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earthquakes

earthquakes
earthquakes

Just the Basics…

Rock Deformation & Past Plate Tectonics

different plate tectonic boundaries = different stresses

different stresses = different deformation of rocks

so, reverse is also possible:

from present rock deformation, we can interpret past stresses

& past plate tectonic patterns

Stress can be uniform (pressure) or directed

Simple burial results in uniform stress.

But plate tectonics can produce three types of directed stress:

TENSIONAL–plates pull apart, stretches rock

COMPRESSIONAL– plates push together, squeezes rock

SHEAR–plates slip past one another, distorts rock

while stress is the force that acts on a rock, strain or deformation is the response of the rock to that stress

Deformation (strain) has three stages:

Elastic Deformation - reversible;

energy stored & released

as stress decreases, rock reverts to its original size and shape.

(elastic behavior)

If the elastic limit is exceeded, then Ductile Deformation occurs –non-reversible, permanent change in size and/or shape.

('plastic' behavior)

If stress increases beyond the range of ductile deformation,

the rock Fractures (brittle behavior)

Whether a rock behaves in a brittle or ductile manner depends on:

composition

rate of stress

high rate (fast) -> brittle behavior.

temperature

high temp (deep) -> ductile behavior

pressure of overlying rocks

high (deep) -> ductile behavior

ductile rock deformation (folding) tend to be slow (years to million's of yrs) while brittle deformation (fracture/faulting) can be abrupt (seconds)

Ductile Deformation varies by type of stress:

Tension – stretching & thinning

Shear – distortion

Compression – folds

so, widespread folding generally linked to convergent plate margins

Brittle Deformation

Fracture can result in joints or faults:

joints– fractures w/ no movement

(often due to release of pressure as rocks are exposed at surface) important in groundwater flow and weathering/erosion

faults - fractures along which movement has occurred

(due to directed stress)

important in earthquakes and interpreting past tectonic events

as with ductile deformation,

different plate tectonic processes = different stresses

different stresses = different fault types

so in present rock record:

different faults = different stresses = different plate tectonic history

generally, only relative motion can be determined,

not worried about absolute motion

Faults with dominantly vertical motion

(Dip-Slip Faults)

1. Normal Faults

form from tensional stresses

dominate at divergent boundaries

(rift zones and spreading centers)

2. Reverse Faults

form from compressional stress

dominate at convergent boundaries

(subduction & continent collision zones)

Faults with dominantly horizontal motion

(Strike-Slip Faults)

Right-Lateral and Left-Lateral relative motions occur

form from shear stress

dominate along transform plate margins

Earthquakes

Most earthquakes result from sudden movement along faults,

released energy was stored during elastic deformation.

and shaking (‘quaking’) of earth is itself an example of elastic behavior

but faulting is brittle behavior,

so earthquakes only occur in the lithosphere.

(asthenosphere & lower mantle deform in ductile fashion

due to high pressure and temperature)

rocks strongest under compression

rocks weakest under tension

so strength of earthquakes reflects type of stress

The origin of an earthquake is its focus (hypocenter)

(usually <100 km, but can be up to 700 km deep in subduction zones)

A quake's epicenter is the area on the surface of the earth

directly above its focus.

The locations & depths of most earthquakes

are related to their plate tectonic setting.

shallow depth = <70 km

intermediate depth = 70 - 300 km

deep depth = 300 – 670 km

Divergent Plate Boundaries

1) continental rifts

earthquakes occur along normal faults

are usually weak and shallow

2) spreading centers

most earthquakes occur along normal faults

(or strike slip faults on transform offsets)

are usually weak and always very shallow

(<20 km)

Transform Plate Boundaries

earthquakes tend to occur along strike-slip faults;

most transform faults link segments of ocean ridges, earthquakes along these oceanic transform faults are usually weak, as lithosphere is thin and

warm

( shallow quakes <20 km)

earthquakes along continental transform boundaries are also shallow, but can be much stronger as lithosphere is cool and thick

Convergent Plate Boundaries

1) continent collision boundaries

earthquakes tend to occur on reverse faults,

can be very strong, and extend to 300 km depth.

2) subduction boundaries

Some very shallow, relatively weak earthquakes occur on normal faults

along top surface of bending plate

but most earthquakes occur on reverse faults in both subducting and

overriding plates

quakes can be up to 670 km deep!

because they form from compression,

shallow quakes in subduction zones can be very powerful

Intraplate Earthquakes

are relatively rare and are generally shallow, moderate quakes

however one of the strongest series of quakes recorded at

New Madrid, Missouri - 1811-1812

along an ancient failed continental rift

because lithosphere is cool and unbroken,

damage can extend across a wide area

Seismic Waves

Energy released during an earthquake is transmitted as

seismic waves

Only energy moves through Earth, no material

Seismic waves include both

body and surface waves

Body waves travel through a medium

(ex. - sound waves)

Surface waves travel along the medium's surface

(ex. - water waves)

Compression Waves or P- Waves (Primary) fastest seismic waves, first to arrive at a seismic station alternating stages of compression and expansion,

in the direction of wave travel

These waves change both the volume and density of the material they travel through

(so they can travel through gas, liquid or solid)

Shear Waves or S- Waves (Secondary)

Second waves to arrive at a seismic station

shear forces perpendicular to the direction of wave travel

These waves change only the shape of the material they travel through.

as gases and liquids are not elastic,

shear waves can only travel through solids.

Surface Waves

last to arrive at a seismic station, but have greatest amplitude cause most earthquake dam age, but yield no information on Earth’s interior

at least two types:

snake-like side to side motion

rolling wave - similar to water waves

Because of the differences in their speed, the arrival of seismic waves can

be used to locate earthquakes

Earthquakes also provide most of our knowledge of the Earth's interior. Detailed study of seismic body waves reveal variations in temperature,

composition and physical state.

?denser material = faster

?more rigid material = faster

?cooler material = faster

Seismic waves are refracted and reflected at physical boundaries.

Different types of waves react differently to physical state.

You will be expected to know how P-waves and S-waves react at boundaries between different Earth layers!

crust/mantle (moho)

change: P S

lithosphere/LVZ (asthenosphere)

change: P S

base of LVZ (asthenosphere)

change: P S

transition zone (400 and 670 km)

change: P S

mantle/core = lower mantle/outer core

only boundary where composition and physical state both change change: P S

outer core/inner core

change: P S

Earthquakes and Society

Different scales are used to measure earthquakes:

R ICHTER S CALE is based on the amplitude of P and S waves

100 kilometers from the epicenter

Moment-Magnitude Scale is more accurate, but its calculation involves amplitude of waves, area and amount of slip as well as characteristics of

rock involved

Both scales are logarithmic!

amplitude of waves on seismograms increases by 10 but each division is equivalent to a ~32x increase in energy!

primary damage – due to ground motion, can be severe

but secondary damage – due to fire, landslides, liquefaction (shaking of

water-saturated soil), and tsunamis

often account for the greatest loss of life and property.

Timing can be critical!

Prediction?

Intrinsic difficulty of mixing human and geologic time scales

long term prediction relatively accurate

but short term prediction may be impossible

Control?

earthquake resistant building is important,

but there is no earthquake-proof construction

1) construction design and 2) emergency response capabilities

are the main factors in reducing earthquake death tolls

Management?

lubricate faults to ‘manage’ motion?

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