Estimating the crust permeability from fluid-injection-induced seismic emission at the KTB site

Shapiro, Serge A.; Huenges, Ernst; Borm, G.

doi:10.1111/j.1365-246x.1997.tb01215.x

Cited by 521 publications

(588 citation statements)

References 11 publications

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“…7) reveal D values range between 1.2 and 3.5 m 2 /s. This data range is in accordance with the majority of other examples (Shapiro et al 1997;Hainzl 2004;Hainzl and Ogata 2005;Hainzl et al 2012;Shelly et al 2013a, b).…”

Section: Hydraulic Diffusivity Of Clusterssupporting

confidence: 80%

“…where D is the hydraulic diffusivity, P is pore pressure, and t is the time since the first contact of the pore pressure source with the host rock (Shapiro et al 1997;Yamashita 1997). In this case, however, because available observations from the initial stages of the earthquake swarm are limited, no explicit indications for diffusion were noted.…”

Section: Relocation Based On Temporary Network Datamentioning

confidence: 86%

“…As shown in previous works (Shapiro et al 1997;Hainzl 2004;Hainzl and Ogata 2005;Hainzl et al 2012;Shelly et al 2013a, b), although D is generally expected to range between 0.01 and 10 m 2 s -1 in the crust (Scholz 2002), this can also vary depending on crustal medium. One extreme example was presented by Noir et al (1997) who reported a D value of about 2 km 2 /min for a sequence in Central Afar, and a high diffusion rate also characterizes Yellowstone Lake (Farrell et al 2010).…”

Section: Hydraulic Diffusivity Of Clustersmentioning

confidence: 96%

“…We therefore tested the fluid implication hypothesis for the Rushan earthquake swarm by plotting the distance, d, between the first located event and all others within each cluster as a function of time, t. Unsurprisingly, data reveal a diffusion pattern within every d-t diagram (Fig. 7), and the data envelope also corresponds to the theoretical curve defined by ffiffiffiffiffiffiffiffiffiffi 4pDt p (Shapiro et al 1997). Thus, fitting results (Fig.…”

Section: Hydraulic Diffusivity Of Clustersmentioning

confidence: 99%

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Rushan earthquake swarm in eastern China and its indications of fluid-triggered rupture

Zheng

et al. 2017

Earthq Sci

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An extraordinary earthquake swarm occurred at Rushan on the Jiaodong Peninsula from October 1, 2013, onwards, and more than 12,000 aftershocks had been detected by December 31, 2015. All the activities of the whole swarm were recorded at the nearest station, RSH, which is located about 12 km from the epicenter. We examine the statistical characteristics of the Rushan swarm in this paper using RSH station data to assess the arrival time difference, t S À P , of Pg and Sg phases. A temporary network comprising 18 seismometers was set up on May 6, 2014, within the area of the epicenter; based on the data from this network and use of the double difference method, we determine precise hypocenter locations. As the distribution of relocated sources reveals migration of seismic activity, we applied the mean-shift cluster method to perform clustering analysis on relocated catalogs. The results of this study show that there were at least 16 clusters of seismic activities between May 6, 2014, and June 30, 2014, and that each was characterized by a hypocenter spreading process. We estimated the hydraulic diffusivity, D, of each cluster using envelope curve fitting; the results show that D values range between 1.2 and 3.5 m 2 /d and that approximate values for clusters on the edge of the source area are lower than those within the central area. We utilize an epidemic-type aftershock sequence (ETAS) model to separate external triggered events from self-excited aftershocks within the Rushan swarm. The estimated parameters for this model suggest that a = 1.156, equivalent to sequences induced by fluid-injection, and that the forcing rate (l) implies just 0.15 events per day. These estimates indicate that around 3% of the events within the swarm were externally triggered. The fact that variation in l is synchronous with swarm activity implies that pulses in fluid pressure likely drove this series of earthquakes.

