1. SPACE DYNAMIC
WEATHER AND CLIMATE
(a) Differencebetween weather and climate
There is a slight differencebetweenweather and climate. Weatherrefersto
as the actualstateof atmosphereand climaterefersto the averagestateof
atmosphere.
By definition:
Weather is the conditionof the atmospherewith regard toitselements for
a certainplaceand at specific moment. It is the dailyatmospheric condition
of a placeat particular time. It isthe conditionof being hot, windy, cold,
foggy, or cloudy. Weather changesfrom timeto timeand from place to
place. The conditionof the atmosphereisdetermined by the elementsof
weather which are:
o Temperature
o Humidity
o Atmospheric pressure
o Clouds
o Precipitationand
o Winds
Climate isthe averageatmosphericconditionover a long period of time
over 30 to 40 years withina specific geographicalarea.
Factors that influence weather and climate
Weather and climateareinfluenced by the factorslike;
-Temperature
-Precipitation
-Humidity
-Pressure
2. -Winds
-Cloud cover
-Sunshine
-Altitudeand
-Oceancurrents.
Measuring and recording theelementsof weather and climateis done at a
weather station.
WEATHER STATION isa placethat is set asidefor the purpose of
observing measuring and recording weather elements.
Element of weather
1. TEMPERATURE
Temperatureisthedegree of a heat of a body. It is a measureor degree of
hotness of an object or place .Temperatureismeasured by an instrument
called thermometer. Thelines joining all places with equaltemperatureare
3. called isothems
RECORDING TEMPERATURE
1. The mean(or overage) dailytemperatureisobtained byadding thedaily
maximumand the daily minimum temperatureand dividing thesum by
two.
2. The daily rangeof temperatureisobtained bysubstracting thedaily
maximumtemperaturebythe daily minimum temperaturewhich is,
daily max temp – daily minimum temperature
4. 3. The mean (or average) monthly temperatureisobtained bydividing the
sum of daily meantemperatureofa month by thenumber of days in that
particularmonth
4. The monthlyrange of temperatureisobtained bysubtractingthelowest
daily temperatureofa month from the highest meandaily temperatureof
that particular month.
5. The mean(or average) annualtemperatureisobtained bydividing the
sum of the monthly mean temperaturesofthe particular year by12.
6. The meanannual rangeof temperatureisobtained bysubstracting the
lowest mean monthly temperatureofa year from the highest meanmonthy
temperatureofthat sameyear.
FACTORS AFFECTING INSOLATION ORTEMPERATUREOF A PLACE
Factorsthat influencethe amount of insolationreceived any point and
thereforeits radiationbalanceand heat budget varyconsiderablyover time
and space.Theyincludethe following.
(a) Seasons and angle of incidence
The earth as a planet moves along its orbit throughout theyear under this
movement inclinationof the earth variesand theangle of which the sun
rays strikesthe earth'ssurfacechangeswith seasons.
Also thedistanceof the earth from the sun variesfrom month to month.At
spring and autumnequinoxes.(21th March and 23rd September) theangleof
incidenceat theequator is 90º making anarea to have high temperature
throughout theyear.Temperatureisdistributed equallyinboth
hemispheres.At thesummer and winter solsctice(21th Juneand 22nd
December) due to earth tilting thesun is overhead at the tropicswherethe
hemisphereexperiencesummer willreceive maximuminsolation.Theangle
of incidenceisthe most important factor which influencestheamount of
insolationof a place on theearth'ssurface.
5. (b)Distance from the sea
There is often a considerabledifferencesbetweentemperatureofland and
water surface. The reason for thisis that land surfaceheatsand cool more
slowly than thesea.
Due to this summer temperatureincoastalareasarelower than in
continentalinterior. Likewisewinter temperaturewillbe higher in coastal
areasthanin continentalinterior ifthe windsblow towardstheshore
During the day and during night the situationisrelated toland and sea
breeze. Areaswhose temperaturesaregreatlyaffected bythe sea are
reffered to as maritime.Thegreater distancefrom thesea the colder the
winter it will be and the warmer the summer develops.
6. (c)Altitude
The rateat which temperaturedecreaseswith increasing altitudeiscalled
lapse rate. Normallyair temperaturedecreaseswith increasing heightat a
rateof 0.6ºc R.r 100 meters.Thisisbecausewhen earth surfaceis heated it
passes itsheat on air making atmospherebeing heated from below and not
directlyfrom thesun.This affect temperaturebecausethehigher you go the
cooler it becomes. Altitudeexplainswhyhighlandsin the tropicsareever
7. cold e.g Mt. KilimanjaroinTanzania.
(d) Aspect
Thisrefers to the directioninwhich a slope falls.Some slopes are exposed to
the sun thanothers.The atmosphereofthe north facing slopes of highlands
in the northernhemispherealso called ubac arecooler than theslopes
facing south adret.Thesamething appears inthe southernhemisphere
(e) Latitude
It is the angular distancefrom the equator tothe poles. It determinesboth
the length of day throughout theyear and the intensityand possible
durationof sunlight received.
8. As one moves pole wardsfrom theequator he experiences
gradual progressivedecreaseintemperature. Thisisbecausethe sun
strikesthe equator moreintensitythanit does in the poles two observations
canexplainthis phenomenon.
(i)At the equator thebeam of light strikethe earth'ssurfacecovering a
smaller surfacearea thanin the poles wherethe same beam of light covers a
larger surfacearea.
(ii)At theequator thebeam of light striketravels a short distancehence
experiencing lessatmospheric effectslike absorptionreflectionand
scattering.At thepoles thebeam of light travels a longer distanceand it
experiencesmoreeffects in the atmosphere.
(f) Cloud cover
The atmosphereof areascovered with heavy clouds is cooler thanthat of
areaswith clear skies.Thisis because cloudsprevent insolationto reach
sand sea surface.
(g) Length of day and night
Insolation is only received during day light hours and reachesits peakat
noon .The longer the period of solar insolationthe greater thequantityof
radiationreceived at a givenplace on theearth'ssurface.Thereareno
9. seasonal variationsat theequator wheredays and nightsareof equal
length throughout theyear.In contrast polar regionsreceiveno insolation
during part of winter when there is continuousdarknessbut may received
up to 24 hours of insolationduring partsof the summer when the sun never
sinks below the horizon .This occursin thelands of the midnight sun
(f) Prevailing winds.
Temperatureofthe wind is affected by the temperatureofit'sarea of origin
and of the surfaceover which it blows normal windsblowing from the sea
during winter warmstheatmosphereof the land near thesea while winds
blowing from the sea during summer cools the atmosphereof thecoast
(g)Ocean currents
Warm oceancurrentscarrywarm water polewards and rise the air
temperatureofthe maritimeenvironmentswheretheyfollow while cold
ocean currentscarrycold water to the equator and so lower the
temperatureofthe coast areas.
Factors affecting the flow of ocean Currents
Oceancurrents – this is the horizontalmovement of masswater in a
defined direction.Themovement is due to densityvariationat various
depthsgovernent by the temperatureand salinity.The meeting of two
currentsconverging uponone another causessinking of water which
counter balanceswith ascending masses.
Salinitydifferences
Density of ocean water is caused by amount of salts the more salt in an
ocean thedenser the water will be.Denser water sinks in water with low
densitywhich causes the formationofocean currents.
Temperature
Temperaturecausesdifferencesinwater densitywhich causesocean water
to move. The cold water is denser than warm water, thistendsto make
polar cold water sink to the bottom thenflow downwardstowardsthe
equator whilethe warmer less denser water at the tropic moveson the
10. surfacetowardsthepoles .After being cooled it sinks againand moves
towardstheequator hence the oceancurrent.
Prevailing winds
When wind blows over oceansurfaceit pushes water surfaceand forms the
ocean current .Prevailing windsthereforecausethewater to move to the
directiontheyblowing to winds causedrift currents. Anexampleof drift
currentsis the north Atlantic drift which iscaused by the westerly windsin
the Atlantic ocean.
Rotationof the earth
Thiscauses the current flow to be affected as they aredeflected or pushed
according toFerrell’s law. Ferrell’s law slatesthat"Anythingmoving freely
in the northernhemispherewill be deflected to itsright while in the
southernhemisphereit will be indirectlythough thewinds where in the
northernhemisphereoceancurrent are deflected to their right whilein the
southernhemisphereto their left ".
Shapeof landmasses
The flow of ocean water canalso be directed bythe landmass.Theocean
currentsareturned from their straight coursebythe shape of adjacent
landmassor coast line.
What isa temperatureanomaly?
The term temperatureanomalyis used specificallytodescribetemperature
differencesfrom a mean.It shows the differencebetweenthe mean
temperatureofa placeand the meantemperatureofother places with the
samelatitudein thesame month.
For example:Anarea which has a mean Januarytemperatureof4ºc, which
is 20ºc higher thantheaveragefor other locationlaying at 58 degree
latitudenorth.such anomaliesresult primaryfrom theueven heating and
cooling rates of land and sea and areintensified by the horizontaltransfer
of energy by oceancurrentsand prevailing winds.
2. ATMOSPHERIC PRESSURE
Air has weight and therefore it exertsthe pressurecalled atmospheric
pressureon the earth surface.Pressurevarieswith thetemperatureand
11. altitude, and an instrument which measurepressureiscalled barometer.
There aretwo types of mercury
(i)barometer
(ii)aneroid barometer
The lines which join all placeswith equal pressureare called bars.Thus
pressurevaries from one place to another it is not the same in one or all the
regions.
FACTOR INFLUENCINGVARIATION IN ATMOSPHERIC
PRESSURE
Temperature
As temperaturedecreasepressurerisesat the sameheight due to low
temperaturecold air tend to sink, thus inducing high pressuretodevelop
But as temperatureincreaseshot air tendsto rise making it possible for low
pressureto develop over thearea.
Altitude
Usually pressureof the atmospheredecreasewith increasing height.
Pressureis therefore lower at the mountaintop thanat thesea level.This is
becauseat the sea level air hasto support a greater height thanit does on
the top of mountain.Thusthereisless force or weight of air at the mountain
top thanat the sea level.
12. Revoluationof the Earth
The earth revolutioncausesseasons wheresome seasons arewarm while
others arecold .Revolution of the earth affectsthe positionof the low
pressurebelt i.e doldrum. Normally doldrum moves northwardsand
southwardsof the equator depending onthe seasons.
