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Eastern Pacific feedbacks and the forecast of extreme El Niño events
Ken TakahashiInstituto Geofísico del Perú, Lima, Peru
B. Dewitte, J. Reupo, A. Wittenberg, B. Orihuela
Ciencia para protegernos Ciencia para avanzar
NOAA Climate Prediction Center, College Park, MDNovember 12, 2015
Equ
ator
ial s
ea s
urfa
ce t
empe
ratu
re (
SS
T)
Wes
tE
ast
Sea
leve
l pr
essu
re
Commonly used ENSO indices
EOF-based SST anomaly patterns/indices
Takahashi et al., 2011
E pattern C pattern
E index
C index
C in
dex
E index
SST indices for Dec-Feb
Niñ
o 3.
4
Niño 1+2
The eastern Pacific warming was proportionally much more pronounced during the extreme El Niño
Annual rainfall in the northern coast of Peru (Piura, 5°S)
The two extreme El Niño produced as much rainfall as the next 40 rainiest years combined.
1982-83
1997-98
1972-73
Sea surface temperature
anomaly patterns
El Niño: East Pacific only
Lavado y Espinoza, 2014
Enhanced coastal rainfall
Reduced rainfall in the
Andes and Amazon
Takahashi et al., 2011
Correlation with annual rainfall
Local effect Teleconnections
AtlánticoPacífico
El Niño: Central Pacific only
Every El Niño has a different combination of these two patterns
PC1 PC1
PC2
E
C
E
C
Takahashi et al., 2011
GFDL CM2.1 reproduces the observed E-C relationship
Bimodal probability distribution functions for El Niño peaks*Model data for 1300 years
(250 EN peaks)
K-mean clusters in colors
Triangles = cluster centers
C
ETakahashi and Dewitte, 2014
Strong and moderate El Niño regimes in the GFDL CM2.1 climate model and observations
E ≈ 1.8
* EN peaks = maxima in PC1 of near-equatorial SST
Ocean heat budget for El Niño growth according to E
Strong EN
Moderate EN
Strong EN Moderate
EN
Phase 1:Jan (0)-Jul (0)
Phase 2:Jul (0)-Jan (1)
“Nonlinear dynamical heating” (= nonlinear advection)
Linear vertical advection
Linear horizontal advection
Nonlinear advection contributes with 11% (obs) and 13% (CM2.1) to advective growth of strong El Niño
Observational(DRAKKAR)
Model(CM2.1)
Takahashi and Dewitte, 2015
Observed* nonlinear Bjerknes feedback (SST/rain/wind)
The response in convection and wind stress to SST is more than 3 times for E > 1.5, i.e. strong eastern Pacific warming -> stronger Bjerknes feedback)
All monthly data
Percentiles (10,25,50,75,90%) binned by SST indices.
Piecewise linear fit: Multivariate adaptive regression splines
Takahashi and Dewitte, 2015
EE
Eas
t P
ac O
LR a
nom
(W
m-2)
EP
zon
al s
tres
s an
om (
Nm
-2)
Linear regression of SST (colors), OLR (contours) and wind stress on the E index in observations
* Similar in CM2.1 but shifted westwards
Takahashi and Dewitte, 2015
Strong El Niño in observations and the GFDL CM2.1 climate model
C E
Heat content
Thermocline tilt
CP zonal
stress
EP zonal stress
Obs:1982-831997-98
CM2.110, 25, 50, 75, 90% percentiles(PI control: 500 years)
Strong EN in CM2.1 very consistent with obs
A precursor of strong EN
Takahashi and Dewitte, 2015
12
Central Pac zonal wind stress anom in Aug(0)
Observations and GFDL CM2.1
Eastern Pacific warming (E) in
Jan(1)
10%
90%
The precursor zonal wind stress is partly (but not all) given by the Bjerknes feedback
Takahashi and Dewitte, 2015
In the 1972-73 and 1997-98 events, most of the stress was “coupled”.
Zonal wind stress in August
OLR in August
Total
Coupled*
Uncoupled *Coupled = Linear
regression onto E and
C
July Clim.
July 1982
In August 1982 there was substantial forcing from the SW Pacific (Harrison, 1984; also Hong et al., 2014)
August central Pacific zonal stress: Extreme El Niño predictor
(Takahashi & Dewitte, 2015)
Approx. threshold
Zonal wind precursors of strong EN in CM2.1Comparing the free control and the initialized hindcasts
Takahashi and Dewitte, 2014
Obs & PI control run Forecasts initialized in August
1982
1997
10%
90%
Dashed lines = 10% and 90% percentiles from CM2.1 PI ctl run
NMME* model SSTA bias-corrected forecasts (°C) of extreme El Niño (1982-83, 1997-98)
ObsMME mean
Ensemble means of individual models
*North American Multi-Model Ensemble (Kirtman et al., 2014). Thanks to NOAA, NSF, NASA and DOE
GFDL CM2.1 bias-corrected forecasts* (lead 7.5)
CM2.1 w/CM2.1 PI patterns
CM2.1 w/obs patternsObserved
E index
C index
* 10-member ensemble means
Relative amplitude (regression coefficient) of forecasted /observed E and C (GFDL CM2.1*, 1982-2012)
E
C
E
C
Linear regression (relative amplitude) Linear correlation
Persistence
* 10-member ensemble means
2015-16 Niño 1+2 bias-corrected SST anomaly forecasts (June IC)
GFDL CM2.1 aer04
NOAA CFS2
+
NASA GMAO
Data: NMME project (Kirtman et al, 2013)
GFDL CM2.1 aer04
NOAA CFS2
+
NASA GMAO
Data: NMME project (Kirtman et al, 2013)
2015-16 Niño 1+2 bias-corrected SST anomaly forecasts (November IC)
GFDL CM2.1 aer04
NOAA CFS2
+
NASA GMAO
Summary• Extreme El Niño appears to correspond to a separate dynamical regime.• Convectively-nonlinear Bjerknes feedback in the eastern Pacific appears to
be important for the growth of extreme El Niño events.• This nonlinearity, in a recharge-discharge model, can reproduce the two
regimes.• Large westerly wind around August is a predictor of extreme El Niño.
External wind forcing played a large role in 1982-83.• Ongoing research (preliminary results): Nonlinear interaction between fast
model (CM2.1) drift and forecasted interannual variability shifts the threshold behaviour to the west.