Atmospheric Circulation and Weather Systems PDF

CHAPTER ATMOSPHERIC CIRCULATION AND WEATHER SYSTEMS E arlier Chapter 9 described the uneven pressure is measured with the help of a distribution of temperature o...

CHAPTER ATMOSPHERIC CIRCULATION AND WEATHER SYSTEMS E arlier Chapter 9 described the uneven pressure is measured with the help of a distribution of temperature over the mercury barometer or the aneroid barometer. surface of the earth. Air expands when Consult your book, Practical Work in heated and gets compressed when cooled. This Geography — Part I (NCERT, 2006) and learn results in variations in the atmospheric about these instruments. The pressure pressure. The result is that it causes the decreases with height. At any elevation it varies movement of air from high pressure to low from place to place and its variation is the pressure, setting the air in motion. You already primary cause of air motion, i.e. wind which know that air in horizontal motion is wind. moves from high pressure areas to low Atmospheric pressure also determines when pressure areas. the air will rise or sink. The wind redistributes the heat and moisture across the planet, Vertical Variation of Pressure thereby, maintaining a constant temperature In the lower atmosphere the pressure for the planet as a whole. The vertical rising of decreases rapidly with height. The decrease moist air cools it down to form the clouds and amounts to about 1 mb for each 10 m bring precipitation. This chapter has been increase in elevation. It does not always devoted to explain the causes of pressure decrease at the same rate. Table 10.1 gives differences, the forces that control the the average pressure and temperature at atmospheric circulation, the turbulent pattern selected levels of elevation for a standard of wind, the formation of air masses, the atmosphere. disturbed weather when air masses interact with each other and the phenomenon of violent Table 10.1 : Standard Pressure and Temperature at tropical storms. Selected Levels Level Pressure in mb Temperature °C ATMOSPHERIC P RESSURE Sea Level 1,013.25 15.2 Do you realise that our body is subjected to a 1 km 898.76 8.7 lot of air pressure. As one moves up the air gets varified and one feels breathless. 5 km 540.48 –17. 3 The weight of a column of air contained in 10 km 265.00 – 49.7 a unit area from the mean sea level to the top of the atmosphere is called the atmospheric The vertical pressure gradient force is much pressure. The atmospheric pressure is larger than that of the horizontal pressure expressed in units of milibar. At sea level the gradient. But, it is generally balanced by a average atmospheric pressure is 1,013.2 nearly equal but opposite gravitational force. milibar. Due to gravity the air at the surface is Hence, we do not experience strong upward denser and hence has higher pressure. Air winds. 2015-16 ATMOSPHERIC CIRCULATION AND WEATHER SYSTEMS 89 Horizontal Distribution of Pressure purposes of comparison. The sea level pressure distribution is shown on weather maps. Small differences in pressure are highly Figure 10.1 shows the patterns of isobars significant in terms of the wind direction and corresponding to pressure systems. Low- pressure system is enclosed by one or more isobars with the lowest pressure in the centre. High-pressure system is also enclosed by one or more isobars with the highest pressure in the centre. World Distribution of Sea Level Pressure The world distribution of sea level pressure in January and July has been shown in Figures 10.2 and 10.3. Near the equator the sea level Figure 10.1 : Isobars, pressure and wind systems in pressure is low and the area is known as Northern Hemisphere equatorial low. Along 30° N and 30o S are velocity. Horizontal distribution of pressure is found the high-pressure areas known as the studied by drawing isobars at constant levels. subtropical highs. Further pole wards along Isobars are lines connecting places having 60o N and 60o S, the low-pressure belts are equal pressure. In order to eliminate the effect termed as the sub polar lows. Near the poles of altitude on pressure, it is measured at any the pressure is high and it is known as the polar station after being reduced to sea level for high. These pressure belts are not permanent Figure 10.2 : Distribution of pressure (in millibars) — January 2015-16 90 FUNDAMENTALS OF PHYSICAL GEOGRAPHY Figure 10.3 : Distribution of pressure (in millibars) — July in nature. They oscillate with the apparent Pressure Gradient Force movement of the sun. In the northern The differences in atmospheric pressure hemisphere in winter they move southwards produces a force. The rate of change of pressure and in the summer northwards. with respect to distance is the pressure Forces Affecting the Velocity gradient. The pressure gradient is strong where