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Mesoscale Convective Systems Associated with African Easterly Waves. Niamey. Bamako. 30 th AMS Conference on Hurricanes and Tropical Meteorology. Matthew A. Janiga and Chris D. Thorncroft University at Albany, SUNY. 500 km. What do we know about the AEW-MCS Relationship?. 12.5°-20°N. - PowerPoint PPT Presentation
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Mesoscale Convective Systems Associated with African Easterly Waves
30th AMS Conference on Hurricanes and Tropical Meteorology
Matthew A. Janiga and Chris D. ThorncroftUniversity at Albany, SUNY
NiameyBamako
500 km
Adapted from Fink and Reiner (2003)
Squall Line Generation
12.5°-20°N
5°-12.5°NMid-level Vortex
What do we know about the AEW-MCS Relationship?
Longitude
Lati
tude
NW
NE
• Fink and Reiner (2003) found that squall line generation primarily occurred NW of the mid-level AEW vortex and south of the northern AEW low-level vortex.
• Dissipation occurred in the ridge.
What is responsible for this relationship?
• The NW squall line initiation maximum is related to a westerly low-level jet (LLJ) with high equivalent potential temperature (θe) (Berry and Thorncroft, 2005).• The westerly LLJ is associated with the northern low-level vortex.
SHL – Saharan heat lowLLJ – Low-level jet
ITD – Intertropical discontinuityAEJ – Africa easterly jet (at 600 hPa)
X – Vorticity maximum or trough
Based on Berry and Thorncroft (2005) and others
What is still not understood?
a) How AEW Structure Supports Convective Development…– The vertical distribution of moisture and temperature.– This is important for forecasting convective systems
associated with AEWs.
b) Properties of Precipitation Features (PFs) in the AEW envelope…
– The size, intensity, and vertical development of the PFs.– The vertical structure of convective and stratiform regions.– The vertical structure of convection affects the heating
profiles and the upscale impact of convection on the AEWs.
• TRMM 3B42 is a continuous gridded rain rate dataset (Huffman et al., 2007) utilizing passive microwave, precipitation radar (PR), geostationary infrared (IR), and rain gauge data.– Wavenumber-frequency filtered TRMM 3B42 is used to
determine AEW phase and amplitude.
• The NCEP Climate Forecast System Reanalysis (CFSR) (Saha et al., 2010) is one of the latest-generation reanalyses.– Analyses are composited by AEW phase to diagnose the
thermodynamic and kinematic AEW structure.
• TRMM PR and TMI orbital swaths contain information on the vertical structure of convection and PF properties.– Orbital data is binned by AEW phase using 3B42 rain rate
filtered for synoptic westward propagating convection.
Data
Convection as Viewed by the TRMM Platform
C
S
Determining Maximum and Minimum Phases of TD Filtered 3B42
3B42 (shaded, mm hr-1) and TD filtered 3B42 RR (every 1.5σ).
Composite Domain
Maximum
MinimumStandard Deviation of TD filtered 3B42 RR
TD FilterPeriod: 2.5-10 days
Wavenumbers: -20 to -7 (2000-5600 km)
Domain: 5-12.5°N, 10°W-20°E
Determining Increasing and Decreasing Phases of TD Filtered 3B42
3B42 (shaded, mm hr-1) and TD filtered 3B42 dRR/dt (every 1.5σ).
Increasing
Decreasing
Composite Domain
Standard Deviation of TD filtered 3B42 dRR/dt
TD FilterPeriod: 2.5-10 days
Wavenumbers: -20 to -7 (2000-5600 km)
Domain: 5-12.5°N, 10°W-20°E
AEW Phase Partitioning using Wavenumber-Frequency Filtered 3B42
MAXMIN
INC
DEC
TOOWEAK
1.5σ
TRMM Orbital Binning Schematic
MAX
MIN
DEC
INC
AEW Phases for > 1.5σ Amplitude (shaded) and TD Filtered 3B42 RR (every 1.5σ).
