Abstract:
Analysis of a seismic event, such as a microseismic event caused by hydraulic fracturing, comprises measuring seismic waves emitted by the event and converting the measurements into two values for magnitude of explosion or implosion and for magnitude of displacement discontinuity at a plane, together with two directions, a direction of a normal to the plane and a direction of displacement; where the two values and the two directions compose the moment tensor describing the seismic event. The measurements may be converted into the moment tensor and decomposed into the values and directions. The values and directions associated with several seismic events may be displayed concurrently on a graphic display as a graphic representation of multiple events, where each event may be depicted with magnitude of expansion or contraction represented by a volume and the plane represented as a laminar object.

Description:
FIELD OF THE INVENTION 
       [0001]    This invention relates to monitoring of microseismic events, that is small seismic events which occur below ground as a result of changes in the stress within geological formations. Monitoring of microseismic events is a way to observe, remotely, events taking place below ground. Examples of fields where microseismic monitoring can be useful are hydraulic fracturing, where the microseismics give evidence of the location, time and nature of the fractures produced, reservoir monitoring, where microseismics give evidence of changes in stress in the reservoirs due to production and pumping, waste disposal, where the injection may cause events on existing or new faults, carbon sequestration, where events may be caused by the pressure of injected CO 2  which threaten the integrity of the storage reservoir, and monitoring large infrastructures such as dams and reservoirs, where the load or changes in underground water may cause events which threaten the structures. 
       BACKGROUND OF THE INVENTION 
       [0002]    In conventional seismic monitoring one or more seismic sources, such as airguns, vibrators or explosives are activated and generate sufficient acoustic energy to penetrate the earth. Reflected or refracted parts of this energy are then recorded by seismic receivers such as hydrophones and geophones. 
         [0003]    In passive seismic monitoring there is no actively controlled and triggered source. The seismic energy is generated through so-called microseismic events caused by subterranean shifts and changes that at least partially give rise to acoustic waves which in turn can be recorded using the known receivers. These microseismic events may be the result of human activity, such as pumping a pressurized fluid into a subterranean location to create a hydraulic fracture. Passive seismic monitoring has some similarity to the study of earthquakes, in that the time and location of a seismic event is not known beforehand, while the obvious difference is that an earthquake is a much more energetic and spatially distributed seismic event. 
         [0004]    It is well known that the characteristics of a seismic event can be expressed as the moment tensor and many textbooks and papers have accepted that the moment tensor is an appropriate way to describe a small seismic source. The moment tensor is a three by three symmetric matrix of values which give the magnitudes of all the possible force couples. Its name arises because it has the units of force times distance, hence a moment. 
         [0005]    At a seismic event there is a localized, transient, failure of the constitutive law of elasticity. The difference between the model stress calculated from the constitutive law of elasticity and the true stress is referred to as the stress glut: thus 
         [0000]      σ glut =σ model −σ true    (E1)
 
         [0006]    The moment tensor M is the integral of the rate of change of the stress glut over the volume and time period in which the seismic event occurs: 
         [0000]    
       
         
           
             
               
                 
                   
                     
                       
                         M 
                         = 
                           
                          
                         
                           
                             ∫ 
                             
                               0 
                               - 
                             
                             T 
                           
                            
                           
                             
                               ∫ 
                               
                                 V 
                                 S 
                               
                             
                              
                             
                               
                                 
                                   ∂ 
                                   
                                     σ 
                                     glut 
                                   
                                 
                                 
                                   ∂ 
                                   t 
                                 
                               
                                
                               
                                   
                               
                                
                               
                                  
                                 V 
                               
                                
                               
                                   
                               
                                
                               
                                  
                                 t 
                               
                             
                           
                         
                       
                     
                   
                   
                     
                       
                         = 
                           
                          
                         
                           
                             ∫ 
                             
                               V 
                               S 
                             
                           
                            
                           
                             
                               [ 
                               
                                 σ 
                                 glut 
                               
                               ] 
                             
