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Geophysical imaging of subsurface structures in volcanic area by seismic attenuation profiling
© The Author(s) 2017
- Received: 22 August 2016
- Accepted: 20 December 2016
- Published: 3 January 2017
Geophysical imaging by using attenuation property of multichannel seismic reflection data was tested to map spatial variation of physical properties of rocks in a volcanic area. The study area is located around Miyakejima volcanic island, where an intensive earthquake swarm was observed associated with 2000 Miyakejima eruption. Seismic reflection survey was conducted five months after the swarm initiation in order to clarify crustal structure around the hypocenters of the swarm activity. However, the resulting seismic reflection profiles were unable to provide significant information of deep structures around the hypocenters. The authors newly applied a seismic attribute method that focused seismic attenuation instead of reflectivity to the volcanic area, and designed this paper to assess the applicability of this method to subsurface structural studies in poorly reflective volcanic areas. Resulting seismic attenuation profiles successfully figured out attenuation structures around the Miyakejima volcanic island. Interestingly, a remarkable high-attenuation zone was detected between Miyakejima and Kozushima islands, being well correlated with the hypocenter distribution of the earthquake swarm in 2000. The high-attenuation zone is interpreted as a fractured area that was developed by magma activity responsible for the earthquake swarms that have been repeatedly occurring there. The present study can be one example showing the applicability of seismic attenuation profiling in a volcanic area.
- Seismic attenuation
- Poorly reflective
- Earthquake swarm
As a high-resolution geophysical imaging technique to figure out subsurface structures, seismic reflection survey has been widely used in the areas of oil and gas explorations and crustal studies. Seismic reflection profiles are the most general product, enabling us to visually recognize formation boundaries as continuous reflections. Moreover, the seismic reflection amplitude provides the physical properties of rocks such as acoustic impedance as well as type of pore fluid in subsurface.
However, it is difficult to deduce the subsurface structures from reflection profiles collected in less reflective areas: volcanic area and highly faulted area where continuous reflections are inherently difficult to be observed. Therefore, several techniques, but not many, have been tested: seismic attribute analysis (e.g., Tokuyama et al. 1988), seismic scattering analysis (Mikada et al. 1997). These methods focused on some attributes other than reflection amplitude and successfully detected subsurface information. From the same point of view, we applied a seismic attribute using attenuation property, “seismic attenuation profiling (SAP)” (Tsuru and No 2011; Tsuru et al. 2014), in a volcanic area between Miyakejima, Kozushima and Niijima island volcanos in Japan.
The objective of the present study is to image a highly fractured zone that was possibly caused by earthquake swarm activity associated with Miyakejima eruption in 2000. Although seismic attenuation is well investigated in studies using VSP data (e.g., Hauge 1981; Worthington and Hudson 2000), well log data (e.g., Matsushima 2006) and core samples (e.g., Tompkins and Christensen 2001; Tsuji and Iturrino 2008), it is rarely applied to surface seismic reflection data except previous studies on a direct hydrocarbon indication (Dasgupta and Clark 1998), a fault seal ability evaluation (Tsuru et al. 2014) and Q tomography/migration for oil and gas industry (e.g., Zhou et al. 2011).
The SAP method is a technique to image seismic attenuation structure from seismic reflection data (Tsuru and No 2011; Tsuru et al. 2014). The method has an advantage in application to geophysical imaging or rock property estimation of less reflective areas such as volcanic area and highly faulted area, because it does not require continuous reflections. On the other hand, the present SAP method using spectral ratio has a disadvantage in resolution because it requires an averaging process to mitigate the influences from abnormal values caused by local noises: About 100 samples and 15 traces are used in vertical direction and horizontal direction, respectively, in the present study.
In general, the spectral ratio method uses two each of amplitude spectrums that are calculated in two each of time windows consecutively set on seismic records. However, this method is very sensitive to noise (Tonn 1991). Previous authors therefore coped with this issue by some ways. For example, Dasgupta and Clark (1998) used only limited area of seismic reflection data around the area of interest in Q calculation. Tsuru et al. (2014) used a stacked seismic record and adopted amplitude spectrums of seafloor reflections as the denominator of the left side of Eq. (5). In the present study, amplitude spectrums of the uppermost part of the area of interest were used as the denominator (Appendix Fig. 12). On the other hand, the numerator spectrums were calculated in time windows set from top to bottom of seismic reflection profile.
Effective frequency band of input data
Dominant frequency range of reflections
Frequency dependency of attenuation
Seismic wave attenuates more largely in proportion to the increase of frequency. In other words, attenuation can be easily detected with higher frequency. Therefore, we finally selected 21–37.5 Hz, which is higher half of the 5–37.5 Hz, as the “p” computation band. Thus, we assumed that Q was constant within such a narrow frequency band.
