EVAT 554 OCEAN-ATMOSPHERE DYNAMICS SVERDRUP TRANSPORT LECTURE 15 (Reference: Peixoto & Oort, Chapter 8,10)

Slides:



Advertisements
Similar presentations
Section 2: The Planetary Boundary Layer
Advertisements

SIO 210: Dynamics VI (Potential vorticity) L. Talley Fall, 2014 Talley SIO210 (2014)1 Variation of Coriolis with latitude: “β” Vorticity Potential vorticity.
Wind-Driven Circulation in a Stratified Ocean Consider the ocean in several isopycnal layers that can be separated into two groups: Layers that outcrop.
Dynamics V: response of the ocean to wind (Langmuir circulation, mixed layer, Ekman layer) L. Talley Fall, 2014 Surface mixed layer - Langmuir circulation.
Wind Forced Ocean Circulation. Ekman Spiral and Ekman Mass Transport.
Western Intensification Subtropical gyres are asymmetric & have intense WBC’s Western intensification is created by the conservation of angular momentum.
Steady State General Ocean Circulation “steady state” means: constant in time, no accelerations or Sum of all forces = 0 Outline:1. Ekman dynamics (Coriolis~Friction)
Ocean & Atmospheric circulation redux 1) Unequal planetary heating creates pressure gradients which make winds blow on ocean surface in trade-wind & westerly.
What drives the oceanic circulation ? Thermohaline driven (-> exercise) Wind driven (-> Sverdrup, Ekman)
Wind-driven Ocean Circulation
© 2002 Brooks/Cole, a division of Thomson Learning, Inc. Ekman Spiral and Transport The motion of the water at the surface is driven by the wind. Each.
Surface Water Equations
Wind-driven circulation II
Define Current decreases exponentially with depth. At the same time, its direction changes clockwise with depth (The Ekman spiral). we have,. and At the.
Evaporative heat flux (Q e ) 51% of the heat input into the ocean is used for evaporation. Evaporation starts when the air over the ocean is unsaturated.
Define Current decreases exponentially with depth and. At the same time, its direction changes clockwise with depth (The Ekman spiral). we have,. and At.
Class 8. Oceans II. Ekman pumping/suction Wind-driven ocean flow Equations with wind-stress.
Vorticity Measure of angular momentum for a fluid
Term Paper Guide Find an oceanic or relevant atmospheric phenomenon you are interested in (e.g., ENSO, PDO, AMO, TAV, IOD, NAO, hurricane activity, regional.
Alternative derivation of Sverdrup Relation Construct vorticity equation from geostrophic balance (1) (2)  Integrating over the whole ocean depth, we.
Ocean Circulation Currents. Horizontally Vertically.
OCEAN CURRENTS.
Term Paper Guide Find an oceanic or relevant atmospheric phenomenon you are interested in (e.g., ENSO, PDO, AMO, TAV, IOD, NAO, hurricane activity, regional.
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS FILTERING OF EQUATIONS FOR OCEAN LECTURE 10 (Reference: Peixoto & Oort, Chapter 3,8)
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS FILTERING OF EQUATIONS OF MOTION FOR ATMOSPHERE (CONT) LECTURE 7 (Reference: Peixoto & Oort, Chapter 3,7)
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS FILTERING OF EQUATIONS FOR ATMOSPHERE (CONT) LECTURE 6 (Reference: Peixoto & Oort, Chapter 3)
For a rotating solid object, the vorticity is two times of its angular velocity Vorticity In physical oceanography, we deal mostly with the vertical component.
Wind Driven Circulation III Closed Gyre Circulation Quasi-Geostrophic Vorticity Equation Westward intensification Stommel Model Munk Model Inertia boundary.
For a rotating solid object, the vorticity is two times of its angular velocity Vorticity In physical oceanography, we deal mostly with the vertical component.
Typical Mean Dynamic Balances in Estuaries Along-Estuary Component 1. Barotropic pressure gradient vs. friction Steady state, linear motion, no rotation,
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS
An example of vertical profiles of temperature, salinity and density.
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS EQUATIONS OF MOTION (CONT); ENERGY EQUATION LECTURE 4 (Reference: Peixoto & Oort, Chapter 3)
How Does Air Move Around the Globe?
Schedule for final exam
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS TIME-DEPENDENT DYNAMICS; WAVE DISTURBANCES LECTURE 21.
For most of the basin Question
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS GYRE-SCALE OCEAN CIRCULATION LECTURE 16 (Reference: Peixoto & Oort, Chapter 8,10)
Question: Why 45 o, physics or math? andare perpendicular to each other 45 o relation holds for boundary layer solution Physics: Coriolis force is balanced.
A Synthetic Drifter Analysis of Upper-Limb Meridional Overturning Circulation Interior Ocean Pathways in the Tropical/Subtropical Atlantic George Halliwell,
12.808, Problem 1, problem set #2 This is a 3 part question dealing with the wind-driven circulation. At 26 o N in the N. Atlantic, the average wind stress.
Class 8. Oceans Figure: Ocean Depth (mean = 3.7 km)
Ocean Dynamics Previous Lectures So far we have discussed the equations of motion ignoring the role of friction In order to understand ocean circulations.
Geostrophy, Vorticity, and Sverdrup
Wind-driven circulation II ●Wind pattern and oceanic gyres ●Sverdrup Relation ●Vorticity Equation.
Ekman Spiral Boundary layer flow under horizontal homogeneous condition Assuming steady state and neglecting thermodynamic effect, Using K-theory Further.
CoriolisPressure Gradient x z CURRENTS WITH FRICTION Nansen’s qualitative argument on effects of friction CoriolisPressure Gradient x y CoriolisPressure.
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS UPWELING AND DOWNWELLING; EKMAN TRANSPORT LECTURE 14 (Reference: Peixoto & Oort, Chapter 8,10)
Forces and accelerations in a fluid: (a) acceleration, (b) advection, (c) pressure gradient force, (d) gravity, and (e) acceleration associated with viscosity.
Stommel and Munk Theories of the Gulf Stream October 8.
The Oceanic General Circulation. Regardless of hemisphere or ocean basin, there is an intense current on the western boundary.
Typical Mean Dynamic Balances in Estuaries Along-Estuary Component 1. Barotropic pressure gradient vs. friction Steady state, linear motion, no rotation,
Sverdrup, Stommel, and Munk Theories of the Gulf Stream
CEE 262A H YDRODYNAMICS Lecture 17 Geostrophy. Often in analyzing large-scale flows we find that the momentum equations simplify greatly, i.e. we can.
Class Meeting Nov. 26, 2:00pm-4:45pm
Define and we have • At the sea surface (z=0), the surface current flows at 45o to the right of the wind direction Depends on constant Az => • Current.
Wind-driven circulation
Define and we have • At the sea surface (z=0), the surface current flows at 45o to the right of the wind direction Depends on constant Az => • Current.
Define and we have • At the sea surface (z=0), the surface current flows at 45o to the right of the wind direction Depends on constant Az => • Current.
How to create a subtropical gyre circulation I
Assume geostrophic balance on -plane approximation, i.e.,
Ekman layer at the bottom of the sea
Gyres of the world oceans
Wind Driven Circulation III
EVAT 554 OCEAN-ATMOSPHERE DYNAMICS
The β-spiral Determining absolute velocity from density field
WIND-DRIVEN OCEAN CIRCULATION
Western Boundary Currents
Week 6-7: Wind-driven ocean circulation Tally’s book, chapter 7
TALLEY Copyright © 2011 Elsevier Inc. All rights reserved
Presentation transcript:

EVAT 554 OCEAN-ATMOSPHERE DYNAMICS SVERDRUP TRANSPORT LECTURE 15 (Reference: Peixoto & Oort, Chapter 8,10)

Sverdrup Transport Let us consider again the approximate form of the governing equations for the horizontal circulation where we ignore horizontal, but not vertical friction: Let us rewrite the friction terms in terms of stress, and multiply through by ,

Sverdrup Transport Integrate these equations vertically, from some depth h well below the Ekman depth:

Sverdrup Transport Now re-arrange the equations Evaluate the right hand side…

Sverdrup Transport

Multiply first equation by cos  and differentiate the two equations with respect to latitude and longitude respectively

Sverdrup Transport

Re-arrange, and collect like terms, Since there can be no vertically-integrated mass convergence,

Sverdrup Transport Re-arrange this equation, We can then write, Sverdrup Equation And define,

Sverdrup Transport

Sverdrup Transport represents the total mass transport in the wind-influenced layer, including both Ekman and Geostrophic transport, each of which can be written separately, (from previous lecture)

Sverdrup Transport Lets estimate the Ekman and Sverdrup Transports at 35N Ekman Transport

Sverdrup Transport Express these as Volume Transports

Sverdrup Transport Express these as Basin-Integrated (Atlantic) Volume Transports

Sverdrup Transport Express these as Basin-Integrated (Atlantic) Volume Transports =-1 “Sverdrups” =-10 Sverdrups

Windstress and Circulation in the Upper Ocean Ekman circulation contributes no depth- integrated flow (a geostrophic return flow balances near- surface Ekman flow) By contrast, Sverdrup transport contributes a non-zero depth-integrated flow

Sverdrup Transport By continuity, we require

Sverdrup Transport By continuity, we require

Sverdrup Transport By continuity, we require This equation can be integrated from the eastern boundary...

Sverdrup Transport What about the western boundary???