                              
                             
                                 
                             
                              
                             
                                
                               V 
                             
                           
                         
                       
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     2 
                   
                   ) 
                 
               
             
           
         
       
     
         [0007]    where T is the duration of the event (which we assume occurs at time zero), 
         [0008]    V S  is the volume of the source (i.e. seismic event), and 
         [0009]    [σ glut ] is the change (saltus) of the stress glut during the event. 
         [0010]    Provided the seismic event is small compared with the seismic wavelength and is of short duration (both of which are normally the case for a microseismic event) it can be regarded as a point source and the stress glut can be written as 
         [0000]      σ glut ( x,t )= MH ( t )δ( x−x   S )   (E3)
 
         [0011]    where H(t) is the Heaviside step function, δ(x) is the three-dimensional Dirac delta function, and x S  is the location of the point source. 
         [0012]    It is well known that for a small and short seismic event which can be regarded as a point source, the particle displacement, i.e. the displacement at one or more receivers, which may be observed as velocity or acceleration, is related to the moment tensor by the Green function: 
         [0000]        u ( t, x   R )= G   σ ( t, x   R   ,x   S ): M    (E4)
 
         [0013]    where u is the particle displacement, G σ  is the third-order stress Green tensor and : is the scalar product, or contraction over two indices, of the tensors. The Green function can be calculated for the elastic Earth model using a known technique, e.g. ray theory or finite-difference method. Determining the moment tensor is then a linear inverse problem and methods to analyze a linear inverse problem are well known. 
         [0014]    A description of the moment tensor to describe a point source seismic event is given in Section 3.3 of Aki and Richards (2002). Observing the moment tensor from seismic data is referred to in U.S. Pat. Nos. 5,377,104 and 7,647,183 and US published applications 2005/0190649 and 2010/0157730. 
         [0015]    The subsequent step of interpretation of the moment tensor presents difficulties. It is desirable to decompose the moment tensor into other quantities in order to obtain a physical interpretation of the seismic event. There is a standard decomposition of seismic moment tensors, which has been used in earthquake studies and in microseismic monitoring. This is to decompose the moment tensor using its principal values (usually termed eigenvalues) and its axes, i.e. 
         [0000]    
       
         
           
             
               
                 
                   
                     M 
                      
                     
                       ( 
                       
                         
                           
                             
                               T 
                               ^ 
                             
                           
                           
                             
                               N 
                               ^ 
                             
                           
                           
                             
                               P 
                               ^ 
                             
                           
                         
                       
                       ) 
                     
                   
                   = 
                   
                     
                       ( 
                       
                         
                           
                             
                               T 
                               ^ 
                             
                           
                           
                             
                               N 
                               ^ 
                             
                           
                           
                             
                               P 
                               ^ 
                             
                           
                         
                       
                       ) 
                     
                      
                     
                       ( 
                       
                         
                           
                             
                               Λ 
                               T 
                             
                           
                           
                             0 
                           
                           
                             0 
                           
                         
                         
                           
                             0 
                           
                           
                             
                               Λ 
                               N 
                             
                           
                           
                             0 
                           
                         
                         
                           
                             0 
                           
                           
                             0 
                           
                           
                             
                               Λ 
                               P 
                             
                           
                         
                       
                       ) 
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     5 
                   
                   ) 
                 
               
             
           
         
       
     
         [0016]    The eigenvalues are ordered, i.e. 
         [0000]      Λ T ≧Λ N ≧Λ P    (E6)
 
