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Ta't! #a ,r$s(2' %!! $# v($'t! s!' a-'(t1$s $tra!r('ar(a$'t$ 8#1%t1a't$s $ 1'!s ('sta't$s a !tr!s7 %!! &$!s t$'(! !%as(2' $ %!,r!)ar $' el %a,+t1#! a't$r(!r P$r!7 a# (-1a# 01$ s1%$$ %!' #as r$sta't$s a-'(t1$s at!s8r(%as7 $'tr! $ $stas 8#1%t1a%(!'$s s$ ,1$$ $'%!'trar 1' %($rt! !r$'V7 1'a %($rta r$-1#ar(a7 1'a $t$r('aa ,a1ta 01$ $s #a 01$ %ara%t$r(;a $# %!,!rta($'t! &a)(t1a#V $ #as ,r$s(!'$s / #!s v($'t!s s!)r$ $# ,#a'$ta Est$ %!,!rta($'t! &a)(t1a#V $s el 01$ ,r$t$'$!s $s%r()(r $' #as #+'$as 01$ s(-1$'7. Para $##! va!s a r$%1tr(r a# $,#$! $ a,as 01$ %art!-ra8($' #a (str()1%(2' $ #as ,r$s(!'$s / #!s v($'t!s $(!sV s! )r$ # a s1,$r8(%($ t$tr$str$7 #! %1a# '! $9a $ s1s%(tar ,r!)#$as (,!rta't$s7. S( $' %1a#01($r a-'(t1 at!s8r(%a $# va#!r $(! %!'st(t1/$ 1'a a)stra%%(2' %ar$'t$7 $' #a a/!r+a $ #!s %as!s $ 1'a r$a#(a %!'%r$ta7 $' #as a-'(t1$s 01$ a&!ra '!s !%1,a' a $st$ ,r!)#$a s$ aWa$' !tr!s '1$v!s. P!r #! 01$ r$s,$%ta a# v($'t!7 #a ,r!,(a %!'s($ra%(2' $ v($'t!s $(!sV %ar$%$ $ s$'t(!7 %!' #! %1a# $' $st$ %as! ,!r v($'t!s $(!s &$!s $ $'t$'$r #!s v($' t!s =s 8r$%1$'t$s / &a)(t1a#$s $' 1'a ;!'a aa Ést!s7 a$=s7 s$ %!'%()$' ,ara 259
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4 Las perturbaciones que se desarrollan en el seno de una corriente general de vientos, tales como las perturbaciones frontales que recorren los vientos del oeste de las latitudes medias o los ciclones
tropicales que se generan dentro de la corriente de los alisios, constituyen,buenos eemplos de esta afirmaci!n
"#G$M %& ' (resiones y vientos medios al nivel del mar en los meses de enero y ulio Al nivel del mar las presiones y los vientos dibuan grosso nrodo grandes bandas latitudinales ) *ste comportamiento latitudinal es muc+o ms evidente en el +emisferio -ur, eminentemente ocenico, que en el +emisferio .orte, don/ de la alternancia entre mares y continentes impone rupturas y discontinuidades
en estas bandas Asirnis/ mo se producen diferentes situaciones entre el verano y el invierno, entre las cuales la ms destacada es el despla0amiento en latitud de las bandas de presi!n y viento "uente1 L!pe0 2enn3de0, 4ubio 4ecio y Cua/ drat, Gl'ognif!a Física, Madrid, Ctedra, '556, pg 78'
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"IG$M % 6 istribuci!n media de la presi!n en los niveles altos de la atm!sfera Altura geopotencial
