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MkrGeo

An original point of view

Panoramas, Weather

Horizontal visibility as a main factor of long-distance observations, part 1 – weather, astronomical and optical elements

Navajo Mountain seen from Bryce Canyon National Park

Navajo Mountain seen from the Bryce Canyon National Park.

 

This article is sort of a continuation of issues related to light scattering in the Earth’s atmosphere as well as haze presence. These subjects are closely associated with each other, so some stuff presented here can be pretty much similar and it will be developed on the grounds of my previous articles. This 2-partial article leads to explain when is the best time to attend to long-distance observations and what elements contribute to this kind of tourism and photography.

  1. WHAT IS THE VISIBILITY?

At the beginning let’s say what is the visibility. Visibility has varied and diverse meanings. I will considerate visibility in the meteorological aspect. In meteorology, visibility determines the degree of atmosphere clarity and is usually referred to as the maximum horizontal distance through the atmosphere, that object can be seen by the unaided eye (Bennett, 2016). There are 2 kinds of visibility:
Vertical visibility, that determines how far can we see up or down. In practice, this feature is varied due to meteorological conditions (like planetary boundary layer) described in the previous article. The vertical visibility is also a distance, that an observer can see vertically into a surface-based obscuring phenomenon, such as fog, rain, and snow (McGraw-Hill Dictionary, 2003). In aviation the vertical visibility is the maximum height from which a pilot can recognize ground features when the surface is obscured because of a meteorological phenomenon.
Horizontal visibility, which is usually more important, because it affects our ability to view the distant landscape features. Those distant landscape features are prominent objects, that can be identified with the naked eye, typically referred to the atmospheric or meteorological visual range (Malm, 2016).

Visibility can be treated as an environmental quality that is valued for aesthetic reasons that are difficult to express or quantify (Hyslop, 2009). Everywhere we have locations, that can boast a scenic landscape closer or further. Unfortunately, air pollution and another big haze concentration can degrade closer scenic vistas and obscure those, located further from the observer. The particular matter affects visibility in multiple ways: obscure distant objects drain the contrast from a scene and discolors the sky (Hyslop, 2009).

In previous decades the visibility was almost exclusively used to denote the human capability to detect,  recognize and identify objects. Since the industrial revolution,  when many pollutants have been emitted into the atmosphere visibility emerged as an aesthetic concern especially within protected areas. In this article, I would like to enclose the factors, which influence the horizontal visibility range, highly important for long-distance observation purposes.

               2. INFLUENCE OF THE DIFFERENT FACTORS ON THE HORIZONTAL VISIBILITY    RANGE
2.1. ASTRONOMICAL FACTORS

The most obvious astronomical factor is the diurnal position of the Sun, our other main source of illumination at night. The position of the Sun will determine our angle between the source of illumination and the object observed. In my previous article about the haze, I have developed this topic. When our object is to be found in more or less the same direction as Sun, then it can be hardly recognized due to whitish haze appearance caused by forward scattering. Furthermore, the angle at which the Sun illuminates a vista or landscape feature  (Sun angle) plays another important role. First, at higher Sun angles there is less scattering of light by the intervening atmosphere in the direction of the observer. Second the vista reflects more light; consequently, more image-forming information (reflected photons from the vista) reaches the eye. The contrast detail and scene are enhanced  (Malm, 2016). The distant objects watched on the same part of the sky when Sun is located are more or less shaded by themselves, hence provides fewer details. It is far better to see the objects on the opposite side of the Sun, which is much better illuminated. Conversely is in case of twilight, when objects being on the similar azimuth to Sun plunged in the horizon are better visible due to light scattering properties (see below) (Pic. 1).

Sun shifting against the vista and horizontal visibility

Pic. 1 The effect of progressively shifting Sun angle on the appearance of a vista as seen from Canyonlands National Park. In each image air quality is the same. 1, 2 – represents a moment after sunrise, when the Sun angle-vista-observer geometry results from a large amount of scattered light added to the sight path, which is caused by forward scattering; 4 – a vista around noon, when angular distance to the Sun is the biggest, hence visibility is the best (Malm, 2016).

The effect of change Sun position in horizontal visibility

Pic. 2 The effect of changes in Sun angle as well as the cumulus clouds effect in the La Sal Mountains. The top image shows the vista during the morning, a bottom one the same vista during the afternoon hours. (Malm, 2016).

The situation changes rapidly when looking at the distant objects around sunrise or sunset. To be more precise, a very important moment of the day is a golden hour with Sun above the horizon. This is the time, when surrounding view changes in general. For the Sun angle-vista-observer geometry is very unfavourable due to forward scattering, which increases at the solar azimuth, as Sun goes down. Conversely to solar azimuth, the Sun altitude is low enough to give a decent view towards the antisolar direction. The view towards the opposite side to the solar position is good during a whole period between noon and golden hour, however when Sun is located lower on the sky, then view appears to be the best. This is driven by the extinction, which starts play a big role, hindering some part of direct sunlight on a longer way throughout Earth’s atmosphere. It results from a bit less amount of light scattered on haze particles and molecules, giving a view more discernable. Remote mountains have a bigger contrast against the yellowish sky beyond then (Pic. 3).

Visibility pattern during golden hour webcam Tenerife and La Palma

Pic. 3 Comparison of the visual range at the antisolar point during the morning hours, where the upper image shows a view at 15min after sunrise and lower shows the same view about 1,5h after sunrise. On the left the northernmost part of the Gomera island with Roque de Fuera at 43 km distance. On the right a south part of La Palma island as seen from about 110 km distance. The visibility appears to be slightly better at the golden hour time on the upper image. Webcam location the Royal Sun Hotel near Los Gigantes at the Tenerife island (Deckchair.com).

When sunlight diminishes around sunrise or sunset then remote objects seem to be visible better in all directions, except an exact solar azimuth. This is the time, when direct sunlight scattering on aerosols vanishing (Pic. 4, 5). Indirect sunlight conditions the haze particles or air molecules eliminates the visual contrast that would have made the most distant horizon visible. The contrast changes depend on the illumination and extinction coefficient.

Visibility sunrise sunset 45 min seen through webcam Tenerife and Gomera

Pic. 4 A visual range comparison on shifting solar position at the same moments against sunrise and sunset. 1 – view at 45m after sunrise; 2 – view at 45m before sunset, where: 1 a distant La Palma island is seen from 110km, which doesn’t appear on image 2. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com)

Horizontal visibility sunrise sunset 15 min webcam Tenerife and Gomera

Pic. 5 A visual range comparison on shifting solar position at the same moments against sunrise and sunset. 1 – view at 15m after sunrise; 2 – view at 15m before sunset. Comparing to the Pic. 3 both vistas appear to look more clear due to vanishing sunlight. Moreover, a local sunset transition is to be noticed in image 2, where: A – shows sunlit haze and B shows shaded haze. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com)

Horizontal visibility sunrise sunset webcam Tenerife and Gomera

Pic. 6 A visual range comparison on shifting solar position at the same moments against sunrise and sunset. Comparing to the Pic. 3 and Pic. 4 both vistas appear to look the best due to tailing off a direct sunlight scattering on the near-ground conditions. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com).

