Why do we have storms in atmosphere?. Mid-atmosphere (500 hPa) DJF temperature map What are the...
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Transcript of Why do we have storms in atmosphere?. Mid-atmosphere (500 hPa) DJF temperature map What are the...
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Why do we have storms in atmosphere?
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Mid-atmosphere (500 hPa) DJF temperature map
What are the features of the mean state on which storms grow?
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Zonal thermal winds, and zonal mean cross sections
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The DJF Atlantic Jet
10 m/s
10 m/s20 m/s
20 m/s30 m/s
30 m/s
0 m/s
0 m/s
40 m/s
Sector zonal mean cross section
Thermal wind map (250 hPa – 850 hPa)
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Are atmospheric jets stable?Will perturbations to the jet immediately decay? Does the jet support instabilities?
Analogy: Ball on top of a hill
Answer #1: Perturbations to the jet seem to grow in magnitude;The jet is unstable.
Answer #2: The jets are the time mean of the atmospheric flow;Something most kill the instability and return the flow to the time
mean.
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Velocity Shear
The velocity shear between the two layers leads to an instability
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Consider two different mean stateswith different velocity shears
5 m/s
- 5 m/s - 10 m/s
10 m/s
The systems have the same linear momentumBut the system with more shear has more kinetic energy
x
y
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Can the perturbations extract energy from the flow?
• Key concept: If the perturbations can decrease the velocity shear in the flow, the flow will have less energy
• This energy will go to the perturbations
• Therefore, in order for the perturbations to grow in shear flow, they must transport momentum against the shear of the flow
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Lets put this in mathematical terms
dUdy > 0
x
y
MEAN STATE Which perturbation stream functionwill grow?
A
B
C
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Which way do perturbations transport momentum
When v’ is positive, u’ is zeroWhen u’ is negative, u’ is zero
u’v’ = 0
When v’ is positive, u’ is negativeWhen v’ is negative, u’ is positive
u’v’ < 0
u’v’ > 0
When v’ is positive, u’ is positiveWhen v’ is negative, u’ is negative
No momentum transport
Negative momentum transportIn the y direction
Positive momentum transportIn the y direction
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Barotropic Conversion
Mean State Shear
Perturbation Stream Function
Energy flow from mean state to the perturbation if :
u’v’ dUdy
< 0
And the initial perturbationwill grow
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• Simple analogy: If we perturb a ball, lying on top
topography from its resting position, will it continue to move away or will it return to the original position
Stable Neutrally stable
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Ideal Flow and most unstable mode
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Barotropic Normal Modes
'
''
'ddU v
t dydx
0D
Dt
Linearize about a basic state with zonally invariant zonal velocity
( , ) ( ( ), 0)U V U y
The equation becomes
In the spatial domain, we require that the solution at each grid point grows linearly
We assume a sinusoidal structure in x and discrete structure in y ' 2 /( ) i mx D
nG y e
1 1 11 1 1 1
1
1
n Nn n n
n k N n nN N N
N k N N N
G M M M G G
G M M M G GtG M M M G G
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Is this the form of instability which is most pronounced in the atmosphere
10 m/s
10 m/s20 m/s
20 m/s30 m/s
30 m/s
0 m/s
0 m/s
40 m/s
Sector zonal mean cross section
Thermal wind map (250 hPa – 850 hPa)
There is much more vertical sheer than horizontal sheer in the jetThis is a different form of instability because it is in hydrostatic and geostophic balance
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Mid-atmosphere (500 hPa) DJF temperature map
Can we extract energy from this?