and Direction of Wind the isobars are close to each other and is weak where the isobars are apart. You already know that the air is set in motion due to the differences in atmospheric pressure. Frictional Force The air in motion is called wind. The wind It affects the speed of the wind. It is greatest at blows from high pressure to low pressure. The the surface and its influence generally extends wind at the surface experiences friction. In upto an elevation of 1 - 3 km. Over the sea addition, rotation of the earth also affects the surface the friction is minimal. wind movement. The force exerted by the rotation of the earth is known as the Coriolis Coriolis Force force. Thus, the horizontal winds near the earth surface respond to the combined effect The rotation of the earth about its axis affects of three forces – the pressure gradient force, the direction of the wind. This force is called the frictional force and the Coriolis force. In the Coriolis force after the French physicist who addition, the gravitational force acts described it in 1844. It deflects the wind to the downward. right direction in the northern hemisphere and 2015-16 ATMOSPHERIC CIRCULATION AND WEATHER SYSTEMS 91 to the left in the southern hemisphere. The The wind circulation around a low is deflection is more when the wind velocity is called cyclonic circulation. Around a high high. The Coriolis force is directly proportional it is called anti cyclonic circulation. The to the angle of latitude. It is maximum at the direction of winds around such systems poles and is absent at the equator. changes according to their location in The Coriolis force acts perpendicular to the different hemispheres (Table 10.2). pressure gradient force. The pressure gradient The wind circulation at the earth’s surface force is perpendicular to an isobar. The higher around low and high on many occasions is the pressure gradient force, the more is the closely related to the wind circulation at higher velocity of the wind and the larger is the level. Generally, over low pressure area the air deflection in the direction of wind. As a result of will converge and rise. Over high pressure area these two forces operating perpendicular to each the air will subside from above and diverge at other, in the low-pressure areas the wind blows the surface (Figure10.5). Apart from around it. At the equator, the Coriolis force is convergence, some eddies, convection zero and the wind blows perpendicular to the currents, orographic uplift and uplift along isobars. The low pressure gets filled instead of fronts cause the rising of air, which is essential getting intensified. That is the reason why tropical for the formation of clouds and precipitation. cyclones are not formed near the equator. Pressure and Wind The velocity and direction of the wind are the net result of the wind generating forces. The winds in the upper atmosphere, 2 - 3 km above the surface, are free from frictional effect of the surface and are controlled mainly by the pressure gradient and the Coriolis force. When isobars are straight and when there is no Figure 10.5 : Convergence and divergence of winds friction, the pressure gradient force is balanced by the Coriolis force and the resultant wind blows parallel to the isobar. This wind is known General circulation of the atmosphere as the geostrophic wind (Figure 10.4). The pattern of planetary winds largely depends on : (i) latitudinal variation of atmospheric heating; (ii) emergence of pressure belts; (iii) the migration of belts following apparent path of the sun; (iv) the distribution of continents and oceans; (v) the rotation of earth. The pattern of the movement of the planetary winds is called the general circulation of the atmosphere. The general circulation of the atmosphere also sets in motion the ocean water circulation which influences the earth’s Figure 10.4 : Geostropic Wind Table 10.2 : Pattern of Wind Direction in Cyclones and Anticyclones Pressure System Pressure Condition Pattern of Wind Direction at the Centre Northern Hemisphere Southern Hemisphere Cyclone Low Anticlockwise Clockwise Anticyclone High Clockwise Anticlockwise 2015-16 92 FUNDAMENTALS OF PHYSICAL GEOGRAPHY climate. A schematic description of the general The general circulation of the atmosphere circulation is shown in Figure 10.6. also affects the oceans. The large-scale winds of the atmosphere initiate large and slow moving currents of the ocean. Oceans in turn provide input of energy and water vapour into the air. These interactions take place rather slowly over a large part of the ocean. General Atmospheric Circulation and its Effects on Oceans Warming and cooling of the Pacific Ocean is most important in terms of general atmospheric circulation. The warm water of the central Pacific Ocean slowly drifts towards South American coast and replaces the cool Peruvian current. Such appearance of warm water off the coast Figure 10. 