the dynamics of observed tropopause polar vortex (tpv) life cycles
DESCRIPTION
The dynamics of observed tropopause polar vortex (TPV) life cycles. Steven Cavallo Advisor: Greg Hakim. University of Washington Department of Atmospheric Sciences. Outline. What are vortices? Distinguishing between waves and vortices Previous studies and results Climatology of TPVs - PowerPoint PPT PresentationTRANSCRIPT
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The dynamics of observed tropopause polar vortex (TPV)
life cycles
Steven Cavallo
Advisor: Greg Hakim
University of Washington
Department of Atmospheric Sciences
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Outline•What are vortices? Distinguishing between waves and vortices
•Previous studies and results
•Climatology of TPVs
•Numerical case study
•Conclusions and future work
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Why do we care about TPVs?Tropopause polar vortices (TPVs) are:
•Vortices that occur well poleward of the jet stream
•Based on the tropopause
•Cold core
Although there is considerable understanding about the life cycles of surface extratropical cyclones, relatively less is known about the upper-level disturbances governing them
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What are vortices?
• In a materially conserved field, nonlinear solutions are vorticesFluid parcels are bound by closed contours of that field
• It is advantageous to trace fluid parcels using a materially
conserved field such as potential vorticity (PV)
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Vortices and Ertel potential vorticity Ertel’s theorem says that
where is the Ertel potential vorticity (EPV), is the absolute 3-D vorticity, is the density, is a frictional force vector, and is the potential temperature.
EPV is conserved when the diabatic and frictional terms are zero.
•This study will examine non-conservative processes contributing to changes in EPV from the diabatic term.
aD D F
Dt Dt
2a U
/a
F
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Potential Vorticity & Isentropic Surfaces
Cross section of potential vorticity surfaces (black) in PVU and isentropic surfaces (red) in Kelvin from the pole (left) to the equator (right). The 2 PVU surface is indicated by the bold black line where a PVU = potential vorticity unit = m2 K kg-1 s-1
(Adapted from Hoskins 1990)
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What is this study about?This study examines
1) A climatology of TPVs:
Where do they form and decay?
Where do their amplitudes change the most?
Are there any large scale, recurring patterns that may be associated with these?
2) Numerical case study:
What mechanisms during their lifecycles contribute most to their growth and decay?
Can we isolate and generalize any of these mechanisms?
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TPV climatology and composites: Definitions
amp
What is amp?
- core
core = lcc
lcc
Other terminology:
•Maximum 24-hour growth: The point along a vortex track in which amp increased the most within a 24-hour period
•Maximum 24-hour decay: The point along a vortex track in which amp decreased the most within a 24-hour period
Other definitions:
•Genesis: The beginning of a vortex track
•Lysis: The end of a vortex track
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What we know about TPVs
Hakim and Canavan, 2003
•TPVs have characteristic life-cycles, growing in amplitude by about 50% within the first 48-72 hours and slowly decaying
•Annual frequency of anticyclones greatest in Summer
Frequency Strength
•Annual frequency and strength of cyclones greatest in late Winter and late Autumn
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TPV climatology and composites•Data include vortices lasting at least 2 days and spent at least 60% of their lifetimes north of 65N
•Genesis and lysis
Regions of greatest cyclone
and anticyclone genesis and decay
Composites based on maximum
cyclogenesis region
194 cases
141 cases
123 cases
•Maximum 24-hour growth and decay
Regions of strongest growth and decay
Composites based on maximum 24-hour growth for cyclones
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TPV climatology
Density of tropopause polar cyclones that developed within a 5 latitude by 15 longitude box centered at each location from 1948-1999.
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TPV composites: Cyclogenesis
0 hours
-24 hours-72 hours
•500 hPa geopotential height anomalies
•Significant at 95% confidence level by student-t test
•Centered at: 75N, 85W
+48 hours
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TPV composites: Cyclogenesis
•The Aleutian low is a common precursor no matter which way we look at it
Aleutian ‘-’ and western North American ‘+’ anomalies
Greenland disturbance
Canada cyclogensis
Siberian ‘-’ anomaly
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TPV climatology: Growth and decay
Growth
Growth
Decay
Decay
Cyclones
Anti-cyclones
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TPV climatology
Density of tropopause polar cyclones with 24-hour potential temperature
amplitude increases from 5-20K within a 5 latitude by 15 longitude box centered at each location from 1948-1999.
