Abstract:
A method for processing data from dual sensor receivers to produce a combined seismic trace. A first seismic trace is received from a geophone and second seismic trance from a hydrophone in a dual sensor receiver. This first and second seismic traces are transformed into a first and second seismic spectrum. The seismic spectrums are deghosted to obtain deghosted spectrums. The seismic spectra may be added to obtain a deghosted third spectrum. An inverse power is computed for each of the deghosted spectra. The inverse powers for each deghosted spectra are divided by sums of the deghosted spectra to obtain diversity filters. The first and third diversity filters are applied to the first seismic spectrum to obtain a scaled first seismic spectrum. The other scaled spectra are formed in a like manner. The diversity scaled seismic spectrum is inversely transformed to obtain the combined seismic trace.

Description:
CROSS REFERENCES TO RELATED APPLICATIONS  
       [0001]    This application is a Continuation-in-Part of U.S. patent application Ser. No. 09/598,718 filed on Jun. 21, 2000 and U.S. Provisional Patent Application No. 60/141,197 filed on Jun. 25, 1999. These entire specifications are hereby fully incorporated by reference. 
     
    
     
       BACKGROUND OF THE INVENTION  
         [0002]    1. Field of the Invention  
           [0003]    The present invention relates generally to the field of seismology, and more particularly to the processing of signals from dual-sensor arrays to eliminate undesired seismic energy.  
           [0004]    2. Description of the Related Art  
           [0005]    The field of seismology focuses on the use of artificially generated elastic waves to locate mineral deposits such as hydrocarbons, ores, water, and geothermal reservoirs. Seismic exploration provides data that, when used in conjunction with other available geophysical, borehole, and geological data can provide information about the structure and distribution of rock types and their contents.  
           [0006]    Most oil companies rely on seismic interpretation for selecting the sites in which to invest in drilling oil wells. Despite the fact that seismic data is used to map geological structures rather than finding petroleum directly, the gathering of seismic data has become a vital part of selecting the site of exploratory and development wells. Experience has shown that the use of seismic data greatly improves the likelihood of a successful venture.  
           [0007]    Seismic data acquisition is routinely performed both on land and at sea. At sea, seismic ships may trail a streamer or cable behind the ship as the ship moves forward. Alternatively, the ships may deploy receivers and allow the receivers to rest on the ocean floor. This is known as an on-bottom cable (OBC) operation. In OBC operations a second ship typically deploys a seismic source with which to generate seismic waves. Processing equipment aboard the two ships controls the operation of the seismic source and receivers and processes the acquired data.  
           [0008]    The cables normally include electrical or fiber-optic cabling for connecting the receivers to seismic monitoring equipment on a ship. The receivers may be uniformly spaced along the cables, and the cables may typically be several miles in length. Data is digitized near the receivers and transmitted to the ship through the cabling.  
           [0009]    Various types of seismic sources are used to generate seismic waves for the seismic measurements. To determine the location and configuration of subsurface structures, the seismic source emits seismic waves that travel through the water and earth. These seismic waves generate reflections at various interfaces, including the interfaces created by the presence of the subsurface structures. By determining the length of time that the seismic waves take to travel from the seismic source to the subsurface structure and back to the seismic receivers, an estimate of the distance to subsurface structure can be obtained. By estimating the distance from the various receivers to a subsurface structure, the geometry or topography of the structure can be determined. Certain topographical features are indicative of oil and/or gas reservoirs.  
           [0010]    Two primary types of receivers are used in seismology: hydrophones and geophones. Most commonly used for marine seismology are the hydrophones, sometimes called marine pressure phones. These receivers detect pressure changes, and are usually constructed using a piezoelectric transducer that generates a voltage proportional to the pressure change it experiences. Geophones are particle motion detectors commonly used for land seismology and may be particle displacement, particle velocity or particle acceleration detectors. Geophones are directional, i.e., they provide outputs that are dependent on the orientation of the sensor, whereas hydrophones are omnidirectional.  
           [0011]    Recently, seismologists have begun using dual sensor receivers for OBC operations. Dual sensor receivers include both a hydrophone and a geophone. Signal traces from each sensor are processed and combined so as to produce an improved seismic trace. The directionality of a geophone allows a well-designed system to reduce or eliminate ghosts and other signal artifacts from the hydrophone signal. Ghosts are undesirable seismic signals which have at some stage traveled upwards towards the sea surface before traveling down to the receiver.  
           [0012]    The simultaneous collection of pressure and velocity or other particle motion information has the general potential to allow separation of upgoing and downgoing energy, and thus perform ghost removal for marine data. In the special case of the receivers being positioned on the sea floor, it should also be possible to remove all energy that is trapped in the water layer (simple water bottom multiple energy). However, this requires scaling one of the signal traces by a factor that is dependent on the reflectivity at the water bottom. Inclusion of effects of the source ghost as well as receiver ghost have led to development of so called “Baccus filter methods” which attempt to remove the source ghost as well as the receiver ghost.  
           [0013]    Existing processing methods for reducing ghosts and signal artifacts generally make some combination of the following assumptions: that the seismic waves are vertically incident plane waves, that the geophone response is onmidirectional, that the hydrophone and geophone have similar impulse responses, that the sensors are perfectly coupled, and that the sensors have similar noise characteristics. In fact, some field systems are now manufactured to “balance” the response of the two detector types in an attempt to make these assumptions valid and to avoid any requirement for additional scaling. However, since some of these conditions are deterministic and measurable, it would be desirable to provide for a processing method that does not limit its accuracy by making any of these assumptions. Additionally it would be preferable to combine the signals in a way which improves the signal-to-incoherent-noise ratio in the combined result.  
           [0014]    It is noted that no currently available methods address the angular dependence of the reflectivity of the ocean floor. Any attempt to provide a simple scalar correction is at best only a first order approximation, since reflectivity may depend on the angle of incidence. It may be argued that the range of incident angles in seismic data is small enough for the approximation to be valid, but this is unlikely to be true for reflections in shallow water layers.  
           [0015]    It is notable that most current methods are designed to combine the signals from a hydrophone and a geophone by simple scaling and summation. It is desirable to make the scalars be dependent on the signal (regardless of the method of determination). We describe here a method of combination which is dependent on Signal to Noise, and additionally may be different for each frequency recorded. The result has the benefit of having better signal to noise characteristics than any simple summation method.  
         SUMMARY OF THE INVENTION  
         [0016]    Accordingly, there is disclosed herein a method for processing data from dual sensor receivers to produce a combined seismic trace. A first seismic trace is received from a geophone and second seismic trance from a hydrophone in a dual sensor receiver. This first and second seismic traces are transformed into a first and second seismic spectrum. The seismic spectrums are deghosted to obtain deghosted spectrums. The seismic spectra may be added to obtain a deghosted third spectrum. An inverse power is computed for each of the deghosted spectra. The inverse powers for each deghosted spectra are divided by sums of the deghosted spectra to obtain diversity filters. The first and third diversity filters are applied to the first seismic spectrum to obtain a scaled first seismic spectrum, applying the second and third diversity filters are applied to the second seismic spectrum to obtain a scaled second seismic spectrum. The first scaled and second scaled seismic spectra are added to obtain a diversity scaled seismic spectrum. The diversity scaled seismic spectrum is inversely transformed to obtain the combined seismic trace. 
       
