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Khoury, D.; Millet, M.; Jabali, Y.; Delhomme, O. Physical and Chemical Aspects of Fog Water. Encyclopedia. Available online: https://encyclopedia.pub/entry/53341 (accessed on 29 April 2024).
Khoury D, Millet M, Jabali Y, Delhomme O. Physical and Chemical Aspects of Fog Water. Encyclopedia. Available at: https://encyclopedia.pub/entry/53341. Accessed April 29, 2024.
Khoury, Dani, Maurice Millet, Yasmine Jabali, Olivier Delhomme. "Physical and Chemical Aspects of Fog Water" Encyclopedia, https://encyclopedia.pub/entry/53341 (accessed April 29, 2024).
Khoury, D., Millet, M., Jabali, Y., & Delhomme, O. (2024, January 02). Physical and Chemical Aspects of Fog Water. In Encyclopedia. https://encyclopedia.pub/entry/53341
Khoury, Dani, et al. "Physical and Chemical Aspects of Fog Water." Encyclopedia. Web. 02 January, 2024.
Physical and Chemical Aspects of Fog Water
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This entry is adapted from the peer-reviewed paper 10.3390/environments10120224

Fog water have been rapidly increasing due to its negative impacts on different environmental processes. However, fog water harvesting has become beneficial in various countries to overcome water scarcity. Accurate fog forecasting remains a challenging issue due to its spatio-temporal variability and uncertainties despite the development and efforts made to understand its chemistry and microphysics. The literature proved that the decrease in fog frequency over time in most countries is mainly attributed to the improvement in air quality or the change in regional climatic conditions. 

fog impacts fog lifecyle fog

1. Introduction

Atmospheric pollution, characterized by measurements of biological, physical, or chemical contaminants, has become an international policy problem having harmful consequences for human health and ecosystems [1][2]. Accordingly, fog droplets are composed of a mixture of organic and inorganic compounds resulting from scavenging hygroscopic particles and water-soluble trace gases. Fog droplets are formed on aerosol particles in a supersaturated atmosphere. However, the pollution loadings of these particles are higher than those in clouds and precipitation [3]. It is the result of the synergic effect of weather factors (relative humidity (RH), wind direction (WD), wind velocity (WS), temperature (T), pressure (P), etc.) and pollution (presence of aerosols) [4]. Its chemical composition is an important tool for the complementary analysis and identification of air and long-range transport (LRT) pollutants because fog is formed in a shallow boundary layer which is conducive to fog formation and has the ability to trap local and regional pollutants. According to the American Meteorological Society (AMS), fog comprises a large number of small water droplets in the liquid form or ice crystals suspended in the atmosphere reducing the visibility below 1 km (0.62 miles) in the surrounding area [5]. Surface visibility is critical for aviation, transportation, and land safety, causing significant human and financial losses, and is responsible for serious air, land, and water transportation [6][7][8]. Modern aircraft have no difficulties with fogs of 1 km, but some restrictions can be imposed when the visibility degrades to lower than that. Visibility of less than 500 m is classified as fog [9]. The reduction in visibility depends on the resulting distribution of fog droplets and on the concentration of cloud condensation nuclei (CCN). The densest and thickest fog mainly occurs in urban or industrialized areas in the presence of a high number of polluted particles in the air acting as CCN for water droplets [5][10]. Fog is of great meteorological significance due to its strong relation to humidity factors and its capability of reducing the temperature amplitude and local character of formation. Its formation, existence, and dissipation are strongly influenced by numerous factors including local orographic conditions (changes in atmospheric conditions), atmospheric circulations (heat distribution by large-scale air masses), and the actual synoptic situation (pressure pattern, fronts, wind direction, wind speed, etc.) [10]. The presence of natural fog affects many environmental components including global and local climate, air quality, water quality, air–surface interactions, the thermal and radiative budget of the atmosphere, etc. [11][12]. It has severe impacts on social life leading to an increase in the number of injuries due to the reduced visibility whether in water, air, or land transportation [5][12]. Fog has also direct and indirect adverse impacts on human beings (primary and secondary) [13]. However, it has a beneficial effect on decreasing the concentration of different air pollutants, cleaning the atmosphere through the wet deposition phenomenon, and agricultural and water supply activities [14][15]. Therefore, monitoring these climatic events in the different environmental matrices is crucial to better understand the consequences of their presence in the environment and to meet the criteria for defining good air quality.
Fog droplets acquire their chemical composition by mechanisms similar to those of cloud water droplets [16]. The solute concentrations in fog water (organic acids, heavy metals, ions, etc.) are usually up to 100 times higher than those observed in precipitation due to the longer residence time in the atmosphere and their smaller droplet size. The longer residence time makes possible the higher accumulation of the products of the liquid-phase processes. The major composition of fog water is the result of the interaction of sulfur dioxide (SO2), nitrogen oxide (NOx), carbon dioxide (CO2), hydrogen chloride (HCl), and ammonia (NH3) with water in an oxidative atmosphere (oxygen (O2), ozone (O3), sunlight, etc.) and in the presence of trace metals that may act as redox catalysts (iron (Fe), copper (Cu), manganese (Mn), and organic materials including dust, soot, and hydrocarbons (HCs)) [17]. Fogs act as a micro-reactor for chemical and photochemical reactions with atmospheric oxidants such as singlet oxygen, hydroxyl radical, nitrate radical, etc. They are important media for aqueous-phase reactions where inorganic gases such as SO2, NOx, and dissolved volatile organic compounds (VOCs) are oxidized.

2. Fog Types

Several points of view have been widely used in fog classification. It might be based on thermodynamic properties (mixed-phase fog), physical (freezing and ice fogs) and dynamical processes (turbulence and mixing fogs), the chemical composition of particles (dry fog), weather features (frontal fog), and the physiographic character of the surface (valley fog). Another point of view suggests that fog might be divided into three categories: liquid fog, mixed-phase fog, and ice fog. The latter forms when the temperature falls below −10 °C, liquid fog forms when the temperature is higher than −10 °C, and the mixed-phase fog forms between −10 °C and −30 °C [18]. However, fog might also form under special conditions. For instance, ice fog can occur at a temperature of −20 °C in the case of excessive vapor being absorbed by ice nuclei under steady-state conditions in the absence of mixing processes [11]. Willett proposes a fog classification based on favorable synoptic conditions. He sub-categorizes them into numerous types that might be formed in the atmosphere [19]. They include advection fog, valley fog, upslope fog, freezing fog, ice fog, steam fog, precipitation fog, and radiation fog [11][20][21][22][23][24]. Each type of fog is defined by a special physical process responsible for its formation [11]. Advection fog results in locations where warm air passes over cooler ocean water. As this process occurs, the temperature drops to the dew point, and water vapor condenses in the warm air, producing an RH of 100% and leading to the formation of fog. It mainly occurs in windy conditions such as on the Pacific coast of the US and San Francisco where the ocean is significantly cooler than the surrounding land. Typical fogs extend up to a few hundred meters in height [25]. Valley fog is formed during winter in mountain valleys where the dense air is trapped in the valley. In this area, the dense air settles down the valley and condenses to form fog. It is essentially due to a temperature inversion along with warmer air flowing above the valley. It may last for a few days during winter in calm conditions. Upslope fog occurs when the air flow rises up the terrain and cools it adiabatically to its saturation temperature allowing water vapor to condense to form fog. When it is seen from below, it is viewed as stratus clouds; as one goes up into the cloud, it is viewed as fog. This type is also known as the orographic fog. Freezing fog is formed when water droplets in the air mass become supercooled, and solid surfaces are frozen. As the fog intensity increases, the ground, trees, and other objects are glazed by a layer of rime or frost. Freezing foggy events occur at temperatures below 0 °C. Ice fog develops in Polar or Arctic regions where air temperature is below freezing. It is usually observed at high altitudes, in calm and clear weather, and in extremely cold air (<−29 °C). Ice fog is composed of ice crystals suspended in the air instead of supercooled water droplets. It results when water vapor is released into the atmosphere and is then condensed to form droplets that are rapidly frozen into ice particles. Steam fog is somehow the reverse of the advection fog. It occurs when cold air passes over relatively warm water. The air is cooled and moistened, causing the dew point to increase, causing condensation of water vapor leading to the formation of fog. It is a common phenomenon occurring during early winter and autumn, in middle latitudes, near rivers and lakes where water is still warm [26][27][28]. Precipitation fog is associated with weather fronts, especially warm frontal boundaries. It is formed when warm rain falls through cold and almost saturated air. When the precipitation falls down into colder air, the quantity of water vapor in the atmosphere is increased through evaporation, causing the dew point to rise and the cool air to become saturated to form fog. It is also known as frontal fog [25][29][30][31][32]. Radiation fog is known as ground or continental fog that does not reach any of the clouds overhead. It usually occurs at night under stable conditions (clear sky and calm wind) and dissipates in the morning as the ground warms by increasing the heating rate from thermal radiation. This type is common in continental climates during winter under anticyclonic conditions (high pressure). Radiation fog is produced when the heat absorbed by the surface is radiated into the air, cooling the ground and causing a temperature inversion. As the surface cools, a layer of moist air is created near the ground and reaches its dew point. At this point, condensation occurs, resulting in the formation of fog [33]. The depth of the radiation fog increases as long as sufficient moist air is available. Typical ground fogs reach 100 to 200 m in height. Radiation fog is a mixture of liquid droplets, gaseous species, wet aerosols, and dry PM, resulting from complex interactions among these phases, contributing to the enrichment of fog droplets with inorganic and organic contaminations. Briefly, two basic concepts lead to fog formation: either air temperature reaches the dew point, forming advection, upslope, and radiation fog, or sufficient vapor is added to the air, forming frontal and evaporation fog [34].