Within the frequency band of 21–37.5 Hz, average Q values were computed along a stacked seismic trace at every CDP. Spectrum of the denominator of the left side of Eq. (5) was computed within a time window of the traveltime between 2.5 and 3.0 s at every CDP, which approximately corresponds to the uppermost part of the volcanic rocks in the study area. Spectrum of the numerator was computed within each time window, which was set on the seismic trace one by one from top to bottom. Then a seismic attenuation profile (SAP) was created.
On June 26, 2000, small volcanic earthquakes began to be recorded at observation stations west of the summit of the Miyakejima volcano, and subsequently an earthquake swarm initiated (Sakai et al. 2001). The swam migrated northwestward toward the direction of Kozushima and Niijima and then developed the most intense earthquake swarm ever observed in and around Japanese archipelago (Japan Meteorological Agency 2000; Uhira et al. 2005). The main eruption of the Miyakejima volcano occurred at the summit on July 8, 2000 (e.g., Sakai et al. 2001). A number of earthquakes occurred during a period of these two months (Nishizawa et al. 2002). The hypocenter depths of the 2000 swarm activity between Miyakejima and Kozushima were clearly shown by several studies: 2–13 km determined by Ocean Bottom Seismometers (OBS) for the time period between 08/07/2000 and 02/08/2000 (Sakai et al. 2001), 5–20 km by OBS for 11/07/2000 and 31/07/2000 (Nishizawa et al. 2002), 3–20 km by OBS for 21/01/2001 and 13/02/2001 (Nishizawa et al. 2002) and 5–22 km by land networks for 26/06/2001 and 15/07/2001 (Uhira et al. 2005).
Wide-angle seismic refraction surveys, which were conducted four months after the swarm initiation, discovered relatively low P-wave velocity zones in the upper crust between Kozushima and Miyakejima (Kodaira et al. 2002; Nishizawa et al. 2002) and an intra-crustal reflection phase immediately below the swarm (Kodaira et al. 2002).
Seismic line specifications and data acquisition parameters
NW → SE
NE → SW
SW → NE
S → N
November 21–27, 2000
Air-gun array, 8 × 1500 cu. in., 2000 psi, towing depth 10 m
Streamer cable, 156 channel, array hydrophones (32 phones/channel), towing depth 20 m
Source–receiver offset length
As input data of SAP calculation, post-stack migrated records were used in the present study. Post-stack data have an advantage from the viewpoint of S/N ratio because random noise and remaining multiples are strongly suppressed by stacking effect, and reversely it has a disadvantage in preservation of original frequency contents because NMO correction distorts frequency of reflection even if the NMO velocity is correct. On the other hand, pre-stack data have a disadvantage in S/N ratio, and reversely it has an advantage in frequency preservation. S/N ratio of the seismic reflection data from KR00-08 Cruise is not so high due to the seasonal wind as mentioned in “Study area and data specifications” section, and therefore, the post-stack data were selected as the input data for SAP computation in the present study. Also, frequency distortion caused by NMO correction is not so large in the depths below 10 km (Appendix 2).
Figure 3b shows SAP profile of interval Q, which came out of the average Q values of Fig. 3a. Abnormally large interval Q values can be recognized locally along the lower boundary of the down-warping high-attenuation zone detected on the average Q SAP profile. Drastic change in the average Q near the lower boundary of the high-attenuation zone caused the abnormally large interval Q values. This result indicates difficulty in the conversion from average Q to interval Q by SAP for the seismic reflection data used in the present study, and we therefore use average Q SAP profiles in the following discussions.
Figures 4, 5 and 6 show both the reflection profiles and average Q SAP profiles of KR102-KR104, and every SAP profile does not show such a remarkable variation in attenuation as that of KR101 has demonstrated. However, although it is a little vague, down-warping high-attenuation features seem to be imaged on both KR102 and KR103. Regarding KR104 and KR101, relatively high-attenuation areas can be seen in the southern half of the line and in the southeast end of the line, respectively, which are segments that pass near the volcanic edifice of the Miyakejima.
Here we discuss whether or not SAP method is applicable to tectonic study in volcanic area and whether or not the down-warping high-attenuation feature reflects any subsurface structures. In the present study, we assumed that spatial variation in reflectivity is so small over the poorly reflective area that the spatial variation in reflectivity does not affect that in attenuation. In a drastic way of expression, the reflectivity can be assumed almost uniform within the poorly reflective area, for wavelength used in the seismic reflection survey. It is therefore considered that the observed down-warping high-attenuation feature has no relationship with variation in reflectivity.