    
    
     BRIEF DESCRIPTION OF THE DRAWINGS  
       [0017]    A better understanding of the present invention can be obtained when the following detailed description of the preferred embodiment is considered in conjunction with the following drawings, in which:  
         [0018]    [0018]FIG. 1 is a theoretical hydrophone ghost response;  
         [0019]    [0019]FIG. 2 is the corresponding hydrophone ghost spectrum;  
         [0020]    [0020]FIG. 3 is a theoretical geophone ghost response;  
         [0021]    [0021]FIG. 4 is the corresponding geophone ghost spectrum;  
         [0022]    [0022]FIG. 5 is an exemplary spectrum of hydrophone and geophone data;  
         [0023]    [0023]FIG. 6 is a simple sum of the hydrophone and geophone spectra;  
         [0024]    [0024]FIG. 7 shows three estimates of a de-ghosted spectrum;  
         [0025]    [0025]FIG. 8 shows a comparison of combined spectral estimates;  
         [0026]    [0026]FIG. 9 shows an exemplary reverberation spectrum for a reflectivity of 0.4;  
         [0027]    [0027]FIG. 10 shows an exemplary reverberation spectrum for a reflectivity of 0.2  
         [0028]    [0028]FIG. 11 shows a comparison of de-reverberated combined spectral estimates;  
         [0029]    [0029]FIG. 12 shows exemplary time-domain traces of hydrophone and geophone data;  
         [0030]    [0030]FIG. 13 shows a comparison of combined hydrophone and geophone data;  
         [0031]    [0031]FIG. 14 shows an expanded time view of the combined hydrophone and geophone data;  
         [0032]    [0032]FIG. 15 shows a flowchart of the present method with a de-reverberation option; and  
         [0033]    [0033]FIG. 16 shows a flowchart of the present method without a de-reverberation option. 
     
