Transcript Tornadogenesis within Quasi-Linear Convective Systems
MICROBURSTS
Nolan T. Atkins
Lyndon State College
Prepared for COMET Mesoscale Analysis and Prediction Course 2002 (COMAP 2002)
13 June 2002
OUTLINE
1. Introduction – Early Discovery 2. Climatology 3. Forcing Mechanisms 4. Microburst Conceptual Models 5. Wet Versus Dry Microbursts 6. Detection 7. Forecasting
INTRODUCTION – EARLY DISCOVERY
Aerial damage surveys by Fujita of 3 April 1974 super outbreak revealed unusual “starburst” surface wind damage pattern
“Starburst” wind damage pattern
315 fatalities, 5484 injuries 15% of damage paths were caused by outburst winds
Figure from Fujita 1985
INTRODUCTION – EARLY DISCOVERY
“Starburst” damage pattern was very much different than swirling damage left behind in wake of tornado Idea of “down burst” was conceived
“Starburst” wind damage pattern in corn field
Much like “pointing the nozzle of a garden hose downward”
Figure from Fujita 1985
INTRODUCTION – EARLY DISCOVERY
On 24 June 1975, Eastern Airlines Flight 66 (Boeing 727) crashed while attempting to land at New York’s JFK Intl airport 112 fatalities, 12 injuries Cause of crash was unknown, though thunderstorms were observed in the area In an attempt to unravel the mystery behind the crash, Captain Homer Mouden (from the Flight Safety Foundation at the time) approached Fujita and asked him to investigate reasons for the crash
INTRODUCTION – EARLY DISCOVERY
After analyzing
only
flight data recorders, pilot reports and an airport anemometer, Fujita hypothesized that Flight 66 flew through a low-level diverging wind field – downburst First suggestion that a “starburst” wind pattern may be a cause for airline crashes
Figure from Fujita 1985
INTRODUCTION – EARLY DISCOVERY
Fujita’s concept of a downburst, a strong downdraft which induces an outburst of damaging winds on or near the ground, was met with some skepticism Many meteorologists at the time, believed that the downdraft should be relatively weak by the time it reaches the ground Resolution of Fujita’s downburst theory ultimately led to the creation of the Northern Illinois Meteorological Research on Downbursts (NIMROD) field program employing NCAR Doppler radars
INTRODUCTION – EARLY DISCOVERY
On 29 May, 1978, the first radar-detected downburst was observed by the NCAR CP-3 Doppler radar by Fujita and Jim Wilson Radial velocities from first radar-detected downburst The existence of the downburst had been verified.
Since then, a flurry of observational, applied and theoretical work surrounding the downburst has been pursued
Figure from Wilson 2001
Climatology
A national climatological summary of downbursts, unfortunately, does not exist Kelly et al. (1985) have produced a climatology of damaging wind gusts.
Based on 75,626 severe thunderstorm reports from 1955-1983.
Does NOT distinguish damage created from different convective modes (for example, RIJ associated with a bow echo) Three categories of wind gusts were created Severe thunderstorm wind gusts, 1955-1983.
Damaging Strong Violent Total Gust speed unknown 25.8-33.5 m/s > 33.5 m/s
From Kelly et al. (1985)
Annual number 1114 375 113 1602 Percent 70 23 7
Climatology
Damaging wind gusts: Primarily a summer time phenomena
From Kelly et al. (1985)
Climatology
Damaging wind gusts: Most events occur during late afternoon However, a non negligible number of events occur between midnight and noon
From Kelly et al. (1985)
Climatology
1.
2.
3.
Geographical Distribution of damaging wind gusts: Two major frequency axes: Southern MN – IA – IL – IN – OH (NW flow events) NW IA – Kansas City, MO – KS – OK – TX Possibly a third from eastern TX – AL – up to New England High probability of a population bias in data
From Wakimoto (2002)
Climatology
Kelly et al. results are similar to those by Fujita (1981) for the year 1979
From Fujita (1981)
Climatology
1.
2.
3.
4.
