Figure 3 The rays forming overlying the initial velocity model.
For this experiment we are limiting ourselves to a 2-D earth model. As shown in Figure , our selected set of earthquakes are approximately oriented along the receiver line. For this experiment we assume constant velocity out of plane. We do 2-D ray tracing and then correct all lengths by
Each arrival time also has a variance associated with it. The inverse of these variances form a noise covariance operator for the inversion. We invert for the change in slowness by minimizing the fitting goal,