Abstract:
The invention concerns a method of acquiring vibroseismic data concerning a zone of the subsoil. This method comprises the following steps: —operating a vibroseismic source so that it transmits a first vibroseismic signal having a first amplitude ( 101, 201 ), —operating the source so that it transmits a second vibroseismic signal having a second amplitude different from the first amplitude ( 103, 203 ), —recording first data corresponding to the first signal after propagation in the medium to be explored ( 102, 202 ), —recording second data corresponding to the second signal after propagation in the medium to be explored ( 104, 204 ). The method supplies information for filtering the surface waves (ground roll).

Description:
[0001]    The invention concerns the seismic exploration of an underground zone on land. 
         [0002]    The use of seismic waves generated artificially for the imaging of geological layers has been used for more than 50 years. The most widely used waves are by far reflected waves and more precisely reflected compressional waves. 
         [0003]    During seismic prospection operations, a vibrator equipment generates a vibroseismic signal that propagates in particular in the form of a wave that is reflected on interfaces of geological layers. These waves are received by geophones, which convert the displacement of the ground resulting from the propagation of the waves into an electrical signal recorded by means of recording equipment. 
         [0004]    Analysis of the arrival times and amplitudes of these waves makes it possible to construct a representation of the geological layers on which the waves are reflected. One of the complications in terrestrial seismic surveys is that the reflected waves are not the only ones to be recorded. In particular, the wave associated with the largest proportion of energy is the surface wave that propagates along the surface of the ground. This wave is similar to the one that propagates on the surface of the water when for example a pebble is caused to fall on it. It is commonly referred to as “ground roll”, a word which designates the rotation movement of the particles on the surface of the ground. The surface wave or ground roll interferes with the reflected waves and obscures their image. 
         [0005]    There are other stray waves generated but they are in general less disturbing. 
         [0006]    Hereinafter, the terms “surface waves” and “reflected waves” will be used to designate the parts of a seismogram respectively representing the corresponding waves. 
         [0007]    There currently exist two main techniques for separating the surface waves in the recorded seismic data. 
         [0008]    The most widespread technique used is an apparent-speed filtering that separates the slow surface waves from the more rapid reflected waves. 
         [0009]    The second technique is that of the polarisation filter. Surface waves produce a circular movement of the surface of the ground whereas reflective waves produce a linear movement. It is this difference that is used by the polarisation filter. 
         [0010]    It is also known (Martin, J. E., Jack, I. G. “The behaviour of a seismic vibrator using different phase control methods and drive levels” First Break, November 1990) that the variation in the level of the force generated by a vibrator is represented by a variation in the propagation times of the reflected waves. This variation in time is in general interpreted as a variation in propagation velocities in the compressed area under the plate of the vibrator. 
         [0011]    It was observed that this variation in time was not identical for all types of waves. In particular, for the reflected waves used to obtain almost all the images in oil exploration seismics, this variation is obviously very small whereas for surface waves it may be much greater. 
         [0012]    The present invention takes advantage of this observation. 
         [0013]    According to a first aspect, an object of the invention is a method of acquiring vibroseismic data concerning an underground zone supplying the information for separating the surface wave components contained in the vibroseismic data. 
         [0014]    According to this first aspect a method of acquiring vibroseismic data concerning an underground zone is provided, comprising the following steps:
       operating a vibroseismic source so that it transmits a first vibroseismic signal having a first amplitude,   operating the source so that it transmits a second vibroseismic signal having a second amplitude, different from the first amplitude,   recording first data corresponding to the first signal after propagation in the medium to be explored,   recording second data corresponding to the second signal after propagation in the medium to be explored.       
 
         [0019]    The method proposed takes advantage of the difference in propagation time relating to the variation in the force level generated by the source. By virtue of this difference, an estimate of the surface waves can be derived from the first and second data with a view to filtering thereof. 
         [0020]    The method can also be used for separating the compressional waves converted into shear waves in the case where these are recorded by means of 3-component geophones. This is because the phenomenon is associated with the source and affects indifferently the compressional waves that are reflected and those that are converted into shear waves. 
         [0021]    Likewise, the method can be applied to the shear waves emitted by a shear wave source. 
         [0022]    Furthermore, the method proposed applies directly to diffracted surface waves. 
         [0023]    A method for the seismic exploration of an underground zone is provided according to a second aspect, comprising the following steps:
       operating a vibroseismic source so that it transmits a first vibroseismic signal having a first amplitude,   operating the source so that it transmits a second vibroseismic signal having a second amplitude different from the first amplitude,   recording first data corresponding to the first signal after propagation in the medium to be explored,   recording second data corresponding to the second signal after propagation in the medium to be explored,   deriving an estimate of the surface waves contained in these data from the first and second data recorded, and   subtracting this estimate from the first data.       
 