Earth rotation asa ball causesformationof subtropicalhigh-pressurebelt
around 35º north and south of the equator whereair sinks down and gets
compressed .Due to thiscompressionthe sinking of air is heated up and
rises again. Thesame situationtakesplacearound circumpolar or
temperaturebelt around 60º north and south of the equator.Thesearethe
areaswhere the warm subtropicalair risesover the cold polar air expands
and getscooler.Thissituationresult intoDepression cyclonic or frontal.
PLANETARY PRESSURE BELTS
THE WORLD PRESSURE BELTS
These canbe analyzed according totemperatures:
(i)Equatoriallow pressure belt / equatorinallytrough
Thisis called doldrum it is located around 5º north and south of the
equator.Theair hererises due to high temperatureit isa wind a
convergencezone. This meanswinds meet there and it is called
intertropicalconvergencezone (ITCZ)
(ii)Subtropichigh pressurebelt (Horse latitudes)
Thisis located at 30º north and south of the equator with descending air
current due to heat of temperature. High pressureis attributedby
accumulationofcold air which moves from the equator towards poles.This
belt is also referred to as the"horse belt".
(iii)Temperaturelow pressure belt (sub polar low temperaturebelts)
Thisis found at 60º north and south of the equator. It is also known as
cyclonic activities zoneor zone of convergence. Existanceoflow pressureis
mainlydynamic rather thana result of temperaturechange.
13. (iv) Polar high-pressurebelt
Thisis confined at 90º north and south of the equator. Pressureis
permanentlyhigh due to low temperatureattributed bya dense descending
air from the temperaturelow pressure belt.
3. SUNSHINE
Thisis another element of weather. The durationofsunshine is partyof a
functionof latitude. For the hours of light (that ispossible sunshine) vary
with these season in different latitudes.It is also a functionof daytime
cloudiness .
MEASUREMENT ANDRECORDING OF SUNSHINE
The durationof bright sunshineismeasured by means of campbellstokes
recorder, a solid sphere of glass 10cm in diameter. Thisform the rays of
sunshine onto a sensitized card graduatedinhours and so burn a line
during thetimethe sun is shinning .Faint sun,light sun, near dawn or dusk
or when the sun is partiallyabscured isnot recorded .Tables of sunshine
14. data areprepared from these record, in the form of either absolutesolution
in hours per day or as percentageofpossible sunshine per dayor month.
When meansfigureshas been obtained over the requisitenumber ofyears,
the value for each statecanbe plotted, and lines of equal meandurationof
sunshine isohels can be interpolated.
4. HUMIDITY
Thisis refered to as the atmospheric moister.Themoister is obtained from
varioussources such as oceans, lakes,seas, dams,pondsand rivers. It is of
high importanceasfar as weather as climateisconcerned. Air absorbs
water through theprocess of evaparationwhich result in water changing
from itsliquid stateto gaseousstate,thegaseousstateis called water
vapour. The amount of water vapour in the air is called humidityand it is
measured by an instrument called hydrometer placed inthe Stevenson
screen.
15. FACTOR INFLUENCINGHUMIDITY
-Air pressure
When air is compressed, it warmsup and its densitybecomeslower .Thus
at low altitudewherepressureis high air will absorb more moister. At high
altitudewherepressureis lower air expandsand cools and itscapacityto
absorb moister isreduced.
-Latitude
Humidityhigher inlower latitudesthaninhigher latitudebecausethere
is greater rateof evaporationat lower latitudesdue to high
temperature.Likewisethemount of moister in the air is higher in
summer .
-Temperature
Arisein temperaturelowersrelativehumidityifthe amount of moister
remainsconstant becausewhenair is heated it expands.Thevolume
16. increaseand therefore distributionofwater vapour per unit.Volume
becameless.The air will have a greater capacityof holding more water
vapour if air is cooled it contractsand decreaseinvolume making thespace
which moister canoccupybecomeless .That is why if air continuesto cool it
will reach saturationand it getsrid of excess water vapour through
condensation.
-Moisturesupply
If the supply of moistureincreasestheair will have moreof it ,they
making absolutehumiditytobehigher .If the temperatureiftheair
increasesit will absorb even more moisture.Thissituationmakesallplaces
which are near large water bodiesto be humid especiallyif the temperature
is high causing a lot of evaporation. Areasthat arefar awayfrom large
water bodiessuch as desertscenter has little water vapour the air has high
capacityof holding moisture.
IMPORTANCE OF WATER VAPOUR IN THE ATMOSPHERE
- Evaporationformsprecipitation,which providesfresh water plantsand
animals.
- It absorbsboth incoming and radiated energyfrom the sun.
- It conveys Latent heat into the atmosphere
The amount of water vapour the atmospherecanhold depends upon the
temperatureofthe air thehigher the temperatureofthe air the higher the
capacityof it to hold water .
COMMON WAYS OF STATING WATER VAPOUR (HUMIDITY )
(I) Absolutehumidity
Thisis theactualamount of water vapour in a specific volume of
atmosphere i.ethe massof water vapour per cubic unit of air and it is
normally expressed in g/m3
(II) Relative humidity
Thisis theproportionof water vapour present in the air compared tothe
maximumamount ofwater vapour, possible at the same temperatureand it
is usually expressed in percentage.Normallysaturated air hasrelative
humidity100%.
5. PRECIPITATION
17. Thisrefers to water that falls on the earth in liquid or solid forms.Some
commonforms of precipitationarerain, snow, sleet and hail.
Rain
Thisis most commonform of precipitationspread everywhere and it is
liquid form.It forms when tiny water dropletsmergetogether around the
nuclei to form raindrops.After becoming heavyenough they fall down to
the earth surfaceas rain.Rainfallismeasured by an instrument called rain
gaugeand the lines which joinall placeswith equal rainfallare called
isohyets.
Snow
Thisis refered to as solid precipitation, which formswhenair cools to
below the dew point or freezing point and fall down as icewhile falling the
icecrystals mayjoin together toform snow flake.
Sleet
Thisis a frozen or partly frozen raindroplet; it so often referred to as frozen
rain. It is hazardousas it maydestroy crops, bring down power lines and
tree branches
Hail
Thisis caused by super cooling of water particlesina convectionalup shaft
.This super cooling formsthe hail stones .These stone vary in size
depending on the intensityof cooling by that convectionalcewent. It is
more hazardousthansleet. Hail can causecoderabledamagetoproperty
and plantssome hail stones weight up to 2.5 Kilogram which mayhit the
ground at speed of up to 160 km/hr.
All forms of precipitationresult from rising and cooling of air to below the
dew point where condensationbegins.Thevisibleeffect here is clouds in
order for precipitationtooccur the small dropletsof water in clouds must
join together indrops too largeto remainor be sustained in theatmosphere
thus they prefer to fall down on the earth surfaceasprecipitation.
18. CAUSES OF RISING OF AIR
When air risesthere is less pressureon it at the new altitude.Asa result the
temperatureofthe rising air islowered and cools causing that air to
descend and becomewarm. The rateof cooling or heating that resultsfrom
thisverticalmovement of air (ascending deslending) is called adiabatic
rate.
For saturated air therateof temperaturechangeis0.6ºc per 100 meters,
which forms unsaturatedair rateis1ºc per 100 metersand it is called dry
adiabaticrate.
CAUSES OF AIR RISING FOR PRECIPITATION
The causesof air rising arealso known as the types of rainfall or the factors
that influencerainfall. The factorsincluderelief convectionand the water
bodies.
(i) Orographic or reliefcause
Orographic causeofair rising forms orographicor relief rainfall.It forms
when air is forced to ascend as a result of relief featuressuch as mountains
or plateaus. Wheremoist air reachesthe mountainprecipitationformsand
it is called windward sidewhile the other passaway from windward form
the leeward side or rainshadow.
19. When moist air is forced to rise over a mountainrange,cloudsand rain
often occur.
(ii) convectionalcause
Here air is forced to rise as a result of intense heating thesurfaceair is
heated and verticalupshaft toair occur thisprocess is called convectionand
it forms convectionalrainsit is common in summer or hot seasons.
20. (iii) Frontal or cyclonic cause
Wheretwo bodiesof air masses coming from different directionsand with
different characteristicsintermsof temperatureand moisturecontent
meet, the warmer air will be forced to rise and condense to form
precipitation. Thepoint where these two windsor air meet is called front
hence frontalof cyclonic rainfall.
21. Warm air isforced to rise when it is under cut by colder air,cloudsand
sometimesRain.
Importanceof precipitation
i. It maylower temperature
ii. It supplieswater to streamsand rivers
iii. It is a sourceof water watering crops
iv. It absorbssolar radiations
IMPACTS OF PRECIPITATION.
Impactsof precipitationcanbecategorized intopositiveand negative.
(i) Development of water bodies: precipitationencouragesthe
development of water bodiessuch as rivers and lakes. These areimportant
for irrigation, hydroelectricpower generation,transport, supplyof H2O for
domestic and industrialuseand fishing.
22. (ii) Cleaning the atmosphere. Thefalling drops collect the dust particles
and deposit them on thesurface, keeping the atmospherecleanor less
polluted.
(iii) Temperatureregulation: -precipitationespeciallyrainfall, regulatesthe
temperaturesuch that theatmosphereattainsmoderateweather condition
rather thanextremes.
(iv) Soil development precipitationalsoplays an instrumentalrolein soil
development. It encouragestheweathering of rocksand the decomposition
of organic matter. Wherethereis high precipitationchemical
decompositiontakesplaceeffectively.
(v) Encouraging plant growth: precipitationsupplieswater thesurface,
which used by plant for growth. Thishas advantageinthe development of
Agriculturesincewhereis effectiveplant growth there is positive
agriculturaldevelopment.
(vi)Soil erosion:thistakesplacewhen rainfall is very heavy. Erosion is more
pronounced in the areaswhere the surfaceis bareand sloppy Erosion
destroys vegetation, houses, transport systemsetc.
(vii) Outbreakof diseases:when thereis precipitationwater borndisease
such as dysentery. Typhoid, diarrhea and cholera, aswell malaria arevery
common
(viii) Floods: Heavy precipitationleadsto theoccurrenceof floods, which in
turndestroy crops, houses,kill animalsand people etc.
23. (ix) Mass – wasting (massmovement) takes placeas result of the
disturbancescaused byprecipitationon the weathered rock particles. Mass
movement can destroycrops, kill people and animalsand destroy electricity
supply networks as well as causing a lot of damage.
