MET 333 – AULA 3 -...
Transcript of MET 333 – AULA 3 -...
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AULA 3
CAMADA LIMITE ATMOSFÉRICA
– PARTE CONVECTIVA
E ESTÁVEL
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Sunrise Noon Sunset Sunrise
Residual Layer Residual Layer
Stable (nocturnal) Layer
2000
1500
1000
500
0
Inversion
He
igh
t (m
ete
rs)
Adapted from Introduction to Boundary Layer Meteorology -R.B. Stull, 1988
Convective
Mixed Layer
Stable (nocturnal) Layer
Atmospheric Boundary Layer
Diurnal Variation
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ATMOSPHERIC TURBULENCE
•Turbulence due to two effects:
–Atmospheric heating, and resulting convection due to
density gradient
–Mechanical turbulence due to velocity gradient
•The flux Richardson number Rf is the ratio of these
two effects:
•The numerator can be negative, representing a loss
of kinetic energy by buoyancy
stressesshear by
energy kinetic of production
buoyancyby
energy kinetic of production
fR
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The Convective Boundary Layer (CBL)
• When turbulence in the atmospheric boundary layer is maintained
largely by buoyant production the boundary layer is said to be in a
convective state
• The source of buoyancy is the upward heat flux originating from the
ground heated by solar radiation.
• Convective turbulence is relatively vigorous and causes rapid
vertical mixing in the atmospheric boundary layer.
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Essential processes to be represented in the CBL
(2) Land/surface processes (surface fluxes)
(1) Turbulent mixing (turbulent fluxes)
(3) Entrainment (exchange fluxes)
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Estimating the height of the planetary boundary
layer
The stable value cannot be higher than the neutral
The unstable value cannot be less than the
neutral
Inversion layer limitation
Under unstable conditions, the determination of zp is not
critical: a temperature inversion which limits the extent of
vertical mixing is generally present at zi < zp
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Convective mixed layer (CML):
Growth
The turbulence (largely the
convectively driven
thermals) mixes (entrains)
down potentially warmer,
usually drier, less turbulent
air down into the mixed
layer
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(3) Entrainment
The third essential process is entrainment
Top-down diffusion of an scalar.
Laboratory experiment by Harm Jonker (TUD)
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07/03/2010
0
200
400
600
800
1000
298 299 300 301 302 303 304 305 306
T e m p Pot (K)
Alt
itu
de
(m
)
00:09
02:03
04:03
06:03
08:03
10:03
12:03
14:03
16:03
18:03
20:03
22:03
23:51
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Sunrise Noon Sunset Sunrise
Residual Layer Residual Layer
Stable (nocturnal) Layer
2000
1500
1000
500
0
Inversion
He
igh
t (m
ete
rs)
Adapted from Introduction to Boundary Layer Meteorology -R.B. Stull, 1988
Convective
Mixed Layer
Stable (nocturnal) Layer
Atmospheric Boundary Layer
Diurnal Variation
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