8 AEW phases are identified using the 3B42 TD filtered RR and dRR/dt. The AEW phase and amplitude is used to partition orbital data binned to the same 1.0°x1.0° grid.
3B42 TD RR (standard deviations)
3B42
TD
dRR/
dt (s
tand
ard
devi
ation
s)
Maximum
Minimum
AEW Structure
Phase 1 is located ahead of the trough.
The cold-core AEWs have troughs and ridges which peak between 600-700 hPa.
There is a quadrapole of temperature anomalies. This is because the temperature gradient reverses above 700 hPa.
Trough Ridge
Moisture and Thermodynamics
There is increased moisture ahead of the and within the AEW trough. Within and ahead of the ridge is dry.
High low-level θe (and CAPE) is found ahead of the trough with lower low-level θe in the southerlies.
Moist Dry
HighCAPE
LowCAPE
ShearThe AEJ strengthens ahead of the trough and weakens behind it.
Surface westerlies are enhanced ahead of the trough.
Both of these act to increase the shear ahead of the trough and weaken it behind the trough.
Enhanced Shear Reduced Shear
Variation of Rainfall and Stratiform Ratios by Wave Phase
The TD waves show a clear transition from convective to stratiform rainfall between the leading and trailing edges of the convective envelope.
Does the structure of the convective and stratiform precipitation vary too?
Black solid = Total rain rateBlue solid = Stratiform rain rateRed solid = Convective rain rate
Black dashed = Stratiform fraction
RIDGE N TROUGH S RIDGE
Wave Phase (Precipitation – 3B42)
Wave Phase (Dynamics - CFSR)
Wave-Phase CFADs (Convective)
• Two convective modes are apparent over this region.– A deep mode where
convection reaches the tropopause.
– A shallow mode where most of what is observed is below the melting level.
The % of reflectivity values falling in each bin at each level. Composite of all 8 phases for convective precipitation.
Domain: 5-12.5°N, 10°W-20°E.
Deep ModeShallow
Mode
Wave-Phase CFADs (Convective)
7:INC 8
1: MAX
5: MIN
3: DEC2
4 6
Comp.
Shows a composite CFAD for all phases and the differences between each phase. CFADs are normalized for each phase.
The main difference is a tendency towards increased shallow-warm rain in the suppressed phase and deep convection in the enhanced phase.
Wave-Phase CFADs (Stratiform)
• The stratiform regions have lower reflectivity values than the convective regions. The reflectivity also doesn’t extend as high.
• A kink toward high reflectivity values is found between 4-5 km associated with the bright band / melting level.
The % of reflectivity values falling in each bin at each level. Composite of all 8 phases for stratiform precipitation.
Domain: 5-12.5°N, 10°W-20°E.
Bright Band / Melting Level
Wave-Phase CFADs (Stratiform)
7:INC 8
1: MAX
5: MIN
3: DEC2
4 6
Comp.
The main difference is a tendency towards increased reflectivity in the enhanced phase and reduced reflectivity in the suppressed phase.
The enhanced phases have a deeper column of observable reflectivity above the melting level.
Modification of the Diurnal Cycle
Enhanced(Phase 1)
Suppressed(Phase 5)
The enhanced phase has the “flattest” diurnal cycle with the largest fractional contributions from early morning (0000-0600 LT) rainfall.
In the suppressed phase, the greatest percentage occurs at 1800 LT. There is very little contribution from the diurnal minimum (0600-1200 LT).
Climatology
The % of the diurnal cycle’s rainfall coming from each 3-hr block (local time) for Phase 1, Phase 5,
and the domain climatology.
Domain: 5-12.5°N, 10°W-20°E
Identification of Precip. Features (PFs)
• Precipitation features (PFs) are defined as contiguous regions of rain rate > 0 mm hr-1 from the TRMM PR (no size criteria are applied).
• 3 PF characteristics are defined using the rain rate, reflectivity profiles, and collocated TMI data.– PF Size– 18 dBZ echo top– Minimum 85 gHZ temperature
• We focus on the total rainfall from PFs at falling in each PF characteristic value bin.
