6. cooling of the ocean plates (lithosphere) william wilcock
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OCEAN/ESS 410. 6. Cooling of the Ocean Plates (Lithosphere) William Wilcock. Lecture/Lab Learning Goals. Understand the terms crust, mantle, lithosphere and asthenosphere and be able to explain the difference between oceanic crust and lithosphere - PowerPoint PPT PresentationTRANSCRIPT
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6. Cooling of the Ocean Plates (Lithosphere)
William Wilcock
OCEAN/ESS 410
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Lecture/Lab Learning Goals• Understand the terms crust, mantle, lithosphere and
asthenosphere and be able to explain the difference between oceanic crust and lithosphere
• Understand the concepts that govern the relationships that describe the cooling of a halfspace.
• Be able to use h≈√κt or equivalently t=h2/κ• Know how heat flow is measured and how it varies with
the age of the ocean lithosphere.• Understand the relationship between ocean depth and
plate age • Be able to obtain and fit a profile of seafloor bathymetry
to a square root of age model - LAB
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Oceanic Plates form by Cooling
Mantle melt
adiabatically rising mantle material
magma
MOR
Mantle
sediments, cold crust & mantle
island arctrench
earthquakes
ocean crust earthquakescontinental crust
melt
fracture zone
trench
1300°C
Heat Loss
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Chemical &
Composition
Geophysical
Crust/Mantle versus Lithosphere/Asthenosphere
1000°C
1300°C
Thermal and mechanical structure
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TerminologyOceanic Crust - Obtained by partial melting of the mantle (~6 km thick)It is a chemical boundary layer
Lithosphere - The upper rigid layer that has cooled below ~1000ºC. It is the rigid layer that defines the plate. It thickens with age and approaches 100 km at 100 MirIt is a mechanical boundary layer and a thermal boundary layer.
Asthenosphere - The region immediately underlying the lithosphere (from ~100 - 200 km depth) is weak (has a low viscosity). This is because it lies near its melting point.
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1300°C
Wet S
olidus
Dry S
olidus
Geothermfor Old Ocean Plate
Asthenosphere
Lithosphere
Temperature-Depth Plot for
Mantle Beneath Old Oceanic
Plates
The solidus is the temperature at which a rock first starts to melt. The mantle contains a small amount of water (<1%) which lowers the solidus temperature.
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The Lithosphere Forms by Conductive Cooling
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Heat Conduction
Fourier’s Law
Heat Flux, W m-2
Negative because heat flows down the temperature gradient
Thermal Conductivity, W K-1m-1
Typical values•Aluminum, 237 W K-1m-1
•Expanded Polystyrene, 0.05 W K-1m-1
•Rocks 1 to 5 W K-1m-1
Temperature gradient, K m-1
Temperature, T
Depth, y
Heat Flow
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Because the heat flow is vertical, the cooling of any column of the oceanic lithosphere is the equivalent to the cooling of a half space. The relationship between age, t and horizontal position x is
t = x / u
where u is the half spreading velocity
Cooling of a column of the lithosphere
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Cooling of a Half-space
T
Dep
th
y, km
TmT0
y, km
TmT0
y, km
TmT0
t = 0- t = 0+ t > 0
Temperature
The math is quite complex but we can gain some insight into the form of the solution from the simple thought experiment that we considered during the last lecture.
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How Quickly Do Objects Cool By Heat Conduction?
The green object contains twice as much heat energy (because it is twice as thick), but looses heat at only half the rate (because the temperature gradient is halved). It takes four times as long to cool the green object.
It takes four times as long to cool to twice the depth.
