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We have studied the geochemistry of 3 subduction melange units from the Shimanto belt of Japan using XRD, XRF, and La-ICPMS.

The subduction thrust interface represents a zone of concentrated deformation, coupled to fluid generation, flow, and escape. Here, we review the internal structure of the megathrust as exposed in exhumed accretionary complexes, and identify a deformation sequence that develops as material entering the trench is subducted through the seismogenic zone. Initial ductile flow in soft sediment generates dismembered, folded and boudinaged bedding that is cross-cut by later brittle discontinuities. Veins formed along early faults, and filling hydrofractures with the same extension directions as boudins in bedding, attest to fluid-assisted mass transfer during the shallow transition from ductile flow to brittle deformation. In higher metamorphic grade rocks, veins cross-cut foliations defined by mineral assemblages stable at temperatures beyond those at the base of the seismogenic zone. The veins are, however, themselves ductilely deformed by diffusion and/or dislocation creep, and thus record fracture and fluid flow at a deeper brittle-to-ductile transition. The results of numerical models and mineral equilibria modeling show that compaction of pore spaces may occur over a wide zone, as under-consolidated sediments carry water under the accretionary prism, to where the last smectite breaks down at a temperature of ≤ 150˚C. However, at temperatures above clay stability, no large fluid release occurs until temperatures where lawsonite, and subsequently chlorite, break down, generally in excess of 300˚C. In thermal models and strength calculations along overpressured subduction interfaces where phyllosilicates form an interconnected network that controls rheology, as is generally observed, the deep brittle-viscous transition – analogous to the base of the seismogenic zone – occurs at temperatures less than 300˚C. We therefore suggest that the seismogenic zone does not produce fluids in significant volumes; however, major fluid release occurs at or near the base of the seismogenic zone. These deep fluids are either trapped, thus enabling embrittlement and features such as episodic tremor and slow slip, or flow updip along a permeable interface. Overall, we highlight fluid production as spatially intermittent, but fluid distribution as controlled also by the permeability of a deforming zone, where secondary porosity is both generated and destroyed, commonly in sync with the generation and movement of fluids.

Table of Contents; Letter from the Editorial Committee Chair; 2011-12 Editorial Committee members

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