A. Travel Time, Reflection, Refraction of P & S Waves

1. Travel time of body waves gives us VP, VS, and  (density) as a function of depth.

2. Velocity of P & S waves increases with depth.

• Lower density than oceanic crust.

• Higher density than continental crust.

• Crust floats in equilibrium on the denser mantle beneath.

b. Low velocity zone: Convection in mantle distributes heat evenly.

• Pressure changes the crystal structure of minerals causing a slow in seismic wave velocity.

d. Outer core boundary is 2900 km deep.

• TM: Melting temperature of ultramafic rocks.

• S waves cannot propagate through the outer core (liquid).

A. Intensity: Intensity scales measure the effects rather than the energy release of an earthquake.

2. Body waves spread and travel as a sphere.

a. We can adjust this to maximize signal to form two frequency bands.

4. Example: Waves came in at about 45 on the up and NE direction.

1. Not always accurate; local geology (soils, rocks) affect shaking intensity.

Some topics in this essay:
Scale Mathematical, PKIKP PKJKP, Teleseismic Seismograms, Interseismic Deformation, Intensity Maps, Aftershocks Foreshocks, XII Earthquakes, Shadow Zones, Pyroxene Low, Resonant Frequency, = wave, inner core, outer core, main shock, body waves, = wave inner, short period, crust •, wave inner, fault slip, wave inner core, fault slip rate, seismic waves, continental crust •, = 20 sec,