and therefore denser) air promoting vertical mixing. Clear nights push conditions toward stable as the ground cools faster establishing more stable conditions and inversions. Wind increases vertical mixing, breaking down any type of stratification and pushing the stability class towards neutral (D).[12]
Table 1: The Pasquill stability classes
Stability class
Definition
Stability class
Definition
A
very unstable
D
neutral
B
unstable
E
slightly stable
C
slightly unstable
F
stable
Table 2: Meteorological conditions that define the Pasquill stability classes
Surface windspeed
Daytime incoming solar radiation
Nighttime cloud cover
m/s
mi/h
Strong
Moderate
Slight
> 50%
< 50%
< 2
< 5
A
A – B
B
E
F
2 – 3
5 – 7
A – B
B
C
E
F
3 – 5
7 – 11
B
B – C
C
D
E
5 – 6
11 – 13
C
C – D
D
D
D
> 6
> 13
C
D
D
D
D
Note: Class D applies to heavily overcast skies, at any windspeed day or night
Incoming solar radiation is based on the following: strong (> 700 W m−2), moderate (350–700 W m−2), slight (< 350 W m−2)[13]
Other parameters that can define the stability class
Advanced air pollution dispersion models – they do not categorize atmospheric turbulence by using the simple meteorological parameters commonly used in defining the six Pasquill classes as shown in Table 2 above. The more advanced models use some form ofMonin–Obukhov similarity theory. Some examples include:
AERMOD[17] – US EPA's most advanced model, no longer uses the Pasquill stability classes to categorize atmospheric turbulence. Instead, it uses the surfaceroughness length and theMonin–Obukhov length.
ADMS 4[18] –United Kingdom's most advanced model, uses the Monin-Obukhov length, theboundary layer height and the windspeed to categorize the atmospheric turbulence.
(Work on this section is continuously in progress)
Building effects or downwash: When an air pollution plume flows over nearby buildings or other structures, turbulent eddies are formed in the downwind side of the building. Those eddies cause a plume from a stack source located within about five times the height of a nearby building or structure to be forced down to the ground much sooner than it would if a building or structure were not present. The effect can greatly increase the resulting near-by ground-level pollutant concentrations downstream of the building or structure. If the pollutants in the plume are subject to depletion by contact with the ground (particulates, for example), the concentration increase just downstream of the building or structure will decrease the concentrations further downstream.
Deposition of the pollution plume components to the underlying surface can be defined as either dry or wet deposition:
Dry deposition is the removal of gaseous or particulate material from the pollution plume by contact with the ground surface or vegetation (or even water surfaces) through transfer processes such asabsorption and gravitationalsedimentation. This may be calculated by means of adeposition velocity, which is related to the resistance of the underlying surface to the transfer.
Wet deposition is the removal of pollution plume components by the action of rain. The wet deposition of radionuclides in a pollution plume by a burst of rain often forms so calledhot spots of radioactivity on the underlying surface.
Inversion layers:[5] Normally, the air near theEarth's surface is warmer than the air above it because the atmosphere is heated from below as solar radiation warms the Earth's surface, which in turn then warms the layer of the atmosphere directly above it. Thus, the atmospheric temperature normally decreases with increasing altitude. However, under certain meteorological conditions, atmospheric layers may form in which the temperature increases with increasing altitude. Such layers are called inversion layers. When such a layer forms at the Earth's surface, it is called asurface inversion. When an inversion layer forms at some distance above the earth, it is called aninversion aloft (sometimes referred to as acapping inversion). The air within an inversion aloft is very stable with very little vertical motion. Any rising parcel of air within the inversion soon expands, therebyadiabatically cooling to a lower temperature than the surrounding air and the parcel stops rising. Any sinking parcel soon compresses adiabatically to a higher temperature than the surrounding air and the parcel stops sinking. Thus, any air pollution plume that enters an inversion aloft will undergo very little vertical mixing unless it has sufficientmomentum to completely pass through the inversion aloft. That is one reason why an inversion aloft is sometimes called a capping inversion.
Mixing height:[5] When an inversion aloft is formed, the atmospheric layer between the Earth's surface and the bottom of the inversion aloft is known as themixing layer and the distance between the Earth's surface and the bottom of inversion aloft is known as themixing height. Any air pollution plume dispersing beneath an inversion aloft will be limited in vertical mixing to that which occurs beneath the bottom of the inversion aloft (sometimes called thelid). Even if the pollution plume penetrates the inversion, it will not undergo any further significant vertical mixing. As for a pollution plume passing completely through an inversion layer aloft, that rarely occurs unless the pollution plume's source stack is very tall and the inversion lid is fairly low.
ADMS 3 (Atmospheric Dispersion Modelling System) – advanced atmospheric pollution dispersion model for calculating concentrations of atmospheric pollutants emitted both continuously from point, line, volume and area sources, or intermittently from point sources.
^Pasquill, F. (1961).The estimation of the dispersion of windborne material, The Meteorological Magazine, vol 90, No. 1063, pp 33-49.
^Pasquill, F. (February 1961). "The estimation of the dispersion of windborne material".Meteorological Magazine.90:33–49.
^Seinfeld, John (2006).Atmospheric Chemistry and Physics: From Air Pollution to Climate Change. Hoboken, New Jersey: John Wiley & Sons, Inc. p. 750.ISBN978-0-471-72018-8.
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