Initial seismic observations from a deep borehole drilled into the Canadian Shield in northeast Alberta
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The availability of a deep borehole in northeastern Alberta provides an unprecedented opportunity to study the in situ metamorphic craton rocks. This borehole reaches a depth of 2.4 km, with 1.8 km in the crystalline rocks, and is the only known borehole allowing access into the deeper rocks of the metamorphic Canadian Shield. In 2011, a zero-offset vertical seismic profile (VSP) was acquired to assist in the interpretation of seismic reflection data and geophysical logs. Three sets of upgoing tube waves interpreted from the raw profile correspond to the small-scale fluctuations in the borehole diameters and fracture zone in the crystalline rocks. A comparison between sonic log velocities and VSP velocities reveals a zone with increased velocity that could be due to the change in rock composition and texture in the basement rocks. The final processed profile is used to generate corridor stacks for differentiating between primary reflections and multiples in the seismic reflection profile. Analysis of the zero-offset VSP verifies existing log interpretation on the presence of fractures and the possible lithological changes in the metamorphic rocks of the Canadian Shield.
KeywordsZero-offset VSP Canadian Shield Craton rocks Metamorphic rocks Velocity seismic profiling Tube waves
Active-source seismic reflection profiling has played key roles in helping to shape our concepts of the structure and assembly of the earth’s continental cratonic crust since the discovery in the 1960s that reflections returning from it can be detected (e.g., Kanasewich and Cumming 1965). Without ‘ground truthing’ through drilling, however, the interpretations of such profiles remain speculative, and even though these reflections may lie only a few kilometers beneath the surface, interpretations become ‘certain’ according to Birch’s (1952) definitions, much like studies of the less accessible earth’s mantle. Ultimately returning events signal variations in density and seismic wave speeds over relatively small distances relative to the seismic wavelength are related to changes in lithology or mechanical properties (i.e., fracturing). The only way to truly know this is to directly sample the earth by drilling; it is important to take advantage of any opportunities that may arise to learn more about the sources of seismic reflectivity in such crystalline crust.
To our knowledge, there are no statistics on the number of boreholes drilled globally into the metamorphic crystalline cratons. With the vast mineral deposits they hold, it would not be surprising if this figure reached into the many hundreds of thousands or even more. Understandably, their locales are biased to economically important sites, but even so there is regrettably little public information available for more detailed scientific investigations. Despite this, there have been a small number of boreholes drilled for scientific research purposes such as the KTB pilot ‘Vorborhrung’ and the 9,101-m main ‘Hauptborhrung,’ Germany (Emmermann and Wohlenberg 1989; Emmermann and Lauterjung 1997), the 2,500-m Outokumpu Deep Drilling Project, Finland (Kukkonen 2011), and the 5,158-m Donghai borehole, China (Ji and Xu 2009; Luo and Pan 2010). At this writing, the Collisional Orogeny in the Scandinavian Caledonides (COSC) project in Sweden (Lorenz et al. 2011) has completed the first of its two 2,500-m-deep boreholes. Many of these drilling projects are associated with the International Continental Drilling Program (ICDP). There are also a limited number of borehole investigations in Western Canada that take advantage of mineral exploration programs (e.g., Drury 1985; Mwenifumbo et al. 2004).
Active seismic investigations, more commonly referred to as vertical seismic profiles (VSP) within such wells are rarer still, but have been important in helping us to decipher what the source of crustal reflections are. Detailed borehole seismic surveys have been carried out at Kola (Pavlenkova 1992; Carr et al. 1996; Ganchin et al. 1998), KTB (Li and Richwalski 1996; Lüschen et al. 1996; Harjes et al. 1997; Okaya 2004; Rabbel et al. 2004), and Outokumpu (Duo 2011; Heinonen et al. 2011; Kukkonen et al. 2012; Schijns et al. 2012). Surveys in similar crystalline lithologies but in more tectonically active zones include studies at Soultz-sous-Forêts, France (Place et al. 2011), and Cajon Pass, California (Rector 1988), for mineral exploration (e.g., Miao et al. 1994; Eaton et al. 1996), and for repository characterization (e.g., Cosma et al. 2001).
