Relatively few data have been published that demonstrate that sediment gravity flows can be generated from slides and slumps. Such evidence can be found in a north-trending, seaward-prograding, continental-slope sequence which existed in central Nevada during the early Paleozoic. Translational slides on this slope are up to 400 m wide and 10 m thick. These slides moved semilithified, black, thin-bedded, hemipelagic limestone. Once the slide was in motion its transformation into mass flows began at its base and thin margins. Probably the rupture strength of these parts of the slide was exceeded and movement by plastico-viscous flow resulted because of a variety of factors which includes strain, mechanical shock, and incorporation of water. The development of clasts in the asal shear zone and thin margins of the slides resulted from overfolds and nearly horizontal beds within the slides which gradually separated into thin tabular fragments. Clast development progressed as the slide continued to move downslope until the base and margins of the slide attained a completely conglomeratic texture. The clasts at this stage assumed a random or subparallel orientation supported by a carbonate mudstone matrix.

Conglomeratic debris-flow deposits generated by these slides occur in channels up to 400 m wide and 12 m thick. Field data suggest that a downslope transition occurs from debris flow to turbidity-current flow. Many of the conglomeratic turbidity-current flows on the lower slope probably originated as debris flows which in turn were generated from slides higher on the slope. These turbidity-flow deposits occur in channels up to 100 m wide and 2 m thick and contain clasts identical to those in the debris-flow deposits.

A further genetic link may exist between these slides and the slide-generated mass-flow deposits. The mechanics of flow and the resulting fabric and sedimentary structures in the mass-flow deposits were influenced by the nature of the clasts generated by the slides. Preliminary data suggest that the size, shape, and original orientation of the slide-derived clasts were strongly controlled by the bedding characteristics, degree of induration, and style of deformation of the slides.

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