Een msF de la superficie isobara de 988 +(a en enero y ulio& *n las capas altas de la atm!sfera la circulaci!n del aire es muc+o ms regular que en los niveles superficiales dado que a+ora no intervienen las influen/ cias perturbadoras de los mares y continentes Aqu el comportamiento latitudinal es evidente, con altas presiones en las latitudes tropicales, baas presioIHe- en las polares y fluos del oeste entre ambas, en las lati&& tudes medias "uente1 yeney, Elh11e11ts di "t"orologii, (ars, Masson, '5%<
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v($'t!s ali sios6 v($'t!s )asta't$ %!'sta't$s / r$-1#ar$s 01$ r$%!rr$' $stas #at(t1$s a 1'a v$#!%(a $(a $ 1'!s k3&. Est=' %!'st(t1(!s ,!r a(r$ (v$r-$'t$ $s$ #as a#tas ,r$s(!'$s s1)tr!,(%a#$s / s1 $str1%t1ra v$rt(%a# r$8#$9a %#ara$'t$ $st$ &$%&!. E# a#(s(! s$ %!,!'$7 $' $8$%t!7 $ !s %a,as v$rt(%a#$s %#ara$'t$ (8$r$'%(aas: 1'a %a,a ('8$r(!r7 1/ &1((8(%aa ,!r s1 tra/$%t! !%$='(%!7 / !tra s1,$r(!r7 =s %=#(a / s$%a7 01$ s$ s$,ara $ #a a't$r(!r a travs $ 1'a ('v$rs(2' tr(%a .. Esta (' v$rs(2' '! s$,ara !s asas $ a(r$ (8$r$'t$s7 s('! 01$ $s ('t$r'a a# ,r!,(! a#(s(! / tra1%$ #a s1)s($'%(a -$'$ra#(;aa $# a(r$ $' #a r$-(2' a'a't(a# $ $st!s v($'t!s: #!s a't(%(%#!'$s s1)tr!,(%a#$s. E# $%a'(s! -$'$ra!r $ #a ('v$rs(2' tr(%a a ,art(r $ #a s1)s($'%(a $s $# s( -1($'t$: %1a'! $# a(r$ $s%($'$ $' v$rt(%a# s$ va %a#$'ta'! a(a)=t(%a$'t$7 ,$r!7 a$=s7 s$ va %!,r(($'! $' #as %a,as )a9as7 %!' #! %1a# $# a(r$ s1,$r(!r $s%($' $ =s 01$ $# ('8$r(!r.. As+ ,1$s7 $# ,r!%$s! $ %a#$'ta($'t! $ #as %a,as s1,$((!r$s $s =s ('t$'s! 01$ $# $ #as ('8$r(!r$s /7 $' %!'s$%1$'%(a7 $# -ra($'t$ tr(%! v$rt( %a# s$ va &a%($'! %aa v$; $'!s a%1sa! / ,!r $'$ =s $sta)#$. C1a'! $# $s %$'s! $# a(r$ $s #! s18(%($'t$$'t$ (,!rta't$7 $sta ,r!-r$s(va $sta)(#(;a%(2' $# -ra ($'t$ ,1$$ ar #1-ar a #a a,ar(%(2' $ 1'a ('v$rs(2' tr(%a7 01$ s$ s(t1ar= ,r$%(sa $'t$ $' $# '(v$# $' $# 01$ s$ $t($'$ #a s1)s($'%(a7 '(v$# $' $# 01$ s$ va a-!#,a'! $# a(r$ ,r!%$$'t$ $ #as %a,as s1,$r(!r$s. 2-(%a$'t$7 #a ('v$rs(2' s$r= ta't! =s ar%aa / ta't! =s )a9a %1a't! =s (,!rta't$ s$a $# !v(($'t! s1)s($'t$ $# a(r$. P!r $# %!'tra((!7 s( $# !v(($'t! s1)s($'t$ $s )(# / #!s ,r!%$s!s %!'v$%t(v!s $sarr!##a!s $s$ #a s1,$r8(%($ s!' (,!rta't$s7 #a ('v$rs(2' s$ $#$var= $' a#t1ra / ,$r$r= ('t$'s(a Kvas$ 8(-1ra ?.HL.