3. Fog Forecasting

Fog is an important meteorological phenomenon that should be predicted accurately due to its strong influence on the economy and personal safety. Poor forecasting leads to a greater disruption to surface, sea, and air transport with subsequent increased risk to the economy and personal and social life. Fog is influenced by numerous factors, covering multiple temporal and spatial scales [11]. Fog formation is correlated with the presence of meteoroidal conditions such as low temperature, wind speed, wind direction, and very high relative humidity. In fact, fog does not always occur in windless and calm conditions. A historical dense foggy event was reported by Scott in 1896, stating that fogs with strong winds accompanied by heavy rain occurred in the British Isles. Fog-related events associated with strong winds are estimated to be about 135 in 15 years [35][36]. In 1892, fog formation was found to be related to the role of aerosols. Mensbrugghe states that “aqueous vapor condenses in the air only in the presence of solid particles around which the invisible vapor becomes a liquid” [37]. Additionally, Willett emphasizes the importance of CCN in fog formation. He reports that dust particles, hygroscopic particles, and those having an electric charge or ions facilitate fog formation [19]. The presence of hydrophilic particles is an important key that facilitates the condensation of water vapor into fog droplets. The pollution does lead to fog formation, and the heterogeneous nucleation of pollution condensation nuclei leads to fog droplet formation. The increasing quantity in polluted atmospheres decreases the surface tension, causing the pollution particles to be activated at lower relative humidity and resulting in a denser and thicker fog [38]. All these factors lead to the accumulation of pollutants in a stable and strong inversion boundary layer which is responsible for fog maintenance. Thus, air saturation with water vapor and favorable meteorological conditions are two driving parameters of fog formation. Fog appearance and dissipation are still not very clear since they are directly related to turbulence, microphysical and radiative processes, thermodynamics, and surface conditions. The reason behind that could be that fog is sensitive to the complex balance mechanism among all the processes. The initial conditions of turbulence and humidity are critical for the prediction of fog events. Some researchers suggest that fog is formed due to a turbulent mixing between nearly saturated eddies with slightly different temperatures when the colder air mixes and cools the hotter moister air reaching the saturation. Other researchers suggest that a virtual cessation of turbulence is necessary before fog formation. In this mechanism, it is assumed that the high levels of turbulence cause saturation to occur at the surface in the form of dew, preventing the coalescence of fog droplets and fog formation. Once formed, its further maturation or dissipation depends on the evolution of its physical processes and the environmental conditions that govern the removal and production of liquid water. Overall fog forecasting remains difficult and challenging since it depends on a large number of physical and chemical processes along with non-linear interactions. Factors that may be involved are many: atmospheric stability, radiation balance, moisture availability, turbulence, advection, topography, and microphysics [39]

4. Fog Frequency

The United States National Oceanic and Atmospheric Administration (US NOAA) runs the Global Daily database from over 8000 stations worldwide to make a useful comparison regarding the average annual fog frequency. A twenty-year period, between 1991 and 2010, is investigated to obtain precise meteorological data. The annual number of foggy days and annual cycle of fog widely vary according to local conditions and weather factors. The high occurrence of fog water usually occurs where water vapor is in excess such as in locations near the ocean, river, lake, sea, and other humid sites as well as where favorable conditions are present (i.e., cooling). Other factors including local conditions (altitude, type of land), mesoscale (distance to the coast, exposure to advection air masses), and synoptic scale (cyclonic scale) affect the duration and frequency of fog. The highest fog frequency has been observed in Washington/US (NDF = 311), Śnieżka/Poland (298), and Harz/Germany (284). High fog occurrence has also been detected in equatorial and subequatorial zones such as in Iquitos/Peru (102), due to the extremely high humidity and nocturnal radiative cooling. Fog occurrence is found to be high in montane tropical atmospheres such as in Quito/Ecuador (208). Further, in tropical and subtropical zones next to the coast, fog frequency is also high such as in Chile (189), where the region is influenced by cold oceanic air masses. In polar zones, the occurrence of foggy events is also high such as in Nuuk/Greenland (81) and Marambio/Antarctic (138), where advection fog is dominant. However, fog frequency all over the world has shown a significant decrease. Statistical results show that the strongest relation to fog occurrence is air pollution. In the case air pollution becomes less severe, environmental factors such as wind speed, urban heat island (UHI), relative humidity, and inversion layer become decisive in controlling its occurrence and duration [40]. Literature studies reported a decrease in the majority of fog stations worldwide. Williams et al. reported that the change in regional climatic conditions such as the ongoing intensification effect of UHI or atmospheric circulation leads to an increase in air temperatures contributing to a decrease in the fog frequency in southern California [41][42]. Aerosols are found to have a direct relation with fog evolution [43].

5. Fog Nucleation and Activation

5.1. Fog Nucleation

The formation of fog water requires relatively high humidity conditions ranging from undersaturated to slightly supersaturated conditions [44]. The presence of atmospheric aerosols is a key factor for droplet formation, where they can grow in size more easily in a saturated atmosphere [38]. The process of forming the droplet nuclei, known as the nucleation scavenging process, is of great significance for cloud, particle, and fog formation [45]. The presence of hydrophilic inorganic species including sulfate, nitrate, and ammonium (SNA) and soluble elements including magnesium and calcium plays a vital role in fog formation by acting as CCN. The presence of water-soluble organic carbon (WSOC) has been pointed out to modify the hygroscopicity of aerosol particles and enhance their tendency to act as CCN [46]. The availability of trace metals like copper, manganese, and iron also plays a significant role in aerosol–fog interactions by acting as catalysts for aqueous-phase reactions.
Numerous types of AA particles are capable of acting as CCN. Some of the AAs are generated from natural sources (sea spray, volcanic debris, biogenic aerosol, etc.), while others are derived from human-made activities (industrial emissions, agricultural activities, biomass burning, fossil fuel combustion, etc.) [47][48]. In the presence of small amounts of water supersaturation, AAs tend to grow spontaneously to form fog droplets. Particles containing water-soluble compounds are more desirable to act as CCN over those containing largely insoluble compounds [49]. Particles with diameters ranging from 0.001 to 0.2 µm play a significant role in fog/cloud and precipitation microphysics. In fogs, aerosols are activated and grow into droplets whenever their size is greater than 0.1 µm and smaller than 1 µm. This means that the accumulation-mode particles are mainly responsible for fog formation. Particles with diameters greater than 1 µm may grow but without being activated [49][50][51]. In the case the particle concentration is high and/or the supersaturation level is low, the minimum size of the particle required for activation is 0.5 µm [51]. The accumulation-mode particles are formed through the coagulation of smaller particles that belong to the Aitken nuclei (<0.1 µm) or from the condensation of vapors into existing particles, forcing them to grow [52]. They are characterized by their long residence time and high concentrations compared to other modes. The accumulation-mode particles account for a substantial fraction of the total aerosol mass and have the greatest surface area. This makes them of high importance to atmospheric heterogeneous chemistry. Such particles are released through the incomplete combustion of coal, oil, wood, gasoline, etc.

5.2. Fog Activation

For a complete understanding of the activation process, the size distribution and chemical composition of AAs must be taken into consideration. The size of AAs is highly connected with water vapor supersaturation in fogs which is a key for the activation process. Particles are divided into two categories: activated and non-activated particles. In the case the critical supersaturation level (SScr) is lower than the actual supersaturation, particles are activated. In the case the SScr is higher than the actual supersaturation, particles grow to their equilibrium diameters by capturing water but remain inactivated [53][54]. Thus, the ability of CCN to be activated into droplets is determined by the physical and chemical properties of AAs [51][55]. The spontaneous growth of CCN into fog droplets under supersaturated water vapor conditions is described by the classic theory of Kohler. The rate of droplet growth depends on the initial size of aerosols and their solubility [56]. CCN activation depends on the interrelation between the Raoult effect—known as the water activity—and the Kelvin effect. In the Raoult effect, the potential of CCN activation increases with decreasing water activity or increasing solute concentration. In the Kelvin effect, the potential of CCN activation decreases with the decreasing size of the water droplet or increasing surface tension. Through the Raoult effect, certain aerosol particles absorb water vapor at a relative humidity below 100%, and then they grow in size. In this way, they reach sufficient diameters for the Kelvin effect to occur leading to the creation of droplets, absorbing water vapor at their disposal. The transition from the Raoult effect to the Kelvin effect is the activation process of CCN [54][57]. Therefore, aerosols are considered to be “activated” once these droplets reach a certain size, where they are more easily grown within a saturated environment [56].

