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ACRE Downscaling: 20C Reanalysis Application for Paleoclimate tracer simulations. Dyn . Downscaling with 20C-Rean 20C Isotope Reanalysis Kei Yoshimura. 20 th century Reanalysis (Compo et al., 2011). 1 December 1918 . Using only surface pressure data historically recorded since 1870’s - PowerPoint PPT Presentation
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ACRE Downscaling: 20C Reanalysis Application for Paleoclimate
tracer simulations
1. Dyn. Downscaling with 20C-Rean2. 20C Isotope Reanalysis
Kei Yoshimura
20th century Reanalysis (Compo et al., 2011)
• Using only surface pressure data historically recorded since 1870’s
• Ensemble Kalman Filter for data assimilation (56 member)
• T62L28 GFS with NOAH LSM
• Reanalysis skill is comparable to current Day-3 forecast skill (Whitaker et al., 2009)
• Ensemble Mean (EM) fields are publically available.
Whitaker et al. (2009)
1 December 1918
SLP 500 hPa GPH
Question for Dynamical Downscaling
Are the ensemble mean fields appropriate as lateral
boundary conditions for dynamical downscaling?
ORIG EM19
C20
CDi
ffNO!
Global Dynamical Downscaling
Transient component of moisture divergence is smoothed out in Ensemble mean
Tota
l div
erge
nce
Mea
nTr
ansie
nt19C 20C
No di/convergence
uq
uq
qu
Straight forward remedy: Downscale a single member many times
and making an average of them.
Is there any other way to reduce computation?
Modification of single member by ensemble mean increment
• where F is full field of physical variable, n is an ensemble member, bar indicates ensemble mean, and <> indicates running mean (e.g. one-month).
• The downscaling will be performed using Fnnew as a lateral boundary forcing.
Time
Single member forecast Fn
Other members
Monthly running mean of a single member <Fn>
Monthly running mean of all members <Fbar>
incrementCorrected member
nnnewn FFFF
Specification of experiments• Atmospheric Forcing: 20thC Reanalysis (Compo et al., 2011)
– Also regarded as “truth”.• Experiments: Different by the atmospheric forcings.
– EM: Ensemble mean is used.– S1: Arbitrary chosen single member (run01) is used. – S3: Mean of the runs in which arbitrary chosen three single members
(run01, run11, & run21) are used.– S6: Similar to S3, but 6 single members (S3 + run31, run41, & run51) are
used. – MS: Modified single member is used.
• Periods: – 1871-2008 for EM and MS.– 1871-1873 and 1981-1983 for S1-S6.
• Model: IsoGSM with global spectral nudging (Yoshimura et al., 2008)
Seasonal mean precipitation with MS fieldORIG MS
19C
20C
Diff
DJF mean of moisture divergence in MSTo
tal d
iver
genc
eM
ean
Tran
sient
19C 20C
Appropriate di/convergence
RMSD in 500Z against “truth” 19C 20C
Glob
eN
HSH
RMSD in Precipitation against “truth”19C 20C
Glob
eN
HSH
RMSD in Wind against “truth”19C 20C
Glob
eN
HSH
Figure 10: Global mean precipitation by each experiments from 1871 to 2008. Original 20th century Reanalysis (green), EM (black), and MS (blue) are shown for all period. Those runs with the direct use of single members (which consists S6) are shown only for 1871-73 and 1981-83.
Long term global precipitation
EM
MS
Summary of Part 1• Use of ensemble mean field as atmospheric forcings for
downscaling study makes big shortcomings, particularly too small precipitation, when the spread of ensemble members is large.
• Downscaling of each single ensemble member is straightforward, but requires lots of resources and time.
• To avoid these problems, we propose a new method which modifies a single member field to have the same monthly skills as ensemble mean field (MS method) .
• Use of the MS method clearly improves skill than direct usage of a single member. About the same skill as when 3 members are directly used.
2. 20C Isotope Reanalysis
VSurface vapor d18O anomaly at 116W 34.5N
-2
-1.5
-1
-0.5
0
0.5
1
1.5
2
1979 1984 1989 1994 1999 2004
anom
aly d18O
s1f23yr running mean (f2)3yr running mean (s1)
Bristlecone pine tree at SE CA
nudged
free
Yoshimura et al., 2008
Oceanic sediment d18O (millions yBP)Icesheet cores d18O ・ dD (~800 kyBP)Icecap cores d18O ・ dD (~20 kyBP)Speleothem d18O (~2000 yBP)Treering d18O (~1000 yBP)Coral d18O (~400 yBP)
Impact Analysis (a.k.a., forward proxy modeling)
Model WorldReal World
Ice Coreδ18O
Temperature
Precipitation
Circulation
Source
Snow/Glacier
Etc.Etc.
