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A Case Study of the April 18, 2004
Severe Weather Event across Upstate New York
By Michael L. Jurewicz, Sr. and Michael Evans
1. Introduction
A mesoscale convective system (MCS) moved across southern Ontario
during the early morning hours of April 18, 2004 (1200 to 1500 UTC), producing
widespread wind damage. As the MCS progressed eastward from late that morning
into the afternoon (1500 to 1900 UTC), it continued to bring significant wind
damage, as well as large hail, to parts of western and central New York State.
In fact, wind gusts of 80 to 100 mph were recorded in the Niagara Falls area
and an F0 tornado touched down in the Finger Lakes region in Cayuga county. By
late afternoon, the convection began to weaken over the Catskill Mountains.
An interesting aspect of this event was that the MCS propagated through
environments characterized by relatively cool, stable boundary layer conditions
during the majority of its life cycle. Normally, lower-level stability does
not promote the downward transfer of strong winds to the surface. Thus, the
magnitude of the winds observed on this day over such a large area and
prolonged time period becomes particularly noteworthy.
In this study, we’ll track the MCS from its inception during the
evening of April 17th over the Upper Midwest to its eventual demise
over eastern New York State late in the afternoon on the 18th.
Synoptic and mesoscale settings will be examined during this period, with an
emphasis on factors that likely contributed to convective initiation,
intensification, or weakening. Also, some theories will be proposed on how
downdraft intensity was able to be maintained despite marginal, and even
unfavorable at times, lower-level conditions. Radar perspectives are given
from both the Buffalo, NY (KBUF) and Binghamton, NY (KBGM) WSR-88D’s, once the
convection reached New York State. Lastly, a summary is presented.
2. Synoptic Overview
Late in the afternoon on April 17th, a warm front at the
surface stretched eastward from a deepening low pressure system in Colorado
across the central Plains (Fig. 1). However, there was little or no convective
development across the region at this time. Note the cool, dry air mass in
place across the Dakotas and Minnesota (surface dew points mostly in the 20s and
30s F). Meanwhile, in the warm sector, a strong southerly flow was advecting
higher theta-e air (surface dew points into the 60s F) northward from Oklahoma
and eastern Kansas towards the vicinity of the warm frontal boundary across
southern Nebraska and Iowa. A tightening temperature and moisture gradient
seemed to be developing along and just north of the warm front.
By 0000 UTC on the 18th, an increasingly favorable
environment for convective initiation was developing across portions of Iowa
and Minnesota. At 300 mb (Fig. 2a), the main jet axis extended from the base
of an amplified trough over the southwestern United States across parts of the
Rockies and northern Plains, then eventually into southern Canada. Embedded
within this jet core was a 100+ kt speed maximum over southern Ontario. Iowa
and Minnesota were located underneath the right-entrance region of the
aforementioned jet streak at this time. At mid-levels, the atmosphere was
destabilizing. Iowa and southern Minnesota were located along the southern
edge of the stronger westerlies at 500 mb (Fig. 2b). Short-wave energy within
this belt of more pronounced flow was flattening the large-scale ridge axis and
resulting in height falls and cooling at this level. Meanwhile, at 700 mb (Fig. 2c),
a trough extended from the Dakotas southeastward across southern Minnesota
and into Iowa. A tight thermal gradient and strong warm advection were
associated with this trough. At 850 mb (Fig. 2d), the key feature was a west
to east oriented warm front, that stretched across Nebraska, northern Iowa, and
northern Illinois. A 30-40 kt low-level jet was transporting higher theta-e
air northward and over the warm frontal boundary itself (see the axis of
10-12ºC dew points near the Iowa/Minnesota border). An initialized Eta
horizontal cross-section (Fig. 3) of divergence, omega, and wind from 0000 UTC
on the 18th, showed a particularly deep layer of ascent across
northern Iowa and southern Minnesota. The lift in this area appeared to result
from a pronounced convergence/divergence couplet. Strong low-level convergence
was noted below 800 mb; likely a result of close proximity to both the surface
warm front and nose of the low-level jet. Mid-level divergence was also seen;
likely a result of being located on the tail end of a 60-70 kt jet streak at
500 mb.