    
       [0034]    While the invention is susceptible to various modifications and alternative forms, specific embodiments thereof are shown by way of example in the drawings and will herein be described in detail. It should be understood, however, that the drawings and detailed description thereto are not intended to limit the invention to the particular form disclosed, but on the contrary, the intention is to cover all modifications, equivalents and alternatives falling within the spirit and scope of the present invention as defined by the appended claims, such as for example, where an accelerometer is used as a geophone.  
       DETAILED DESCRIPTION OF PREFERRED EMBODIMENTS  
       [0035]    Turning now to the figures, FIG. 16 shows a first method for processing dual sensor seismic data. Each receiver includes a hydrophone and a geophone that detect seismic waves. The seismic traces acquired by the hydrophone sensors and geophone sensors are available from blocks  102  and  104  respectively. In block  106 , the geophone traces are multiplied by a position and time dependent function to correct for the incidence angle of arriving waves. The hydrophone and corrected geophone data is transformed to the frequency domain, and in block  108 , the transformed geophone data is combined with the transformed hydrophone data as a prelude to an estimation procedure for calculating dc-ghosting filters. In blocks  110  and  112 , theoretical de-ghosting frequency spectra are applied to approximately correct the transformed hydrophone data and angle-corrected geophone data. The results of blocks  108 ,  110 , and  112  should contain the same signal content (the deghosted signal), but will be different because of the different noise in hydrophone and geophone signals, and because of the method of derivation. These signals are processed in block  114  to determine an optimum de-ghosted spectrum using a diversity technique. In block  116  the optimum de-ghosted spectrum is used to determine minimum phase diversity filters for the hydrophone and geophone traces. In block  118 , the diversity filters are applied to the hydrophone and geophone traces, and the filter outputs are summed to produce an output seismic trace which is available in block  120 . Each of the blocks is discussed in greater detail below.  
         [0036]    [0036]FIG. 15 shows an improved method for processing dual sensor seismic data. This improved method includes additional steps to determine and correct for the effect of reflectivity coefficient as it relates to reverberation. In block  122 , an autocorrelation of the diversity-summed seismic trace is calculated to estimate the a reflectivity coefficient. In block  124 , this estimated coefficient is used to determine a second correction filter for the once-corrected geophone trace from block  106 . The twice-corrected geophone trace is then provided to block  126  for diversity filtering and summing to produce an “R-corrected” output seismic trace, which is provided in block  128 . FIG. 15 also shows optional outputs of intermediate traces in the process. In addition to the output trace in block  120  that corresponds to the output from the previous method, a summed trace with correction only for the angular dependence of the geophone is available in block  130 . Each of the method blocks is now described in greater detail.  
         [0037]    Method block  106  represents a scaling operation to correct the geophone traces for the incidence angle of seismic waves. The user inputs relevant to this block include: an enable switch to indicate whether or not this scaling operation is to be performed, a maximum gain, and a seismic wave velocity.  
         [0038]    Method block  106  multiplies the geophone traces by a scale factor S1 that is dependent on offset (receiver location) and time:  
       S1   =     min        [       1       |     1   -       [     x     t                 v       ]     2             ,     G   max       ]                             
 