         [0017]    and the corresponding axes are known as the tension, {circumflex over (T)}, neutral, {circumflex over (N)}, and pressure, {circumflex over (P)}, axes. The principal axes describe the orientation of the seismic event, and the principal values the nature or type of seismic event. The standard method of interpretation is to transform these eigenvalues into parts that represent certain basic types of seismic event, e.g. one or more of an explosion, dipole(s), double couple(s), compensated linear vector dipole(s) (Knopoff and Randall, 1970; Jost and Herrmann, 1989; Riedesel and Jordan, 1989). Unfortunately the decomposition is always non-unique. 
         [0018]    Many physical models generate the same moment tensor. The usual approach when implementing this standard method of decomposition is to choose the two simplest types of seismic event which are explosion and slip on a fault. However such decomposition leads to a value for explosion, a value for slip on a fault and a remainder which is not easy to interpret. More difficulty in interpretation arises if the geological formation in which the seismic event occurs is anisotropic or if the so-called displacement discontinuity (the movement of one portion of the formation relative to another) is not confined to slip on a fault but includes movement of one portion towards or way from another, for instance when a hydraulic fracture opens or closes. 
       SUMMARY OF THE INVENTION 
       [0019]    Broadly the present invention provides a method of analysing an underground seismic event comprising: 
         [0020]    receiving and measuring seismic waves emitted by the seismic event; and 
         [0021]    converting the measurements of the seismic waves into
       a value for magnitude of explosion or implosion,   a value for magnitude of displacement discontinuity at a plane,   the direction of a normal to that plane, and   a direction of displacement;       
 
         [0026]    where the two said values and the two said directions compose the whole moment tensor describing the seismic event. Of course, once the two directions have been obtained, the angle between them, i.e. the angle between the displacement direction and the normal to the plane follows directly. The terms “explosion” and “implosion” are customary terms in the field of seismic studies. They denotes that a seismic event involves expansion or contraction but they do not specify the cause of the expansion or contraction. 
         [0027]    In some forms of the invention the method includes a step of converting the measurements of the seismic waves to values in a moment tensor describing the event; and then carrying out a novel decomposition of the moment tensor into the magnitude value for explosion, the magnitude value for displacement discontinuity at a plane, the direction of a normal to that plane, and the displacement direction, where the two said values and two said directions compose the whole of the said moment tensor. 
         [0028]    However, it is within the scope of this invention to proceed from the measurements to the values and directions without going through the intermediate stage of converting to a moment tensor. 
         [0029]    The reception and measurement of seismic signals may be carried out with known receiving devices such as geophones or hydrophones. The conversion of the measurements into the values and directions may be carried out by a program running on a digital computer and the values and directions so obtained may be stored in computer memory and/or output from the computer. Such output may take various forms, including display on a monitor or other display device, or printing to paper, or storage in a portable form of non-volatile memory, or transmission over a network such as transmission to another computer. The output may be machine readable data, data in alphanumerical characters or output to drive a graphic display. 
         [0030]    In some forms of this invention, values and directions are obtained in accordance with this invention for a number of seismic events and are output so as to be shown concurrently as a graphic representation. This may be output as a graphic display on a monitor or other display device or may be printing as a graphic. Each seismic event may then be represented by objects and/or symbols at a point in the graphic corresponding to the location (or the centre of the location) of the seismic event. A graphic display may be such that some of the said values and/or directions are displayed while others are hidden. 
         [0031]    It is possible that the output from a computer will not be the values and directions directly obtained by the decomposition procedure but will instead consist of or include data obtainable through further processing of the values and directions. 
         [0032]    The output may at least include (i) a value indicating magnitude of explosion or implosion and (ii) data indicating the said plane. Preferred possibilities for such graphic representation are:
       value of the volume change due to the explosion (or implosion) represented as a sphere or other volume;   displacement discontinuity plane, i.e. fault plane, represented as a laminar object, for example a disc, pictured as lying in the plane;   displacement direction indicated by an arrow or other linear element.       
 
         [0036]    The value of the multiplication product of the displacement discontinuity times the fault area may be represented by the size of the laminar object and by the length of the linear element. 
     