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^ A) Flanco E del anticiclón con fuerte inversión térmica próxima a la superficie terrestre -ubsidencia acusada& 2F "lanco J del anticicl!n con inversi!n tDrmico dDbil y elevado -ubsidencio poco acusada
y fuerte convecci!n superficial
"rG$M K# isimetra entre el flanco este y el flanco oeste de los anticiclones subtropicales *n el flanco oriental de los anticiclones subtropicales la inversi!n tDrmica del alisio es muy intensa y cercana a
la super ficie terrestre *llo se eplica por la baa temperatura del aire superficial Econ procedencia norte y recorrien do corrientes marinas frasF y por el +ec+o de que el aire circula desde las 0onas continentales a las oceni cas *n el flanco occidental sucede lo contrario aqu el aire es ms clido por su procedencia tropical y su trayectoria sobre corrientes clidas y, adems, se dirige desde el ocDano +acia reas continentales, en las que los relieves montaNosos eercen un efecto de disparo sobre Dl, obligndolo a elevarse Como consecuencia de todo ello la estructura del alisio es diferente en uno y otro flanco
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"IG$M %&<& Pona de convergencia intertropical y doldnr111s en la confluencia de los alisios de los dos +emis/ ferias El cintur!n de las baas presiones ecuatoriales reviste dos formas fundamentales1 la 0ona de conver/ gencia intertropical EPCIIF, con enfrentamiento violento de los alisios de los dos +emisferios, que se sue le producir en la 0ona central de los dos anticiclones, y los doldn1111s, con ausencia de enfrentamiento y encalmamiento del aire Qstos se suelen registrar en el flanco oriental de los anticiclones
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F"#$%A &.'. 4epresentaci!n esquemtica del mon0!n de a India durante el verano& urante el verano los alisios del +emisferio -ur atraviesan el ecuador y se dirigen, ya como vientos del -J, +acia la potente de/ presi!n continental que se constituye entonces en el continente euroasitico& *llo supone un importante despla0amiento de la PCI I en estas latitudes& "uente1 urand/astDs, Geogr11.fí11 di los 11ires, 2arcelona, Ar($#7 4>B7 ,=- ?
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"IG$4A %&&;& 4epresentaci!n esquemtica det mon0!n africano durante el verano *n el continente africano tambiDn se constituye durante el verano una depresi!n tDrmica lo suficientemente importante como para generar un fen!meno de mon0!n, con atracci!n de los alisios del +emisferio -ur& *n este caso, sin embar go, el enfrentamiento entre masas de aire parece ser ms compleo que en el caso de la India "uente1 u= rand/astDs, Geogrefia de los airt's, 2arcelona, Ariel, '5:6, pg& %6 268 269
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Corte esquemtico de la atm!sfera de las latitudes medias1 posici!n del frente polar y del et $no de los +ec+os ms relevantes de la circulaci!n en las latitudes medias es la eistencia en ellas de frecuentes perturbaciones frontales, conocidas genDricamente como perturbaciones del frente polar, so bremontadas en altura por la corriente en c+orro polar o #et strea111 *n la gDnesis de ambos fen!menos, que estn estrec+amente relacionados, interviene el gran contraste tDrmico que se produce en estas latitudes en// tre el aire polar y el aire tropical "uente1 enderson=-ellers y 4obinson, $o11%t'111&orar di11ullolog', Londres, Longman -cientific and Tec+nical, '5:;, pg ':6 "'G$M ?.? stre11111 _
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A: Anticiclón de ,loueo
