use of the nondivergent wind for diagnosing banded precipitation systems
DESCRIPTION
Use of the Nondivergent Wind for Diagnosing Banded Precipitation Systems. Thomas J. Galarneau, Jr., and Daniel Keyser Department of Earth and Atmospheric Sciences University at Albany/SUNY Albany, NY 12222. 10th Northeast Regional Operational Workshop - PowerPoint PPT PresentationTRANSCRIPT
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Use of the Nondivergent Wind for Diagnosing Banded Precipitation Systems
Thomas J. Galarneau, Jr., and Daniel KeyserDepartment of Earth and Atmospheric Sciences
University at Albany/SUNY
Albany, NY 12222
10th Northeast Regional Operational WorkshopNOAA/National Weather Service, Albany, NY
6 November 2008
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Background• Mesoscale bands modulate the spatial distribution
and intensity of precipitation associated with cyclones– Cold-season examples include snowbands within coastal
extratropical cyclones– Warm-season examples include coastal fronts within
landfalling and transitioning tropical cyclones
• CSTAR pedigree for mesoscale substructure within cold- and warm-season cyclones affecting the northeastern U.S. (e.g., Novak et al. 2004, 2006; DeLuca 2004; Klein 2007)
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Fig. 3 from Nicosia and Grumm (1999)
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Figs. 4b and 5b from Nicosia and Grumm (1999)
700 hPa Geo. height
700 hPa Frontogenesis
6-h 40-km Meso Eta forecast valid at1800 UTC 4 Feb 1995
Frontogenesis
€
θes
A B
€
EPVg* < 0
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Fig. 2a from Novak et al. (2004)
0000 UTC 6 Feb 2001
WSR-88D Radar Mosaic
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80-km NCEP Eta analysis at 0000 UTC 6 Feb 2001
Figs. 12c,d and 14a,b from Novak et al. (2004)
700 hPa Geo. height750–650 hPa Frontogenesis750–650 hPa Deformation
700 hPa Geo. height750–650 hPa Frontogenesis750–650 hPa Warm-air advection
A
B
A BA B
EPV*
Frontogenesis
RH
€
θes
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Conceptual Models
Single-banded event Nonbanded event
Fig. 15 from Novak et al. (2004)
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Conceptual Models
Single-banded event
Fig. 2 from Novak et al. (2006)
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Motivation• Continuing increases in the horizontal and
vertical resolution of global analyses are resulting in the improved representation of mesoscale circulation systems
• Extend applicability of balanced framework in diagnosing mesoscale circulation systems by replacing the geostrophic wind (Vg) and full wind (V) with the nondivergent wind (Vnd)
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Motivation• Use of Vnd in place of Vg and V in a
balanced framework is hypothesized to produce cleaner and more coherent diagnostic signatures of mesoscale circulation systems
• This hypothesis is addressed here for mesoscale precipitation bands within cold-season cyclones affecting the northeastern U.S.
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1.0GFS
0.5GFS
€
rV g
€
rV g
€
rV nd
€
rV nd
Effect of Resolution Increase
700 hPa h (dam), θ (K), Q (arrows > 2.5 1010 K m1 s1), Q (1014 K m2 s1)
1800 UTC 14 Feb 2007
€
rQ
€
∇•r Q
10
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• Novak et al. (2006, p. 19) discussion of EPV* for the 25 December 2002 snowband case:
• We suggest that in curved flow Vnd better represents the balanced wind than Vg or V
Calculation of EPV*
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• Use of Vnd in EPV* calculation is hypothesized to minimize the spatial extent of EPV* < 0, and the occurrence of localized regions of EPV* << 0 (i.e., EPV* bull’s-eyes)
• This modification to the EPV* calculation may lead to a more accurate assessment of the contribution of CSI to the formation and evolution of mesoscale precipitation bands
Calculation of EPV*
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Goals
• Examine mesoscale precipitation bands for two northeast U.S. cyclones– 14 February 2007– 16 April 2007
• Compare structures shown by diagnostics using Vg, Vnd, and V
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Datasets
• 0.5 NCEP GFS analyses
• NCDC WSR-88D radar archive
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Diagnostics
€
rV =
r V g +
r V ag =
r V nd +
r V ir
€
rV nd = ˆ k ×∇ pψ
€
rV g =
1
fˆ k ×∇ pΦ
nondivergent wind
geostrophic wind
full wind