5.3. Effects of CCN

The radiative effects of aerosols on fog may be classified as direct, indirect, and semi-direct [58]. First, aerosols may scatter and absorb solar radiation (short and long waves). Second, aerosol particles may scatter, absorb, and emit thermal radiation. Third, aerosol particles may act as CCN. The first two mechanisms are the direct effects, while the last one is the indirect effect. The semi-direct effect is a consequence of the direct effect of absorbing aerosols [59][60][61][62]. Direct radiative forcing of aerosols may either cool (nitrates, sulfates, etc.) or warm the atmosphere (black carbon (BC)), depending on the proportion of the scattered light to the absorbed light. The scattering aerosols have a cooling effect on the atmosphere, whereas the absorbing aerosols have a heating effect on the atmosphere. Absorbing CCN is also known to influence fog formation because when air temperature increases, the relative humidity is reduced, prohibiting the appearance of fog or shortening its life in the case it is formed through enhancing droplet evaporation [63]. This is one of the main reasons for declining fog frequency along with the effects of urban heat intensification [42][64][65][66]. Both direct and semi-direct effects of aerosols have been studied by Bott using numerical simulations. The latter shows that urban aerosols containing particularly soot absorb solar radiation and thus increase the cooling rate of the surface and accelerate fog formation. This is the direct effect. The same aerosol that absorbs more solar radiation leads to fog dissipation. This is the semi-direct effect [58].

5.4. Droplet Size Dependence

The chemical composition of fog varies according to the droplet size mainly due to two reasons. The first reason is the inhomogeneous chemical composition of the CCN, while the second reason is the differences in the solubility rates of the gas uptake by small and large fog droplets. Smaller fog droplets are much more concentrated and grow faster than larger droplets as long as there is enough water vapor for condensation. The possible explanations for the enrichment of major inorganic solutes and organic carbon in smaller fog droplets include the higher dissolution rate of CCN in smaller amounts of water, differences in condensational growth, and the higher surface/volume ratio of the small droplets promoting greater surface area for gas/liquid transport and consequently more chemical reactions. The distribution of the chemical components across the aerosol size distribution depends on the chemical composition of the CCN on which the fog droplets form. The smallest activated droplets are formed on the smallest CCN, whereas the largest droplets are formed on the largest CCN. Thus, species contained in small accumulation-mode particles (e.g., SNA) are enriched in smaller fog droplets, and species originally found in the coarse mode such as calcium, magnesium, chloride, and sodium are enriched in larger fog droplets. However, large droplets are unnecessary to be more diluted than the smaller droplets. Through numerical simulations, Pandis et al. stated that droplets whose diameter is 20 μm have a bigger solute concentration than 10 μm droplets by a factor of 3.6 [67]. Thus, fog chemistry varies from one case to another with droplet size including the rate of condensation on CCN, rate of dilution, rate of soluble gas uptake, and rate of chemical reactions (e.g., S(IV) oxidation) [68].

6. Fog Impacts

6.1. Air Quality

The high fog frequency in a particular region affects the air quality of that region. The most popular effect of the fog–aerosol interaction is commonly known as haze or smog (a combination of smoke and fog) [69][70]. There are mainly two forms of smog: the classical smog (London type) [71] and the photo-chemical smog (Los Angeles type) [72]. The latter is caused by the interaction of CO, O3, VOCs, and NOx with solar radiation and occurs near mid-day, especially during the summer season [73]. The classical smog is caused by the interaction of SO2 with PM and takes place in winter and autumn near the ground at temperatures around 0 °C in windless conditions. Once the haze fog contains the atmospheric pollutants, air quality decreases. The trapped NOx and HCs near the ground surface are converted into harmful O3. The greenhouse gases (GHGs) highly spread in the air are also trapped within the stable layer of the inversion zone. All these trapped pollutants in the inversion layer remain suspended and will have an adverse impact on the ecosystem and climate change.

6.2. Human Health

Depending on the chemical and physical nature and composition of fog droplets, fog water has direct and indirect adverse effects on human health (skin and eye damage, respiratory and radiation diseases, secondary health effects, etc.) [74][75][76]. Exposure to fine aerosol particles, especially acidic species, nitric acid sulfur dioxide, sulfur oxide, and microbes, increases the morbidity and mortality of diseases in the respiratory system, cardiopulmonary system, throat irritation, cardiovascular system, muscular system, and lung cancer [74][77]. Exposure to sulfuric dioxide tends to affect the respiratory tract, leading to aggravation in asthmatics. Exposure to nitrogen dioxide demonstrates a slight unfavorable impact on the respiratory system at ambient concentrations. The inhalation of fog with high sulfuric acid concentrations has no clear influence on pulmonary activity, only a slight impact on the respiratory system [78][79]. The relation between asthma patients and air pollution or meteorological factors has been further investigated over a period of two years on 102 adults (44 patients are non-atopic while the rest are atopic). The results show that hospital visits increase on foggy days compared to fog-free days, especially on days with lower pH and low levels of gaseous air pollutants. An increase in hospital visits is observed when the concentrations of NO2 and NO are low in the case of non-atopic patients. Meanwhile, hospital visits of atopic patients increase with decreasing NO2 and SO2 concentrations. The reason might be possibly due to the scavenging of these pollutants by fog which could increase the acidity of fog water. Tanaka et al. state that adverse bronchial epithelium problems might be caused by several possible mechanisms associated with H+, O3, H2SO4, and HNO3 [74]. Thus, the fact that airway resistance caused by acidic pollutants increases might be due to the reduced absorption capacity of the hydrogen ions in the airway mucus [80]. The neutralization of naturally occurring acid fog with ammonia may reduce the impact of the inhaled acid aerosol during foggy days. Ammonia might neutralize about one-quarter of inhalable acid in healthy volunteers [81]. Concerning the meteorological conditions, the high ozone concentrations and the low day-to-day temperature differences lead to an increase in hospital visits for non-atopic patients. In both cases, high water vapor pressure favors the increase in hospital visits [82].

6.3. Transportation and Economy

Fog affects a wide range of human activities. It may cause high costs, inconvenience, and even death [83]. It reduces visibility which acts as a barrier for driving, sailing, or even flying [84]. The total financial and human loss for fog-related transport accidents (sea, air, and land) is approximately the same as that of tornadoes, hurricanes, and winter storms in some cases [11][85]. Adverse visibility and ceiling conditions lead to 35% of weather-related accidents in civil aviation and cause, on average, 168 mortal casualties per year. In fog-prone regions, fog is cited up to 10% of the time as the principal source of accidents, especially in multiple-vehicle crashes. In the case of dense foggy events, airports refuse to accept planes and cancel take-offs due to security reasons such as the cases reported in Canada and the US [6][86]. This may cost the airlines between USD 5,000 and USD 25,000 for any delayed or canceled flight. Concerning sea transportation, many shipping operations are either stopped or slowed-down in the case where the visibility is lower than 0.5 km, and the economic losses typically range between USD 10,000 and USD 25,000/day/ship and cost millions of dollars for moderately active ports [11]. The estimation of the economic losses in 2006 associated with dense fog events in the pre-Christmas period was at least GBP 25 million at seven British airports. Approximately 50 people die yearly in Canada due to vehicle accidents in which fog is the main cause. Fog-related accidents resulted in 13,720 deaths between 1995 and 2004 in the US. The presence of fog led to 1122 fatal air accidents and killed around 229 people in the US between 1982 and 2013. In addition, the Aviation Safety Network reported that six planes have crashed in Iran due to poor visibility conditions, and 353 persons have been killed since 1988 [87]. Overall, a huge number of deaths is reported worldwide in fog-related ship collisions, vehicle crashes, and aviation [84].

6.4. Benefits

Despite the severe negative impacts of fog around the world, it proves its beneficial impacts in terms of water applications, agricultural applications, and ecosystems. Fresh water scarcity has become a major problem facing humanity and is expected to further intensify due to the rapid increase in population density and climate change. Fog harvesting started between 1901 and 1904 in South Africa, and continuous progress has been achieved regarding this issue. The number of its research interests addressing technical aspects, policies, community development, economics, and impacts has increased, in addition to the increase in the operational fog water collection systems over time [88][89][90][91][92]. The number of publications on fog water collection revealed a growing interest and has increased from 4 (between 1981 and 1990) to 223 (between 2011 and 2020), most of them focusing on the experimental or technical part of fog collection [91]. An efficient option to overcome this issue is fog water harvesting using either the standard fog collector (SFC) or the large fog collector (LFC) using mesh nets (Rachel nets). The mesh materials can be nylon, polyethylene, and polypropylene (Shade cloth) which are able to capture different quantities of water from fog [93]. The size of the SFC, which was developed by Schemenauer and Cereceda, is 1 m2, while that of the LFC varies between 40 and 48 m2, and the ratio of width to height must be between 2.5 and 3 [94]. The number of fog collectors depends on many factors such as fog thickness, duration, and frequency, along with the water demand and financial capacity. The collectors are placed perpendicular to the prevailing wind [95]. The cost of the LFC is regulated by the price of mesh varying between USD 25 and 50 per 1 m2. Fog collection starts when fog droplets come into contact with the mesh net standing perpendicular to the fog-carrying winds where they are impacted. As fog droplets increase in size by coagulation, they find their way to the collection reservoir by gravity.