As judged from radar, satellite, and lightning analyses, thunderstorms
first developed between 0030 and 0100 UTC on the 18th near the
Iowa/Minnesota border (Fig. 4). During the evening, convection slowly
organized as it pushed eastward from northern Iowa and southern Minnesota
across Wisconsin and Lake Michigan (Fig. 5). Between 0100 and 0600 UTC,
thunderstorms became locally severe. Severe reports primarily consisted of
large hail during this period (Fig. 6). The comparatively small number of wind
reports versus large hail suggested that most of the storms were not
surface-based. Regional stability profiles from that evening implied that most
of the convection was indeed elevated in nature (Fig. 7 and Fig. 8). Another
horizontal cross-section (using RUC data this time, Fig. 9), from 0600 UTC on
the 18th, continued to show a deep layer of upward vertical motion
collocated with the developing MCS over Wisconsin. Through 0600 UTC on the 18th,
it is apparent that the combination of large-scale lift, steep mid-level lapse
rates (Figs. 10a and 10b),
and pronounced shear north of the surface warm front
was able to maintain convective development and organization, despite the
presence of low-level stability. It is also evident, however, that stable
boundary layer conditions effectively prevented strong winds from mixing all
the way down to the surface within multi-cell or isolated supercellular
clusters.
From 0600 to 1100 UTC, the MCS moved steadily eastward across Lake
Michigan and Lower Michigan. However, very little severe weather was reported
during this period (refer back to Fig. 6). This was an indication that strong
winds were still not able to penetrate through to the surface. Note the
relatively cool, stable lower-level conditions that the MCS encountered over Lower
Michigan during the pre-dawn hours on the 18th (Figs. 11a
and 11b).
However, between 1100 and 1200 UTC, more organized linear structures began to
develop on radar across eastern Lower Michigan and southern Lake Huron, with a
corresponding increase in lightning activity and cooling trend in cloud top
temperatures (Fig. 12 Fig. 13).
It was also during this period that reports of
wind damage started to become more prevalent. In fact, a wind gust of 70 mph
was recorded near Michigan’s shoreline with southern Lake Huron just after 1100
UTC.
An inspection of the synoptic-scale environment at 1200 UTC on the 18th
showed that the MCS continued to benefit from large-scale forcing. The upper-level
flow became strongly diffluent (Fig. 14a). The atmosphere also continued to
undergo destabilization at mid-levels, just ahead of the MCS. An approaching
500 mb short-wave trough, moving along the southern fringe of the stronger
westerlies, resulted in modest height falls and cooling at that level
(Fig. 14b and Fig. 15).
Meanwhile, pronounced warm advection was taking place over the
eastern Great Lakes region in the 850-700 mb layer
(Fig. 14c and 14d).
Close proximity to the nose of the 850 mb jet also supplied an influx of
higher theta-e air and promoted strong low-level convergence.
As the MCS continued eastward into and across southern Ontario between
1200 and 1500 UTC, strong winds became the primary severe threat and reports of
wind damage were widespread. As mentioned before, though, little in the way of
strong surface winds was associated with the MCS prior to around 1100 UTC. A
common theme during the overnight period (from 0100 to 1100 UTC on the 18th)
was that the MCS encountered relatively cool, stable boundary layer
environments from northern Iowa all the way across the majority of Lower
Michigan. The authors earlier theorized that the lack of strong winds resulted
from their inability to penetrate the stable surface-based layer and mix down
to ground level. Given a similar lower-level environment over eastern Lower
Michigan and near Lake Huron around daybreak (surface temperatures generally
between 50 and 55F), as compared to areas upstream during the overnight period,
why the sudden development of strong, damaging winds with this convective
system?