Outside of the crystalline rock masses, VSP studies have been used to assist with geothermal development. At the Larderello geothermal field in central Italy, Cameli et al. (1995) analyzed VSP data with other geological and geophysical information to help identify important seismic reflectors inside the metamorphic basement. These sub-horizontal reflectors were found to correlate with a producing fracture zone that intersected a borehole in the geothermal reservoir. At the Kakkonda geothermal reservoir in Japan, VSP imaging shows an up-dip pattern, which was associated with the slope of an anticline. This interpretation was used to constrain the positioning of seismic reflectors deduced from the poor quality seismic reflection survey and revealed geological structures that were not previously apparent in the seismic data (Nakagome et al. 1998). At the Rye Patch geothermal field in Nevada, Gritto et al. (2003) used multiple VSP surveys to obtain information on the velocity structure and the reflectivity of the subsurface. The goal was to explore the structural features that may control geothermal production in the area. Based on the changes in velocity and strong seismic reflectivity, it was suggested that localized geological heterogeneity is present in the area as a result of hydrothermal alteration and volcanic deposition. Despite the uncertainty in the identification and mapping of faults in this area, the VSP surveys indicated the existence of at least one fault which led to further investigation of the field using a 3D seismic reflection survey.
The physical properties of metamorphic rocks in Alberta beneath the Western Canada sedimentary basin (WCSB) are poorly understood since subsurface studies in the province have primarily been driven by the petroleum industry with a central focus on the sedimentary layers (Bartetzko et al. 2005). That said, over 4,000 exploratory boreholes have penetrated the metamorphic Precambrian basement in Western Canada, but coring and logging into the basement rocks are almost exclusively limited to the sedimentary successions (Pană 2003). The boreholes that do cross the Precambrian unconformity penetrate at most a few meters into the basement. While the cores and cutting materials obtained from these boreholes have provided key information in developing the age and radioactivity of the rocks, there is insufficient core or log information on the geophysically important properties of the basement (Burwash and Culbert 1976; Burwash and Cumming 1976; Burwash 1979; Drury 1988). This lack of access has limited scientific studies of the craton to the few short core samples and to remote mapping of Proterozoic tectonic terranes using magnetic surveys.
To date, study of the Canadian Shield has been investigated mainly on the surface through geological and geophysical field mapping (e.g., Langenberg and Nielsen 1982; Goff et al. 1986; Burwash et al. 1994, 2000; McDonough et al. 2000). The exposed Canadian Shield in the northeastern part of Alberta allows for direct mapping of the Proterozoic metamorphic rocks where the exposed geology can be traced unambiguously into the subsurface using magnetic mapping (Ross 2000). The complex metamorphic rock assemblages of the Canadian Shield rocks dip gently toward the southwest at 4–5 m per kilometer and are overlain by the Paleozoic passive margin and WCSB. The Shield beneath the borehole consists of massive to foliated granitoids, banded granite gneisses, and layered to banded metasediments (Langenberg and Nielsen 1982). In the Hunt well, a rock sample at 2,350 m is identified as foliated meta-granite composed mostly of quartz and feldspars (Walsh 2013; G. Njiekak, personal communication, January 23, 2014; Chan and Schmitt 2014). The uppermost 541 m of the geological column consists of Paleozoic and Cretaceous sediments which are well sealed behind three different steel casings (Fig. 2).
The Precambrian crystalline basement is commonly hypothesized to have been reactivated during the Phanerozoic eon (541 Ma to present), which may explain the long, linear, or anomalous trends of the sedimentary deposits. As a result of the Proterozoic orogenic activity from more than 1.8 Ga, faults and shear zones formed at the time have been interpreted in the shallow seismic profiles that offset the Phanerozoic section (Ross and Eaton 1999). Understanding the metamorphic basement rocks beneath the WCSB in Alberta is accomplished by interpreting the crustal seismic data and potential field maps (e.g., Ross et al. 1991; Pilkington et al. 2000; Lyatsky and Pană 2003). According to these magnetic-based interpretations, the borehole lies in the Taltson Magmatic Zone, a region believed to have been produced subduction-related plutonism (Ross 2002).
Seismic reflection profile
A number of deep seismic reflection profiles were obtained over the craton in Western Canada in the 1990s as part of the LITHOPROBE Alberta and TransHudson Orogen transects (Clowes 2010). These programs collected deep seismic profiles to the east, south, and west of the borehole (e.g., Hope et al. 1999; Bouzidi et al. 2002; Hajnal et al. 2005). The closest of these still lies more than 500 km away from the Hunt well and none of them cross the Taltson Magmatic Zone.