7. Fog Collectors

Fog water collection has a long history. So far, several techniques and collectors have been developed and applied for the collection of fog samples including active and passive fog collectors. Passive collectors solve the problem of unavailable main power at the site. However, they might be contaminated by an unknown fraction of drizzle, conventional precipitation, and horizontal wind-driven rain. Many experiments employ passive fog collectors in which wind is the principal factor that drives fog droplets to the sampler where they are collected via their impaction on strings. The deposition plate is the simplest passive fog sampler. It includes a horizontal plate on which fog droplets are settled. The next fog collector is the string screen sampler. Fog droplets are collected through their impaction on a string screen. The droplets adhere to the string, move down along the string, and are collected in trays [96]. In active fog systems, the air flow containing water droplets is forced by mechanical means using either forced flow through rotating motors or fans and pumps to achieve the same end. The first type of active collector is described by Jacob et al. [97]. In this type, fog condenses on the wires, the baffle smoothes the flow of the air, and the fan pulls the air past the wires. Fog droplets collected on the wires move down the wire and are then collected in a clean bottle. The Caltech Active Strand Cloud Collector (CASCC) is another type of active fog collector developed by Daube et al. [98] and then modified to include droplet-size fractionation [99]. The CASCC has been used in numerous field studies [68][100][101][102][103][104][105][106][107][108][109]. Fog water droplets are collected by inertial impaction on Teflon strands. The strands are inclined 35 degrees from the vertical. The collected droplets condense together and flow down into a Teflon trough by aerodynamic and gravity forces. Samples are then delivered to the collection bottle. Larger CASCCs are described in Fuzzi et al. [110], Minami and Ishizaka [111], and Sasakawa and Uematsu [112].

8. Fog Water Chemistry

Fog consists of water droplets suspended in the air whose diameters typically range from 1 to 100 µm. The LWC is generally smaller than that of rain and cloud waters and varies between 0.01 and 0.5 g m−3. Chemical species found in fogs exist in three phases as gases, interstitial aerosols, and inside the droplet as liquids. The physico-chemical relations among particles, gases, and fog droplets affect fog chemical composition. The incorporation of gases and fine particles into the aqueous phase is a multi-step process. The molecules are first diffused toward the liquid surface where mass transfer across the gas/liquid interface and chemical reactions occur (if any). After that, the species are diffused into the fog droplet [109][113]. The overall atmospheric concentration of any species “i” in fogs is given by Equation (1) [114].
C i t = C i l ∗ L W C + P i R ∗ T − 1 + C i a
where [Ci]t is the total concentration of any species i (mol m−3), [Ci]l is the concentration of the species “i” in the droplet phase (mol m−3), LWC is the liquid water content (dm3 m−3), Pi is the partial pressure of species “i” in the gas phase (atm), R is the universal gas constant (m3·atm K−1 mol−1), T is the temperature (K), and [Ci]a is the concentration of the species “i” in the aerosol (mol m−3).
The LWC is an important microphysical parameter that controls fog chemistry. The solute concentration in fog water is proportional to its atmospheric loading but inversely proportional to the LWC which decreases with increasing the LWC. However, instead of falling along a straight line, it has seen an exponential function of the trend. An increase in LWC in fog water leads to a diluting effect of the solute [115][116][117][118][119][120]. However, LWC alone cannot always explain the temporal evolution in terms of the concentrations [109][111]. The latter is determined by many factors in addition to LWC such as the rate of the chemical reactions, gas scavenging, air masses, and other microphysical properties. Other studies show that no relation exists between LWC and DOC given the differences in gas and particle-phase organic carbon concentrations [109][121]. During the formation stage, the concentration of pollutants tends to be the highest under the high-temperature inversion where the LWC and the surface area per unit volume (S/V) are the lowest. However, the ratio of surface to LWC is large, meaning higher scavenging efficiency with respect to the dilution effect. Therefore, the concentrations stay at high levels. During the maturation stage, the pollutant concentrations tend to decrease dramatically over the course of the fog event. In this phase, the surface area will be higher leading to an increase in the scavenging potential of pollutants and their subsequent deposition. Further, the LWC also rises with the increase in the supersaturation levels in the maturation period of fog leading to a dilution effect. During the dissipation phase, the surface area will be lower again, meaning that the scavenging potential is lower, and thus, the deposition will be smaller. In addition, the LWC is lower, and the ratio of surface to LWC increases, contributing to a gradual increase in the pollutant concentrations [122][123].

8.1. Processes Controlling Fog Chemistry

Fog influences the ecosystem by concentrating, transforming, and depositing atmospheric pollutants into the surface. The interactions between aerosols and fog alter the chemical composition of fog droplets which is governed by aqueous-phase reaction rate and the scavenging effect. Fog droplets can effectively trap pollutants near the surface and enhance the formation of secondary aerosols through liquid-phase oxidation reactions leading to an increase in the aerosol concentration [69][124][125]. Fog may also decrease the ambient aerosol concentration by removing part of the aerosol particles through the continuous scavenging and settling effects [126][127][128]. A decrease in the atmospheric particle loading could increase the ambient supersaturation when ignoring the changes in the source term of supersaturation. In this way, the CCN activation rate increases, altering the chemical and microphysical characteristics of fog [63].

8.1.1. Oxidative Reactions

Fog droplets are considered efficient scavengers of boundary pollutant layers and may provide a favorable environment to produce strong acids through aqueous-phase reactions [121][128][129]. It is evident that aqueous-phase chemistry in fog droplets could lead to a substantial formation of SOA material by transforming volatile gas-phase species to less volatile (semi-volatile) material that remains in the particle phase upon drop evaporation [130]. The size of the new products is larger than their original size [131]. The aqueous-phase oxidation is of special interest for SO2 and NO2 during the occurrence of fogs. The production of S(VI) from the oxidation of S(IV) is one of the most important liquid-phase reactions altering fog acidity, reducing visibility, and causing negative effects on human life and climate [97][128][132]. The production of sulfate may occur in both phases; however, it will be faster in the aqueous phase. One possible mechanism for the oxidation of SO2 includes the gas-phase oxidation of SO2(g) to sulfuric acid (H2SO4(g)), followed by condensation of H2SO4(g). Another possible mechanism might be the dissolution of SO2(g) into an aqueous solution to form sulfurous acid (H2SO3(aq)), followed by the aqueous conversion of the latter to H2SO4(aq). The production of nitrate ( N O 3 − ) is also possible during fog events through an aqueous-phase reaction. Even though the direct oxidation of nitrogen dioxide (NO2) and nitric oxide (NO) is theoretically possible, their kinetics are very slow to produce significant amounts of N O 3 − . The high N O 3 − amount produced through the aqueous-phase reaction is mainly derived from the dissolution of nitric acid (HNO3) or dinitrogen pentoxide (N2O5) and nitrate aerosols. Another pathway might be the oxidation of N O 2 − to N O 3 − in the liquid phase after the production of N O 2 − from nitrous acid (HNO2) [114][133]. 

8.1.2. Acid–Base Interaction

The high acidity of fog water causes severe damage to the environment because of its high potential to destroy materials, vegetation, and human health. Fog is considered acidic when its pH is lower than 5 and alkaline when its pH is higher than 6. The main strong acidic compounds emitted to the atmosphere are H2SO4 and HNO3. The acidity of fog water differs from one region to another due to the presence of many acidic species. In remote environments, fog water droplets are partly acidified due to the dissolution of carbon dioxide (CO2). In regions where the pollution is critical, further acidification occurs by scavenging H2SO4 and HNO3. In polluted and pristine atmospheres, low molecular weight (LMW) carboxylic acids, such as formic and acetic acids, are the major contributors to increased fog water acidity. Carbonyls and dicarbonyls also have a significant role in increasing acidity due to their high levels in the air and their capability to react with the dissolved SO2. However, the presence of some alkaline species (especially N H 4 + , Ca2+, and Mg2+) titrate and neutralize the free acidity under high nitrate and sulfate conditions. They react with HNO3 and H2SO4 at high humidity to produce concentrated ammonium and sulfate salt droplets. 

8.1.3. Fog Scavenging

Fog scavenging is the process through which the suspended particles in the atmosphere are transferred into the aqueous phase of fog water [134]. Organic matter in fog droplets comprises a wide variety of compounds that might enter fog drops either through particle scavenging or through absorption from the gas phase, depending on whether the organic compound is found primarily in the gas or particle phase in the atmosphere; therefore, its entry route into fog drops will differ. Fog scavenging processes reduce the atmospheric loading of aerosols by promoting wet removal and modifying the particle size distribution of aerosols and their hygroscopicity. Previous studies show a decrease of 78% and 65% for ultrafine and accumulation-mode particles, respectively, before and after fog formation [135][136]. This proves the effective scavenging impact of fog on air pollutants and its beneficial effect in washing and cleaning the atmosphere. Fog scavenging mainly takes place either through nucleation scavenging or impaction scavenging. The latter occurs when the interstitial particles (non-activated particles) are incorporated into fog droplets by collision with a droplet, with possible collection mechanisms like inertial impaction, phonetic effects, and Brownian diffusion. However, the former occurs whenever aerosols acting as CCN are activated to generate fog droplets in a supersaturated atmosphere. This pathway mainly dominates in fog aerosol scavenging [117][137]. The scavenging efficiency of different species varies between different chemical species and mainly depends on their water solubility. Studies reveal that fog scavenging removes more water-soluble inorganic components than organic matter [138]. Lower efficiency is observed for carbonaceous hydrophobic species like EC or BC, and higher efficiency is observed for water-soluble species such as SNA [128][137][138].

