geographi l5 2

8/17/2019 geographi l5 2

1/164

• Latitudinal variation

• It decreases fromequator to poles

• But highest

temperature is notat the equator butat the tropics

• Reason: high

rainfall, cloud cover(high albedo/reection ofsunrays

!emperature "attern of the #cean


2/164

•

$emisphericvariation

•%orthernhemisphere

&armer thansouthern

•Reason: largeland mass in

northernhemisphere 'high energy

!emperature pattern of the #ceans


3/164

• nclosed seas

• )arginal seas oftropics &armerthan open #cean

* marginal seas oftemperate regioncooler than openseas

• Reason: lessmi+ing of &ater



4/164

• #cean

currents

• armocean

current '&arminge-ect

• .old ocean

currentcoolinge-ect



5/164

• p0&elling and

do&0&elling

• p&elling bringcool &ater from

depth 'lo&erdo&n the surfacetemp



6/164


7/164


8/164

•Bigger thesi3e of ocean0better mi+ingof &ater and

heat• Lo&er annual

range

•

"aci4c ocean 'lo&er annualrange than5tlantic #cean

5nnual range of temperature


9/164

"relims6778

9 .onsider the follo&ingstatements:

; 5nnual range oftemperature is greater in"aci4c ocean than in

5tlantic ocean6 5nnual range of

temperature is greater in

northern hemisphere thatin southern hemisphere

"


10/164

"relims6778

hich of the statement iscorrect=

a ; only

b 6 only

c Both ; and 6

d %either ; or 6

5ns B"aci4c #cean ' bettermi+ing

"


11/164


12/164


13/164

!emperature of the ocean


14/164

• 5mount of salt found in ;777 gm of&ater

• %acl (8A, )g.l6 (;;, )g, .a

• %a and .l has high residual time inocean &ater ' very gradual removal '

thatDs &hy, they remain in thehighest proportion


15/164

• Irrespective of absolute salinity of the&ater, the proportion of the saltremain same in all parts of the

oceans

• 5mount of addition or e+traction offresh &ater compared to salt content

in the #cean &ater decides absolutesalinity of the #ceans


16/164


17/164

• "hysical removal ' &aves brea2 atthe beaches, salt0spray

• Biological removal ' marine life formse+tract calcium from sea &ater fortheir bones

Removal of


18/164

• 5ddition of fresh &ater EF Rainfall,ino& of large river, melting ofglacier EF less salinity

• Reduction of fresh &ater EF increasein temperature, high evaporation,&indy (&ind accelerate the

evaporation

@ariation in salinity


19/164

• > ppt ' salinity of 5tlantic #cean

• 1ead 7 salinity, La2e van(C77, La2e rmia

• )an seldom dro&ned in sea &ithhigh salinity

• Because, high salinity E high density


20/164

•


21/164

• %orthern

hemisphere '&armer ' highevaporation 'saline

• But in southern"aci4c0 roaringC7, furious >7and shrin2ing G7screaming 87 'very fast &inds

• $igh evaporation

EF high salinity

"attern in variation of salinity


22/164

• ;st 0 #cean

currents

• &arm oceancurrent li2e,

highevaporation

• .old currentled to p0

&elling: cooler&ater fromdepth come atthe surface EF

lo& salinity

Local @ariations in


23/164


24/164

• ?th ' ino& of

large rivers• Hanga '

Brahmaputra o&

into Bay of Bengal• Bay of Bengal less

saline than5rabian sea

Local @ariations in


25/164

Mississippi in G.ofMexico

Amu darya, Syr

darya to Aral sea

Rivers ino& to the seas


26/164

Black seaPersian gulf

Rivers ino& to the seas


27/164

• Cth ' glaciers

• Baltic sea receivefresh &ater from

melting of glaciers' lo& salinity

Local @ariations in


28/164

•


29/164

• quator ' salinity increases &ithdepth upto some layer 'thandecreases &ith depth

• Beyond equator ' salinity decreases&ith depth

• @ertical salinity variation of oceans is

complicated

• %o uniform layering

@ertical pattern of salinity


30/164

!emperature of ocean&ater

variations


31/164


32/164

• arly atmospherehas $ and $e in

abundance0lighter gasesescaped

• 1uring early life ofthe earth 'e+tensivevolcanism0

degassing %,


33/164

• ater vapour

condensed 'clouds ' rainfall'&ashed outbul2 of the .#6

into #ceans .o6E 77?

