2. The elastic wave equationSeismology and the Earth’s Deep Interior The Elastic Wave Equation  Elastic waves in infinite homogeneous isotropic media  Numerical simulations for simple sources  Plane wave propagation in infinite media  Frequency, wavenumber, wavelength  Conditions at material discontinuities  Snell’s Law  Reflection coefficients  Free surface  Reflection Seismology: an example from the Gulf of Mexico

3. The elastic wave equationSeismology and the Earth’s Deep Interior Equations of motion What are the solutions to this equation? At first we look at infinite homogeneous isotropic media, then:

4. The elastic wave equationSeismology and the Earth’s Deep Interior Equations of motion – homogeneous media We can now simplify this equation using the curl and div operators and … this holds in any coordinate system … This equation can be further simplified, separating the wavefield into curl free and div free parts

5. The elastic wave equationSeismology and the Earth’s Deep Interior Equations of motion – P waves Let us apply the div operator to this equation, we obtain where or P wave velocity Acoustic wave equation

6. The elastic wave equationSeismology and the Earth’s Deep Interior Equations of motion – shear waves Let us apply the curl operator to this equation, we obtain we now make use of and define to obtain Shear wave velocity Wave equation for shear waves

7. The elastic wave equationSeismology and the Earth’s Deep Interior Elastodynamic Potentials Any vector may be separated into scalar and vector potentials Shear waves have no change in volume P-waves have no rotation where F is the potential for P waves and Y the potential for shear waves

8. The elastic wave equationSeismology and the Earth’s Deep Interior Seismic Velocities Material and SourceP-wave velocity (m/s)shear wave velocity (m/s) Water15000 Loose sand1800500 Clay1100-2500 Sandstone1400-4300 Anhydrite, Gulf Coast4100 Conglomerate2400 Limestone60303030 Granite56402870 Granodiorite47803100 Diorite57803060 Basalt64003200 Dunite80004370 Gabbro64503420

9. The elastic wave equationSeismology and the Earth’s Deep Interior Solutions to the wave equation - general Let us consider a region without sources Where n could be either dilatation or the vector potential and c is either P- or shear-wave velocity. The general solution to this equation is: Let us take a look at a 1-D example

10. The elastic wave equationSeismology and the Earth’s Deep Interior Solutions to the wave equation - harmonic Let us consider a region without sources The most appropriate choice for G is of course the use of harmonic functions:

11. The elastic wave equationSeismology and the Earth’s Deep Interior Solutions to the wave equation - harmonic … taking only the real part and considering only 1D we obtain cwave speed kwavenumber lwavelength Tperiod wfrequency Aamplitude

12. The elastic wave equationSeismology and the Earth’s Deep Interior Spherical Waves Let us assume that h is a function of the distance from the source where we used the definition of the Laplace operator in spherical coordinates let us define to obtain r with the known solution

13. The elastic wave equationSeismology and the Earth’s Deep Interior Geometrical spreading so a disturbance propagating away with spherical wavefronts decays like... this is the geometrical spreading for spherical waves, the amplitude decays proportional to 1/r. r If we had looked at cylindrical waves the result would have been that the waves decay as (e.g. surface waves)

14. The elastic wave equationSeismology and the Earth’s Deep Interior Plane waves... what can we say about the direction of displacement, the polarization of seismic waves?... we now assume that the potentials have the well known form of plane harmonic waves shear waves are transverse because S is normal to the wave vector k P waves are longitudinal as P is parallel to k

15. The elastic wave equationSeismology and the Earth’s Deep Interior Heterogeneities.. What happens if we have heterogeneities ? Depending on the kind of reflection part or all of the signal is reflected or transmitted.  What happens at a free surface?  Can a P wave be converted in an S wave  or vice versa?  How big are the amplitudes of the  reflected waves?

16. The elastic wave equationSeismology and the Earth’s Deep Interior Wavenumber, slowness, phase velocity

17. The elastic wave equationSeismology and the Earth’s Deep Interior Reflection at an interface

18. The elastic wave equationSeismology and the Earth’s Deep Interior Boundary Conditions... what happens when the material parameters change? r 1 v 1 r 2 v 2 welded interface At a material interface we require continuity of displacement and traction A special case is the free surface condition, where the surface tractions are zero.

19. The elastic wave equationSeismology and the Earth’s Deep Interior Reflection and Transmission – Snell’s Law What happens at a (flat) material discontinuity? Medium 1: v 1 Medium 2: v 2 i1i1 i2i2 But how much is reflected, how much transmitted?

20. The elastic wave equationSeismology and the Earth’s Deep Interior Reflection and Transmission coefficients Medium 1: r1,v1 Medium 2: r2,v2 T Let’s take the most simple example: P-waves with normal incidence on a material interface A R At oblique angles conversions from S-P, P-S have to be considered.

21. The elastic wave equationSeismology and the Earth’s Deep Interior Reflection and Transmission – Ansatz How can we calculate the amount of energy that is transmitted or reflected at a material discontinuity? We know that in homogeneous media the displacement can be described by the corresponding potentials in 2-D this yields an incoming P wave has the form

22. The elastic wave equationSeismology and the Earth’s Deep Interior Reflection and Transmission – Ansatz... here a i are the components of the vector normal to the wavefront : a i =(cos e, 0, -sin e), where e is the angle between surface and ray direction, so that for the free surface where P PrPr SV r e f what we know is that

23. The elastic wave equationSeismology and the Earth’s Deep Interior Reflection and Transmission – Coefficients... putting the equations for the potentials (displacements) into these equations leads to a relation between incident and reflected (transmitted) amplitudes These are the reflection coefficients for a plane P wave incident on a free surface, and reflected P and SV waves.

24. The elastic wave equationSeismology and the Earth’s Deep Interior Case 1: Reflections at a free surface A P wave is incident at the free surface... P P SV i j The reflected amplitudes can be described by the scattering matrix S

25. The elastic wave equationSeismology and the Earth’s Deep Interior Example

26. The elastic wave equationSeismology and the Earth’s Deep Interior Case 2: SH waves For layered media SH waves are completely decoupled from P and SV waves There is no conversion only SH waves are reflected or transmitted SH

27. The elastic wave equationSeismology and the Earth’s Deep Interior Example

28. The elastic wave equationSeismology and the Earth’s Deep Interior Case 3: Solid-solid interface To account for all possible reflections and transmissions we need 16 coefficients, described by a 4x4 scattering matrix. P PrPr SV r PtPt SV t

29. The elastic wave equationSeismology and the Earth’s Deep Interior Case 4: Solid-Fluid interface At a solid-fluid interface there is no conversion to SV in the lower medium. P PrPr SV r PtPt

30. The elastic wave equationSeismology and the Earth’s Deep Interior Reflection coefficients - example

31. The elastic wave equationSeismology and the Earth’s Deep Interior Refractions – waveform effects

32. The elastic wave equationSeismology and the Earth’s Deep Interior Reservoir example

33. The elastic wave equationSeismology and the Earth’s Deep Interior Example: Gulf of Mexico

34. The elastic wave equationSeismology and the Earth’s Deep Interior Summary  Reflection and transmission coefficients can be derived using plane waves and boundary conditions  Cases include:  solid-solid  solid-fluid  fluid-solid  solid-free surface  fluid-free surface  The angular dependence of R-T coefficients is complex. Their behaviour allows constraining the change of physical properties.