6 : Simplified general circulation of Peru is known as the El Nino. The El of the atmosphere Nino event is closely associated with the pressure changes in the Central Pacific The air at the Inter Tropical Convergence and Australia. This change in pressure Zone (ITCZ) rises because of convection caused condition over Pacific is known as the by high insolation and a low pressure is southern oscillation. The combined created. The winds from the tropics converge phenomenon of southern oscillation and at this low pressure zone. The converged air El Nino is known as ENSO. In the years rises along with the convective cell. It reaches when the ENSO is strong, large-scale the top of the troposphere up to an altitude of variations in weather occur over the 14 km. and moves towards the poles. This world. The arid west coast of South causes accumulation of air at about 30o N and America receives heavy rainfall, drought S. Part of the accumulated air sinks to the occurs in Australia and sometimes in ground and forms a subtropical high. Another India and floods in China. This reason for sinking is the cooling of air when it phenomenon is closely monitored and is reaches 30o N and S latitudes. Down below used for long range forecasting in major near the land surface the air flows towards the parts of the world. equator as the easterlies. The easterlies from either side of the equator converge in the Inter Seasonal Wind Tropical Convergence Zone (ITCZ). Such circulations from the surface upwards and The pattern of wind circulation is modified in vice-versa are called cells. Such a cell in the different seasons due to the shifting of regions tropics is called Hadley Cell. In the middle of maximum heating, pressure and wind belts. latitudes the circulation is that of sinking cold The most pronounced effect of such a shift is air that comes from the poles and the rising noticed in the monsoons, especially over warm air that blows from the subtropical high. southeast Asia. You would be studying the At the surface these winds are called westerlies details of monsoon in the book India : Physical and the cell is known as the Ferrel cell. At polar Environment (NCERT, 2006). The other local latitudes the cold dense air subsides near the deviations from the general circulation system poles and blows towards middle latitudes as are as follows. the polar easterlies. This cell is called the polar Local Winds cell. These three cells set the pattern for the general circulation of the atmosphere. The Differences in the heating and cooling of earth transfer of heat energy from lower latitudes to surfaces and the cycles those develop daily or higher latitudes maintains the general annually can create several common, local or circulation. regional winds. 2015-16 ATMOSPHERIC CIRCULATION AND WEATHER SYSTEMS 93 Land and Sea Breezes as the valley breeze. During the night the slopes get cooled and the dense air descends As explained earlier, the land and sea absorb and transfer heat differently. During the day the into the valley as the mountain wind. The cool air, of the high plateaus and ice fields draining land heats up faster and becomes warmer than the sea. Therefore, over the land the air rises into the valley is called katabatic wind. Another type of warm wind occurs on the leeward side giving rise to a low pressure area, whereas the of the mountain ranges. The moisture in these sea is relatively cool and the pressure over sea is relatively high. Thus, pressure gradient from winds, while crossing the mountain ranges condense and precipitate. When it descends sea to land is created and the wind blows from the sea to the land as the sea breeze. In the night down the leeward side of the slope the dry air gets warmed up by adiabatic process. This dry the reversal of condition takes place. The land air may melt the snow in a short time. loses heat faster and is cooler than the sea. The pressure gradient is from the land to the sea Air Masses and hence land breeze results (Figure 10.7). When the air remains over a homogenous area for a sufficiently longer time, it acquires the characteristics of the area. The homogenous regions can be the vast ocean surface or vast plains. The air with distinctive characteristics in terms of temperature and humidity is called an airmass. It is defined as a large body of air having little horizontal variation in temperature and moisture. The homogenous surfaces, over which air masses form, are called the source regions. The air masses are classified according to the source regions. There are five major source regions. These are: (i) Warm tropical and subtropical oceans; (ii) The subtropical hot deserts; (iii) The relatively cold high latitude oceans; (iv) The very cold snow covered