This profile reveals numerous gentle to steeply east-dipping reflectors in the Precambrian basement (Fig. 3b, c). Due to the crookedness of the seismic profile, energy from out of plane can degrade the overall stacked image, and reflections in the shot gathers may also not be properly imaged. Some of the observed reflections in the profile are also possibly out-of-plane reflections (side-swipes) that could indicate more complex 3D structure. As the profile is somewhat crooked, normal incidence data may not represent a vertical plane and may contain geological information from out-of-plane sections. Multiple reflections produced within the overlying sediments are also often a problem in deep seismic profiles over sedimentary basins (e.g., Bouzidi et al. 2002). To overcome some of these deficiencies, reprocessing of this profile focused on both the multiples and near-surface noise attenuation to improve the temporal resolution of the stacked seismic sections. This included implementation of frequency-wavenumber filtering, radial trace transform, predictive deconvolution, and time-variant filtering techniques. The section was migrated using finite difference migration. Further details of this reprocessing sequence are again found in Chan (2013).
The final stacked and migrated seismic surveys reveal eastward-dipping reflectors in the crystalline basement at 960, 1,450, and 2,750 m depth (Chan 2013). With the study borehole at a maximum depth of 2,363 m, the reflectors at 960 and 1,450 m might intersect the borehole at an offset of 165 m. Such dipping reflectors could be related to structural features, such as faults and/or fracture zones that could play significant roles in improved permeability toward the development of engineered geothermal systems in the Precambrian basement rocks. This motivates us to investigate the origin of these reflectors by acquiring a zero-offset VSP in the Hunt well.
Vertical seismic profiling
Surface seismic surveys offer substantial coverage of the subsurface when no existing boreholes are available in the study area. However, the complex structures of fractured reservoirs in the crystalline basement cannot always be properly resolved at the reservoir scale (e.g., Schutter 2003; Luthi 2005; Al-Ali et al. 2009; Place et al. 2011). Consequently, borehole geophysical surveys such as the vertical seismic profiling are utilized to minimize the ambiguity in the interpretation of seismic reflection surveys.
Many important reflectors detected by several VSPs recorded in the metamorphic basement could be attributed to the change in petrophysical characteristics of the rocks, particularly changes in fracture density, rather than contrasts in lithology (Cameli et al. 1995). Interval velocities extracted from the VSP data are useful in determining the variation of seismic velocity with depth with possible geological significance. Besides using the VSP data for reflectivity and velocity analysis, they can be interpreted separately for fracture analysis and toward an understanding of the degree of seismic anisotropy in the rock mass (e.g., Schijns et al. 2012). Such information is useful for the development of a geothermal reservoir and provides input parameters for the fracturing and reservoir simulation of a geothermal system.
Acquisition parameters of the zero-offset vertical seismic profile
Year of acquisition
6000-lb IVI Minivib™
10–160 Hz linear
Sercel’s SlimWave™ borehole geophone chaina
2 horizontal and 1 vertical 15 Hz geophones
Number of 3C geophones sondes
Top measured depth (relative to KB)
Bottom measured depth (relative to KB)
Number of measured levels
Sampling depth interval
Correlated record length
Processing sequence for the zero-offset vertical seismic profile
Geometry setup and trace editing
Prepare data for processing and eliminate bad traces
Correlate vibroseis trace with the sweep wave train
Stacking at constant recording depth
Increase signal-to-noise ratio with repeated recordings at common depth
Separate X, Y, Z component
First arrival picking
Calculate interval velocity and generate time-depth relationship
Compensate for energy losses
Minimize the effect of tube waves
Separate and enhance the downgoing and upgoing wavefields
Remove multiples from the upgoing wavefield
Apply vertical summation to yield a single stacking trace emphasizing upgoing events
To separate the upgoing and downgoing events from the seismic data, various numerical procedures can be applied to attenuate the downgoing modes without seriously affecting the upgoing events (Hardage 2000). The median filter technique was used for separation of the upgoing from the downgoing wave fields. It is considered as a data smoothing filter by selecting the median value of an ascending-ordered sequence of numbers from a moving window of input data (Stewart 1985; Hardage 2000). Two major advantages of using this type of filter are its ability to reject noise spikes and to pass step functions (i.e., discontinuities in the data) without smearing the edges. One important note in the wavefield subtraction process is that first-break times must be interpreted carefully to minimize any static time shift error in the wavefield separation (Stewart 1985; Hardage 2000).