    
     
       BRIEF DESCRIPTION OF THE DRAWINGS 
         [0037]      FIG. 1  is a diagram showing the angle and bi-axes in the plane of the tension, {circumflex over (T)} and pressure, {circumflex over (P)} principal axes; 
           [0038]      FIG. 2  diagrammatically illustrates displacement discontinuity; 
           [0039]      FIG. 3  illustrates a display glyph, and 
           [0040]      FIG. 4  illustrates a display of multiple glyphs. 
       
    
    
     DETAILED DESCRIPTION 
       [0041]    The reception of seismic waves from a seismic event and the measurement of those waves may be carried out using known apparatus and the measured data may be converted to a moment tensor or other data suitable for further calculation by known techniques. The present invention then envisages a novel decomposition of the moment tensor. 
         [0042]    The following description will first explain the two values and two directions which are the novel decomposition of the moment tensor and then explain how the decomposition of the moment tensor can be carried out. 
         [0043]    It has previously been pointed out that the stress glut and the stress free strain are equivalent descriptions of a seismic event. See Backus and Mulchay (1976a,b) and see also Robinson (1951) and Eshelby (1957) for introduction of the term stress free strain. The stress-free strain is the strain that the region of the seismic event would undergo if the surrounding material were not present. It can be calculated from the stress glut as 
         [0000]    
       
         
           
             
               
                 
                   
                     
                       
                         
                           e 
                           free 
                         
                         = 
                           
                          
                         
                           s 
                           : 
                           
                             σ 
                             glut 
                           
                         
                       
                     
                   
                   
                     
                       
                         = 
                           
                          
                         
                           
                             e 
                             model 
                           
                           - 
                           
                             s 
                             : 
                             
                               σ 
                               true 
                             
                           
                         
                       
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     7 
                   
                   ) 
                 
               
             
           
         
       
     
         [0044]    where S is the fourth-order compliance tensor. Note that the stress-free strain is not the difference between the model and true strains, as can be seen from the definition and the final expression in equation (E7), which is not the true strain. 
         [0045]    The integral of the rate of change of the stress-free strain over the volume and time period in which the seismic event occurs is 
         [0000]    
       
         
           
             
               
                 
                   
                     
                       
                         D 
                         = 
                           
                          
                         
                           
                             ∫ 
                             
                               0 
                               - 
                             
                             T 
                           
                            
                           
                             
                               ∫ 
                               
                                 V 
                                 S 
                               
                             
                              
                             
                               
                                 
                                   ∂ 
                                   
                                     e 
                                     free 
                                   
                                 
                                 
                                   ∂ 
                                   t 
                                 
                               
                                
                               
                                   
                               
                                
                               
                                  
                                 V 
                               
                                
                               
                                   
                               
                                
                               
                                  
                                 t 
                               
                             
                           
                         
                       
                     
                   
                   
                     
                       
                         = 
                           
                          
                         
                           
                             ∫ 
                             
                               V 
                               S 
                             
                           
                            
                           
                             
                               [ 
                               
                                 e 
                                 free 
                               
                               ] 
                             
                              
                             
                                 
                             
                              
                             
                                
                               V 
                             
                           
                         
                       
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     8 
                   
                   ) 
                 
               
             
           
         
       
     
         [0046]    where T is the duration of the event (which commences at time zero), V S  is the volume of the source, and [e free ] is the change (saltus) of the stress free strain during the event. For a seismic event which can be regarded as a point source: 
         [0000]        e   free   =DH ( t )δ( x−x   S )   (E9)
 
         [0047]    where H(t) is the Heaviside step function, δ(x) is the three-dimensional Dirac delta function, and x S  is the location of the source. 
         [0048]    We refer to the term D as the potency tensor. This tensor has not previously been described in the literature but the term ‘potency’ has previously been used for a scalar term derived from a scalar moment magnitude. 
         [0049]    The potency tensor is next decomposed by a method which can be applied to any real, symmetric, second-order tensor (Fedorov 1968 see page 72) which is referred to here as biaxial decomposition. The eigen-decomposition for the potency tensor is 
         [0000]    
       
         
           
             
               
                 
                   