A possible key to answering the above question lies with the evolution
of the mid-level environment along the track of the MCS. Let’s take a look
back at Figs. 7a and 7b. The initial-hour RUC sounding at this time (0300 UTC)
showed that the MCS was encountering an environment characterized by fairly
moist mid-levels and dry lower-levels. Although this "inverted-V" type
signature can provide a favorable situation for microbursts, the lack of strong
wind reports in the vicinity indicated that, in this particular case,
downdrafts were generally not strong enough to reach the surface. The boundary
layer air was likely too cool and the mid-level air not dry enough to enhance
any potential downdrafts. Now let’s view Figs. 8a and 8b once again. As
compared to 0300 UTC, the environment at this juncture (0600 UTC) near the MCS
featured cooler, moister lower-levels and slightly drier mid-levels. Although
mid-level lapse rates were steepening with time, the degree of mid-level drying
still seemed insufficient to significantly enhance downdraft speeds. Given the
added detractor of pronounced low-level stability, the atmosphere was not
conducive to downward momentum transfer. By 0900 UTC over central Lower
Michigan (Figs. 11a and 11b), as compared to 3 hours earlier, more earnest
mid-level drying had developed. Dew point depressions had increased from about
10oC to 13o-14oC in the 600-700 mb layer. However, no severe weather was
occurring near this time, thus indicative of the fact that any downdrafts were
still not forceful enough to punch through the surface-based stable zone. A
subjective analysis of the initial-hour RUC sounding (Fig. 11b), using about
650 mb as the level of downdraft origination and minimum wet-bulb potential
temperature, showed that the parcel trajectory (following the moist adiabat
downward) would ultimately meet the environmental temperature line near the
surface. Such an occurrence would presumably diminish fall speeds as the parcel
neared ground level. This reinforces the above notion that mid-level drying,
to this point, was still not enough to completely overcome the strength of the
low-level inversion, despite increasing Downward Convective Available Potential
Energy (DCAPE) aloft. Now let’s peruse the 1200 UTC sounding (Fig. 16) from Detroit,
MI (KDTX). KDTX was just southwest of where the MCS was located at about 1200
UTC (refer to Fig. 13). Although a shallow inversion/zone of stability
remained below 900 mb, it is evident that the process of mid-level drying we
began to see over Lower Michigan about 0900 UTC had further intensified in the
last 3 hours. Dew point depressions in the 600-700 mb layer had now increased
to about 17o-18oC. Utilizing a similar analysis to the one we employed on Fig. 11b,
it now appeared that the added mid-level drying would produce enough DCAPE
to potentially bring any downdrafts all the way down to ground level, despite
lingering cool surface temperatures. Not coincidentally, perhaps, reports of
strong surface winds/wind damage started to increase in frequency just prior to
the time the KDTX sounding was taken.
As judged from the 0900 UTC RUC and 1200 UTC DTX soundings
(Fig. 11b and Fig. 16),
the main thrust of mid-level dry advection occurred around 650 mb.
Using initial-hour model data from the RUC and a series of satellite/radar
images (not shown) between 0300 and 1200 UTC on the 18th, the
movement/development of the mid-level dry punch was compared to the track of
the MCS (Fig. 17a and Fig. 17d).
For much of the night, the main supply of dry
mid-level air and the MCS were well separated. However, the prevailing
southwesterly flow advected the dry air aloft from the Ohio Valley into Lower
Michigan during the pre-dawn hours. By 1200 UTC, a layer of well mixed, very
dry air at mid-levels had crossed directly into the path of the MCS. The
timing of this interaction seems to further substantiate its potential role in
facilitating the downward transfer of strong winds.
As briefly discussed earlier, once the evolution towards linear
development had taken place, an organized squall line produced a swath of wind
damage from extreme eastern Lower Michigan through southern Ontario between
1100 and 1500 UTC. Some of the recent research on quasi-linear convective
systems (QLCS) has focused on the relationship between low-level vertical shear
and cold pool maintenance. Such findings suggest that shear magnitudes of
30-40 kt or more in the lowest 2-5 km tend to produce the longest lived squall
lines, with deeper, more erect meso-vortices embedded within them (Trapp and
Weisman, 2003). For this event, by 1500 UTC, hourly meso-analyses from the
Storm Prediction Center (SPC) showed 0-1 km shear values of 25+ kt (Fig. 18a)
extending from southern Ontario towards the Niagara Peninsula of
western New York State. Meanwhile, deeper-layered shear exceeded 50 kt over
the same area (Fig. 18b). In light of the above cited study, such observed
shear magnitudes appeared to be more than sufficient to maintain the integrity
of any linear convective elements and associated smaller scale vortices.