As shown in Figs. 3, 4, 5 and 6, every SAP profile shows a trend that the uppermost part has the highest attenuation. Although the top of each SAP profile was placed by zeros due to the unsuitable condition of spectral ratio computation in water layer, the areas of the highest attenuation can be correlated with the lower half of the stratified layers on the reflection profiles. The areas can be interpreted as volcaniclastic layers from the sedimentological point of view around the study area. Moreover, every SAP profile has a common attenuation feature that the shallower parts show relatively high attenuation while the deeper parts relatively low attenuation, which is consistent to a general attenuation structure in the crust. The above-mentioned characteristics commonly observed on every SAP profile can be considered to be one of the evidences that this method is applicable to tectonic study in poorly reflective area, in addition to previous studies in the oil industry (e.g., Tsuru et al. 2014; Zhou et al. 2011), if the down-warping high-attenuation feature were reasonably explained.
sedimentary rocks such as volcaniclastic rocks that deposited between two volcanos: Miyakejima and Kozushima,
relatively porous and/or fractured zones within volcanic basement.
As for the former, no reflections can be seen on the relevant part of the reflection profile (Fig. 2). Moreover, no volcaniclastic layers that reach 20 km in thickness have been observed on any seismic lines in the study area. Therefore, we eliminate the former from discussion and examine possibility of the latter below.
As shown in Fig. 10, every hypocenter distribution indicates a down-warping feature on the NW–SE section, which is similar in shape with that of high-attenuation zone on the SAP profile of KR101. Particularly, those features resulted from OBS networks deployed above the earthquake swarm (Sakai et al. 2001; Nishizawa et al. 2002) are important in evaluating the shape and depth of hypocenter distribution. On the other hand, the hypocenter distribution of Uhira et al. (2005) may be strictly inappropriate to evaluate the shape and depth of the swarm activity because it was determined by land network. However, its distribution is indispensable to investigate the early stage of the 2000 swarm activity that initiated from the Miyakejima side.
Thus, the down-warping high-attenuation zone on the SAP profile is appeared to reflect the 2000 swarm area, which would be dominated by fractures, from the similarity in shape. However, considering the difference in depth between the high-attenuation zone and the hypocenter distributions from OBS networks, it would be impossible that the high-attenuation zone is explained by only the 2000 swarm. Accordingly, we concluded that the down-warping high-attenuation zone observed on the SAP profile of KR101 reflects a fractured area that were developed by magma activity responsible for the earthquake swarms that have been repeatedly occurring between Miyakejima and Kozushima.
This conclusion can be supported by the low-velocity zones that were specified by the wide-angle seismic refraction surveys (Kodaira et al. 2002; Nishizawa et al. 2002), because seismic attenuation is correlated with seismic velocity (Tompkins and Christensen 2001; Tsuji and Iturrino 2008). However, why is not the dominant down-warping high-attenuation feature observed on the lines KR102-104? Although this issue is difficult to be revealed due to the limited data, we interpret that this may be caused by the difference in distance of ray paths that have influence on attenuation. As shown in Fig. 7, the deeper events (>7 km) of the swarm form a very thin (2 km thick) plane of a NW–SE strike and a vertical dip (Sakai et al. 2001), like a flower structure consisting of strike-slip faults. The seismic reflection waves collected on the lines KR102-104 should get across the plane, while those on the KR101 should propagate through the plane. Accordingly, the most predominant high-attenuation feature would be shown up on a seismic line running over and along the thin plane.
The present study suggested a possibility that the seismic attenuation profiling (SAP) can map physical properties of rocks in poorly reflective area such as volcanic area, where seismic reflection profile is difficult to provide structural information or physical properties because of very few reflections.
The down-warping high-attenuation zone was mapped by SAP between Miyakejima and Kozushima. This would reflect a fractured area that was developed by magma activity responsible for the earthquake swarms that have been repeatedly occurring there. The zone is also consistent with the low-velocity zone deduced from the previous wide-angle seismic refraction studies.
TT is responsible in the whole part of the manuscript. TN conducted a part of the data processing of the seismic reflection data and contributed to the interpretation and the discussions. GF contributed to the data acquisition of the seismic reflection data, a part of the SAP calculation procedure and the discussions. All authors read and approved the final manuscript.
Thanks are due to JAMSTEC for disclosure of the seismic reflection data of KR00-08 survey and Captains, Seismic Party, and the crew of the R/V KAIREI for their efforts to acquire data of good quality in difficult weather conditions. We are deeply grateful for Editor Dr. Yosuke Aoki and two anonymous referees whose comments and suggestions helped to improve and clarify the manuscript. The survey was conducted as JAMSTEC Frontier Research Program for Subduction Dynamics and a research program supported Special Coordination Funds of the Ministry of Education, Culture, Sports, Science and Technology of Japan.
The authors declare that they have no competing interests.
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