GEOLOGY 415/515: EARTHQUAKE GEOLOGY C. Rubin, Central Washington University
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Transcript of GEOLOGY 415/515: EARTHQUAKE GEOLOGY C. Rubin, Central Washington University
GEOLOGY 415/515:EARTHQUAKE GEOLOGY
C. Rubin, Central Washington University
INTEGRATE COMPLEMENTARY TECHNIQUES TO STUDY LITHOSPHERIC DEFORMATION
Each have strengths & weaknesses
Important to understand what can & can’t do
Jointly give valuable insight
Introduction
Earthquakes: fundamental concepts & focal mechanisms
Earthquakes: magnitude, earthquake cycle
Tectonic geodesy
Strike-slip faults
Normal faults
Subduction zones (Megathrust earthquakes)
Thrust/Reverse faults
Plate interiors
Earthquake recurrence & hazards
Studying the lithosphere involves integrating plate tectonics, seismology, geodesy, geology, rock mechanics,
thermal studies, modeling and much more
No clear dividing lines between subfields
“When we try to pick out anything by itself, we find it hitched to everything else in the universe.”
John Muir
“Half of what we will teach you in the next few years is wrong. The problem is we don’t know which half”
Medical school dean to incoming students
EARTHQUAKES & TECTONICSLocations map
plate boundary zones & regions of intraplate deformation even in underwater or remote areas
Focal mechanisms show strain field
Slip & seismic history show deformation rate
Depths constrain thermo-mechanical structure of lithosphere
PACIFIC
NORTH AMERICA
San Andreas Fault, Carrizo Plain
36 mm/yr
PLATE KINEMATICS, directions and rates of plate motionsCan observe directlyPrimary constraint on lithospheric processes
PLATE DYNAMICS, forces causing plate motions Harder to observe directly Observe indirect effects (seismic velocity, gravity, etc) Models are key Closely tied to mantle dynamicsKinematics primary constraint on models
Most destructive earthquakes occur where large populations live near plate boundaries.
The highest property losses occur in developed nations where more property is at risk, whereas fatalities are highest in developing nations.
Estimates are that the 1990 Northern Iran shock killed 40,000 people, and that the 1988 Spitak (Armenia) earthquake killed 25,000.
Even in Japan, where modern construction practices reduce earthquake damage, the 1995 Kobe earthquake caused more than 5,000 deaths and $100 billion of damage.
On average during the past century earthquakes have caused about 11,500 deaths per year.
The earthquake risk in the United States is much less than in many other countries because large earthquakes are relatively rare in most of the U.S. and because of earthquake-resistant construction
EARTHQUAKES & SOCIETY
Hazard is the intrinsic natural occurrence of earthquakes and the resulting ground motion and other effects.
Risk is the danger the hazard poses to life and property.
Although the hazard is an unavoidable geological fact, risk is affected by human actions.
Areas of high hazard can have low risk because few people live there, and areas of modest hazard can have high risk due to large populations and poor construction.
Earthquake risks can be reduced by human actions, whereas hazards cannot
Bam, Iran earthquake: M 6.5 30,000 deathsSan Simeon, CA earthquake: M6.5 2 deaths
Earthquakes don’t kill people (generally, tsunami exception), buildings kill people
NATURAL DISASTERS: HAZARDS AND RISKS
Earthquake locations map narrow plate boundaries, broad plate boundary zones & regions of intraplate deformation
even in underwater or remote areas
INTRAPLATE
NARROW BOUNDARIES
DIFFUSE BOUNDARY ZONES
BASIC CONCEPTS:
KINEMATICS CONTROL
BOUNDARY NATURE
Direction of relative motion between plates at a point on their boundary determines the nature of the boundary.
