# Introduction to Seismology Spring 2008

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1 MIT OpenCourseWare Introduction to Seismology Spring 2008 For information about citing these materials or our Terms of Use, visit:

2 04/30/2008 Today s lecture (Part 1) 1. Fault geometry 2. First motions 3. Stereographic fault plane representation 1 Fault geometry There are three main types of faults: 1. Normal faults 2. Reverse faults 3. Stike-slip faults We can think of these three types of faults as forming a set of basis functions. All faults can be described as a combination of these 3 basis faults. The fault geometry is described in terms of the orientation of the fault plane and the direction of slip along the plane. The geometry of this model is shown in figure 2. The dip angle δ is the angle between the fault plane and the horizontal. The slip angle, λ is the angle between the slip-vector and the horizontal. The stike angle φ is used to orientate this system relative to the geographic one. It is defined as the angle in the plane of the earth s surface measured clockwise from north to the x 1 axis. We can use the slip angle, λ to specify the type of motion on the fault. λ = 0 implies left-lateral (sinstral) fault motion λ = 180 implies right-lateral (dextral) fault motion λ = 270 implies normal faulting (extension) λ = 90 implies reverse faulting Most earthquakes consist of a combination of these motions and have a slip angle between these values. Seismologists refer to the direction of slip in an earthquake and the orientation on the fault on which it occurs as the focal mechanism. They typically display the focal mechanisms on maps as a beach-ball symbol. We will talk more about this

3 Right-lateral strike slip Left-lateral strike slip Dip slip (reverse) Dip slip (normal) Figure by MIT OpenCourseWare. Figure 1: Basic types of faulting. Strike-slip motion can be right- or left-lateral. Dip slip-faulting can occur as either reverse or normal faulting (1) 2

4 representation later in the lecture 2 First Motions The focal mechanism uses the fact that the pattern of radiated seismic waves depends on the fault geometry. The simplest motion is the first motion, or polarity, of body waves. The first motion is compression if the station is located so that material near the fault moves towards the station, or dilation where the motion is away from the station. A vertical-component seismogram will record either an upward or downward first motion, corresponding to either compression or dilation. Figure 2 illustrates the first motion concept for a strike-slip earthquake on a vertical fault. Two vertical planes are shown in the diagram, which are related to the geometry of the fault -One of these is the fault plane -One of these runs perpendicular to the fault plane and is known as the auxiliary plane. These planes define four quadrants. Two of these are compressional and two of these are dilational. If these perpendicular planes can be found the fault geometry will be known. One difficulty is that the first motion on the actual fault plane is the same as that on the auxiliary plane. The first motions alone are therefore insufficient to resolve which plane is the actual fault plane. This is a fundamental ambiguity 3

5 in inverting seismic observations for fault models. Additional geologic or geodetic information is needed to identify which is the actual fault plane. 3 Stereographic projections The fault geometry can be found from the distribution of data on a sphere around the focus. We can trace rays from the earthquake onto a hemisphere using the eikonal equation. We can then use a stereographic projection to transform the hemisphere to a plane. The graphic construction that allows us to do this is called a stereonet (figure 3) Consider how planes will appear on this net. -A vertically dipping, N-S striking plane will plot as a straight line. -A N-S striking plane with a different type will appear as a curve going from top to bottom. -A horizontal plane will appear as a perimeter. -Different type of fault will appear differently on a stereonet (see figure 5). For example, a four-quadrant checkerboard indicates pure strike-slip motion. 4

6 5

7 4 Beach Balls We established earlier that you can represent focal mechanisms using beach ball diagrams. Using a simple model, faulting will occur on planes, 45 from the maximum and minimum compressive stresses. It follows that the maximum compressive (P) and minimum compressive stress (T) axis are found by bisecting the compressional quadrants respectively. Note: The tension (T) axis is actually the minimum compressive stress, because compression occurs at the source. The upward and downward first motions are from the observers point of view, but the P and T axes refer to what is happening at the source. The beach-ball representation of focal mechanisms is important in tectonic studies. 6

8 A NORTHERN MID-ATLANTIC RI Date: 2007/ 1/ 1 Centroid Time: 1: 5:16.1 GMT Lat= Lon= Depth= 12.0 Half duration= 0.7 Centroid time minus hypocenter time: 2.7 Moment Tensor: Expo= Mw = 5.0 mb = 4.8 Ms = 0.0 Scalar Moment = 3.49e+23 Fault plane: strike=210 dip=28 slip=-84 Fault plane: strike=23 dip=63 slip=-93 5 The Harvard-CMT catalogue Figure by MIT OpenCourseWare. Seismologists collect data in real-time when there is an earthquake and produce a representation of the focal-mechanism of an earthquake as a beach-ball diagram. These are listed as entries in the Harvard-CMT catalogue. Each entry includes the following data: -the location of the earthquake -the time at which it occurred -the depth of the earthquake -the half-duration of the earthquake Note that there are four different measurements of the magnitude of the earthquake listed in the Harvard-CMT catalogue. Note also that 2 sets of values for the strike, slip and dip directions of the fault plane are listed. This is because we are unable to distinguish between the fault plane and the auxiliary plane when these entries are produced. 7

9 Lecture Notes (Part 2) MOMENT TENSOR To know the source properties from the observed seismic displacements, the solution of the equation of motion can be separated as below. Where u is the displacement, f is the force vector. The Green s function G gives the displacement at point i j x that results from a unit force function applied at point x. Internal forces, f, must act in opposing directions, - f, at a distance d so as to conserve momentum (force couple). For angular momentum conservation, there also exists a complementary couple that balances the forces (double couple). There are nine different force couples as shown in Figure 1. o (1) ij Figure 1. The nine different force couples for the components of the moment tensor. [Adapted from Shearer 1999] 1

10 Lecture Notes (Part 2) We define the moment tensor M as: M ij represents a pair of opposing forces pointing in the i (2) direction, separated in the j direction. Its magnitude is the product fd [unit: N-m] which is called the seismic moment. For angular momentum conservation, the condition M ij = M ji should be satisfied, so the moment tensor is symmetric. Therefore we have only six independent elements. This moment tensor represents the internally generated forces that can act at a point in an elastic medium. The displacement for a force couple with a distance d in the xˆ k direction is given by: The last term can be replaced by the moment tensor and thus: (3) (4) There is a linear relationship between the displacement and the components of the moment tensor that involves the spatial derivatives of the Green s functions. We can see the internal force f is proportional to the spatial derivative of moment tensor when equation (1) and (4) are compared. Consider right-lateral movement on a vertical fault oriented in the x 1 direction and the corresponding moment tensor is given by: (5) Where M o = μds is called the scalar seismic moment. This is a measure of earthquake size and energy (6) release where: μ is shear modulus, D = D( x) / L is average displacement, and s is area of the fault. can M o 2

11 Lecture Notes (Part 2) be time dependent, so that ( t) = μd ( t) s( t). The right-hand side time dependent terms become the M o source time function, x(t), thus the seismic moment function is given by We can diagonalize the moment matrix (6) to find principal axes. In this case, the principal axes are at 45 to the original x 1 and x 2 axes. (7) The principal axes become tension and pressure axis. The above matrix represents that x 1 coordinate is the tension axis, T, and x 2 is the pressure axis, P. (Figure 2) (8) Figure 2. The double-coupled forces and their rotation along the principal axes. [Adapted from Shearer 1999] *adapted from Lecture Notes 3

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