The extinction coefficient means how quickly the beam is attenuated as it passes through the medium. The small extinction coefficient means, that the medium is relatively transparent to beam. For example, our beam is a remote object and the medium is the air. Diminishing and disappearing sunlight when the sky remains bright push the contrast threshold of the human eye makes the distant target visible (more details in the next part of this article). The air molecules and haze particles don’t scatter the sunlight anymore. Sunset marks the moment when forward scattering disappears. The opposite situation occurs daily at sunrise, where forward scattering appears again. This moment is called a sunrise or sunset transition, which has been described more in my previous article. A practical explanation of this phenomenon can be found in Pic. 6, when looking at points A and B marked by the red arrow. They show a rough sunset transition moment, which changes a visual range abruptly. At the Pic. 6, image 2 the point A is an example, where forward scattering still occurs due to direct sunlight presence. Point B is already shaded with a lack of direct sunlight scattering, which makes far better contrast against still illuminated the lower part of the atmosphere. It makes, that our object is perfectly visible.
Forward scattering usually makes an object less visible than backward scattering. When forward scattering disappear it gives way to see the remote objects, that we were not able to see during the sunlight conditions (Pic. 7).

Horizontal visibility before and after sunrise, sunrise transition seen on webcam Florence

Pic. 7 A visual range comparison at the sunrise transition moment, where a forward scattering starts to play a serious role. View from the Westin Excelsior at Florence towards Tuscan-Emilian Apennines ranges located 15-25 km ahead (Deckchair.com).

Sunset transition seen on Tatra Mountains

Pic. 8 A perfect example of sunset transition. Tatra Mts seen from about 130km distance (Poland), where yellow arrows show peaks, located behind the still illuminated haze, where direct sunlight scattering plays the main role. Conversely, the shadow, marked blue, is deprived a direct illumination. Illuminated peaks marked by the yellow arrow are much less visible than others. This situation can last even a few seconds, until the Sun hides behind mountains afterward, making them all perfectly visible (credits: Damian Bogacz).

After the sunset, the light scattering takes place in the atmosphere. For our line of sight, we face a secondary scattered light, present in the lower, shaded part of the atmosphere. Moreover mostly the atmospheric aerosols have an extinction coefficient decreasing in magnitude with increasing wavelength (Horvath, 1967).

Horizontal visibility at civil twilight in webcam La Palma and Gomera from Tenerife

Pic. 9 A visual range comparison when Sun is 3 deg below the horizon at the symmetric moments against noon. In this case, the much better view is in the evening, when Gomera and La Palma are located near the solar azimuth. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com).

Horizontal visibility at he beginning of civil twilight via webcam Gomera from Tenerife

Pic.10 A visual range comparison when Sun is 6 deg below the horizon (civil twilight) at the symmetric moments against noon. In this case, the much better view is in the evening, when Gomera and La Palma are located near the solar azimuth. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com).

We have to bear in mind that a favourable visibility conditions after sunset will last as long as the stratosphere (ozonosphere) is illuminated (Pic. 10, 11). After this, the light scattered in the upper part of the atmosphere is too weak to make a good contrast with the distant object observed.

Horizontal visibility at nautical twilight via webcam Gomera seen from Tenerife

Pic. 11 A visual range comparison when Sun is 9 deg below the horizon at the symmetric moments against noon. In this case, the much better view is in the evening, when Gomera and La Palma are located near the solar azimuth. In the evening, the La Palma is near the “edge” of the stratosphere illuminated, hence is becoming invisible for the observer. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com).

Horizontal visibility at nautical twilight under moonlight condition via webcam

Pic. 12 A visual range comparison when Sun is 12 deg below the horizon (nautical twilight) at the symmetric moments against noon. In this case, the visible objects appear only at the solar azimuth during the evening, unless Moonlight dominates on the sky, making objects visible (after longer exposure) even in the antisolar direction. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com).

In the nighttime hours is really hard to distinguish some distant object, unless they are illuminated by local light pollution or moonlight. In the second case everything is going to be analogous to daylight conditions, however capturing proper pictures will require a long time exposure, unlike webcam example provided. (Pic. 13).

Horizontal visibility under moonlight conditions captured by webcam at the Tenerife

Pic. 13 A Gomera and La Palma island seen from the Tenerife, where: 1 – moonless night, 2 – moonlight with antilunar direction, 3 – moonlight with the Moon-vista-observer view geometry. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com).

Widok nocą spod schroniska PTTK Turbacz na Pasmo Łososińskie

Pic. 14 An example of visibility conditions during the night at 3rd quarter Moon and some light pollution in places. A view from the Turbacz mountain hostel towards the Łososina range, seen from about 40km and captured by simple compact camera Canon A540, ISO 100, 15s  f.2/6, gamma modified.

Now let’s see an example of a perfect quality of distant view in the night conditions, as we can gain with long exposure and light pollution assist (Pic. 15).

Tatry z Pradziada Artur Robak

Pic. 15 Tatra Mts seen from Pradziad, 200-240 km distance (credits: Artur Robak).

To summarize this section I would like to show the visibility conditions under a different Sun position against the horizon at the antisolar direction, unaffected by forward scattering.

Horizontal visibility at antisolar direction from Tenerife

Pic. 16 The visual range comparison within different solar position altitude horizon at antisolar direction, where: 1 – 4 deg below the horizon; 2 – 3 deg below the horizon; 3 – 2 deg below the horizon; 4 – 1 deg below the horizon; 5 – sunrise; 6 – 5 min after sunrise; 7 – 15 min after sunrise; 8 – 1h after sunrise. Optionally image 7 shows the best conditions for long-distance observations as well as potentially image 5, where a distant view unobstructed by illuminated haze can be merged with the horizon not bright enough. View from Royal Sun Hotel near Los Gigantes at the Tenerife. (Deckchair.com).

Looking on pic. 16 we can say straight, that the best visibility conditions at the Sun – observer – vista geometry occur about 15-20 min after sunrise or before sunset, which has been marked in image 7. Some of you will ask, why particularly at that moment, whereas image 5 shows even better conditions for La Palma island. The point is, that the sunrise or sunset transition at antisolar direction is to be seen in the sky too. In the consequence, these objects, which lie very far from the observer can be merged with the receding twilight wedge, which makes the horizon still not bright enough. Only the prominent mountains, which are high enough, can rise above this line, making a decent contrast between themselves and bright sky beyond, as the La Palma island does in the example provided.

Below I have gathered all major moments when visibility towards particular direction changes throughout the day (Pic. 17, 18).

Horizontal visibility during the day senn via webcam in Florence morning

Pic. 17 View from the Westin Excelsior at Florence towards Tuscan-Emilian Apennines ranges located 15-25km ahead, where:  1 – At nautical dawn; 2 – at civil dawn; 3 – at Sunrise; 4 – 5min after Sunrise; 5 – 15 min after sunrise; 6 -30min after sunrise; 7 – 1h30m after sunrise; 8 – 3h after sunrise; 9 – at noon; 3,4sunrise transition moment (Deckchair.com)

Horizontal visibility during the day afternoon via webcam in Florence

Pic. 18 View from the Westin Excelsior at Florence towards Tuscan-Emilian Apennines ranges located 15-25km ahead, where: 1 – at noon; 2 – 3h before sunset; 3 – 1h30m before sunset; 4 – 30m before sunset; 5 – at sunset; 6 – 15min after sunset; 7 – at civil dusk; 8 – 50m after sunset; 9 – at nautical dusk (Deckchair.com)

It’s good to mention also about a seasonal variation of the sunrise and sunset azimuth, also in understanding with civil and nautical twilight azimuth, which can improve or deteriorate the visual range at a particular direction.
An important astronomical factor, which can decide about seeing the distant objects, even when they are totally hidden behind a thick haze is solar ephemera. Knowing roughly an azimuth of sunrise or sunset we can try to capture a distant mountain on its disk (Pic. 19). It also works in the case of Moon, however, when haze is too thick Moon tends to disappear before the set.

2018-09-18 Polonina Caryńska zachód Słońca Tatry

Pic. 19. Sunset roughly above Tatra Mts, as seen from Połonina Caryńska in Bieszczady (Poland) at about 170km distance. Normally these mountains were invisible that day (credits: Adrian Weimer).