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"IG$4A %& 5 2ao indice de circulaci!n en el fluo del oeste en altura Cuando el ndice de circulaci!n en la corriente en c+orro es bao, Dste forma profundas ondulaciones Eondas de 4ossbyF que constituyen antici/ clones en sus crestas y marcadas depresiones en sus vaguadas
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2. !s MECANISMOS REGUADORES DE A CIRCUACIN GENERA ATMOSFÉRICA
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% '8& *squema de los cambios en las ondas de 4ossby desde altos ndices de circulaci!n a baos n dices, y viceversa& 2a circulaci!n del fluo 0onal de oeste en altura oscila entre ndices de circulaci!n altos y baos en un lapso de veinte a sesenta das, lo cual origina importantes cambios en el tiempo en las 0onas afectadas por esta oscilaci!n "uente1 enderson/-ellersy 4obinson, $o11tet11&orar c)inatolog, Londres, Longman -cientific and Tec+nical, #5:;, pg ':6 F"#$%A
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? H *l +ec+o se puede comprobar eperimentalmente +aciendo girar con la mano una bolita atada a un +ilo) Cuando la velocidad de giro de la bolita es pequeNa, el radio de giro es grande -i darnos ms impul/ so a la bolita y aumentamos su velocidad de giro, el +ilo se enrolla en el dedo para acortar el radio de giro
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'nomento de rotaci!n alrededor del ee de los polos Las coladas meridianas, tanto polares como ecuato/ riales, tienden a mantener constante su momento de rotaci!n alrededor del ee de los polos en su despla/ 0amiento& Como en estos despla0amientos cambia su radio de giro, se 'nodifica tambiDn su velocidad ¡¡. neal de giro J/*, aumentando en el caso de las coladas ecuatoriales y disminuyendo en el caso de las po lares *l resultado es que adquieren un movimiento relativo respecto al de la Tierra, que +ace que se conviertan en coladas del J en el caso de las coladas ecuatoriales y del * en el de las polares
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21 Confluencia en altura y descenso del aire
286 ';& 2ifurcaci!n de la corriente en c+orro La disfluencia de la corriente en c+orro EAF determina la bifurcaci!n de Dste en dos ramales ello genera un vaco de aire en altura que tiende a rellenarse con aire ascendente desde las capas baas& *n el punto 2, sin embargo, +ay una confluencia de la corriente en c+o rro que produce un agolpamiento de aire y su consecuente descenso F+#$%A C
+acia las capas baas de la atm!sfera& "uente1 Medina, t'%t'orología )sica sin*&tica, Madrid, (araninfo, '5%;, pg ''5
a #!s a't(%(%#!'$s Kv($'t!s s1,$r-$!str28(%!sL 01$ $' t!r'! a #as $,r$s(!'$s Kv($'t!s s1)-$!str28(%!sd. C!! %!'s$%1$'%(a $ $st!s &$%&!s s$ va a ,r!1%(r 1'a ar%aa (s($tr+a $' $# %!,!rta($'t! $# a(r$ $' #!s 8#a'%!s !r($'ta# / !%%($'ta# $ #as va -1aas Kvas$ 8(-1ra ?.4?L. E' $# 8#a'%! !r($'ta# $ #as va-1aas $# a(r$ %(r%1#a #$'ta$'t$ $' t!r'! a #a $ ,r$s(2'7 $' ta't! 01$ $# a't(%(%#2' s(t1a! $' #a %r$sta 01$ #a ,r$%$$ -$'$ra v($'t!s s1,$r-$!str28(%!s =s r=,(!s. a %!'s$%1$'%(a $s 01$ $# a(r$ $#a't$r! $s%a,a r=,( a$'t$ ($'tras 01$ $# 01$ %(r%1#a $tr=s va ra#$'t(;a! / '! ,1$$ a#%a';ar#!7 -$ '$r='!s$ as+ 1'a (v$r-$'%(a (,!rta't$ $' $st$ 8#a'%! !r($'ta# $ #a va-1aa. Esta (v$r-$'%(a atra$ a# a(r$ s(t1a! $' #as %a,as )a9as $ #a at2s8$ra7 $# %1a# %!($';a a as%$'$r $' $s,(ra# %(%#2'(%a7 $%ava'! ('$(ata$'t$ 1'a $,r$s(2' $' $# s1$#!. C1a'! $st$ 8$'2$'! s$ s1,$r,!'$ a 1'a ;!'a $ 81$rt$ %!'trast$ tr(%! s1,$r8( %(a# E/ $##! $s 8r$%1$'t$ a! 01$ $star'!s $' 1'as #at(t1$s 1/ ,r!%#(v$s a #a 8r!' t!-'$s(s #a $s,(ra# %(%#2'(%a ()19aa ,!r $# a(r$ $' s1 as%$'s! $t$r('a 1'a !' 1#a%(2' $# 8r$'t$ / #a a,ar(%(2' %!'s$%1$'t$ $ 1'a ,$rt1r)a%(2' a !s 8r$'t$s Kvas$ 8(-1ra ?4BL. D$ &$%&! $stas ,$rt1r)a%(!'$s s1$#$' 1)(%ars$ s($,r$ $' #a ,art$
