Geologic Evolution of the Northernmost Coast Ranges and by K. R. Aalto, G. D. Harper, G. A. Carver, S. M. Cashman, W.

By K. R. Aalto, G. D. Harper, G. A. Carver, S. M. Cashman, W. C. Miller, H. M. Kelsey(auth.)

About The Product

Published by means of the yank Geophysical Union as a part of the Field journey Guidebooks Series.

This guidebook describes the geology of components we are going to stopover at within the western Klamath Mountains and Coast levels of northernmost California. Articles are prepared within the order of our shuttle, from Medford to Crescent urban on road 199, and south to Eureka on coastal street one hundred and one. Authors summarize the local geologic surroundings and result of their learn and prior reviews of the components we are going to stopover at in overview papers. therefore the geologic heritage worthy for interpretation of box stops is supplied with out the necessity of extra papers.


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Extra info for Geologic Evolution of the Northernmost Coast Ranges and Western Klamath Mountains, California: Galice, Oregon to Eureka, California July 20-28, 1989

Example text

Surrounding strata, in some cases, can remain unaffected and thus stratigraphic sections can thin at the expense of some layers while others survive intact. Mesoscopic faults disrupt bedding pervasively, so that it is difficult to trace a single bed over more than several Faults are commonly meters (Figure 18) oriented at 30-60° to bedding and consistently show normal offset. Many are calcite-filled. Motion on these faults results in the formation of lozenges that can become isolated by intrusion of mudstone, which appears to have flowed ductilely into fractures and around ends FIGURE 17 Structural data for the Figure of sandstone beds.

3 IV II ,/~ ' // k~~ - . . I.. > . '. _. ,A -. Im 2 3 4 5 6 LOG T H I C K N E S S BED THIC((NESS v FIGURE 4 S t r a t i g r a p h y o f t h e "Road S e c t i o n " a t P o i n t S t . George. Bouma IV d i v i s i o n s a r e shown w i t h l o w e r - c a s e base l e t t e r s . Roman n u m e r a l s f o l l o w t h e A a l t o (1976) model ( T a b l e 1 ) . F a c i e s D a n d E a r e l a b e l e d with upper-case l e t t e r s . Black d e p i c t s t h i c k s h a l e b e d s and s h a l e ripup clasts.

Fractures that formed during folding are oriented subparallel to axial surfaces of folds and truncate the fractures that define earlier-formed lozenges. Enderts Beach shear zone. At Enderts Beach a subhorizontal shear zone places northwest to southeast-dipping, thinlybedded, facies E turbidites above thickly-bedded, facies B and C sandstones (Figures 30 and 31). The shear zone is estimated to be 10 m thick at the maximum, but its upper contact is not exposed. The thinly bedded turbidites probably are overlevee interchannel or interlobe submarine fan deposits, once in depositional contact with channel or suprafan lobe sandstones (Aalto, 1986b) .

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