A lunar ephemera may help to capture a distant object only when haze concentration is low. Then a moonrise or moonset above some remote and not illuminated enough object will be beneficial (Pic. 20).

Zachód Księżyca nad Tatrami

Pic. 20 Stacked moonset above the Tatra Mts. as seen from about 130km distance (credits: Tomasz Ziajor).

The details of checking the solar and lunar ephemera have been described in this article.

2.2. WEATHER FACTORS

A. AIR MASSES

Every air mass provides different conditions of horizontal visibility. I am going to remind a bit of some stuff from my previous article, where I shortly explained the air mass influence on the visual range. Basically, the map below shows the types of air masses, as an influence on the weather throughout the year (Pic. 21).

Air masses type coming to Europe

Pic. 21 Type of air masses creating a weather conditions in Europe throughout the year (based on Europe physical map from Geology.com), where: Ac – Arctic continental, Pc – Polar continental, Tc – Tropic continental, Tm – Tropic maritime, rPm – returning Polar maritime, Pm – Polar maritime, Am – Arctic maritime.

The Arctic air mass, which we can divide on continental and maritime one is the clearest, which comes to Europe. The reason for its transparency lies in the lowest amount of particles coming from the local basement. The polar regions are (at least now) mostly covered by ice and snow, hence all particles, which could potentially be blown by wind are trapped underneath. It makes the arctic mass the clearest air mass, as we can see. However, it’s good to point out, that the clearest is the Arctic continental air mass, which comes to Europe from Barents Sea direction. The Arctic maritime air mass may contain some marine aerosols, which will impair the visibility a bit. Moreover, this kind of air mass always features a bigger humidity level (showers in places), which is unfavourable for visibility too.
Because of increasing pollution around the Globe, we must be aware, that arctic air mass contains some arctic haze, which enters from lower altitudes and urban areas through the long-range pollution pathways.
An Arctic air mass comes to northern and central parts of Europe. Usually, this air mass is transformed, when entering on the southern part of the continent.

The polar maritime air mass is another common air mass, which influences the weather in Europe. Within this air mass, we can make a division between Polar maritime air mass and returning Polar maritime air mass. The second one arises out of a long journey above the sea surface, which takes the air first southwards the North Atlantic and next north-eastwards towards western Europe. In general, Polar maritime air mass brings good, or even excellent visibility depending on the period of the year, when hit the ground (is ground warmer or colder) and local weather patterns (some showers in places may strongly interrupt a visual range). We can expect this air mass when the wind blows from west and north-west towards Europe. A returning polar maritime air mass feature only moderate visibility due to big humidity and marine aerosols concentration. It comes usually from WSW and SW directions to continental Europe.

Horizontal visibility under arctic and polar maritime air mass Tatras from Bieszczady, Carpathians

Pic. 22 A Tatra Mts saw from Wielka Rawka at Bieszczady Mts (Poland), located about 170km ahead. The photo contains a vista under 2 different conditions, where: 1 – at the Arctic continental mass influence; 2 – at the Polar maritime air mass influence. The basic difference between these 2 masses lies in transparency. Because arctic air mass doesn’t contain a haze, the observer is capable to distinguish even relief of distant objects, rather than outline only, which is featured by polar maritime air mass, due to a maritime haze presence. Anyway, in both cases we can say, that visibility is excellent (Image 1 credits: Dominik Jakubowski).

Polar continental air mass influences a bit less into the weather in Europe, because the western winds take hold for most of the year on the continent. However, during the winter period, the frequency of this air mass is bigger, than during the summer. Next to more extremal temperatures, as we can observe under this air mass condition, the visual range is rather moderate or good, but not perfect. Despite a low level of humidity, this kind of air mass may contain a lot of continental haze (rural continental aerosols) or some pollutants, especially during the summer. In winter, when eastern Europe is covered by snow, this air mass features better visibility conditions.

Horizontal visibility conditions under polar maritime and returning polar maritime air mass

Pic. 23 View on Ely Cathedral from New Farm at Reed near Royston (UK) at 47 km distance, where: 1 – view at returning Polar air mass influence; 2 – view at Tropic maritime air mass influence. A returning air mass influence brings usually a moderate or at most a good visibility with a range about 100 km.

Horizontal visibility under tropical maritime air mass Snowdonia National Park

Pic. 24 View from Llanberis, Llyn Peris to towards Pen Y Pass and Mt. Snowdon range (UK), located only 8 km ahead. This is an example of extremely poor visibility due to strong Tropic maritime air mass influence on the much colder ground spreading through the Cambrian Mts.

Tropical maritime air mass usually coming to Europe from the southwest. In all periods of the year, this air mass brings the higher temperature and big humidity, which results in a really poor visibility. Because this air mass is originated at tropical latitudes, it features very often higher temperatures, than the ground underneath, which leads to additional humidity increment.

The tropical continental air mass is the last type of air mass, that enters Europe from time to time. Likewise a maritime one, the tropical continental maritime usually plays a big role in the Mediterranean region, unlike central Europe, where it comes occasionally. Usually, this type of air mass brings much higher temperatures and dry air, often abundant with dust from the desert. In this configuration, combined with a usually colder surface, the visibility conditions are also quite poor, or at most moderate.

Planetary boundary layer seen above Bieszczady Mountains

Pic. 25 View from the Wielka Rawka peak at Bieszczady Mts towards invisible Tatra Mts under Tropic continental air mass influence. The planetary boundary layer has been strongly emphasized due to a high dust concentration (credits: Robert Bogacz).

Because this article can read people from another part of the world I would like to mention another two major air masses, that are an equatorial and antarctic one.

Equatorial air mass has only maritime features. It usually brings frequent thunderstorms and high temperatures. In this case, the visibility conditions are usually restricted and depends on local weather pattern only. However, even in this climes, some days with decent visibility can be recorded (Pic. 26). Higher air mass temperature has an ability to store a bigger amount of water, decreasing a humidity level at once.

Raung seen from Uluwatu, horizontal visibility under equatorial air mass

Pic. 26 Partially covered by cumulus clouds the Raung volcano as seen from the Uluwatu Temple (Indonesia) at about 140km distance. This is one of the most distance views as we can get under equatorial air mass conditions. The picture has been dehazed a bit.

Antarctic air mass has only continental features due to massive land surrounding a south pole. This air mass appears to be the clearest air mass observed on the Earth, especially now, when the ice sheet on the arctic area has been melting down. This the most transparent air mass can be polluted only by arctic haze, which origin is the same as in the arctic.

B. VISUAL RANGE CHANGES INSIDE A PARTICULAR AIR MASS

Previously I have considered the usual characteristics of the visibility conditions in the main type of air masses, however, there are many variations in individual air masses (Ackerman, Knox, 2007).
These changes are:
Day-night – day humidity variations – the humidity is getting lower as the day warms, hence visibility is believed to be better during the midday time hours and usually the best on the early afternoon, which is the warmest period of the day (Pic. 27, 28). A humidity level can be also modified by wind speed.

Humidity changes meteo.icm.edu example

Pic. 27 A humidity changes between 29.11 and 1.12.2018 on Rzeszów (Poland). The lowest level of humidity tends to occur on the early afternoon, when weather is stable (Meteo.icm.edu.pl).

Percentage of the particular visual range conditions at Carpathian Foothills

Pic. 28 A percentage of the visual range throughout the year at the Gaik-Brzezowa weather station on Carpathian Foothills (Lesser Poland). The chart clearly shows, that the best visibility appears to be in the early afternoon in southern Poland (credits: Grzegorz Luranc dissertation).

