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![Page 1: Yanjun Jiao and Colin Jones University of Quebec at Montreal September 20, 2006 The Performance of the Canadian Regional Climate Model in the Pacific Ocean.](https://reader035.fdocuments.in/reader035/viewer/2022070400/56649f135503460f94c26f81/html5/thumbnails/1.jpg)
Yanjun Jiao and Colin Jones
University of Quebec at Montreal
September 20, 2006
The Performance of the Canadian Regional Climate Model in the Pacific Ocean
![Page 2: Yanjun Jiao and Colin Jones University of Quebec at Montreal September 20, 2006 The Performance of the Canadian Regional Climate Model in the Pacific Ocean.](https://reader035.fdocuments.in/reader035/viewer/2022070400/56649f135503460f94c26f81/html5/thumbnails/2.jpg)
OUTLINE:
1. Experiment configurations
2. Results from original CRCM (precipitation, cloud and relative humidity)
3. Modification to the CRCM model physics
4. Results of CRCMM
5. Summary
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CRCM4 domain in cylindrical projection
CRCM4 domain in PS projection
180km (60ºN) resolution
11575 grid points
29 Gal-Chen levels
15-min time step
Output every 3hrs
1. Experiment configurations
Sponge zone (9 grid points)
GPCI 2D domain (5ºS-45ºN,160ºE-120ºW)
GPCI cross-section (13 points)
ISCCP cloud cover (JJA 1998)
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CRCM4
0.25º TRMMStratiform precipitation
Convective precipitation
Total precipitation
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ISCCP
CRCM4Total cloud
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Siebesma et al. (2004)
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![Page 8: Yanjun Jiao and Colin Jones University of Quebec at Montreal September 20, 2006 The Performance of the Canadian Regional Climate Model in the Pacific Ocean.](https://reader035.fdocuments.in/reader035/viewer/2022070400/56649f135503460f94c26f81/html5/thumbnails/8.jpg)
1) The eddy diffusivities calculation of the ECMWF.
2) A switch to turn off the shallow convection.
3) The trigger function of shallow convection (DTRH).
4) The cloud base mass flux closure=f (w*).
5) Variable cloud radius of the deep convection=f(wLCL).
6) Variable minimum cloud-depth=f(TLCL).
7) A dilute updraft ascent.
8) Xu-Randall cloud scheme.
9) Evaporation of falling large scale precipitation.
3. Modification to the model physics of CRCM4
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zpbl
0.1zpbl
buofxs < 0 buofxs > 0
3.1 Modification to vertical diffusion
(ECMWF documentation CY28r1)
Revised Louis scheme
KM lM2 U
zfM (Ri)
K H lH2 U
zf H (Ri)
fM (Ri) 1
110Ri(1 Ri) 1 2
f H (Ri) 1
110Ri(1 Ri)1 2
M ( ) (1 16 ) 1 4
H ( ) (1 16 ) 1 2
KM lM
2
M2
U
z
K H lM2
MH
U
z
KM kzwturb (1z
zi
)2
K H kzwturb (1 z
zi
)2 M
H
wturb (u*3 0.6w*
3)1
3
K H CentrQov
z
v
(v )k1 2 1
Cpd
(sk sk1 0.5( )(qk qk1)(sk sk1)
KM kzu(1z
zi
)2 1
M
K H kzu(1 zzi
)2 1H
Troen and Mahrt (1986)
• Non-local diffusion when eddies have a similar size as the PBL
• Explicit entrainment parameterization in the PBL top
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(vmix v
env )Tv
Tv
RH
0 Tv
0.2 (P
P0
)Rd
C pd
2) The trigger function of shallow convection
1) A switch to turn off the shallow convection once deep convection has been detected on the same grid point
3.2 Modification to shallow convection (BKF)
TvRH
0.20(RHLCL 0.70)q mix /qs
t0.70 RHLCL 0.90
(1.0 /RHLCL 1.0)q mix /qs
tRHLCL 0.90
Mb 0.03w
w*gzb
v
(w''v )s
13
3) The closure of cloud base mass flux (Grant 2001 and Neggers et al. 2004)
free convective vertical velocity scale
-0.01
0
0.01
0.02
0.03
0.04
0.05
0.06
0.5 0.6 0.7 0.8 0.9 1 1.1
Relative Humidity
DTR
H
CAPE adjustment closure: mass flux at cloud base is totally controlled by the conditions in the cloud layer
Mb f (CAPE)
Subcloud convective velocity scaling closure: links the mass flux at cloud base to the TKE in subcloud layer.
Based on the observation that shallow cumulus clouds (visible part because of condensation) often root deeply into the subcloud mixed layer (invisible dry thermal)
CTL
LCL
wDeep convection is driven by latent heat release in the convective cloud
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Cdepth 3500
Cdepth 2000 TLCL 0C
2000100TLCL 0 TLCL 20C
4000 TLCL 20C
Rmin 1500
Rmin 1000 WLCL 0
1000(1 0.1WLCL ) 0 WLCL 1.0
2000 WLCL 1.0
2) The minimum cloud-depth threshold has been parameterized according to the cloud-base temperature rather than remaining constant.
1) Cloud radius of the deep convection vary with the vertical velocity at lifting condensation level (LCL)
3.3 Modification to deep convection
Kain (2004)
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3) A dilute updraft ascent has been used to calculate CAPE, which provides a more accurate calculation in convection rainfall and mass flux
3.3 Modification to deep convection
(e )lup
(e )l1env
(e )l1up
pumf l1
puerl1
pudrl1
pumf l
(e )lenv
l 1
l
(e )l1up (e )l
up (e )LCLup
(e )l1up (e )l1
env (1 )(e )lup
puerl1 (pumf l pudrl1 puerl1)
Equivalent potential temperature in undilute updraft (produces a significant larger CAPE than actual one)
Equivalent potential temperature in dilute updraft
• Reduces the CAPE value in highly unstable regimes (especially for dry condition)
• Reduces the precipitation and the degree of stabilization
CAPE g eup
eenv 1
LCL
ETL dz
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CLS RH p 1 exp( q l
[(1 RH)qsat ] )
, if RH 1
1.0, if RH 1
3.4 Modification to cloud scheme
Xu and Randall (1996)
where p 0.25 100. 0.49
q l is cloud liquid water
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3.5 Modification to large scale precipitation
(evaporation of falling precipitation from ECMWF)
E prec 5.44 10 4 (1. cld)(1. RH)qsat (p
ps
)1 2 Pl1
5.910 3
0.577
Kessler (1969)
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CRCM4
CRCMM
0.25º TRMM
JJA 1998 precipitation over GPCI 2D domain
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CRCM4
CRCMM
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ISCCP
CRCMM
CRCM4
JJA 1998 total cloud over GPCI 2D domain
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CRCMM
CRCM4
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Vertical profile of the relative humidity
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Siebesma et al. (2004)
Vertical profile of the cloud cover
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Vertical profile of vertical velocity (Pa/s)
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Thanks to the GPCI, some deficiencies in the CRCM4 have been found.
The CRCMM is better than CRCM4 in the field of:
1) Precipitation
2) Total cloud cover (shallow cumulus region).
3) Vertical profiles of relative humidity, cloud and vertical velocity.
4) Still have some space to improve in convective precipitation (too strong), PBL (too moist and sharp), and LWP (too low in stratocumulus region) ……
•Testing the sensitivities to horizontal and vertical resolutions
(180km ~ 90km ~ 45km and L29 ~ L47)
• Testing over the North America (AMNO domain)
(CLASS, winter and summer)
5. Summary
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