Drill Bit Noise Illuminates the San Andreas Fault

Vasconcelos, Ivan; Snieder, Roel; Sava, Paul; Taylor, Tom; Malin, Péter; Chavarria, Andres

doi:10.1029/2008eo380001

Cited by 10 publications

(7 citation statements)

References 5 publications

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“…Because of their subvertical attitude and signal loss to near-surface attenuation and noise, this structure would have been difficult to image with standard surface reflection profiling. Further signal processing of the Seismic While Drilling data was done by Vasconcelos et al (2008) (Fig. 4c).…”

Section: Illustrative Examplesmentioning

confidence: 99%

“…On land, the elimination of near-surface attenuation and suppression of surface noise has also allowed observation of Vasconcelos et al 2008) what appear to be Krauklis wave resonances in subsurface fractures (Sicking and Vermilye 2019;Liang et al 2017;Tary et al 2014a, b). Figure 5a shows a spectrogram obtained by the stacking of frequency-time-amplitude data from a 12-level 2.5 km deep borehole seismometer string at a geothermal development site in Finland.…”

Section: Illustrative Examplesmentioning

confidence: 99%

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Borehole Seismic Networks and Arrays

Bohnhoff

Malin

2020

Encyclopedia of Solid Earth Geophysics

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Borehole strings and chains; Buried grids; Downhole networks and arrays; Vertical arrays; VSP DefinitionIn the broadest sense, borehole networks and arrays are assemblies of geophysical instruments placed in the subsurface via boreholes. This article focuses on their seismological applications. While common usage often blurs the distinction between a network and an array, this article explicitly distinguishes between their operational theories and engineering practices, and in the case histories and examples provided. To strictly qualify as an array, the assembly of instruments must include matching or similar sensors located at different depths in one well or lateral separated in different wells. The combined natural-frequency responses and spacing of the sensors must also include a range over which they can be used to improve signal detection and analysis via time series processing. Outside of this range a borehole assembly acts as a network of independent detectors. Early DevelopmentsThe general use of boreholes for making subsurface seismic measurements appears to have begun nearly 100 years ago. McCollum and LaRue (1931) report that "during the past year

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Section: Illustrative Examplesmentioning

confidence: 99%

Section: Illustrative Examplesmentioning

confidence: 99%

Borehole Seismic Networks and Arrays

Bohnhoff

Malin

2020

Encyclopedia of Solid Earth Geophysics

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“…Ambient-field reflection seismology has been demonstrated from the surface ( Figure 4-2) (Draganov, et al, 2007(Draganov, et al, , 2009 [28,29], with an application to imaging a geothermal field summarized by Tibuleac The target receiver used for imaging is indicated (red star ), and the background color image (with thin dashed lines, question marks, and "b" and "c" labels) is from independent seismic imaging (colors indicate seismic-velocity variations) [31].…”

Section: Ambient-field Seismic Imagingmentioning

confidence: 99%

Enhanced Geothermal Systems

Jeanloz¹,

Stone²

2013

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“…I exemplify the interferometric imaging condition method with a synthetic example simulating the acquisition geometry of the passive seismic experiment performed at the San Andreas Fault Observatory at Depth (Chavarria et al 2003;Vasconcelos et al 2008). This numeric experiment simulates waves propagating from three microearthquake sources located in the fault zone (Fig.…”

Section: Examplementioning

confidence: 99%

Micro-earthquake monitoring with sparsely sampled data

Sava

2011

J Petrol Explor Prod Technol

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Micro-seismicity can be used to monitor the migration of fluids during reservoir production and hydrofracturing operations in brittle formations or for studies of naturally occurring earthquakes in fault zones. Microearthquake locations can be inferred using wave-equation imaging under the exploding reflector model, assuming densely sampled data and known velocity. Seismicity is usually monitored with sparse networks of seismic sensors, for example located in boreholes. The sparsity of the sensor network itself degrades the accuracy of the estimated locations, even when the velocity model is accurately known. This constraint limits the resolution at which fluid pathways can be inferred. Wavefields reconstructed in known velocity using data recorded with sparse arrays can be described as having a random character due to the incomplete interference of wave components. Similarly, wavefields reconstructed in unknown velocity using data recorded with dense arrays can be described as having a random character due to the inconsistent interference of wave components. In both cases, the random fluctuations obstruct focusing that occurs at source locations. This situation can be improved using interferometry in the imaging process. Reverse-time imaging with an interferometric imaging condition attenuates random fluctuations, thus producing crisper images which support the process of robust automatic micro-earthquake location. The similarity of random wavefield fluctuations due to model fluctuations and sparse acquisition is illustrated in this paper with a realistic synthetic example.

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Drill Bit Noise Illuminates the San Andreas Fault

Cited by 10 publications

References 5 publications

Borehole Seismic Networks and Arrays

Borehole Seismic Networks and Arrays

Enhanced Geothermal Systems

Micro-earthquake monitoring with sparsely sampled data

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