(x) Water pollutionis caused by surfacerun – off cover land Flow and
foods, which collect variouswaste materialsand emptythem in the water
bodieslike rivers. Dams and naturallakes. Some of thepollutants are
deleteriouscharmatultohumanhealth.
6. WINDS
A wind is air in motionwhich alwaysmove from high pressureto low
pressure belts.Wind speed is measured by an instrument called
anemometer whilewind directionismeasured bywind vane. During wind
movement it causessome balancessuch as temperaturebalance, humidity
balanceand pressure balance.
FACTORS WHICH ACCOUNT FOR DIRECTION AND STRENGTHOF
WIND
1. Pressuregradient
24. Variationof pressurefrom one place to another due to variationinpressure
causeswind to develop and move from high – pressurebelt to low-
pressurebelt: the larger the pressuregradient thegreater the winds speed.
2. Coriolis force
Thisis theforce due to earth rotation: It obeys theFerrell's law which state
that"Anyobject moving freely in the northernhemisphereis deflected to its
right whilesouthern hemisphereis deflected to itsleft". Thisforce is called
Coriolis forceand the resultant wind is called geostrophic wind.
3. Friction
Thisis commonespeciallyup to 900 metersabove the sea level due to
mountainsand big valleys, which may reducethe speed and changethe
directionof winds. The influence of frictionstronger on sand surfacethan
on water.
4. centrifugalforce
Thisis theforce due to earth curvatureand thisforce actsoutward whenan
air stream moves on a curved courseas in a pressure system with closed or
curved isobarsis subjected tocentrifugalforceacting outwardsfrom the
center of curvature.
WINDSYSTEMS
Wind systems arerelated to pressurebelts these windsare called prevailing
winds and they are deflected according toferrell's law prevailing windsare
those which blow more frequentlythan other wind in a particular region.
Among these winds aretradewinds westerly and polar.
(i)Tradewinds
These winds meet at the doldrum they arenoted for their constancyof force
and direction.Theyareterribletropical stormswhich occur at certain
season. At the equatorialbelt the air is heated and rises to be replaced by
air moving in (winds) from north and south.Theseform north east trade
25. winds and south east tradewinds which obey ferrell's law.
(ii)Westerlywinds
These blow acrosslatitude35º and 60º to the polar front these winds are
characterized byconstant strength and directioninthesouthern
hemispherewhile in thenorthern hemisphereand masses disrupt much of
their strength .These windsinclude north west and south west westerly
(iii)Polar winds
These winds areof solid air they are morepronounced in the southern
hemisphereand irregular inthe northernhemispheredue to interruption
by mountains.
(iv)Monsoon winds
These are seasonal windsif the pressureof a largecontinent is high the
wind will blow out of it to the sea where pressureis low These arecalled
''offshore winds".
These winds arecommonduring winter in Asia as inland temperatureis
very low while sea temperatureisstill warm and less dense.If the
pressure over a largecontinent is low thanwindsblow intoit from the sea
where pressureis higher.Thesewindsare called "onsharewinds" and they
are commonin Asia during summer.
(v)The upper air movement
Prevailing windsarenormally surfacewinds not very far from the earth's
surface. These systems of wind are of high speed and high altitude
approximately1000 to12000 metersabovethe sea level withinthese winds
are narrow bandsof extremelyfast moving air known as "jet streams"
JET STREAMS
Evidences of strong windsin the upper tropospherefirst camewhen first
world war, several interwar ballonsblown off- coursewere observed
26. travelling at speed in eccess of 200 km per hour. Pilots in thesecond world
war, flying at height above8km found east ward flightsmuch faster and
their returnwestward journeymuch slower thanexpected. Theexplanation
was to and to be a belt of upper air westernizesthe Rossby wave which
form a computepatternaround theglobe.
FIVE MAIN JET STREAMS ARE
There arefive recognizablejet streams, twoareparticularlysignificantwith
a third having seasonal importance
i. Polar front jet stream (PEJS)
Thisoccursin middle latitudesbetween40 and 60 degreesand a height of
9000 – 12000 meter moreor less at the tropopauseinthe hemisphere. The
winds form the divisionbetween theferrell's and polar cells which is the
boundarybetweenwarm tropicaland cold polar air these winds are
responsiblefor giving fine or wet weather on the earth'ssurface.
ii) Sub tropicalset stream (STJS)
Thisoccursat about 12000 metersand 25 to 30 degreesfrom the equator
and form the boundarybetweenthe Hadley and Ferrell cell in effect vortex
associated with themid-latitudecell. They have lower velocitycompared to
PFJS but follow thewest-east pattern.
iii) EquatorialEasterliesset stream (EEJS)
Thisis moreseasonal being associated with thesummer monsoon of the
Indiansub continent.
iv) Arctic set streams(AJS)
Thishas been traced acrossAlaska and Canada at about 7600 meters.
v) Polar night set stream (PNJS).
Thisis recentlydiscovered above the Aretic circleinthe lower Stratosphere.
27. LOCAL WINDS.
Local winds arecontrolled by the surrounded”terrain”or environment they
are not controlled by planetary system of thewinds they are rather diurnal
thanseasonal. There windsdo affect animals, plantsand movement of
industrialpollutants.
LOCAL WINDS INCLUDE THE FOLLOWING
1) Anabatic and Katabatic
i) Anabatatic winds
These are cold local windswhich blow from, the valley buttonup to the
hilltops. They blow in the afternoonespecially in summer. During the day
28. the slopes exruince. Low pressuredue to direct sun rays which makethem
hot and windsmove from buttonupwards. They further condense and
come down causing thebecomefoggy. There winds are called
Anabatic winds.
ii)Katabatic winds.
These are cold local windswhich blow down from hilltops they occur
during thenight where air is rapidlycooled by terrestrialradiationonthe
upper slopes. During the night thevalley slopes becomevery cold as they
lose the heat rapidly, hence high pressure on them. Due to convectional
currentsthevalley buttom becomeswarm creating low pressure. Winds
sink down through the valley slopes and rise up from thevalley buttom .
These winds arecalled Katabolic winds.
29. 2) Land and sea braze.
During the day land becomeswarm morerapidlythanthe sea. Thus winds
tend to move from the sea breeze.
During the night theland cools more rapidlythansea. Thus wind tends to
move from land to the sea thisactionis called land breeze.
Day
31. commonin Alps Mountainsof Switzerland.Whereduring winter theFohn
winds descend from the SwissAlps into Switzerland.
During the sameperiod cold winds blow from Francesouth ward
torwardsMediterraneanSea. These windsare called "Mistral" but in
USA thesame winds arecalled "chinook". Thissituationoccurs
mostly in the leeward side of the mountain. Somelocal windsblow
from the high pressureover the Sahara duringspring. Thesewinds
are warm, dustyand dry becausethey originatefrom thedesert which
is dry.
The Harmattan.
These are NE windswhich blow from the Sahara acrossWest Africa
betweenNovember and March. Thesewinds aredry and dusty becausethey
originatefrom thedesert. The windsblow during winter towardstheGulf of
Guinea where theland is cold while over Mediterraneansea pressureis low
becausethe sea is much warmer thantheland.
Berg winds:
These are thewinds which originatefrom theplateau of South Africa
during winter. At thistimethe high pressure lies over the plateau and it is a
regionof descending air the windsblow out toward the South SE and
SW.Thosewindsare warmer
4) Adiabatic cooling and warming:
32. Thisis thechangeof heat per unit area. It occurswhen air is heated on the
ground which makes it to rise as it raisesit becomescool and sinks down.
Thisis adiabatic cooling and heating.
AIR MASSES
Air mass is a largevolume .of air whose temperatureand humidityare
fairly uniform and covers all extensiveareassuch as desert and ocean
surfacesmoving horizontally at different levels.
- Characteristicsofair mass normally comefrom the regionwhere the air
masses were formed. These characteristicsareretained bytheair mass may
be warm, dry or moist.
CLASSIFICATION OF AIR MASSES.
Air masses areclassified on thebasisof the sourceregions trajectryand
characteristicsof both temperatureand humidity. Onthe basisof
temperaturetheycanbe categorized aspolar and tropicalair masses. By
combining temperatureand humidityfour maincategoriescanbe
distinguished asfollows.
i)Tropical continental.(Tc or CT).
They originateover the continentsin the low latitudessuch as in the desert.
They tend to be warm and dry. But near the equatorialthereistropical
equatorialcontinentalair mass, which consistsreasonableamount of
moisture. Enough to cause precipitation. A good exampleis tropical
continentalair massover the Sahara desert, which iscalled the Harmattan.
ii) Tropical maritime (Tm or mT).
These originateinthe tradewind belts and subtropicaloceansnear the
equator theyare refered to as Equatorialair masses(E) these arewarm and
moist such that theyto yield heavy precipitation, thunderstormsetc
becauseof being unstable. A good exampleis tropicalmaritimeair masses
which originatefrom Atlantic
33. iii)Polar continental (Pc or cP):
These originatefrom thecold land surfacelike the Arctic and Antarctic
regions, including centralAsia,northernCanadawherethey develop in
winter. These air masses arevery cold, dry and stablesuch that they
prevent theformationof rainshowers.
iv)Polar maritime (Pm or mP).
These originateover the oceans 50º North and south of the equator they
are cool, moist and unstable. They yield heavy precipitationastheymove in
land in middlelatitudesand high latitudes.
CYCLONES,ANTICYCLONESAND DEPRESSIONS
i) What areweather cyclones, anticyclonesand depressions?
ii) Explain theFormationof these aspects
iii) Explainthe weather associated with them.
CYCLONES
These are areasof Low- pressuresystem, which originatesontemperature
Latitudebetween200 -600 north and south of the equator cyclonesoccur all
over theoceans except in northernAtlantic ocean. Theisobarsthat
represent a cyclone on a map areclosely spaced and they form a circular
shape. Strong wind spiralsor tends to move towardsthe center clockwisein
the southernhemisphereand anticlockwiseinthenorthernhemisphere.
They also tend to rush upward with strong force called vortex which
surround the center of the cynodes.
IMPORTANCE OF CYCLONES:
The rapid rising air givesto torrentialrainfalland the strong blowing wind
causesconsiderabledamagetopropertysuch as crops and buildings.