The % of the rainfall coming from a range of PF characteristic bins for Phase 1,
Phase 5, and the domain climatology.
Domain: 5-12.5°N, 10°W-20°E
Enhanced(Phase 1)
Suppressed(Phase 5)
Climatology
Object Size
85 GHz PCT
Compared to the suppressed phase, the enhanced phase has a larger contribution of its rainfall from PFs with • higher echo tops • larger PFs • colder minimum 85 GHz temps.
Summary of the AEW-Convection Relationship
• AEWs increase the vertical extent, size, and rainfall intensity of convective systems.
• The enhanced (suppressed) phases particularly enhance (suppress) rainfall early in the day (0000-0900 LT).
• Shear, instability, lift, and moisture are all increased in the northerlies.
Questions?
Percent of Rainfall From Various PF Characteristic Values
Volumetric Rain Contribution: System Size
The “50/50 split” of the volumetric rain bins at each 1.0°x1.0° grid box.
The regions with high rain rates are dominated by contributions from large PFswhile the cold tongue and Egypt are dominated by very small systems.
10000
Volumetric Rain Contribution: Echo Tops
• There is an axis of intense convection stretching from Sudan westwards toward Senegal.
• A second region of intense convection is found on the slopes where the Great Escarpment meets the Congo Basin.
• Add 85 gHZ PCT
MCSs associated with the “Helene AEW” of 2006
Triggering occurs near the Jos Plateau ahead of the AEW trough.
Life-Cycle of the Niamey MCS
Sep. 7, 1200Z2006
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
In the late afternoon convection expands in coverage.
Life-Cycle of the Niamey MCS
Sep. 7, 1800Z2006
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
Most of the other convection weakens but the Niamey MCS strengthens as the nocturnal LLJ develops.
Life-Cycle of the Niamey MCS
Sep. 8, 0000Z2006
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
More intensification occurs through 0600Z when the LLJ reaches its peak intensity.
Life-Cycle of the Niamey MCS
Sep. 8, 0600Z2006
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
As the LLJ weakens at 1200Z the MCS begins to dissipate.
Life-Cycle of the Niamey MCS
Sep. 8, 1200Z2006
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
925 hPa θe (K, shaded), streamfunction (x106 m2s-1,
contours), winds (ms-1, vectors), and vorticity (> 2.5x10-5 s-1,
pattern).MCS
NV
NV
MCS
925 hPa θv (K, shaded), streamfunction (x106 m2s-1,
contours), winds (ms-1, vectors), and vorticity (> 2.5x10-5 s-1,
pattern).
Sep. 8, 0600Z2006
Niamey Radar
150 km
Niamey Radar
150 km
Niamey Radar
150 km
Niamey Radar
150 km
Niamey Radar
150 km
Niamey Radar
150 km
Niamey Radar
150 km
Niamey Radar
150 km
Niamey Radar
150 km
Sep. 9, 1800Z2006
Triggering occurs in the late afternoon.
Life-Cycle of the Bamako MCS
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
Sep. 10, 0000Z2006
Intensification occurs as the LLJ begins to develop.
Life-Cycle of the Bamako MCS
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
Sep. 10, 0600Z2006
Continued intensification occurs up through 0600Z when the LLJ reaches its peak intensity.
Life-Cycle of the Bamako MCS
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
Sep. 10, 1200Z2006
The MCS begins to weaken at 1200Z as the LLJ begins to weaken.
Life-Cycle of the Bamako MCS
IR (shaded) and 700 hPa Streamfunction
(x106 m2s-1, contours)
NV
NV
MCS
MCS
925 hPa θe (K, shaded), streamfunction (x106 m2s-1,
contours), winds (ms-1, vectors), and vorticity (> 2.5x10-5 s-1,
pattern).
925 hPa θv (K, shaded), streamfunction (x106 m2s-1,
contours), winds (ms-1, vectors), and vorticity (> 2.5x10-5 s-1,
pattern).
Sep. 10, 0600Z2006
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km
Bamako Radar
150 km