Fairly long-lived squall lines did, in fact, prevail on this day. The
earlier described swath of severe weather over southern Ontario continued
downstream. Strong winds, wind damage, and/or large hail affected numerous
locations across western and central New York State well into the
afternoon (Fig. 19). We’ll look at some of the mesoscale aspects of this event
and give a closer radar perspective in the next section.
3. Brief Mesoscale Description and WSR-88D Perspective
The leading edge of the gust front associated with the main squall line
crossed into western New York over Niagara county around 1500 UTC. It was near
this time that the convective system, perhaps, reached its peak intensity.
Low-level velocity returns of greater than 60 kt were observed from the KBUF
WSR-88D (Fig. 20). As stated in the introduction, very strong surface winds
were experienced throughout this area. Officially, a wind gust of over 90 mph
occurred at the Niagara Airport. A small sampling of some of the damage
inflicted is shown in Fig. 21.
As discussed near the end of section 2, the strong vertical shear in
place seemed to be an important contributor in maintaining the gust front intensity
over an extended time period. Another factor may have played a supporting
role, as well. Mesoscale surface analyses at 1600 UTC (Fig. 22) showed the
development of an inverted trough, which extended from near Buffalo, NY (KBUF)
eastward to just south of Syracuse, NY (KSYR) and Utica, NY (KUCA). Such a
trough is frequently observed in easterly or southeasterly flow situations
across western and central New York State. This troughing is likely a result
of downslope flow coming off the Allegheny Plateau and on to the comparatively
flat terrain south of Lake Ontario. Since the track of the MCS across New York
State was essentially normal to the orientation of the trough axis, it is
possible that the convergence/surface vorticity associated with the trough
could have enhanced the lift near the leading edge of the gust front.
Occurrences of severe weather continued to be associated with the MCS
until just past 1800 UTC (refer back to Fig. 19). The most significant damage
within this specific time period occurred over Cayuga county in central New
York, where storm surveys later revealed that an F0 tornado briefly touched
down. Some radar images from the KBGM WSR-88D are displayed close to the time
of tornado development and associated damage photos are also shown
(Fig. 23 and Fig. 24).
At last, between 1800 and 2100 UTC on the 18th, convection
began to wane in intensity as it approached the Catskill Mountains in eastern
New York State. By this time, shear magnitudes had started to decrease. An
initial-hour RUC sounding (Fig. 25) at 1900 UTC, just ahead of the convective
system, showed a remaining presence of dry air in the mid-levels, to
potentially enhance downdraft strength. However, this sounding also showed
that 0-1 km shear values had weakened to 10-15 kt, while the deeper-layered
shear (0-6 km) was down to about 40 kt. Compare these values to those observed
just a few hours earlier
(Fig. 18a and Fig. 18b).
Afterwards, no additional severe weather occurred and thunderstorms continued to weaken.
4. Summary
An MCS first began to form near the Iowa/Minnesota border during the
evening of April 17, 2004. Due to favorable large-scale support, the
convective system gradually organized itself during the night as it pushed
eastward across the Great Lakes region. Storms were locally severe during the
overnight period, but severe reports consisted primarily of large hail. The
authors contend that this was due to the elevated nature of the thunderstorms,
given the track of the MCS north of a surface warm front and within a
relatively cool, stable lower-level environment.
Just before daybreak on April 18th, a sudden increase in the
frequency of strong winds/severe wind reports occurred, despite the continued presence
of lower-level stability. The authors theorized that the interaction between
the MCS and a pronounced mid-level dry punch facilitated the downward transfer
of strong winds to the surface. Increased DCAPE associated with the dry
mid-level air was finally able to overcome the surface-based inversion and
bring downdrafts to ground level. Thereafter, a swath of wind damage occurred
from extreme eastern Lower Michigan across southern Ontario, and then through
western and central New York during the morning and early afternoon hours of
the 18th. Once the squall line/gust front became established, a
favorable cold pool/shear relationship existed to increase the longevity of the
system, given the strong low-level vertical shear in place.
Once the MCS reached western and central New York, the mesoscale
environment may have further enhanced the strength of the squall line. A west
to east oriented surface trough developed on the morning of the 18th
across upstate New York. Since the track of the MCS was nearly normal to the
orientation of the trough, extra low-level convergence and surface vorticity
may have enhanced lifting at the leading edge of the convective line/gust
front.
