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• W2182105286 abstract "The <TEntrecasteaux Zone, encompassing the North d'Entrecasteaux Ridge and the Bougainville Guyot, collide with the central New Hebrides Island Arc. The d'Entrecasteaux Zone trends slightly oblique to the 10-cm/yr relative direction of plate motion so that the ridge and the guyot scrape slowly (2.5 cm/yr) north, parallel to the trench. The North d'Entrecasteaux Ridge consists of Paleogene mid-ocean ridge basalt basement and Pliocene to Pleistocene sediment. The Bougainville Guyot is an andesitic, middle Eocene volcano capped with upper Oligocene to lower Miocene and Miocene to Pliocene lagoonal limestones. Geophysical and geologic data collected prior to Leg 134 indicate that the two collision zones differ in morphology and structure. The North d'Entrecasteaux Ridge extends, with a gentle dip, for at least 15 km eastward beneath the arc slope and has produced a broad (20-30 km), strongly uplifted area (possibly by 1500-2500 m) that culminates at the Wousi Bank. This tectonic pattern is further complicated by the sweeping of the ridge along the trench, which has produced a lobate structure formed by strike-slip and thrust faults as well as massive slumps north of the ridge. South of the ridge, the sweeping has formed large normal faults and slump scars that suggest collapse of arc-slope rocks left in the wake of the ridge. In the Bougainville collision zone, the unbroken cap of the guyot extends for only 1 km eastward beneath the arc slope. In contrast with the arc slope landward of the North d'Entrecasteaux Ridge, the arc slope east of the guyot has been deeply indented and considerably shortened along east-dipping thrust faults. The only equivalent to the Wousi Bank that has developed east of the guyot is a narrow compressive antiform 800 m in height. The collision zones between the North d'Entrecasteaux Ridge and Bougainville Guyot show some similarities. Seismic reflection data suggest that in both zones material from the downgoing plate may accrete locally to the arc slope. Moreover, the arc slope in both collision zones is affected by large mass wasting and strong tectonic erosion. Geophysical data suggest that slump material may be as thick as 2-3 km along the arc slope. Tectonic erosion reaches a maximum when arc-slope rocks collapse in the wake of the North d'Entrecasteaux Ridge and after a seamount disappears in the subduction zone as in the case of the Malakula reentrant south of the Bougainville Guyot. This deep morphological reentrant is interpreted as a scar of a past collision and subduction of a seamount. Geologic data collected during Nautile dives along the arc slope east of the d'Entrecasteaux Zone indicate that the superficial lithology of the arc slope consists of Pliocene to Pleistocene volcaniclastic rocks and sediments derived from the island arc. However, massive lavas and accreted rocks were also found locally along the arc slope. The presence of fractured andesite exposed along the south flank of the Wousi Bank suggests that the North d'Entrecasteaux Ridge collision deformed the island-arc basement. At the toe of the arc slope, against the ridge's north flank, sheared upper Oligocene to lower Miocene nannofossil ooze and chalk are interpreted as rocks accreted from the downgoing plate. Landward of the Bougainville Guyot, a 500-m-thick wedge, including imbricated upper Oligocene to lower Miocene reefal limestones with upper Eocene reefal debris and middle Eocene pelagic sediments, could have formed by tectonic accretion of guyot material." @default.
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• W2182105286 title "2. THE D'ENTRECASTEAUX ZONE-NEW HEBRIDES ISLAND ARC COLLISION ZONE: AN OVERVIEW 1" @default.
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