8.1.4. Fog Deposition

Wet deposition is the process in which particles and gases are removed from the atmosphere by their impaction on the earth’s surface (fog water) or by their absorption into droplets followed by droplet precipitation (rainfall). Wet deposition steadily decreases the atmospheric pollutant loadings in fog droplets during a foggy event. However, the uptake through evaporative water loss upon fog dissipation causes an increase in the pollutant concentrations in the atmosphere. Most fog droplets evaporate before being deposited, altering the chemical and physical properties of the residual particles. These particles become more active, acting as future CCN and promoting future fog formation. This cycle is termed the smog–fog–smog cycle [139]. The importance of the removal process depends on the frequency of occurrence of fog, its duration, and the scavenging efficiency [140]. Fog droplets can be deposited though gravitational settling or turbulent deposition much faster than fine particles are deposited through dry deposition processes. These processes are highly important when fog is in contact with the surface.

References

  1. Hyslop, N.P. Impaired Visibility: The Air Pollution People See. Atmos. Environ. 2009, 43, 182–195.
  2. Manisalidis, I.; Stavropoulou, E.; Stavropoulos, A.; Bezirtzoglou, E. Environmental and Health Impacts of Air Pollution: A Review. Front. Public Health 2020, 8, 14.
  3. Li, X.; Li, P.; Yan, L.; Chen, J.; Cheng, T.; Xu, S. Characterization of Polycyclic Aromatic Hydrocarbons in Fog–Rain Events. J. Environ. Monit. 2011, 13, 2988.
  4. Mohan, M.; Payra, S. Urban Environment of Megacity Delhi, India. Environ. Monit. Assess. 2009, 151, 265–277.
  5. Pérez-Díaz, J.; Ivanov, O.; Peshev, Z.; Álvarez-Valenzuela, M.; Valiente-Blanco, I.; Evgenieva, T.; Dreischuh, T.; Gueorguiev, O.; Todorov, P.; Vaseashta, A. Fogs: Physical Basis, Characteristic Properties, and Impacts on the Environment and Human Health. Water 2017, 9, 807.
  6. Leung, A.C.W.; Gough, W.A.; Butler, K.A. Changes in Fog, Ice Fog, and Low Visibility in the Hudson Bay Region: Impacts on Aviation. Atmosphere 2020, 11, 186.
  7. Peng, Y.; Abdel-Aty, M.; Lee, J.; Zou, Y. Analysis of the Impact of Fog-Related Reduced Visibility on Traffic Parameters. J. Transp. Eng. Part Syst. 2018, 144, 04017077.
  8. Abdel-Aty, M.; Ekram, A.-A.; Huang, H.; Choi, K. A Study on Crashes Related to Visibility Obstruction Due to Fog and Smoke. Accid. Anal. Prev. 2011, 43, 1730–1737.
  9. Frank, G.; Martinsson, B.; Cederfelt, S.-I.; Berg, O.; Swietlicki, E.; Wendish, M.; Yuskiewicz, B.; Heintzenberg, J.; Wiedensohler, A.; Orsini, D.; et al. Droplet Formation and Growth in Polluted Fogs. Contrib. Atmos. Phys. 1998, 71, 65–85.
  10. Croft, P.J.; Pfost, R.L.; Medlin, J.M.; Johnson, G.A. Fog Forecasting for the Southern Region: A Conceptual Model Approach. Weather Forecast. 1997, 12, 545–556.
  11. Gultepe, I.; Tardif, R.; Michaelides, S.C.; Cermak, J.; Bott, A.; Bendix, J.; Müller, M.D.; Pagowski, M.; Hansen, B.; Ellrod, G.; et al. Fog Research: A Review of Past Achievements and Future Perspectives. Pure Appl. Geophys. 2007, 164, 1121–1159.
  12. Gultepe, I.; Milbrandt, J.A.; Zhou, B. Marine Fog: A Review on Microphysics and Visibility Prediction. In Marine Fog: Challenges and Advancements in Observations, Modeling, and Forecasting; Koračin, D., Dorman, C.E., Eds.; Springer Atmospheric Sciences; Springer International Publishing: Cham, Switzerland, 2017; pp. 345–394.
  13. Herckes, P.; Chang, H.; Lee, T.; Collett, J.L. Air Pollution Processing by Radiation Fogs. Water. Air. Soil Pollut. 2007, 181, 65–75.
  14. Mazzoleni, L.R.; Ehrmann, B.M.; Shen, X.; Marshall, A.G.; Collett, J.L. Ultrahigh-Resolution Fourier Transform Ion Cyclotron Resonance Mass Spectrometry Identification of Water-Soluble Atmospheric Organic Matter in Polluted Fog Waters, (Invited). Michigan Tech. 2010, 2010, A14D-01.
  15. Yin, H.; Ye, Z.; Yang, Y.; Yuan, W.; Qiu, C.; Yuan, H.; Wang, M.; Li, S.; Zou, C. Evolution of Chemical Composition of Fogwater in Winter in Chengdu, China. J. Environ. Sci. 2013, 25, 1824–1832.
  16. Beiderwieden, E.; Wrzesinsky, T.; Klemm, O. Chemical Characterization of Fog and Rain Water Collected at the Eastern Andes Cordillera. Hydrol. Earth Syst. Sci. 2005, 9, 185–191.
  17. Kim, H.; Collier, S.; Ge, X.; Xu, J.; Sun, Y.; Jiang, W.; Wang, Y.; Herckes, P.; Zhang, Q. Chemical Processing of Water-Soluble Species and Formation of Secondary Organic Aerosol in Fogs. Atmos. Environ. 2019, 200, 158–166.
  18. Petterssen, S. Weather Analysis and Forecasting, 2nd ed.; McGraw-Hill Publ. Inc.: New York, NY, USA, 1956; Volume 2, 266p.
  19. Willett, H.C. Fog and haze, their causes, distribution, and forecasting. Mon. Weather Rev. 1928, 56, 435–468.
  20. Lewis, J.; Koracin, D.; Rabin, R.; Businger, J. Sea Fog off the California Coast: Viewed in the Context of Transient Weather Systems. J. Geophys. Res. Atmospheres 2003, 108, 2002JD002833.
  21. Tardif, R.; Rasmussen, R.M. Event-Based Climatology and Typology of Fog in the New York City Region. J. Appl. Meteorol. Climatol. 2007, 46, 1141–1168.
  22. Perez-Diaz, J.L.; Alvarez-Valenzuela, M.A.; Sanchez-Garcia-Casarrubios, J.; Jimenez-Lopez, S. Ice Surface Entropy Induction by Humidity or How Humidity Prompts Freezing. arXiv 2015, arXiv:1509.06728. Available online: http://arxiv.org/abs/1509.06728 (accessed on 26 October 2023).
  23. Stolaki, S.; Haeffelin, M.; Lac, C.; Dupont, J.-C.; Elias, T.; Masson, V. Influence of Aerosols on the Life Cycle of a Radiation Fog Event. A Numerical and Observational Study. Atmos. Res. 2015, 151, 146–161.
  24. Zhou, Y.; Niu, S.; Lü, J.; Zhou, Y. The Effect of Freezing Drizzle, Sleet and Snow on Microphysical Characteristics of Supercooled Fog during the Icing Process in a Mountainous Area. Atmosphere 2016, 7, 143.
  25. Byers, H.R. General Meteorology, 4th ed.; McGraw-Hill: New York, NY, USA, 1974.
  26. Saunders, P.M. Sea Smoke and Steam Fog. Q. J. R. Meteorol. Soc. 1964, 90, 156–165.
  27. Økland, H.; Gotaas, Y. Modelling and prediction of steam fog. Contrib. Atmos. Phys. 1995, 68, 121–131.
  28. Gultepe, I.; Isaac, G.A.; Williams, A.; Marcotte, D.; Strawbridge, K.B. Turbulent Heat Fluxes over Leads and Polynyas, and Their Effects on Arctic Clouds during FIRE.ACE: Aircraft Observations for April 1998. Atmosphere-Ocean 2003, 41, 15–34.
  29. George, J.J. Fog: Its Causes and Forecasting with Special Reference to Eastern and Southern United States, (I). Bull. Am. Meteorol. Soc. 1940, 21, 135–148.
  30. George, J.J. Fog: Its Causes and Forecasting With Special Reference to Eastern and Southern United States, (II). Bull. Am. Meteorol. Soc. 1940, 21, 261–269.
  31. George, J.J. Fog: Its Causes and Forecasting with Special Reference to Eastern and Southern United States, (III). Bull. Am. Meteorol. Soc. 1940, 21, 285–291.
  32. Petterssen, S. Introduction to Meteorology, 3rd ed.; McGraw-Hill Publ. Inc.: New York, NY, USA, 1969.