Data from Downburst field programs: Northern Illinois Meteorological Research on Downburst (NIMROD) – 1978 Joint Airport Weather Studies (JAWS) – 1982 FAA/Lincoln Lab Operational Weather Studies (FLOWS) – 1985/86 Microburst and Severe Thunderstorm (MIST) project - 1986
From Wakimoto (2002)
Climatology
186 microbursts during JAWS over 86 days Diurnal variation similar to Kelly et al. (1985)
Figures from Wakimoto (1985)
Climatology
62 microbursts during MIST over 61 days Diurnal variation similar to Kelly et al. (1985) Data from field programs suggest downbursts occur frequently
Figures from Atkins and Wakimoto (1991)
Forcing Mechanisms – Updrafts and Downdrafts UPDRAFT
Ascends supersaturated r c +r r +r i negate updraft Latent heat release enhances UD Microphysical details not that important Entrainment is detrimental
DOWNDRAFT
descends largely subsaturated r c +r r +r i enhance downdraft evap cooling/sub/melt enhances DD microphysics can be very important mid-level entrainment can enhance DD, low-level entrainment can be detrimental
Forcing Mechanisms
Q: What physical processes are responsible for generating strong, low-level downdrafts?
The answer can be found in the vertical momentum equation:
d w dt
1
p
z
g
v vo
c c p v p
p o
r c
r r
r i
I II III IV I – Vertical gradient of perturbation pressure II – Thermal buoyancy (parcel theory) III – perturbation pressure buoyancy IV – Condensate loading of cloud, rain and ice water
Forcing Mechanisms
I – Vertical gradient of perturbation pressure 1
p
z
In weakly sheared environments promoting the formation of ordinary cells, the vertical perturbation pressure gradient force tends to be weak This force becomes more important in more strongly sheared environments Example: occlusion downdraft within supercell thunderstorms
Forcing Mechanisms
II – Thermal buoyancy
g
v vo
Well-understood process in convective downdrafts –
is the most important forcing mechanism for most convective downdrafts
Created by the evaporation, melting and sublimation of cloud and precipitation particles within a sub saturated parcel of air In weakly precipitating downdrafts: The downdraft can simply be though as the competing processes of negative buoyancy generation through condensate phase changes and adiabatic compressional warming Note the use of the
virtual potential temperature
Downdraft intensity has been shown to increase within higher relative humidity environments at low levels by increasing the v difference between the
sub saturated
downdraft parcel and the environment (e.g., Srivastava 1985; Proctor 1989)
Forcing Mechanisms
Yes, observational and modeling studies (e.g., Kamburova and Ludlam 1966; Leary and Houze 1979; Srivastava 1985; Proctor 1989) have shown that the downdraft often descends sub saturated. Cooling due to condensate phase changes does not completely compensate for adiabatic compressional warming This may be true even with heavier precipitation events: Byers and Braham (1949) noted “humidity dips” associated with Florida and Ohio thunderstorm downdrafts Thus, microphysical details, while not as important for updrafts, appear to be quite important for generating stronger downdrafts: Numerical calculations (e.g., Kamburova and Ludlam 1966; Srivastava 1985, 87; Proctor 1989) suggest that the maintenance and intensity of a downdraft by falling precipitation is a function of: Precipitation type (i.e., rain, snow, hail or graupel) Precipitation size Precipitation intensity and duration
Forcing Mechanisms
III – Perturbation pressure buoyancy
c g c p v p p o
This term is ignored in Parcel Theory Has been shown to be relatively weak in comparison to the thermal buoyancy and vertical perturbation pressure gradient terms within convective storms (Schlesinger 1980) Perturbation pressure buoyancy term has been shown to have appreciable magnitudes where the updraft penetrates the tropopause
Forcing Mechanisms
IV – Condensate Loading
g
r c
r r
r i
Long been recognized as an important process for the initiation and maintenance of downdrafts (e.g., Brooks 1922) Compared to thermal buoyancy, this term is often of secondary importance for downdraft maintenance and intensity (but not always).
