Krauklis wave in a stack of alternating fluid-elastic layers

Korneev, Valeri

doi:10.1190/geo2011-0086.1

Cited by 27 publications

(12 citation statements)

References 24 publications

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“…Krauklis (1962), Lloyd and Redwood (1965), and Paillet and White (1982) are among the first to study Krauklis waves. After Maksimov et al (2011) andKorneev (2011) already used this terminology, several active researchers in this area have recently suggested (Korneev et al, 2012) to consistently name this wave mode the Krauklis wave, after its first investigator.…”

Section: Introductionmentioning

confidence: 95%

“…They are highly dispersive with a very low-phase velocity at low frequencies (Ferrazzini and Aki, 1987;Ashour, 2000;Korneev, 2008). There has been some confusion about the terminology because they have been referred to as Krauklis waves in Korneev (2011) and Frehner (2013), Stoneley-guided waves in Korneev et al (2009), , and Korneev (2010), crack waves in Chouet (1986) and Yamamoto and Kawakatsu (2008), slow Stoneley waves in Ferrazzini and Aki (1987), or Stoneley waves in a fracture in Ashour (2000). Strictly speaking, a Stoneley wave is an interface wave propagating along an interface between two solid (elastic) half-spaces (Stoneley, 1924) and a Scholte wave is an interface wave propagating along an interface between a solid (elastic) and a fluid (viscous) half-space (Scholte, 1942a(Scholte, , 1942b.…”

Section: Introductionmentioning

confidence: 98%

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Krauklis wave initiation in fluid-filled fractures by seismic body waves

Frehner

2014

GEOPHYSICS

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Krauklis waves are a special wave mode that is bound to and propagates along fluid-filled fractures. They can repeatedly propagate back and forth along a fracture and eventually fall into resonance emitting a seismic signal with a dominant characteristic frequency. They are of great interest because this resonant behavior can lead to strongly frequency-dependent propagation effects for seismic body waves and may explain seismic tremor generation in volcanic areas or affect microseismic signals in fractured fluid reservoirs. It has been demonstrated that Krauklis waves can be initiated by a seismic source inside the fracture, for example by hydrofracturing. Here, the aim is to study Krauklis wave initiation by an incident plane P-or S-wave in numerical simulations. Both seismic body waves are reflected and scattered at the fracture, but also, two Krauklis waves are initiated with significant amplitude, one at each fracture tip (i.e., at the diffraction-points of the fracture). Generally, the incident S-wave initiates largeramplitude Krauklis waves compared to the incident P-wave case. For both incident wave modes, the initiation of Krauklis waves strongly depends on the fracture orientation. In the case of an incident P-wave, large-amplitude Krauklis waves are initiated at moderate (12°-40°) and high (>65°) inclination angles of the fracture with a distinct gap at approximately 50°. The dependency of Krauklis wave initiation on fracture orientation is almost inversed in the case of an incident S-wave and the largest-amplitude Krauklis waves are initiated at an S-wave incidence angle of approximately 50°. The initiation of large-amplitude Krauklis waves by both P-and S-waves has important implications for earthquake signals propagating through fluid-bearing fractured rocks (volcanic areas, fluidreservoirs) or for seismic exploration surveys in fractured reservoir situations.

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Section: Introductionmentioning

confidence: 95%

Section: Introductionmentioning

confidence: 98%

Krauklis wave initiation in fluid-filled fractures by seismic body waves

Frehner

2014

GEOPHYSICS

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“…11). Previous authors (Frehner & Schmalholz 2010;Korneev 2011;Maksimov et al 2011) highlighted the effects generated by seismic waves propagating along fluid-filled fractures. Incident body waves may generate secondary seismic waves called Krauklis waves that may fall into resonance emitting a dominant frequency (Frehner 2014) while propagating back and forth along fluid-filled fractures.…”

Section: Discussionmentioning

confidence: 99%

Subsurface fluid distribution and possible seismic precursory signal at the Salse di Nirano mud volcanic field, Italy

Lupi¹,

Ricci

Kenkel

et al. 2015

Geophys. J. Int.

