|Series||Geophysical References Series|
|Title||Problems in Exploration Seismology and their Solutions|
|Author||Lloyd P. Geldart and Robert E. Sheriff|
|Store||SEG Online Store|
- 1 Chapter 7 Seismic equipment
- 2 7.1 Radiolocation errors because of velocity variations
- 3 7.2 Effect of station angle on location errors
- 4 7.3 Transit satellite navigation
- 5 7.4 Effective penetration of profiler sources
- 6 7.5 Directivity of linear sources
- 7 7.6 Sosie method
- 8 7.7 Energy from an air-gun array
- 9 7.8 Dominant frequencies of marine sources
- 10 7.9 Effect of coil inductance on geophone equation
- 11 7.10 Streamer feathering due to cross-currents
- 12 7.11 Filtering effect of geophones and amplifiers
- 13 7.12 Filter effects on waveshape
- 14 7.13 Effect of filtering on event picking
- 15 7.14 Binary numbers
Chapter 7 Seismic equipment
7.1 Radiolocation errors because of velocity variations
Ground conductivity affects radio-wave velocity because of currents induced in the earth. Range calculations assuming that travel is over normal seawater thus may be in error if this is not true. What errors are involved for travelpaths over the terrains in Table 7.1a?
|Dry sand||299 900|
Radio-navigation methods are used to determine distances in marine surveys and the velocity is generally assumed to be that over saltwater.
Let be velocity over normal seawater and velocity over other terrains. If we use to calculate ranges, the error in range calculations will be and the relative error is m/km. When , the error will be positive, meaning that the calculated range is too great. The results are shown in Table 7.1b.
|Terrain||Velocity (km/s)||Error (m/km)|
|Dry sand||299 900||–0.8|
7.2 Effect of station angle on location errors
If the error in Shoran time measurements is , what is the the size of the parallelogram of error in Figure 7.2a when (a) and (b) ? Take the velocity of radio waves as km/s.
Shoran is a radio-navigation device which measures the 2-way traveltime between the point of observation and a fixed station. Using two fixed stations, the point of observation can be located by swinging arcs centered at the two stations; for large distances the arcs become nearly straight lines.
The traveltimes are subject to error , so the ranges are , , 2. Swinging the four arcs corresponding to these time values, we get a parallelogram of error such as that in Figure 7.2a; the location lies somewhere inside this parallelogram.
In Figure 7.2a, the error in range
The long diagonal m.
The short diagonal m.
To get the figure for we merely reverse the arrow on or ; therefore the error values are the same as for .
7.3a Determine the acceleration of gravity at the orbit of a Transit satellite 1070 km above the Earth, knowing that at the surface of the Earth is 9.81 m/s, and that the gravitational force varies inversely as the square of the distance between the centers of gravity of the masses. The radius of the Earth is 6370 km.
A satellite is in a stable orbit around the Earth when the gravitational force pulling it earthward equals the centrifugal force , where is the acceleration of gravity, and the satellite’s mass and velocity, and the radius of its orbit about the center of the Earth.
The radius of the satellite’s orbit is km. Since is proportional to the force of gravity, at the satellite’s orbit,
7.3b What is the satellite’s velocity if its orbit is stable?
For a stable orbit, the gravitational acceleration is balanced by the centripetal acceleration.
7.3c How long does it take for one orbit?
The length of the nearly circular orbit is km, so the time for one orbit is
7.3d How far away is the satellite when it first emerges over the horizon?
In Figure 7.3a, is the point of observation. The satellite first becomes visible when it reaches the tangent to the Earth at . The tangent is normal to the radius at , so
7.3e What is the maximum time of visibility on a single satellite pass?
In Figure 7.3a the angle subtended at the center of the Earth by is
The satellite is visible while it traverses an arc subtending . Since the entire orbit is traversed in 6395 s, the time of visibility is minutes, 25 seconds.