continents in high latitudes; (v) Permanently ice covered continents in the Arctic and Antarctica. Accordingly, following types of air- masses are recognised: (i) Maritime tropical (mT); (ii) Continental tropical (cT); (iii) Maritime polar (mP); (iv) Continental polar (cP); (v) Continental arctic (cA). Tropical air masses are warm and polar air masses are cold. Fronts When two different air masses meet, the Figure 10.7 : Land and sea breezes boundary zone between them is called a front. The process of formation of the Mountain and Valley Winds fronts is known as frontogenesis. There In mountainous regions, during the day the are four types of fronts: (a) Cold; (b) Warm; slopes get heated up and air moves upslope (c) Stationary; (d) Occluded. When the and to fill the resulting gap the air from the front remains stationary, it is called a valley blows up the valley. This wind is known stationary front. When the cold air moves 2015-16 94 FUNDAMENTALS OF PHYSICAL GEOGRAPHY anticlockwise cyclonic circulation. The cyclonic circulation leads to a well developed extra tropical cyclone, with a warm front and a cold front. The plan and cross section of a well developed cyclone is given in Figure 10.9. There are pockets of warm air or warm sector wedged between the forward and the rear cold air or cold sector. The warm air glides over the cold air and a sequence of clouds appear over the sky ahead of the warm front and cause precipitation. The cold front approaches the warm air from behind and pushes the warm air up. As a result, cumulus clouds develop along the cold front. The cold front moves faster than the warm front ultimately overtaking the warm front. The warm air is completely lifted up and the front is occluded and the cyclone dissipates. The processes of wind circulation both at the surface and aloft are closely interlinked. Figure 10.8 : Vertical Sections of : (a) Warm Front; The extra tropical cyclone differs from the (b) Cold Front; (c) Occluded Front tropical cyclone in number of ways. The extra tropical cyclones have a clear frontal system towards the warm air mass, its contact zone is called the cold front, whereas if the warm air mass moves towards the cold air mass, the contact zone is a warm front. If an air mass is fully lifted above the land surface, it is called the occluded front. The fronts occur in middle latitudes and are characterised by steep gradient in temperature and pressure. They bring abrupt changes in temperature and cause the air to rise to form clouds and cause precipitation. Extra Tropical Cyclones The systems developing in the mid and high latitude, beyond the tropics are called the middle latitude or extra tropical cyclones. The passage of front causes abrupt changes in the weather conditions over the area in the middle and high latitudes. Extra tropical cyclones form along the polar front. Initially, the front is stationary. In the northern hemisphere, warm air blows from the south and cold air from the north of the front. When the pressure drops along the front, the warm air moves northwards and the cold air move towards, south setting in motion an Figure 10. 9 : Extra tropical cyclones 2015-16 ATMOSPHERIC CIRCULATION AND WEATHER SYSTEMS 95 which is not present in the tropical cyclones. A schematic representation of the vertical They cover a larger area and can originate over structure of a mature tropical cyclonic storm the land and sea. Whereas the tropical cyclones is shown in Figure 10.10. originate only over the seas and on reaching A mature tropical cyclone is characterised the land they dissipate. The extra tropical by the strong spirally circulating wind around cyclone affects a much larger area as the centre, called the eye. The diameter of the compared to the tropical cyclone. The wind circulating system can vary between 150 and velocity in a tropical cyclone is much higher 250 km. and it is more destructive. The extra tropical The eye is a region of calm with subsiding cyclones move from west to east but tropical air. Around the eye is the eye wall, where there cyclones, move from east to west. is a strong spiralling ascent of air to greater height reaching the tropopause. The wind reaches maximum velocity in this region, Tropical Cyclones reaching as high as 250 km per hour. Tropical cyclones are violent storms that Torrential rain occurs here. From the eye wall originate over oceans in tropical areas and rain bands may radiate and trains of cumulus move over to the coastal areas bringing about and cumulonimbus clouds may drift into the large scale destruction caused by violent outer region. The diameter of the storm over winds, very heavy rainfall and storm surges. the Bay of Bengal, Arabian sea and Indian This is one of the most devastating natural ocean is between 600 - 1200 km. The system calamities. They are known as Cyclones in