1. Earthquakes and seismo-tectonics

2. Elastic rebound model of earthquakes
An earthquake is a rapid release of stored elastic strain on 1-30 s time-scales. The earthquake happens (nucleates) when the stress on a fault plane exceeds the strength (frictional) of a fault plane in a region. Then, the inertial accelerations can ‘run-away’ to rupture a significant length of the fault plane.
Movement of plates (blocks) on either side of fault produce accumulating stress over time.
This accumulating stress creates accumulating strain that localizes along the fault plane.
The fault brittle strength is exceeded making an earthquake that ruptures and causes the strain energy to be relieved (note straight ‘strain’ lines after rupture).

4. Locating an earthquake approximately
t = x/v
Know velocity (v)
But don’t know x
Eq origin time ???
The arrival-times of the first arriving P-wave is measured. From this arrival-time measurement we now know that station (A) is closest to the earthquake and station (B) the farthest away. WHY ?
Thus, to honor the travel-time measurements, we know that the earthquake epicentre is somewhere within the shaded region in (b).
To locate an earthquake we must ‘solve’ for the location (x,y,z) and origin time. Note this method is very poor for locating the depth below the surface of the earthquake.

5. Locating earthquake more exactly using P and S arrival times
If we know the P- and S-wave velocity structure AND can measure the P- and S-wave arrival times, then an earthquake’s origin-time and location can be estimated.
The S-P interval time will tell you the distance of the earthquake. Then, a circle can be drawn around the recording station at that distance. Do that for 3 or more S-P interval times and the earthquakes location can be estimated as the intersection ‘point’ of the circular arcs.

6. Constrain the depth of an earthquake using pP phase
The hypocentre is where the earthquake occurred and is denoted by its latitude, longitude and depth.
The epicentre is just the latitude and longitude of the earthquake.
For an earthquake that occurs at depth (most earthquakes occur between 5-40 km depth), the depth of the earthquake can be constrained by measuring the arrival time of both the first arrival P-wave and the surface reflection phases called little-p big-P (pP). Note that the time separation between P and pP phases increases with the increasing depth of the earthquake.

7. Force types: linear, couple, double couple
linear-force cc force-couple c force-couple double couple
Torques
Forces
Elastic medium
A force has direction and magnitude. A linear force is just one force vector. A torque is a rotational force that requires two force vectors and is define as τ=2F*d where d is the ½ length of moment arm. A double couple is two force couples with opposite signs; this means the net torque is ZERO! All earthquakes are double-couples, otherwise angular momentum would NOT be conserved (a mortal sin!). Not confirmed until 1950’s!

8. Seismic P and S-wave radiation patterns to applied force impulse (hammer blow)
When a force is applied over a finite time, the force-impulse (F*∆t) excites radiation of seismic (elastic) waves. (a) The direction of the hammer impulse makes the rock to the north compress and the rock to the south dilitate which is the P-wave. S-wave radiate to the E and W. (b) Given the direction of the force-impulse (hammer blow), the first motion recorded by station to the north will be compressive, and conversely the first motion recorded to the south will be dilitational. (c) S-wave radiation pattern is a maximum in the E and W directions. Note that the S-waves are transverse waves.

9. Earthquake double couple force
The force system driving an earthquake is a double couple. WHY ?
The fault plane, its displacement, and the auxiliary fault plane.
The P-wave radiation pattern. (+) defines compressional (up) first motion and (-) defines dilitational (down) first motion. The double couple force system that drives the earthquake defines a compression and tension axis at 45⁰ angle to the fault and auxiliary planes.

10. First motion of P-wave
Important: from the seismic first motion analysis it is IMPOSSIBLE to know which of the two planes is the one that ruptures (the fault or auxiliary plane). One must use other information to resolve the fault plane ambiguity.

11. Lower hemisphere focal sphere
To handle arbitrary fault planes in 3-dimensions, a sphere is place around the earthquake hypocentre. The sphere is oriented with respect to the cardinal directions.
Shows the fault and auxiliary fault planes (strike and dip).
(b) Because 3-d drawings are a pain, a lower hemisphere projection is used to exactly represent the geometry in (a). The hypocenter is at the middle of the ‘beach-ball’ and the fault and its auxiliary plane are shown. The P-wave first-motion for rays going downwards are shaded gray (compressional) and white (dilatational).