Spreading centers - both plates move away from boundary
Subduction zones - subducting plate moves toward boundary
Transform faults - relative plate motion parallel to boundary
Real boundaries often combine aspects (transpression, transtension)
Transtension - Dead Sea transform
Arabia
Sinai
4 mm/yr
Boundaries are described either as
- midocean-ridges and trenches - emphasizing morphology
- or as divergent (spreading centers) and
-convergent (subduction zones) - emphasizing kinematics
NOMENCLATURE:
Latter nomenclature is more precise because there are
- elevated features in ocean basins that are not spreading ridges
- spreading centers like theEast African rift within continents
-continental convergent zones like the Himalaya may not have active subduction
BOUNDARY TYPE CHANGES WITH ORIENTATION
PACIFIC - NORTH AMERICA
PACIFIC wrt NORTH
AMERICApole
CONVERGENCE - ALEUTIAN TRENCH
54 mm/yr
EXTENSION -GULF OF CALIFORNIA
STRIKE SLIP - SAN ANDREAS
1989 LOMA PRIETA, CALIFORNIA EARTHQUAKEMAGNITUDE 7.1 ON THE SAN ANDREAS
Davidson et alDavidson et al
1989 LOMA PRIETA, CALIFORNIA EARTHQUAKE
The two level Nimitz freeway collapsed along a 1.5 km section in Oakland, crushing cars
Freeway had been scheduled for retrofit to improve earthquake resistance
1989 LOMA PRIETA, CALIFORNIA EARTHQUAKE
Houses collapsed in the Marina district of San Francisco
Shaking amplified by low velocity landfill
1964 ALASKA EARTHQUAKE Ms 8.4 Mw 9.1
Pacific subduction beneath North America
~ 7 m of slip on 500x300 km2 of Aleutian Trench
Second or third largest earthquake recorded to date
~ 130 deaths
Catalyzed idea that great thrust fault earthquakes result from slip on subduction zone plate interface
TRENCH-NORMALCONVERGENCE - ALEUTIAN TRENCH54 mm/yr
PACIFIC NORTH AMERICA
1971 Ms 6.6 SAN FERNANDO EARTHQUAKE
1.4 m slip on 20x14 km2 fault
Thrust faulting from compression across Los Angeles Basin
Fault had not been previously recognized
65 deaths, in part due to structural failure
Prompted improvements in building code & hazard mapping
Caused some of the highest ground accelerations ever recorded. Even a moderate magnitude earthquake can cause considerable damage in a populated area.
Although the loss of life (58 deaths) was small due to earthquake-resistant construction the $20B damage makes it the most costly earthquake to date in the U.S.
Los Angeles Basin
Thrust earthquakes
indicate shortening
1994 Northridge Ms 6.7
AFTTERSHOCKS
Materials at distance on opposite sides of the fault move relative to each other, but friction on the fault "locks" it and prevents slip
Eventually strain accumulated is more than the rocks on the fault can withstand, and the fault slips in earthquake
Earthquake reflects regional deformation
ELASTIC REBOUND OR SEISMIC CYCLE MODEL
Earthquakes are most dramatic part of a seismic cycle occuring on segments of the plate boundary over 100s to 1000s of years.
During interseismic stage, most of the cycle, steady motion occurs away from fault but fault is "locked", though some aseismic creep can occur on it.
Immediately prior to rupture is a pre-seismic stage, that can be associated with small earthquakes (foreshocks) or other possible precursory effects.
Earthquake itself is coseismic phase, during which rapid motion on fault generates seismic waves. During these few seconds, meters of slip on fault "catch up" with the few mm/yr of motion that occurred over 100s of years away from fault.
Finally, postseismic phase occurs after earthquake, and aftershocks and transient afterslip occur for a period of years before fault settles into its steady interseismic behavior again.
ELASTIC REBOUND OR SEISMIC CYCLE MODEL
Materials at distance on opposite sides of the fault move relative to each other, but friction on the fault "locks" it and prevents slip
Eventually strain accumulated is more than the rocks on the fault can withstand, and the fault slips in earthquake
Earthquake reflects regional deformation
ELASTIC REBOUND OR SEISMIC CYCLE MODEL
1906 SAN FRANCISCO EARTHQUAKE (magnitude 7.8)
~ 4 m of slip on 450 km of San Andreas ~2500 deaths, ~28,000 buildings destroyed (most by fire)
Catalyzed ideas about relation of earthquakes & surface faults
Boore, 1977
Over time, slip in earthquakes adds up and reflects the plate motion
Offset fence showing 3.5 m of left-lateral strike-slip motion along San Andreas fault in 1906 San Francisco earthquake
~ 35 mm/yr motion between Pacific and North American plates along San Andreas shown by offset streams & GPS
Expect earthquakes on average every ~ (3.5 m )/ (35 mm/yr) =100 years
Turns out more like 200 yrs because not all motion is on the San Andreas
Moreover, it’s irregular rather than periodic
SEISMIC CYCLE AND PLATE MOTION
EARTHQUAKE RECURRENCE IS HIGHLY VARIABLEReasons are unclear: randomness, stress effects of other
earthquakes on nearby faults…
M>7 mean 132 yr s 105 yr
Sieh et al., 1989
Extend earthquake history with paleoseismology
CHALLENGES OF STUDYING EARTHQUAKE CYCLE
Cycle lasts hundreds of years, so don’t have observations of it in any one place
Combine observations from different places in hope of gaining complete view
Unclear how good that view is and how well models represent its complexity
Research integrates various techniques:
Most faults are identified from earthquakes on them: seismology is primary tool to study the motion during earthquakes and infer
long term motion
Plus
- Historical records of earthquakes
- Field studies of location, geometry, and history of faults
- Geodetic measurements of deformation before, during, and after earthquakes
- Laboratory results on rock fracture
SAR image of Hayward fault (red line), part of San Andreas fault system, in the Berkeley (east San Francisco Bay) area. Color changes from orange to blue show about 2 cm of gradual movement.