  33. Maalick, Z.; Kühn, T.; Korhonen, H.; Kokkola, H.; Laaksonen, A.; Romakkaniemi, S. Effect of Aerosol Concentration and Absorbing Aerosol on the Radiation Fog Life Cycle. Atmos. Environ. 2016, 133, 26–33.
  34. Ahrens, C.D.; Henson, R. Meteorology Today: An Introduction to Weather, Climate, and the Environment; Cengage Learning: Boston, MA, USA, 2021.
  35. Scott, R.H. Fogs Reported with Strong Winds during the 15 Years 1876–90 in the British Isles. Q. J. R. Meteorol. Soc. 1894, 20, 253–262.
  36. Scott, A. Notes on some of the difference between fogs, as related to the weather systems which accompany them, submitted to the Fog Committee. Q. J. R. Meteorol. Soc. 1896, 97, 41–65.
  37. Mensbrugghe, V. The formation of fog and of clouds, translated from Ciel et Terre. Symons’s Monthly Meteor. Magazine 1982, 27, 40–41.
  38. Poku, C.; Ross, A.N.; Blyth, A.M.; Hill, A.A.; Price, J.D. How Important Are Aerosol–Fog Interactions for the Successful Modelling of Nocturnal Radiation Fog? Weather 2019, 74, 237–243.
  39. Bari, D.; Bergot, T.; Tardif, R. Fog Decision Support Systems: A Review of the Current Perspectives. Atmosphere. 2023, 14, 1314.
  40. Bokwa, A.; Wypych, A.; Hajto, M.J. Impact of Natural and Anthropogenic Factors on Fog Frequency and Variability in Kraków, Poland in the Years 1966–2015. Aerosol Air Qual. Res. 2018, 18, 165–177.
  41. Baldocchi, D.; Waller, E. Winter Fog Is Decreasing in the Fruit Growing Region of the Central Valley of California: DECREASING FOG. Geophys. Res. Lett. 2014, 41, 3251–3256.
  42. Williams, A.P.; Schwartz, R.E.; Iacobellis, S.; Seager, R.; Cook, B.I.; Still, C.J.; Husak, G.; Michaelsen, J. Urbanization Causes Increased Cloud Base Height and Decreased Fog in Coastal Southern California. Geophys. Res. Lett. 2015, 42, 1527–1536.
  43. Van Oldenborgh, G.J.; Yiou, P.; Vautard, R. On the Roles of Circulation and Aerosols in the Decline of Mist and Dense Fog in Europe over the Last 30 Years. Atmos. Chem. Phys. 2010, 10, 4597–4609.
  44. Pruppacher, H.R.; Klett, J.D. Cooling of Moist Air. In Microphysics of Clouds and Precipitation; Mysak, L.A., Hamilton, K., Eds.; Atmospheric and Oceanographic Sciences Library; Springer: Dordrecht, The Netherlands, 2010; Volume 18, pp. 485–501.
  45. Nanev, C.N. Theory of Nucleation. In Handbook of Crystal Growth; Elsevier: Amsterdam, The Netherlands, 2015; pp. 315–358.
  46. Facchini, M.C.; Fuzzi, S.; Zappoli, S.; Andracchio, A.; Gelencsér, A.; Kiss, G.; Krivácsy, Z.; Mészáros, E.; Hansson, H.; Alsberg, T.; et al. Partitioning of the Organic Aerosol Component between Fog Droplets and Interstitial Air. J. Geophys. Res. Atmospheres 1999, 104, 26821–26832.
  47. Seinfeld, J.H.; Pandis, S.N. Atmos. Chemistry and Physics: From Air Pollution to Climate Change, 3rd ed.; Wiley: Hoboken, NJ, USA, 2016.
  48. Tomasi, C.; Lupi, A. Primary and Secondary Sources of Atmospheric Aerosol. In Atmos, Aerosols; Tomasi, C., Fuzzi, S., Kokhanovsky, A., Eds.; Wiley: Hoboken, NJ, USA, 2017; pp. 1–86.
  49. Noone, K.J.; Ogren, J.A.; Hallberg, A.; Heintzenberg, J.; Ström, J.; Hansson, H.-C.; Svenningsson, B.; Wiedensohler, A.; Fuzzi, S.; Facchini, M.C.; et al. Changes in Aerosol Size- and Phase Distributions Due to Physical and Chemical Processes in Fog. Tellus B Chem. Phys. Meteorol. 1992, 44, 489.
  50. Ming, Y.; Russell, L.M. Organic Aerosol Effects on Fog Droplet Spectra. J. Geophys. Res. Atmospheres 2004, 109, 2003JD004427.
  51. Hammer, E.; Gysel, M.; Roberts, G.C.; Elias, T.; Hofer, J.; Hoyle, C.R.; Bukowiecki, N.; Dupont, J.-C.; Burnet, F.; Baltensperger, U.; et al. Size-Dependent Particle Activation Properties in Fog during the ParisFog 2012/13 Field Campaign. Atmos. Chem. Phys. 2014, 14, 10517–10533.
  52. Swietlicki, E.; Hansson, H.-C.; Hämeri, K.; Svenningsson, B.; Massling, A.; McFiggans, G.; McMurry, P.H.; Petäjä, T.; Tunved, P.; Gysel, M.; et al. Hygroscopic Properties of Submicrometer Atmospheric Aerosol Particles Measured with H-TDMA Instruments in Various Environments—A Review. Tellus B Chem. Phys. Meteorol. 2008, 60, 432.
  53. Mazoyer, M.; Burnet, F.; Denjean, C.; Roberts, G.C.; Haeffelin, M.; Dupont, J.-C.; Elias, T. Experimental Study of the Aerosol Impact on Fog Microphysics. Atmos. Chem. Phys. 2019, 19, 4323–4344.
  54. Ovadnevaite, J.; Zuend, A.; Laaksonen, A.; Sanchez, K.J.; Roberts, G.; Ceburnis, D.; Decesari, S.; Rinaldi, M.; Hodas, N.; Facchini, M.C.; et al. Surface Tension Prevails over Solute Effect in Organic-Influenced Cloud Droplet Activation. Nature 2017, 546, 637–641.
  55. Bourcier, L.; Masson, O.; Laj, P.; Chausse, P.; Pichon, J.M.; Paulat, P.; Bertrand, G.; Sellegri, K. A New Method for Assessing the Aerosol to Rain Chemical Composition Relationships. Atmos. Res. 2012, 118, 295–303.
  56. Poku, C.; Ross, A.N.; Hill, A.A.; Blyth, A.M.; Shipway, B. Is a More Physical Representation of Aerosol Activation Needed for Simulations of Fog? Atmos. Chem. Phys. 2021, 21, 7271–7292.
  57. Mazoyer, M. Impact du Processus d’activation sur les Propriétés Microphysiques des Brouillards et sur Leur Cycle de Vie. Ph.D. Thesis, Institut National Polytechnique de Toulouse, Labège, France, 2016.
  58. Iorga, G.; Stefan, S. Sensitivity of cloud albedo to aerosol concentration and spectral dispersion of cloud droplet size distribution. Atmósfera 2007, 20, 247–269.
  59. Charlson, R.J.; Schwartz, S.E.; Hales, J.M.; Cess, R.D.; Coakley, J.A.; Hansen, J.E.; Hofmann, D.J. Climate Forcing by Anthropogenic Aerosols. Science 1992, 255, 423–430.
  60. Haywood, J.M.; Shine, K.P. The Effect of Anthropogenic Sulfate and Soot Aerosol on the Clear Sky Planetary Radiation Budget. Geophys. Res. Lett. 1995, 22, 603–606.
  61. Ackerman, A.S.; Toon, O.B.; Stevens, D.E.; Heymsfield, A.J.; Ramanathan, V.; Welton, E.J. Reduction of Tropical Cloudiness by Soot. Science 2000, 288, 1042–1047.
  62. Lohmann, U.; Feichter, J. Global Indirect Aerosol Effects: A Review. Atmos. Chem. Phys. 2005, 5, 715–737.
  63. Guo, L.; Guo, X.; Fang, C.; Zhu, S. Observation Analysis on Characteristics of Formation, Evolution and Transition of a Long-Lasting Severe Fog and Haze Episode in North China. Sci. China Earth Sci. 2015, 58, 329–344.
  64. Gautam, R.; Singh, M.K. Urban Heat Island Over Delhi Punches Holes in Widespread Fog in the Indo-Gangetic Plains. Geophys. Res. Lett. 2018, 45, 1114–1121.
  65. LaDochy, S.; Witiw, M. The Continued Reduction in Dense Fog in the Southern California Region: Possible Causes. Pure Appl. Geophys. 2012, 169, 1157–1163.
  66. LaDochy, S. The Disappearance of Dense Fog in Los Angeles: Another Urban Impact? Phys. Geogr. 2005, 26, 177–191.
  67. Pandis, S.N.; Seinfeld, J.H.; Pilinis, C. Chemical Composition Differences in Fog and Cloud Droplets of Different Sizes. Atmos. Environ. Part Gen. Top. 1990, 24, 1957–1969.
  68. Collett, J. Internal Acid Buffering in San Joaquin Valley Fog Drops and Its Influence on Aerosol Processing. Atmos. Environ. 1999, 33, 4833–4847.