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TPV composites: 5-20K Greenland Growth
•500 hPa geopotential height anomalies
•Significant at 95% confidence level by student-t test
•Centered at: 75N, 45W
0 hours
-48 hours-168 hours
+168 hours
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TPV composites: Greenland Growth
•500 hPa geopotential height anomalies
•Significant at 95% confidence level by student-t test
•Centered at: 75N, 45W
0 hours
-48 hours-168 hours
+168 hours (10K+ growth)
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TPV composites: Greenlandmaximum 24-hour cyclone growth
Greenland disturbance
Amplification
Movement toward Siberia
Pacific and Atlantic coast ‘+’ anomalies
Atlantic ‘+’ anomaly Hudson Bay
Alaska ‘-’ anomaly
Pacific re-development
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TPV composites: 5-20K Canada Growth
•500 hPa geopotential height anomalies
•Significant at 95% confidence level by student-t test
•Centered at: 75N, 45W
0 hours
-24 hours-168 hours
+48 hours
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TPV composites: 5-20K Canadian maximum 24-hour cyclone growth
Canada disturbance Mid-Pacific ‘-’ anomaly
Amplification Blocking Ridge pattern
•Growth dominated by local effects
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TPV composites: 10K+ Canada Growth
•500 hPa geopotential height anomalies
•Significant at 95% confidence level by student-t test
•Centered at: 80N, 125W
0 hours
-24 hours-96 hours
+96 hours
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TPV composites: 10K+ Canadian maximum 24-hour cyclone growth
Northern Canada disturbance Circumpolar wave pattern
Amplification Across-pole wave pattern
High amplitude anomalies
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Numerical Case Study
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Potential vorticity diagnosis methods•Thermodynamic energy equation:
, , , , ,t rad t pbl t cumulus t mix t microphysics
D
Dt
, ,t radiation t microphysics
, ,a
t radiation t microphysics
D
Dt
where t,rad, t,pbl, t,cumulus, t,mix and t,microphysics are the tendencies due to the effects of radiation, the planetary boundary layer, cumulus processes, mixing & diffusion, and microphysics.
EPV for inviscid flow:
•Now we will examine the feedbacks between radiation and latent heating in the upper troposphere
(in the upper troposphere)
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Potential vorticity: Diabatic mechanismsWhat might we expect from both radiation and latent heating when latent heating is smaller than radiational heating?
•Blue curve is a possible heating rate from latent heating
•Red curve is an oscillatory approximation of radiational heating rates from the cloud (following Liou, Ch. 4)
Latent heating
Radiational heating
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Potential vorticity: Diabatic mechanisms
What might we expect from both radiation and latent heating?
(if the vorticity vector is entirely vertical)
_a latent heating
D
Dt
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Potential vorticity: Diabatic mechanisms
What might we expect from both radiation and latent heating?
(if the vorticity vector is entirely vertical)
a radiation
D
Dt
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Potential vorticity: Diabatic mechanisms
What might we expect from both radiation and latent heating?
(if the vorticity vector is entirely vertical)
_a radiation latent heating
D
Dt
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Potential vorticity: Diabatic mechanismsWhat PV changes might we expect from both radiation and latent heating when radiation dominates?
•Red curve is the sum of the PV changes due to the latent heating and radiation profiles prescribed here
Net EPV change from both radiation and latent heating
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Potential vorticity: Diabatic mechanismsWhat might we expect from both radiation and latent heating when latent heating is larger than radiational heating?
•Blue curve is a possible heating rate from latent heating
•Red curve is an oscillatory approximation of radiational heating rates from the cloud (following Liou, Ch. 4)
Latent heating
Radiational heating
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Potential vorticity: Diabatic mechanismsWhat PV changes might we expect from both radiation and latent heating when latent heating dominates?
•Red curve is the sum of the PV changes due to the latent heating and radiation profiles prescribed here
Net EPV changes from both latent heating and radiation
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Potential vorticity: Diabatic mechanisms
•The horizontal components of vorticity act to direct maximum PV destruction due to latent heating above and downstream of the maximum latent heating
(Stoelinga, 1996)
But…we also have to worry about the feedbacks between the cloud and the radiation
_
( )latent heating
D PV
Dt
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Vortex tracks
November 2005 TPV
Tropopause core
GFS analysis 01 November 2005 00 UTC – 07 December 2005 00 UTC
November 5
November 22
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November 2005 TPV: WRF numerical simulations
•Outline of November 2005 TPV WRF simulations:
Initialization November 5, 2005 over Siberia
Motivation: TPV strengthening phase
Initialization November 22, 2005 over Hudson Bay
Motivation: TPV weakening phase & movement over extensive sounding network
•Horizontal grid spacing 30 km, 31 vertical levels
•5-class microphysics, RRTM longwave radiation
•GFS analysis and boundaries updated every three hours
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November 2005 TPV: WRF results Tropopause core
Vortex track (red) and topography (colors)
meters
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November 2005 TPV: WRF results
Time-height section of total EPV changes due to diabatic effects averaged within the 285K tropopause closed contour
Pre
ssur
e (h
Pa)
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November 2005 TPV: WRF results
Time-height section of cloud water and ice mixing ratios (colors) and EPV creation due to radiational cooling (magenta contours)
averaged within the 285K tropopause closed contour
Pre
ssu r
e (h
Pa)
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November 2005 TPV: WRF results
Time-height section of EPV changes from radiation + EPV changes from latent heating (colors) averaged within the 285K tropopause
closed contour. Magenta line is the zero contour.