 – Air turbulences – plays also a huge role throughout the day and are strongly associated with the humidity variations under convective weather conditions. When the temperature rises, the steaming from the ground rises too and vertical turbulent updrafts become stronger. More intensive steaming from ground leads to increased humidity, which next is transported up, resulting from a cumulus clouds development, just above the planetary boundary layer. This humid air is superseded by drier air, coming from a “free atmosphere”, that penetrates down. The result of this phenomenon is easy to spot between morning and early afternoon. In the morning our vista is misty, whereas the sky is free of clouds. After a few hours, when vertically developed clouds drift across the sky, our vista is a bit more clear. These situations can be observed usually during a warm period of the year.

 – Atmospheric pressure – a high atmospheric pressure leads to low wind speed, which causes increased pollutant concentration close to the pollutant sources and visibility deterioration  (Majewski et. All, 2015) unlike low pressure, which due to increasing wind speed provides effective ventilation, especially for urban areas. The low-pressure conditions are associated with convective weather, as described above.  Convective weather produces low-pressure areas with convergence winds. A low-pressure area is produced at the boundary between warmer and colder air mass. More information about this will be provided in the next section. The opposite situation occurs under anticyclone weather conditions, when atmospheric pressure is higher. Then weather can be more stable for a longer time, resulting in a subsidence inversion development. This subsidence inversion can develop up to 2 km above ground depending on the pressure level. The subsidence inversion is a result of atmospheric pressure increases, which leads to air compression and heating. Warming of this air increases evaporation, causing usually clear skies within high-pressure systems. This inversion resists convection of surface air since the surface air is stable and causes air pollution to be trapped at the surface. As the result the visibility is really poor within this inversion layer, unlike the area above, which is unusually clear due to unusually dry air (Pic. 28) In the meantime underneath, where visibility is higher, some horizontal cloud development may occur. These clouds are difficult to disperse during the winter when the sun shines too low above the horizon and provides too weak radiation.

Mala Fatra subsidence inversion Slovakia

Pic. 29 A good example of subsidence inversion at Mala Fatra Mts. (Slovakia), which strongly divides the areas of opposite visibility conditions. Moreover, in places stratus clouds are produced. the height of this inversion depends on the pressure (Astropolis.pl).

Subsidence inversion is different between winter and summer. In the warm period of the year, this inversion is less pronounced, at least during the day, when tails off due to much stronger solar radiation unlike in winter. Hence we won’t observe a vast visibility difference between the inversion layer and layer above, as we can see in a colder part of the year.

 – Temperature – is also an important weather element, which merges with pressure and humidity issues. Once the temperature is higher, then the water, being on the ground has a bigger ability to evaporation, however, a single air cube has a bigger volume at once. Then in wet areas, especially when water is colder than air the visibility conditions won’t be favourable. On the contrary, rising temperatures above dry (or frozen during the winter) landmass will decrease humidity, making a visual range more extended (like in the desert areas in the western USA). Inside the inversion layer, where the temperature is lower, the humidity level is higher, what we can see in a mist, fog or partially developed cloud deck.

Seasonal variations – can be significant, depends where you live. In marine climes, there won’t be as considerable difference as in continental climates. However in general the time with the best visibility occur during the winter, when low temperature hinders steaming from the ground and when cooler and clearer air masses take hold. For instance, a dry continental Polar or Arctic mass usually extends visual range during the winter, because these masses travel across a massive land covered by snow. However, it refers to the upper part of the air, which lies above the inversion layer, described below. A season with the worst visibility is the summer when high temperature causes intensive heating and steaming from the ground and water. Then humidity increases, impairing visibility. This situation can turn rapidly when much colder air mass approaches, what happens from time to time, usually after a heatwave.  Then, if the surface over which an air mass is located is warmer than the air mass, the lower layers will be heated. It incurs a decrease of humidity and good visibility. This situation is observed when colder maritime air mass comes on the warmer continental surface (Pic. 30). The opposite situation can be observed during the spring or winter, when much warmer air mass comes onto the surface, which is colder. Then the lower layers are gradually cooled. As the result water vapor and atmospheric impurities tend to be concentrated in low layers decreasing the visibility effectively (Pic. 31).

Horizintal visibility under polar air mass Split Croatia

Pic. 30 One of the best visibility conditions is just after passing a cold front and entering a colder Polar marine air mass on much warmer surface. Split and Biokovo Mts beyond (Croatia), seen from 35-40 km distance.

Horizontal visibility under tropical air mass Wales

Pic. 31 One of the worst visibility conditions after entering much warmer Tropical maritime air mass onto the colder area. View on Carnedd Llewelyn 1064m in Snowdonia National Park from Beaumaris at Anglesey island, located at only 14 km distance.

Except for the tropic air mass advections, spring as a period feature one of the best visibility conditions, becuase the temperature is still low and ground still cool, which prevents of steaming. Polar continental air mass, which enters to Europe doesn’t contain many aerosols, because this mass originates above still snow-covered (or if not, wet) areas of Eurasian inland. Arctic air masses can also occur during this time.
Autumn is a period with also good visibility, when a Polar maritime or Arctic mass occurs. During this time poor visibility can be observed during Tropic and Polar continental air mass advections. Another favourable factor for good visibility during the autumn is limited cloudiness in this period of the year.
The situation will be different i.e. in the USA, where excellent visibility is observed also during the summer. It arises out of a dry huge massive of land and high temperatures. Moreover, the period of the worst visibility doesn’t indicate, that moments with good atmospheric clarity won’t occur. It depends on the local weather pattern, being various between years.

Wind speed and direction – a good example here is the Foehn – a rain shadow wind (Pic. 31), which passes over the mountains and lose most of its moisture on windward slopes.

Foehn wind general pattern

Pic. 32 A general mechanism of the foehn wind occurrence (Wikimedia.org).

Being deprived of humidity at the leeward side this wind brings good or even perfect visibility conditions next to the pleasant warm (Pic. 32). Usually watching the main mountain range, above which a Foehn wind passes over an observer can spot a cloudy wall.

Widok na Tatry z Gór Świętokrzyskichi

Pic. 33 A foehn wind can bring excellent visibility conditions with an achievable visual range up to 200km or even more. Tatra Mts with foehn wall cloud as seen from about 200 km distant Świetokrzyskie Mts (Poland)(credits: Natan Bugajski).

Wind plays a leading role in clearing the atmosphere from air pollutants. Usually, under windy conditions, the visibility appears to be better. On coastlines, when the wind is strong a lot of foam and seawater droplets are risen from the seafloor reducing the visibility considerably (Pic. 34).

Santander coast Spain and a lot of maritime aerosols

Pic. 34 A strong wind blowing from the sea can rise a lot of water droplets and maritime aerosols, making a misty appearance. View from Santander coastline near Palacio de Magdalena on Faro de Cabo Ajo with a lighthouse at the 15 km distance.

 – The atmosphere density – varies in a vertical profile. As height increases the density of the atmosphere is lower. The densest atmosphere is in the lowest part of the planetary boundary layer, which is called as a surface layer (Pic. 36). Usually, the visibility range is the worst there and improves as altitude increases (Pic. 35). We can often see it on the pictures with a separated mountain ranges, which appear to look slightly more fuzzy at the bottom. However, in very transparent atmosphere conditions this phenomenon appears too and can be mistaken with the Mach Bands optical illusion, which has been described in my previous article (Pic. 37). A considerable improvement of the visibility is noticeable when crossing the planetary boundary layer or at least the inversion layer.

Navajo Mtountain seen from Bryce Canyon National Park

Pic. 35 A Navajo Mt. as seen from Bryce Canyon National Park at 131 km distance (Utah, USA) is a good example of visual range changes in the vertical profile. Whereas a top of the mountain is transparent, the bottom slopes plunge in the haze, which become bigger as close to the main ground level (surface layer).