• Wind definitions
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Diagnostics
• Petterssen frontogenesis
€
E = E st2 + E sh
2( )
1
2
€
E st =∂u
∂x−
∂v
∂y
€
E sh =∂v
∂x+
∂u
∂y
€
d
dt∇ pθ = −
1
2∇ pθ D − E cos δ −α( )[ ]
€
D =∇ p •r
V
angle between isentropes and axes of dilatation
resultant deformation
horizontal divergence
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Diagnostics
• Saturation equivalent potential vorticity
• Q-vectors
– Potential temperature in Q-vector calculation is smoothed by a Gaussian filter (weight of 25)
€
EPV* = −g ζ p + f( )∂θes
∂p+ g
∂v
∂p
∂θes
∂x−
∂u
∂p
∂θes
∂y
⎛
⎝ ⎜
⎞
⎠ ⎟
€
rQ = −
∂r
V
∂x• ∇ pθ, −
∂r V
∂y• ∇ pθ
⎛
⎝ ⎜
⎞
⎠ ⎟
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L
L
L
L
LL
LL
L
12Z
00Z/15
00Z/14
00Z/14
12Z12Z
00Z/13
00Z/12 12Z
12Z
12Z
12Z
12Z
12Z
12Z
00Z/15
00Z/14
12Z
00Z/1400Z/13
00Z/1200Z/15
14 February 2007
Position of key synoptic features marked every 12 h
L primary cyclone; L secondary cyclone upper-level PV anomaly
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Source: http://www.erh.noaa.gov/er/aly/past.htm
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dBZ1200 UTC 1500 UTC
1800 UTC 2100 UTC
NYMA
CT RI
VT
NH
ME
PA
14 February 2007 WSR-88D base reflectivity mosaic
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approximateband position
SLP (hPa), 1000–500 hPa thickness (dam)
€
rV g
€
rV nd
1800 UTC 14 Feb 2007
€
rV
700 hPa h (dam), θ (K), Q (arrows > 2.5 1010 K m1 s1), Q (1014 K m2 s1)
€
rQ
€
∇•r Q
10
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approximateband position
SLP (hPa), 1000–500 hPa thickness (dam)
700 hPa h (dam), 750–650 hPa frontogenesis [K (100 km)1 (3 h)1], 750–650 hPa E (105 s1)
€
rV g
€
rV nd
1800 UTC 14 Feb 2007
€
rV
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Frontogenesis [K (100 km)1 (3 h)1], EPV* (PVU), θes (K)
€
rV g
€
rV nd
1800 UTC 14 Feb 2007
€
rV
RH (%), (103 hPa s1)
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12Z12Z
12Z12Z
12Z
12Z
12Z
12Z
12Z
00Z/12
00Z/17
00Z/1600Z/15
00Z/1400Z/17
00Z/16
00Z/1500Z/14
00Z/13
L
L L
L
L
00Z/17LL
00Z/16
00Z/15
12Z
12Z
12Z
00Z/15
16 April 2007
Position of key synoptic features marked every 12 h
L primary cyclone; L secondary cyclone upper-level PV anomaly
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Source: http://www.erh.noaa.gov/er/aly/past.htm
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Source: http://www.erh.noaa.gov/er/aly/past.htm
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dBZ2100 UTC 0000 UTC
0300 UTC 0600 UTC
NYMA
CT RI
VT
NH
ME
PA
15–16 April 2007 WSR-88D base reflectivity mosaic
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approximateband position
SLP (hPa), 1000–500 hPa thickness (dam)
€
rV g
€
rV nd
0000 UTC 16 Apr 2007
€
rV
700 hPa h (dam), θ (K), Q (arrows > 2.5 1010 K m1 s1), Q (1014 K m2 s1)
€
rQ
€
∇•r Q
10
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SLP (hPa), 1000–500 hPa thickness (dam)
approximateband position
€
rV g
€
rV nd
0000 UTC 16 Apr 2007
€
rV
700 hPa h (dam), 750–650 hPa frontogenesis [K (100 km)1 (3 h)1], 750–650 hPa E (105 s1)
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Frontogenesis [K (100 km)1 (3 h)1], EPV* (PVU), θes (K)
€
rV g
€
rV nd
0000 UTC 16 Apr 2007
€
rV
RH (%), (103 hPa s1)
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Case Summary Schematics
Novak et al. (2004)conceptual model
L
14 Feb 2007
L
16 Apr 2007
StreamlinesDeformationFrontogenesis
Upper-level jet
700 hPa
500 km
N
E
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Concluding Remarks• Increases in horizontal and vertical resolution of
global analyses are leading to the improved representation of mesoscale circulation systems, but also are resulting in noisier diagnostics using Vg
and V
• Use of Vnd in place of Vg and V was hypothesized to produce cleaner and more coherent diagnostic signatures of mesoscale circulation systems
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Concluding Remarks• Use of Vnd in place of Vg and V has been shown to
produce improved signatures of Q divergence, Petterssen frontogenesis, and moist symmetric stability within banded precipitation systems for two cold-season cyclone cases over the northeastern U.S.: 14 February and 16 April 2007
• sd
• Results for these two cases agree with previous work on mesoscale band formation– Deep-layer frontogenesis slopes toward colder air– Band forms on warm-air side of frontogenesis maximum
in presence of weak moist symmetric stability