• #+ygen ' fromanaerobicrespiration ofbacteria li2e,.ynobacteria

#rigin of the 5tmosphere on arth


34/164


35/164

• %, #, $ and 5rgon are permanentgases

• ater vapour, .o6, o3one 0F variablegases, H$H

• %, 5rgon ' inert gases

• 5tmospheric gases0 no chemicalinteraction among them

• !hey donDt lose their properties

• !hey act as a single uni4ed gas

"roportion of gases


36/164


37/164

• 7 of

atmosphere&ithin ?6 2m

• !ropopause E

$eight A 2m atpoles, ;A 2m atequator

• 5t equator

cumulonimbusclouds

!roposphere


38/164

• !emperature

decrease as heightincreases

• !ransparent toinsolation

(short&ave

• $eated byterrestrial radiation

(long&ave• H$Hs absorbs long

&ave terrestrialradiation

Hreenhouse e-ect in troposphere

9uestio


39/164

"relims

67;6

9 normally, the temperaturedecreases &ith increase in

height from the earthDssurface, because,

; 5tmosphere can be

heated up&ard only fromearthDs surface

6 !here is more moisture in

upper atmosphere? !he air is less dense in

upper atmosphere

"


40/164

"relims

67;6

a ; only

b 6 and ?

c ; and ?

d ;,6 and ?

5ns .

Less dense E lessamount of H$Hs E lo&temp

"


41/164

• !emperatureincreases &ithheight

•Because ofthe presenceof o3one layer

• #3one

absorbs @rays fromisolation

stratosphere

9uestio


42/164

"relims

67;;

9 !he Jet aircrafts y veryeasily and smoothly in lo&er

stratosphere hy=; !here are no clouds or

&ater vapour in lo&er

stratosphere6 !here are no vertical

&inds in lo&er

stratosphere

5ns ; in &rong, 6 is correct

"


43/164

•5bsence of H$Hs

• !emperaturedecreases &ithheight

)esosphere


44/164

)esospheric

clouds• .louds visible

at highlatitudes

• 1uring summerseason

• .ondensation

of mi+ture ofmeteoric dustand somemoisture

%octilucent clouds


45/164

• !emperatureincrease &ithheight

•

Hases in ionic state' trap insolation 'e+tremely hot

• But ions are highly

dispersed• p to A77 2m from

earth

!hermosphere


46/164

• Krom A72m toGC7 2m

•

%umber ofionic layers

• seful inradio0

communication

Ionosphere


47/164

• $igh energy

sunrays andcosmic raysbrea2 the atomsof air molecules '

become ionised(*ve charged

• Behave as free

particles• 5t night time,

only cosmic raysioni3ation 0&ea2

Ionosphere


48/164

lay

ers

#eig#

t

$re%u

ency

Prese

nce

format

ion1 G70

72mLK 1ay0

time70?A72m

)K,$K

1aynight

H FC772 )K, 1ay

Layers of Ionosphere

9uestio


49/164

"relims

67;;

9 5 layer in arthDsatmosphere called

ionosphere facilitates radiocommunication hy=

; "resence of o3one cause

reection of radio &avesto earth

6 Radio &aves has long

&avelength

Both statements are &rong

"


50/164

• Beyond GC7 2m

• $ighly rari4edatmosphere

• @ery high

temperature0but di-erentfrom airtemperature0

because noe+istence of air0temp canDt befelt

+osphere


51/164

• Hlo&ing lightsat mid0nightsat high

latitudes• 5t height of

e+osphere andmagnetospher

e

5urora


52/164

• sun emit solar&ind/storm fromits corona

•


53/164

• .ollision of charged

particles(isoni3ation inmagnetosphere

• Ionised particles

emit light 'releaseenergy

• charged particlesinteract &ith

geomagnetic 4eldlines

• !hus, visible onhigh latitudes

5uroras


54/164

• !he averagetemperature of theearth ;> degree

• arth maintains inu+and out0u+ of theenergy, but out0u+ isnot immediate, it haslong time gap !hat is

&hy, the temperatureis maintained

$eat budget


55/164

• Kirst ?>

absorbed by#3one layer

• !hen ;>by cloud

cover• #nly >7

energyreached tothe earthsurface

$eat budget 0 Incoming


56/164

• 67 is lost in

latent heat ofevaporation;7 lost insensible heat

(temperature ofthe body

• ;> absorbed

by H$Hs• Remaining >

&as released inthe space

$eat budget 0 outgoing


57/164

• Ratio bet&een thetotal solar radiationfalling upon asurface and theamount reected

