Dynamics II: lecture 5

Gerrit Lohmann date: May 17, 2021

Organization of

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

May 17, 14:00: Lecture 5 (online G. Lohmann, 50 min)

klick here for the zoom session

5th lecture (link)

Read Chapter 11 (The thermohaline circulation of the ocean) in Marchal and Plumb

Reading/learning might take 90 min.

 

Fifth lecture (link to pdf will become available here)

Content in the script: Deep ocean circulation, Conceptual models

Potential vorticity is conserved

 

DDt(ζ+f)+(ζ+f)(ux+vy)=0

Couples depth, vorticity, latitude

– Changes in the depth results in change in ζ.

– Changes in latitude require a corresponding change in ζ.

Cape

Dietrich et al. (1980)

 

Ocean with depth h(x,y)

 

DDt(ζ+fh)=0

Cape

Steward, Oceanography

Angular Momentum and Hadley Cell

 
Subtropical and polar jet

Hadely Cell

 

 

 

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

Amplitude of overturning

ddtΦmax=aρ0(ρnorthρsouth)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(ρnorthρsouth)

because the adjustment of Φmax is quasi-instantaneous due to adjustment processes, e.g. Kelvin waves.

THC

Schematic picture of the hemispheric two box model (a) and of the interhemispheric box model

THC

a) The Atlantic surface density is mainly related to temperature differences. b) But the pole-to-pole differences are caused by salinity differences. }