FORMATION OF CYCLONES.(Requiredconditions)
34. i) Abundant sourceof warm moist air of temperatureabout 27ºc tothesea
surface
ii) Air must blow in ward and riserapidlyto great height to giveclouds of
great verticalextent, capableofproviding torrentialrainfall.
- A Tropicalcyclonedevelops wherethe air mass brought byto northern
and southerntradewindsmeet that is along the inter – tropicalfront. They
form; over the oceans as theair masses which have traveled over the oceans
have warm moist lower air while the upper layer of air masses tends to be
cool and dry. When two such air masses meet one is lifted up over the other
the rising air cools its moisturecondensesto provide rainfall(torrential).
Tropicalcyclonesmove in a westerly directiononreaching laid they
graduallydie act becausethesupply of warm moist air is cut off.
Warm sea surfaceof temperature27ºc
WEATHER ASSOCIATED WITH TROPICAL CYCLONES
Before thetropicalcyclones arrive
i)Air becomesvery still
ii) Temperatureand humidityrises.
iii) Thickcloudsappear or develop
35. iv) Windsblow violently
v) Dense clouds and torrentialrainfallreducesvisibilitytoa few meters
Examplesof tropicalCyclones aretornadoes, Hurricanesand typhoons.
TORNADO
Thisis a small cyclone that appearsasa blackfunnel cloud, hanging from
high clouds. Its color is a result of themoistureand debrisbeing carried by
wind at a speed of up to 400km/ hr on the ground. It covers a small area of
about 90 – 500 metersin diameters
- The originmechanism of tornadoesis not properlyunderstood however
they are commonlyand mostly associated with theconditionprovided by
the meeting of cold, dry and hot moist air.
- Thus they are associated with cold front originatedwhereturbulence
along therefronts is greatest. Most occur in the USA and are concentrated
in the centralstateof OKLAHOMA.
HURRICANES
These occur in West Indies islands in the Caribbean. Thewind is generally
very slow.
They have similar characteristicswith typhoonsbut the only differenceis
intensitydurationand locality
- Weather associated with hurricanes:
.Calm dense clouds and stormyweather
. Rainless/ dry weather.
TYPHOONS:
Typhoons occur in China. They are most frequent from July to October and
violence is common.
36. They have very steep gradient and cover an area of 30 to 300 kilometersin
diameter. Theyoccur around 20o- 60o north and south of the equator.
- Weather associated with typhoons
Over cast sky
Torrentialrainaccompanied bythunder and lighting
Verydestructive toboth humanand property. For example
50000 people were killed in 1922 on thecoast of china.
ANTICYCLONE
Thisis an area of high pressure which when shown on the isoline map, has
an oval circular shapeofclosed isobar.
Notethat, the highest pressureis near the centre. An anticyclonedevelops
in a regionwhere the air is descending and the winds associatedwith it
blow outwardsin a clockwise directionintheNorthernhemisphereand
anticlockwiseinthesouthern hemispherein West Africa during thedry
season anticyclonecover the Sahara and theyare associated with the
Harmattan.
WEATHER CONDITION ASSOCIATED WITH ANTICYCLONES.
Anticyclonesareassociated with thefire weather, calm air and high
temperatureinsummer but low in winter and clear skies. During winter
intense cooling of the lower atmospheremayresults in thickFog.
DEPRESSION
These are largeareas of low pressuredue to meeting of warm equatorial
and cold polar air. They areoval or circular shared on mapswith closed
isobars. Air of depressioncirculatesanticlockwisedirectioninthe Northern
hemisphereand a clockwisein the southern hemispherewherethey blow
towardsthecenter.
- Depressions mainlydevelop in temperaturelatitudeswhenhumid
tropicalair meetswith cold polar air especially around; latitude60º north
and south of the equator wherewesterly winds meet with polar winds. The
37. zone or boundarywhere these windsmeet or converge is called "polar
front” it is in thiszone where depressionsform.
- Depression arerarely stationaryand theymove in a generale.g. sterly
direction. Somearesmall: others arelarge, but all of them are associated
with unsettled weather usually with overcast skies and periodsof
continuousrain.
- The rain is caused by the uplifting ofthe warm moist tropicalair bythe
cool drier polar air, as they meet or converge at the polar front. Such rainis
called “depressionRain" and it is generally lighter thanconvectionalrain
and has longer durationup to several days.
WEATHER ASSOCIATED WITH DEPRESSION.
Depressions areassociated with clear sky except the circuscloudswhich are
little bit high, winds blow from the south east, after a definitetime, a clouds
cover develops and heavy rainoccursand the warm front then passes, when
the rainstops wind directionchangesand start blowing from south west.
Temperaturerisesand thereoccursmore humid air.
HYDROLOGICAL CYCLE (WATER CYCLE)
38. Hydrologicalcycle (water cycle) refers to the endless circulationofwater
from the surface(rivers, lakes, oceansand vegetation) intothe atmosphere
through evaporationor transpirationand thenbackto the surfaceasrain,
snow, hail or another form of precipitation. Theprocessesinvolved in
hydrologicalincludeevaporationor transpirationcondensationafter
cooling and later precipitationthecombined processof evaporationand
transpirationisknown as evapo –transportation
At first water, getsinto theatmosphereas water vapour through
evaporationfrom the surfaceor transpirationfrom parts.
Later as most air rises, it cools through expansion, leading tocondunsation
through condensationwater dropletsor dropsare formed which later fall
onto the surfaceas precipitation. Aswaterfallsonto the surface, some of the
water in filtratesand percolatesintothe ground to form underground
water. Someflow on the surfaceas surfacerun – off (overland flow) or
stream flow into the oceansor lakes. Someis evaporated backintothe
atmospheretodrive forth the process of hydrologicalcycle. In the process
of hydrologicalcycle,insolationis very important sinceit providesthe
energy that facilitatesevaporationprocess.
39. The diagram aboveshowsthe process which lead to theformationof
precipitationwhich arepart and parcelof the hydrologicalcycle. These
processes includeevaporationor evapo-transpirationcooling condensation
and precipitation
CONDENSATION.
Condensationis the processthrough which the atmosphericwater vapor is
converted into liquid asa result of cooling. If the temperatureisbelow the
freezing point condensationcanbe skipped.Theprocessin which water
vapor changesdirectlyintosolid statewithout passing through liquid state
is called "sublimation". Theterm also applied when the changetakesplace
from solid stateto water vapor without passing through theliquid state
when the temperatureareextremelyhigh.
WAYS IN WHICH AIR COOLS:
40. There areseveral waysthrough which cooling in theair takes placeand
these canbe identified asfollows.
i)Directionradiationofheat energy from the surfaceleads to the cooling of
the air, since heat energy is lost into the atmosphere. Theloss of heat
energy makesthe surfacebecomecold hence influences the temperatureof
air above it.
ii)Horizontalair movement over the cold surface(advection) mayalso lead
to the cooling effect.
iii) Also cooling cantake placewhen warm air mass meetswith cold air
mass on mixing along the the front,thetemperatureofwarm air declines,
leading to cooling.
iv)Another way through which air tendsto cool is by the ascent.The
ascending air cools adiabaticallyasresult air massexpension.
CONDITION FOR CONDENSATION TO OCCUR
Condensationis determined byseveral factorsthat includecooling,
presenceof microscopic particlesand presenceof water vapor.
i)Atmosphericcooling.
The cooling of the atmosphereoccursthrough variouswayswhich include
contact with thecold surfacesmixing ofair masses or through mechanical
uplift.
ii)Existenceofwater vapor
When the air saturated, anyadditionalmoistureintheatmosphereleadsto
Condensation.
iii)Presenceeof microscopicparticlesinthe atmosphere. Theseact as
condensationnuclei which providethe starting point for condensation.
Water vapor molecules tend to collect around the particlestoform water
droplets when the particlesareabsent, condensationtakesplacewith
difficultyunless the atmosphereissuper saturated.
41. COMMON FORMSOF CONDENSATION.
Condensationmanifestsinvarious form namely
Dew
Frost
Clouds
Fog.
Dew
Dew consists of water dropletscondensed and deposited on the cold solid
surfaces. It usually Forms during long nightswith clear skies having little or
no wind when the atmosphereisrelatively moist.Whenthesky is clear
there occurshigh rateof outgoing radiation, which inturnleads to the
cooling of surface.
Frost
Is the term used of meandew that becomesfrozen. The conditionthat favor
itsformationarethe same those. For formationof dew except the
condensationoccursunder freezing point.Desert and semi-desertsare
places wheredew and frost commonoccursat night, since these areascan
sometimesexperiencelow night temperatureaslow below O0C.
Log and mist,Haze.
Fog and mist areclouds at ground level, which result from moisture
condensationand they may extend far in the atmosphere.Fofand Mist
differ in visibility.
Mist forms wheremoist air cools below dew point. Condensationtakes
placebut theresultant water dropletsremainsuspended in kilometers. On
the other hand Fog is like mist and forms in the sameway but it is much
denser as it reduces visibilitytoless thana kilometer. There arevarious
types of fog depending on their mode of formation.
TYPES OF FOG
i)Advection Fog:
Refers to Fog caused by the cooling of warm moist air. Transported over the
42. cold surface. Also, advectionFog can be caused by the cold air passing over
a warmer sea surfacethan mixeswith thewarm air prevailing there.
ii)Radiation Fog
Thisoccurswhen land surfaceis suddenly cooled by radiationwheretheair
upon it becomes chilled which results into condensation. It commonin hilly
areas.
iii)FrontalFog
Thisforms due to passageof warm air over cold air. The warm air is
thereforechilled to form Fog.It forms at the Front of depression.
iv)Upslopeor expansion Fog chill Fog
Refers to the Fog formed when the air-massmoves upslope leading to
adiabaticcooling due to air mass expansion. It forms simplelow sheet
cloud which mayenvelop the hills like, what happenson the hills of
western. Britainwhenmoist air is moving on land
v) Steam Fog
Is the type advectionFog formed when a cold air- mass passesover much
warmer water surfacesuch that water appearsto"steam" In latitudeit is
referred to as ice-Fog. Wherethe moistureinthe air is converted into ice
crystals, steam Fog is rare and does not last for a long period of time.
vi)Sea Fog
Is formed when thesea air cools over thecold ocean currents. It differs
from the steam Fog,inthat the sea Fog does not appear assteam but just as
normalFog. Also in steam Fog, themoving air is cold and stableand warms
over thewarm water surface.
vii)Smog Fog
Thisis Fog plus smoke and industrialpollutant likeCO2, CO and SO2 it is
usually yellowish in color and acidic insmell,smog is commonin big cities
e.g. Ruhr industrialarea inGermany. Fog has major environmentalhazards
particularlyon transportation.
viii)Rime
When a Fog composed of super cooled droplets is driven by slight wind
against prominent objectssuch astelegraph poles, wiresand treesthe
drops freeze on them as rime. The temperatureofboth droplets and the
43. objectsis below freezing point. The rimehasthe white, opaque appearance.
