ocean circulation and sea ice in the mpi-m ipcc experiments · 2005. 12. 15. · atmospheric and...
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Ocean circulation and sea ice in the MPI-M IPCC experiments
Johann JungclausMax- Planck- Institut für Meteorologie
Hamburg
+ M. Esch, H. Haak, F. Landerer, M. Boettinger, E. Roeckner ++
Introduction: The role of the ocean in the climate system
The oceans store and transporthuge amounts of heat
The ocean provide the slowcomponent of variability and its inertia may mask global climate change
The ocean provides also a storage and transportmeans for carbon. (25% of anthropogenic carbonemission are taken up bythe oceans)
European temperature March 2005
Atmospheric and oceanic heat transportstotal
atmos
ocean
90S 60S 30S EQ 30N 60N 90N
6
-4
4
0
-6
-2
2
Atmosphere and oceantransport about 6 PW (1 PW=1015 W) heat from theequator to high and middlelatitudes
The global oceanaccounts for 1/3 (ca. 2 PW) of this. The Atlantic heat transport is about 1.3 PW
The Thermohaline Circulation (THC)
Evidence from the past
Abrupt climate changes in the past are associated withdisturbances of the Atlanic Thermohaline Circulation caused byexcessive fresh water input into the North Atlantic
Effects of a possible sea change
Eiszeit oder Treibhaus?
PM September 2004 Titel
Sea ice in the climate systemSea ice effectively decouples ocean and atmosphere. Owing to its high albedo itreflects sun light back to space. Loss of seaice will enhance oceanic heat uptake (icealbedo feedback).
Therefore the sea ice covered regions arevey sensitive to global change
Sea ice stores huge amounts of fresh water. Its release under warming condition mayinfluence the THC.
The presence of sea ice influencesatmospheric circulation.
Sea ice changes will influence the marineand terrestrial ecosystems, and high latitude societies and economics.
The coupled ocean atmosphere ModelECHam5: MPI atmosphere model (Roeckner et
al., 2003), interactive runoff and glacier calving scheme.
Resolutions: T63L31 (IPCC)
OASIS 3.0 PRISM coupler
MPI-OM (C-HOPE) (Marsland et al., 2003)C-Grid, z-level, partial cells, BBL
parameterizationHibler-type sea ice model incl. snow and
fractional ice coverConformal mapping: 1.5° with refinement in
grid pole regions
NO FLUX ADJUSTMENT
ECHam5
OASIS
MPI-OM
Ocean model grid
Every 5th grid line is shown here; in the vertical, there are40 unevenly spaced depth levels
Ocean model grid
How well does the model reproduce the presentclimate ?
SST is in general agreement with observations but biases > 1º C are common owing to unresolved processes/features.
These errors are not a unique MPI-OM/ECHAM feature.Jungclaus et al., 2005
Precipitation (modeled – observed)
[mm/day]Precipitation bias is most pronounced in equatorial region(Double ITCZ)
Jungclaus et al., 2005
Northern hemisphere sea ice conc.Chapman & Walsh 1996 Model (T63/GR1.5 ctrl.)
March
September
Jungclaus et al., 2005
Southern hemisphere sea ice conc.Model (T63/GR1.5)Chapman & Walsh 1996
March
September
The Atlantic Meridional Overturning Circulation
Jungclaus et al., 2005
Meridional heat transport in the Atlantic
ECHAMT63/L31, MPI-OM 1.5
Jungclaus et al., 2005
Results from the IPCCscenario experiments
Atm. CO2 concentration Glob. Atm. Surface air temperature
Figure by M. Boettinger, DKRZ
IPCC Experiments A1B: SST difference end of 21th century minus 20th century
Widespread warming, North Atlantic shows effect of weaker THC
A1B: Sea surface salinity difference end of 21th century minus 20th century
What is the fate of the MOC?In a warmer climate, the heating of the upper ocean is
accompanied by freshening in high latitudes and salinification in low latitudes (acceleration of thehydrological cycle). Surface waters in the deep waterformation regions become lighter and the watercolumn is more stably stratified.