     
    
     
       PRESENTATION OF THE FIGURES 
         [0030]      FIG. 1  depicts schematically a device for transmitting and receiving vibroseismic waves, 
           [0031]      FIG. 2  depicts schematically a first signal (weak signal) and a second signal (strong signal) as transmitted by the device in  FIG. 1 , 
           [0032]      FIG. 3  is a diagram depicting schematically recordings obtained by the device in  FIG. 1  after propagation of the second signal in the subsoil, 
           [0033]      FIG. 4  is a diagram depicting schematically recordings obtained by the device in  FIG. 1  after propagation of the first signal in the subsoil and equalisation, 
           [0034]      FIG. 5  is a diagram obtained by subtraction of the diagrams in  FIGS. 3 and 4 , 
           [0035]      FIG. 6  is a diagram obtained after integration of the diagram in  FIG. 5 , corresponding to an estimation of the surface signals, 
           [0036]      FIG. 7  is a diagram obtained after subtraction of the diagrams in  FIGS. 3 and 6 , corresponding to a recording in which the surface signals have been eliminated, 
           [0037]      FIG. 8  depicts schematically steps of a seismic exploration method according to a first embodiment of the invention, 
           [0038]      FIG. 9  depicts schematically steps of a seismic exploration method according to a second embodiment of the invention. 
       
    
    
     DETAILED DESCRIPTION 
       [0039]      FIG. 1  depicts schematically a device for transmitting and receiving vibroseismic waves intended for seismic exploration in a land environment. 
         [0040]    The device comprises a source consisting of a vibrator  1  operable to generate a seismic signal, a set of receivers  2  (or geophones) for receiving a seismic signal and converting it into an electrical signal and a recorder  3  for recording the electrical signals generated by the receivers. The source  1 , the receivers  2  and the recorder  3  are positioned on the surface of the ground  5 .  FIG. 1  depicts a single vibrator but it should be understood that the source may be composed of several vibrators, as is well known to persons skilled in the art. 
         [0041]    In operation, the source  1  is operated so as to generate a vibroseismic signal. This signal propagates firstly on the surface of the ground, in the form of surface waves  4 , and secondly in the subsoil, in the form of waves  6  that generate reflected waves when they reach an interface  7  between two geological layers. Each receiver  2  receives both a surface wave  4  and a reflected wave  6  and converts them into an electrical signal in which are superimposed the component corresponding to the reflected wave and the one that corresponds to the surface wave, which is undesirable and which is to be filtered. 
       First Embodiment 
     Simplified Model 
       [0042]    A simple model consists of describing a seismogram SR(t,d) derived from a signal transmitted by the vibroseismic source S with a force d and observed by the receiver R as a function of time t as the sum of two components associated respectively with the reflected waves P(t,d) and the surface waves G(t,d). 
         [0000]        SR ( t,d )= P ( t,d )+ G ( t,d )  [1]
 
         [0043]    The variable d is used to designate a force so as to avoid confusion with the frequency. The variable d in reality designates the drive, that is to say the percentage of the maximum force available for a given type of vibrator. It is the drive that is used by land geophysicists to modify the force applied to the ground. 
         [0044]    In this model, the variation in the force from b (low) to h (high) results in an identical variation in amplitude and a different variation in time for each of the two components: 
         [0000]    
       
         
           
             
               
                 
                   
                     SR 
                      
                     
                       ( 
                       
                         t 
                         , 
                         h 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       P 
                        
                       
                         ( 
                         
                           t 
                           , 
                           h 
                         
                         ) 
                       
                     
                     + 
                     
                       G 
                        
                       
                         ( 
                         
                           t 
                           , 
                           h 
                         
                         ) 
                       
                     
                   
                 
               
               
                 
                   [ 
                   2 
                   ] 
                 
               
             
             
               
                 
                   
                     SR 
                      
                     
                       ( 
                       
                         t 
                         , 
                         b 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       P 
                        
                       
                         ( 
                         
                           t 
                           , 
                           b 
                         
                         ) 
                       
                     
                     + 
                     
                       
                         G 
                          
                         
                           ( 
                           
                             t 
                             , 
                             b 
                           
                           ) 
                         
                       
                        