The impact from each component is not quantifiable.
Ice Coreδ18O
Temperature
Precipitation
Circulation
Source
Snow/Glacier
Etc.Etc.
The impact from each component is explicitly quantifiable.
Uncertainty of the impacts is quantifiable by reproducibility.
Why 20C Isotope Reanalysis?
Isotopes in GCM/RCM
• Incorporate water isotopes as passive tracers in GCMs/RCMs. Whenever water phase change takes place, isotopic water (HDO, H2
18O) behave differently to ordinary water (H2O).
Risi et al. 2008Courtesy of JMA
H18OH
HD16O
Typical convective precipitation process
Number of GNIP sites where correlation is significant for 1980-1999
ECHAM GISS-E IsoGSM-R2 IsoGSM-20C
CorrelationNH (210) 147 171 (81%) 174 (83%) 171 (81%)
Tropics (142) 68 82 (58%) 96 (68%) 105 (73%)SH (37) 22 (60%) 18 25 (68%) 25 (67%)
Anomaly Correlation
NH (146) 13 (9%) 12 114 (78%) 93 (63%)Tropics (67) 9 12 (18%) 32 (48%) 34 (50%)
SH (29) 1 3 (10%) 12 (41%) 12 (41%)
GoodBad GoodBad
Comparison with GNIP data
Treering δ18O in Cambodia
Larger amplitude?
Wrong phase?@Kirirom national park
Courtesy of M. Zhu and L. Stott
Courtesy of L. Stott
Treering δ18O in West US
Seawater δ18O from Coral and Model near Philippines
R= 0.54
R= 0.55
δ18Osw (Red: Model Blue: Coral)
SSS (Red: Model Blue: SODA)
Kojima et al., submitted
1860 1880 1900 1920 1940 1960 1980 2000 20200.1
0.150.2
0.250.3
0.350.4
0.45
-0.100.10.20.30.40.50.60.7
IsoGSM2 IsoGSM1 coral
Bunaken (2N 125E)
Cora
l δ18
Osw
(‰)
Mod
eled
δ18
Osw
(‰)
1860 1880 1900 1920 1940 1960 1980 2000 2020-0.1
-0.050
0.050.1
0.150.2
0.25
-0.4-0.3-0.2-0.100.10.20.3
Cora
l δ18
Osw
(‰)
Mod
eled
δ18
Osw
(‰)Philippine (13N 124E)
Seawater δ18O from Coral and Model
Courtesy of K. Kojima
-0.4
-0.2
0
0.2
0.4
0.6
0.8
0 2000 4000 6000
Tropical pacific
South Pacific
SE-Asia
Indian sea
Atlantic
相関
係数
年平均降水量のばらつき(mm/year)
-0.6-0.4-0.2
00.20.40.60.8
1
0 500 1000
Reproducibility of Interannual δ18Osw and Precip Amount
Large Precip Variability → Local precipitation is recordedSmall Precip Variability → Other factors (current, river flow, etc) may play big roles.
Std Dev of Annual Precip (mm/year)
Corr
elati
on
Kojima et al., in prep.
Icecore δ18O at Eclipse Icefieldlon=-139.47 ; lat=60.51
1920 1925 1930 1935 1940 1945
-20
-18
-16
-14
-12
-10
-8
-6
-4
-2
0
-33
-28
-23
-18
-13
poDelta18O
1970 1975 1980 1985 1990 1995
-25
-20
-15
-10
-5
0
-33
-28
-23
-18
-13
poDelta18O
Yalcin et al., 2003; 2006
Icecap δ18O at Mt Huascaranm, Peru lon=-77.6 ; lat=-9.1
1915 1920 1925 1930 1935 19400
2
4
6
8
10
12
-25
-20
-15
-10
-5
0
5
10
core1core2po
1965 1970 1975 1980 1985 19900
2
4
6
8
10
12
-25
-20
-15
-10
-5
0
5
10
core1core2po
Thompson et al., 1995
Summary of Part 2
• First 20th century Quasi Reanalysis for Isotope is now available.