Thisis a commonfeatureon the mountainsof Britain.
CLOUDSAND CLOUDSFORMATION
Cloud is another element of weather. It is defined as a mass of water vapour
which hangsin the sky. Clouds are a form of condensationwhich consistsof
water dropletsor of tiny icebar tidesfloating at various levels from the
ground to the very high altitudes. At 12000m abovethesea level.
- Mist and Fog aremade of water dropletsand in this repast theyare
types of cloud, but they form near the surface.
- The clouds give hint on thetype of weather that islikely to occur
through their shape, height and and natureof movement. Thus they are
carefully studied by meteorologistsinorder to prepareweather forecast and
variousprecautionaryinformationonthe impeding weather phenomena.
On the map cloud cover can be represented by using the lines.
CLASSIFICATION OF CLOUDS
There aremany different types of clouds, but they areoften difficult to
distinguish astheyform constantlychanges. The general classificationof
clouds was proposed by LUKE HOWARD in 1803 this classificationis
based on form appearanceand height and he used four Latin words cirrus,
cumulus, stratus and nimbus.
- High clouds (6,000 to12,000m)
- Middleclouds (2,100 to 6,000m)
- Low clouds (below 2,100m)
a) High clouds 6,000 – 1,200m (consistsof cirruswhich start with
cirro.)
i) Cirrusis composed of small icecrystals, wispy, fibrousor feather. Its
a appearanceisminbandsor patches.
44. ii) Cirrocumulus –is composed of ice crystals:” globular or ripplelike in
appearancelookslike ripplesor wavy structuresinthe sand on a sea shore)
Forming a thincloud.
iii) Cirrostratus- it looks like a thinwhite, almost transparentsheet that
gives the sun and moon haloes.
b) Middleclouds below 2,100 - 6,000m (consistsof clouds whose names
start wish acto)
i) Altocumulus – is composed of water dropletsin layers or patches
globular or bumpy. Looking with Flattened based arranged inline or waves.
Thisindicatesfair weather.
ii) Altostratus –is composed of water dropletsforming sheets of grey or
water looking clouds, partlyor totally covering the sky.
c) Low clouds below 2100m.
i) Stratocumulus: isa largeglobular mass: bumpy – looking soft
and grey in appearanceforming pronouncesregular patten. It is in fact
darker, lower and a heavier type of actocumuluscloud. It always allows the
penetrationofsome our rayscalled crepuscular rays.
ii) Stratus –is fog- like low cloud forming a uniform layer: brings
dull weather and often carom paled by drizzle.
iii) Nimbostratus –Darkgrey and rainy – looking dense and shape
less often gives continuousrainclouds of great verticalextent.
iv) Cumulus: round topped and flat based forming a whitish grey
globular mass consisting ofindividualcloud units.
v) Cumulonimbus – is a lowering cloud which is usually whiteor
blackappearing as globular masswhose rounded tops often spread out
forming an anvil structure. It is associated with convectionrainlightingand
thunder. This cloud is sometimescalled "thunder head".
45. NB:
Cirrusand curriform cloudsoccupyhigh level and form high clouds; clouds
that start with actoarefound in the middlelevel constituting middle
clouds. Nimbusisthe term that appliesto rainbearing clouds; stratus
appliesto clouds that form layers or uniform cover and cumulusis the term
used for clouds that occur in a massivenature.
Clouds at different levels and extent
46. The Amount of cloud cover is estimated inoktas; one oktasrepresents one
– eighth of the sky covered with clouds.
WEATHER CHANGES
ATMOSPHERIC STABILITY AND INSTABILITY
Atmospheric stability
The stateof stabilityiswhen a rising parcelof unsaturated air coolsmore
rapidlythanthe air surrounding it. If thereis nothing to force the parcelof
air to rise such as mountainsor fronts it will sink backto itsstarting points.
The air is described asstablebecausedew point may not have been reached
and the only clouds which might havedeveloped would show flat topped
cumuluswhich do not produceprecipitation. Stabilityisoften linked with
anticyclones.
- Absolutely stableis experienced whenthe ELR is less than theSALR
(SaturatedAdiabaticLapseRate). During absolutestabilityeven the
saturated air, which isusually buoyant (light), tends to cool faster that the
surrounding air and keeps on sinking rather thanrising. Stabilityisalso
called stableEquilibrium.
Atmospheric instability:
Conditionsof instabilityariseinon hot days when localized heating of the
ground warmsthe adjacent air byconductioncreating,ahigher lapserate.
The resultant parcelof rising unsaturated air coolsless rapidlythanthe
surrounding air. In thiscase the environmentallapse ratelies to the left of
the Dry Adiabatic LapseRate, therising air remainswarmer and lighter
thanthe surrounding air.
Should it be sufficientlymoist and if dew point is reached, then the upward
movement may be accelerated toproducetowering cumulusor
cumulonimbustypeclouds. Thunderstormsarelikely and saturated air
following the release of latent heat,willcool at the saturated Adiabatic lapse
rate.
CONDITIONAL INSTABILITY.
Thistype of instabilityoccurswhentheELR is Lower thanthe DALR but
higher thanthe SALR. It is the most commonof the three conditions.
47. The rising air is stablein its lower layers and being cooler thanthe
surrounding air would normally sink backagain.
However if themechanism which initiallytriggered theup lift remains,
then the air will be cooled to its dew point. Beyond thispoint cooling a
slower SALR and the parcelmaybecome warmer thanthesurrounding air.
It will now continue to raisefreely even if the uplifting mechanismis
removed as it is now in an unstablestate.
Instabilityisconditionaluponthe air being forced to risein the first place,
and later becoming saturated sothat condensationoccurs. Theassociated
weather is usually fine in areasat altitudesbelow condensationlevel but
clouds and showery in those above.
- What tonote is that
Unstableair mass is regarded tobe either conditionalor potential.It canbe
conditionalifafter it has reached dew point it cools very slowly to retain
warmnessthat the surrounding and forced to rise higher and higher.
- It is regarded tobe potentialifthe conditionair is forced to rise above
cold air mass. Atmosphericinstabilityisassociatedwith relativefall in
temperature, high humidity(dampness) heavyclouds, sand, heavy rainfall.
These conditionscanbe summarized asfollows:
Stabilitywhen ELR< DALR or (DALR> ELR)
Absolutestabilitywhen ELR< SALR or (SALR >ELR)
NeutralEquilibrium when ELR = DALR or (DALR =ELR)
Absoluteinstabilitywhen ELR > DALR or (DALR < ELR)
Conditioninstabilitywhen ELR is betweenDALR and SALR.
Diagramsrepresentingatmosphericstabilityand instability.
48. In diagramabove.
The line for DALR is below the line for ELR. Indicating thattheDALR is
greater thantheELR and thereforethe air is cooling faster thanthe ELR
leading at atmospheric stability. Inthis casethere is no verticalair – mass
movement since the cold dense air mass tends to sink down to the surface.
49. In the diagram above:
the line for SALRis below theline for ELR indicatingthat theSALRis
greater thantheELR and thereforethe saturated air iscooling faster than
the ELR Leading to atmospheric stability. Alsoin this casethe verticalair-
mass movement is limited, sincethe denser air masstends to sink down to
the surface.
In the diagramabove, theELR is below the line for DALR indicating that
the ELR is greater that theDALR and thereforethe dry pocket of air is
cooling at a lower ratethanthe ELR, Leading atmospheric instability.
Also in thiscase, the verticalair – mass movement is pronounced since the
pocket air mass tends to risebecauseof buoyancyor lightness. Under this
situation, thesecanbe condensation, freezing and precipitationinthe
atmosphere. Stormsalsodevelop, affecting theearth's surfaceand its
variousfeatures.
50. In the above diagram:
One can find that beforecondensationis thelower altitude, theair is dry
and DALR is greater thantheELR. The atmosphereexperiencesstability.
As air is forced to risethe cooling processleads to condensationwhich
saturatestheair. The saturated air becomeswarm due tothe additionof
moisturewhich haslatent heat. It then startsrising spontaneouslywhile
cooling at the SALR, which is lower thanthe ELR. This situationmanifests
the attainmentofa stateconditionalinstability.
CAUSES OF AIR – MASS ASCENT.
Pocketsof air areforced to rise several ways, which include;
51. i) When the air- massis heated or warmed by conduction, air risesin
conductiontheheat energy which is reflected from the earth’ssurface
warmsthe air resting above; then verticalconvectionalcurrentssetsup.
Thisphenomenon leads to the formationof convectionalrainand it is
commonin the equatorialand tropicalareas. Theconvectionrainfalls in
the afternoonand is usually accompaniedbyrainfalland thunder.
ii) The pocket of air can riseafter being forced mechanicallytorise up the
slope incasethe wind blows against themountainside. The air massthat
rises cools leading to condensationand later the formationoforographic
rain, which is commonin mountainareaslike Kilimanjaro, Uluguru,
Rungwe, Meru and Usambara inTanzania.
52. iii) Thethird way involves the situationwhereone air – mass, usually
warm is forced by another massof air which is usually cold. The warm air
rises above thecold air creating a zone of contact inbetweenthem called
front. In most cases of raising air a verticalelement is introduced which isa
form of convergent rotation. Under thissituationa depressionis usually
created, which isassociated with law pressure formationofclouds and
rainfallformation.
It should be noted that when the air-massiswarm, it tends to expand and
it always lighter, such that it keeps on rising above.