A processing workflow was applied to the zero-offset VSP to assist in the interpretation of seismic reflection data and borehole logs as outlined in Table 2. Data analysis was performed carefully on the vertical component of the borehole seismic data to obtain a proper velocity profile for seismic processing and toward understanding the origin of tube waves. Because of the problems with sonde coupling in parts of the borehole, the interpretation of the reflectors in the lower section of the borehole is supported by the synthetic seismograms generated using the sonic logs.
First-break times were carefully and manually picked on the vertical component traces since automated time picking becomes more complicated with the presence of random noise. Amplitude noise results in smeared first arrivals that affect the accuracy of travel time determination. The zero-crossing point from trough to peak was used as the selection criterion for the first-break picking. In situ interval velocities were determined from the travel times and plotted in Fig. 7 for comparison with other sonic log measurements, including full-waveform sonic (FWS), dipole shear sonic imager™ (DSI), and sonic scanner™ logs.
Sonic logging provides measurements of interval velocities at higher frequencies (approximately 20 kHz) and penetration depth of a few centimeters in the borehole. Initial comparison of sonic log velocities to VSP velocities is difficult due to the frequency dispersion resulting from both rock property and scale-dependent effects (Sams et al. 1997; Schmitt et al. 2007). There is a significant amount of variation in VSP interval velocity as minor fluctuations of even the level of the digitization period of 1 ms in the first arrival pick could easily cause nonphysical variations in the velocities with the depth sampling interval of 2.5 m. This error is reduced using larger intervals in the velocity calculation at the cost of reduced resolution. This step is facilitated by smoothing the interval velocities using a simple difference in times and depths over 50 samples (122.5 m interval), followed by applying a linear slope fit of all times over the selected samples and its 95 % confidence limit.
Figure 7 reveals an increase in velocity with depth. At the open hole section of the borehole (below 1,006 m depth), the interval velocity from the VSP survey varies approximately from 5,500 to 6,500 m/s in the crystalline basement rocks. The observed values are consistent with the single laboratory measurement of P-wave speed of nearly 5,800 m/s at a confining pressure of 60 MPa on a meta-granite core sample acquired from 2,350 m near the bottom of the borehole (Chan and Schmitt 2014). Between 1,400 and 1,900 m depth, there are relative increases in both the interval velocities and density (RHOB). This zone is also identifiable in the high-frequency velocity profiles extracted from the borehole sonic logs. A possible explanation for this observation is the change in rock composition and texture in the basement rocks (Vernik et al. 1994). Unfortunately, with the limited cores available in this deep borehole, it is difficult to understand the exact causes of the localized increases in velocity and density in the basement. The increase near 1,760 m depth can be correlated with the potential mafic dyke that was previously interpreted in Chan (2013).
Corridor stack and synthetic seismogram
It is interesting to note some of the behaviors of the upgoing reflections in Fig. 8a. The strong events within the sedimentary column are easily seen and abruptly terminate as expected at its bottom near 541 m. The seismic events in the sedimentary section are all associated with known geological contacts (Fig. 8b) as determined by Chan (2013). One strong event originating at ~880 m depth is clearly seen as an upgoing reflection within the metamorphic column. This event is not horizontal suggesting that it is produced by a dipping reflector, and indicates the existence of reflectivity in the crystalline Canadian Shield. However, the lack of log information in this zone precludes a complete determination of the source of this event.
Here, the times of the corridor stack through the open hole section are of poorer fidelity than the upper cased section of the borehole. Using the corridor stacks to differentiate between primary reflections and multiples is questionable, but they are still useful in the interpretation of horizons in the overlying Phanerozoic sediments. The successions are in the upper 300 ms of the corridor stack data in which the borehole contains the steel casing and thus provides better geophone coupling. Borehole rugosity, as indicated by the caliper log, affects the clamping of the geophone to the formation which resulted in weaker recorded signals. Another problem was due to the insufficient length of the tool arms to lock the tool in place in the wide open hole section. As such, it poses a challenge to differentiate primaries and multiples from the VSP data set in the corridor stacks. To mitigate this, synthetic seismograms are generated from the sonic logs and employed to compare the reflectors with the VSP corridor stacks.