7.4 Effective penetration of profiler sources
7.4a Sieck and Self (1977) summarize “acoustic systems” as shown in Table 7.4a. For each of these systems, calculate the wavelengths and penetration depths given by Denham’s (1982) rule, that the maximum useable frequency is , where = traveltime. Reconcile your results with the stated purposes.
|Fathometers||12–80||To map water bottom|
|Water-column bubble detectors||3–12||To locate bubble clusters, schools of fish|
|Side-scan sonar||38–250||To map bottom irregularities|
|Tuned transducers||3.5–7.0||To penetrate 30 m|
|Imploders||0.8–5.0||To penetrate 120 m, find gas-charged zones|
|Sparkers||0.04–0.15||To map 1000|
Acoustic systems include several devices that use sound waves to measure distances in water. Transducers emit sound waves, usually short pulses, the travel-times of which are used to measure distances. Fathometers are transducers that emit and record high-frequency pulses (usually about 100 kHz); they determine water depth from the two-way traveltime of the sea-floor reflection. Fathometers have little penetration, but similar devices using frequencies in the range kHz may penetrate as much as 30 m.
Side-scan sonar utilizes a towed transducer that emits high-frequency pulses and measures the traveltime of energy back-scattered by irregularities on the bottom.
The sparker is an energy source using the discharge of a large capacitor to create an electric arc between two electrodes in water, the sudden vaporization of the water being equivalent to an explosion.
Imploders create voids in the water and the effect of water rushing into the voids is to generate seismic waves; an example is the water gun which has two chambers, one being filled with air at high pressure, the other containing water; release of the air into the water chamber forces the water out at high velocity, thus creating voids into which the surrounding water collapses.
Denham (1982) devised an empirical rule relating the maximum useable frequency to the two-way traveltime : , the useful frequency cutoff being determined by the increased absorption of higher frequencies and the background noise level. Note that high-frequency loss in water is very small, so the time is that below the seafloor.
We assume a value 1500 m/s for the velocity of sound in water, so . Taking as the depth of penetration, Denham’s rule gives where is in kilohertz. The results are given in Table 7.4b.
|System||Frequency (kHz)||Wavelength (m)||Penetration depth (m)|
Maximum penetration is given by the energy that the systems inject into the earth, higher frequency systems generally giving less energy. The bubble detector might locate a cluster of bubbles or a school of fish, but certainly not individual bubbles or individual fish.
7.4b Trade literature claims 30-cm resolution with imploders and 2–5 resolution with sparkers. How do these figures compare with the resolvable limits?
The resolvable limit (see problem 6.18) is and using the shorter wavelengths in Table 7.4b gives resolvable limits of 0.5 to 0.08 m for imploders and 9.5 to 2.5 m for sparkers. Thus the claims in the trade literature are reasonable.
7.5 Directivity of linear sources
7.5a In Figure 7.5a, a linear vertical source (such as a column of explosives) of length , being a constant and the wavelength, is activated at all points simultaneously at time . Taking the initial waveform as , show that the effect at point is
What is the array response?
A distributed source can be thought of as an array. The array response is the ratio of the output of an array to the output when all of the elements are concentrated at the midpoint of the array.
Detonating cord is an explosive cord with a constant velocity of detonation; it is used to connect two charges in order to delay detonation of the second charge. Detonation of the first charge initiates detonation in the cord, which in turn detonates the second charge. By varying the length of cord, detonation of the second charge can be delayed a desired amount.
Although the explosive is exploded instantaneously, energy from different parts of the column arrive at at different times because they must travel different distances. Denoting by , the total effect at at time will be
To integrate we must get a relation between and . We assume that ; then
Noting that and , this becomes
where sinc .
If the linear source is replaced by a concentrated source of equal strength at the center , the effect at would be . Dividing the right-hand side of equation (7.5c) by this quantity, we get for the array response
7.5b An explosion initiated at the top of the explosive column in Figure 7.5a travels down the column with velocity . Show that the array response is
where is the velocity in the rocks. Under what circumstances does equation (7.5e) reduce to equation (7.5d)?