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How do Storms Grow? Perturbations (Storms) extract energy from the
mean state via two different mechanisms
Meridional Temperature Gradient(Baroclinic)
Velocity Shear(Barotropic)
High Energy
Low Energy
High Energy
Low Energy
Wind VectorsIsotherms
Hot
Cold
Not too hot
Not too cold
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Atmospheric available potential energy- energy decrease by flattening isotherms
Temperature Potential Temperature
Equator Pole
Equator Pole
Equator Pole
Equator Pole
Height
Height
Height
Height
cold
coldhot
hot
More Energy
Less Energy
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Simple model of baroclinic instability
x
y
z
Top layer
Bottom layer
MEAN STATE
•2 layer model
•Uniform meridional temperature gradient
•No zonal variations
warm
cold
FASTEST GROWING PERTURBATION
Contours = perturbation stream functionColors = tendency in stream function
•Peturbations slant against the vertical shear
•This causes the energy to be converted to the eddies
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• The maximum growth of perturbations is: .31 f N-1 Eady Growth Rate
• Using values for the mid-latitude atmosphere, the perturbations will double in magnitude every 2 days, ocean = 20 days
• The horizontal spatial scale of the perturbations is 4000 km in the atmosphere, 400 km in the ocean
Results of the simple model
dUdz
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Tilt of baroclinic modes
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What happens to eddies as they are advected by the mean flow
T=0, u’v’ dU =0 dY
u’v’ dU >0 dY
T=1
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Layered eddy advection
UpperLevel mean
flow
LowerLevel mean
flow
T= 0 days T= 2 days T= 4 days
v’t’ < 0
u’v’ = 0
v’t’ = 0
u’v’ > 0
dTdydUdy
dTdydUdy
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Atmospheric Energy Reservoirs
Mean StatePotential EnergyEquator to Pole TemperatureGradient
Mean StateKinetic Energy
Large Scale Circulation
Transient Eddy Potential Energy
Transient thermal
anomalies
Transient EddyKinetic Energy
Transient Circulations
10X >
-v’t’ dTdy
w’α’ N2
u’v’ dUdy
BaroclinicGrowth
BarotropicDecay
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Lifecycles in simple models
Chang and Orlanski , 1993
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Baroclinic Instability explains the Locations of storm tracks
Storm activity
High pass height variance at 250 hPa
75 m2
75 m2
105 m2
Baroclinicity
Eady Growth Rate
.6 /day
.6 /day
Hoskins, Valdes, 1989
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Different Ways of defining a storm-trackHigh Pass Eulerian variancesHigh pass filter a field and take the variance
z’2 (250 hPa) v’2 (300 hPa) slp’2
v’t’ (850 hPa)u’v’ (250 hPa)
Chang, 2002
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Alternative approach, Lagrangian tracking
Dotted red lines = tracksColored boxes = size
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Defining a storm track, continuedTrack features (Lagrangian) and keep track of where they pass and
how strong their central value is
Sea level pressure features- track density.
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The picture in 1888
Hinman, 1888
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What seeds storms?
Cyclogenesis density at 850 hPa.
Courtesy of Sandra Penny
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Seasonality of storminess
Pacific StorminessV’2 (300 hPa)
Atlantic StorminessV’2 (300 hPa)
Pacific BaroclinicityU(500 hPa) – U(925 hPa)
Atlantic storm activity follows the baroclinicity, but Pacific does notChang, 2002
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Mid-winter suppression of the Pacific storm track
Courtesy Camille Li
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Ideas on Midwinter Suppression
DJF
SON
Weaker seeding in winter?From Sandra, again
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Last Glacial Maximum Storm Tracks
V’T’ throughout the troposphere (colors) and upper level jet (contours) during the winter
LGM has less storm activity
LGM - MODERN
MODERN
LGM
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LGM baroclinicity
LGM
Modern
LGM - MODERN
LGM has more baroclinicity
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Do faster growing storms meanbigger storms?
Composite Storm size (m)
Composite storm growth
Rate (per day)
LGM
MODERN
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Do faster growing storms meanbigger storms?
LGM
MODERNProbabilitydistributionfunction
of initial size,growth rate, and growth period for LGM and Modern
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Predicted and observed storm sizedistribution for LGM and modern
LGM
MODERN
Predicted frominitial size
and growthPDF
Observed inmodel
Bottom line, storm size not proportional to growth rate/instability in mean state
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Baroclinic instability in the ocean