Using the method of characteristics, we can derive a system of ordinary differential equations that define the ray trajectories. To do so, we need to transform equation (16) to the following form:

(22) |

(23) |

where *s* is a running parameter along the ray, and it is related to traveltime as follows:

Using equation (16) to calculate the various derivates of *F*, we obtain the following
system of ordinary differential equations:

(26) |

(27) |

(28) |

and

where , , and , and the same holds for and (Figure 9

Figure 9 shows sixteen rays originating from a source on the surface at the
position *x*=0
for inhomogeneous models all of which have *v*_{v}=*v*=1.5+0.5 *z*+0.2 *x* km/s
and .These models differ in their shear wave velocities with rays given in the black curves corresponding to
the ratio, *r*, of the vertical *S*-wave to *P*-wave velocities of 0.5, and rays given in the gray curves to *r*=0.
The sixteen rays have ray parameters ranging from zero to the maximum value of 1/*V*_{h} (*V*_{h}
is the horizontal velocity), with a fixed ray-parameter spacing of 1/(15 *V*_{h}).
These rays terminate at the
same time of 8 s, and the wavefronts (given by the dashed curves) are plotted at about 1.6-s intervals.
The wavefronts corresponding to the different models are practically coincident. This implies that
traveltimes extracted from ray tracing are independent of the shear wave velocity, and the acoustic
ray equations derived above are almost as accurate as the conventional anisotropic ray tracing
equations Cervený and Hron (1980). The distribution of the rays also indicates that the geometrical
spreading features
of the two models are practically identical.

B

10/9/1997