In part (a), the entire column exploded at . We now consider the case where the explosion starts at point and travels down the column with velocity , that is, the explosion starts at at , where . Writing , , the wave generated by the element dz arrives at with the phase Using equation (7.5b) the phase becomes
Assuming a harmonic wave function , we can write
where amplitude, , . Integrating, we obtain
If we locate the same amount of explosive at and explode it at , we get at
hence the array response is
Omitting the first factor, which is independent of and and hence is merely a scale factor, we have
[The minus sign for sinc occurs here and not in equation (7.5d) because the direction of integration is opposite to that assumed in deriving equation (7.5d)]. For an instantaneous explosion the result is given by equation (7.5d), namely
Equation (7.5c) reduces to equation (7.5d) whenever . For , i.e., for rays traveling almost vertically downward, the required condition is that . For most explosives, km/s, so should be no more than about 1.5 km/s, the velocity of water, for the two equations to give nearly the same result.
7.5c Calculate the array response for a column 10 m long, given that m, km/s, km/s, and , , , .
Differences in directivity are negligible when the charge length is much smaller than the wavelength.
7.5d If the column in part (c) is replaced by six charges, each 60 cm long and equally spaced to give a total length of 10 m, the charges being connected by spirals of detonating cord with detonation velocity 6.2 km/s, what length of detonating cord must be used between adjacent charges to achieve maximum directivity downward?
Let be the length of detonating cord between successive charges; maximum directivity downward is achieved when the traveltime through the explosive column is the same as that in the adjacent rocks. In part (c) we were given km/s, km/s, so , hence m.
7.5e What are the relative amplitudes (approximately) of the waves generated by the explosives in part (d) at angles , , , and when m?
An approximate solution can be obtained by assuming that the average velocity is equal to ; this means that the traveltime down through the 10 m column of explosives is the same as that for a wave in the adjacent 10 m of rock. In this case, , and
7.6 Sosie method
7.6a Imagine an impulsive source striking the ground at times apart, where is a random number between 10 and 20, and is the sampling interval. Assume reflections with arrival times and amplitudes as follows:
Each new impact generates the reflection sequence.
One wants the reflections for each impact to add constructively, so Sosie processing involves adding the geophone responses for several impacts after each response has been shifted so that is the same for the responses from all the impacts. Add the reflection sequences as would be done in Sosie recording for 10, 20, and 30 impulses to see how the signal builds up as the multiplicity increases.
The Sosie method often uses impactors as seismic sources. Each impactor strikes the ground at random intervals 5 to 10 times per second for approximately 3 minutes, a total of 900–1800 impacts, the times between impacts being much shorter than the reflection wavetrain. Each impact generates the reflection sequence. The reflections from each impulse are much smaller than the noise but the Sosie process builds up the reflections systematically while the noise partially cancels.
In digital recording, an analog signal is measured at fixed intervals , called the sampling interval; is usually 1 or 2 ms. Table 6.22a is a table of random numbers.
We obtained 29 random numbers in the 10–20 range by reading systematically from Table 6.22a, using even or odd values to determine the tens place and every 4th digit to give the units place. We used these numbers as the time intervals between 30 successive impacts. The impact times we used are listed in Table 7.6a.
The time required for 30 impacts separated by about plus the record length means that we have about 500 samples. We have made the impact intervals about 1/3 of the length of the reflection wavetrain.
Table 7.6b lists for the first ten impulses the signal sequences starting at each impulse time, each sequence having length , hence they overlap. is the sum of the signal values occurring at time . Toward the right, subsets of are listed, each being long, each subset constituting noise for the other subsets. Finally the subsets are summed. Figure 7.6a shows the reflection wavetrain and the result of summing the first 10, 20, and 30 impulses. (The data for the impulses 11–30 are not listed.)