                     D 
                      
                     
                       ( 
                       
                         
                           
                             
                               
                                 X 
                                 ^ 
                               
                               1 
                             
                           
                           
                             
                               
                                 X 
                                 ^ 
                               
                               2 
                             
                           
                           
                             
                               
                                 X 
                                 ^ 
                               
                               3 
                             
                           
                         
                       
                       ) 
                     
                   
                   = 
                   
                     
                       ( 
                       
                         
                           
                             
                               
                                 X 
                                 ^ 
                               
                               1 
                             
                           
                           
                             
                               
                                 X 
                                 ^ 
                               
                               2 
                             
                           
                           
                             
                               
                                 X 
                                 ^ 
                               
                               3 
                             
                           
                         
                       
                       ) 
                     
                      
                     
                       ( 
                       
                         
                           
                             
                               Δ 
                               1 
                             
                           
                           
                             0 
                           
                           
                             0 
                           
                         
                         
                           
                             0 
                           
                           
                             
                               Δ 
                               2 
                             
                           
                           
                             0 
                           
                         
                         
                           
                             0 
                           
                           
                             0 
                           
                           
                             
                               Δ 
                               3 
                             
                           
                         
                       
                       ) 
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     10 
                   
                   ) 
                 
               
             
           
         
       
     
         [0050]    where Δ 1 ≧Δ 2 ≧Δ 3  are the ordered real eigenvalues, and {circumflex over (X)} i  are the corresponding orthonormal eigenvectors. 
         [0051]    The potency tensor can then written in the dyadic expansion 
         [0000]    
       
         
           
             
               
                 
                   
                     
                       
                         D 
                         = 
                           
                          
                         
                           
                             
                               Δ 
                               1 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               1 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               1 
                               T 
                             
                           
                           + 
                           
                             
                               Δ 
                               2 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               2 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               2 
                               T 
                             
                           
                           + 
                           
                             
                               Δ 
                               3 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               3 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               3 
                               T 
                             
                           
                         
                       
                     
                   
                   
                     
                       
                         = 
                           
                          
                         
                           
                             
                               Δ 
                               2 
                             
                              
                             I 
                           
                           + 
                           
                             
                               ( 
                               
                                 
                                   Δ 
                                   1 
                                 
                                 - 
                                 
                                   Δ 
                                   2 
                                 
                               
                               ) 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               1 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               1 
                               T 
                             
                           
                           - 
                           
                             
                               ( 
                               
                                 
                                   Δ 
                                   2 
                                 
                                 - 
                                 
                                   Δ 
                                   3 
                                 
                               
                               ) 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               3 
                             
                              
                             
                               
                                 X 
                                 ^ 
                               
                               3 
                               T 
                             
                           
                         
                       
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     11 
                   
                   ) 
                 
               
             
           
         
       
     
         [0052]    We define an angle φ from 
         [0000]    
       
         
           
             
               
                 
                   
                     
                       cos 
                        
                       
                           
                       
                        
                       φ 
                     
                     = 
                     
                        
                       
                         
                           
                             
                               Δ 
                               1 
                             
                             - 
                             
                               Δ 
                               2 
                             
                           
                           
                             
                               Δ 
                               1 
                             
                             - 
                             
                               Δ 
                               3 
                             
                           
                         
                       
                        
                     
                   
                   , 
                   
                     
 
                   
                    
                   
                     
                       sin 
                        
                       
                           
                       
                        
                       φ 
                     
                     = 
                     
                        
                       
                         
                           
                             
                               Δ 
                               2 
                             
                             - 
                             
                               Δ 
                               3 
                             
                           
                           
                             
                               Δ 
                               1 
                             
                             - 
                             
                               Δ 
                               3 
                             
                           
                         
                       
                        
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     12 
                   
                   ) 
                 
               
             
           
         
       
     
         [0053]    which will be real and 0≦φ≦π/2 because of the ordering. 
         [0054]    The next step is to define the unit vectors 
         [0000]      {circumflex over (Φ)} ± =cos φ{circumflex over ( X )} 1 ±sin φ{circumflex over ( X )} 3    (E13)
 
