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Extra info for Ancient Seismites (GSA Special Paper 359)
The base of the channel rests directly on the sand filling of the large vent (clastic dike 1, CD1 in Fig. 4). The absence of any soil development over the vent sand indicates a minimal time interval between the sand blow and channel deposition. The lag-gravel deposit appears to be conformably interbedded with the middle of the stream channel, but laterally lies unconformably over small sand-blow vents, ejected sand from one vent, and the older fluvial and lacustrine deposits. The upper part of the channel, above the lag gravel, accumulated in a syndepositional syncline along the main fault and thus reflects a surface rupture and is interpreted as a paleoseismite.
1984, Surface faulting accompanying the Borah Peak earthquake, Idaho: Geology, v. 12, p. 664–667. , Scott, W. S. Geological Survey Open-File Report 85-290, p. 236–263. , 1989, Source parameters of Montana earthquakes (1925–1964) and tectonic deformation in the northern Intermountain Belt: Bulletin of the Seismological Society of America, v. 79, no. 1, p. 31–50. , Quaternary geology of the Western Madison Range, Madison Valley, Tobacco Root Range, and Jefferson Valley—Rocky Mountain Friends of the Pleistocene, August 15–19, 1990, Fieldtrip Guidebook: Indianapolis, Indiana University, Department of Geology, p.
These features were located with an accuracy of about 1 cm. , Seed, 1968) (Figs. 2 and 3). A northeast-trending line of springs along a poorly defined, degraded (probably due to mass wasting) scarp, which is roughly along the road, appears to mark the fault between these landslides. Overall, this sinuous trace is approximately 19 km long. The maximum scarp height is about 9 m in the vicinity of the trench. Here, the older Pinedale alluvial fan (Figs. 2 and 3) appears to be partially exhumed along a horst and graben set of scarps.