         [0039]    where x is the offset (horizontal distance from source to receiver), t is time, and v is the specified velocity of the seismic waves. In one preferred embodiment, the velocity v is assumed to be constant. However, the velocity may also be specified as a function of time or depth.  
         [0040]    [0040]FIG. 5 shows an example of a trace from a dual sensor receiver. The hydrophone and geophone traces are largely dominated by noise. The spectral content which results from a direct sum of the two traces is shown in FIG. 6.  
         [0041]    The Hydrophone data and angle-corrected geophone data are frequency transformed prior to being summed in method block  108  and prior to being operated on in method blocks  110 ,  112 . These three blocks serve to provide estimates of the deghosted seismic information. The user inputs relevant to this block include: water depth and estimate of the ghost magnitude (close to unity). The hydrophone data H(t) and corrected geophone data G(t) are Fourier transformed to the frequency domain. The resulting spectra H(F) and G(t), respectively, are complex-valued functions over a frequency range from 0 Hz to the Nyquist frequency.  
         [0042]    Method blocks  108 ,  110 ,  112  each calculate an estimate for the amplitude spectra after de-ghosting:  
           EST 1( f )= SQRT (( realH ( f )+ realG ( f )) 2 +( imagH ( f )+ imagG ( f )) 2 ))  Estimate 1  
           EST 2( f )= SQRT ( realH ( f ) 2   +imagH ( f ) 2 ))/ AMPGhostH ( f )  Estimate 2  
           EST 3( f )= SQRT ( realG ( f ) 2   +imagG ( f ) 2 ))/ AMPGhostG ( f )  Estimate 3  
         [0043]    Estimate 1 is the estimated amplitude spectra that result from a simple summation of hydrophone and geophone traces. Estimate 2 is the amplitude spectra of hydrophone traces divided by the ghost response spectrum of a hydrophone. Estimate 3 is similarly the amplitude spectra of geophone traces divided by the ghost response spectrum of a geophone.  
         [0044]    The amplitude spectrum for the hydrophone ghost response can be constructed theoretically from the assumption that it is the combination of two delta functions (spikes) of unity magnitude. The first spike is a positive spike at time t=0, and the second spike is a negative spike delayed by the two-way travel time in the water layer, as shown in FIG. 1. The second spike is an echo of the source reflecting off the water92s surface. The complex-valued frequency spectrum for this response is:  
           Hghost (Real)=1−cos(2 .pi.f.t )  
           Hghost (Imaginary)=1−sin(2. pi.f.t)    
         [0045]    where “t” is the two way travel time in the water layer:  
           t= 2×water depth/water velocity  
         [0046]    The amplitude spectrum of this response is:  
           AMPGhostH ( f )=max( SQR T ( Hghost (real) 2   +Hghost (imaginary) 2 ),  G   min )  
         [0047]    [0047]FIG. 2 shows the amplitude spectrum before the minimum limit constraint is imposed. Since this spectrum can go to zero, and a divide by AMPGhostH(f) is required, the minimum value of AMPGhostH(f) is constrained by the user provided minimum level ghost limit G min , such that AMPGhostH(f) is always greater than G min .  
         [0048]    The amplitude spectrum for the geophone ghost response can similarly be constructed theoretically from the assumption that it is the combination of two delta functions of unity magnitude. The first spike is a positive spike at time t=0, and the second spike is a positive spike delayed by the time for a two way trip in the water layer, (the same time as utilized in the hydrophone ghost) as shown in FIG. 3. The complex-valued frequency spectrum for this response is:  
           GhostG (Real)=1+cos(2. pi.f.t )  
           GhostG (Imaginary)=1+sin(2. pi.f.t )  
         [0049]    where “t” is the two way travel time in the water layer as defined previously. The amplitude spectrum is similarly constructed:  
           AMPGhostG ( f )=max( SQRT ( GhostG (real) 2   +GhostG (imaginary) 2 ),  G   min )  
         [0050]    [0050]FIG. 4 shows the amplitude spectrum for the geophone ghost response before the minimum limit is imposed.  
         [0051]    The three estimates of the de-ghosted amplitude spectra generated by blocks  108 ,  110 , and  112  will be different due to the presence of noise on individual traces. It is noted that the second and third estimates generated by blocks  110  and  112  respectively, will be dominated by noise in the regions where they are divided by small numbers in the ghost spectra. These portions of the estimates may even be the largest amplitudes in the spectra.  
         [0052]    These de-ghosted estimates contain both signal and noise. The signal component may be small in comparison with the noise levels. However, the signal component is consistent throughout all the estimates, whereas the noise is different on each estimate. This characteristic makes these estimates candidates for the use of “diversity methods” for determining an optimum summation for computing the “optimum” amplitude spectrum (the spectrum having the largest signal-to-noise ratio).  