Density and sonic logs are first used to calculate a set of reflection coefficients (RC), which are then frequency-filtered to match the bandwidth of the seismic data. A seismic wavelet is the response of the seismic system and is defined by estimating the pulse from the real seismic data or using a standard pulse with a defined polarity, peak frequency, and phase. This seismic wavelet is used to convolve with the RC in time to generate the final synthetic seismogram. For this study borehole, the sonic log was extracted from the sonic scanner™ data set acquired in 2013 in the open hole section of the borehole (1,006–2,320 m). The reflection coefficient is convolved with wavelets extracted from the 2D seismic reflection survey discussed in Sect. 3 and generated with two different frequency ranges (10–160 and 10–60 Hz) close to those of the available seismic data sets (Chan 2013).
Comparisons between the corridor stacks from the VSP data and synthetic seismograms from the sonic logs are illustrated in Fig. 8c. The goal of this process is to identify the true reflectors and artifacts in the corridor stacks using the synthetic seismograms. This process focuses on the depth ranges between 1,006 and 1,800 m where there is reasonable overlapping of data between the VSP and sonic log. Four identifiable reflectors (#1–#4) in the VSP corridor stacks are labeled in Fig. 8c. Events #1 (1,408 m) and #4 (1,695 m) are identifiable in both data sets, which indicate changes in acoustic impedance at those depths.
As observed in the velocity profiles in Fig. 7, large velocity variations are subjected to the minor fluctuations in the first-break picks of the VSP data. Such fluctuations affect the seismic impedance contrasts leading to the anomalous reflectors in the corridor stacks. Two such reflectors are labeled as #2 and #3 in the corridor stacks (Fig. 8c). These reflectors are questionable as they do not align with any of the reflectors in the synthetic seismograms. One explanation is that these reflectors are artifacts in the stack as they are located close to depths that experience both borehole caving and change in borehole diameter between 1,654 and 1,740 m depth (Chan 2013), as seen in the caliper logs in Fig. 7. These affect the quality of the data sets, which also lead to the inaccurate travel times recorded at these receiver levels.
Tube waves are Stoneley waves that occur at the low frequencies of seismic data and are generated when the fluid in the well is displaced by a seismic source such as ground roll. From the perspective of seismic imaging, they are considered as one of the most damaging types of noise in a VSP because they are a strong coherent noise mode that repeats itself in every seismic shot (e.g., Hardage 1981, 2000; Greenwood et al. 2012) and as such cannot be removed by simple stacking of traces. In a cased borehole, a tube wave is an interface wave when the Rayleigh wave propagates down the borehole along the interface between the fluid in the borehole and the borehole wall. In the open hole sections, the tube waves are influenced by changes in the borehole diameter (e.g., variations in casing, borehole caving, fractures), casing conditions, cement bonding, or contrasts in acoustic impedance (Hardage 2000). In the context here, the tube waves are most useful as a tool to assist in the delineation of permeable fracture zones (e.g., Huang and Hunter 1984; Beydoun et al. 1985; Toksöz et al. 1992; Bakku et al. 2013).
Tube waves dominate both the downgoing and upgoing events at later times in the basement section of the zero-offset VSP. They can be created by compressional body waves when they encounter strong impedance contrasts within a borehole, such as casing point, change in borehole diameter, or permeable fractures. A total of three major sets of tube waves intersecting the borehole are interpreted from the processed section at 1,010 ± 5, 1,402 ± 20, and 1,635 ± 5 m. The larger error at 1,402 m depth is due to the relatively lower signal-to-noise ratio compared to other depths in the open hole section, which greatly mask the origin of the tube waves (Fig. 6). Multiple-scattered tube waves are observed at the same depth from the numerous downgoing events in the profile. These downgoing tube waves can be traced upward to determine their points of origin as labeled in Fig. 6. The amplitude for the first downgoing tube waves fade near the surface, but the linear slope of this wave is traced upward toward the first casing shoe depth at approximately 94 m. The exact origins of these downgoing waves are unknown. One likely explanation is the ground roll impinging on the well head and propagating downward into the subsurface (e.g., Li and Richwalski 1996). An alternative explanation is the presence of an air wave that provides a pressure pulse into the open borehole.
The relatively stronger sets (higher amplitude) of upgoing tube waves are at approximately 1,010 and 1,635 m depth. These are close to the depth levels in which there are impedance contrasts at 1,006 and 1,654 m, which suggests that small-scale fluctuations in the borehole diameter (22–60 mm) are sufficient to generate tube waves in borehole seismic data (Fig. 2). The casing shoe at 1,006 m corresponds to a change in borehole impedance and a change in diameter at the end of the casing shoe, which creates a tube wave as a propagating body wave.