This will affect the sinking of deep water and the MOC.
Feedbacks such as salt advection by the ocean maycounteract or enhance the decrease of the MOC.
The relative role of individual feedbacks appears to behighly model dependent.
Estimates from different models (Third Assessment Report (TAR))
Figure from IPCC, 2001
Projections for the Atlantic MOC for the 21st C
Global Atm. Surfacetemperature[ºC]
Atlantic Meridional overturningcirculation
[Sv, 1Sv=106m3s-1]
and beyond...
Global Atm. Surfacetemperature[ºC]
Atlantic Meridional overturningcirculation
[Sv, 1Sv=106m3s-1]
Temporal evolution of Atlantic upper oceansalinity
Difference betweenzonally averagedsalinity in the A1B experiment and the 20th
century mean
Positive salinityanomalies in the North Atlantic evolve as a resultof northward salttransport.
Temporal evolution of zonally averagedsurface air temperature
A1B
Future evolution of Arctic sea ice
Figure by M. Boettinger, DKRZ
Animation by M. Boettinger, DKRZ
Animation by M. Boettinger, DKRZ
Impact of Arctic climate change: New seatransportation routes?
Figure by BBC
Open water in the North East Passage (in % of the total area of the coastal corridor)
Time (yr)
% o
f ope
nw
ater
September August October March
Great future for Arctic shipping but at whichcosts for the environment?
Ship emissions as observed from space;
will we see a similar track around Siberia?
What are climate model results good for?ACIA, the Arctic Climate Impact Assessment
An international project of the Arctic Council and the International Arctic Science Committee (IASC), to evaluate and synthesize knowledge on climate variability, climate change, and increased ultraviolet radiation and their consequences.
The model results were mainly basedon the IPCC TAR (2001) experiments.
ACIA International Scientific Symposium held in Reykjavik, Iceland in November 2004.
http://www.acia.uaf.edu
ConclusionsThe new coupled model simulates a reasonable climate withoutflux adjustment.Improvements in comparison with the IPCC TAR models areseen in ocean heat transport, sea ice, and other featuresIn the IPCC scenarios, the Atlantic MOC decreases over the 21st
century but slowly recovers thereafter; this is also the case ifthere is an additional fresh water input from a melting Greenlandice sheet. (This may be model dependent)The model show a considerable and rapid loss of Arctic sea icein the 21st century. While winter sea ice cover is only slightlyreduced the Arctic ocean is projected to become ice free in summer in the 2nd half of the 21st century
Data issues
Data are available on original grid (256x220x40 grid points) and (partly) on IPCC standard 1º grid (360x180x40).
Data format is „EXTRA“ (a fortran binary) or NetCDF
10 yr monthly mean of a 3d- data field requires 1.1 GB on original (EXTRA) and 1.25 GB (NetCDF) on regular grid.
10 yr monthly mean of a 2d- data field requires 27 MB on original and 32 MB on regular grid.
Owing to technical problems not all data have beentransferred fo PCMDI.
Data will also be stored in M&D CERA data base
Thank You….
No total breakdown of the MOC....What if we include the meltdown of Greenland ?
The present simulations do not include ice sheet dynamics. Icesheet model projections show a considerable loss of Greenlandice mass (with a high range of uncertainty); estimates rangefrom 0.01 to 0.1 Sv for various scenarios.
From the IPCC experiments one can deduce a melting rate of about 0.03 Sv for the A1B scenario at the end of the 21st
century.
A sensitivity experiment under A1B forcing is carried out where an additional fresh water inflow is prescribed around Greenland. The flux is ramped up from 0 Sv in 2000 to 0.09 Sv in 2100.
Effect of additional melt water input fromGreenland on the MOC