## 8 April 2009

Earthquake waves
The chief tool to study the Earths interior are
waves from earthquakes.

Diamond anvil cell
To understand what happens to solids at high pressure,
one must try to subject solids to high pressure in the
lab.
One way to do this is with the diamond anvil cell.
(This is also a good way to shatter perfectly good diamonds!)

High pressure "gun"
Another way to produce high pressures in a lab is to
use a gun.
This gives high pressures, but only for a very short time.

Preliminary Reference Earth Model
(PREM)
Combining what we know of physics (equation of hydrostatic equilibrium, equation
of state of materials at various pressure etc) with what we know
from observations (mass and radius of Earth, behavior of
seismic waves etc) we can try to produce a self-consistent model
of physical conditions inside the Earth.
(Stellar astronomers use very similar ideas to make models of stars.)

This table shows some results of one such model.
One striking number is the central density of 13000 kg/m**3. This
is about 1.6 the lab density of iron, and shows the effects of
compression by the bulk of the Earth.
Iron may seem incompressible in a lab, but with enough pressure,
its density will increase, like air in a bicycle pump.

Graphs of Earth model
Graph X.42 shows some results of Earth model in graphical form.
(I don't know if the plotted numbers are from the PREM or another model.)
Graph X.43 shows some of the complications of seismic wave analysis,
which include wave reflections and refractions.

Temperature vs depth in Earth
The temperature structure reveals some interesting structure.
Near the surface (top 100 km or so) there is a large temperature
gradient, with T changing by 5-20 degrees every km you go down.
At around 100 km depth, the gradient quickly drops to something like
0.5 degree per km, which holds more or less all the way to the mantle- outer core
boundary.

The low temperature gradient in the mantle is due to tranport of heat by
convection, which is an efficient heat transport mechanism.
In the top 100 km, the rock is "brittle", and convection
is not possible- rather, heat transport is by conduction.