"IG$4A V%&' %& "en!menos de convergencia y divergencia en la corriente en c+orro por cambios en la velo/ ciclad del viento& A igualdad de gradiente de presiones el viento fluye ms deprisa en tomo a los anticiclo nes que en tomo a las depresiones& *llo genera un fen!meno de divergencia Esale ms aire del que entraF en la 0ona oriental de las vaguadas y otro de convergencia Eentra ms aire del que saleF en su 0ona occiden/ tal& *l resultado final es que en la 0ona oriental de las vaguadas se generan depresiones con fuerte ascenso del aire, frente a la 0ona occidental, en la que predomina la subsidencia& "uente1 ufty, f11troducci*11 a la clitnatología, 2arcelona, Ariel0 '5:<
A01+ #! 01$ s$ -$'$ra $s 1' a-!#,a'Q$'t! $ a(r$7 1'a %!'v$r-$'%(a7 %!! %!'s$ %1$'%(a $ #a #$'ta %(r%1#a%(2' 01$ s$ r$-(stra $' t!r'! a #a $,r$s(2' / #a %(r%1#a%(2' =s r=,(a 01$ -$'$ra $# a't(%(%#2' $ #a %r$sta 01$ #$ s1%$$ Kvas$ 8(-1ra ?4?dP!r $##! $' $sta ;!'a s1$#$ ,r$!('ar #a s1)s($'%(a $# a(r$ a%!,aWaa $ $sta)(#(a at!s8r(%a / a#ta ,r$s(2' $' $# s1$#! .. E' %!'s$%1$'%(a7 s$ ,1$$ a81ar 01$7 s( )($' #as ,$rt1r)a%(!'$s s1,$r8(%(a#$s s!' 81'a$'ta#$s ,ara $,#(%ar #a a%$#$ra%(2' $ #a %!rr($'t$ $' %&!rr! s1,$r(!r7 sta a s1 v$; %!'tr()1/$ a -$'$rar $sas (sas ,$rt1r)a%(!'$s. D$ &$%&!7 #as ,$rt1r)a%(! '$s $# 8r$'t$
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F"#$%A & &': GDnesis de las perturbaciones frontales en el flanco este de las vaguadas de la corriente en
c+o/ rro& Cuando una divergencia en la corriente en c+orro se superpone a una 0ona frontal, la espiral cicl!ni/ ca dibuada por el aire superficial en su ascenso determina la ondulaci!n del frente, surgiendo as una per/ turbaci!n a dos frentes& "uente1 A+rens, euorolog tod n 1i1troductio11 to /eat)er, c!i1nate and the en0iran 111e11t, Minnesota, Jest (ublis+ing Co&, '5:6, pg &795
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a) 1urvatura de la corriente al atravesar perpendicularmente una cadena de montaGas ,4 1ompresión vertical de lo columna de aire en lo cum,re de la cadena y expansión ver tical en la ladero de sotavento c) Expansión 5oriontal de la columna de aire en lo cum,re de la cadena montaGoso
F"#$%A &.+H0 *fecto +idrodinmico del relieve sobre una corriente de aire& La compresi!n vertical que su/ fre la columna de aire en la cumbre de la cadena montaNosa +ace que aumente su radio de giro y, en con/ secuencia, disminuye su velocidad de giro cicl!nico, lo que propicia la aparici!n de un torbellino relativo anticicl!nico @0 en suma, de una cresta anticicl!nica& *n sotavento la columna de aire aumenta su altura y disminuye su radio de giro& *sto le +ace aumentar su velocidad, adquiriendo torbellino relativo cicl!nico y curvatura tambiDn cicl!nica "uente1 (DdDlaborde, BLes donnDes de la climatologieX, en Etuclo&idie de la 2l"iade. Giogra&hie. G"n"rale, (ars, Gallimard, '5;;, pg) :8
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"IG$4A %&68& "rontogDnesis en las costas orientales de los continentes del +emisferio .orte en las latitudes medias las costas orientales de los continentes en las latitudes medias del +emisferio norte son 0onas tD picamente frontogenDticas porque en ellas se enfrentan la masa de aire polar procedente de los anticiclo nes continentales y la masa de aire tropical procedente de las altas presiones subtropicales ) "uente1 -tra+= ler, Geogrefía Física, 2arcelona, Omega, '5%<, pg '%<
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