• First comparisons with paleoclimate proxy data are now underway.
• This effort helps to develop the “forward proxy modeling” approach to more comprehensively understand the proxy data.
Thank you!
Type Dataset Name Source Variable Since Time Resolution Location (resolution) Ref.
Direct obs.CRUTEM3 T T 1850 monthly global land (5x5) Brohan et al., 2006
GPCP V4 P P 1901 monthly global land (0.5x0.5) Beck et al., 2005
Proxy grid data
tree ring T 1600 annual W. N. America Briffa et al., 1992
tree ring T and P 1602 annual N. America Fritts 1991
documentary and others SLP 1500 seasonal N. Atlantic and
EuropeLuterbacher et al.,
2004
Isotope data for regional simulation
GNIP precipitation d18O and dD 1960 monthly global land (600sites) IAEA/WMO, 2006
stream water d18O and dD 1980 monthly USA Kendall and Coplen, 2001
tree ring d18O, dD, d13C 1800 1y-5y N. AmericaVarious; reviewed by McCarroll and Loader,
2004
Isotope data for global simulation
shallow ice core d18O and dD 1860 1y-5yAntarctica,
Greenland, high mountains
Various; sorted by Schneider and Noone, 2007
snow d18O and dD 1960 occasional AntarcticaVarious; collected by Masson-Delmotte et
al., 2008
tree ring d18O 1500 1y-5y Various Various; e.g., Tsuji et al., 2006
ground water d18O 1960 occasional Various Various
speleothem d18O, d13C 1200 annual southern Oman Fleitmann et al., 2004
speleothem d18O, Ca/Mg, d13C, etc 1800 monthly China Johnson et al., 2006
Pseudo Global Warming (Kawase et al., 2009)との違いKawase et al., 2009
低周波:モデル高周波:観測(再解析)本手法
低周波:観測(アンサンブル平均)高周波:モデル
Time
Single member forecast Fn
Other members
Monthly running mean of a single member <Fn>
Monthly running mean of all members <Fbar>
incrementCorrected member
Method (c.f. Roden et al., 2000)
• Data– NPP weighted annual temperature for esat
– NPP weighted annual RH for eair
– NPP weighted annual d18O in vapor for Rair
– NPP weighted annual surface pressure for eleaf
– NPP&amount weighted annual rain water d18O for Rsw
• Rleaf= a*[1.032*Rleaf*(esat-eleaf)/esat +1.021*Rleaf*(eleaf-eair)/esat + Rair*eair/esat]
1860 1880 1900 1920 1940 1960 1980 2000 20200
0.050.1
0.150.2
0.250.3
0.350.4
0.450.5
-0.3-0.2-0.100.10.20.30.4
IsoGSM2 IsoGSM1 coral
Cora
l δ18
Osw
(‰)
Mod
eled
δ18
Osw
(‰)
Fiji (18S 179E)
1860 1880 1900 1920 1940 1960 1980 2000 2020-0.1
00.10.20.30.40.50.6
-0.4-0.200.20.40.60.811.21.4
IsoGSM2 IsoGSM1 coral
Cora
l δ18
Osw
(‰)
Mod
eled
δ18
Osw
(‰)Nauru (0.5S 166E)
サンゴ同位体比から得られる海水同位体比の再現性
Courtesy of K. Kojima
Spectral Nudging + Isotope GSM– Poor man’s data assimilation for isotopes –
IsoGSMSIO/UT Isotopic Global Spectral Model
H18OH
HD16O
)m/s(71)m/s(71
1
_
_
VCVBVAhhRRR
mvk
aseaemvkE
a
aa
CTTS
SDDS
ejmk
ejmkeff
20003.0111/_
_
a
a
aaa
hDDh
RRdmdRm
ne
e
vrr
1/,1
,1 a
a
qmRmqR
RRmmRRR
rv
rvvrr
/1/
00
00000
Surface evaporation (MJ79)
Ice crystal formation (JM84)
Rain drop evaporation (S75)
Fourier series
Nudge scale Nudging
Forecast
f
Use large scale (>1000km) winds from R2 to constrain dynamical field, so that the isotopic field is also constrained and reproduced in daily to inter-annual time scales.
Yoshimura and Kanamitsu, 2008; Yoshimura et al., 2008
http://meteora.ucsd.edu/~kyoshimura/IsoGSM1
Previous works