A simple thought Experiment
Depth
TemperatureT1 T
2
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Approximate Thickness of the Cooled LayerThe exact shape of the curves is difficult to derive but we can write an approximate thickness for the cooled region as
where κis the thermal diffusivity and has an a value of 10-6 m2 s-1
For example at t = 60 Myr (= 60 x 106 x 365 x 86400 s)
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60 Myr
35 km
70 km
15 MyrTemperature Profiles
(Geotherms) at 2 different
ages
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Consequences of Plate Cooling1. Heat Flow
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Heat Conduction
Fourier’s Law
Heat Flux, W m-2
Negative because heat flows down the temperature gradient
Thermal Conductivity, W K-1m-1
Typical values•Aluminum, 237 W K-1m-1
•Expanded Polystyrene, 0.05 W K-1m-1
•Rocks 1 to 5 W K-1m-1
Temperature gradient, K m-1
Temperature, T
Depth, z
Heat Flow
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Heat Flow Probe
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Heat Flow Measurements
Thermistors. Measure temperature gradient
Heater. After measuring the thermal gradient a pulse of heat is introduced and the rate at which it decays is can be used to estimate the thermal conductivity.
Seafloor
Requires Sediments - Difficult near the ridge
Average value for the oceans is ~100 mW m-2
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Heat Flow Versus Age1
hfu
(h
eat
flo
w u
nit)
= 4
2 m
W m
-2
Model Exceeds Observations. Hydrothermal cooling
Mean Value
Range of Values
Prediction of the half space model
Observations exceed model. Plate reaches maximum thickness
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Plate Cooling ModelThe lithosphere has a maximum thickness of ~100 km. Convective instabilities in the asthenosphere prevent it growing any thicker
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Consequences of Plate Cooling2. Seafloor Depth
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Seafloor Depth
Hot, ρ = 3300 kg m-3
Cool , ρ = 3400 kg m-
3
The depth of the seafloor can be calculated using the principal of isostacy - different columns contain the same mass (i.e., the lithosphere floats). Because warm rocks have a lower density (denoted by the symbol ρ) than cold ones, the seafloor is shallower above young ocean lithosphere.
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Seafloor Depth Versus AgeThe half-space model predicts that the depth increases as the square root of age. This model works out to about 100 Myr at which point depths remain fairly constant (more evidence for the plate model)
Misfit suggests Plate model
Half-Space model
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Age of the Seafloor - Inferred from Magnetic Lineations
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Revisiting Lab 2
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Age of Surface (billions of years)
4 3 2 1
Rel
ativ
e am
ount
of
surf
ace
are
a
Planetsform
2/3 of Earth’s surface formedwithin the last 200 million years
Age of Terrestrial Planet Surfaces
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EarthPlate tectonics replace 2/3 of the surface every ~100
Myr and modifies the remaining 1/3 on geologically short timescales.
Evidence at a scale we might see on other planets
1. Linear rifts and arcuate compression zones
2. Transform faults and fracture zones (adjacent transform faults are parallel).
3. Continuous plate boundaries
4. Volcanic Island chains - plates moving over fixed mantle plume (melt source)
5. Topography variations consistent with aging plates.
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Global Bathymetry
Sandwell and Smith
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Mars
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Mars
•Last eruption on Olympus Mons 2 to ~100 Myr ago •Surface appears to be one plate•Evidence for plate tectonics in the past is controversial
•Smaller radius means it cooled down quicker than earth and the lithosphere (the rigid cold layer) is thicker - too strong for plate tectonics•Large volcanoes show surface has not moved relative to mantle plumes
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Mantle Convection in Mars
model by Walter Kiefer
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Venus
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VENUS•Burst of volcanism 600-700 MYrs ago•Either steady state ‘plate tectonics’ stopped then or Venus undergoes episodic bursts of volcanism
•Venus has lost its water. •Water in the mantle may be critical for plate tectonics because it weakens the mantle and lubricates the motion of the plates.•In the absence of lubrication the heat from radioactivity may build up inside Venus until it is released in catastrophic mantle overturning events.
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1300°C
Wet S
olidus
Dry S
olidus
Geothermfor Old Ocean Plate
Asthenosphere
Lithosphere
Temperature-Depth Plot for
Mantle Beneath Old Oceanic
Plates
The solidus is the temperature at which a rock first starts to melt. The mantle contains a small amount of water (<1%) which lowers the solidus temperature.