downslope wind storms - department of atmospheric and...
TRANSCRIPT
![Page 1: Downslope Wind Storms - Department of Atmospheric and ...aos453/lectures/lecture_06_downslope_wind.pdf · • Downslopewind storms are related to mountain waves • Mountain waves](https://reader034.vdocuments.net/reader034/viewer/2022042921/5f696dc68c90ef0dec3ba1b1/html5/thumbnails/1.jpg)
Downslope W
ind Storm
s
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Equation of M
otion for frictionless flow:
∂V ∂t
=l−∇k−α∇p+g
If w
e assu
me a horizo
ntally homogen
eous, hydrostatic referen
ce state w
here su
bsrript "o
":
α
o∂p
o/∂z=−g
and so, su
btrac
ting:
∂V ∂t=l−∇k−αo∇p+α'/αog
where primes are dev
iations from base state. Integrate equations of motion for frictionless flow
along the trajec
tory of the flow (⋅ds):
∂V ∂t
s∫⋅ds=l
s∫⋅ds−
∇k⋅ds
s∫−
αo∇p'⋅ds
s∫−
α'/αo
()g⋅ds
s∫Allow only for flow in x/z plane, assu
me Lam
b vec
tor is small l:0
(),
and flow is stea
dy state ∂V ∂t
=0
, an
d then
we get B
ernouli's equation
1
/2V
2
+α'/αo
()gz+
αodsp
s∫
How does
acc
eleration over the
wing affec
t pressure field?
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Flow M
ountain R
idge
•In
finitely long m
ountain, no flow aro
und ridge
•Consider first an airplane wing:
α'/αog=αo∂p
'/∂s
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Small Ridge
•Sim
ilar to airplane wing:
α'/αog=αo∂p
'/∂s
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Mes
o-B
eta Sca
le R
idge
•Res
onan
t gravity res
ponse
is involved
, low pressure shifts
increa
singly down strea
m as the sc
ale of the ridge
bec
omes
larger:
α'/αog:αo∂p
'/∂s
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Witch
of Agnes
i Ridge
•Lets co
nsider a “W
itch
of Agnes
i”, bell sh
aped
mountain
(norm
ally use
d for an
alytica
l mountain w
ave studies)
hav
ing the fo
rmula:
–a is the half-width, h is the max
imum height, and d is
the distance
fro
m the ridge top, an
d z_s is the
topography height.
2
22
s
az
ha
d=
+
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More about W
itch
of Agnes
i
•Eas
y for an
alytica
l so
lutions
•NOT a sine wav
e, is a bell sh
aped
ridge that
contains a sp
ectrum of wav
e co
mponen
ts
represe
nting m
any w
avelen
gths
•Some parts of the ridge may
be at super
Rossby rad
ius sc
ale an
d some may
be at
sub-R
ossby rad
ius sc
ale fo
r instan
ce
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Fro
udeNumber
•Im
portan
t influen
ces on atm
osp
here
resp
onse
to flow over an object:
–(a) Len
gth sca
le of the object
–(N
) Bru
nt-Vas
allaifreq
uen
cy, the vertica
l stab
ility pro
viding a res
toring force fo
r gravity
wav
es:
–(U
) velocity of flow norm
al to the ridge
1 2g
Nzθ
θ∂
=
∂
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Fro
udeNumber
•Define Fro
udeNumber:
inertial frequen
cy/
Bru
nt-Vas
allai Frequen
cyr
Ua
FN
==
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Inertial C
utoff, ie
Rossby
Number
•The co
riolis param
eter is an
other importan
t
param
eter. If the mountain is big enough,
we get lee
cyclogen
esis, not gravity w
aves
!
So w
e must consider the Rossby N
umber,
ie:
o
RaR
L=
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Flow O
ver a R
idge
•W
e co
nsider flow over shallow (h << dep
th of
troposp
here) ridges
of se
veral half-widths an
d look at the
resu
lts of a linea
r an
alytica
l so
lution for the W
itch
of
Agnes
imountain.
•The so
lution to the linea
r pro
blem yields a wav
e eq
uation
of the fo
rm:
w-vertica
l velocity
z-height ab
ove su
rfac
e
k –
vertica
l wav
e number
l –Sco
rer Param
eter(
)2
20
ttzz
wl
kw
+−
=
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Vertica
l W
ave Number
•L_x is the horizo
ntal wav
elen
gth of the
gravity w
ave. This param
eter in the vertica
l
wav
e eq
uation is purely nonhydrostatic!
2
x
kLπ
=
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Sco
rer Param
eter
•This param
eter is related to the
tran
smissivityof the atmosp
here to gravity
wav
es considering only hydro
static
pro
cesses
22
2
22
1N
dU
lU
Udz
=−
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When
Gravity W
aves
?