         [0055]    which we will call the bi-axes. The potency tensor (E11) can then be rewritten 
         [0000]    
       
         
           
             
               
                 
                   D 
                   = 
                   
                     
                       
                         Δ 
                         2 
                       
                        
                       I 
                     
                     + 
                     
                       
                         
                           
                             Δ 
                             1 
                           
                           - 
                           
                             Δ 
                             3 
                           
                         
                         2 
                       
                        
                       
                         ( 
                         
                           
                             
                               
                                 Φ 
                                 ^ 
                               
                               + 
                             
                              
                             
                               
                                 Φ 
                                 ^ 
                               
                               - 
                               T 
                             
                           
                           + 
                           
                             
                               
                                 Φ 
                                 ^ 
                               
                               - 
                             
                              
                             
                               
                                 Φ 
                                 ^ 
                               
                               + 
                               T 
                             
                           
                         
                         ) 
                       
                     
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     14 
                   
                   ) 
                 
               
             
           
         
       
     
         [0056]    An advantage of this biaxial decomposition given in (E14) over the eigen-decomposition given in (E10) and (E11) is that it remains valid for degeneracies, i.e. 
         [0057]    for Δ 1 =Δ 2 =Δ 3  when the bi-axes are not required, 
         [0058]    for Δ 1 =Δ 2  when φ=π/2, and for Δ 2 =Δ 3  when φ=0. 
         [0059]    The bi-axes are illustrated in  FIG. 1 , which shows the bi-axes {circumflex over (Φ)} ±  in the plane of the 
         [0060]    {circumflex over (T)} and {circumflex over (P)} principal axes. In addition  FIG. 1  shows the planes perpendicular to the bi-axes {circumflex over (Φ)} ±  as broken lines denoted with the dual vectors {circumflex over (Φ)} ±  where 
         [0000]      {circumflex over (Φ)} ±   =±{circumflex over (X)}   2 ×{circumflex over (Φ)} ±   (E15)
 
         [0061]      FIG. 1  also shows the angle φ between one of the bi-axes and the {circumflex over (T)} principal axis, while two more broken lines indicate the usual fault and auxiliary planes at an angle φ=π/4=45° to the {circumflex over (T)} principal axis. 
         [0062]    Equation (E14) could be used to decompose any potency tensor. The first term in (E14) represents an isotropic strain event and the second is a dyadic form that represents a displacement discontinuity on a fault. However, in anisotropic media, an isotropic stress event such as a change in hydrostatic pressure, will not bring about a strain event which is also isotropic: on the contrary an anisotropic strain will occur. In such circumstances it would be difficult to give a physical interpretation of the first term in equation (E14). Therefore, in order to decompose the moment tensor in accordance with the biaxial decomposition set out above, we first subtract an isotropic stress event (in effect representing a seismic event which is solely expansion or contraction) from the moment tensor so as to leave a tensor representing a seismic event which is displacement discontinuity alone. Consequently, in the biaxes decomposition of the remaining potency tensor, the isoptropic part is zero. The subtraction from the moment tensor is 
         [0000]        M   DD   =M−M   EXP   I    (E16)
 
         [0063]    where M EXP  is the scalar magnitude of the isotropic stress event causing expansion or contraction and I is the identity tensor. 
         [0064]    In order that M DD  is a moment tensor for a seismic event consisting solely of displacement discontinuity, M EXP  must be such that the intermediate eigenvalue Δ 2  of the potency tensor from M DD  is zero. 
         [0065]    In order to determine M Ex p we begin with an arbitrary value for M EXP . We reduce the remaining part of the moment tensor to its potency tensor 
         [0000]      D=s:M DD    (E17)
 