TYPES OF TEMPERATURE INVERSIONS
a) According tothecauses, temperatureinversionscanbe categorized into
four types namely :
- Subsidenceinversions
- Advectioninversions
- Radiation(nocturnal) inversion
- Frontal inversion
53. i)SubsidenceInversionis formed where the air is descending in the high
pressurezones. The sinking of the air leads to compression, which in turn
causestemporaryinversionat a higher level in the atmosphere. Thistypeof
inversion is also called high inversion and usually last a long time.
ii) Advectioninversion is caused by a warm air massadvancing acrossthe
cold surface. The lower portiongets cold while the upper part remainwarm
thiscan happenover thecolder sea in summer or over the land massin
winter.
iii)Radiation(nocturnal) inversionisthe type of inversionthat occurs
during night when the land is very cold becauseof having lost most of the
heat energy through radiation. Nocturnalinversionoccursexclusively over
the land as the ground cancool much more quicklyafter sunset, thanthe
sea. It is also called ground level inversion as it is near the surface. This
type of inversion disappearswhenthe sun rises in the Morning.
vi) Frontal inversion which occursasa result of the formationofwarm and
cold front due to meeting of two air masses. Thewarm air rises over the
cold air mass keeping the atmosphereabovewarm whilenear the surface.
b) According tothelevel of occurrence:According tolevel of occurrence
temperatureinversioncanbeclassified as ground level and high level
inversions.
i.Ground level inversion is the type of inversion that takesplace near
the surfaceof the earth due to cooling, caused by the lose of radiant energy
into thespace. The air near the surfacetends to be cooler thanthe air above
it. Sinceit is in contact with thecold surface. It takes placeat night and
disappearsinthe morning whenthe sun arisesNocturnalinversionis
good.Example;
54. The above hypotheticaldiagramindicatesthattemperatureinversiontakes
placenear the ground level due to the influenceof surfaceradiationsuch
that as one moves from 0 to 45 meters abovethe sea level will experience
the rise in temperature. After 45 metersof altitudethetemperaturestarts
decreasing at a normal lapse rate.
ii.High level temperatureinversion
Takes placeat upper levels of the atmospherefor example, after 145 meters
above the sea level . It canbe caused by air subsidencepresence of water
vapour or a layer of Carbondioxideand Ozone. It is usually last longer than
55. the ground level temperatureinversion.
iii.Theabovehypotheticaldiagram illustratesthat from 0 to 145 metersis
above the sea level the temperaturedecreaseswith altitudeat a normal
lapse and after 145 metersit tends to increasewith increasein
altitude(temperatureinversionoccurs).
ATMOSPHERE
Thisis thethis layer of gasesheld on the earth by the gravitationattraction.
Composition of atmosphere
Describeand explainthe compositionof theatmosphereatmosphereis
composed of the following;
56. i. Mixtureofvariousgases theseincluded oxygen21% nitrogen78% Argon
0.09% and Carbondioxide0.03%othersincludeneon, xenon, krypton
helium and others in minutepercentages
ii. Dust particledust particles maybe naturalor artificialwhere
naturaldust particlesarethose caused by wind and volcanic eruptionwhile
arterialdust particlesarethosederived from industrialpollution
iii. Water vapour thisis colourless, odourless gas in form of water
which makesup a perfect mixturewith gases. The degreeat which water
vapour is present in the atmosphereintermed as humiditywater vapour
condenses in term of rainsnow, mist excess water vapour bringsabout
capitationinform of rainsnow, sleet and hail when water vapors is present
in the atmosphereinsmall quantityextremedrynessof air many cause
occur of hot desert.
THE STRUCTURE OF ATMOSPHERE
Atmosphereisdivided into layers according totemperaturetheselases are
i. Homosphereand
ii. Heterosphere
A. HOMOSPHERE
Thisis thelower part of atmosphererunning from 0-80km above the sea
level. Thislayer has there sub layers which areTroposphereStratosphere
and Mesosphere.
1. Troposphere
Thisis thelowest part of homospherefound between 0-9milesor 0-15km
above sea level, the layer is composed of gases water vapour and dust. All
processes of rainformationtakeplacein this zone and temperature
decreaseswith altitudeat a normal lapse rate. The lapse ratein
Troprosphereis 0.6 ºC per 100 metreswhich is equivalent to 6.5ºCper
1000 metresrise. The lapse theresult of thefact that the earth'ssurfaceis
warmed by incoming solar rotationwhich inturnheats theair next to it by
conduction, convectionand radiation. Thetropopausewhich formsthe
57. upper limit to earth'sclimateand weather is marked byan isothermallayer
where temperatureremainsconstantsat -80ºC.
2. Stratosphere
Thisis thesecond part of homospherelying above tropopausebetween48
kilometresabove the sea level. Much of the zone layer is concentratewithin
thiszone particularly15 to50 kilometresabove the earth’ssurface.
Sometimestheterm ozonesphere is used to refer the layer where there is
concentrationofozone gases. Temperatureremainsunchanged with
increasing height at tropopausebut later it start to increasewith height the
lower stratospherecover about 15 to25 kilometrefrom the earth'ssurface
thisis the layer in which temperatureremainconstant. Thissteadyiscase
in temperature(temperatureinversion) iscaused by concentrationzone
(O3) thisgas absorbsincoming ultra violet (UV) radiationsfrom sun. The
stratopausewhich markstheupper limit of thiszone is other isothermal
layer where temperature doesnot changewith increasing height.
3. Mesosphere
Thisis thethird part of homosphere lying abovestratopausebetween48to
80 kilometersabove the sea level where temperaturedecreaseswith
altitudeup to -100ºCat 80 kilometersabove the sea level. Temperature
falls rapidlyif thereis no water vapour, clouds, dust particlesor ozone to
absorb incoming radiations. Thusthislayer experiencestheatmosphere
lowest temperatureand strongest wind. Themesopauselike the tropopause
and stratopausewhich istheupper limit of this zone records theminimum
temperaturethatmayfall to -100ºC and thus shows no further changesin
temperature.
B. HETEROSPHERE
Thisis is thesecond zone of atmospherewheretemperatureincreaseswith
altitudefrom -100ºC at 80 kilometresto about 500ºCat 8o-5,000
kilometresabove the sea level. The increaseof temperatureisassumed to
be so becauseof lack of water vapour and dust particleszone. The upper
part of this zone is called Ionosphere which is sometimesdivided into
exosphereand thermosphere. In the thermospheretemperaturerises
rapidlywith height perhapsto reach 1500 ºC . This is due to an increasing
proportionof atomic oxygenin theatmospherewhich like ozone layer
absorbsincoming Ultra Violet radiations.
58. TEMPERATURE INVERSION
Temperatureinversionrefersto the increaseintemperaturewith height
above the earth’ssurface. Thisphenomenon is a reverse of the normallapse
ratein the atmosphere; it isthe exceptionallapserate. This situationof
increasein temperaturewith altitudeiswhat called reverse lapse rateor
abnormallapse. In temperatureinversionit meansthat, temperatureinthe
air far abovethe ground.
CAUSES OF TEMPERATURE INVERSION
I. Presence of ozone layer in the atmosphere
Ozone in the atmosphereabsorbsenergyfrom the sun especially ultra
violet(UV) rays. The reactionbetweentheserays and ozone gives out heat
whit warmsthe atmospherefrom the ground surface.
II. Formation of fronts
Thistakes placewhen twoair masses of different temperaturemeets. On
meeting thewarm air rises above the cold air. Under thissituationtwo
fronts areformed such that thewarm front is aboveand the cold air leading
to temperatureinversion.
III. Air subsidence
When thereis high pressure air tends to descend or sink down. The
downward of air leads to compressionor frictionbetweenmolecules thus
creating warm conditioninthelevel.
IV. Atmosphere components
Water vapour and dust particlesat a higher level, keep the atmosphere
warmer thannear the surfacesince it preserves energy from the sun for a
longtimewhich leads to temperatureinversion.
V. Advection
When the massof warm air passesover the cold surfaceitslower part is
cooled by the cold surfaceleaving the upper portionwarm becauseof being
far awayfrom the influenceof thiscold surface.
VI. Radiation
59. Radiationofinfra red energy from the earth'ssurfacemakesthe ground
cool very quickly. The cold surfacecools the air immediatelyaboveleaving
the other layer far above warm. For example; during clear settled weather,
as radiationofheat takes placeduring thenight the air on hill - slopes is
rapidlycooled and thusdense air drawndown wardsfilling valleys or
basinswith cold air possibly at temperaturebellow freezing point, when the
upper slope are markedlywarmer.
VII. Water vapour
Water vapour at higher altitudeskeepsthe atmospherewarmer thanair the
surfacesince it preserves heat energy for a long time. Thisalso causes
temperatureinversion.
EFFECTSOF TEMPERATURE INVERSION
1. The warmer layer of air above the cold air may lead to increasein
atmospherestabilityand verticalair mixing assuch the temperatureis
always calm with no precipitation. But when inversionoccursdue to the
development of precipitationand formationof cyclonic storm.
2. Temperatureinversionleadsto the formationof fog and smog. Smog
is commonin the industrialized areaswith a of smoke which is produced
from industries. Thesmoke so produced mixeswith fog to from smog.
3. Air pollutiontakes placewhen there is temperatureinversion.Theair
is polluted becauseof the sinking of particleswhich arehanging inthe
atmospheredue to the fact that the warm air abovethe cold air is less
dense and thus not capableof holding the particlessincethey aredenser
thanthe warm air. The sinking down of air to the lower atmospherelevel
causesair pollution which affect humanhealth, animaland plants. It can
causeitching of body, inflammationofeyes and coughing.
THE HEAT BUDGET
The sun's energy is called insolationor solar radiationwhich turnsintoheat
energy at the earth surface. Insolation travels through spacefrom the sun
inform of waves and interact with outer edgeof atmospherebeforereaching
the earth'ssurface. Totalamount of solar radiationreleased from the sun is
100% sincethe earth is neither warming up nor cooling down, therebe a
balancebetweenincoming insolationand outgoing terrestrialradiation.
The atmospheric conditionthereforereducestheamount of solar insolation
60. through threeprocesses;
1. By absorption: About 15% of totalsolar radiationisabsorbed inthe
atmospherebythe atmospherecomponents. Thegreater absorbersare
water vapour, dust particlesand clouds.
2. By reflection: Certainamount of solar radiation isreflected backinto the
spaceby clouds, dust particlesand ground. The amount of insolation
reflected depends on the surfacebut the averagereflectionamountsto40%
of totalinsolation.