Tatry z Zagorzyc (Witold Ochał) mach bands

Pic. 36 Zoomed view on Tatra Mts from Zagorzyce (Lesser Poland) at about 130 km distance with a clear influence of the surface layer with slightly bigger haze concentration (credits: Witold Ochał, Vitoos.blox.pl).

Mach bands example, Bryce Canyon National Park

Pic. 37 A few separate mountain ranges seen from one place look a bit different due to haze presence, especially in the surface layer. However, under excellent visibility conditions, the surface layer haze can be easily mistaken witch the Mach Bands optical illusion. Bryce Canyon National Park – looking towards Grand Staircase-Escalante National Monument, Utah, USA.

 – Cloud cover – this is ambiguous for visibility conditions. In general, the clouds shouldn’t affect on air transparency, although their presence interrupts a visual range so much. First of all, the “safest” cloud decks for visibility conditions are the high-level or some mid-level clouds (i.e. cirrostratus, altostratus), which prevents a vista from solar beams and their scattering. On top of that these clouds often make a better contrast with distant objects, at least during the day (Pic. 38).  More details about this I wrote in the next section below. Once lower levels of clouds or vertical developed ones are present on the sky, then our visual range can be interrupted. Some prominent mountain ranges can appear on the same level or even above the cloud layer and be invisible for the observer (Pic. 39).

Kral'ova Hola widiana z Magury Wątkowej

Pic. 38 Low Tatra Mts. (Kralova Hol’a) seen from Magura Wątkowa (Poland) from about 120 km. The sky was veiled by cirrostratus clouds, that made a whitish appearance, giving a better contrast with remote mountain outlines.

Kralova Hola seen from Spisska Magura

Pic. 39 Low Tatra Mts (Kralova Hol’a range) as seen from the Veterny Vrch summit (Spisska Magura)(Slovakia) at about 60km distance. Despite decent visual range under Polar maritime air mass, the mountain ranges are not fully visible for observer due to thick thunderstorm clouds presence. For longer distances, the mountains can merge with clouds and being totally invisible.

Situation changes, when Sun is below the horizon enough, being not able to illuminate the clouds, which for solar direction means a moment of civil twilight (for high-level clouds only). Then clouds usually reflect a light scattered in the atmosphere (or another remote cloud) only, which is too faint to give them a bright appearance. Contrasting with the still bright section of the sky around solar azimuth, these clouds look dark grey or completely dark at deeper twilight. As the result a contrast between them and distant objects is really low. Even if visibility is very good an observer is not able to spot the remote mountain (Pic. 11, 40), unless the clouds are patched in places (Pic. 41).

La Palma seen from the Tenerife via webcam

Pic. 40 View from Royal Sun Hotel near Los Gigantes at the Tenerife towards La Palma island located about 110 km ahead (marked by the red rectangle), which is covered by thick and shaded stratocumulus cloud, which reflects the light only scattered in the atmosphere. As the result it appears to look dark grey likewise the mountainous island beneath. It makes a very low contrast between the cloud and island, making this land almost invisible (Deckchair.com).

Tatra Mts Krzysztof Augustyn and high level cloud deck

Pic. 41 When the cloud layer is patched or thin enough, then even after sunset remote mountains can be visible (Tatra Mts saw from about 130 km distance)(Poland)(credits: Krzysztof Augustyn).

In general, as long as the high-level cloud reflects direct sunlight, even red, the contrast between shaded distant mountain below is decent to make it still visible (Pic. 42). Unfortunately, it happens only, when the clouds are thin enough, leading solar beams to overexpose them. Otherwise, their bases won’t be able to make a good contrast with a distant land, which is perfectly visible in the case of stratocumulus clouds versus for example cirrus ones.

View on Mogielica, horizontal visibility changes in terms of cloud illuminance by Sun

Pic. 42 A zoomed view on Mogielica Mt. from the Dynowskie Foothills at about 110 km distance (Poland). Comparison of the vista just before and just after sunset with high-level cirrostratus clouds and mid-level stratocumulus clouds present on the sky. In both cases, the stratocumulus cloud, because of their thickness deteriorates the vista considerably, when located at the observer – object – cloud geometry. Cirrostratus, because is thin enough, remains overexposed and as long the Sun illuminates it, the contrast with the distant object is fair enough to make it clearly visible.

C. AIR MASS DYNAMIC IMPACT ON VISIBILITY

Previously I described weather elements, which can influence visibility conditions within one particular air mass. Now we should consider the visual range changes in terms of more than one air mass.

Pressure systems are the main weather patterns, which causes the air mass dynamics. We have a high and low-pressure area. High-pressure areas form due to downward motion through the troposphere. Weather, typical for high-pressure systems has been described above. Usually, a high-pressure system brings stable weather with one air mass laying in some area.
Let’s talk more about low-pressure areas, which very often cause an air masses movement. Low-pressure area forms as a result of convective motions, which leads to pressure drop and convergent winds, blowing from outside to inside. Another way to form a low-pressure area is the temperature gradient between two different air masses. It results in creating two noticeable borders between these 2 (or sometimes more) air masses. These borders are a cold front and warm front (Pic. 43).

Low pressure system pattern

Pic. 43 A typical view of the low-pressure area (Themarineobserver.com).

The low pressure is related to one very important thing: when the frontal band passes, the air mass obviously changes. Important is the assumption, that the air coming behind the atmospherical front is always clearer than the “older” air being before the frontal band. Better is when the front brings precipitation because the aerosols can be removed from the air easily. It is not a rule, that the air can be more advantageous when the front is much colder. Usually, much colder fronts bring the air with big humidity. In this case, the cloud base level is also low and appreciably reduces visibility. After passing the cold front we get a lowered cloud, which further existence depends on the wind. Slower vanishing of clouds above mountains can make our observation disintegrated. However not always must be like this. There are many cases, when after the cold frontal band the visibility is appreciably better, except some isolated clouds with passing rainfalls, deteriorating atmospherical horizontal transparency in places. It happens usually in three cases: when cold frond passes above the much warmer surface, when frontal rainfall is strong and when after cold frontal band wind is strong. A first case refers to the situation, which has been mentioned in the previous section: much warmer surface causes heating of the air mass, which gets more volume and visibility decreases. On the other hand, we can observe quite strong vertical cloud development with passing rainfalls and thundershowers, which are an effect of steaming from this much warmer surface. The best effect is to be observed when this air mass passes above the sea or lake, then we experience a lake effect with cloudiness and passing precipitation. In these cases the visibility will be often partially impaired by precipitation. A strong rainfall at the cold front zone, clears up the atmosphere from a haze, making it more transparent ultimately. The atmosphere can be also cleared by the strong wind, which blows out any pollutants from the air. Sometimes we experience this situation, when after passing a cold front the wind starts to blow strongly. It can be also the time with a nice visual range. To summarize this thing we can say, that the freshest air comes always just behind the atmospheric front, which is a basic principle for long-distance observations.

The low-pressure area brings also a warm section, located between a warm and cold front. During the warm section of the low-pressure area, we can be able to see far. It happens, because warm air has less moisture. This situation occurs in a colder part of the year. The warm section should be geographically wide enough however the problem is that colder front, coming behind the warm one is quicker. The visibility area should be far enough from the cyclone center, where cloudiness and precipitation occurs. Better is when the wind in the warm section is stronger otherwise the weather tends to be misty. The air should not be too warm due to steaming.

Stable weather for a longer time at some area causes, that existing air mass transfers and “getting older” deteriorating the visibility. It also refers to the air masses, that come already transformed into the observed areas like arctic air mass crossing wide steppe areas before an approach to central and southern Europe. Usually, the atmosphere is the most transparent at 1st and sometimes at 2nd day after a fresh air mass approaching (Pic. 44).