Note the result for the two smallest reflections with amplitudes , that is, the 3rd (negative) reflection at and the 5th at ; the 3rd shows up clearly, but the 5th is no larger than the “noise,” which in this exercise is that caused by the overlapping signals. The noise is attenuated relative to the reflections as more sequences are added.
7.6b In part (a), we examined how the reflection sequence builds up. We now examine the effect of random noise by adding random noise values between to the signal. We obtain these from a random-number table by some scheme, such as systematically selecting pairs of numbers and changing the first member of each pair to a minus sign whenever it is odd and to a plus sign whenever it is even. The signal sequence has an rms value of 2.7, so adding noise values within the range (rms value 3.9) gives a signal/noise ratio of about 0.7.
The first page of our worksheet is shown as Table 7.6c. The first column is the sample number , the 2nd is the signal sequence from Tables 7.6a,b, the 3rd is the added noise, and the fourth the sum of the signal and noise. The signal plus noise subsets, each starting at the time of a source impact, are listed to the right followed by their sum.
The first 45 members of 30 subsets, each starting at one of the impulses, is shown in Table 7.6d. Summations for 10, 20, and 30 of the subsets are shown in Table 7.6e and in Figure 7.6b.
Examination of the numbers in the signal + noise columns in Table 7.6c indicates the difficulty of finding any of the signals. Table 7.6e lists the sums of the first subset, the first two subsets, then the first 4, 10, 20, and 30 subsets, with the times of the signals underlined. The first member of the signal sequence, which considerably exceeds the average noise, becomes distinguishable with the addition of only a few subsets, whereas the two smallest signal members (at times 13 and 33) still do not stand out even after summing 30 subsets. The broad, smeared-out peak between times 14 and 18, which corresponds roughly to the repetition rate of the impulses, would probably be erroneously interpreted as the interference of several reflections.
7.7 Energy from an air-gun array
How much energy is released (approximately) by the air-gun array in Figure 7.7a when the input pressure is 2000 psi (14 MPa)? Assume that the change is adiabatic, that is, constant, where , are pressure and volume, that the final pressure is 2 atmospheres, and that the guns are far enough apart that they do not interact.
An air gun consists of two chambers, both filled with air at high pressure. The two chambers are connected by a shuttle that is held in a closed position. When the restraining force is suddenly diminished the shuttle moves, allowing the air to vent into the water, creating the effect of an explosion. The energy release depends upon the change in air pressure and the volume of the chambers that discharge air into the water; the latter is usually given in cubic inches.
Energy released work done by expanding gas . For an adiabatic change, or . Thus,
7.8 Dominant frequencies of marine sources
The dominant period of a marine seismic source is often determined by the source depth; this is the case when the second half-cycle of the downgoing wave is reinforced
by the ghost reflection at the surface. Assuming that this is true for the source signatures in Figure 7.8a, determine their depths.
For discussion of reinforcement depth in marine recording, see problem 3.5. The ghost is the wave reflected at the surface (or at the base of the LVL) with a reversal of phase (see problem 3.8).
When a gas at high pressure is suddenly generated by an underwater explosion or injected into the water by an air gun at sufficient depth that the gas does not quickly escape into the air, oscillation occurs as the gas expands until stopped by the water pressure, then contracts until the gas pressure becomes very high,
|a) air gun||22||8|
|b) air-gun array||24||9|
|c) sleeve exploder||26||10|
|g) water gun||22||8|
after which it expands again and the cycle is repeated. Each expansion is effectively a new activation of the source and so a new reflection sequence is generated. This phenomenon is called the bubble effect.
Air guns are described in problem 7.7, imploders, water guns, and sparkers in problem 7.4. Flexichoc, sleeve gun, Vaporchoc, and Maxipulse are devices (now obsolete) designed to diminish the bubble oscillation. Flexichoc used the explosion of a small charge at the center of a steel cage that attenuated the bubble, the sleeve gun utilized the explosion of a propane-oxygen mixture inside a flexible chamber with the gases vented to the surface, Vaporchoc injected superheated steam into the water, and Maxipulse recorded the bubble oscillation for later processing to remove the bubble effects.
