Backbone of the Americas: Shallow Subduction, Plateau by Suzanne Mahlburg Kay, Victor A. Ramos, William R. Dickinson

By Suzanne Mahlburg Kay, Victor A. Ramos, William R. Dickinson

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By Suzanne Mahlburg Kay, Victor A. Ramos, William R. Dickinson

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Read Online or Download Backbone of the Americas: Shallow Subduction, Plateau Uplift, and Ridge and Terrane Collision (Geological Society of America Memoir 204) PDF

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Extra resources for Backbone of the Americas: Shallow Subduction, Plateau Uplift, and Ridge and Terrane Collision (Geological Society of America Memoir 204)

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12A) in addition to Cayman strike slip. Eastern extensions of the Cayman transform system beyond the limit of the Cayman Trough disrupted and displaced segments of the Greater Antilles arc in islands lying to the south and east of Cuba (Figs. 12A and 12B). Restoration of Cayman-related strike slip clarifies the relation of the ancestral Cretaceous-Paleogene Antillean arc system, which includes increments as old as mid-Cretaceous in age (Pin- dell and Barrett, 1990), to North and South America (Fig.

12B). Along the northern fringe of Cuba, the north-facing Greater Antilles island arc partially subducted the southern edge of Florida– Bahama carbonate platforms in late Eocene time (45–40 Ma). The western end of the colliding arc system was bounded by the Yucatan transform (Fig. 12B), along which the western end of the arc slid northward with respect to North America. The Yucatan basin was formed as a backarc basin that was later trapped north of the Cayman Trough (Fig. 12A) by lateral displacement of the continental Chortis block and Nicaraguan Rise.

11) were subparallel to the trends of the migratory volcanic fronts, and not parallel to the directions of arc migration. This relation argues that backarc crustal extension was driven by deviatoric intracrustal stresses oriented normal to the axis of crustal thickening along the Cordilleran orogen, and it was not controlled in azimuth by the migration path of the evolving arc axis. Basin-range block faulting of classic style began at ca. 5 Ma in the northern Basin and Range Province, within the Numic subtaphrogen (Dickinson, 2002), which was located to the west and northwest of the Colorado Plateau, but this faulting was delayed until ca.

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