Horizontal visibility changes when air mass getting older

Pic. 44 View towards Tatra Mts from Bieszczady Mts (Poland) at about 170km distance on two separate days, where 26.06.2007 was the 1st day with Polar maritime air mass and 28.06.2007 was a 3rd day with the same air mass. The air 2 days later was less transparent. Despite no big difference with Tatras appearance, I should add, that the photo below has been taken under cloudy conditions, which prevented light scattering.

In the case of cyclones always the front, from where air mass is coming is clearer than the back. Visibility is also better when closer to the anticyclone center. Favourable conditions provide also the pressure increase with the wind, when air is mixing. Sometimes it can have a negative side when the wind rises aerosols from the naked ground. The anticyclone presence favour the planetary boundary layer development, where the haze is enslaved and visibility reduced.

The thermal inversion (typical for the colder part of the year) brings very favourable horizontal visibility conditions, although it may not work for extremal distances.  The main role plays the altitude of the inversion boundary (inversion layer thickness), which depends on the pressure level and distance from the anticyclone centre. Saying again, it can reach even up to 2000m above ground. Another role plays an age of inversion. Older inversions behave in a different way, the boundary can be fuzzier.

Taking into account the dynamic weather features is very important to check the weather both for the observation place and the object observed, especially on longer distances, which will be explained in the next part of this article. The weather conditions for an observed object are beyond the horizon. For instance, medium-level and high-level clouds can complicate the observation conditions significantly, especially during the light level drop around dawn and dusk (Pic. 40, 41). Sometimes the different weather conditions occur in close distance from the observer. Then watching in the opposite direction we can have two different visibility patterns (Pic. 45).

Viuew from Boston St Botolph's church tower

Pic. 45 View from the St. Botolph’s Church tower at Boston (UK): 1 – Towards Hunstanton Old Lighthouse (35km), 2 – towards Tattershall Castle (17km) and unfortunately invisible Lincoln Cathedral (45km). The weather changes occurred just behind the Tattershall Castle, making everything beyond invisible due to much higher humidity and stratocumulus cloudiness, unlike to opposite, the eastern side of the view, where the atmosphere was much more clear.

It is nice, when the sufficiently big and stable high-pressure area is located towards the object observed.

Is good to observe the local weather conditions both for surface and certain altitude due to difference with humidity and cloud level, which I will develop in the next part of this article.

D. HAZE CONCENTRATION

In general, the appearance of the visibility of haze is determined by the concentration and distribution of light scattering and absorbing particles (Malm, 2016). We have 2 basic types of haze (Pic. 46), whereas the uniform haze is much worse because it generally obscures all landscape features in the scene and might be harder to differentiate from naturally occurring background haze (Malm, 2016). Next, to these 2 basic types of haze we can point also a plume, which has a layered character and arises out of pollution emission from i.e. chimneys or wildfires, which impair visibility partially on elevated level (Pic. 47).

Haze types

Pic. 46 Types of haze according to Malm, 2016.

Horizontal visibility impairment by plume

Pic. 47 A plume from an uncontrolled coal-fired power plant near Mazatlan (Mexico), viewed: a) a few kilometers downwind from the plant, c) tens of kilometers away from the plant, where b) plume doesn’t tend to mix with a stable atmosphere (Malm, 2016).

Different pollutants absorb different wavelengths of light. Due to their thickness and local atmosphere stability, we can observe their impact on the vista. For example, black carbon absorbs all wavelengths of light making its plume dark appearance. Another pollutant, a nitrogen dioxide gas absorbs more in the blue, than in the red spectrum (Malm, 2016). When nitrogen dioxide combines with varied background illumination, it yields a very brown atmospheric discoloration (Pic. 49). If a volume of the atmosphere contains a lot of nitrogen dioxide is shaded and if light passes through this shaded portion of the atmosphere, the light reaching the eye will be deficient with photons in the blue part of the spectrum (Malm, 2016). As a consequence, the light will appear brown or reddish in colour. However, if the light is allowed to shine on, but not through, that the same portion of the atmosphere, scattered light reaches the observer’s eye and the light appear to be gray in nature (Malm, 2016)(Pic. 48, 49, 50).

Carbon dioxide pattern

Pic. 48 A blue photo depletion in nitrogen dioxide, being present in the atmosphere (Malm, 2016).

Carbon Dioxide and horizontal visibility

Pic. 49 Brown discoloration resulting from an atmosphere containing nitrogen dioxide, being shaded by clouds viewed against the blue sky. Light scattered by a particular matter in that atmosphere can dominate light absorbed by carbon dioxide, causing a grey or blue-appearing haze (Malm, 2016).

Layered haze Denver Colorado

Pic. 50 Inversion layer over Denver, Colorado, that trapped carbon dioxide emissions. Because carbon dioxide gas absorbs more in the blue portion of the spectrum, the result is a brown haze layer (Malm, 2016).

Depending on the weather conditions (turbulent or stagnant atmosphere) we can point the three ways, that air pollution can visually degrade a scenic vista (Pic. 50).

Light pollution impact on horizontal visibility

Pic. 51 The three ways, that air pollution can degrade a scenic vista, where: A – pollutants mixed with the atmosphere under turbulent conditions, creating a layered haze; B – haze appearance as a coherent plume under stagnant atmosphere conditions during the winter; C – layered haze appearance under stagnant atmosphere conditions during the winter (Malm, 2016).

In the layered haze, typical is the contrast edge distinguishing a clear background above from the impaired landscape below. This situation is typical for temperature inversion, when haze with  (often) air pollutants is trapped near the ground. The layered haze can be misleading for observers being onside of layer, where the horizon is partially or even totally obscured unless this layered haze is thin enough to show a pristine view above (Pic. 52).

Tatry z Jastrzebia Zdroju, Grzegorz Luranc

Pic. 52 Tatra Mts seen from Jastrzebie Zdrój (Poland) at about 130 km distance. In general, a vista is fuzzy, what is an effect of location the observation place inside a layered haze (inversion layer), whereas just above the atmosphere is transparent with an excellent visual range (credits: Grzegorz Luranc).

In the meantime above around a few hundred meters view can be completely different with background haze only (near Rayleigh scattering conditions). In this event for people being on the bottom of the basin haze will have a uniform character whereas for mountaineers being above it will appear as a layer.
A naturally due to the various air masses we have various levels of uniform haze (Pic. 53).

Uniform haze and different conditions of horizontal visibility

Pic. 53 A view on the Garden Wall from Lake McDonald (Glacier National Park, USA) vista, presenting a different level of uniform haze (Malm, 2016).

A uniform haze shouldn’t be confused with a regional haze. The regional haze refers to more to a large spatial scale of visible pollution. The regional haze understanding depends on the geometry and the observer. Above I wrote about the situation when an observer is located underneath the haze layer and he is not aware of perfect visibility, above this layer of haze. Here I would like to point, that observer, being inside the layered haze can judge the haze to be uniform in that he would not observe a haze with a defined edge (Malm, 2016). When the observer is located above the layered haze, when hiking in mountainous regions, then he is able to see a regional haze in extend, which appears to be layered in the vertical profile.

Regional and uniform haze impact on horizontal visibility

Pic. 54 View on the La Sal Mountains from Canyonlands National Park with the effect of regional and uniform haze, where: a – transparent view, b – uniform haze with decreasing density towards the mountain summits, c – layered haze, d – uniform haze with cloud deck hiding the mountain tops (Malm, 2016).