The phase of a ghost is reversed by reflection at the surface, hence to reinforce the downgoing wavelet the ghost must return to the source at time , where is the period measured in Figure 7.8a. Therefore the depth of the source m, taking velocity in water m/s. The results are shown in Table 7.8a.
7.9 Effect of coil inductance on geophone equation
If we wish to take into account the small inductance term in the geophone equation (7.9a), show that, for a harmonic wave, it can be included approximately in the term involving the damping factor in equation (7.9b).
The moving-coil electromagnetic geophone is widely used for land seismic work. The basic elements are a case with attached magnet and a coil suspended in the magnetic field by means of springs in such a way that, when an arriving seismic wave moves the case vertically, the inertia of the coil causes it to remain relatively stationary, that is, it moves in a different manner from that of the case; the relative motion between the coil and the magnetic field induces a voltage in the coil that is a replica of the seismic signal that caused the ground motion.
Flexichoc and Vaporchoc are trademarks of Compagnie Géneralé de Géophysique; Maxipulse is a trademark of Western Geophysical Company.
Let , , , and be the mass, radius, number of turns, and current in the coil, and the resistance and inductance of the coil; is the magnetic field strength, the mechanical damping factor (the damping force being vertical velocity of the coil relative to ), electromagnetic force on the coil per unit current, the vertical displacement of the geophone case. Using these symbols, the geophone equation (see Sheriff and Geldart, 1995, 218–20) is
It is usually assumed that is small enough that it can be set equal to zero. In this case the geophone equation reduces to
where natural frequency of oscillation of the coil and
The quantity is called the damping factor for the following reason. If in equation (7.9b), the equation becomes that for undamped simple harmonic motion; if the geophone is at rest and the coil is set in motion, it oscillates forever (theoretically) with undiminished amplitude. However, if , the amplitude decreases steadily by a fixed proportion each cycle; this decrease in amplitude is called damping [see also equation (2.18b)].
If in equation (7.9a) we set in all terms except the first, we get equation (7.9b) plus the additional term . Assuming input of the form , we have , hence . Therefore we can take the term in equation (7.9b) into account by changing the coefficient of to .
7.10 Streamer feathering due to cross-currents
7.10a A 96-channel streamer with 25-m groups has the hydrophones spaced uniformly throughout its length. The lead-in and compliant sections together are 200 m in length and the tail section and buoy connection are 150 m long. Assume a source 100 m behind the ship, ship’s speed of 5.8 knots, and a 1.9 knot current perpendicular to the direction of travel.
What are the perpendicular and inline components of the distance to the farthest active group center with respect to the traverse direction?
Marine seismic work usually employs hydrophones to receive the seismic signals. These consist of piezoelectric crystals which generate a voltage difference between opposite faces when subjected to a pressure. The hydrophones are enclosed in a neutrally buoyant tube called a streamer (Figure 7.10a) which is towed by the ship. A number of hydrophones, spread over as much as 25 m, are connected together to form each group. Lead-in and compliant sections are inserted between the ship and the near end of the streamer; these increase the distance between the ship and the cable and reduce the effects of sudden changes which might jerk or break the streamer. A location sensor and radar target are usually placed on a tail buoy so that the end of the streamer can be located and the amount of feathering (sideways drift of the streamer) determined.
Common-midpoint (CMP) recording is discussed in problem 5.12.
We assume that the source is in the line between the ship and the streamer. We take the origin at the source and the -axis along the line of traverse. With 200 m lead-in and compliant sections and active streamer length of m, the farthest group center is m from the ship (assuming distances are to the group centers). The last group has a velocity of 5.8 knots along the -axis and 1.9 knots along the -axis, hence the streamer will be at the angle (see Figure 7.10b). The coordinates of this group center with respect to the source are m, m.