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Section: Hydraulic Diffusivity Of Clusterssupporting

confidence: 80%

Section: Relocation Based On Temporary Network Datamentioning

confidence: 86%

Section: Hydraulic Diffusivity Of Clustersmentioning

confidence: 96%

Section: Hydraulic Diffusivity Of Clustersmentioning

confidence: 99%

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Rushan earthquake swarm in eastern China and its indications of fluid-triggered rupture

Zheng

et al. 2017

Earthq Sci

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“…However, in all cases, the value of the critical hydraulic parameter, hydraulic diffusivity, was assumed or inferred, for example, from the spreading of seismicity [e.g., Talwani and Acree, 1984;Shapiro et al, 1997] or the lag between the onset of seismicity and impoundment of reservoirs [Talwani and Acree, 1984]. This study is perhaps the first, direct in situ measurement of hydraulic diffusivity in a shear zone.…”

Section: Introductionmentioning

confidence: 99%

In situ measurements of hydraulic properties of a shear zone in northwestern South Carolina

Talwani¹,

Cobb²,

Schaeffer³

1999

J. Geophys. Res.

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Abstract. Subsequent to the initial impoundment of the Bad Creek Reservoir in northwest South Carolina in January 1991, lake level fluctuations (up to 33 m d Ϫ1 ) caused delayed (98 hours) correlative water level changes in an observation well (OW3) 250 m away. The bottom of the well is connected to the bottom of the reservoir by a shallowly dipping, 1 m wide shear zone. The amplitude of water level changes in OW3 was 0.19 of that in the reservoir. The amplitude ratio, R, of the water level changes in OW3 to those in the reservoir is a measure of the pore pressure transmitted through the shear zone. Assuming one-dimensional diffusion of pore pressure in the shear zone between the reservoir and OW3, these values of time lag and amplitude ratio of the water level fluctuations changes yield estimates of 0.05 m 2 s Ϫ1 for hydraulic diffusivity and 1.1 ϫ 10 Ϫ15 m 2 for permeability of the shear zone. In subsequent years the time lag decreased to 72 hours and R increased to 0.23, suggesting a nearly 60% increase in the two hydraulic parameters. We interpret the increase to be owing to flushing of fines in the shear zone due to the pumping action of lake level fluctuations or due to dissolution. After 1994, there were no further changes in these parameters suggesting steady state conditions. Our analysis demonstrated that the fluid pressure flow is restricted to the shear zone and the pore pressure transmitted through the shear zone showed a lognormal relationship with the frequency of lake level fluctuations, R ϭ 0.5 exp (Ϫ14.93/T), where T (days) is the period of lake level changes. Spectral analyses of the data were used to obtain a frequency independent hydraulic diffusivity (ϳ0.076 m 2 s Ϫ1 ) of the shear zone after it had reached steady state conditions. Using the undrained response of the reservoir, an in situ estimate value 0.66 was obtained for the Skempton's coefficient. The hydraulic diffusivity ϳ0.1 m 2 s Ϫ1 was found to be lower than that encountered at other locations of induced seismicity in the region.

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Background and delayed-triggered swarms in the central Southern Alps, South Island, New Zealand

Boese

Jacobs

Smith

et al. 2014

Geochem. Geophys. Geosyst.

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Low-magnitude earthquake swarms (M L 2.8), consisting of up to 47 events of similar waveforms, have been observed repeatedly in the central Southern Alps, a rapidly uplifting orogen bounded by the transpressive Alpine Fault in the South Island of New Zealand. We compare nine background swarms recorded between November 2008 and April 2010 with five delayed-triggered swarms that occurred after the M W 7.8 Dusky Sound and the M W 7.1 Darfield (Canterbury) earthquakes. The two types of swarms are similar in terms of the magnitudes, depths, focal mechanisms, and interevent times of the constituent microearthquakes, and appear to both involve the rupture of steeply dipping faults in highly fractured crust in a 10 km 3 12 km area in the center of the SAMBA network. The delayed-triggered swarms occurred at similar epicentral distances (c. 4.53 the rupture length of the mainshocks) to the Dusky Sound and Darfield earthquakes, commenced shortly after the passage of the surface waves, continued for 5 and 2 days, respectively, and were followed in each case by a 2 day long quiescent period, which may suggest clockadvanced of faults in their failure-cycle. Triggering thresholds of 0.01 MPa proposed elsewhere are similar to the dynamic stress changes computed for the Southern Alps (0.09 MPa). However, as 98% of the locatable triggered events occurred several hours after the surface waves had passed, the dynamic stress changes associated with the surface waves themselves are unlikely to have triggered the earthquakes directly. Instead, we suggest that the locations and delays of the triggered swarms are more consistent with triggering by pore pressure diffusion.

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Estimating the crust permeability from fluid-injection-induced seismic emission at the KTB site

Cited by 521 publications

References 11 publications

Rushan earthquake swarm in eastern China and its indications of fluid-triggered rupture

Rushan earthquake swarm in eastern China and its indications of fluid-triggered rupture

In situ measurements of hydraulic properties of a shear zone in northwestern South Carolina

Background and delayed-triggered swarms in the central Southern Alps, South Island, New Zealand

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