                       
                           
                       
                        
                       With 
                     
                   
                 
               
               
                 
                   [ 
                   3 
                   ] 
                 
               
             
             
               
                 
                   
                     P 
                      
                     
                       ( 
                       
                         t 
                         , 
                         b 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       b 
                       h 
                     
                     · 
                     
                       P 
                        
                       
                         ( 
                         
                           
                             t 
                             + 
                             
                               τ 
                               P 
                             
                           
                           , 
                           h 
                         
                         ) 
                       
                     
                   
                 
               
               
                 
                   [ 
                   4 
                   ] 
                 
               
             
             
               
                 
                   
                     G 
                      
                     
                       ( 
                       
                         t 
                         , 
                         b 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       b 
                       h 
                     
                     · 
                     
                       G 
                        
                       
                         ( 
                         
                           
                             t 
                             + 
                             
                               τ 
                               G 
                             
                           
                           , 
                           h 
                         
                         ) 
                       
                     
                   
                 
               
               
                 
                   [ 
                   5 
                   ] 
                 
               
             
           
         
       
     
         [0045]    where τ P  designates the delay of the low-amplitude component with respect to the high-amplitude component for the components associated with the reflected waves, 
         [0046]    and τ G  designates the delay of the low-amplitude component with respect to the high-amplitude component for the components associated with the surface waves. 
         [0047]    By substitution, equation [3] becomes: 
         [0000]    
       
         
           
             
               
                 
                   
                     SR 
                      
                     
                       ( 
                       
                         t 
                         , 
                         b 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       b 
                       h 
                     
                     · 
                     
                       [ 
                       
                         
                           P 
                            
                           
                             ( 
                             
                               
                                 t 
                                 + 
                                 
                                   τ 
                                   P 
                                 
                               
                               , 
                               h 
                             
                             ) 
                           
                         
                         + 
                         
                           G 
                            
                           
                             ( 
                             
                               
                                 t 
                                 + 
                                 
                                   τ 
                                   G 
                                 
                               
                               , 
                               b 
                             
                             ) 
                           
                         
                       
                       ] 
                     
                   
                 
               
               
                 
                   [ 
                   6 
                   ] 
                 
               
             
           
         
       
     
         [0048]    Therefore: 
         [0000]    
       
         
           
             
               
                 
                   
                     SR 
                      
                     
                       ( 
                       
                         
                           t 
                           - 
                           
                             τ 
                             P 
                           
                         
                         , 
                         b 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       b 
                       h 
                     
                     · 
                     
                       [ 
                       
                         
                           P 
                            
                           
                             ( 
                             
                               t 
                               , 
                               h 
                             
                             ) 
                           
                         
                         + 
                         
                           G 
                            
                           
                             ( 
                             
                               
                                 t 
                                 + 
                                 
                                   τ 
                                   G 
                                 
                                 - 
                                 
                                   τ 
                                   P 
                                 
                               
                               , 
                               b 
                             
                             ) 
                           
                         
                       
                       ] 
                     
                   
                 
               
               
                 
                   [ 
                   7 
                   ] 
                 
               
             
           
         
       
     
         [0049]    By difference with equation [2], there is obtained: 
         [0000]    
       
         
           
             
               
                 
                   
                     
                       SR 
                        
                       
                         ( 
                         
                           
                             t 
                             - 
                             
                               τ 
                               P 
                             
                           
                           , 
                           b 
                         
                         ) 
                       
                     
                     - 
                     
                       
                         b 
                         h 
                       
                        
                       
                         SR 
                          
                         
                           ( 
                           
                             t 
                             , 
                             h 
                           
                           ) 
                         
                       
                     
                   
                   = 
                   
                     
                       b 
                       h 
                     
                     · 
                     
                       [ 
                       
                         
                           G 
                            
                           
                             ( 
                             
                               
                                 t 
                                 + 
                                 
                                   τ 
                                   G 
                                 
                                 - 
                                 
                                   τ 
                                   P 
                                 
                               
                               , 
                               b 
                             
                             ) 
                           
                         
                         - 
                         
                           G 
                            
                           
                             ( 
                             
                               t 
                               , 
                               h 
                             
                             ) 
                           
                         
                       
                       ] 
                     
                   
                 
               
               
                 
                   [ 
                   8 
                   ] 
                 
               
             
           
         
       
     
         [0050]    which can also be written: 
         [0000]    
       
         
           
             
               
                 
                   