7.10b If the average velocity to a reflector 2.00 km below the source is 3.00 km/s and if the reflector dips perpendicular to the traverse direction, (i) by how much will the arrival time be changed for the far trace, and (ii) if this should be attributed to a change in velocity rather than cross-dip, what velocity would it imply?
(i) We shall use a derivation similar to that in problem 4.2g except that the problem is now three dimensional, so we take the receiver coordinates as . Because the dip is along the -axis, the coordinates of the image point are , being the slant depth (2.00 km). We now have
the plus sign for the last term being used when the dip and feathering are in the same direction.
When the streamer is tracking behind the boat, and equation (7.10a) gives
When the feathering is in the downdip direction, km, km, and
When the streamer is drifting updip, the sign of the -term is reversed, so
(ii) At the source we observe the traveltime
If we attribute the difference in traveltimes because of dip to a velocity change rather than to dip, we can determine the velocity as follows:
When the streamer is feathering in the down-dip direction,
For updip feathering,
Compared with the actual value of 3.00 km/s, these results are in error by 14% and 19% for the downdip and updip cases, respectively.
7.10c Assume that the amount of sideways drift of the streamer is ascertained by radar sighting on the tail buoy with an accuracy of only ; (i) how much change will this produce in locating the far group? (ii) How much change in arrival time will be associated with this uncertainty?
i) The radar sighting gives the angle of feathering . The center of the last group is 2590 from the ship, so taking an origin at the ship, the and coordinates of the group are , ; . The errors in and due to radians are
ii) When is positive, i.e., , m, m. When is negative, the sign of is reversed. We use equation (7.10a) to find the traveltimes, that is,
where km, km, km, km/s, , and we use the plus sign for the -term when the cable is drifting downdip, the minus sign when the drift is updip. We have four cases to consider: the drift is down- or updip, and is or .
7.10d The midpoint traces that are to be combined in a CMP stack will be distributed over what distance?
We determine the shifts from the line of traverse of groups #96 and #1, subtract these shifts, then divide by 2 to get the shifts of the midpoint. Thus, the shift relative to the ship of group center #96 is
For group #1,
The midpoints are shifted by half of these amounts, so the spread of the midpoints is: m, m.
7.11 Filtering effect of geophones and amplifiers
Use Figures 7.11a and 7.11b to determine the filter equivalent of a geophone with Hz and , feeding into an amplifier with a 10–70 Hz bandpass filter and a 4-ms alias filter.
A filter, whether analog or digital, is a device that attenuates certain ranges of frequencies present in a signal. A geophone is equivalent to a filter because the response determined by equation (7.9b) is frequency dependent; when the input is harmonic such that the vertical velocity of the geophone is , the solution is [see Sheriff and Geldart, 1995, 220, equation (7.20)]
where the impedance and the phase shift are both functions of , being the natural frequency of the geophone (see problem 7.9) and the frequency of the ground motion.
The geophone sensitivity is a measure of the geophone output for a given ground velocity; it is defined by the relation
Because the numerator is proportional to , is independent of and depends only upon the properties of the geophone and the ratio (see Sheriff and Geldart, 1995, 220, for more details).
Figure 7.11a shows (rationalized) as a function of for various values of the damping factor (see problem 7.9).
Seismic amplifiers include various types of filters. Band-pass filters pass a band of frequencies and discriminate sharply against frequencies outside the band, as shown in Figure 7.11b; the limits of the passband are usually taken as the frequencies at which the attenuation is 3 dB. Alias filters have a very steep high-frequency cutoff and are used to attenuate alias frequencies (see problem 9.4).