  69. Zhang, D.; Zhang, Z.; Li, J.; Chang, Y.; Du, Q.; Pan, T. Regulation of Vapor Pressure Deficit by Greenhouse Micro-Fog Systems Improved Growth and Productivity of Tomato via Enhancing Photosynthesis during Summer Season. PLoS ONE 2015, 10, e0133919.
  70. Peng, Z.; Wu, L. A New Perspective on Formation of Haze-Fog: The Fuzzy Cognitive Map and Its Approaches to Data Mining. Sustainability 2017, 9, 352.
  71. Allaby, M. Fog, Smog, and Poisoned Rain; Facts on File: New York, NY, USA, 2008.
  72. Osibanjo, O.O.; Rappenglück, B.; Retama, A. Anatomy of the March 2016 Severe Ozone Smog Episode in Mexico-City. Atmos. Environ. 2021, 244, 117945.
  73. Hu, Y.; Lin, J.; Zhang, S.; Kong, L.; Fu, H.; Chen, J. Identification of the Typical Metal Particles among Haze, Fog, and Clear Episodes in the Beijing Atmosphere. Sci. Total Environ. 2015, 511, 369–380.
  74. Tanaka, H.; Honma, S.; Nishi, M.; Igarashi, T.; Teramoto, S.; Nishio, F.; Abe, S. Acid Fog and Hospital Visits for Asthma: An Epidemiological Study. Eur. Respir. J. 1998, 11, 1301–1306.
  75. Kampa, M.; Castanas, E. Human Health Effects of Air Pollution. Environ. Pollut. 2008, 151, 362–367.
  76. Hutchings, J.W.; Ervens, B.; Straub, D.; Herckes, P. N-Nitrosodimethylamine Occurrence, Formation and Cycling in Clouds and Fogs. Environ. Sci. Technol. 2010, 44, 8128–8133.
  77. Pope, C.A. Respiratory Disease Associated with Community Air Pollution and a Steel Mill, Utah Valley. Am. J. Public Health 1989, 79, 623–628.
  78. Avol, E.L.; Linn, W.S.; Wightman, L.H.; Whynot, J.D.; Anderson, K.R.; Hackney, J.D. Short-Term Respiratory Effects of Sulfuric Acid in Fog: A Laboratory Study of Healthy and Asthmatic Volunteers. JAPCA 1988, 38, 258–263.
  79. Lavorini, F.; Fontana, G.A.; Pantaleo, T.; Camiciottoli, G.; Castellani, W.; Maluccio, N.M.; Pistolesi, M. Fog-Induced Respiratory Responses Are Attenuated by Nedocromil Sodium in Humans. Am. J. Respir. Crit. Care Med. 2001, 163, 1117–1120.
  80. Hackney, J.D.; Linn, W.S.; Avol, E.L. Potential Risks to Human Respiratory Health from “Acid Fog”: Evidence from Experimental Studies of Volunteers. Environ. Health Perspect. 1985, 63, 57–61.
  81. Clark, K.W.; Anderson, K.R.; Linn, W.S.; Gong, H. Influence of Breathing-Zone Ammonia on Human Exposures to Acid Aerosol Pollution. J. Air Waste Manag. Assoc. 1995, 45, 923–925.
  82. Percy, K.E.; Jensen, K.F.; McQUATTIE, C.J. Effects of Ozone and Acidic Fog on Red Spruce Needle Epicuticular Wax Production, Chemical Composition, Cuticular Membrane Ultrastructure and Needle Wettability. New Phytol. 1992, 122, 71–80.
  83. Croft, P.J. Fog. In Encyclopedia of Atmos. Sciences; Holton, J.R., Curry, J.A., Pyle, J.A., Eds.; Academic: San Diego, CA, USA, 2003; pp. 777–792.
  84. Forthun, G.M.; Johnson, M.B.; Schmitz, W.G.; Blume, J.; Caldwell, R.J. Trends in Fog Frequency and Duration in the Southeast United States. Phys. Geogr. 2006, 27, 206–222.
  85. Gultepe, I.; Pearson, G.; Milbrandt, J.A.; Hansen, B.; Platnick, S.; Taylor, P.; Gordon, M.; Oakley, J.P.; Cober, S.G. The Fog Remote Sensing and Modeling Field Project. Bull. Am. Meteorol. Soc. 2009, 90, 341–360.
  86. Wong, D.K.Y.; Pitfield, D.E.; Caves, R.E.; Appleyard, A.J. Quantifying and Characterising Aviation Accident Risk Factors. J. Air Transp. Manag. 2006, 12, 352–357.
  87. Aviation Safety Network. Aviation Safety Database. 2021. Available online: https://aviation-safety.net/database/ (accessed on 12 May 2020).
  88. Olivier, J. Fog-Water Harvesting along the West Coast of South Africa: A Feasibility Study. Water SA 2002, 28, 349–360.
  89. Fessehaye, M.; Abdul-Wahab, S.A.; Savage, M.J.; Kohler, T.; Gherezghiher, T.; Hurni, H. Fog-Water Collection for Community Use. Renew. Sustain. Energy Rev. 2014, 29, 52–62.
  90. Qadir, M.; Jiménez, G.; Farnum, R.; Dodson, L.; Smakhtin, V. Fog Water Collection: Challenges beyond Technology. Water 2018, 10, 372.
  91. Qadir, M.; Jiménez, G.C.; Farnum, R.L.; Trautwein, P. Research History and Functional Systems of Fog Water Harvesting. Front. Water 2021, 3, 675269.
  92. Azeem, M.; Guérin, A.; Dumais, T.; Caminos, L.; Goldstein, R.E.; Pesci, A.I.; De Dios Rivera, J.; Torres, M.J.; Wiener, J.; Campos, J.L.; et al. Optimal Design of Multilayer Fog Collectors. ACS Appl. Mater. Interfaces 2020, 12, 7736–7743.
  93. UNEP. Sourcebook of Alternative Technologies for Freshwater Augmentation in Some Countries in Asia; UNEP, Unit of Sustainable Development and Environment General Secretariat, Organisation of American States: Washington, DC, USA, 1997.
  94. Schemenauer, R.S.; Cereceda, P. A Proposed Standard Fog Collector for Use in High-Elevation Regions. J. Appl. Meteorol. 1994, 33, 1313–1322.
  95. NISA (University of South Africa). Research Report; UNISA (University of South Africa): Cape Town, Australia, 2008.
  96. Lange, C.A.; Matschullat, J.; Zimmermann, F.; Sterzik, G.; Wienhaus, O. Fog Frequency and Chemical Composition of Fog Water—A Relevant Contribution to Atmospheric Deposition in the Eastern Erzgebirge, Germany. Atmos. Environ. 2003, 37, 3731–3739.
  97. Jacob, D.J.; Waldman, J.M.; Haghi, M.; Hoffmann, M.R.; Flagan, R.C. Instrument to Collect Fogwater for Chemical Analysis. Rev. Sci. Instrum. 1985, 56, 1291–1293.
  98. Daube, B.C., Jr.; Flagan, R.C.; Hoffmann, M.R. Active cloudwater collector. U.S. Patent No. 4697462, 25 May 1987.
  99. Munger, J.W. The Chemical Composition of Fogs and Clouds in Southern California. Ph.D. Thesis, California Institute of Technology, Pasadena, CA, USA, 1989.
  100. Khoury, D.; Millet, M.; Jabali, Y.; Delhomme, O. Analytical Procedure for the Concomitant Analysis of 242 Polar and Non-Polar Organic Compounds of Different Functional Groups in Fog Water. Microchem. J. 2023, 185, 108235.
  101. Collett, J.; Daube, B.; Munger, J.W.; Hoffmann, M.R. Cloud Water Chemistry in Sequoia National Park. Atmos. Environ. 1967 1989, 23, 999–1007.
  102. Klemm, O.; Bachmeier, A.S.; Talbot, R.W.; Klemm, K.I. Fog Chemistry at the New England Coast: Influence of Air Mass History. Atmos. Environ. 1994, 28, 1181–1188.
  103. Hoag, K. The Influence of Drop Size-Dependent Fog Chemistry on Aerosol Processing by San Joaquin Valley Fogs. Atmos. Environ. 1999, 33, 4817–4832.
  104. Wrzesinsky, T.; Klemm, O. Summertime Fog Chemistry at a Mountainous Site in Central Europe. Atmos. Environ. 2000, 34, 1487–1496.
  105. Anastasio, C.; McGregor, K.G. Chemistry of Fog Waters in California’s Central Valley: 1. In Situ Photoformation of Hydroxyl Radical and Singlet Molecular Oxygen. Atmos. Environ. 2001, 35, 1079–1089.
  106. Collett, J.L.; Bator, A.; Sherman, D.E.; Moore, K.F.; Hoag, K.J.; Demoz, B.B.; Rao, X.; Reilly, J.E. The Chemical Composition of Fogs and Intercepted Clouds in the United States. Atmos. Res. 2002, 64, 29–40.
  107. Thalmann, E.; Burkard, R.; Wrzesinsky, T.; Eugster, W.; Klemm, O. Ion Fluxes from Fog and Rain to an Agricultural and a Forest Ecosystem in Europe. Atmos. Res. 2002, 64, 147–158.