• Represents as

• arthDs avg 5lbedo

E ?>• Lo&est0 dar2 soil

• highest 0 sno&fall

5lbedo


58/164

surface AledoKresh

sno&

A707

1esert ?>0C>

Hrasses 6G.rops ;>

Bri 2 0 ; 06

5lbedo 0 table

9 hi h f th f ll i 9uestio


59/164

"relims

67;7

9 hich one of the follo&ingreect bac2 more sunlight as

compared to other three=a sandy desert

b "addy crops

c Land covered &ith freshsno&

d "rairie land

5ns .

"


60/164

!ori"ontal

•

&hen there is pressuregradient

• from high pressure tolo& pressure EFadvection

•

&hen air get &arm,gets e+pands,becomes lighter EFmove up&ards EFconvection

&ertical

)ovement of air


61/164

• hen air gets

hotter thansurrounding air, itrises up&ard

• If it has moisture 0latent heat ofcondensation 'more heated ' &ill

go up 0 formclouds 0can bringrainfall Einstability

@ertical movement of air 0 instability


62/164

• hen air is coolerthan surrounding 'it cannot move

up&ard• sin2ing air

• atmosphericstability or anti0

cyclonic condition• $igh pressure on

ground

@ertical movement of air 0 stability


63/164

Lo& pressure ' $igh pressure


64/164

• !he rate at &hich airpac2et cools &hilerising

• 5vg adiabatic lapserate is GC degree/2m

• !hat is air pac2etgets cool by GCdegree aftercovering one 2mup&ard

5diabatic lapse rate


65/164

• if air pac2et has highmoisture content0 notget cool so fast

• Its adiabatic lapserate MGC degree/2mN C degree/2m EF5LR

• et air can reachhigher distances &ithlo& lapse rate EFcreate instability

et adiabatic lapse rate


66/164

• If air pac2et is dry,

it does not havemuch moisture, it&ill get cool veryfast )ore thanGC degree/2m 'li2e, ;7degree/2m

•1ry air createstable condition

1ry 5diabatic Lapse rate

.onditions of stability and


67/164

situation condition

.onditionalstability

&hen &et5LRM normal

5LR M dry 5LR5bsolute

stability

&hen normal

5LRM &et 5LRM 1ry 5LR

.onditions of stability andInstability

increasing


68/164

increasingheight

temperature of airdecreasing,but reverseis

happenedthan it iscalled

tem eratur

!emperature Inversion


69/164

• ;st

• 5t !ropopause' temperaturestartsincreasingfrom here

•


70/164

• 6nd

• 5 cool &internight, the airabove the coldsurface gets cool

• But the air layerabove that coollayer is till

&armer !hen, bygoing up&ard, airdoes not getcooler but &armer

+ #f temperature Inversion


71/164

• ?th

• @alley inversion• &inter ' cool air

descends tovalley

• plift the &armair of valley

• 1escending

cool air0damage crops0frost

+ #f temperature Inversion

Implications of temperature


72/164

$ormation

of fog

'arm air cooled

y cold airelo( )condensation )

tiny (aterdroplets* lo(&isiility

Kormation offrost

ater moisturefro3en &ithcontact cold

surface0 dama e

Implications of temperatureinversion

9 hat do you9uestio


73/164

mains67;?

9 hat do youunderstand by

phenomenon ofOtemperature inversionP

in meteorology= $o&does it a-ect &eatherand habitants of the

place= (>

"


74/164

Condensation of(ater droplet +esult

5t heights .louds

5t lo&er level Kog

on the cold

surface

1e&

drop !urn into ice

crystal in e+treme

Krost

.ondensation of &ater droplets

f f i f f


75/164

Ad&ection

Mo&ing of (armair o&er cold

Radiat

ion

inter nights '

loss of heat dueto terrestial

radiation ' coldsurface )oving of

&arm air over

Reason for formation of fog

1 i l l f i ibili


76/164

1ecreasing level of visibility


77/164

fog

•

ater dropletcondensed around adust particle

• It reduces thevisibility, damage thecrops

• ater droplet

condensed around aparticle of pollutant,li2e


78/164

9 "hotochemical smog is 9uestio


79/164

"relims

67;?