It is, however, important for downdraft initiation
Forcing Mechanisms
Entrainment Entrainment has long been recognized as an important process affecting the strength of updrafts within convective storms Weakens the updraft by mixing environmental air into buoyant parcels Largely explains why Parcel Theory over estimates the maximum vertical velocity expected for a surface-based ascending parcel, i.e.,
W
max 2
CAPE
For downdrafts, it is generally thought that entrainment of dry environmental air promotes downdraft initiation and maintenance by increased evaporation, melting and sublimation of cloud and precipitation particles within sub saturated downdraft parcels of air.
However………..
Forcing Mechanisms
Entrainment Numerical simulations by Srivastava (1985) and Proctor (1989) suggest that entrainment can be
detrimental
to downdraft strength!
Srivastava’s Model configuration: 1-D, time-dependent model of evaporatively driven downdraft Initial downdraft at top of model domain specified by P, T, RH, W, DSD Environmental RH = 70%
From Srivastava (1985)
Forcing Mechanisms
Entrainment Resolution of these two conflicting ideas may be related to where and when entrainment is occurring: Entrainment may be
beneficial
for downdraft initiation and subsequent maintenance say near cloud base.
Entrainment may be
detrimental
for downdraft maintenance at low levels since the virtual potential temperature difference between the
sub saturated
negatively buoyant downdraft parcel and the environment will decrease, particularly if the mixing ratio of the environment is larger than that of the downdraft parcel.
Microburst Conceptual Models
Fujita defined a downburst as a
strong downdraft which induces an outburst of damaging, highly divergent winds on or near the ground
.
The scale of the downburst varies from less than 1 km to 10s of km.
Thus, he subdivided downbursts into
macrobursts
and
microbursts
according to their horizontal scale of damaging winds:
Macroburst:
A large downburst with its outburst winds extending in excess of 4 km in horizontal dimension. An intense macroburst often causes widespread, tornado-like damage. Damaging winds, lasting 5 to 30 minutes, could be as high as 60 m/s.
Microburst:
A small downburst with its outburst, damaging winds extending only 4 km or less. In spite of its small horizontal scale, an intense microburst could induce damaging winds as high at 75 m/s.
Microburst Conceptual Models
The F2 Andrews Air Force Base Microburst on 1 August 1983
Figure from Fujita 1985
Microburst Conceptual Models
One of the earliest conceptual models was put forth by who else…., yes, Fujita (1985).
The midair microburst may or may not reach the ground At touchdown, the microburst is characterized by a shaft of strong downward velocity at its center and strong divergence.
Soon thereafter, an outburst of strong, accelerating winds within a rotor circulation spreads outward.
The strongest winds are generally found in the base of the rotor circulation and can have a significant impact on aviation operations
Figure from Fujita 1985
Microburst Conceptual Models
Numerical Simulations of a microburst and associated rotors
Figure from Orf et al. (1996) Figure from Proctor et al. (1988)
Microburst Conceptual Models
Observations of a microburst and associated rotor
Figure from Kessinger et al. (1988) Also see Wilson et al. (1984)
Presumably, the rotor is generated through tilting of vertical vorticity and/or baroclinically along the leading edge of the outflow As the outflow and rotor spreads out, the rotor circulation is enhanced through vortex stretching
Microburst Conceptual Models
3-Dimensional conceptual model of a microburst (Fujita, 1985) Notice the intense small-scale (< 4 km; misocyclone) rotation associated with the microburst This rotation is a relatively common feature associated with microbursts Some studies suggest the rotation enhances microburst strength (e.g., Rinehart el al. 1995; Fujita 1985; Wakimoto 1985) Other studies suggest that the rotation weakens the microburst (e.g., Kessinger et al. 1988; Proctor 1989)
Figure from Fujita (1985)
Microbursts – Wet and Dry
A large number of studies have shown that microburst winds are associated with a continuum of rain rates, ranging from heavy precipitation from deep cumulonimbi to virga shafts from altocumuli or high-based cumulonimbi.