By late afternoon on the 18th, once shear profiles and
synoptic scale uplift decreased, convection began to weaken across eastern New
York State.
5. FIGURES
Figure 1. Visible satellite image at 2100 UTC, April 17th.
Surface frontal analysis is in green, MSLP analysis is in tan, and the surface
observations are in blue. <<<back>>>
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Figure 2a. 300 mb analysis at 0000 UTC, April 18th. <<<back>>>
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Figure 2b. 500 mb analysis at 0000 UTC, April 18th. <<<back>>>
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Figure 2c. 700 mb analysis at 0000 UTC, April 18th. <<<back>>>
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Figure 2d. 850 mb analysis at 0000 UTC, April 18th. <<<back>>>
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Figure 3. Eta initialized cross-section at 0000 UTC, April 18th.
The horizontal axis (x-axis) is drawn from eastern Kansas to northern
Wisconsin. Solid blue contours represent units of divergence and dashed blue
contours represent units of convergence. Wind barbs are depicted in green.
Omega is shaded, with warm colors showing ascent and cool colors showing
descent. <<<back>>>
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Figure 4. IR satellite image from 0045 UTC, April 18th.
Surface frontal analysis is in tan, MSLP analysis is in blue, and surface
observations are in yellow. Positive cloud-to-ground lightning strokes are
depicted with green pluses (+) and negative cloud-to-ground lightning strokes
are depicted with orange minuses (-). <<<back>>>
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Figure 5. CONUS-scale composite WSR-88D imagery (2 km resolution) at 0600 UTC, April 18th. <<<back>>>
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Figure 6. Summary of severe weather reports from 1200 UTC, April 17th until 1200 UTC, April 18th. <<<back>>>
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Figure 7a. IR satellite image at 0315 UTC, April 18th.
Surface frontal analysis is in tan. Surface-based lifted indices are in yellow
(positive values are shown with solid contours and negative values are shown
with dashed contours). Positive cloud-to-ground lightning strokes are depicted
by orange pluses (+). Negative cloud-to-ground lightning strokes are depicted
by light blue minuses (-). <<<back>>>
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Figure 7b. RUC initial-hour point sounding (using point A (labeled in
black) from Fig. 7a) at 0300 UTC on April 18th. <<<back>>>
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Figure 8a. IR satellite image at 0600 UTC, April 18th.
Surface frontal analysis is in tan. Surface-based lifted indices are in yellow
(positive values are shown with solid contours and negative values are shown
with dashed contours). Positive cloud-to-ground lightning strokes are depicted
by orange pluses (+). Negative cloud-to-ground lightning strokes are depicted
by light blue minuses (-). <<<back>>>
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Figure 8b. RUC initial-hour point sounding (using point A (labeled in
black) from Fig. 8a) at 0600 UTC on April 18th. <<<back>>>
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Figure 9. RUC initialized cross-section at 0600 UTC, April 18th.
The horizontal axis (x-axis) is drawn from northern Missouri to Lake Superior.
Solid blue contours represent units of divergence and dashed blue contours
represent units of convergence. Wind barbs are depicted in green. Omega is
shaded, with warm colors showing ascent and cool colors showing descent. <<<back>>>
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Figure 10a. RUC initial-hour 700-500 mb lapse rates at 0600 UTC, April
18th. Fig. 10b depicts these steep lapse rates persisting
downstream along the path of the MCS. <<<back>>>
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Figure 10b. SPC hourly meso-analysis of 700-500 mb lapse rates at 1800
UTC, April 18th. <<<back>>>
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Figure 11a. IR satellite image at 0915 UTC, April 18th.
Surface frontal analysis is in tan. Surface observations are in blue.
Positive cloud-to-ground lightning strokes are depicted by green pluses (+).
Negative cloud-to-ground lightning strokes are depicted by orange minuses (-). <<<back>>>
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Figure 11b. RUC initial-hour point sounding (using point A (labeled with
a green star in the upper left of the figure, and by a black dot in Fig. 11a)
at 0900 UTC on April 18th. <<<back>>>
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Figure 12. CONUS-scale composite WSR-88D imagery (2 km resolution) at 1200 UTC, April 18th.
<<<back>>>
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Figure 13. Visible satellite image at 1215 UTC, April 18th.
