# Interpreting marine refraction data

Series | Geophysical References Series |
---|---|

Title | Problems in Exploration Seismology and their Solutions |

Author | Lloyd P. Geldart and Robert E. Sheriff |

Chapter | 11 |

Pages | 415 - 468 |

DOI | http://dx.doi.org/10.1190/1.9781560801733 |

ISBN | ISBN 9781560801153 |

Store | SEG Online Store |

## Problem 11.17

How many distinct separate head waves are indicated in Figure 11.17a, and what are their apparent velocities? Calculate the depths and velocities of the respective refractors, assuming (i) no dip, (ii) dip to the right, (iii) dip to the left.

### Solution

We take at as the source and the geophone at km as . Four wavetrains are observed (Figure 11.17b). The slowest (which one has to view at grazing incidence to pick) has an apparent velocity of about 1.40 km/s; the arrival time at is off scale. This is the direct water wave, but its velocity is low for water, perhaps because of interference with a dispersive channel wave, loss of early cycles, or because the distance (calculated from water-borne direct waves seen at a floating sonobuoy) is not exact. Because of the uncertainty in the traveltime, we shall use the value 1.50 km/s for the water velocity.

The next event (L) has an apparent velocity of about 1.70 km/s and an arrival time of 6.84 s; the intercept time is difficult to determine because the event seems to be curved. It is probably a head wave at or near the sea floor.

The next fastest refraction (M) has an apparent velocity of about 2.19 km/s between and 4 km and an apparent velocity of 2.67 km/s for km; this change in velocity may be due to a change in dip or it may indicate the presence of two separate events. We shall consider only the velocity 2.67 km/s, the travel time being 5.38 s, and the intercept time 0.95 s.

Refraction N has a linear alignment and an apparent velocity of 5.45 km/s, traveltime of 3.97 s, and an intercept of 1.77 s; it is probably from a basaltic basement surface.

The measured data are:

If L is a head wave, the intercept time should be s. Thus we conclude that L is not a head wave from a planar refractor; it may be a dispersive water wave or part of a reflection, but we have insufficient data to identify it. Disregarding L, we are left with only the water layer and the two refractors M and N.

**(i) Assuming no dip:**

**Refraction M**

We have the following data: km/s, km/s, s.

Then,

**Refraction N:**

**(ii) Assuming dip to the right**

In this case, the profile is in the downdip direction, the arrival times, velocities, and intercept times are unchanged except that the velocities are now apparent velocities and the intercept times give slant depths normal to the beds. Note that the water depth increases to the right because horizon M dips to the right.

**Refractor M**

We have: km/s, km/s, , s. Using equation (4.24d), we write

(this is the slant water depth at ).

**Refractor **

We could use Adachi’s method (problem 11.5), but the given data are not in a form suitable for this method. Instead we shall strip off (problem 11.6) the surface layer after which we have two parallel horizons, and therefore can use equation (4.18a) to solve for horizon N.

The slant depth of horizon M at the source is 0.82 km. At the slant depth is

Thus to locate horizon M we swing arcs at and with radii 0.82 and 1.87 km, respectively, then draw horizon M tangent to the arcs (see Figure 11.17c).

To solve for N, we need the total time that the refraction from N spends in the water layer. For this we need the angle of approach to the surface of head wave N. Equation (4.2d) states that the angle of approach is given by

Figure 4.2c shows that is relative to the vertical, so if the ray emerges from horizon M at the angle of refraction , , whereas the angle at which the ray left source is . Therefore we draw a ray from down to M at the angle to the vertical and another down from to M at the angle to the vertical (see rays and in Figure 11.17c). The total length () is () km; dividing by 1.50 gives 1.73 s to be subtracted from , leaving s for the traveltime relative to M. Also the distance km. The intercept times for both M and N are based on the normals to the beds; since the beds are parallel, we can subtract from [see part (i)] to get , the intercept time of N for the virtual source . This gives s.

We must correct the apparent velocity km/s. We write this as s/km. The event N in Figure 11.17b is linear from to beyond km, so we write s/km. The numerator is the difference between at and 6 km, and Figure 11.17c shows that the correction is s. Thus s. The correction to is negligible, so we get km/s.

We can now get the depth of N below M. We have

Because horizons M and N are parallel, we find the intercept time of N relative to M by subtracting the intercept times in part (i), so

Thus

Then, since the depth of M at is 0.82 km,

**(iii) Assuming dip to the left**

Because of the shallow depth of M we check to see where it outcrops. The horizon M passes through the point , (see part (ii)) with slope , Thus it will outcrop at km. But Figure 11.17c shows that event M exists at offset of 12 km, hence the assumption of dip to the left is not consistent with the given data.

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Refraction blind spot | Spatial sampling restrictions |

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Geologic interpretation of reflection data | 3D methods |

## Also in this chapter

- Salt lead time as a function of depth
- Effect of assumptions on refraction interpretation
- Effect of a hidden layer
- Proof of the ABC refraction equation
- Adachi’s method
- Refraction interpretation by stripping
- Proof of a generalized reciprocal method relation
- Delay time
- Barry’s delay-time refraction interpretation method
- Parallelism of half-intercept and delay-time curves
- Wyrobek’s refraction interpretation method
- Properties of a coincident-time curve
- Interpretation by the plus-minus method
- Comparison of refraction interpretation methods
- Feasibility of mapping a horizon using head waves
- Refraction blind spot
- Interpreting marine refraction data