         [0053]    To avoid excessive sensitivity to small amplitude values, a small amount of white noise may be added to each of the spectral estimates prior to their usage. The noise levels may be computed according to the user specified noise percentage:  
           Hnoise=Average ( AMP 2( f ))·Noise%  Hydrophone noise  
           Gnoise=Average ( AMP 3( f ))·Noise%  Geophone noise  
         [0054]    So that the final adjusted estimates of the de-ghosted spectrum are given as  
           EST 2( f )= Hnoise+SQRT ( realH ( f ) 2   +imagH ( f ) 2 ))/ AMPGhostH ( f )  
           EST 3(/)= Gnoise+SQRT ( realG ( f ) 2   +imagG ( f ) 2 ))/ AMPGhostG ( f )  
         [0055]    The de-ghosted spectrum estimates are shown in FIG. 7. These estimates are derived from the traces shown in FIGS. 5 and 6. Note that the high amplitude “noise” in each representation is different.  
         [0056]    Method block  114  determines the appropriate scaling factors for combining the spectrum estimates to obtain an “optimum” de-ghosted spectrum. As part of the process, the method block  114  estimates the noise ration between the geophone and the hydrophone. The user input relevant to this block is a power diversity exponent exp (defaults to 2).  
         [0057]    For each estimated de-ghosted amplitude spectrum, method block  114  computes the inverse power:  
           INV 1( f )=1/( EST 1( f ) exp )  
           INV 2( f )=1/( EST 2( f ) exp )  
           INV 3( f )=1/( EST 3( f ) exp )  
         [0058]    and sums the inverse powers:  
           SUM ( f )= INV 1( f )+ INV 2( f )+ INV 3( f )  
         [0059]    The method block  114  then determines the diversity scaling factors:  
           SCALE 1( F )= INV 1( f )/ SUM ( f )  
           SCALE 2( f )= INV 2( f )/ SUM ( f )  
           SCALE 3( f )= INV 3( f )/ SUM ( f )  
         [0060]    If an intermediate output is desired from block  114 , then block  114  may apply these scale Factors to the complex valued frequency spectrum of the hydrophone data and corrected geophone data:  
           DeghostR ( f )= RealEST 1( f )* SCALE 1( f )+ realH ( f )* SCALE 2( f )+ realG ( f )* SCALE 3( f )  
           DeghostI ( f )= IMAGEST 1( f )* SCAL 1 E ( f )+ ImagH ( f )* SCALE 2( f )+ ImagG ( f )* SCALE 3( f )  
         [0061]    This can be re-stated in the following form:  
           DeghostR ( f ) realH ( f )*( SCALE 2( f )+ SCALE ( f ))+ realG ( f )*( SCALE 3( f )+ SCALE 1( f ))  
           DeghostI ( f )= ImagH ( f )*( SCALE 2( f )+ SCALEI ( f ))+ ImagG ( f )*( SCALE 3( f )+ SCALEI ( f ))  
         [0062]    [0062]FIG. 8 compares the simple average of the hydrophone and geophone traces with the diversity-scaled summation. Also shown is the reverberation spectrum which will be addressed later. Both traces (hydrophone and geophone) contained random noise, but in addition, there is mono-frequency noise on one component that is not on the other. This is well attenuated by the diversity procedure.  
         [0063]    Method block  116  takes the above-calculated diversity scale factors in the frequency domain, and calculates the complex-valued amplitude spectrum of minimum phase filters which have the same energy spectrum as the scalar values. A pair of filters is calculated, one for the hydrophone data and one for the geophone data. Given a desired amplitude spectrum, various existing techniques may be used to calculate the minimum phase filter that possesses the desired amplitude spectrum.  
         [0064]    Method block  118  takes the minimum phase diversity filters, applies them to the frequency-transformed hydrophone traces and angle-corrected geophone traces, and sums the filtered results. An inverse Fourier transform of this sum provides the output result available in block  120 . However, as indicated in FIG. 8, a reverberation artifact is still present. A “de-reverberation” option is preferably provided as indicated in FIG. 15.  
         [0065]    The de-ghosted amplitude spectrum is perturbed by the reverberation sequence due to sound trapped in the water payer. This reverberation sequence is given by:  
         [0066]    1,−Re iωx ,+R iω2t ,−R 3 e iω3t  etc.  
         [0067]    Where each subsequent bounce is delayed by the two way time in the water layer. The net effect of this is to introduce a “ripple” into the amplitude spectrum. FIGS.  9  and show that this ripple is not a big feature even for large values of “R” the reflectivity of the water bottom. FIG. 9 shows a reverberation spectrum for a reflectivity of 0.4, and FIG. 10 shows a reverberation spectrum for a reflectivity of 0.2.  
         [0068]    As developed below, a comparison of the autocorrelation values at zero lag and at the reverberation lag provides for an efficient estimate of the reflectivity R. This computation may be performed using only the amplitude spectrum values of the deghosted trace, and omitting the phase values.  
         [0069]    The zero lag value of the autocorrelation is given as  
         A        (   0   )       =       ∑     j   =   0     n          R     2      j                               
 