There is
no positive correlation
between downburst winds and surface precipitation rates Accordingly, microbursts are subdivided into wet/high reflectivity and dry/low reflectivity events and are defined as follows (Fujita and Wakimoto 1981; Wilson et al. 1984; Fujita 1985):
Dry/low reflectivity microburst
: A microburst associated with < 0.25 mm of rain or a radar echo < 35 dBZ in intensity
Wet/high-reflectivity microburst
: A microburst associated with > 0.25 mm of rain or a radar echo > 35 dBZ in intensity
Dry Microbursts - Observations
Produced from innocuous pendent virga shafts from weakly precipitating altocumulus
Photographs taken by B. Waranauskas, from Fujita (1985) of virga and curl of dust associated with the rotor circulation with a dry microburst Example of altocumuli producing dry microbursts Photograph taken by B. Smith (from Wakimoto 1985)
Dry Microbursts - Observations
Dual-Doppler radar observations of a dry microburst outflow (also see Wilson et al. 1984)
figure from Hjelmfelt (1988)
Figure from Fujita (1985)
Figure from Fujita (1985)
Dry Microbursts - Observations
Figure from Wakimoto et al. (1994)
Dry Microbursts - Environment
Deep, dry-adiabatic, well-mixed boundary layer.
High cloud bases – 500 mb Dry sub cloud layer (3-5 g/kg) with mid-level moisture present
Figure from Wakimoto (1985) (Also see Krumm 1954; Wilson et al. 1984; McCarthy and Serafin 1984; Fujita 1985; Mahoney and Rodi 1987; Hjelmfelt 1988)
Dry Microbursts - Environment
Dry microbursts are largely driven by negative thermal buoyancy created by the evaporation, melting and sublimation of precipitation When a deep, dry adiabatic layer is present, only light precipitation is required to generate strong downdrafts…., why? Compressional warming
can not
counteract negative buoyancy created by precipitation phase changes Parcel accelerates to the ground Note that surface parcel temperature may not be much different than environment, may actually be warmer! (Fujita 85; Srivastava 85; Proctor 89)
Based on a figure from Wakimoto (1985)
Dry Microbursts - Environment
With a slightly more stable layer just below cloud base, for example, it may not possible to generate a strong downdraft. Thus, deep, dry-adiabatic sub cloud layers are crucial for producing strong dry microbursts Numerical simulations also suggest that low level environmental moisture helps produce stronger downdrafts by increasing the v difference between the sub saturated parcel and environment (e.g., Srivastava 1985; Proctor 1989)
Based on a figure from Wakimoto (1985)
Dry Microbursts – Microphysical Considerations
In addition to the environmental profiles of temperature and moisture, dry microburst strength has been shown to be a function of: Precipitation intensity, size, and phase In particular, sublimation from snowflakes has been shown to very very effective at generating strong dry microbursts (Proctor 1989; Wakimoto 1994). Why?
Numerous low-density snowflakes readily sublimate Large latent heat due to sublimation Sublimation cooling (also melting) occurs quickly at relatively high altitudes (Srivastava 1987) – allowing the downdraft parcels to accelerate through a deep dry-adiabatic layer.
Dry Microbursts – Microphysical Considerations
Some visual evidence of the sublimation process was presented by Wakimoto et al. (1994)
Figure from Wakimoto et al. (1994)
Wet Microbursts - Observations
Produced by deep cumulonimbus with warm cloud bases in more humid environments
Figure from Fujita (1985) Photo copyrighted and taken by Mike Smith Figure from Atkins and Wakimoto (1991). Photo taken by K. Knupp
Figure from Atkins and Wakimoto (1991).
Wet Microbursts - Observations
Wet Microbursts - Observations
Figures from Kingsmill and Wakimoto (1991)
Wet Microbursts - Environments
Relative to dry microbursts, wet events form in more stable environments Accordingly, it is more difficult for negative thermal buoyancy to counteract compressional warming Thus, more precipitation is required to enhance negative thermal buoyancy production and increase precipitation loading
Figure from Atkins and Wakimoto (1991)
Wet Microbursts - Environments
Notice that for lapse rates > 8.5 ºC km -1 , both wet and dry microbursts are observed to occur However, when the lapse rate is < 8.0 ºC km -1 , only wet microbursts occur Virtually no microbursts occur when the lapse rate was less than 7.0 ºC km -1 .