Surface frontal analysis is in tan and the surface observations are in blue.
Positive cloud-to-ground lightning strokes are depicted by green pluses (+).
Negative cloud-to-ground lightning strokes are depicted by orange minuses (-). <<<back>>>
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Figure 14a. 300 mb analysis at 1200 UTC, April 18th. <<<back>>>
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Figure 14b. 500 mb analysis at 1200 UTC, April 18th. <<<back>>>
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Figure 14c. 700 mb analysis at 1200 UTC, April 18th. <<<back>>>
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Figure 14d. 850 mb analysis at 1200 UTC, April 18th. <<<back>>>
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Figure 15. Water vapor imagery at 1215 UTC, April 18th.
Solid orange contours represent units of initialized vorticity from the 1200
UTC, 18 April run of the Eta model. <<<back>>>
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Figure 16. Observed sounding from Detroit, MI (KDTX) at 1200 UTC on
April 18th. <<<back>>>
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Figure 17a. Initial-hour RUC relative humidity (RH) values (shaded) at
650 mb from 0300 UTC, April 18th. Warm colors represent dry air (RH
values of generally 30% or less) and cool colors represent moist air (RH values
of generally 60% or greater). Radar, satellite, and lightning analyses (not
shown here) were used to depict the position of the MCS at this time. <<<back>>>
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Figure 17b. Initial-hour RUC RH values (shaded) at 650 mb from 0600
UTC, April 18th. Warm colors represent dry air (RH values of
generally 30% or less) and cool colors represent moist air (RH values of
generally 60% or greater). Radar, satellite, and lightning analyses (not shown
here) were used to depict the position of the MCS at this time. <<<back>>>
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Figure 17c. Initial-hour RUC RH values (shaded) at 650 mb from 0900
UTC, April 18th. Warm colors represent dry air (RH values of
generally 30% or less) and cool colors represent moist air (RH values of
generally 60% or greater). Radar, satellite, and lightning analyses (not shown
here) were used to depict the position of the MCS at this time. <<<back>>>
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Figure 17d. Initial-hour RUC RH values (shaded) at 650 mb from 1200
UTC, April 18th. Warm colors represent dry air (RH values of
generally 30% or less) and cool colors represent moist air (RH values of
generally 60% or greater). Radar, satellite, and lightning analyses (not shown
here) were used to depict the position of the MCS at this time. <<<back>>>
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Figure 18a. SPC hourly meso-analysis of 0-1 km shear vectors at 1500
UTC, April 18th. <<<back>>>
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Figure 18b. SPC hourly meso-analysis of 0-6 km shear vectors at 1500 UTC, April 18th. <<<back>>>
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Figure 19a. Summary of severe weather reports from 1200 UTC, April 18th
until 1200 UTC, April 19th. <<<back>>>
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Figure 19b. Zoomed-in severe weather summary across southern Ontario
and New York State from 1200 to 1800 UTC on April 18th. <<<back>>>
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Figure 20a. A 0.5o base reflectivity image from the KBUF WSR-88D just
prior to 1500 UTC, April 18th. <<<back>>>
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Figure 20b. A 0.5o base velocity image from the KBUF WSR-88D just prior
to 1500 UTC, April 18th. <<<back>>>
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Figure 21. Damage photos from Niagara county, NY on April 18th. <<<back>>>
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Figure 22. Visible satellite imagery from 1600 UTC, April 18th.
Surface frontal analysis is in tan, MSLP analysis is in yellow, and surface
observations are in blue. Positive cloud-to-ground lightning strokes are
depicted by green pluses (+) and negative cloud-to-ground lightning strokes are
depicted by orange minuses (-). <<<back>>>
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Figure 23a. A 0.5o base reflectivity image from the KBGM WSR-88D just
before 1700 UTC on April 18th. <<<back>>>
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Figure 23b. A 0.5o storm relative motion (SRM) image is displayed from
the KBGM WSR-88D just before 1700 UTC on April 18th. <<<back>>>
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Figure 24. Damage photos from Cayuga county, NY on April 18th. <<<back>>>
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Figure 25. RUC initial-hour point sounding over central New York (just
northeast of BGM) at 1900 UTC on April 18th. <<<back>>>
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