This movement is called aseismic creep because the fault moved slowly without generating an earthquake
GEODETIC DATA GIVE INSIGHT INTO DEFORMATION BEYOND THAT SHOWN SEISMOLOGICALLY
Study aseismic processes
Study seismic cycle before, after, and in between earthquakes, whereas we can only study the seismic waves once an earthquake occurs
ELASTIC REBOUND MODEL OF STRIKE-SLIP FAULT AT A PLATE BOUNDARY
Large earthquakes release all strain accumulated on locked faultbetween earthquakes
Coseismic and interseismic motion should equal relative plate motion
Interseismic strain accumulates near fault
ELASTIC REBOUND MODEL OF STRIKE-SLIP FAULT AT A PLATE BOUNDARY
Fault parallel interseismic motion on fault with far field slip rate D, locked to depth W, as function of cross-fault distance y
s(y) = D/2 + (D / π) tan -1 (y/W)
Width of strain accumulation zone comparable to locking depth
FAR FIELD SLIP RATE D ~ 35 mm/yr
Z.-K. Shen
PACIFIC-NORTH AMERICA PLATE BOUNDARY ZONE: PLATE MOTION &
ELASTIC STRAIN
~ 50 mm/yr plate motion spread over ~ 1000 km
~ 35 mm/yr elastic strain accumulation from locked San Andreas in region ~ 100 km wide
Locked strain will be released in earthquakes
Since last earthquake in 1857 ~ 5 m slip accumulated
Elastic strain
Broad PBZ
EARTHQUAKE CYCLE
INTERSEISMIC:
India subducts beneath Burma at about 20 mm/yr
Fault interface is locked
EARTHQUAKE (COSEISMIC):
Fault interface slips, overriding plate rebounds, releasing accumulated motion and generating tsunami HOW OFTEN:
Fault slipped ~ 10 m --> 10000 mm / 20 mm/yr = 500 yrLonger if some slip is aseismic
Faults aren’t exactly periodic, likely because chaotic nature of rupture controls when large earthquakes occur
INDIA BURMA
Tsunami generated
SUMATRA TRENCH
TSUNAMI GENERATED ALONG FAULT, WHERE SEA FLOOR DISPLACED, AND SPREADS
OUTWARD
http://staff.aist.go.jp/kenji.satake/animation.gif
Red - up motion, blue downHyndeman and Wang, 1993
SEISMIC WAVES
COMPRESSIONAL (P)
AND SHEAR (S) WAVES
P waves longitudinal
waves
S waves transverse
waves
P waves travel faster
S waves from earthquake
generally larger
EARTHQUAKE LOCATION
Least squares fit to travel times
Accuracy (truth) depends primarily on velocity model
Precision (formal uncertainty) depends primarily on network geometry (close stations & eq within network help)
Locations can be accurate but imprecise or precise but inaccurate (line up nicely but displaced from fault)
Epicenters (surface positions) better determined than depths or hypocenters (3D positions) because seismometers only on surface
IMPROVE EARTHQUAKE LOCATION
Precision can be improved by relative location methods like Joint Epicenter Determination (JED) or master event
Or via better velocity model, including methods that simultaneously improve velocity model (double-difference tomography)
Dewey, 1987
IMPROVE EARTHQUAKE LOCATION
Precision can be improved by relative location methods like Joint Epicenter Determination (JED) or master event
Or via better velocity model, including methods that simultaneously improve velocity model (double-difference tomography)
Dewey, 1987