                     
                       SR 
                        
                       
                         ( 
                         
                           
                             t 
                             - 
                             
                               τ 
                               P 
                             
                           
                           , 
                           b 
                         
                         ) 
                       
                     
                     - 
                     
                       
                         b 
                         h 
                       
                        
                       
                         SR 
                          
                         
                           ( 
                           
                             t 
                             , 
                             h 
                           
                           ) 
                         
                       
                     
                   
                   = 
                   
                     
                       ( 
                       
                         
                           τ 
                           G 
                         
                         - 
                         
                           τ 
                           P 
                         
                       
                       ) 
                     
                     · 
                     
                       
                          
                         
                           G 
                            
                           
                             ( 
                             
                               t 
                               , 
                               h 
                             
                             ) 
                           
                         
                       
                       
                          
                         t 
                       
                     
                   
                 
               
               
                 
                   [ 
                   9 
                   ] 
                 
               
             
           
         
       
     
         [0051]    and by integration makes it possible to determine the surface wave 
         [0000]    
       
         
           
             
               
                 
                   
                     G 
                      
                     
                       ( 
                       
                         t 
                         , 
                         h 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       1 
                       
                         ( 
                         
                           
                             τ 
                             G 
                           
                           - 
                           
                             τ 
                             P 
                           
                         
                         ) 
                       
                     
                     · 
                     
                       
                         ∫ 
                         
                             
                         
                         
                             
                         
                       
                        
                       
                         
                           [ 
                           
                             
                               SR 
                                
                               
                                 ( 
                                 
                                   
                                     t 
                                     - 
                                     
                                       τ 
                                       P 
                                     
                                   
                                   , 
                                   b 
                                 
                                 ) 
                               
                             
                             - 
                             
                               
                                 b 
                                 h 
                               
                                
                               
                                 SR 
                                  
                                 
                                   ( 
                                   
                                     t 
                                     , 
                                     h 
                                   
                                   ) 
                                 
                               
                             
                           
                           ] 
                         
                          
                         
                             
                         
                          
                         
                            
                           t 
                         
                       
                     
                   
                 
               
               
                 
                   [ 
                   10 
                   ] 
                 
               
             
           
         
       
     
         [0052]      FIG. 8  depicts schematically steps of a seismic exploration method comprising a vibroseismic acquisition method according to the invention, composed of steps  101 - 104 , and a method of filtering the surface waves, according to a first embodiment ( 105 - 109 ). 
         [0053]    In a first step  101 , the source  1  consisting of a vibrator is controlled so as to generate a first vibroseismic signal S 1  (strong signal) having a first amplitude. This first amplitude is appropriately the optimum amplitude from the standpoint of seismic imaging. To this end, the vibrator is adjusted so as to apply vibrations to the ground with a first force level h (high level), for example with a drive d of 80%. 
         [0054]    In a second step  102 , the recorder  3  records first data. 
         [0055]    The first data recorded are shown in  FIG. 3 . These first data comprise a set of signals (or traces) recorded as a function of time and resulting from the propagation of the first seismic signal, each signal having been generated by a receiver  2 . 
         [0056]    The first data comprise data corresponding to surface waves  4  and data corresponding to reflected waves  6 . 
         [0057]    In a third step  103 , the vibrator  1  is controlled so as to generate a second vibroseismic signal S 2  (weak signal) having a second amplitude. For this purpose, the vibrator is adjusted so as to apply vibrations to the ground with a second force level b (low level), for example with a drive d of 20%. The second signal S 2  is identical to the first signal S 1 , except that it has an amplitude less than that of the signal S 1 , as shown in  FIG. 2 . 
         [0058]    It should be noted that the terms “first” and “second” are used here only to distinguish on the one hand the signals emitted at the high level and on the other hand the signals emitted at the low level, as well as the data respectively recorded following these emissions. The terms “first” and “second” in no way indicate a chronological order. The order in which the two emissions take place and subsequently the recordings is indifferent in attaining the objectives of the invention. The emission of a high signal may precede that of a weak signal, or vice versa. 
         [0059]    In a fourth step  104 , the recorder  3  records second data. 
         [0060]    In a fifth step  105 , the delays τ P  and τ G  between the components P(t,h) and P(t,b) and between the components G(t,h) and G(t,b) are determined from the first and second data. 
         [0061]    In a sixth step  106 , the second data are processed in the following manner: the amplitudes of the traces are multiplied by a factor 
         [0000]    
       
         
           
             h 
             b 
           
         
       