•Gravity w
ave so
lutions only exist when
•Therefore, there is a “sh
ort w
ave cu
toff”sc
ale, below
which gravity w
aves
can
not ex
ist:
–L_z is the vertica
l wav
elen
gth of the gravity w
ave
–L_x is the horizo
ntal wav
elen
gth of the gravity w
ave
22
0l
k−
>
22
22
zx
LL
ll
kππ
=>
−
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Narro
w R
idge:
Evan
esce
nt wav
es
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Med
ium R
idge:
Mountain (gravity)
wav
es
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Typical M
ountain W
ave (L
enticu
lar) C
loud
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Mountain W
ave –Len
ticu
larCloud
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Double W
ave (L
enticu
lar) C
loud
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Flying Sau
cer W
ave Cloud
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Len
ticu
larCloud
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Bro
ad R
idge:
Lee
Cyclogen
esis
for larg
er m
odes
,
GW
for sm
aller
modes
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Med
ium-N
arro
w ridge, but with
Sco
rer Param
eter (l) varying w
ith
height. This “trap
s”sh
orter w
aves
of the “W
itch
of Agnes
i”
mountain, but tran
smitts
vertica
lly
the longer ones
, lead
ing to lee
wav
es.
-This is mostly a
nonhydro
static
effect –
why?
-The sh
orter w
aves
hav
e
solutions in low lev
els
where l is large, but do not
above, so they
reflect off
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Lee
Wav
es
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Lee
Wav
es
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Mountain (Gravity) W
aves
•; i.e. static stab
ility dominates
over inertia
•or ; i.e. effec
t of stab
ility
dominates
over C
oriolis
•, i.e. sca
le is larg
er than
short-
wav
e cu
toff for gravity w
aves
xR
LL
<
2/
xL
lπ
>
1oR
>
1rF<<
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Vertica
lly Pro
pag
ating G
ravity
Wav
es
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Gravity w
ave ab
sorb
ed at critical lev
el w
here
phas
e sp
eed equals wind spee
d and air
statically stable above
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Effec
t of moisture on M
ountain
Wav
es
•Effec
t is to les
sen the Bru
nt Vas
allai
freq
uen
cy bec
ause
laten
t hea
t reduce
s lapse
rate:
2
2
2
1ln
1
vls
vls
lmoist
vls
p
pLr
Lr
rRT
Ng
Lr
zcTz
z
cRT
θε
+
∂
∂∂
=+
−
∂
∂∂
+
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•In
crea
ses dep
th of mountain w
ave
•In
crea
ses horizo
ntal wav
elen
gth
•M
ay cau
se some trap
ping of sh
orter
wav
elen
gths
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Theo
ry of DownslopeW
ind
Storm
s
•They
go by a number of nam
es:
–Chinook w
inds (R
ock
ies, Indian nam
e that
mea
ns “s
now eater”
–Foeh
nwind, nam
e use
d in E
uro
pe
–San
ta A
na wind, nam
e use
d in Southern
Californ
ia
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•Downslopewind storm
s are related to
mountain w
aves
•M
ountain w
aves
will loca
lly incrreas
ethe
winds on the lee side of the mountain, but
typically not to sev
ere levels
•But in downslopewind cas
es they
get very
stro
ng rea
ching sev
ere levels ro
utinely (>
55 kts)
•Lets look at a famous docu
men
ted
windstorm
hitting B
oulder C
olorado on 11
January, 1972
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Klemp and L
illy T
heo
ry
•Bas
ed on hydro
static sim
ulations
•Partial reflection of gro
up velocity off of
tropopau
secrea
ting res
onan
ce
•Nee
d tro
popau
seheight to be integer
number of half wav
elen
gths ab
ove su
rfac
e
•Res
onan
ce increa
ses am
plitude of mountain
wav
e…no w
ave break
ing in their
hydro
static theo
ry
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Clark
and Pelteir
(1977)
•Sam
e effect but upper w
ave break
s
•The break
ing upper w
ave des
tabilizes
upper
troposp
here an
d lower stratosp
here ducting
the underlying m
ountain w
ave more
•Strong amplifica
tion of lower tro
posp
here
wav
e
•Critica
l level at ¾
optimal
zL
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Influen
ce of M
id-L
evel Inversion
•Created
by a cold pool to the wes
t an
d to
the ea
st, su
ch as a Great B
asin H
igh to w
est
of Rock
ies an
d A
rctic High to eas
t
•In
version nea
r or just above ridge top
•In
version traps wav
e en
ergy below, lead
ing
to large am
plifica
tion down low and
form
ation of a hydraulic jump
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Hydraulic Ju
mp A
nalogy
•Curren
t thinking among m
ountain m
eteo
rologists
•Im
agine flow along a rock
y strea
m bed
:
–W
ater under air is an
alogous to the layer of co
ld stable
air at the su
rfac
e under les
s stab
le air above! Notice
the
water w
aves
are trapped
fro
m m
oving upward into the
air as
the wav
es in the stab
le lay
er of air are trap
ped
from m
oving upward into the less stable air.
–W
hen
water is much
dee
per than
rock
s, turb
ulence
, water flows ac
ross the ro
cks with little turb
ulence
. Y
ou
could tak
e a boring raft trip down such
a lam
inar
stream
.
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•Now imag
ine that the water lowers to be just
dee
per than
the ro
cks. Now you hav
e whitew
ater!
The water plunges
down the lee side of the ro
cks
and even
digs a little hole, dep
ressing the su
rfac
e
and blowing out ro
cks etc.
•The sa
me is tru
e fo
r the downslopewind. T
rapped
ben
eath the inversion, the wav
e am
plifies
and
break
s, clowingout Boulder!
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Wind Spee
dPotential T
emperature
Class C
ase Study: Feb
ruary 3, 1999 w
est of Boulder
1400 U
TC
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