         [0070]    so that:  
           A (0)·(1− R   2 )=1− R   n+2    
         [0071]    If R&lt;1 then  
         A        (   0   )       =     1     1   -     R   2                               
 
         [0072]    The required time lag value of the autocorrelation is given as:  
         A        (   t   )       =       ∑     j   =   0     n          -     R       2      j     +   1                                 
  A ( t )·(1− R   2 )=− R−R   n+2    
         [0073]    If R&lt;1 then  
         A        (   t   )       =       -   R       1   -     R   2                               
 
         [0074]    So the value of reflectivity can be computed as the ratio of the time lag value to the zero lag value of the autocorrelation:  
           A        (   t   )         A        (   0   )         =     -   R                           
 
         [0075]    If the values of the amplitude spectrum of the optimum de-ghosted data are given as  
         [0076]    DEG(f)  
         [0077]    Then the power spectrum is computed as:  
           PWR ( f )= DEG ( f ) 2    
         [0078]    and the zero lag value of the auto correlation is computed as:  
         L                 A                   G        (   0   )         =         P                   WR        (   0   )         +     P                   WR        (   Nyquist   )           =     2          ∑     f   =   i     j          P                     WR        (   f   )       .                                   
 
         [0079]    Where the indices “i” and “j” include all values off except Zero and Nyquist. The time lag value of the autocorrelation is computed as:  
         L                 A                   G        (   t   )         =         P                   WR        (   0   )         +     P                   WR        (   Nyquist   )           =     2          ∑     f   =   i     j          P                     WR        (   f   )       ·     cos        (     2      π                 f                 t     )                                       
 
         [0080]    Where “t” is the two way time in the water layer.  
         [0081]    Method block  122  takes the diversity-summed data from block  118  and the previously calculated two-way travel time for sound in the water layer, and calculates an auto-correlation of the diversity-summed data at zero and at the water depth reverberation period. This autocorrelation value yields an estimate of the reflectivity R of the water bottom:  
       R   =       L                 A                   G        (   t   )           L                 A                   G        (   0   )                                 
 
         [0082]    Method block  124  takes this reflectivity estimate and scales the angle-corrected geophone data by the following scalar:  
         SCALAR=(1+ R )/(1− R )  
         [0083]    Method block  126  takes the “R-scaled” geophone data and, using the previously determined diversity filters for diversity scaling, adds it to the hydrophone data in the frequency domain. First, three traces are calculated:  
           T 1= H ( f )+ G ( f ).SCALAR  
           T 2= H ( f )  
           T 3= G ( f ).SCALAR  
         [0084]    These traces are then summed (in the frequency domain) on the basis of the diversity filters previously computed, and the final result inverse transformed to yield the optimum de-reverberated trace.  
           Finalreal ( f )= T 1 real ( f )* SCALE 1( f )+ T 2 real ( f )* SCALE 2( f )+ T 3 real ( f )* SCALE 3( f )  
           Finalimag ( f )= T 1 imag ( f )* SCALE 1( f )+ T 2 imag ( f )* SCALE 2( f )+ T 3 imag ( f )* SCALE 3( f )  
         [0085]    [0085]FIG. 11 shows a comparison of the spectra of (1) a simple sum of the traces, (2) a simple sum of the hydrophone data with the “R-scaled” geophone data, and (3) a diversity sum of the hydrophone data with the R-scaled geophone data. It is noted that the “peak” which represents a concentrated noise presence at a particular frequency is largely eliminated due to the robustness of the new method.  
         [0086]    [0086]FIG. 12 shows a time-domain example of hydrophone and geophone traces from a dual sensor receiver. FIG. 13 shows the time-domain comparison of the various combination methods including (1) a simple sum (largest amplitude), (2) a simple sum of the hydrophone and the R-scaled geophone, and (3) a diversity scaled sum of the hydrophone and R-scaled geophone trace (smallest amplitude). FIG. 14 shows an expanded time view of FIG. 13 along with the unscaled hydrophone and geophone traces.  
         [0087]    Numerous variations and modifications will become apparent to those skilled in the art once the above disclosure is fully appreciated.