Gerrit Lohmann date: May 17, 2021
Lecture: May 17. (Monday), 14:00 Prof. Dr. Gerrit Lohmann
Tutorial: May 17. (Monday), ca. 15:30 Justus Contzen, Lars Ackermann
Time required for Sheet 2: 8 h
Reading/learning might take 90 min.
Content in the script: Deep ocean circulation, Conceptual models
DDt(ζ+f)+(ζ+f)(∂u∂x+∂v∂y)=0
Couples depth, vorticity, latitude
– Changes in the depth results in change in ζ.
– Changes in latitude require a corresponding change in ζ.
Dietrich et al. (1980)
DDt(ζ+fh)=0
Steward, Oceanography
Tropical air rises to tropopause & moves poleward
Deflected eastward by the Coriolis force
Subtropical jet: forms at poleward limit of Hadley Cell
It tends to conserve angular momentum, friction small
equatorward moving air: westward component
Friction: transfer of momentum from atmosphere to oceanic Ekman layer
Vorticity dynamics for the ocean and include the wind stress term
Dtu−fv=−1ρ∂p∂x+1ρ∂zτxz Dtv+fu=−1ρ∂p∂y+1ρ∂zτyz
DDt(ζ+f)−(ζ+f)hDDth=1ρ(∂∂x∂zτyz−∂∂y∂zτxz)⏟curl∂zτ.
DDt(ζ+fh)=1ρhcurl∂zτ
applied globally using the wind stress from Hellerman and Rosenstein (1983). Contour interval is 10 Sverdrups (Tomczak and Godfrey, 1994).
V=1ρβ(∂τyz∂x−∂τxz∂y)=1ρβcurlτ
wE as the Ekman vertical velocity the bottom of the Ekman layer wE=−∫0−E∂w∂zdz=∂∂xUE+∂∂yVE
curlτ produces a divergence of the Ekman transports leading to wE at the bottom
wE=∂∂x(τyρf)−∂∂y(τxρf)=curl(τρf)≃1ρfcurlτ
The order of magnitude of the Ekman vertical velocity:
typical wind stress variation of 0.2Nm−2 per 2000 km in y-direction:
wE≃−Δτxρf0Δy≃1103kgm−30.2Nm−210−4s−12⋅106m≃32myr
The center of a subtropical gyre is a high pressure zone: clockwise on the Northern Hemisphere
Ekman surface currents towards the center of the gyre
The Ekman vertical velocity balanced by wE=wg vertical geostrophic current in the interior
geostrophic flow towards the equator
returned flow towards the pole in western boundary currents
brings warm water northward where it cools.
returns southward as a cold, deep, western-boundary current.
Gulf Stream carries 40 Sv of 18°C water northward.
Of this, 15 Sv return southward in the deep western boundary current at a temperature of 2°C.
brings warm water northward where it cools.
returns southward as a cold, deep, western-boundary current.
Gulf Stream carries 40 Sv of 18°C water northward.
Of this, 15 Sv return southward in the deep western boundary current at a temperature of 2°C.
Calculation:
cp⏟4.2⋅103Ws/(m3kg)⋅ρ⏟103kg/m3⋅Φ⏟15⋅106m3/s⋅ΔT⏟(18−2)K=1⋅1015W
The flow carried by the conveyor belt loses 1 Petawatts (PW), close to estimates of Rintoul and Wunsch (1991)
brings warm water northward where it cools.
returns southward as a cold, deep, western-boundary current.
The deep bottom water from the North Atlantic is mixed upward in other regions and ocean, and it makes its way back to the Gulf Stream and the North Atlantic. Thus most of the water that sinks in the North Atlantic must be replaced by water from the far South Atlantic and Pacific Ocean.
The the conveyor is driven by deepwater formation in the northern North Atlantic.
The conveyor belt metaphor necessarily simplifies the ocean system, it is of course not a full description of the deep ocean circulation.
Broecker's concept provides a successful approach for global ocean circulation, although several features can be wrong like the missing Antarctic bottom water, the upwelling areas etc..
metaphor inspired new ideas of halting or reversing the ocean circulation and put it into a global climate context.
interpretation of Greenland ice core records indicating different climate states with different ocean modes of operation (like on and off states of a mechanical maschine).
Modelled meridional overturning streamfunction in Sv 106 = m3 /s in the Atlantic Ocean. Grey areas represent zonally integrated smoothed bathymetry
Meteor Expedition, the first accurate hydrographic survey of the Atlantic from Wuest (1935).
Meteor Expedition, the first accurate hydrographic survey of the Atlantic from Wuest (1935).