Figure from Srivastava (1985)
Wet Microbursts - Environments
Numerical simulations by Srivastava (1985) and Proctor (1989) are consistent with the observations by Srivastava (1985) that suggest progressively larger amounts of precipitation are required to form microbursts in increasingly more stable environments
Figure from Wakimoto (2002), based on figure from Srivastava (1985)
Wet Microbursts – Microphysical Considerations
Similar to dry microbursts, the ice phase has been shown numerically (Srivastava 1987; Proctor 1989) and observationally (Wakimoto and Bringi 1988) to be important Hail in particular, provides cooling throughout the entire depth of the downdraft extent – very important at low levels below cloud base!
Figure from Wakimoto and Bring (1988)
Wet Microbursts – Microphysical Considerations
Unlike dry microbursts, precipitation loading can be important for the initiation and initial maintenance of the wet microburst at higher levels Notice that within the wet microburst, parcels can be warmer than the surrounding environment! (also see Wei et al. 1998 and Igau et al. 1999 for tropical downdrafts) Below cloud base in the dry adiabatic, well-mixed layer, thermal buoyancy becomes very important
Figure from Proctor (1989)
Microburst Detection
Wilson et al. (1984) showed that Doppler radar could detect events at close range. Events during JAWS showed: Typical downdraft is 1 km wide Spread out horizontally below a height of 1km AGL Median time from initial divergence at the surface to maximum differential velocity across microburst is 5 minutes Height of maximum differential velocity is about 75 m AGL Median velocity differential was 22 m/s over an average distance of 3.1 km They are short-lived, low-level, small-scale events.
Microburst Detection
Roberts and Wilson (1989) suggest that the following radar attributes can be used to detect microburst development: Descending reflectivity cores Increasing radial convergence within cloud Rotation reflectivity notches These typically appeared 2-6 minutes prior to initial surface outflow Their results suggest 0-10 minute microburst nowcasts are possible
Microburst Detection - Examples
Descending reflectivity cores
Figure from Wakimoto (2002), original figures from Kingsmill and Wakimoto (1991)
Microburst Detection - Examples
Increasing radial convergence within cloud
Figure from Fujita (1985)
Rotation
Microburst Detection - Examples
Figure from Roberts and Wilson (1989)
Microburst Detection - Examples
Reflectivity notch
Figure from Roberts and Wilson (1989)
Other automatic detection schemes and algorithms are discussed in Dance and Potts (2002)
Microburst Forecasting
When the environmental wind shear is relatively weak, the vertical profile of temperature and moisture can be used to assess microburst potential (Johns and Doswell 1992) Dry Microbursts: Deep dry adiabatic sub-cloud layer to mid levels Moist mid tropospheric layer, dry low-levels Marginal updraft instability Updraft sounding indices can not be used to forecast microburst potential or severity
Figure from Wakimoto (1985), also see Krumm (1954), Beebe (1955) and Caracena et al. (1983)
Microburst Forecasting
Wet Microbursts: Moist low levels up to 3-5 km, dry mid levels Dry adiabatic sub-cloud layer 1.5 km deep Weak capping inversion
Figure from Atkins and Wakimoto (1991) Also see Caracena and Maier (1987)
Microburst Forecasting
e difference from surface to emin ( D e ) of 20 K or so appears to be a characteristic of wet microburst producing environment D e values less than 13 K produced thunderstorms, but no wet microbursts The Cape Canaveral Air Station have developed the MDPI = D e /30. (Wheeler and Roeder 1998). MDPI > is interpreted as high wet microburst probability, issued only when thunderstorm activity is forecast > 60%
Figure from Atkins and Wakimoto (1991)
Microburst Forecasting
While sounding indices for predicting updraft strength work reasonably well, the same can not be said for predicting peak downdraft strengths with sounding indices: Downdraft sensitivity to microphysics Largely sub saturated descent Nonlinear relationship between maximum downdraft vertical velocity and outflow speeds (it’s not 1:1!!).
