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![Page 1: 3/14/20051/32 Coastal Processes and Arctic Climate Change Are they resolved? Do they matter? How do they scale? Andreas Münchow College of Marine Studies.](https://reader034.fdocuments.in/reader034/viewer/2022051821/56649d3e5503460f94a16db3/html5/thumbnails/1.jpg)
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Coastal Processes and Arctic Climate Change
Are they resolved? Do they matter?
How do they scale?
Andreas MünchowCollege of Marine Studies
University of Delaware
Collaborators:Drs. Falkner, Garvine, Melling, Weingartner
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Hypotheses/Conclusions•Large, abrupt pulses of freshwater discharges do not disturb the thermohaline circulation substantially;
•Freshwater driven flows scale with the internal deformation radius L~10-km (“eddy” scale);
•Scaling implies small across-shore (~10-km) and long along-shore (~1000-km) correlation scales;
•“Measured” (and modeled) freshwater fluxes do not resolve relevant scales;
•Nares Strait mooring array designed to resolve the internal deformation radius, freshwater fluxes, and dynamics.
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Coastal Processes and Arctic Climate Change:
1. Insulation of the Arctic ice-cover from warm
Atlantic water at depth, i.e., “maintenance of the
Arctic halocline”
2. Arctic freshwater and the global thermohaline
circulation (nonlinear, multiple equilibria)
How to move water across sloping topography?
global
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Hypotheses/Conclusions•Large, abrupt pulses of freshwater discharges do not disturb the thermohaline circulation substantially;
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Today’sclimate
Greenland Ice Core Data oxygen isotopes 18O ~ T temperature
Figure from Alley et al. (2001)
Climate of last 10,000 years appears most anomalous.
18O
COLD
WARM
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Hysteresis Loop of Climate ChangeO
vert
urni
ng C
ircu
lati
on 100 mSv
Rahmstorf (2000)
Nonlinear response of thermohaline circulation to freshwater pertubations
Caveats:
•Location of current climate?•100-500 year duration•Distance to convection sites
Stommel (1961)
COLD
WARM
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Hysteresis Loop of Climate ChangeO
vert
urni
ng C
ircu
lati
on 100 mSv
Rahmstorf (2000)
Stommel (1961)
COLD
WARM
Freshwater FluxAlley (2001)
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Freshwater Flux: ∫ u(s-s0)/s0 dA
0.1 Sv = 0.1106 m3/s = 100 mSv = 3,150 km3/year
Arctic RiversBering StraitDavis Strait
Lena RiverAmazon RiverLake Ontario
Arctic Ice Volume
Lake Agassiz*
110 mSv70 mSv
100 mSv
17 mSv200 mSv
9 mSv
>1,000 mSv
3,800 km3/y2,200 km3/y3,000 km3/y
510 km3/y6,300 km3/y
270 km3/y
30,000 km3
>30,000 km3/y(*) glacial lake dammed by Laurentian ice sheet burst ~8200 BP (Barber et al., 1999, Nature)
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Today’sclimate
YoungerDryas
Greenland Ice Core Data oxygen isotopes 18O ~ T temperature
Adapted from Alley et al. (2001)
Climate of last 10,000 years appears most anomalous.
18O
COLD
WARM
LakeAgassizdischarge
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Hypotheses/Conclusions
•Large, abrupt pulses of freshwater discharges do not disturb the thermohaline circulation substantially;
•Freshwater driven flows scale with the internal deformation radius L (“eddy” scale);
√∆/0 g D / f ~ 10 km
+∆
D
f is Coriolis “force”
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“derived” velocity
Nares Strait Hydrography, Aug.-2003
Pics-AprilPics-August
Density
Temp.
Salinity
Canada Greenland
LL
D
view from Greenland across Nares Strait
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David Huntley (UDel) with “sonar” in Aug. 2003
Velocity:Radars + Sonars
Radars send and receiveelectromagnetic waves (radio, police)
Sonars send and receives acoustic waves (sound, whales)
Same physics.
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•
•
t0
t0+16 hrs
east west
Barrow Canyon Velocity Section:
Synoptic velocity observation in Barrow Canyon, Alaska(view is to the south):
The flow scales with the internal deformation radius, about 5-km.
The flow is also unsteady.
Münchow and Carmack (1996)
D
D
L
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I
II
III
Eddies in the ArcticSept.-22, 2004
I II III
USCGC Healy 75-kHz ADCP
L
D
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Interaction of wind- and buoyancy forced motions
Salinity
Fresh riverine water turnsright at the coast.