9 "hotochemical smog isresultant of reaction among

a %#6, #? and pero+yacetylnitrate in the presence ofsunlight

b .#6, #6 and pero+yacetyl

nitrate in the presence ofsunlight

c .#,.#6 and %#6 at lo&

temperatured $igh concentration of %#6,

#? and .# in the evening

"


80/164

"relims

67;?

"hotochemical smog:

%#6, #3one * sunlight

5ns 5

"


81/164


82/164

evaporationprecipitation

ti


83/164

; $igh temperature

6 L" conditions

? Kast moving &ind• ater vapour

evaporate from the&ater body

• vaporation addsmoisture in the air

vaporation

$ idit


84/164

Asolute !umidity

• eight of &atervapour in unit volumeof moist air

• eight of &atervapour per unit &eightof dry air

Specic !umidity

$umidity

" i it ti


85/164

• "recipitation ' &henair is saturated &ith&ater vapour and anye+tra addition result

in precipitationRelative $umidity:

• 5mount of &atervapour present in air

' to amount of &atervapour required forsaturation

• "recipitationdepends upontemperature andmoisture content ofthe air

• $ot air ' saturationreach &ith more

moisture contentthan cold air

"recipitation

! f l d


86/164

!ypes of clouds

! f i f ll


87/164

Con&ectional rainfall

Orograp#ic rainfall

!ypes of rainfall

! f i f ll


88/164

Cyclonic rainfall

$rontal rainfall

!ypes of rainfall

" t f th ld


89/164

• ntire earth is divided into C large pressurebelts

• In reality, belts are not continuous butpoc2ets of lo& and high pressure

• But pressure can be created throughthermal or dynamic reasons

• !hermal: high temperatureEF L", lo&

temperature EF $"• 1ynamic: air rises EF L", air descends EF

$"

"ressure system of the &orld

" t f th ld


90/164

• C belts:

• equatorial lo&pressure belt

• sub0tropical

high pressurebelt

• sub0polar lo&pressure belt

• "olar $ighpressure area

"ressure system of the &orld

quatorial L" belt


91/164

quatorial L" belt

• .onstant insolation• 5ir gets &arm 0L"

• 5ir move up&ard

0F cloud formation0F instability 0Frain in the eveningdaily

• .umulonimbusclouds

• .onvectional

rainfall

quatorial L" belt


92/164

quatorial L" belt

• 5bsence ofadvection of air

• Belt of calm /

1oldrum• Because light,

feeble &inds 0calm region


93/164

• !he air above

equator moveto&ards pole, butcoriolis force 0 theirpath get deected

• !he length of pathincreases !heirenergy reduced inmid0path 0cooled

air subside near ?70C7 deg latitude


94/164


95/164

• Krom the pole, cold

&inds moveto&ards equator

• !he both &armand cold &inds

collide, the &armer&inds from


96/164

• 5ir risen at


97/164

ind system of the &orld

"lanetary &inds


98/164

• &inds blo&ing at

the same directionthroughout the year

• cover largedistances

• $ori3ontalmovement,"ressure beltsystem provide

them the pressuregradient

• .orilis force modifytheir direction

"lanetary &inds

!h i d!rade &inds


99/164

• !he &inds moveto&ards equatorial

lo& pressure EI!.

• I!. ' intertropicalconvergence3one, &here &indconverges

•

!heir direction iseast to &est dueto coriolis force

!rade &inds

!ropical deserts and trade &inds


100/164

• !ropical

easterlies o&s'east to &est

• ind becomesdry &hen they

reaches the&estern coast ofthe continents

• #- 'shore trade

&inds• !rade &ind

deserts

!ropical deserts and trade &inds

!ropical desert and cold currents


101/164

•

6nd• .old currents

providedesiccating

e-ect to trade&ind deserts

• .old current

o& on&esternmargins ofcontinents

!ropical desert and cold currents

9 )aJor hot deserts in9uestio


102/164

)ains67;?