One useful application of tube waves is fracture zone analysis (e.g., Li et al. 1994). The high-frequency tube waves have greater resolution than body waves, which make it possible to detect thin layers including fracture zones (Mjelde 1992). At 1,402 m depth, this set of tube waves does not correlate to any change in borehole diameter but is related to the presence of the fracture zones. This zone is close to the low-resistivity fracture zone that was previously identified in the geophysical well logs and the dipping seismic reflector that may intersect the borehole (Chan 2013). As tube wave energy can be attenuated by fluid interaction between the borehole and the formation rock due to the presence of permeable fractures, this provides a reasonable explanation to the lower amplitudes of this set of upgoing tube waves compared to the tube waves discussed in the previous paragraph.
The final set of upgoing tube waves is identified in Fig. 5 with its depth estimated by extrapolating the downgoing and upgoing tube waves down the section. Under the assumption that the average velocity is constant in the projected section of the borehole, this reflector originates from the bottom of the borehole as a result of a seismic signal below the bottom of the borehole being converted to tube waves.
A zero-offset vertical seismic profile was acquired in a deep borehole near Fort McMurray, Alberta, Canada, as part of the regional geothermal resource investigation. The main intention of this study is to utilize the availability of a deep borehole for the subsurface characterization of the Precambrian basement rocks. The dense recording (2.5 m) of seismic traces of the zero-offset VSP data allows for increased spatial resolution in the study borehole compared to the surface seismic reflection profiles. The processed VSP data and interpretations are discussed with a focus on the output velocity profile, corridor stacks, and tube wave analysis.
The velocity profile calculated from the first arrival picks generates a 1D model of the in situ interval seismic velocity. It is useful toward the velocity analysis of normal moveout correction for processing the seismic reflection data. Localized increases in velocity correlate with density peaks and are possibly related to the changes in rock composition and textures of the metamorphic basement rocks. P-wave velocity ranges between 5,500 and 6,500 m/s. However, a direct comparison of P-wave velocity between the VSP and sonic log data is difficult due to the frequency dispersion effect.
The poor coupling between geophones and the borehole wall contributes to the lower quality of the data in the open hole section. Despite multiple recordings of seismic shots at each depth for common depth stacking, the signal-to-noise ratio of the traces remains poor in the open hole section of the borehole seismic data. Initial interpretation of the corridor stacks was limited to the sedimentary successions behind the cased section of the borehole. This facilitates the horizon interpretation in the surface seismic reflection data and allows for the direct correlation of data in both time and depth. In the metamorphic basement section, the synthetic seismograms generated from the sonic logs help to identify the true reflectors in the corridor stacks generated from the VSP data. They serve to identify the primary reflectors in the borehole seismic data when the signal-to-noise ratio of the data is affected by the condition of the borehole. Interpretations focused on the depth section with overlapping data between 1,006 and 1,800 m. Reflectors are present at two depths in both data sets at 1,408 and 1,695 m, which can then be related back to the seismic reflection profiles to improve the subsurface interpretation of the basement rocks.
Analysis of the upgoing tube waves reveals the effect of borehole diameter changes and the fracture zone that was also interpreted in the available geophysical logs. Tube wave identification is also used to estimate the depth of reflectors originated from beneath the bottom of the borehole by method of extrapolation. One set of tube waves is found to intersect the fracture zone in the borehole corresponding to the results from the geophysical logging. Furthermore, the tube wave close to the bottom of the VSP section appears to be generated by a seismic signal from below the bottom of the borehole.
With the lack of cores available from this deep borehole, the geological reasoning of the seismic reflectors and changes in interval velocities are unverified. Geophysical logging, borehole, and surface seismic data have all been acquired in the deep borehole to allow for an integrated study of the Precambrian basement rocks. This is still an ongoing project, and the sonic scanner™ data acquired in late 2013 will be further analyzed to assist with the understanding of seismic anisotropy in the metamorphic Canadian Shield.
The authors would like to thank the operational support group of the International Continental Scientific Drilling Program (ICDP-OSG) for their assistance in downhole logging, members of the Experimental Geophysics Group (EGG) for their assistance in data acquisition, and Greg Nieuwenhuis for organizing the field logistics for data acquisition. We would also like to thank our reviewers for their insightful and detailed feedback for this paper. This research was sponsored by funding from the geothermal theme of the Helmholtz-Alberta Initiative (HAI).
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