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Atmospheric response
to oceanic temperature anomalies
associated to mesoscale eddies
Guillaume Lapeyre, Riwal Plougonven,Julien Lambaerts et Xavier Perrot
Laboratoire de Météorologie Dynamique, Paris
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Atmosphere-Ocean Interactions
Océan:
Atmosphère:
Different spatial scales: In the Ocean
Basin-scale Circulation (3000km) Western Boundary currents (500km) Méso and submesoscales (10-100km)
In the Troposphere Storm-track (5000km) Fronts (500km)
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Up to 2000s, GCMs studies of the ocean-atmosphere interactions showed that
tropical SST anomalies have a significant impact on extratropical climate
(through interconnexions and planetary waves) extratropical SST anomalies have little effect on
extratropical climate
(except for anomalies of high amplitude) Response localized in the boundary layer
Uncertainty for the existence of coupled modes of atmosphere-ocean at midlatitudes;
Weak predictability of the GCMs at medium range
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Recently, unveiling of strong relations between extratropical SST fronts and storm-tracks:
Minobe et al. (2008) : GCMs at very high resolution (resolution T239 ~ 53km)
Nakamura (2006) : Reanalysis JRA25 (resolution T106 ~120km)
What matters is not the SST anomaly but the SST gradient
To represent this effect, GCMs need to use grid space smaller than 50km
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Nakamura et al. (2008), reanalyses
Along the Antarctic Circumpular Current● Precipitations and zonal wind at surface anchored over the front● Meridional Heat Flux by atmospheric perturbations
( = storm-track) above large-scale SST front
< V' T' > in contours;Heat Flux at surface in
colorr
SST in contours; Precip in color
Zonal wind in contours; SST in color∇
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Minobe et al (2008), GCM
Annual precipitation localized above the Gulf Stream
Effect represented only if Gulf Stream front is resolved (i.e. for large magnitude of SST gradients)
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Past studies: Impact of oceanic large-scale fronts on storm-tracks
However, ocean is not only a region with large-scale currents!!!
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Relative vorticity at a particular day(numerical simulation of the ocean at 1/10 of degree)
Ocean = not only large-scale front but sea of eddies in interaction
Which role in the ocean-atmosphere interactions?
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Oceanic Mesoscales and atmospheric layer
Observations during Oceanographic POMME campaign (North-East Atlantic)
In colorr: wind stressIn contours: SST
(SST in contours)
Impact on turbulent fluxes, surface winds Chelton et al. 2004, Bourras et al. 2004
SST SST Surface Latent heat Flux
Surface Sensible heat Flux
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Effect of oceanic eddies in the atmospheric boundary layer
SST => pressure anomalies (Lindzen Nigam 1987)
wind proportional to
SST => static stability (Wallace et al. 1989)
wind proportional to
∇
∇ SST
SST
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Response à la Lindzen and Nigam
(pressure effect)Ekman-type solution
Response à la Wallace et al.(turbulent vertical mixing)
√U ' 2+V ' 2 ∝ ∣∇ SST∣
W ∝ −∇ 2SST
√U ' 2+V ' 2 ∝ SST '√U ' 2+V ' 2 ∝ SST '
W ∝ U⃗⋅∇ SST
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Analysis of atmospheric response
WRF Model in a domain (512km)2x12km Initially, vertical shear of the zonal wind Forced by fixed SST (destabilizing the
atmosphere)
Vent zonal Vent zonal
SST SST
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SST parallel to wind :
wind
Initial surface wind = 1m/s
Initial surface wind = 10m/s
U ∇ SST
U∇ SST
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wind
Initial surface wind = 1m/s
Initial surface wind = 10m/s
∇ SSTU
U SST
SST transverse to wind:
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Weak wind Strong wind
Response Lindzen & NigamPressure effect
Wallace et al
Vertical mixing
Vertical velocity - SST Laplacian SST gradient
Horizontal wind SST gradient SST anomalies
Involved scales Submesoscales10km
Mesoscales100km
● Depending on the wind amplitude and direction, two responses:
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Idealized simulations of a storm-track
Periodic Canal in aquaplanet mode (with fixed SST and forced à la Held et Suarez through a mean heating)
WRF Model (YSU parameterization for the boundary layer and Monin Obukov for the surface layer)
Domain 9000 x 9000km x 20km altitude DX=18km and 100 levels on the vertical
Allows to represent atmospheric boundary layer, development of storms and effect of oceanic eddies on the atmosphere
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Horizontal SST field
Two simulations in presence of a large-scale meridional SST gradient
CNTR = WITHOUT EDDY = WITHoceanic eddies eddies
x x
yy
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Color : water vapor content at the surface Contours : surface pressure
CNTREDDY
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Temporal-mean of horizontal divergence and U⋅∇ SST
Superposition of the two fields:
The mean divergence● has large anomalies ~ 0.5 f● responds to SST
EDDY-CNTRL
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Work in progress
What is the impact on jet-stream variability and more generally on the storm-track?
Seems to intensify the storm-track Role of water vapor which may promote
stronger ocean-atmosphere interaction through latent heating in the troposphere.
Retroaction of the ocean on these processes?
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Etude de l'effet des tourbillons océaniques sur la couche limite atmosphérique
Champ de SST
zBackground flow
x
Uniform vertical shear :
U = 10 m/s, H = 12 kmH
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What occurs when meso and submesoscale SST anomalies are present?
WRF model in a box (512km)2
x 12km Initial background vertical shear Forced by fixed SST (destabilizing atmosphere)
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Results (no surface winds)
- Laplacien de SST
Réponse à la Lindzen and Nigam∂ω
∂ p=−κ
R log(P0/Ph)
f 2+κ
2 ∇2SST
Vitesse verticaledans la couche limite à 15h