9 Jnorthern hemisphere

are located bet&een670?7 degree %orthlatitudes and on the&estern side of thecontinents hy= (;7

"


103/164

• Krom &est to east

• Krom


104/164

• Krom &est to east

•

Krom


105/164

"relims

67;;

hemisphere are stronger andpersistent than northern

hemisphere hy=

;


106/164

• Krom east to&est

• Krom poles to


107/164

Summer

'inter

5pparent movement of the sun

movement of the pressure system


108/164

Summer

'inter

movement of the pressure system



109/164



110/164

• )onsoon &inds:

seasonal reversalof &inds

• Keature oftropical latitude

• In &inter ' trade&ind blo&s northto south, insummer ' trade

&ind blo&s southto north Sbut inlimited areaT


111/164

• 1ue to apparentnorth&ardmovement of thesun in summer

!hus, the I!. (L"also moves up&ard

• !hus, the area &hich&as under northerntrade &inds in&inter, &ill come

under southern trade&inds in the summer

)onson &inds



112/164


Local &inds : mountains &inds


113/164

Cold (ind

country

(ind

Hreece

Hragale

Italy !remonta

Mountains

'ind

5lps Kohn

Roc2ies

.hinoo2

5ndes on

'arm (inds

Local &inds : mountains &inds

Local &inds : land


114/164

Cold (ind- land

• $" condition in &inter

• 1ivergence of cold air

•


115/164

summer

• $ot0dusty &ind E QlooD

states 'ind

Bihar,

B,5ssam

Ualbais

ha2hi

U% Blosso

msho&er

UR )ango

Pre*monsoont#understorm

Local &inds: India


116/164

)ountain bree3e


117/164

• 1uring night

time: top getscooler thanvalley E $",valley EL"

• ind move hill0top to valley EFmountain bree3e

• 5griculture '

frost bite, chill inhabitation in thevalley

)ountain bree3e

• 1uring day@alley bree3e


118/164

• 1uring daytime: top

gets &armerthan valleyE L", valleyE $"

•


119/164

Land bree3es


120/164

Land bree3es

•

1i-erentialcooling of landand &ater

• 1uring night:

• land cooler E$",

• &ater EL"

• ind move land

to &ater EF landbree3e


121/164


122/164

&orld

"lanetary &ind system@ariable &inds


123/164

• 5roundtropopause, there

is only onegradient

• ind accumulatedabove equatorand rari4edatmosphere abovepoles

•

$" at the equatorand L" at thepoles

pper tropospheric &inds

Heo0strophic &inds


124/164

• strong coriolis

force attropopause

• Because friction isless 0 high speed 0

stronger thecoriolis force

•


125/164

esterlies &inds• !he upper

tropospheric &inds /geo0strophic

&inds blo&from &estto east at

the veryhigh speed

Rossby &aves


126/164

• esterlies at

poles ' tomaintain theangularmomentum0 they

meander EFRossby &aves

• Rossby &aves donot meander

consistently, butfollo& a cycle EInde+ cycle

ossby a es

Vet streams


127/164

•

In &esterlies,there are strong,narro& bands ofhigh speed &ind

EF Vet stream•


128/164

• !here are

situated at themargins ofmeridional cells

•

C permanent Vet streams: 6"olar Vet and 6V

/ t Vet streams


129/164

Permanent et stream

/emporary etstream

V

• Vet stream Vet streams


130/164

• Vet streamembedded in

&esterlies(Rossby &avesat highlatitude, causepressurevariability

• !hatDs &hy

they are calledtravellingdepression

V

Vet


131/164

V g p

eather of )id and high latitude


132/164

• eather of higher latitude is more comple+than &eather of equatorial or tropical regions

• Because tropical and equatorial region areheat surplus region' thermal reasons play

the dominant role• But higher latitude are heat de4cit region '

dynamic reasons play dominant role

•

!hese include ' localised * upper0tropospheric circulations (Rossby &aves, Vetstreams, temperate cyclones

g

5ir mass


133/164

• Large e+tensive bodyof air0mass

(;777sq2m

• $eight upto !ropopause

• 5t particular height,

one air mass &ill haveuniform temperatureand moisture across its&idth

•

5irmasses can bedi-erentiate accordingto their temperatureand moisture content

5i i d5ir mass


134/164

• 5ir mass acquiredproperties fromthe source regions' land, marine,polar, arctic,

5ntarctic E givethem identity +m", c!

