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What
causes contrasting P-T paths of HP rocks in the same subduction
complex?
Take a
look at the video!
Basado en una presentación suministrada por
Taras V. Gerya en marzo de 2021.
Véase: Taras
V. Gerya Bernhard Stöckhert Alexey L. Perchuk (2002). Exhumation of
high‐pressure metamorphic rocks in a subduction channel: A numerical
simulation. Tectonics Volume 21, Issue 6, Pages 6-1-6-19.
https://doi.org/10.1029/2002TC001406
What
causes contrasting P-T paths of HP rocks in the same subduction
complex?
Fusión parcial en el manto
Yaoling Niu (2021) Lithosphere thickness controls the extent of
mantle melting, depth of melt extraction and basalt compositions in
all tectonic settings on Earth – A review and new perspectives.
Earth-Science Reviews 2021, 103614.
https://www.sciencedirect.com/science/article/pii/S0012825221001148?via=ihub#f0015
Un ejemplo de
evolución P-T-t: Mélange de la Sierra del Convento, Cuba
Información está extraída de:
LÁZARO, C., GARCÍA-CASCO, A., NEUBAURER, F., ROJAS-AGRAMONTE, Y.,
KRÖNER, A., ITURRALDE-VINENT, M.A. (2009) Fifty-five-million-year
history of oceanic subduction and exhumation in the northern edge of
the Caribbean plate (Sierra del Convento mélange, Cuba). Journal of
Metamorphic Geology, 27, 19-40. DOI 10.1111/j.1525-1314.2008.00800.x
ABSTRACT. Petrological and
geochronological data of six representative samples of exotic blocks
of amphibolite and associated tonalite‐trondhjemite from the
serpentinitic mélange of the Sierra del Convento (eastern Cuba)
indicate counterclockwise P–T paths typical of material subducted in
hot and young subduction zones. Peak conditions attained were ca.
750 °C and 15 kbar, consistent with the generation of tonalitic
partial melts observed in amphibolite. A tonalite boulder provides a
U‐Pb zircon crystallization age of 112.8±1.1 Ma, and Ar/Ar amphibole
dating yielded two groups of cooling ages of 106–97 Ma (interpreted
as cooling of metamorphic/magmatic pargasite) and 87–83 Ma (interpreted
as growth/cooling of retrograde overprints). These geochronological
data, in combination with other published data, allow the following
history of subduction and exhumation to be established in the region:
(i) a stage of hot subduction 120–115 Ma, developed upon onset of
subduction; (ii) relatively fast near‐isobaric cooling (25 °C·Myr−1)
115–107 Ma, after accretion of the blocks to the upper plate
lithospheric mantle; (iii) slow syn‐subduction cooling (4 °C·Myr−1)
and exhumation (0.7 km·Myr−1) in the subduction channel 107–70 Ma;
and (iv) fast syn‐collision cooling (74 °C·Myr−1) and exhumation (5
km·Myr−1) 70–Ma.
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