the moves slowly about 300 - 500 km per day. Indian Ocean, Hurricanes in the Atlantic, The cyclone creates storm surges and they Typhoons in the Western Pacific and South inundate the coastal low lands. The storm China Sea, and Willy-willies in the Western peters out on the land. Australia. Tropical cyclones originate and intensify over warm tropical oceans. The conditions favourable for the formation and intensification of tropical storms are: (i) Large sea surface with temperature higher than 27° C; (ii) Presence of the Coriolis force; (iii) Small variations in the vertical wind speed; (iv) A pre-existing weak- low-pressure area or low-level-cyclonic circulation; (v) Upper divergence above the sea level system. The energy that intensifies the storm, comes from the condensation process in the towering cumulonimbus clouds, surrounding the centre of the storm. With continuous supply of moisture from the sea, the storm is further strengthened. On reaching the land the moisture supply is cut off and the storm dissipates. The place where a tropical cyclone crosses the coast is called the landfall of the cyclone. The cyclones, which cross 20o N latitude generally, recurve and they are more Figure 10.10 : Vertical section of the tropical cyclone destructive. (after Rama Sastry) 2015-16 96 FUNDAMENTALS OF PHYSICAL GEOGRAPHY Thunderstorms and Tornadoes greater height. This causes precipitation. Later, downdraft brings down to earth the cool air Other severe local storms are thunderstorms and the rain. From severe thunderstorms and tornadoes. They are of short duration, sometimes spiralling wind descends like a occurring over a small area but are violent. trunk of an elephant with great force, with very Thunderstorm s a re caused by intense low pressure at the centre, causing massive convection on moist hot days. A thunderstorm destruction on its way. Such a phenomenon is is a well-grown cumulonimbus cloud called a tornado. Tornadoes generally occur producing thunder and lightening. When the in middle latitudes. The tornado over the sea clouds extend to heights where sub-zero is called water spouts. temperature prevails, hails are formed and they These violent storms are the manifestation come down as hailstorm. If there is insufficient of the atmosphere’s adjustments to varying moisture, a thunderstorm can generate dust- energy distribution. The potential and heat storms. A thunderstorm is characterised by energies are converted into kinetic energy in intense updraft of rising warm air, which these storms and the restless atmosphere again causes the clouds to grow bigger and rise to returns to its stable state. EXERCISES 1. Multiple choice questions. (i) If the surface air pressure is 1,000 mb, the air pressure at 1 km above the surface will be: (a) 700 mb (c) 900 mb (b) 1,100 mb (d) 1,300 mb (ii) The Inter Tropical Convergence Zone normally occurs: (a) near the Equator (b) near the Tropic of Cancer (c) near the Tropic of Capricorn (d) near the Arctic Circle (iii) The direction of wind around a low pressure in northern hemisphere is: (a) clockwise (c) anti-clock wise (b) perpendicular to isobars (d) parallel to isobars (iv) Which one of the following is the source region for the formation of air masses? (a) the Equatorial forest (c) the Siberian Plain (b) the Himalayas (d) the Deccan Plateau 2. Answer the following questions in about 30 words. (i) What is the unit used in measuring pressure? Why is the pressure measured at station level reduced to the sea level in preparation of weather maps? (ii) While the pressure gradient force is from north to south, i.e. from the subtropical high pressure to the equator in the northern hemisphere, why are the winds north easterlies in the tropics. (iii) What are the geotrophic winds? (iv) Explain the land and sea breezes. 2015-16 ATMOSPHERIC CIRCULATION AND WEATHER SYSTEMS 97 3. Answer the following questions in about 150 words. (i) Discuss the factors affecting the speed and direction of wind. (ii) Draw a simplified diagram to show the general circulation of the atmosphere over the globe. What are the possible reasons for the formation of subtropical high pressure over 30o N and S latitudes? (iii) Why does tropical cyclone originate over the seas? In which part of the tropical cyclone do torrential rains and high velocity winds blow and why? Project Work (i) Collect weather information over media such as newspaper, TV and radio for understanding the weather systems. (ii) Read the section on weather in any newspaper, preferably, one having a map showing a satellite picture. Mark the area of cloudiness. Attempt to infer the atmospheric circulation from the distribution of clouds. Compare the forecast given in the newspaper with the TV coverage, if you have access to TV. Estimate, how many days in a week was the forecast were accurate. 2015-16