12. Different fault types: normal, thrust, strike-slip
Different fault types make different beach-ball patterns of compressional and dilitational first motion of the P-wave. Note that the normal and thrust fault planes are the same but the pattern of compression/dilitation is reversed.

14. Plate kinematics and Earthquake mechanisms

15. Max/min stress axes orientation and fault type
σ1 Maximum stress axis
σ3 Minimum stress axis
σ2 Intermediate stress axis

16. Finding ‘best’ fault/auxiliary fault plane using measured first-motions and ‘stereonet’ analysis

17. Double couples again Single couple Single couple makes Rotation WRONG!
Double couple force equivalent
The double couple shown in (d) is equivalent to a compressional stress axis (C-C’) and a tensional (dilatational) stress axis (P-P’)!
Double couple

18. Rupture dimensions and displacement
A fault is often described by three parameters: a plane with a width (W) and length (L) and the average displacement (D) that occur on the fault plane.

19. Earthquake (main shock) and after-shocks
After a significant size earthquake, residual stress exists that cause small earthquakes called ‘after-shocks’. These aftershock can be used to map the vertical and lateral extent (i.e., spatial size) of the main-shock.

20. Measuring ground displacement from GPS to constrain fault plane size
The number are in meters (m) of horizontal displacement caused by the quake.

22. Definition of seismic moment
The definition of the moment for a linear force is M = F*d (N-m).
The definition of the moment of a force couple is: M = F*2b (N-m).
Seismic moment is how seismologist represent the magnitude (energy) of a quake.

23. Use of Rayleigh and Love (surface) waves to estimate earthquake focal mechanism and moment
Using the recorded surface waves to measure earthquake source parameters (time and location and depth) is easy to do and routine. Within seconds after the waves from any earthquake larger than magnitude 5.5 are recorded by a few seismometers, an automatic focal mechanism and moment estimate (magnitude) are calculated and sent out as real-time warnings.

25. A simple definition of seismic magnitude (relative scale)
If one can estimate the distance to the quake using the S-P time and the peak
amplitude of the S-wave, a seismic magnitude (not moment) can be calculated.

26. Regional seismic moment analysis
By adding up all the seismic moment measured from seismograms, one can check to see if the earthquakes are accommodating most of the measured displacement (e.g., as measured by GPS).
It turns out that this analysis shows that most of the displacement on major faults is accommodated by the slip the occurs during infrequent earthquakes.
However, sometimes a fault does NOT make big earthquakes, but instead ‘creeps’ and only makes many small quakes.
e.g., the creeping section of the San Andreas fault shown at left.

27. Importance of accurate velocity model to locate earthquakes

28. Rupture length and seismic moment scaling
(b) Shows that larger earthquake (bigger moments) have bigger rupture lengths.
This is called a scaling. It means that big displacements do NOT happen on small fault plane area!

29. Scaling between energy and moment magnitude
This shows the relation between moment magnitude and energy. On a log base 10 scale (a), the moment versus energy relation is a straight line. This means that moment magnitude is a logarithmic scale (as defined!).

30. Guttenberg-Richter scaling relation
This straight line relation between the logarithm of the number of earthquakes and their magnitude is called the Guttenberg-Richter relation. This means that are A LOT more small earthquakes occur with respect to big earthquakes : e.g., there are a 100,000 magnitude 4 quakes for every magnitude 8 quake! A deep physics finding from this ‘power law’ relation is that earthquakes are a manifestation of a ‘self-organized critical system’.

31. Energy release of earthquakes

32. Real-time global seismic network
Earthquakes are computer detected and located within about 5 sec after P-waves arrive at stations to guide damage estimates and provide tsunami warnings.

33. Weekly earthquakes detected by GSN for 8 months

34. Global Earthquakes Mb > 5.2

36. Damaging Earthquake Risk

37. So. California Earthquake rupture South California 3-d earthquake
So. California Earthquake rupture South California 3-d earthquake.mov seismic earth waves homo.avi

38. Fault induced stress change

39. INSAR demonstration