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Earth System Science II – EES 717

Spring 2012

1. The Earth Interior – Mantle Convection & Plate Tectonics

2. The Atmosphere - Climate Models, Climate Change and Feedback Processes

3. The Oceans – Circulation; climate and the oceans

Key Points to Remember1. The global wind system acts to redistribute heat

between lows and high latitudes.

2. Coriolis force influences the direction of winds as they move from regions of high pressure to regions of low pressure.

3. Differential heating between land and water greatly influences global wind patterns influences global wind patterns.

4. Mid-latitude weather is systems are cyclones and anticyclones. Low latitude circulation is characterized by spiraling Hadley cells.

5. Heat is transported to higher latitudes through convective motions and latent heat transfer.

6. Ocean-Atmosphere interactions are most intense (strong coupling) in the tropics.

The Tropics

Pressure and Winds

Circulation around Highs and Lows & Re-distribution of Heat

Extratropical Circulation – Planetary Waves

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Extropical Dynamics –Frontogenesis

Tropic of Cancer Tropic of Cancer

Temperature

deN

orth

Ocean-Surface Conditions Depend on Latitude, Temperature, and Salinity

Equator Equator

Tropic of Capricorn Tropic of Capricorn

Salinity

Salinity

Temperature

Latit

udSo

uth

Mid Ocean Average Surface Salinity

Table 6-3, p. 166

Sea-surface temperatures during Northern Hemisphere summer

Fig. 6-16, p. 168

Sea-surface average salinities in parts per thousand (‰).

The Ocean Is Stratified by Density

two samples of water can have the same densityat different

Fig. 6-17, p. 169

at different combinations of temperature and salinity!

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The Ocean Is Stratified into Three Density Zones by Temperature and Salinitya.The surface zone or surface layer or mixed surface layer or mixed layerb.The pycnocline, or thermocline or haloclinec.The deep ocean (~ 80% of the ocean is below the surface zone

5 10 15 20 25

Polar

Tropical 2,000Temperate

1,0004,000

6,0002 000h

(m)

h (ft

)

Temperature (°C)

Typical temperature profiles at polar, tropical, and middle (temperate) 2,000

Dep

th

8,000 Dep

t

3,000 10,000

40 50 60 70Temperature (°F)

(temperate) latitudes. Note that polar waters lack a thermocline.

Water Transmits Blue Light More Efficiently Than Red

most of the ocean lies in complete blackness

• Dissolved saltsMajor constituents and trace elementsConservative/nonconservative constituents

• Major Constituents = [] > 1 part per million

Na+ Sodium86 %Cl- Chloride

SO4- SulfateMg2+ MagnesiumCa2+ CalciumK+ Potassium

99 %

86 %

• Trace Elements = [] < 1 part per million

• Distribution with depthPhotosynthesis removes CO2 and produces O2 at the surfaceRespiration produces CO2 and removes O2 at all depthsCompensation depth (Photosynthesis = Respiration)

Gases

photosynthesis

CO2 O2

respiration

Oxygen and CO2 profiles

O2 Concentrations

Photosynthesis

Bottom water enrichment

CO2 Concentrations

Direct solution of gas from the atmosphere

Respiration of marine organisms

Oxidation (decomposition) of organic matter

oxygen minimum

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Surface Currents Are Driven by the Winds

A combination of four forces – surface winds, the sun’s heat, the Coriolis effect, and gravity – circulates the ocean surface clockwise in the Northern Hemisphere and counterclockwise in the Southern Hemisphere forming gyresSouthern Hemisphere, forming gyres.

The North Atlantic gyre, a series of four interconnecting currents with different flow characteristics and temperatures.

Surface Currents Flow around the Periphery of Ocean Basins

The Ekman spiral and the mechanism by which it operates.

Surface Currents Flow around the Periphery of Ocean Basins

Consider the North Atlantic.

The surface is raised through wind motion and Ekman transport to form a low hill. The westward-moving water at B ‘feels’ a balanced pull from two forces: the one due to Coriolis effect (which would turn the water to the right) and the one due to the pressure gradient, driven by gravity (which would turn it to the left).

The hill is formed by Ekman transport. Water turns clockwise (inward) to form the dome, then descends, depressing the thermocline.

Hydrostatic Pressure:

p = −ρgz

z = depth

g = grav. Acc.

ρ = density of seawater

PGF per Unit Mass:

1/ρ x dp/dx = g x tan(θ)

In oceanography, dynamic topography refers to the topography of the sea surface related to the dynamics of its own flow. In hydrostatic equilibrium, the surface of the ocean would have no topography, but due the ocean currents, its maximum dynamic topography is on the order of two meters

Dynamics: The forces and motions that characterize a system

Seawater Flows in Six Great Surface Circuits

Geostrophic gyres are gyres in balance between the pressure gradient and the Coriolis effect. Of the six great currents in the world’s ocean, five are geostrophic gyres. Note the western boundary currents in this map.

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Western boundary currents – These are narrow, deep, warm, fast currents found at the western boundaries of ocean basins.

The Gulf StreamThe Japan CurrentThe Brazil CurrentThe Agulhas CurrentTh E st rn Austr li n Curr nt

Boundary Currents Have Different Characteristics

The Eastern Australian CurrentEastern boundary currents – These currents are cold, shallow and broad, and their boundaries are not well defined.

The Canary CurrentThe Benguela CurrentThe California CurrentThe West Australian CurrentThe Peru Current

Boundary Currents Have Different Characteristics

The general surface circulation of the North Atlantic.

