P-Coda Amplitude As a Measure of Earthquake Magnitude of Local Microearthquake.

Masuda, Koji

doi:10.4294/jpe1952.40.565

Cited by 2 publications

(3 citation statements)

References 12 publications

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“…Therefore, we applied distance correction of to the observed data without taking into account the radiation directions, and discussed the results as some effective values describing very broad distribution. To determine earthquake magnitudes, seismologists commonly use the following linear relation between the logarithm of the seismic amplitude A and the logarithm of the hypocentral distance r [e.g., Masuda , 1992]:

log (A) = b - a log (r), (10)

where a and b are constants:

b = log (A) + a log (r), a n d (11)

i f r = 1, t h e n b = log (A) . (12)

We assume that A (at r = 1, in mm) ≈ A 0 (at r = 0). In other words we use A (at r = 1) as a normalized amplitude defined as A 0 .…”

Section: Discussionmentioning

confidence: 99%

“…Therefore, we applied distance correction of equation (10) to the observed data without taking into account the radiation directions, and discussed the results as some effective values describing very broad distribution. To determine earthquake magnitudes, seismologists commonly use the following linear relation between the logarithm of the seismic amplitude A and the logarithm of the hypocentral distance r [e.g., Masuda, 1992]:…”

Section: Distance Effectmentioning

confidence: 99%

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WITHDRAWN: Source Duration of Stress‐ and Water‐Induced Seismicity as Derived from Experimental Analysis of P Wave Pulse Width in Granite

Masuda¹,

Satoh²

2012

Geophysical Research Letters

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We used analyses of pulse widths of P waves in granite measured during a laboratory experiment to investigate source durations of rupture processes for water‐induced and stress‐induced microseismicity. Water was injected into a dry granite sample under constant axial stress of about 70% of fracture strength and a confining pressure of 40 MPa. After elimination of the effects of event size and hypocentral distance from observed pulse widths we obtained scaled source durations of 0.50 μs and 0.26 μs for stress‐induced and water‐induced microseismicity, respectively. This difference suggests that the rupture velocity of water‐induced microseismicity is greater than that of stress‐induced microseismicity or that fault geometry is more equidimensional in the wet state than in the dry state. Our results suggest that pulse‐width analysis of P waveforms can be used to distinguish water‐induced events from those induced by regional stress and to characterize the faulting process.

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log (A) = b - a log (r), (10)

where a and b are constants:

b = log (A) + a log (r), a n d (11)

i f r = 1, t h e n b = log (A) . (12)

We assume that A (at r = 1, in mm) ≈ A 0 (at r = 0). In other words we use A (at r = 1) as a normalized amplitude defined as A 0 .…”

Section: Discussionmentioning

confidence: 99%

Section: Distance Effectmentioning

confidence: 99%

WITHDRAWN: Source Duration of Stress‐ and Water‐Induced Seismicity as Derived from Experimental Analysis of P Wave Pulse Width in Granite

Masuda¹,

Satoh²

2012

Geophysical Research Letters

Self Cite

View full text Add to dashboard Cite

show abstract

“…Therefore, in applying a distance correction to the observed data, we chose to ignore the direction of radiation and discussed the results as some effective values. The distance correction is in the following linear relation between the logarithms of the seismic amplitude A and the hypocentral distance r , commonly used to determine earthquake magnitudes [e.g., Masuda , ]:

log (A) = b - a log (r),

where a and b are constants and

b = log (A) + a log (r)

…”

Section: Discussionmentioning

confidence: 99%

Source duration of stress and water‐pressure induced seismicity derived from experimental analysis of P wave pulse width in granite

Masuda

2013

Geophysical Research Letters

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[1] Pulse widths of P waves in granite, measured in the laboratory, were analyzed to investigate source durations of rupture processes for water-pressure induced and stress-induced microseismicity. Water was injected into a dry granite sample under constant axial stress of about 70% of fracture strength and a confining pressure of 40 MPa. After the effects of event size and hypocentral distance were removed from observed pulse widths, the ratio of the scaled source durations of waterpressure induced and stress-induced microseismicity was 0.52. The difference in the scaled source durations between waterpressure induced and stress-induced microseismicity suggests that water-pressure induced microseismicity involves a greater rupture velocity or a more equidimensional fault geometry than stress-induced microseismicity. These results suggest that pulse width analysis of P waveforms can be used to distinguish waterpressure induced events from those induced by regional stress and to characterize the faulting process. Citation: Masuda, K.(2013), Source duration of stress and water-pressure induced seismicity derived from experimental analysis of P wave pulse width in granite,

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P-Coda Amplitude As a Measure of Earthquake Magnitude of Local Microearthquake.

Cited by 2 publications

References 12 publications

WITHDRAWN: Source Duration of Stress‐ and Water‐Induced Seismicity as Derived from Experimental Analysis of P Wave Pulse Width in Granite

WITHDRAWN: Source Duration of Stress‐ and Water‐Induced Seismicity as Derived from Experimental Analysis of P Wave Pulse Width in Granite

Source duration of stress and water‐pressure induced seismicity derived from experimental analysis of P wave pulse width in granite

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