     
         [0000]    and the traces are offset in time by τ G −τ P .  FIG. 4  depicts the second data thus processed. 
         [0062]    The effect of this sixth step is to transform the second data so that the reflected wave component P can be superimposed on the reflected wave components P contained in the first data. In other words, the reflected wave components P are referred to a common reference in the first and second data. 
         [0063]    In a seventh step  107 , the second data thus processed or transformed ( FIG. 4 ) are subtracted from the first data ( FIG. 3 ). 
         [0064]    The effect of this seventh step is to eliminate the reflected wave components P.  FIG. 5  shows schematically the subtracted data obtained by the subtraction step. It can be seen in this figure that the reflected waves have disappeared. 
         [0065]    In an eighth step  108 , the subtracted data are integrated with respect to time so as to obtain estimation data GE for the surface wave components (ground roll). 
         [0066]      FIG. 6  shows schematically the estimation data GE. 
         [0067]    In a ninth step ( 109 ), the estimation data of the ground roll ( FIG. 6 ) are subtracted from the first data ( FIG. 3 ) so as to eliminate the surface wave components. 
         [0068]    This ninth step makes it possible to obtain an estimation PE of the data corresponding to the reflected waves. The ground roll has substantially disappeared. 
         [0069]    The model corresponding to the first embodiment described above, based on a description of the effect of a variation in the force applied by equations [4] and [5], is a simplified model that does not take account of other types of wave present in the recordings, in particular the ambient noise (not generated by the source), and certain variables, such as the frequency, the azimuth and the inclination of the rays, which may have a significant impact on this effect. 
         [0070]    To take account of these different variables, a second embodiment can be used, based on a more complex model. 
       Second Embodiment 
     Complex Model 
       [0071]    To take account of all the variables, it is possible to describe the phenomenon in the Fourier domain {f,kx,ky} where f represents the frequency, and kx and ky the wave numbers in horizontal directions X and Y. 
         [0072]    In addition, in this domain, the effect of the ambient noise is easy to control and reduce. 
         [0073]    To simplify the notations the variable f will merely be indicated in place of f,kx,ky. 
         [0074]    By taking identical notations, equations [2] and [3] become: 
         [0000]        SR ( f,h )= P ( f,h )+ G ( f,h )  [12]
 
         [0000]        SR ( f,b )= P ( f,b )+ G ( f,b )  [13]
 
         [0075]    At this stage, it is possible to calculate a change operator O 1 , for example by spectral division: 
         [0000]    
       
         
           
             
               
                 
                   
                     O 
                      
                     
                         
                     
                      
                     1 
                      
                     
                       ( 
                       f 
                       ) 
                     
                   
                   = 
                   
                     
                       P 
                        
                       
                         ( 
                         
                           f 
                           , 
                           h 
                         
                         ) 
                       
                     
                     
                       P 
                        
                       
                         ( 
                         
                           f 
                           , 
                           b 
                         
                         ) 
                       
                     
                   
                 
               
               
                 
                   [ 
                   14 
                   ] 
                 
               
             
           
         
       
     
         [0076]    The most general operator depends on f,kx,ky, the most simple is a scalar. 
         [0077]    The operator O 1  is applied to the data SR(f,b) recorded with a low force b. 
         [0000]        SR 2( f,b )= SR ( f,b )* O 1( f )  [15]
 
         [0078]    By subtracting equation [14] from [11], a filtered estimation of the ground roll is obtained: 
         [0000]        SR ( f,h )− SR 2( f,b )= GE ( f,h )*(1 −O 1( f ))  [16]
 
         [0079]    The final estimation of the ground roll is obtained by application of a reverse filter. 
         [0000]    
       
         
           
             
               
                 
                   
                     GE 
                      
                     
                       ( 
                       
                         f 
                         , 
                         h 
                       
                       ) 
                     
                   
                   = 
                   
                     
                       
                         SR 
                          
                         
                           ( 
                           
                             f 
                             , 
                             h 
                           
                           ) 
                         
                       
                       - 
                       
                         SR 
                          
                         
                             
                         
                          
                         2 
                          
                         
                           ( 
                           
                             f 
                             , 
                             h 
                           
                           ) 
                         
                       
                     
                     
                       1 
                       - 
                       
                         O 
                          
                         
                             
                         
                          
                         1 
                          
                         
                           ( 
                           f 
                           ) 
                         
                       
                     
                   
                 
               
               
                 
                   [ 
                   17 
                   ] 
                 
               
             
           
         
       
     
