1. Geology 5640/6640 Introduction to Seismology 30 Jan 2015 © A.R. Lowry 2015 Read for Mon 2 Feb: S&W 53-62 (§2.4); 458-462 Last time: The Equations of Motion (Wave Equation!) Any imbalance of stress will be offset by acceleration (Newton’s 2 nd : ). This leads to the dynamic equations of motion : We neglect the body force f i (for now) and express in terms of displacement, by substituting Hooke’s law and the definition of the strain tensor. This results in the P-wave equation : in which  is the propagation velocity :

2. This is the wave equation for dilatations only (i.e., a P-wave!) and is more commonly written: where: represents the propagation velocity ! (Note the units: sqrt(Pa (kg m -3 ) -1 ) = sqrt (kg m -1 s -2 kg -1 m 3 ) = sqrt (m 2 /s 2 ) or just m/s). If we recall moreover that We can write in terms of displacement as:

3. We arrived at the P-wave equation using by taking the derivative with respect to x i and summing over i. We could instead take derivatives with respect to x j and by a similar set of steps arrive at: the S-wave equation, in which the S-wave propagation velocity is given by Note the important implication: For the P-wave we have dilatation, but no shear; for the S-wave we have shear, but no dilatation!

4. Here and represent the propagation velocities for the P and S waves respectively. Changes in elastic properties contribute more to velocity variation than changes in density Velocity is sensitive to rock chemistry, packing structure, porosity & fluid type, pressure and temperature. The tricky part is distinguishing which we’re seeing…

5. Rock properties that affect seismic velocity include: Porosity Rock composition Pressure Temperature Fluid saturation  = V p,  = V s are much more sensitive to and  than to  Crustal Rocks Mantle Rocks

6. Partial MeltComposition Porosity/Fluid Temperature Pressure Seismic velocity depends on a lot of fields, but not all are independent: And some fields can be determined to within small uncertainty (e.g. pressure at given depth) Density Velocity

8. So now we have our expressions for the wave equation in terms of displacements: Question is, how do we solve these? Solution is simplified by expressing displacements u in terms of displacement potentials. Helmholtz’ decomposition theorem holds that any vector field u can be expressed in terms of a vector potential  and a scalar potential  as: In our application,  is a scalar displacement potential associated with the P-wave, and  is a vector displacement potential associated with the S-wave.

9. It’s first worth noting a pair of useful vector identities : Then, if we substitute our potentials into our P-wave equation: Rearranging: And hence:

10. Similarly, substituting potentials into the S-wave equation: Here we take advantage of another vector identity: Rearranging: And hence:

11. So what’s the point of this? We want to find some solution, e.g. for P-wave displacement potential, that allows for separation of variables : The eigenfunctions for a partial differential equation of this form (i.e., functions which, if plugged into the equation, will yield solutions of similar form) are: (called the “d’Alembert solution”). Here, i is the imaginary number A is amplitude  is angular frequency 2  /T (& T is time period) k is spatial wavenumber 2  / (& is wavelength)