  108. Ervens, B.; Herckes, P.; Feingold, G.; Lee, T.; Collett, J.L., Jr. Kreidenweis, S.M. On the drop-size dependence of organic acid and formaldehyde concentrations in fog. J. Atmos. Chem. 2003, 46, 239–269.
  109. Lu, C.; Niu, S.; Tang, L.; Lv, J.; Zhao, L.; Zhu, B. Chemical Composition of Fog Water in Nanjing Area of China and Its Related Fog Microphysics. Atmos. Res. 2010, 97, 47–69.
  110. Fuzzi, S.; Orsi, G.; Bonforte, G.; Zardini, B.; Franchini, P.L. An automated fog water collector suitable for deposition networks: Design, operation and field tests. Water. Air. Soil Pollut. 1997, 93, 383–394.
  111. Minami, Y.; Ishizaka, Y. Evaluation of Chemical Composition in Fog Water near the Summit of a High Mountain in Japan. Atmos. Environ. 1996, 30, 3363–3376.
  112. Sasakawa, M.; Uematsu, M. Chemical Composition of Aerosol, Sea Fog, and Rainwater in the Marine Boundary Layer of the Northwestern North Pacific and Its Marginal Seas. J. Geophys. Res. Atmospheres 2002, 107, ACH17-1–ACH17-9.
  113. Ponche, J.L.; George, C.; Mirabel, P. Mass Transfer at the Air/Water Interface: Mass Accommodation Coefficients of SO2, HNO3, NO2 and NH3. J. Atmos. Chem. 1993, 16, 1–21.
  114. Sigg, L.; Stumm, W.; Zobrist, J.; Zuercher, F. The Chemistry of Fog: Factors Regulating Its Composition. ChemInform 1987, 18, 159–165.
  115. Straub, D.J.; Hutchings, J.W.; Herckes, P. Measurements of Fog Composition at a Rural Site. Atmos. Environ. 2012, 47, 195–205.
  116. Aleksic, N.; Dukett, J.E. Probabilistic Relationship between Liquid Water Content and Ion Concentrations in Cloud Water. Atmos. Res. 2010, 98, 400–405.
  117. Elbert, W. Control of Solute Concentrations in Cloud and Fog Water by Liquid Water Content. Atmos. Environ. 2000, 34, 1109–1122.
  118. Elbert, W.; Krämer, M.; Andreae, M.O. Reply to Discussion on Control of Solute Concentrations in Cloud and Fog Water by Liquid Water Content. Atmos. Environ. 2002, 36, 1909–1910.
  119. Kasper-Giebl, A. Control of Solute Concentrations in Cloud and Fog Water by Liquid Water Content. Atmos. Environ. 2002, 36, 1907–1908.
  120. Millet, M.; Wortham, H.; Sanusi, A.; Mirabel, P. Atmospheric Contamination by Pesticides: Determination in the Liquid, Gaseous and Particulate Phases. Environ. Sci. Pollut. Res. 1997, 4, 172–180.
  121. Herckes, P.; Valsaraj, K.T.; Collett, J.L. A Review of Observations of Organic Matter in Fogs and Clouds: Origin, Processing and Fate. Atmos. Res. 2013, 132–133, 434–449.
  122. Nieberding, F.; Breuer, B.; Braeckevelt, E.; Klemm, O.; Song, Q.; Zhang, Y. Fog Water Chemical Composition on Ailaoshan Mountain, Yunnan Province, SW China. Aerosol Air Qual. Res. 2018, 18, 37–48.
  123. Yue, Y.; Niu, S.; Zhao, L.; Zhang, Y.; Xu, F. Chemical Composition of Sea Fog Water Along the South China Sea. Pure Appl. Geophys. 2012, 169, 2231–2249.
  124. Moore, K.F.; Sherman, D.E.; Reilly, J.E.; Collett, J.L. Development of a Multi-Stage Cloud Water Collector Part 1: Design and Field Performance Evaluation. Atmos. Environ. 2002, 36, 31–44.
  125. Nath, S.; Yadav, S. A Comparative Study on Fog and Dew Water Chemistry at New Delhi, India. Aerosol Air Qual. Res. 2018, 18, 26–36.
  126. Li, H.; Wu, H.; Wang, Q.; Yang, M.; Li, F.; Sun, Y.; Qian, X.; Wang, J.; Wang, C. Chemical Partitioning of Fine Particle-Bound Metals on Haze–Fog and Non-Haze–Fog Days in Nanjing, China and Its Contribution to Human Health Risks. Atmos. Res. 2017, 183, 142–150.
  127. van Pinxteren, D.; Fomba, K.W.; Mertes, S.; Müller, K.; Spindler, G.; Schneider, J.; Lee, T.; Collett, J.L.; Herrmann, H. Cloud Water Composition during HCCT-2010: Scavenging Efficiencies, Solute Concentrations, and Droplet Size Dependence of Inorganic Ions and Dissolved Organic Carbon. Atmos. Chem. Phys. 2016, 16, 3185–3205.
  128. Izhar, S.; Gupta, T.; Panday, A.K. Scavenging Efficiency of Water Soluble Inorganic and Organic Aerosols by Fog Droplets in the Indo Gangetic Plain. Atmos. Res. 2020, 235, 104767.
  129. Herckes, P.; Wortham, H.; Mirabel, P.; Millet, M. Evolution of the Fogwater Composition in Strasbourg, (France) from 1990 to 1999. Atmos. Res. 2002, 64, 53–62.
  130. Liu, Y.; Lu, J.; Chen, Y.; Liu, Y.; Ye, Z.; Ge, X. Aqueous-Phase Production of Secondary Organic Aerosols from Oxidation of Dibenzothiophene, (DBT). Atmosphere 2020, 11, 151.
  131. Gilardoni, S.; Fuzzi, S. Chemical Composition of Aerosols of Different Origin. In Atmos, Aerosols; Tomasi, C., Fuzzi, S., Kokhanovsky, A., Eds.; Wiley: Hoboken, NJ, USA, 2017; pp. 183–221.
  132. Sawlani, R.; Agnihotri, R.; Sharma, C.; Patra, P.K.; Dimri, A.P.; Ram, K.; Verma, R.L. The Severe Delhi SMOG of 2016: A Case of Delayed Crop Residue Burning, Coincident Firecracker Emissions, and Atypical Meteorology. Atmos. Pollut. Res. 2019, 10, 868–879.
  133. Acker, K.; Beysens, D.; Möller, D. Nitrite in Dew, Fog, Cloud and Rain Water: An Indicator for Heterogeneous Processes on Surfaces. Atmos. Res. 2008, 87, 200–212.
  134. Collett, J.L.; Sherman, D.E.; Moore, K.F.; Hannigan, M.; Lee, T. Aerosol particle processing and removal by fogs: Observations in chemically heterogeneous central California radiation fogs. Water Air Soil Poll. Focus. 2001, 1, 303–312.
  135. Yuskiewicz, B.A.; Orsini, D.; Stratmann, F.; Wendisch, M.; Wiedensohler, A.; Heintzenberg, J.; Martinsson, B.G.; Frank, G.; Wobrock, W.; Schell, D. Changes in submicrometer particle distributions and light scattering during haze and fog events in a highly polluted environment. Contrib. Atmos. Phys. 1998, 71, 33–45.
  136. Pant, V.; Deshpande, C.G.; Kamra, A.K. Changes in concentration and size distribution of aerosols during fog over the south Indian Ocean. J. Earth Syst. Sci. 2010, 119, 479–487.
  137. Gilardoni, S.; Massoli, P.; Giulianelli, L.; Rinaldi, M.; Paglione, M.; Pollini, F.; Lanconelli, C.; Poluzzi, V.; Carbone, S.; Hillamo, R.; et al. Fog Scavenging of Organic and Inorganic Aerosol in the Po Valley. Atmos. Chem. Phys. 2014, 14, 6967–6981.
  138. Rajput, P.; Singh, D.K.; Singh, A.K.; Gupta, T. Chemical Composition and Source-Apportionment of Sub-Micron Particles during Wintertime over Northern India: New Insights on Influence of Fog-Processing. Environ. Pollut. 2018, 233, 81–91.
  139. Pacyna, J.; Torseth, K. Norwegian institute for air research, (nilu). In Restoration of Forests: Environmental Challenges in Central and Eastern Europe; Springer: Berlin/Heidelberg, Germany, 2012; Volume 30, p. 15.
  140. Barrie, L.A.; Schemenauer, R.S. Pollutant Wet Deposition Mechanisms in Precipitation and Fog Water. Water. Air. Soil Pollut. 1986, 30, 91–104.
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Subjects: Meteorology & Atmospheric Sciences
Contributors MDPI registered users' name will be linked to their SciProfiles pages. To register with us, please refer to https://encyclopedia.pub/register :
Dani Khoury
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Maurice Millet
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Yasmine Jabali
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Olivier Delhomme
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