ALBEDO
Albedo refers to the percentageexpressionofthe ratiobetweencoming
radiationsand theamount reflected. Clouds and to a less extent, the earth
surfaceare theprincipalreflectorsof the incoming radiationsbackinto
space. The albedo varieswith cloud type from 30-40% inthinclouds, to 50-
70% in thicker stratus and 90% incumulonimbuswhereonly 10%
61. insolationreachesthe atmospherebelow the cloud level. Albedo also varies
over different land surfacefrom less than 10% over oceans and darksoil, for
15% over coniferousforest and urbanareas25% over grassland and
deciduousforests40% over light coloured desertsto 85% over reflecting
fresh snow. Thisreducespossibilityat icemeet and disappearson
mountaintopslike Kilimanjaro.
THE OZONE LAYER
The ozone layer is found withinthe stratosphereand it sometimesre-
termed as a shield of life. The layer is highly concerned with humanand all
other earth life and it sets in at an altitudeof about 15km and even upward
to about 55 kilometers. Thislayer serves as a shield protecting the
troposphereand the earth surfacefrom most violent raysor radiationfrom
the sun. If these rays were to reach the earth directly, all bacteriaexposed
would be destroyed and animaltissueswould be damaged.Destructionof
thislayer by some scientific discoverieshasmadetheintensityof ultra
violet rays reaching theearth surfaceto increasecausing globalwarming. If
thissituationisleft to continue, it will causesuffering particularlycancer ,
crop reductionin yield and killing of organismson land, water and air.
FUNCTION OF ATMOSPHERE
1. It is an insulator: It moderatestemperatureduring night winter.
2. It is a filter: It filters solar insolationthrough ozone layer and provides
a layer through which meteorsare burnt intogases.
3. It is a scientific field whereradio, radar, televisionand other
communicationincluding air transport and telephonesare done.
4. It has hydrologicalfunctionwhere rainfallis formed.
5. It support itslife through breathinginanimalsand respirationin
plants.
CLIMATOLOGY
Climatologyisthe studyof climatethat dealswith spatialdistribution
atmospheric phenomena. It mainlydeals with definitionand descriptionof
different climatesintheir geographicalsettings.
62. Meteorology isthestudy of weather. It is a scientific studyofthe physical
process constantlyat work in the atmosphere. It is highly applied in the
forecasting ofthe futuretrend of the weather. It is a branch of Science
which deals with the conditionsof or withinthe atmospheresurrounding
the earth.
Climatologyand meteorology arethe studiesor thesciences which are
concerned with the study of atmosphereand its elements like weather and
climate.
CLASSIFICATION OF CLIMATES
By studying theweather, the atmospheric conditionsprevailingat a given
timein a specific placeor area; it is possible to makegeneralizationabout
the climateof that placeor area basing on the averagenormalcondition
over a period of timeusually 35 years. In seeking a sense of order; the
Geographerstryto group together those partsof world that have similar
measurableclimatic characteristicsintemperature, rainfalldistribution
winds, etc.
Classificationofclimateisdone in different systems.
Greek’s classificationsystem.
Germanyclimatologist classificationsystem.
Koepen's temperaturezones classificationsystem.
Miller'sclassificationsystem.
GREEK CLASSIFICATION SYSTEM
The early Greeks divided the world intothree zones based upon a simple
temperaturedescription. A classificationofclimatebyGreek is based on
temperaturecontrolofthe climateand they completely ignored
precipitation. Under thisapproach climateisdivided into:
i) Tropicalclimatewheretheamount of temperatureishigh.
ii) Temperateclimatewherethetemperatureismoderatei.ebetweenthe
tropicaland polar temperaturecondition.
iii) Polar climatewherethe temperatureisextremelyLow.
KOPPEN’SCLASSIFICATION SYSTEM
63. In 1918 Koppen advanced themodern classificationofclimate. To support
his claim that naturalvegetationboundariesweredetermined byclimate,
he selected as his basiswhat he considered were appropriatetemperature
and seasonal precipitationvalues.
The classificationofclimateby thisapproach isbased on the duration
above or below the value belt. By thisapproach climateisclassified intothe
following belts;
Tropicalbelt
The climatehaving 12 months with temperatureabove20oC.
Sub- tropicalbelt
The climatehaving 4-11months with temperatureabove20oC.
Temperaturebelt
The climatehaving 4 – 12 monthswith temperatureranging from
10oC– 20 oC.
Cold belt
Thisinvolves those areashaving 12 monthswith the temperature
ranging from 10ºCto 20ºC.
Polar belt
The climatehaving 12 months with temperaturebelow 10oC.
CLASSIFICATION BY GERMANY CLIMATOLOGIST
According toGermanyclimatologist, climatedivided intothefollowing
types;
Hot zone climate
The climatewith temperatureisothermof20oC annually.
Cold zone climate
The climatewith annualtemperatureisotherm of10ºCor below.
Temperaturezone
The climatewith temperatureisotherminbetween10oC – 20oC.
64. MILLER’S CLASSIFICATION SYSTEM
In Britain, inthe 1930s, Miller proposed a relatively simpleclassification
based upon five latitudinaltemperaturezones which he determined by
using just threetemperaturefigures. Thisisthe most popular method of
climateclassificationtodaybecauseit combinesboth mapsof
temperatures, showing temperaturebymeansof isothermsand map of
rainfallshowing rainfallby meansof isohyets. It shows a close relationship
to vegetationzones and thisit is easier to use and convenience.
- The structureofclimateclassificationisasfollows;
Hot zone - With temperatureabove20oC.
Warm zone - With temperatureranging from 10oC – 20oC.
Cool zone - With temperatureof 10oC.
Cold zone -With temperaturenear to0oC .
Arctic zone -With temperaturenear to0oC and below.
CLIMATIC FEATURES
Dry warm summerswith offshore trade winds.
A concentrated rainfallin winter with offshore westerly.
Bright sunny weather with hot dry summer and wet mild winter.
Presenceof local winds around the MediterraneanSea e.g.
moroccoand Muscat.
Annual rangeof temperatureishigh about 11ºC
Rainfall is moderateabout 838 mm and normally falls during
winter and it is cyclonic raintype.
Summer temperatureisabout 21ºCand winter is 10oC, hence
high rangeof temperature.
VEGETATION
Evergreen coniferousforest, Mediterraneanbushesand grassessemi arid
shrubsas well as grasses, evergreenMediterraneanforests.
ECONOMIC ACTIVITIES:
Crop cultivationdue to high rainfall and moderatetemperature, Animal
rearing i.e. transhumance(pastoralism) orchard farming with different
kind of fruitsand vegetable(market gardening).
65. EQUATORIAL CLIMATE
Thistype of climateoccursasa belt around the world at about 5º North and
South of the Equator but it is also found around 5º-10º North and South in
some places. The continuityofthis climatehowever is interrupted in
several places by mountainssuch as Andes of South America and theEast
Africa high lands.
DISTRIBUTION OF EQUATORIAL CLIMATE
Zaireand Congo basin, Amazonbasin, East Indies, South Ivory Coast, and
WesternCoast Nigeria, EasternCoast, Malaysia and North eastern
Australia.
PROBLEMS OF CLIMATE CLASSIFICATION
Classificationofclimateposes moredifficultiessincethereis no clear
boundarydue to the fact that climatesareTransitional. Thusall
classificationshaveweaknesses, non is perfect because;
- They do not show transitionzonesbetween climates, and after the
divisionlines arepurely arbitrary.
- They do not allow for mesoscale variationsuch asthe lake and
district or microscalevariation(localvariation).
- They can be criticized for being either too simplistic (miller) or too
complex.
- They ignorehumaninfluence and climaticchangeboth inthe long
term and the short term.
- Most tend to be based upon temperatureand precipitationfigures,
and neglect recent studiesin heat and water budget, air massmovement
and the transfer of energy.
- All suffer from thefact that some areasstill lack the necessary
climatic datatoenablethem to be categorized accurately.
GENERAL CLASSIFICATION OF CLIMATE
A: MEDITERRANEAN CLIMATE
The warm temperatureWesternmarginor the Mediterraneanclimateis
66. confined in the Westernmarginof continentallandmassesbetweenlatitude
30o-40o North and South of theequator.
Areas involved
CentralChile, California, CapeTown, SouthernAustria, South West
Australia, SanFrancisco, and partsof Morocco.
CLIMATE CHANGE
It has been noted that a certainarea experiencea certain climaticcondition.
Thereforeany deviationfrom the expected conditiondenotesfor a climatic
change. There areseveral evidences of climaticchange. Theseinclude;
rocks arefound todayin areaswhich seems to have a different climatic
conditionunder which they formed, fossil landscape, sea level changes,
shifting of vegetationbeltsSahara, etc.
CAUSESOF CLIMATE CHANGE
For the factorsor causesof historicalclimaticchange, refer to the theories
which explainthe iceages.
Note: However todaythe world is experiencing theso called “Global
warming” Scientistshavereached a consensus on this point of global
warming asa published by the InternationalPanelon climatechange
(IPCC).
Global warming mayrefer to the world wideincreasein the lower
atmospheric and terrestrialtemperature. Thismaybe as a result of increase
in the concentrationof one or moregreenhouse gases(GHG) as well as the
Ozone layer depletion. Global warming ismainlytheory assertsthat the
increasing levels of GHG will progressively trap moreof the Earth'sheat,
graduallywarming theglobalclimateasmuch as 3 to 9 degrees. However
the reasons which have been put forward to explainthe scenarioarerelated
to those activitieswhich pump theGHG intothe atmosphere. Therefore
manthrough different activitiescarried out for his triggersoff climate
change.
The Marjoryinclude;
CFC’s and Halons: Scientistsfirst suggested in1974 that theworldwide
use of CFC’s and halons could be destroying theOzone layer.
67. In 1982, British scientist for thefirst timedocumented theexistenceof a
largehole in the ozone layer over the Antarcticathat had beentheoretically
predicted earlier. In thiscase theemitted CFC’s and halon react with the
ozone in the stratospheretobe depleted which formally absorbed some
incoming radiation. CFC’sis emitted from coolants in air conditionersand
refrigerators, propellantsinaerosol spraycans, cleanersfor electronic parts
such as computer chips, productionand burning ofplastic foam products.
Fossil fuel burning: Like coal burning inindustriesbeforethe
introductionofalternativeenergysource; this could emit large amountsof
GHG such as carbondioxideand methaneintothe atmosphere. The
industrialrevolutionsparked off the extractionof the coalto run the
machinesor industrieswhich had sprung up. The perpetualburning meant
continuousemissionof carbondioxideand sulphur hence contributing
through the greenhouseeffect.