• +tensive

homogeneoussurface * longerstay ($"

5ir masses


135/164

• 5ir masses do notstay at theirsource regionsforever, they

move out hilemoving they cameacross other airmasses

Kront


136/164

• !he relativedi-erence bet&eentemperature andmoisture decide

their interaction&ith one another

• !he border/

meeting region ofthe t&o air0massEF Kront

If cold air mass.old front


137/164

• If cold air massmove faster thanthe other than it &illlift the &armer oneup&ard EF coldfront

• the slope &ill besteep E there &illbe sudden up0liftment of the &armair E cumulonimbusclouds Efrontalrainfall

If iarm front


138/164

• If &armer airmass is moreactive than coldfront EF &armfront

•

slope &ill begentler E there&onDt be suddenup0liftment of

&arm air Euniformprolonged rain 'dri33le

Kronts


139/164

Krontal cyclone


140/164

• 5lso called ase+tra0tropicalcyclone,travelling

depressions,cold0corecyclone,&ave

cyclones

)eaning of cyclone


141/164

; Intense L" system

6 5ir converges to&ards thecentre

? .losed isobarsC In %orthern hemisphere

convergence ' anti0cloc2&ise

Isobar


142/164

Normal isoar

Closed isoar

.onditions for L"


143/164

/#ermally induced

•

Because of hightemperature

• + L" at equator

• .onvectional rainfall

at equator

•

pliftment of &arm air• + L" at sub0polar L"

belt

• Krontal rainfall

0ynamically induced

) t f1evelopment of Krontal cyclone


144/164

• )ovement of

airmasses fromtheir source region

• !he &arm andcold air mass face

each other• 5 front is created

bet&een them

•

.alled


145/164

1ocation of air

masses

Circular mo&ement

• .old air mass1evelopment of Krontal cyclone


146/164

• .old air mass

pushed the &armair mass

• Korced upliftmentof &arm air mass

at the cold frontEL"

• !&o cold air massconvergence 'circular due tocoriolis force

)ature stage


147/164

2nteraction of air

masses

1P ) closed isoars

• #ne cold air mass#ccluded front


148/164

• #ne cold air massclimb over othercold air mass'&armfront is destroyed

• .alled occluded

front• Rapid change in

temperature andpressure

• nstable &eatherconditions

• Krontolysis '1issipation of frontal cyclone


149/164

no great

temperaturedi-erencebet&een t&ocold air

masses 'frontdissipated 'L" reduced 'cyclonedissipated


150/164

#ccludedfront

$rontolysis


151/164

"ath of the temperate cyclone


152/164

• 5l&ays &est toeast direction

• Because inuence

of the &etserlies• Hradual

movement0"redictable

&eather

1istribution of temperate cyclones


153/164

$urricane '% !ropical cyclone


154/164

$urricane '%5merica

!yphoon 0 .hina

• Late summer

• Increased sea

surfacetemperature E L"

• .onvergence of airaround L" 3one

• Rising moist (&etair EF absoluteinstability

!ropical cyclone


155/164

•.loud formationEmore and moremoisture ' latentheat of evaporation

EF cumulo nimbuscloud EF cyclone

• .oriolis force

induce spiralmovement of air

• Intensi4cation of

)ature !ropical cyclone


156/164

• Intensi4cation of

L"• .onverging air

near &atersurface

• .irculating airrises above(coriolis force

•

1iverging air atthe top ofcyclone

h f h

ye of the tropical cyclone


157/164

• 5t the centre of the

cyclone ' QeyeD of thetropical cyclone

• It is a pressuredefect Because, atQeyeD a narro&

stream of &inddescend E is $" atQeyeD

• 5t the eye, there is

clear s2y• Beyond eye &all '

e+treme lo& pressure

"roperties of tropical cyclones


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•

)ove s&iftly• It is fuelled by

moisture ' so&hen cyclone is

cut0o- from seaand moveto&ards land ' itstarts

&ea2ening

1istribution of tropical cyclone


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comparison


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/emperate cyclone

• ?70C7 degree latitude

• 1ynamically induced

•

1ue to frontalinteraction

• Kormed over largearea

•

)ove &est to east• Hradual movement '

predictable

• A067 degree latitude

• !hermally induced

• 1ue to increasing •


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/emperate cyclone

• ind speed C70>72mph

• "ressure gradient A7mb

• "o&erful on land

• 5-ect mainland

• )ore time to dissipate

• ind speed F;672mph

•

"ressure gradientMAA7 mb

• ea2ens on land

• 5-ect only coastalareas

• 9uic2ly dissipate aftercoming on land

/ropical cyclone

9 !ropical cyclones arelargely con4ned to

9uestion


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)ains

67;C

largely con4ned to


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&ater

6 arm oceancurrents

? Increase C !ropicalcyclonemove east to&est

> Landmass on&esterncoast


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geographi l5 2