In Table 7.11a the column headed gives values of the geophone sensitivity for taken from Figure 7.11a; since the sensitivity is a ratio of amplitudes, we change the values to decibels in the 4th column. We obtain attenuation of the band-pass filter for the normalized frequencies 0.4, 0.6, etc., from Figure 7.11b using the 10-Hz low-cut and 70-Hz high-cut curves. The alias filter for 4-ms sampling rate is used to obtain the 6th column. The sum of the three attenuations is plotted in Figure 7.11c.
|(Hz)||(dB)||10–70 (dB)||alias (dB)||Sum (dB)|
7.12 Filter effects on waveshape
Figure 7.12a illustrates filter effects. Evaluate the characteristics of (a) low-frequency cut, (b) high-frequency cut, (c) bandwidth, and (d) filter slope on (i) time delay to a point that could be timed reliably, (ii) apparent polarity, and (iii) ringing. The conclusions can be generalized for filters of other design types.
Minimum phase is discussed in Sheriff and Geldart, 1995, Sections 9.4 and 15.5.6.
The first three columns in Figure 7.12a illustrate the effect of increasing the low-frequency cut and the last three columns do the same for the high-frequency cut. Broadly speaking, (i) as low frequencies are increasingly removed, the wavelet becomes more ringy (oscillatory) and energy shifts later in the wavelet; (ii) as high frequencies are removed, the pulse is lengthened without adding more cycles; (iii) as the filter slope increases, the energy is pushed later in the wavelet, resulting in pulse shape changes as evidenced by decreased ratios of first trough to first peak amplitudes.
- Importance of low-frequency cut on
- time-delay: the backward drift of energy means that the first pickable point may be shifted to later time;
- apparent polarity: the backward energy drift also means a weaker first half-cycle, increasing the chance of missing it and picking the next half-cycle with reversed polarity;
- ringing: increases ringing.
- Importance of high-frequency cut on
- time delay: lengthening the pulse delays the first pickable point;
- apparent polarity: no appreciable effect;
- ringing: no appreciable effect.
- Importance of bandwidth: the 6–60 Hz passband is roughly 3.5 octaves, the 6–30 Hz is 2.5 octaves, the 18–60 Hz is 1.5 octaves;
- time delay: with narrower bandwidth, energy shifts backward within the wavelet, making it more difficult to pick early cycles, thus increasing time delays;
- apparent polarity: the same effect increases the likelihood of mistaking wavelet polarity;
- ringing: ringing increases with narrower bandwidth.
- Importance of filter slope on
- time delay: increasing slope increases the delay;
- polarity: since the ratio of amplitudes of the first peak to the first trough changes, apparent polarity can be affected;
- ringing: increases ringing.
7.13 Effect of filtering on event picking
Figure 7.13a shows changes in wave-shape produced by the analog filtering in modern digital instruments. What can you conclude about the effects on picking?
The filtering on traces (b) and (c) is normal alias filtering for 2 ms and 4 ms sampling. Comparison of traces (a), (b), and (c) shows that lowering the high-frequency cut increases the delay. Comparing (c) and (d), we see that increasing the filter slope also increases the delay. Comparing traces (e) and (f) shows that changing the high-frequency slope changes the pulse shape but has little effect on the delay. Changing the low-frequency cut has a similar effect as seen by comparing (c) and (g). Narrowing the bandwidth results in shifting energy backward within the wavelet, decreasing the ability to pick early within the wavelet and increasing the likelihood of misinterpreting polarity.
7.14 Binary numbers
- Express the decimal numbers 19 and 10 as binary numbers.
- Add the binary numbers together and convert the sum to a decimal number.
- Multiply the two binary numbers and convert the product to decimal form.
Mathematical operations are carried out in binary arithmetic in the same way as in decimal arithmetic. As an example of the similarity between decimal and binary arithmetic, when we add 75 to 129, we add 9 to 5 in the right-hand column and get 4 plus 1 to be carried to the next column. In binary addition, we have only the digits 1 and 0; when we add 1 to 1 we get 0 plus 1 to carry to the next column. In subtraction, when we subtract 1 from 0 we must borrow 1 from the next nonzero column to the left. Multiplication is identical in the two systems. To express a decimal number as a binary number, we subtract the largest power of 2 that is less than the decimal number, then follow the same procedure with the remainders until we end up with 1 or 0.