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NARROW
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all geography including DSDP/ODP Sites and Legs
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Magnitude-Related Earthquake Ground Motions
Lg magnitudes and yield estimates for underground Novaya Zemlya nuclear explosions
Eleventh award of the medal of the Seismological Society of America
Lg magnitudes of Degelen, East Kazakhstan, underground explosions
Some Aspects of the Seismic Scaling and the Strong Ground Motion of the Eastern Missouri Earthquake of January 12, 1984
Lg magnitudes of selected East Kazakhstan underground explosions
Estimates of short-period Q values and seismic moments from coda waves for earthquakes of the Beijing and Yun-nan regions of China
Estimates of magnitudes and short-period wave attenuation of Chinese earthquakes from Modified Mercalli intensity data
Comments and Reply on ‘Seismicity of the Colorado Lineament’: REPLY
Spatial attenuation of the Lg wave in the Central United States
Average seismic source-parameter relations for mid-plate earthquakes
Seismicity of the Colorado Lineament
Magnitude: The relation of M L to m bLg
Comments on L. Winkler's “Catalog of U.S. earthquakes before 1850”
On the attenuation of Lg waves in western and central Asia and their use as a discriminant between earthquakes and explosions
The excitation and attenuation of seismic crustal phases in Iran
The body-wave magnitude of the great 1857 California earthquake
On the relation between modified Mercalli intensity and body-wave magnitude
Abstract The combination of moderate seismic activity, sparsity of seismograph stations and relatively low density of population makes it difficult to assign quantitative seismicity values to most of the central United States. In the New Madrid seismic zone, where the level of seismic activity is higher and the number of seismograph stations is more adequate, one can delineate the active fault zone and determine a magnitude-recurrence relation. These capabilities will be extended to other seismic zones as arrays of seismographs are installed for recording microearthquakes, which will give information on fault delineation, focal mechanism, and magnitude frequency. Only after such information is available will we be able to make positive statements relating seismic activity to specific geologic features. The seismicity data suggest that earthquakes that occur outside the recognized seismic zones or major structural features will have a maximum body-wave magnitude m b of 5.5 and that this maximum value will occur only infrequently. Experience shows that if these relatively minor earthquakes are only a few kilometres deep they may have an epicentral intensity at least as large as VII (observed for an earthquake of m b = 3.8), but their magnitude and area of perceptibility will be small. With the exception of the New Madrid seismic zone and possibly the Wabash Valley seismic zone, a conservatively reasonable value for the maximum body-wave magnitude to be expected in the major seismic and structural zones of the central United States is 6.5. For the New Madrid seismic zone an earthquake of body-wave magnitude equivalent to that of a great earthquake (m b = 7.5) can be expected, on the basis of what has already been experienced in 1811-1812. Because of low anelastic attenuation, the earthquakes in the central United States are felt and cause damage over much wider areas than earthquakes of comparable magnitude in the western United States. Further consequences are that the ground shaking has a longer duration and that the ground-motion spectrum shifts at the larger distances to lower frequencies, which results in relatively low ground acceleration for relatively large ground displacements and a greater effect on high-rise than low-rise structures.