Pre
ssur
e (h
Pa)
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November 2005 TPV: WRF results Nov. 22-27Tropopause core
Vortex track (red) and topography (colors)
meters
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November 2005 TPV: Observations
Coral Harbour, NT Sounding WRF tropopause pressure and winds
November 22, 2005 00 UTC
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November 2005 TPV: Observations
November 23, 2005 00 UTC
Coral Harbour, NT Sounding WRF tropopause pressure and winds
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November 2005 TPV: Observations
November 24, 2005 12 UTC
Coral Harbour, NT Sounding WRF tropopause pressure and winds
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November 2005 TPV: Observations
MODIS imagery of TPV induced polar low over Hudson Bay
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November 2005 TPV: WRF results Nov. 22-27
Time-height section of cloud water and ice mixing ratios (colors) and EPV creation due to radiational cooling (magenta contours)
averaged within the 285K tropopause closed contour
Pre
ssur
e (h
Pa)
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November 2005 TPV: WRF results Nov. 22-27
Time-height section of EPV changes from radiation + EPV changes from latent heating (colors) averaged within the 285K tropopause
closed contour. Magenta line is the zero contour.
Pre
ssur
e (h
Pa)
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So what was different between the two cases?
•In Siberia, where the TPV was strengthening, radiation was large compared to microphysics in the upper troposphere
•In Hudson Bay, where the TPV was weakening, radiation was small compared to microphysics in the upper troposphere
Ratio of radiation and microphysics averaged within a closed contour
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A closer look into the microphysics
•Cloud water + ice mixing ratio vertical profile
•Siberia (red) and Hudson Bay (blue) WRF simulations.
•Averages within the 280K closed contour.
t = 6 hours t = 30 hours
t = 54 hours t = 78 hours
Siberia
Hudson Bay
Siberia
Hudson Bay
Siberia
Hudson Bay
Siberia
Hudson Bay
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Conclusions
•TPV cyclogenesis greatest over Queen Elizabeth Islands in Canada
•TPV maximum 24-hour growth was concentrated over both Baffin Island and Greenland
•Strong TP cyclone growth is associated more with non-local effects while weaker growth is associated more with local effects
•TPV strength highly sensitive to the distribution & feedback between latent heating and radiation in the upper troposphere
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Future Work•Zierl and Wirth (1997) showed that in an idealized study that anticyclone strength was highly sensitive to the vertical gradient of radiative heating near the tropopause
•One study looked at radiation and latent heating feedbacks on a surface anticyclone (Curry 1987) and upper level analysis showed differential heating term lowered geopotential heights (Tan and Curry 1989)
•Numerical simulations here of TPV lifecycles suggest that the feebacks between radiation and latent heating are important
•There has been no work examining the feedback between radiation and latent heating on upper level cyclonic vortices!
Now that the primary factors are known, it would be worthwhile to isolate these effects and examine in an idealized setting
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Tropopause uncertainty
Tropopause using 2 PVU (blue line) and 0.25 PVU (red bars)
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TPV climatology
Density of tropopause polar cyclones that decayed within a 5 latitude by 15 longitude box centered at each location from 1948-1999.
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TPV climatology
Density of tropopause polar anticyclones that developed within a 5 latitude by 15 longitude box centered at each location from 1948-1999.
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TPV climatology
Density of tropopause polar anticyclones that decayed within a 5 latitude by 15 longitude box centered at each location from 1948-1999.
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TPV climatology
Density of tropopause polar cyclones with 24-hour potential temperature
amplitude decreases from 5-20K within a 5 latitude by 15 longitude box centered at each location from 1948-1999.
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TPV climatology
Density of tropopause polar anticyclones with 24-hour potential temperature
amplitude increases from 5-20K within a 5 latitude by 15 longitude box centered at each location from 1948-1999.
![Page 56: The dynamics of observed tropopause polar vortex (TPV) life cycles](https://reader035.vdocuments.site/reader035/viewer/2022062309/56815723550346895dc4c32c/html5/thumbnails/56.jpg)
TPV climatology
Density of tropopause polar anticyclones with 24-hour potential temperature
amplitude decreases from 5-20K within a 5 latitude by 15 longitude box centered at each location from 1948-1999.