         [0066]    and find its eigen-decomposition in accordance with equation (E10). M EXP  is adjusted iteratively until Δ 2  becomes zero. 
         [0067]    Various iterative computational processes can be used to adjust M EXP  until Δ 2  becomes zero. We have used the function ‘fzero’ in MATLAB (MATLAB® is a registered trademark of The MathWorks™) to find the zero solution but any bisection/secant or similar algorithm will work. References for the algorithm used in fzero can be found in the MATLAB documentation. The root is straightforward to bracket as for M EXP  large and positive (a large pressure), the eigenvalues will be negative from the resultant compression, and vice-versa for a large negative value. Once the root is bracketed, the algorithm will be robust. 
         [0068]    Having found M EXP  we complete the biaxial decomposition (E14) using (E12) and (E13), and identify it with a displacement-discontinuity source. Thus the moment tensor can be written 
         [0000]        M=V   S   [P]I+  1 / 2 A[d]c : ( {circumflex over (d)}{circumflex over (n)}   T   +{circumflex over (n)}{circumflex over (d)}   T )   (E18)
 
         [0069]    where 
         [0000]      V S [P]=M EXP    (E19a)
 
         [0000]        A[d]=Δ   1 −Δ 3    (E19b)
 
         [0000]        {circumflex over (d)}={circumflex over (Φ)}   ÷   (E19c)
 
         [0000]        {circumflex over (n)}={circumflex over (Φ)}   −   (E19d)
 
         [0070]    In the explosive part (E19a), V S  is the volume of the seismic event and [P] is the pressure step, and in the displacement discontinuity, the fault area is A and the discontinuity is [d]. This is illustrated in  FIG. 2  which shows the fault plane normal to {circumflex over (n)}={circumflex over (Φ)} + with displacement discontinuity [d] in the direction {circumflex over (d)}={circumflex over (Φ)} − . The angle between the fault normal and the displacement direction is ψ=2φ. The advantage of the biaxial decomposition of the potency tensor (E18) is that it is complete and always possible whatever the moment tensor values, and that it represents a physically sensible model. Because a general anisotropic compliance tensor can be used to obtain the potency tensor (E17), another advantage of the method is that it is valid in any anisotropic medium (where the standard decomposition would lead to an output which is hard to interpret). The only ambiguity that remains, which may be removed using geological information about the rock formation and geological environment is that the choice of fault normal and displacement direction, (E19c) and (E19d) can be interchanged. 
       EXAMPLE  
       [0071]    As a test of the bi-axial decomposition procedure, data for a seismic event with random explosive part, random vectors {circumflex over (n)} and {circumflex over (d)}, and random area-displacement, in a transversely isotropic medium (a simple case of an anisotropic medium) were generated and had values 
         [0000]    
       
         
           
             
               
                 
                   
                     M 
                     EXP 
                   
                   = 
                   0.8407 
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     20 
                      
                     
                         
                     
                      
                     a 
                   
                   ) 
                 
               
             
             
               
                 
                   
                     n 
                     ^ 
                   
                   = 
                   
                     ( 
                     
                       
                         
                           0.2866 
                         
                       
                       
                         
                           0.9179 
                         
                       
                       
                         
                           0.2745 
                         
                       
                     
                     ) 
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     20 
                      
                     
                         
                     
                      
                     b 
                   
                   ) 
                 
               
             
             
               
                 
                   
                     d 
                     ^ 
                   
                   = 
                   
                     ( 
                     
                       
                         
                           0.9180 
                         
                       
                       
                         
                           0.3457 
                         
                       
                       
                         
                           0.1942 
                         
                       
                     
                     ) 
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     20 
                      
                     
                         
                     
                      
                     c 
                   
                   ) 
                 
               
             
             
               
                 
                   
                     A 
                      
                     
                       [ 
                       d 
                       ] 
                     
                   
                   = 
                   0.8980 
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     20 
                      
                     
                         
                     
                      
                     d 
                   
                   ) 
                 
               
             
           
         
       
     