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S U M M A R YMud volcanoes are geological systems often characterized by elevated fluid pressures at depth deviating from hydrostatic conditions. This near-critical state makes mud volcanoes particularly sensitive to external forcing induced by natural or man-made perturbations. We used the Nirano mud volcanic field as a natural laboratory to test pre-and post-seismic effects generated by distant earthquakes. We first characterized the subsurface structure of the Nirano mud volcanic field with a geoelectrical study. Next, we deployed a broad-band seismic station in the area to understand the typical seismic signal generated by the mud volcano. Seismic records show a background noise below 2 s, sometimes interrupted by pulses of drumbeatlike high-frequency signals lasting from several minutes to hours. To date this is the first observation of drumbeat signal observed in mud volcanoes.In 2013 June we recorded a M4.7 earthquake, that occurred approximately 60 km far from our seismic station. According to empirical estimations the Nirano mud volcanic field should not have been affected by the M4.7 earthquake. Yet, before the seismic event we recorded an increasing amplitude of the signal in the 10-20 Hz frequency band. The signal emerged approximately two hours before the earthquake and lasted for about three hours. Our statistical analysis suggests the presence of a possible precursory signal about 10 min before the earthquake.

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“…The oscillation inside the resonator is sustained by a "slow wave", whose name varies among authors (Korneev, 2011). In fluid-filled crack models, the frequency response to the crack excitation depends mainly on the crack extent, the parameters of the pressure transient triggering the oscillations (position, area, and source function), and the crack stiffness (Aki et al, 1977;Chouet, 1986).…”

Section: Causes Of Resonance Frequenciesmentioning

confidence: 99%

Potential use of resonance frequencies in microseismic interpretation

Tary

Baan

2012

The Leading Edge

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P a s s i v e s e i s m i c a n d m i c r o s e i s m i c -P a r t 1 1338 The Leading Edge November 2012 SPECIAL SECTION: P a s s i v e s e i s m i c a n d m i c r o s e i s m i c -P a r t 1Potential use of resonance frequencies in microseismic interpretation C ontinuous passive recordings of microseismic experiments can be used to detect and trace the modifications in frequency content during hydraulic fracturing or heavy-oil steam injection. We analyze the performance of four different time-frequency representations, namely the short-time Fourier transform, the S-transform, the continuous wavelet transform, and the autoregressive method, on a real microseismic data set of intermediate quality. We show that time-frequency transforms provide an efficient tool to highlight time-varying resonance frequencies occurring during reservoir fracturing.Four distinct resonance frequencies at ~17, ~35, ~51, and 60 Hz are observed during two experiments using the same experimental setup.The causes of resonance frequencies in hydrofracture experiments are then carefully reviewed to identify the potential causes of the observed values and illustrate how their analysis may help in reservoir management. In our case, resonance frequencies at the receiver side are anticipated to be outside the observed frequency band. In our borehole acquisition configuration, where the geophones and the stimulated reservoir Figure 1. Mean Fourier amplitude spectra for the 12 geophones (vertical component) of the three experiments (geophone 12 being the deepest one). These spectra are obtained by first computing the STFT (window = 1 s), and then averaging over the complete signal to obtain an averaged spectra for the complete experiment. The data are low-pass filtered at 500 Hz as no significant energy is in the frequency band 500-2000 Hz. Note that for the second and third experiments, resonance frequencies are clearly visible at ~17, ~31 (second experiment only), ~35, ~51, and ~60 Hz for most stations (black arrows). The Leading Edge 1339 P a s s i v e s e i s m i c a n d m i c r o s e i s m i c -P a r t 1Corresponding author: tary@ualberta.ca Downloaded 07/03/15 to 130.132.123.28. Redistribution subject to SEG license or copyright; see Terms of Use at http://library.seg.org/

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Krauklis wave in a stack of alternating fluid-elastic layers

Cited by 27 publications

References 24 publications

Krauklis wave initiation in fluid-filled fractures by seismic body waves

Krauklis wave initiation in fluid-filled fractures by seismic body waves

Subsurface fluid distribution and possible seismic precursory signal at the Salse di Nirano mud volcanic field, Italy

Potential use of resonance frequencies in microseismic interpretation

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