Haze tends to be worse when closer to the ground due to bigger humidity and poor ventilation properties (Pic. 35, 36), which has been raised in the previous section. Also, urban areas with surroundings appear to be hazier due to a lot of emissions. Urban haze is specific, because due to high pollutants concentration (higher than in non-urban areas) usually impair the visibility much more. Sometimes even buildings only a few kilometers distant are substantially obscured (Pic. 55, 56).

Los Angeles skyline plunged in thick haze

Pic. 55 A Los Angeles skyline as seen from Griffith Observatory at only about 10 km distance. That day was a big pollutant concentration.

Extremely thick haze in China

Pic. 56 Sometimes a haze layer is very thick, giving a misty appearance for objects at only a few hundred-meter distances (Malm, 2016).

Not to mention, when haze is sufficiently dense to obscure features that are only a few meters distant. In termal inversion conditions, when layered haze is observed in urban areas the highest skyscrapers can extend up through the inversion layer giving very good visibility conditions (Pic. 57). Another haze information has been described in my previous article.

Denver inversion layer impact on horizontal visibility

Pic. 57 A deep inversion with trapped pollutants, causing a shallow haze layer in Denver, Colorado. The depth of the haze is only a tens meters, with buildings extending well above the layer (Malm, 2016).

        2.3 OPTICAL FACTORS

A. LIGHT SCATTERING

There are three major factors determining a visual range by light scattering: an astronomical, haze and cloud coverage. In astronomical point of view important is solar position on the sky, which has been described in the second chapter. However, there are still a few issues, which I must raise up in this section. I was writing about visibility towards solar and antisolar point. I will remind, that at the antisolar direction the distant objects are better visible in daylight because the backward scattering doesn’t reduce the visibility as strong as forward scattering (Pic. 58). Besides these objects are usually not shaded by themselves, giving an observer a chance to see some elements of their relief instead of outline only.

Layered haze scattering light pattern and impact on horizontal visibility

Pic. 58 A practical example of light scattering influence on visibility, where: a – a vista towards the solar direction, where forward scattering dominates, making haze a whitish appearance. The mountains beyond remain visible, however, an observer can see their outlines only; b – an opposite situation, where the same mountain range is seen on the opposite side to the Sun. Then backward scattering gives a bit better chances to spot some objects inside this haze layer. On top of that, an eye is able to distinguish some relief details on the mountain range (Malm, 2016).

Los Angeles forward light scattering on haze

Pic. 59 A forward scattering is the biggest always roughly underneath the Sun. When looking left or right from the middle you spot, that the haze layer has a bit darker appearance, however, the forward scattering still plays a major role up to 90 deg angular distance from the solar azimuth. The Los Angeles panorama from Griffith Observatory.

The situation changes rapidly just after the sunset, when the twilight wedge (belt of Venus) becomes visible. Then these objects became much less visible due to vanishing the contrast between sky and ground and fast decreasing of background luminance (Pic. 16, 18). As the dusk progress, the twilight wedge engulfs more and more of the sky with the horizon. Finally, the angle of visibility in bright atmosphere decrease to more or less 180 deg during the civil twilight to be completely gone at nautical twilight (Pic. 11, 12, 18, 60, 61).

Tatras from Vyhorlat at civil twilight

Slovenskie Rudohorie from Vihorlat at civil twilight

Pic. 60, 61 A mountainous view from Vyhorlat (Slovakia), where 60 – view on Tatra Mts., 61 – View on Slovenske Rudohorie. In both cases the inversion layer is visible. The trapped haze (marked by blue arrow) impair the visibility dramatically because the contrast between hazy sky and remote object is reduced. Haze is not able to scatter the light at this moment, however it extinct the light diffused in the atmosphere (Naobzore.net).

Light scattering is important also during the day. Sunlight, ground-reflected light, and light reflected by other objects (like clouds) are scattered by the intervening atmosphere into the sight path. Clouds play also a different role in visibility conditions. They can extend a visual range through the block of the direct sunlight and decrease the light scattering at once. When the sky is covered by thick clouds then some parts or at least one part of the line of sight is shaded by them. It incurs a nonuniform solar illumination alongside the path and inhomogeneous irradiation of the atmosphere. The molecules and aerosols being on the line of sight have a different incident solar radiance. The illuminated ones scatter light more efficiently, on the contrary to shaded aerosols, which have a weaker scattering. Every shaded section present alongside the line of sight appears to reduce the solar light scattering then. It is strongly related to the light transition phenomena, wherein shaded regions are less amount of light to scatter. At the same time, the distant horizon is being illuminated by strong sunlight, which makes an excellent contrast with shaded regions. This is an event, when stronger light, coming from an illuminated part of the sky beat up much weaker light coming from the shaded object, making it invisible. It happens only if a distant horizon is unobstructed by thick clouds, because otherwise, the view won’t be good. Thick clouds determine a perfect light diffusion, which is next radiated uniformly in all directions (Houghton, 1939).
We can list basic five situations, in which the line of sight between an observer and distant object is partially shaded. More details about it show the mechanism and practical proves below. The majority of these situations are contributing to reducing the attenuation of light reflected from a remote object making him more visible for an observer.

Under clear skies, there is no difference between illumination throughout a whole line of sight (Pic. 62).

Solar irradiation pattern for normal conditions between observer and distant object

Pic. 62 Normal visibility  conditions under clear skies between the observer and distant object, where: x = 0 – observation site, x = d – distant object, L (x) – an level of solar radiation (Vollmer, Schaff, 2018).

Sometimes, when the sky is covered by a lot of patches of clouds a line of sight between an observer and distant mountain can be shaded even a few times (Pic. 63). On this occasion the vista appears to look slightly better, than under clear skies, however, is still not clear enough due to strong light scattering in places.

 

Solar irradiation pattern for partly cloudy conditions between observer and distant object

Pic. 63 Some places get a less amount of solar radiation when shaded by patchy clouds. It can improve visibility a bit, especially at the solar direction.

When the sky at the observation point is cloudy and the sun is shining at the distant object far away (Pic. 64), then the visibility conditions are slightly better, but not perfect. They depend roughly of the part of the line of sight, which is being shaded. Usually, a far, illuminated mountains can merge with the illuminated sky, when a haze concentration level is high.

A solar irradiation pattern where observer is under cloud and distant object under sunlight

Pic. 64 A situation, when the sky above observer is cloudy, but Sun shines on the remote object observed. Depends on how long part of the line of sight is shaded visibility may be better or worst.

The best situation for distant object observation is cloud cover located at the path between an observer and object (Pic. 65), which blocks the sunlight both at observation place and a remote place observed, however, the sky just above horizon remains clear and bright. Then the contrast with the sky beyond is the best, giving much better visibility conditions. One drawback is, that observers can see an outline of this distant object only without any details, because they are being shaded.

Solar irradiation pattern when both observer and distant object are shined but nearly whole line of sight is overcasted

Pic. 65 A situation for the best visibility under overcast sky between the observation site and distant object alongside almost a whole line of sight with a clear sky behind the object, far above the horizon.

The worst situation (Pic. 66) is, when cloudiness appears at the same azimuth with a distant object observed and covers all lower part of the sky down to the horizon. Then only a “grey wall” of clouds is to be seen. An object, even in good visibility conditions can be merged with these clouds, especially when shaded by them. If not, it will be capable to reflect some sunlight from its brighter parts (e.g grassland, snow cap, etc).

Solar irradiation pattern when observer is in sunlight but distant object overcasted

Pic. 66 The worst situation for remote object observed, especially when is located on similar azimuth as Sun position. When the majority of the sight path with the observer’s site is illuminated, but a remote object is shaded by clouds, then it disappears behind the light transition phase and haze illuminated by the sun.

