Publications
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Geologic effects of the March 1964 earthquake and associated seismic sea waves on Kodiak and nearby islands, Alaska
Kodiak Island and the nearby islands constitute a mountainous landmass with an aggregate area of 4,900 square miles that lies at the western border of the Gulf of Alaska and from 20 to 40 miles off the Alaskan mainland. Igneous and metamorphic rocks underlie most of the area except for a narrow belt of moderately to poorly indurated rocks bordering the Gulf of Alaska coast and local accumulations
Authors
George Plafker, Reuben Kachadoorian
Geomorphic effects of the earthquake of March 27, 1964 in the Martin-Bering Rivers area, Alaska
The Alaska earthquake of March 27, 1964, caused widespread geomorphic changes in the Martin-Bering Rivers area-900 square miles of uninhabited mountains, alluvial flatlands, and marshes north of the Gulf of Alaska, and east of the Copper River. This area is at lat 60°30’ N. and long 144°22’ W., 32 miles east of Cordova, and approximately 130 miles east-southeast of the epicenter of the earthquake.
Authors
Samuel J. Tuthill, Wilson M. Laird
The Alaska earthquake, March 27, 1964: regional effects
This is the third in a series of six reports that the U.S. Geological Survey published on the results of a comprehensive geologic study that began, as a reconnaissance survey, within 24 hours after the March 27, 1964, Magnitude 9.2 Great Alaska Earthquake and extended, as detailed investigations, through several field seasons. The 1964 Great Alaska earthquake was the largest earthquake in the U.S.
Authors
David S. McCulloch, Samuel J. Tuthill, Wilson M. Laird, J. E. Case, D.F. Barnes, George Plafker, S. L. Robbins, Reuben Kachadoorian, Oscar J. Ferrians, Helen L. Foster, Thor N. V. Karlstrom, M. J. Kirkby, Anne V. Kirkby, Kirk W. Stanley
Calculations of upper-mantle velocity from published Soviet earthquake data
The lack of information on mantle velocities and crustal structure of the U.S.S.R. has led to a preliminary examination of published Soviet earthquake bulletins in the hope of deriving useful velocity and structure information from the data they contain. Mantle velocities deduced from earthquake data on several Russian earthquakes are in excellent agreement with results of Soviet deep seismic soun
Authors
Robert G. Rodriquez
A final report on computed magneto-telluric curves for hypothetical models of crustal structure
Several mathematical models were investigated to determine the capa-bilities of the magneto-telluric method for determining the resistivity structure of the earth's crust. The model parameters were based on the crust model proposed by Keller (1963). The mathematical technique used was developed by Cagniard (1953). The investigations indicate that a three-layer model approximation of the crust and
Authors
J.I. Pritchard
Effects of the earthquake of March 27, 1964, at Whittier, Alaska
Whittier, Alaska, lying at the western end of Passage Canal, is an ocean terminal of The Alaska Railroad. The earthquake that shook south-central Alaska at 5:36 p.m. (Alaska Standard Time) on March 27, 1964, took the lives of 13 persons and caused more than $5 million worth of damage to Government and private property at Whittier.
Seismic motion lasted only 2½-3 minutes, but when it stopped the W
Authors
Reuben Kachadoorian
Effects of the earthquake of March 27, 1964, at Anchorage, Alaska
Anchorage, Alaska’s largest city, is about 80 miles west-northwest of the epicenter of the March 27 earthquake. Because of its size, Anchorage bore the brunt of property damage from the quake; it sustained greater losses than all the rest of Alaska combined. Damage was caused by direct seismic vibration, by ground cracks, and by landslides. Direct seismic vibration affected chiefly multistory buil
Authors
Wallace R. Hansen
Seismic-refraction measurements of crustal structure between Nevada Test Site and Ludlow, California
Seismic-refraction measurements from nuclear and chemical explosions were made along a line from the Nevada Test Site (NTS) to Ludlow, California, and additional recordings from nuclear explosions were made southward toward Calexico, California. The time of first arrivals from the Ludlow shotpoint is expressed as T0 = 0.00 + Δ/2.50 (assumed), T1 = 1.00 + Δ6.10, T2 = 2.81 + Δ/6.80, and T3 = 5.48 +
Authors
J. F. Gibbs, J.C. Roller
A preliminary summary of a seismic-refraction survey in the vicinity of the Tonto Forest Observatory, Arizona
The U.S. Geological Survey complete d a seismic-refraction survey in the vicinity of the Tonto Forest Seismological Observatory (T.F.S.O.) in April and May 1964. More than 1200 km of reversed profiles were surveyed to determine the crustal structure and crustal and upper mantle velocities in this area. The purpose of this work was to provide information on wave-propagation paths of seismic events
Authors
J.C. Roller, W. H. Jackson, D. H. Warren, J. H. Healy
Crustal structure between Lake Mead, Nevada, and Mono Lake, California
Interpretation of a reversed seismic-refraction profile between Lake Mead, Nevada, and Mono Lake, California, indicates velocities of 6.15 km/sec for the upper layer of the crust, 7.10 km/sec for an intermediate layer, and 7.80 km/sec for the uppermost mantle. Phases interpreted to be reflections from the top of the intermediate layer and the Mohorovicic discontinuity were used with the refraction
Authors
Lane R. Johnson
Seismic-refraction measurements of crustal structure between American Falls Reservoir, Idaho, and Flaming Gorge Reservoir, Utah
Interpretation of a reversed seismic-refraction profile recorded between American Falls reservoir and Flaming Gorge reservoir in May 1963 indicates that the depth to the Mohorovicic discontinuity is about 31 km at American Falls and 37 km at Flaming Gorge. The existence of an intermediate crustal layer at a depth of about 19 to 21 km beneath the profile is well supported by refractions and reflect
Authors
Ronald Willden
Variations in regional traveltimes
Precise epicentral location of a seismic event is made difficult by variations in regional traveltimes. A discussion is presented on delays to be expected in the various segments of a generalized travel path of seismic waves. Traveltime variations caused by changes in crustal structure and velocity introduce a major part of the uncertainty in traveltime at both the seismic source and receiver. Con
Authors
J. H. Healy