That said, previous investigators have developed potential microburst strength indices that can be easily calculated with routinely collected sounding data.
Microburst Forecasting
Proctor (1989) put forth the following “wet microburst potential intensity” index:
I
H
2
m
0
H m
Q v
( 1
k m
) 1 .
5
Q v
(
H m
) / 3 0 .
5 5 Where: H m o is the height of the melting level is the mean lapse rate from the ground to the melting level = 5.5 ºC/km Q v is the mixing ratio If < o , then I < 0 I is larger if: H m is large is large Moist at 1 km and dry at the melting level Worked well for modeled microbursts, but not for observed events
Microburst Forecasting
McCann (1994) modified Proctor’s index in the following way:
WI
5
H m R Q
G 2 30
Q L
2
Q M
0 .
5 Where: WI = Wind Index (WINDEX) H m G is the height of the melting level is the mean lapse rate from the ground to the melting level Q L Q M is the mean mixing ratio of lowest 1km is the mixing ratio at the melting level R Q = Q L /12 but is set to 1 if Q L /12 > 1.
WI is larger if: H m G is large is large (note G 2 dependence) Moist at low levels and dry at the melting level How well does WINDEX work?
24 August 1993
Microburst Forecasting
2000 UTC 2200 UTC
Figure from McCann (1994)
Notice the outflow boundary moving into an area with high WINDEX values Microburst damage in vicinity of DFW was observed on this day Microburst forecasting is intimately related to convective initiation forecasting – monitoring low-level convergence boundaries
Microburst Forecasting
Recently, Geerts (2001) has modified the WINDEX to account for other processes that help to generate strong wind gusts such as the downward transfer of horizontal momentum: He created the GUSTEX to include this process: GU = a WI + 0.5U
500 Where a is a constant (he set it to 0.6) WI = WINDEX U 500 is the 500 hPA wind velocity For Australian wind gust events, he showed a better correlation between GUSTEX and observed gust speed than with WINDEX and observed gust speed.
Microburst Forecasting
Ellrod (1989) and Ellrod et al. (2000) have shown the value of using GOES satellite data form microburst forecasting.
Ellrod et al. (2000) tested the following indices derived from satellite data: 1.
2.
WINDEX DMI = G 700-500hPa + (T-T d ) 700 – (T-T d ) 500 > 6 for dry microbursts to occur (Ellrod and Nelson 1998); DMI 3.
D e Products are creating hourly and have been shown to provide “information useful in the preparation of short range weather forecasts and advisories”.
Conclusions
First discovered by Fujita in mid 70s while surveying tornado damage Immediately realized their significance in creating damage at the surface (up to F3) and in impacting aviation operations No comprehensive microburst climatology exists Data from field programs suggest they are a relatively common occurrence – summertime phenomena, most common mid-late afternoon Primary forcing mechanism is negative thermal buoyancy generated by evaporation, melting and sublimation of cloud and precipitation particles Precipitation loading is also important, particularly with wet microbursts Microphysics are very important for the downdraft that quite often descends subsaturated Entrainment can be beneficial or detrimental depending upon where/when it occurs Microbursts events are associated with a continuum of rain rates and are thus subdivided into “wet” and “dry” events
Conclusions, cont.
Dry microbursts occur within deep, dry-adiabatic subcloud layers and originate from innocuous virga shafts associated with altocumulus Formed from negative thermal buoyancy – ice phase is important!
Wet microburst occur within more stable, humid environments and originate from deep cumulonimbus Formed from negative thermal buoyancy and precip loading – again, ice phase is important!
Detection is challenging, they are short lived, low-level, small-scale in nature There are useful radar attributes that can detect their occurrence 2-6 minutes before damaging winds are observed at the surface In weakly sheared environments, soundings can be used to forecast their occurrence.
Downburst indices are problematic, though recent studies have shown they are of some utility in predicting downburst potential and intensity