Visibility comparison in terms of different solar irradiance patterns

Pic. 67 A visibility comparison against the cloudiness and light scattering, where: 1clear sky, full light scattering on haze particles; 2 – A lot of patches of clouds, which cast shades in places, hence between a multitude of crepuscular rays a visual range appears to be better; 3 – the most unfavourable situation, when a majority of line of sight is illuminated, but remote mountains are shaded by clouds; 4 – the most favourable conditions for extended visual range, where almost a whole path between observer and remote object is shaded, but sky just above horizon remains illuminated directly by Sun; 5 – A situation, when observation site is shaded as well as foreground (blue arrow), but vista beyond is illuminated (red arrow), being better visible in hazy conditions at once.

B. LANDSCAPE (OBJECT) FEATURES

The landscape features include color, texture, form, and brightness (Malm, 2016) and also the anthropogenic feature. The form is to be the easiest way to recognize the remote object. The best example is between lower and higher mountains. Lower mountains appear like domes, beacons or buttes whereas high mountain can be seen like high sharp and steep objects. Color and texture are also important in the case of mountains. When peaks are snow-capped usually will be slightly easier to spot them far on the horizon despite the fact, that snow has the biggest albedo. A good example is a picture below, where snow-capped mountains, located at about 110km distance are barely visible under high haze concentration conditions, thanks to snow coverage (Pic. 68).

Tatry z Liwocza ledwo widoczne

Pic. 68 Tatra Mts, as seen from Liwocz at about 110 km distance. An observer can barely spot some fuzzy outlines because of snow coverage, which has a high albedo and can reflect sunlight much more effectively, than another type of surface. Hence the visual range of these mountains appears to be slightly extended under a high haze concentration level.

Tatry z Poloniny Rownej dobra widocznosc

Pic. 69 Tatra Mts seen from Polonina Runa (Ukraine) at about 200 km distance under transparent atmosphere conditions. Here an observer can easily see, that snow-capped distant mountains are much better visible, as long as they are illuminated by Sun. When shaded, it makes a different contrast with the sky beyond (credits: Shukaj Vitalij, Dalekieobserwacje.eu).

The best moment to recognize these peaks is in an early warm part of the year when these highest parts of the mountains are patched with snow. The color pattern of the landscape is strongly associated with its brightness. Brightness enables the object to be more or less visible. When the object surface is brighter then the sunlight is reflected more effectively. The reflected beam from this object is stronger and more capable to reach the distant observer (Pic. 70).

Horizontal visibility changes due an object illumination Barrington Cambridgeshire

Pic. 70 CEMEX Barrington Landfill Quarry seen from Sharpenhoe village near Luton (UK) ( 39km distance) in both scenarios: 1 – illuminated, 2 – shaded. A good example of an object with a bright surface. In this scenario, the object’s appearance is reliant for direct sunlight.

The anthropogenic feature states whether the object is emitting light  (during the night) or reflecting the light  (in favourable solar angle some skyscrapers can perfectly reflect the sunlight for long distances) (Pic. 71).

Sandy transmitter as an examople of bigger horizontal visibility due artifical illumination

Pic. 71 Sandy Heath transmitting station as seen from Magog Hills near Cambridge (UK) at 28 km distance. The TV transmitter can be easily spotted during the night from long distances because of its own light emission.

Another optical issue arising out of the intervening atmosphere. Image-forming information (radiation) originating from landscape features is scattered and absorbed  (attenuated) as it passes through the atmosphere toward the observer (Malm, 2016).
To summarize this section as well as a light scattering issue let’s have a look at the schematic below (Pic. 72):

Light scattering vista features based on object illumination

Pic. 72 A mechanism of light scattering and optical object features impact on the visual range (Malm, 2016).

C. WHY DISTANT HORIZON APPEARS TO BE BLUE?

The blueness of the sky has been shortly described in this article and also on this occasion.
The blueness of the horizon is caused by the smallish part of the air-tiny hydrocarbon particles released by vegetation, that chemically react with ozone molecules. At the outcome, the blue light is scattered selectively and gives the mountains, remote objects blue appearance. You can always notice even when visibility is perfect and your target is not much distant. Despite many details of its surface, it will have a bluish appearance (Pic. 73).

Blueness of horizon and horizontal visibility, Arizona Monument Valley

Pic. 73 A West Mitten Butte at the Monument Valley (Arizona, USA) seen from: 1 – 1,3 km from southwest, 2 – 1,6 km from north-west (towards solar direction), where a thin bluish appearance is to be seen on shaded part of the butte, 3 – from Forrest Gump Point (15 km) with strong bluish appearance. Even if visibility is perfect, the distant objects always appear to look bluish.

When visibility is worse the objects appear to be bluer i.e. due to nitrogen dioxide gas concentration. If a volume of the atmosphere containing NO2 is shaded and if light passes through this shaded portion of the atmosphere, the light reaching the eye will be deficient in photons in the blue part of the spectrum (Pic. 47,48,49). As a consequence, the light will appear brown or reddish in color (Malm, 2016), which has been discussed in the previous section.

Mariusz Krukar

 

References:

  1. Ackerman S.A., Knox J. A., 2007, Meteorology: understanding the atmosphere, Thompson higher education, Belmont, CA.
  2. Bennett A., 2016, Introduction to atmospheric visibility estimation, (in:) Visibility sensors, Bristol Industrial & Research Associates Ltd. (Biral)
  3. Horvath H., 1967, Atmospheric visibility, (in:) Atmospheric Environment, vol. 15, i.10-11, p.1785-1796
  4. Houghton H.G., 1939, On the relation between visibility and the constitution of clouds and fog, (in:) Journal of the Aeronautical Sciences, vol. 6, no 10, p.408-411
  5. Hyslop N.P., 2009, Impaired visibility: the air pollution people see, (in:) Atmospheric Environment, vol. 43, i. 1, p.182-195
  6. Luranc G., 2012, Wpływ sytuacji synoptycznych na widzialność w województwie małopolskim, Master dissertation, Faculty of Biology and Earth Sciences, Jagiellonian University (Polish)
  7. Majewski G.,et.al, 2015, The impact of selected parameters of visibility: First result from long-term campaign in Warsaw, Poland ,(in:) Atmosphere, v.6, p.1154-1174
  8. Malm W.C., 2016, Visibility: The seeing of near and distant landscape features, Elsevier Inc., New York
  9. McGraw-Hill Dictionary of scientific & technical terms, 2003, The McGraw-Hill Companies Ltd.

 

Links:

  1. Vertical visibility – the Free Dictionary explanation
  2. Vision
  3. The Sun angle calculator
  4. Aerosol optical depth – AERONET archival data
  5. MetOffice: Air-masses-and-Fronts.pdf
  6. Flightlearnings.com: air-masses – explanation
  7. Onlinelibrary.wiley.com: Air masses – rough explanation
  8. Equatorial air mass characteristic
  9. https://geology.com/world/europe-physical-map.shtml
  10. Convection vs subsidence
  11. Types of inversion
  12. Plume Blight
  13. Naobzore.net: atmospheric fronts (Slovak)
  14. Dalekie Vyhlady a mozlivosti ich pozorovania (Slovak)
  15. How far away is the horizon?

Wiki:

  1. Angstrom_exponent
  2. Arctic_haze
  3. Attenuation_coefficient
  4. Foehn_wind

Read also:

  1. What is a light transition? What examples can we see?
  2. Why the haze is an important weather factor, part 1 – types of aerosol and impact on human health
  3. Why the haze is an important weather factor, part 2 – impact on visibility and light scattering
  4. Light scattering in the Earth’s atmosphere, part 1 – scattering and related phenomenas
  5. Light scattering in the Earth’s atmosphere, part 2 – why is the sky blue and how the sky colour change?
  6. Light scattering in the Earth’s atmosphere, part 3 – clouds, haze and surface

 

 

 

 

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