Münchow and Garvine (1993)
L
D
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Hypotheses/Conclusions•Large, abrupt pulses of freshwater discharges do not disturb the thermohaline circulation substantially;
•Freshwater driven flows scale with the internal deformation radius L~10-km (“eddy” scale);
•Scaling implies short across- (~10-km) and long along-shore (~1000-km) correlation scales
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Ward Hunt Ice Shelf
~ 4 km3 fresh water and unique ecosystem lost from dammed epishelf lake in Disraeli Fjord 1999-2002
Mueller et al. (2003)
crack
Ice shelf
EllesmereIsland
Disraeli Fjord
Arctic Ocean
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Ward HuntIce Shelf
1962
1963
1964
Nutt (1966): The drift of ice island WH-5
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Labrador Shelf
Moving ice on the Labrador shelf indicates trapping of fresh water and ice on the shelf
Hudson Strait
LABRADOR
NA
SA
deep convection site winter 1997 (Pickart et al., 2002)
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North(cm/s)
East(cm/s)
Labrador
Labrador Sea
Time (hours)
basinshelf
fresh salty
Velocity
Velocity
Depth
Sal.
Temp.warmcoolcold
Crossing the Labrador Current, July-23, 2003
southward
eastward
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Hypotheses/Conclusions
•Large, abrupt pulses of freshwater discharges do not disturb the thermohaline circulation substantially;
•Freshwater driven flows scale with the internal deformation radius L~10-km (“eddy” scale);
•Scaling implies small across-shore (~10-km) and long along-shore (~1000-km) correlation scales;
•“Measured” (and modeled) freshwater fluxes do not resolve relevant scales
???
??
Chapman and Beardsley (1989) adapted byKhatiwala et al. (1999)
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Davis Strait 3-year Mean1987-1990
~150-m
~300-m
~500-m
with95% confidence levelsfor speed and direction
“Ross” data(Tan et al., 2005)
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Baffin Island Current
West Greenland Current
1.5Sv
0.7Sv
2.3Sv
Velocity normal to Davis Strait mooring section:
3-year mean velocity (contours)over 1987-1990 salinity (color)
3-year mean velocityminus 95% confidence
3-year mean velocityplus 95% confidence
Volume flux: 1.5 ± 0.8 SvFreshwater flux: 75 ± 38 mSv
EOF Analyses
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Davis Strait Northward Flow@ 150-m (“surface”)
Annual harmonic+ Semi-annual harmonic+ record mean
Baffin Island Current
West Greenland Current
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Retreat of Jakobshavn IsbræWest-Greenland
NA
SA
/US
GS
Greenland Ice Sheet
BaffinBay
5-km
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Hypotheses/Conclusions
•Large, abrupt pulses of freshwater discharges do not disturb the thermohaline circulation substantially;
•Freshwater driven flows scale with the internal deformation radius L~10 km (“eddy” scale);
•Scaling implies short across-shore (~10-km) and long along-shore (~1000-km) correlation scales;
•“Measured” (and modeled) freshwater fluxes do not resolve relevant scales;
•Nares Strait mooring array designed to resolve the internal deformation radius, freshwater fluxes, and dynamics
![Page 27: 3/14/20051/32 Coastal Processes and Arctic Climate Change Are they resolved? Do they matter? How do they scale? Andreas Münchow College of Marine Studies.](https://reader034.fdocuments.in/reader034/viewer/2022051821/56649d3e5503460f94a16db3/html5/thumbnails/27.jpg)
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Canadian Archipelago Throughflow Study (CATS):
NA
SA
200
2/22
3
Petermann Glacier
Humbold Glacier
Arctic Ocean
Greenland
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Geostrophic current
Kennedy Channel Hydrography, Aug.-2003
Pics-AprilPics-August
S
Canada Greenland
LL
D
D
view from Greenland across Nares Strait
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Salinity s
Velocity
FreshwaterFlux/unit area
Nares Strait South (Kennedy Channel)
∫ u(s-s0)/s0 dA
∫ u dA
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Across-channel flow
Along-channel flow
Currents@ 100-m
*
Pics-April
Pics-August
.html
Wind
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Hypotheses/Conclusions•Large, abrupt pulses of freshwater discharges do not disturb the thermohaline circulation substantially;
•Freshwater driven flows scale with the internal deformation radius L~10-km (“eddy” scale);
•Scaling implies small across-shore (~10-km) and long along-shore (~1000-km) correlation scales;
•“Measured” (and modeled) freshwater fluxes do not resolve relevant scales;
•Nares Strait mooring array designed to resolve the internal deformation radius, freshwater fluxes, and dynamics.