Deforestation: Thisinvolve the clearing of vegetationand burning of
grassland for either establishment ofsettlement/industriesor agricultural
activities. Thisresultsinto the accumulationofcarbondioxidewhich would
have been taken up by plants.
Cultivation of rice: Thisis couple with the release of methanegasinto
the atmosphere.
Livestock farming: Animalslike cattleproducemethanegasdue to their
microbialfermentativereaction. Thereforethedumping ofcow dung will
release too much methaneas it decomposes. Animalhusbandryisthought
to be responsiblefor much of the increase.
Ozone layerdepletion: The chemicalreactionswhich takeplace
betweenthe GHG may breakdown or deplete the ozone layer. Thismakes it
thinner or drill a hole making it easier for more insolationto pass through
to reach surface. Thereforethe more insolutionreaching theEarth’s
surface, the more thetemperaturewillincreasehence climatechange.
Industrialization: Someindustriesemit GHG intothe atmosphereto
changethe climatethrough thegreenhouseeffect aswell as reacting with
the ozone layer.
Transportation: Automobileemit carbondioxideduring thecombustion
of fuel in the engine which act as GHG to contributetheglobalwarming.
68. EFFECTSOF CLIMATIC CHANGE
The effects we feel or observe are rarely, if ever, the effects of a single factor,
they are combined impactsofthe whole of factors(pollutants) acting over
the totallife span, and frequentlythe effects are synergistic. For instance
both plant and animalsmay be so stressed by climatic changeand become
vulnerable to other environmentalfactorssuch as attackbyparasitesand
diseases.
Given the complexityofthis situation, it isextremelydifficult todetermine
the effect of any particular factor. Neverthelesssome significantprogress
has been madeto link climatechangeand some effects, these mayinclude;
Soils: Higher temperaturescould reducethe water holding capacitiesand
increasesoil moisturedeficits. It should be noted that climatechangewill
alter the chemical, biologicaland physicalpropertiesofthe soils. The
expected temperatureraiseand related prolonged droughtswill increase
the rateof soil organic matter decompositionthusaccelerating land and
soil degradation. Thiswillescalatesoil fertilitydepletionresult into low
productivity. On theother hand, theanticipated floodsin highland areas
will acceleraterunoff and soil erosion.
Flora and fauna: Higher temperaturesand increased water deficits
could meanloss of several species. Thisis becausethe exiting flora and
fauna cannot adjust drasticallyto acclimatizetothenew climatic
conditions.
For instancethe increasing temperaturemayaffect theaquatic animalslike
fish which are used to cool/cold environment. In which additiontothat, the
changein climatewillchangein the qualityof the different habitatsand
consequentlyall the flora and fauna in them. The habitatsmayinclude;
wetlands, forests, etc.
Agriculture: Agriculturalactivitieswhich entirelydepend on rainfallwill
be hit by climatechangesuch as prolonged drought, unreliablerainfallare
evident in some areas. Droughtslower the productivecapacityof rain –fed
agriculturehencereducing theagroexports, increasing food prices,
nutritionaldeficienciesand destabilizethemacroeconomies. Cerealswill
be hit by dry seasons hence a reductioninthe productionofcrops. For
instanceaccordingtoNAPA (2007), intheLake Victoria basininTanzania,
maize productivityisestimatedtoreduceby 17% due to the anticipated
69. climatevariabilitymanifestinginform of temperatureraiseand reduction
in rainfall.
The increasein thenumber of pest and diseases due to climatechangeisa
set-backinthe agriculturalactivities.
Coastal regions: Rise in sea level, increaseinheight of stormsresult into
more flooding especially around estuaries. Flooding affectshousing,
industry, farming, transportand wildlife. Flooding increasesthe
susceptibilityof water borne diseasesalong lake shores, coastlines, and
other placesliable to flooding. For instanceinUganda the outbreaksof
malaria, bilharzia, and other water bornediseases were reported to as often
occurring during and immediatelyafter floods, (UgandanNAPA 2007),
According totheTanzania NAPA (2007), Malariaprevalencehasbeen
reported tom occur in areaswhere it wasnot commonly found in the
previousdecadefor examplein some partsof Kagera, Musoma, Mwanza in
Tanzania; Kisumu and Kiisi in Kenya. In additiontotheeven the icecaps
for instanceon the KilimanjaroMountainhastremendouslyreduced as a
result of accelerated icemelt.
It is also anticipatedtoacceleratethepopular icecap melt too. During the
century, sea level rose about 15 cm (6 inches) due to melting of ice and
expansionof warmer waters. Models predict that sea level may riseas much
as 59 cm (23 inches) during the Century, threatening coastalcommunities,
wetlands, and coralfees. Arctic sea iceis melting. The summer thicknessof
sea iceis about halfof what it was is 1950. Glacier and permafrost are
melting for instanceover the past 100 years, mountainglacier inall areasof
the world have decreased in size and so has the amount of permafrost inthe
Arctic.
Water: Water ismost likely to becomescarcedue to the increased ratesof
evaporationaswell as the variationintherainfall patterninsome areas.
The anticipated climatevariabilityinform of long droughtswill worsen the
availabilityofand accessibilitytocleanwater particularlythepoor or those
who depend on rivers, streams, boreholes. Thisis becausesuch sourcemay
be dried out or lowering of water levels, in springs, rivers, underground
aquifers. Communitieswillveer to any availablewater irrespectiveofits
qualityhence pausing a danger for water borne diseases, hardenthe
productionof hydroelectric power, limit water transport. For instancethe
declining water levels of lake Victoriain2002 to2004 left many boat
landing sites and harbourshigh and dry thusaffecting water transport
70. negatively; the extensionof the Owen falls dam (Kiira and Nalubaale)
opened in 2000 appearstohave been designed to operatewith conditions
of high averagewater levels seen between1960 1990 basing on the inability
of thepower plant to operateat full capacityduring thelow water levels of
2002. In Tanzania, thepower cut off wasextremealso as the mega like
Kidatu could not operateat full capacity. Thiswasportrayed through a
more than12 hours cut off.
Tourism: It predominatelydependson thebeautifulglamorousnatural
featureslike mountains, habitatsand associated flora and fauna. Climate
changewill distort the naturalenvironment toas well affect the tourism
sector negatively. To makemattersworse, floods may destroythe roads to
accessthe distant tourist sites. Thisis becausemost of the tourists
attractionsitesarelocated in theremote areasof which their roads are
impassableduring therainyseason. Sincethe rainfallpatternisunreliable
and unpredictable, thiswillimpedethe movement of the touriststosuch
sites. The scenariowill ultimatelyslump the economieswhich depend on
tourism.
Climatechangewill affect all thedifferent sectors of a countryand
ultimatelythemicroeconomicalstatusof thegreatlyaffected areasor
countriesmoreso the developing countries. Thisis becausethey may not be
robust enough to copeup with the changeshence rendering them
variabilityand change.
Strategies to address Climate change.
It is responsibilityfor all people at a household or communitylevel, NGO’s,
government, regionalgroupings, and the internationalcommunityat large
to striveto reverse the situation. Thisisbecauseeveryone contributestothe
existenceof the problem though the magnitudeof contributiondiffers. To
makemattersworse, theeffects cut across i.e affectsall. However it may be
difficult toreverse thesituationbut theefforts should revolve around
strategiestoadapt tothe climatechangesaswell as reducing theemission
of GHG.
Some of the avenues to fight climatechangemayinclude,
Renewable energy sources: Countriesshould adopt the use of
renewableenergy resourcessuch as solar, nuclear, biogas, geothermal, etc
which are environmentallybenign.
71. In thiscase they should advocateagainst theuseof fossil fuel such as coal,
petroleum and naturalgaswhich emit theGHG.
Afforestation: people should indulgein the policieswhich encouragethe
plantationoftrees such as agro-forestry. Thisis becausetheyact as carbon
sink to minimizetheamount of the carbondioxideinthe atmosphere.
Ambient standards: The Internationalcommunityshould agreeon the
maximumamount ofGHG to be emitted bya source point like an industry.
In the extremecaseswhere theGHG can’t be curtailed, thestrategymaybe
inevitable.
Use of ethanol or gasohol: The vehicles and other automobilesmayreplace
petroleum with the use of ethanol and gasohol Biomassfrom sugar cane
canbe used for the productionofethanol which replacethe usageof fossil
fuel (petroleum inclusive) thiswill minimizetheGHG which could be
emitted thecombustion.
Abatement policies: Countriesshould be stringent onthose who emit more
thanthe ambient standards. Abatement policiesmyinvolve thepay or cost
to cater for the damagecaused bythe extra emissionsthecost as
disincentivestopollution.
Comply to the relevant Conventions: signatoriesshould implement
accordingly. For instancethe 1985 Vienna Convention on the protectionof
the ozone layer Depletion. The convention requirespartiestotakeconcern
to the assessment of the cause, effects of ozone layer depletion as well as
transmissionofinformationand exchangeof informationand Technology
to reduceozone layer depletion.
Note; the convention wasamended in Montreal1987 to becomethe
protocolon substancethat depletetheozone layer. It was later revised in
1990 in London and Stockholm in1991.
It representsa much more significant agreement thantheconvention.
It sets a firm target for reducing and eventually eliminationofconsumption
and productionofa rangeof ozone depleting substances. It recognizesthe
equityof treatment of all Nationsthat produceozone depleting substance
including thedeveloping countrieswhich produceless.
72. The protocolalso deals with the problem of non- partiesby banning trade
in ozone depleting with those statesto controlthe use.
Produceless ozone depleting substances. Thisisattained through
technologicaltransfer.
Restrict theimportationofozone depletion substancesthrough
identifying and monitoring mechanism. For instanceRevenue
authoritieslikeTRA, URA jointlywork with the Environment
authoritieslikeNEMA, NEMCin Uganda and Tanzania respectively.
In thiscase, the environmentalauthoritiesspecifytheozone depleting
substanceswhilethe revenue authoritiesescalatethetaxestonarrow
down the importation.
Research and educationofthe stake-holdersabout the substances.
Thiswill also increaseon thenumber of technicalofficerstoease the
monitoring.
Internationalcooperationthrough thesharing and transfer of
information.
Establishment ofincentiveslike subsidyto encouragetheuse of
substitutesand disincentivestoprohibit theof ozone depleting
substancethrough taxation.
There arevery manykey players toward theadaptationtothe climate
changeand chopping ofGHG emissions.