Lower panel: Salinity and dissolved oxygen on the Hauptschnitt along the western side of the Atlantic.
It is observed that water sinks in to the deep ocean in polar regions of the Atlantic basin at a rate of 15 Sv. (Atlantic basin: 80,000,000 km2 area * 4 km depth.)
– How long would it take to 'fill up' the Atlantic basin?
– Supposing that the local sinking is balanced by large-scale upwelling, estimate the strength of this upwelling.
Hint: Upwelling = area * w
– Compare this number with that of the Ekman pumping!
Timescale T to 'fill up' the Atlantic basin:
T=80⋅1012m2⋅4000m15⋅106m3s−1=2.13⋅1010s=676years
Overturning is balanced by large-scale upwelling:
area⋅w=15⋅106m3s−1
w=0.1875⋅10−6ms−1=5.9⋅10−15my−1.
Ekman pumping wE≃32my−1.
∂∂tv=−1ρ0∂p∂y−fu−κv
∂∂tw=−1ρ0∂p∂z−gρ0(ρ−ρ0)−κw κ as parameter for Rayleigh friction.
∂∂tv=−1ρ0∂p∂y−fu−κv
∂∂tw=−1ρ0∂p∂z−gρ0(ρ−ρ0)−κw κ as parameter for Rayleigh friction.
Using the continuity equation
0=∂v∂y+∂w∂z
one can introduce a streamfunction Φ(y,z):v=∂zΦ;w=−∂yΦ
The associated vorticity equation in the (y,z)-plane is therefore
∂∂t∇2Φ=−f∂u∂z+gρ0∂ρ∂y−κ∇2Φ
∂∂t∇2Φ=−f∂u∂z⏟2.+gρ0∂ρ∂y−κ∇2Φ⏟4.
Term 2. is absorbed into the viscous term (4.)
Φ(y,z,t)=∞∑k=1∞∑l=1Φk,lmax(t)sin(πky/L)×sin(πlz/H) yielding a first order differential equation in time for Φk,lmax(t).
Simple ansatz satisfying that the normal velocity at the boundary vanishes Φ(y,z,t)=Φmax(t)sin(πyL)×sin(πzH)
L and H dentote the meridional and depth extend: y from 0 to L, z from 0 to H
∫L0dy∫H0dz∂∂t∇2Φ⏟1.=∫L0dy∫H0dzgρ0∂ρ∂y⏟2.−∫L0dy∫H0dzκ∇2Φ⏟3.
1. ddtΦmax(π2L2+π2H2)L∫0dysin(πyL)H∫0dzsin(πzH)=4LH(1L2+1H2)ddtΦmax
∫L0dy∫H0dz∂∂t∇2Φ⏟1.=∫L0dy∫H0dzgρ0∂ρ∂y⏟2.−∫L0dy∫H0dzκ∇2Φ⏟3.
1. ddtΦmax(π2L2+π2H2)L∫0dysin(πyL)H∫0dzsin(πzH)=4LH(1L2+1H2)ddtΦmax
2. L∫0dyH∫0dzgρ0∂ρ∂y=gρ0H(ρnorth−ρsouth) with ρnorth=ρ(y=L),ρsouth=ρ(y=0)
∫L0dy∫H0dz∂∂t∇2Φ⏟1.=∫L0dy∫H0dzgρ0∂ρ∂y⏟2.−∫L0dy∫H0dzκ∇2Φ⏟3.
1. ddtΦmax(π2L2+π2H2)L∫0dysin(πyL)H∫0dzsin(πzH)=4LH(1L2+1H2)ddtΦmax
2. L∫0dyH∫0dzgρ0∂ρ∂y=gρ0H(ρnorth−ρsouth) with ρnorth=ρ(y=L),ρsouth=ρ(y=0)
3. κΦmax(π2L2+π2H2)L∫0dysin(πyL)H∫0dzsin(πzH)=κ4LH(1L2+1H2)Φmax
ddtΦmax=aρ0(ρnorth−ρsouth)−κΦmax with a=gLH2/4(L2+H2)
This shows that the overturning circulation depends on the density differences on the right and left boxes.
It is simplified to a diagnostic relation
Φmax=aρ0κ(ρnorth−ρsouth)
because the adjustment of Φmax is quasi-instantaneous due to adjustment processes, e.g. Kelvin waves.
Schematic picture of the hemispheric two box model (a) and of the interhemispheric box model
a) The Atlantic surface density is mainly related to temperature differences. b) But the pole-to-pole differences are caused by salinity differences. }