         [0080]    It remains to subtract this estimation GE(f,h) of the ground roll from the data SR(f,h) in order to obtain an estimation PE(f,h) of the reflected waves. 
         [0000]        PE ( f,h )= SR ( f,h )− GE ( f,h )  [18]
 
         [0081]      FIG. 9  schematically shows steps of a seismic exploration method comprising a vibroseismic acquisition method according to the invention, composed of steps  201 - 204 , and a method of filtering the surface waves according to a second embodiment (steps  205 - 209 ). 
         [0082]    According to a first step  201 , the source  1  is controlled so as to generate a first seismic signal S 1  (strong signal) having a first amplitude. For this purpose, the vibrator is adjusted so as to apply vibrations to the ground with a first force level h (high level), for example with a drive d of 80%. 
         [0083]    According to a second step  202 , the recorder  3  records first data. 
         [0084]    The first data recorded are shown in  FIG. 3 . These first data comprise a set of signals (or traces) recorded as a function of time and resulting from the propagation of the first seismic signal, each signal having been generated by a receiver  2 . 
         [0085]    The first data comprise data corresponding to surface waves  4  and data corresponding to reflected waves  6 . 
         [0086]    According to a third step  203 , the source  1  is controlled so as to generate a second signal S 2  (weak signal) having a second amplitude. For this purpose, the vibrator is adjusted so as to apply vibrations to the ground with a second force level b (low level), for example with a drive d of 20%. The second signal S 2  is identical to the first signal S 1 , except that it has an amplitude less than that of S 1 , as shown in  FIG. 2 . 
         [0087]    In the case of the first embodiment, it should be noted that the terms “first” and “second” are used here only to identify in a practical fashion on the one hand the signals emitted at the high level and on the other hand the signals emitted at the low level, as well as the data respectively recorded following these emissions. The terms “first” and “second” in no way indicate a chronological order. The order in which the two transmissions take place, and consequently the recordings of the data, is indifferent in achieving the objects of the invention. The transmission of a high signal may precede that of a low signal, or vice versa. 
         [0088]    According to a fourth step  204 , the recorder  3  records second data. 
         [0089]    According to a fifth step  205 , a change operator O 1 ( f ) is derived from the first and second data (equation [14]). The derivation of the change operator is based on the fact that there generally exists zones in which the reflected waves P and the surface waves G do not interfere, or do not substantially interfere, and may be separated. 
         [0090]    Using several seismograms associated with different receivers reduces the effect of strict non-compliance with the non-interference condition. 
         [0091]    As required, calculation of the change operator may be the subject of an iteration, in a manner well known to persons skilled in the art. 
         [0092]    According to a sixth step  206 , the change operator O 1 ( f ) is applied to the second data (equation [15]). 
         [0093]    According to a seventh step  207 , the second data thus processed or transformed are subtracted from the first data. 
         [0094]    The effect of this seventh step is to eliminate the reflected pressure wave components P.  FIG. 5  depicts schematically the inverse Fourier transform of the subtracted data. It can be seen in this figure that the reflected waves have substantially disappeared. 
         [0095]    According to an eight step  208 , the inverse operator 
         [0000]    
       
         
           
             1 
             
               1 
               - 
               
                 O 
                  
                 
                     
                 
                  
                 1 
                  
                 
                   ( 
                   f 
                   ) 
                 
               
             
           
         
       
     
         [0000]    is applied to the subtracted data so as to obtain estimated data GE for the surface wave components, or “ground roll”. 
         [0096]      FIG. 6  depicts schematically the inverse Fourier transform of the estimation data GE of the ground roll. 
         [0097]    According to a ninth step  209 , the estimation data of the ground roll ( FIG. 6 ) are subtracted from the first data ( FIG. 3 ), so as to eliminate the surface wave components. 
         [0098]    This step makes it possible to derive an estimate PE of the data corresponding to the reflected waves. In this estimate, the ground roll has substantially disappeared. 
         [0099]    It was noted above that, in the two embodiments described, the chronological order is indifferent: the transmission of the high-level signal may precede that of the low-level signal, or vice versa. With regard to the interval of time separating the two transmissions, several options are possible. The most simple for the separation of the two recordings is to perform the two transmissions and recordings sequentially, without overlap. It can nevertheless also be envisaged to reduce the interval between the transmissions, for improving the productivity of the operations, and have overlapping transmissions and recordings. In the latter case, it will be necessary to reduce the distortion due to the harmonic noise. This may be achieved in an appropriate fashion by the method described in the document FR 2845483.