Unit for measuring flow rates (or volume transported b )by ocean currents):sverdrups1 sv = 1 million cubic meters of water per second

Boundary Currents Have Different Characteristics

Edd f tiEddy formationThe western boundary of the Gulf Stream is usually distinct, marked by abrupt changes in water temperature, speed, and direction.(a) Meanders (eddies) form at this boundary as the Gulf Stream leaves the U.S. coast at Cape Hatteras. The meanders can pinch off (b) and eventually become isolated cells of warm water between the Gulf Stream and the coast (c). Likewise, cold cells can pinch off and become entrained in the Gulf Stream itself (d). (C = cold water, W = warm water; blue = cold, red = warm.)

Vertical Movement of WaterWind induced vertical circulation is vertical movement induced by wind-driven horizontal movement of water.

Upwelling is the upward motion of water. This motion brings cold, nutrient rich water towards the surface.

Downwelling is downward motion of water. It supplies the deeper ocean with dissolved gases.

Consider: West and East Winds

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Nutrient-Rich Water Rises near the Equator

Equatorial upwelling.

The South Equatorial Current, especially in the Pacific, straddles the geographical equator. Water north of the qequator veers to the right (northward), and water to the south veers to the left (southward). Surface water therefore diverges, causing upwelling. Most of the upwelled water comes from the area above the equatorial undercurrent, at depths of 100 meters or less.

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Thermohaline Flow and Surface Flow: The Global Heat Connection

The global pattern of deep circulation resembles a vast “conveyor belt” that carries surface water to the depths and back again. Begin with the formation of North Atlantic Deep Water north of Iceland, which flows south through the Atlantic and then flows over (and mixes with) deep water formed near Antarctica. The combined mass circumnavigates Antarctica and then moves north into the Indian and Pacific ocean basins. Diffuse upwelling in all of the ocean returns some of this water to the surface. Water in the conveyor gradually warms and mixes upward to be returned to the North Atlantic by surface circulation.

Water Masses May Converge, Fall, Travel across the Seabed, and Slowly RiseA model of thermocline circulation caused by heating in lower latitudes and cooling in higher latitudes. The thermocline at middle and low latitudes is “held up” by the slow upward movement of cold water.

The water layers and deep circulation of the Atlantic Ocean. Arrows indicate the direction of water movement. Convergence zones are areas where water masses approach one another.

The Arctic Sea:Relatively enclosed basin (connection to the Pacific through the Bering Strait and to the Atlantic through the Greenland and Norwegian Seas)

Enclosed nature influences ice cover

Circulation: was originally deduced from ice flows and drifting ships, supplemented with di t t t d t hidirect current measurements and geostrophic calculations

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Other Major Current Systems Keep In Mind:Coriolis Force on the Equator is zero

Coriolis Force by 0.5o influences flow of water

Currents To Know:North Equatorial Current (NEC)

South Equatorial Current (SEC)

Equatorial Counter Current (ECC)

E t i l U d C t (EUC)Equatorial Under Current (EUC)

Equatorial Undercurrent (EUC) & Eastward Directed Pressure Gradient

Wind driven water from the surface mixed layer piled on the western side of the basin

Wind stress balances the pressure gradient (Coriolis Force ~= 0 at equator)

Adjustment (depression) of the thermocline on the western end

Baroclinic conditions at depth drive a jet-like current eastward eventually balance by friction (eddy viscosity)

Waves: the ocean can respond to the winds in distant places by means of large-scale disturbances that travel as waves.

Barotropic: surface waves

Baroclinic: density surface (thermocline)

R b (Pl t W )Rossby (Planetary Waves)

Kelvin

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Examples of barotropic and baroclinic waves propagating through the ocean

Most tides are barotropic ‘Kelvin’ waves

Think about what would happen if the wind stress was dramatically reduced or changed directions in the case of the Asian Monsoon

Kelvin Waves

Travel eastward along the equator as a double wave ‘equatorial wave guide’

Travel along coasts (coast on right in the NH and on the left in the SH)

Balance between pressure gradient force and coriolis force.

Kelvin Waves

Surface equatorial kelvin waves travel ~200 m/s

Rossby radius of deformation L = c/f

•High latitudes smaller eddies closely trapped to the coast (increase in planetary vorticity)

•Low latitudes larger radius

Kelvin waves in the thermocline can have dramatic effects, particularly in low latitudes where the mixed surface layer is thin.

Northward migration of ITCZ in western Atlantic generates disturbance that propagates eastward

Splits into two coastal Kelvin waves when hits the eastern boundary

The region of the disturbance where the thermocline bulges upward cold nutrient rich sub-thermocline water can reach the surface

4-6 week travel time

Rossby Waves:

Propagate from east to west across basin

Travel along lines of latitude

Move slower than Kelvin waves

Conservation of Potential Vorticity

Example: Waves in the jet-stream

ENSO: El Nino – Southern Oscillation

“Interest in the phenomenon of El Nino goes back to the mid-19th century but it was the El Nino event of 1972-73 that stimulated large-scale research into climatic fluctuations, which began to be seen as a result of the interaction between atmosphere and ocean.”

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El Nino events are perturbations of the ocean-atmosphere system

Disturbance – a depression in the thermocline accompanied by a slight rise in sea-level propagates eastwards along the Equator as a pulse or series of pulses (Kelvin Waves)