Aftershocks and Fault-Zone Properties

Kisslinger, Carl

doi:10.1016/s0065-2687(08)60019-9

Cited by 111 publications

(80 citation statements)

References 37 publications

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“…There are (1) class 1A aftershocks, those that occur on the same surfaces that slipped during the mainshock; and class 1B aftershocks, those occur in the gouge layer but off the planes that slipped during the mainshock; (2) class 2 aftershocks, those that occur on the same faults, but beyond the rupture termini of the mainshock; (3) class 3 aftershocks, those that occur on the subsidiary faults in the volume of damage zone surrounding the mainshock fault planes; and (4) class 4 aftershocks, remotely triggered aftershocks on faults farther from the principal faults of the mainshock rupture. Kisslinger (1996) proposed three similar classes of aftershocks, but combined our categories 1A, 1B, and 3 into a single category. Even though it might be beyond the limit of earthquake-location technology, the distinction between class 1B and 1A aftershocks is mechanically important, because they occur on different surfaces.…”

Section: (A) Distributions Of Landers Aftershocks and (B) Their Horizmentioning

confidence: 99%

A Structural Interpretation of the Aftershock "Cloud" of the 1992 Mw 7.3 Landers Earthquake

Liu¹

2003

Bulletin of the Seismological Society of America

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We analyze the spatial relationship of relocated aftershocks to the principal rupture planes of the M w 7.3 1992 Landers mainshock from a structural point of view. We find that the aftershocks constitute primarily a several-kilometer-wide damage zone centered on the mainshock rupture planes. The intensity of damage decreases away from the principal faults. Less than half of the aftershocks occurred within 1 km of the mainshock planes, and perhaps only 5% of the aftershocks are candidates for rerupture of the mainshock faults. Moreover, it seems that aftershocks along the Landers rupture have b-values that correlate well with the complexity of the mainshock rupture. Low b-values occur along segments that are simple, whereas higher b-values correlate with sections that are more complex. Thus, structural complexity appears to correlate with a greater relative abundance of small earthquakes. These observations imply that aftershock populations reflect fault populations in the medium surrounding the principal faults rather than the behavior of the mainshock planes themselves.Online material: Arcview information about the surface rupture of the Landers mainshock.

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Section: (A) Distributions Of Landers Aftershocks and (B) Their Horizmentioning

confidence: 99%

A Structural Interpretation of the Aftershock "Cloud" of the 1992 Mw 7.3 Landers Earthquake

Liu¹

2003

Bulletin of the Seismological Society of America

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“…where n(t) represents the number of aftershocks per unit time, K is proportional to the total number of events in the sequence, c is the time interval at the beginning of the sequence during which aftershocks are poorly recorded, and p is often thought to be related to the physical setting of the earthquake sequence [Kisslinger, 1996]. We solve for the constants K, C, and p using a maximum likelihood method [Ogata, 1983] (1.006).…”

Section: Event Identificationmentioning

confidence: 99%

Aftershocks of the March 9, 1994, Tonga earthquake: The strongest known deep aftershock sequence

Wiens¹,

McGuire²

2000

J. Geophys. Res.

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Abstract. The March 9, 1994 (Mw 7.6, depth 564 kin), deep Tonga earthquake produced an exceptionally strong aftershock sequence for a deep earthquake. Using eight temporary broadband stations deployed on the Fiji, Tonga, and Niue islands, we identify 144 aftershocks with mb ranging from 3.2 to 6.0 during the first 41 days following the mainshock. The number and seismic moment of the March 9 aftershocks lie within the range of aftershock productivities of typical shallow earthquakes of similar moment. The aftershocks show a power law decay with time following the mainshock, with an exponent (p value) of-l.0, similar to shallow aftershock sequences. Fifty aftershocks can be accurately located using a hypocentroidal decomposition method; these aftershocks align along a near-vertical ENE striking plane similar to one of the mainshock nodal planes. Sixteen of the 18 well-located aftershocks during the first 2.5 hours are located to the NNE of the mainshock epicenter, consistent with NNE rupture propagation derived from waveform analysis. Later aftershocks are located south of the epicenter, suggesting aftershock expansion beyond the region of substantial moment release in the mainshock. Several of the aftershocks are located outside of the normal bounds of the seismically active slab, consistent with evidence that the mainshock rupture terminated outside the active slab. Five possible foreshocks occurred along the preferred fault plane within the 22 days prior to the mainshock. At least three "triggered" aftershocks occurred at distances of 50 to 110 km within the first six hours following the mainshock; triggered aftershocks in adjacent slab material may be common for large deep earthquakes. While there is some variation in the focal mechanisms of the aftershocks, most resemble the mainshock focal mechanism. All the mechanisms show compressional axes dipping to the west, consistent with background seismicity in this region. Overall, most of the aftershock characteristics of the 1994 Tonga event are similar to those found for shallow earthquakes, suggesting similarities between shallow and deep earthquakes in the mechanical processes that produce aftershocks.

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“…The other two parameters of Omori law c and k provided important insight into aftershocks behaviour. According to Kisslinger (1996) the k-value depends on the total number of events in the sequence and reflects the earliest part of the sequence and accounts for the observed fact that the earliest aftershocks do not follow a steady decay rate rather their rate increases in the first minutes to hours, then begins to decrease. On the other hand c-parameter depends on the activity in the earliest part of the sequence.…”

Section: Discussionmentioning

confidence: 99%

“…All our results are listed in a very informative table where one can read the values computed (Mc, a, b, p, c and k) through this study. Due to intense aftershock activity in short time-span after the mainshock occurrence the c-value of Omori's law (Utsu et al, 1995;Kisslinger, 1996;Woessner et al, 2004) is commonly considered as a time offset estimating for incomplete detection of aftershock activity. Based on the obtained results we can conclude that in average the activity, in Kamchatka, in the first times after the mainshock occurrence the activity is higher than the other examined regions.…”

Section: Discussionmentioning

confidence: 99%

Some Preliminary Results on the Distribution of Aftershock Sequences in Japan-Kuril Islands and Kamchatka

et al. 2017

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Aftershocks and Fault-Zone Properties

Cited by 111 publications

References 37 publications

A Structural Interpretation of the Aftershock "Cloud" of the 1992 Mw 7.3 Landers Earthquake

A Structural Interpretation of the Aftershock "Cloud" of the 1992 Mw 7.3 Landers Earthquake

Aftershocks of the March 9, 1994, Tonga earthquake: The strongest known deep aftershock sequence

Some Preliminary Results on the Distribution of Aftershock Sequences in Japan-Kuril Islands and Kamchatka

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