Plate convergence usually commences with intra-oceanic Subduction, Andean margins commonly start after ophiolite obduction and subduction flip. CONVERGENT PLATE MARGINS Intra-oceanic (ensimatic) subduction Andean margins 3) Continent - continent collision zones. 1). 2). 3).
Subduction, Andean margins commonly start after ophiolite
obduction and subduction flip.
CONVERGENT PLATE MARGINS
Intra-oceanic (ensimatic) subduction
3) Continent - continent collision zones
REMEMBER, IN 3-D A CONVERGENT MARGIN MAY
HAVE DIFFERENT MATURITY ALONG STRIKE!
Frp = g e (m – w) (L/3 +e/2) ≈ 2*1012 Nm-1
Can also be expressed as a function of age:
Frp = gmTt [1 + (m/(m-w)) 2T/] = 1.19x10-3 t (Unit MPa)
g - gravity ≈ 9,8 ms-2
e – elevation of spreading ridge above cold plate ≈ 3,3 km
(e- is a function of the age [t])
m – mantle density, ≈ 3,2 g cm-3w – water density
L – lithosphere thickness ≈ 85km
T - temperature(~1200C), -thermal diffusivity [ms], - coefficient of thermal expansion [ = 3*10-5 K-1]
) - exp(-
= ca 2x1013Nm-1
Thermal Reynolds number
k - conductivity
cp - spesific heat
k - kinematic viscosity
v - subd. velocity
Modeled density structure of subducted MORB, subduction zonesHacker et al. 2003
THE ANATOMY OF A SUBDUCTION COMPLEX and spinel to post-spinel (oxides)
Please notice that Benioff zones frequently have an irregular shape in 3-D (ex.
Banda Arc). 80% of all seismic energy is released in Benioff zones.
The low geotherm in subductions zones makes them the prime example of high P -
low T regional metamorphic complexes. The high geotherm in the arc-region gives
contemporaneous high-T low P regional metamorphism, together these two regions
give rise to a feature known as”Paired Metamorphic Belts”
Accreationary Prism, and spinel to post-spinel (oxides)
Example from Scotland.
Late Ordovician to Late Silurian ca 450-420 Ma
PAIRED METAMORPHIC BELTS and spinel to post-spinel (oxides)
Blueshists normally and spinel to post-spinel (oxides)
Seismic quality factor (Q): The ability to transmitt seismic energy
without loosing the energy. Low Q in high-T regions.
Seismic quiet zones---NB potential build-up to very large quakes!
Arc-splitting - tensional regime above subductions zones. Subduction
High heat-flow in the supra-subductions zone regime give rise to
relatively low shallow sealevel above the back-arc basins. Most
ophiolite complexes have their origin is a supra-subduction environment
3 - D MORPHOLOGY and spinel to post-spinel (oxides)
NB! NOTICE INTRA-SLAB
26/12-2004, Mag 9 earthquake of Sunda arc - Andaman sea and spinel to post-spinel (oxides)
Link: and spinel to post-spinel (oxides)fault plane solution
Link: displacement magnitude
Link: earthquake information in general
The amount of energy radiated by an earthquake is a measure of the potential for
damage to man-made structures. Theoretically, its computation requires summing
the energy flux over a broad suite of frequencies generated by an earthquake as
it ruptures a fault. Because of instrumental limitations, most estimates of energy
have historically relied on the empirical relationship developed by Beno Gutenberg
and Charles Richter:
log10E = 11.8 + 1.5MS
where energy, E, is expressed in ergs.
The drawback of this method is that MS is computed from an bandwidth between
approximately 18 to 22s. It is now known that the energy radiated by an
earthquake is concentrated over a different bandwidth and at higher frequencies.
With the worldwide deployment of modern digitally recording seismograph with
broad bandwidth response, computerized methods are now able to make accurate
and explicit estimates of energy on a routine basis for all major earthquakes. A
magnitude based on energy radiated by an earthquake, Me, can now be defined,
Me = 2/3 log10E - 2.9.
For every increase in magnitude by 1 unit, the associated seismic energy increases
by about 32 times.
Although Mw and Me are both magnitudes, they describe different physical properites
of the earthquake. Mw, computed from low-frequency seismic data, is a measure of
the area ruptured by an earthquake. Me, computed from high frequency seismic data,
is a measure of seismic potential for damage. Consequently, Mw [MW = 2/3 log10(MO) - 10.7]
Mw= µ(area)(displacement)]and Me often do not have the same numerical value.
Frictional heating on faults may result in melting of any rock-coposition
Stress-measurements from grain-size and/or dislocation density (4 to 5 x1013m-2)
in olivine associated with pseudotachylytes in peridotite indicate that peridotites
(mantle rocks) may sustain extreme differential stress: 1-3≈ 3-600 MPa.
Assuming a fault with a modest displacement of d ≈ 1m, and a differential
stress of 300 MPa the release of energy according to equation
(1): Wf = Q + E where Q = heat and E = seismic energy is
Wf = d n = d (1-3)/2 =1m(300MPa)/2 ≈ 1.5 x 108 J m-2 or 47 kWhm-2.
The seismic energy (E) is commonly estimated to be < 5% of Wf on a strong fault, ie.
less than 2.3 kWh m-2 is radiated as seismic waves, the remaining energy (Q) turns to
heat and surface energy (difficult to measure) along the fault.
The process is adiabatic since the fault movement occurs in seconds and no heat is lost
by conduction (thermal diffusivity ~1.5 mm2s-1).
Taking the heat capacity of lherzolite, Cp = 1150 J kg-1 oC-1 and a heat of fusion (Fo)
H = 8.6 x106 Jkg-1 the thermal energy (equation 4) required to melt one kg of peridotite:
(4) Q = Cp(T) + H = 1150Jkg-1oC-1 (1200oC) + 8.6 x106 Jkg-1 = 2.7 x 105 Jkg-1.
On a fault with D = 1m, ~60 kg lherzolite may melt pr m2 of the fault plane,
corresponding to an approximately 2 cm thick layer of ultramafic pseudotachylyte.