         [0072]    These data were combined with values for an example of a transversely isotropic medium with a vertical axis of symmetry (Green Horn shale) which were 
         [0000]      C 11 =34.3, C 33 =22.7, C 44 =5.4, C 65 =10.6, C 13 =10.7   (E21)
 
         [0073]    (the units are not important) and the moment tensor which was derived was 
         [0000]    
       
         
           
             
               
                 
                   M 
                   = 
                   
                     ( 
                     
                       
                         
                           13.1912 
                         
                         
                           8.9642 
                         
                         
                           1.4920 
                         
                       
                       
                         
                           8.9642 
                         
                         
                           14.2235 
                         
                         
                           1.3247 
                         
                       
                       
                         
                           1.4920 
                         
                         
                           1.3247 
                         
                         
                           7.5052 
                         
                       
                     
                     ) 
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     22 
                   
                   ) 
                 
               
             
           
         
       
     
         [0074]    The algorithm described above recovered the exact values (E20) subject to sign and interchanging ambiguities in (E20c) and (E20d). The potency tensor was 
         [0000]    
       
         
           
             
               
                 
                   D 
                   = 
                   
                     ( 
                     
                       
                         
                           0.2363 
                         
                         
                           .04228 
                         
                         
                           0.1381 
                         
                       
                       
                         
                           0.4228 
                         
                         
                           0.2850 
                         
                         
                           0.1227 
                         
                       
                       
                         
                           0.1381 
                         
                         
                           0.1227 
                         
                         
                           0.0479 
                         
                       
                     
                     ) 
                   
                 
               
               
                 
                   ( 
                   
                     E 
                      
                     
                         
                     
                      
                     23 
                   
                   ) 
                 
               
             
           
         
       
     
         [0075]    As the bi-axes are not perpendicular (the angle between vectors (E20b) and (E20c) is about 50.7°) this decomposition differs from the standard fault-slip model. 
         [0076]      FIG. 3  illustrates a graphic representation of a seismic event. The event is represented as a shaped object, here referred to as a glyph. The magnitude of explosion is depicted by a sphere  30  whose size indicates the magnitude of the volume change due to explosion or implosion. One colour may be chosen for spheres denoting expansion and a contrasting colour chosen for spheres denoting contraction. The plane is denoted by a disc  32  and the size of the disc  32  is proportional to the magnitude of displacement. The normal to the plane is denoted here by a broken line  34 . The displacement direction is indicated by arrow  36 . The area of the disc  32  and the length of the arrow  36  are scaled to represent the product A[d] given as (E19b) above. 
         [0077]    Such glyphs may be shown as a picture or as a graphic display in two dimensions or in three dimensions, using known computer graphics techniques.  FIG. 4  is an illustration of one such display. 
       REFERENCES  
       [0078]    The following are mentioned in the text above: 
         [0079]    Aki, K. and Richards, P. G., 2002. Chapter 3 of  Quantitative Seismology,  2 nd  Ed., University Science Books. 
         [0080]    Backus, G. and Mulcahy, M., 1976a. Moment tensors and other phenomenological descriptions of seismic sources—I. Continuous displacements,  Geophys. J. R. Astr. Soc.,  46, 341-61. 
         [0081]    Backus, G. and Mulcahy, M., 1976b. Moment tensors and other phenomenological descriptions of seismic sources—II. Discontinuous displacements,  Geophys. J. R. Astr. Soc.,  47, 301-29. 
         [0082]    Eshelby, J. D., 1957. The determination of the elastic field of an ellipsoidal inclusion, and related problems,  Proc. R. Soc. Lond. A,  241, 376-96. 
         [0083]    Fedorov, F. D., 1968. Theory of Elastic Waves in Crystals, Trans: Bradley, J. E. S. (original in Russian, 1965, Nauka Press, Moscow), Plenum Press, New York. 
         [0084]    Robinson, K., 1951. Elastic energy of an ellipsoidal inclusion in an infinite solid, J. Appl. Phys., 22, 1045-54