Skip to content

Advertisement

  • Research News
  • Open Access

TIARES Project—Tomographic investigation by seafloor array experiment for the Society hotspot

  • 1Email author,
  • 2,
  • 1,
  • 1,
  • 2,
  • 1,
  • 1,
  • 2,
  • 1,
  • 1,
  • 3,
  • 4 and
  • 5
Earth, Planets and Space201264:640040006

https://doi.org/10.5047/eps.2011.11.002

Received: 5 July 2011

Accepted: 12 November 2011

Published: 25 May 2012

Abstract

We conducted geophysical observations on the French Polynesian seafloor in the Pacific Ocean from 2009 to 2010 to determine the mantle structure beneath the Society hotspot, which is a region of underlying volcanic activity responsible for forming the Society Islands. The network for Tomographic Investigation by seafloor ARray Experiment for the Society hotspot (TIARES, named after the most common flower in Tahiti) is composed of multi-sensor stations that include broadband ocean-bottom seismometers, ocean-bottom electro-magnetometers, and differential pressure gauges. The network is designed to obtain seismic and electrical conductivity structures of the mantle beneath the Society hotspot. In addition to providing data to study the mantle structure, the TIARES network recorded unprecedented data of pressure and electromagnetic (EM) signals by tsunamis associated with large earthquakes in the Pacific Ocean, including the 2010 Chilean earthquake (Mw 8.8).

Key words

  • Hotspot
  • mantle plume
  • tsunami
  • ocean-bottom seismograph
  • ocean-bottom electro-magnetometer

1. Introduction

The French Polynesian region is characterized by positive topographic anomalies of 700 m, a concentration of hotspot chains, and a broadly-distributed low-velocity anomaly in the lower mantle revealed by seismic tomography (e.g., Garnero, 2000). These previous observations suggest the presence of a “superplume”, which is a large-scale mantle flow rising from the bottom of the mantle beneath the region (e.g., Larson, 1991). We performed broadband ocean-bottom seismometer (BBOBS) observations over the entire French Polynesian region, from 2003 to 2005, to determine a large-scale seismic structure of the mantle (Suetsugu et al., 2005). Our previous data revealed that large-scale low-velocity anomalies (on the order of 1000 km in diameter), indicative of the superplume, are located from the bottom of the mantle to a depth of 1000 km, and small-scale low-velocity anomalies (on the order of 100 km in diameter) are present above the superplume (Fig. 1, modified from Suetsugu et al., 2009). The small-scale anomalies, possibly mantle plumes, are present beneath the Society and Macdonald hotspots, which agrees with the results obtained from early magnetotelluric tomography (Nolasco et al., 1998). However, the explanation remained unclear because the insufficient station coverage impeded the investigation of the anomaly routes to the hotspots and their depth extents. If the hotspots are fed by the mantle plumes ascending from the lower mantle, a substantial mixing of materials may be occurring between the upper and lower mantle. The results may lead to a significant contribution in understanding the evolution of the Earth.
Figure 1
Fig. 1

Cross-sections of seismic structure in the entire mantle. S-wave velocities are shown for the upper mantle (0–410 km) and the MTZ (410–660 km). The model of Ritsema and van Heijst (2000) is shown for the MTZ structure. P-wave velocities are shown for the lower mantle (660–2900 km). Velocity scales are ±3% in the upper mantle and the MTZ and ±0.75% in the lower mantle. Green diamonds indicate hotspots in the Polynesian region. (a) Cross-section A–A′, passing the Society and Pitcairn hotspots; (b) cross-section B–B′, passing the Society and Macdonald hotspots. Narrow mantle plumes are indicated by arrows. (c) positions of the profiles. “SC,” “PT,” and “MD” in (c) indicate the Society, Pitcairn, and Macdonald hotspots, respectively. Modified from figure 11 of Suetsugu et al. (2009).

2. Seismic, Electromagnetic, and Pressure Observation on the Seafloor

We focused on the Society hotspot by deploying the TIARES network in its vicinity from 2009 to 2010. We installed nine pairs of BBOBSs and ocean-bottom electro-magnetometers (OBEMs) in February 2009 on the seafloor at a depth of 4000–5000 m aboard the research vessel MIRAI of the Japan Agency for Marine-Earth Science and Technology (JAMSTEC) (Fig. 2). The recovery cruises were conducted in November–December 2010 aboard the Tahitian fishing boat Fetu Mana. The project was conducted as a Japan-France cooperative effort. The Japanese BBOBS and OBEM have been developed by the Earthquake Research Institute of the University of Tokyo since 1990 (Fig. 3). The BBOBS was equipped with a broadband sensor that can record ground motions at periods from 0.02 to 360 s, and the OBEM was equipped with a fluxgate magnetometer and two mutually-orthogonal pairs of electrodes that measure variations in three components of the magnetic field and two horizontal components of the electric field (Fig. 3). The differential pressure gauge (DPG) sensors were attached with the BBOBS at two stations (SOC2 and SOC8 in Fig. 2). All instruments were operational for 1.5 years. Refer to Shiobara et al. (2009) for details of the BBOBS and the OBEM, and Araki and Sugioka (2009) for those of the DPG. The French team also installed two IUEM/INSU OBEMs (EM1 and EM2 in Fig. 2) that were used from 2009 to 2010 in the studied region. We designed the TIARES network configuration to determine a detailed structure beneath the Society hotspot down to the top of the lower mantle. This network observation is expected to reveal the mantle plumes which ascend from the lower mantle to the hotspot.
Figure 2
Fig. 2

TIARES stations (large triangles) on a bathymetric map. Open, red, and green triangles represent the stations equipped with BBOBS, OBEMs, and DPGs; BBOBS and OBEMs; and OBEMs, respectively. Other broadband seismic and electromagnetic stations are indicated by small yellow and green triangles, respectively. The red star indicates the Society hotspot.

Figure 3
Fig. 3

(a) BBOBS on board R/V “MIRAI” just before installation. (b) OBEM recovered by the fishing boat “Fetu Mana.”

3. Planned Data Analyses

Figure 4 shows the noise spectra of the SOC1 records computed from 1.5-year-long data. The noise level on the vertical-component is well below that at high-noise land stations (Peterson, 1993) at periods longer than 10 s. This indicates that the vertical component of the BBOBS records are suitable for analyzing Rayleigh waves, which are sensitive to the upper mantle structure, and teleseismic P waves, which are sensitive to the deeper mantle structure; both types of waves have large long-period vertical motions. The noise level of the two horizontal components is lower than that at high-noise land stations at periods between a few seconds and 30 s, indicating that teleseismic S waves in this period range are useful. The horizontal noise level at periods longer than 30 s is comparable to, or greater than, that at high-noise land stations.
Figure 4
Fig. 4

The noise model of the SOC1 BBOBS station. The blue curve indicates vertical noise spectra. Green and red curves are noise spectra of the two horizontal components. Thick curves behind show the low-and high-noise models at land stations (Peterson, 1993).

Hot mantle plumes should be detectable as low seismic of teleseismic body waves will be employed to determine the seismic velocity structure in the mantle transition zone (MTZ), a depth range from 400 to 700 km, and the lower mantle. The topography of the mantle discontinuities (the 410-km and 660-km discontinuities) could be used as a “mantle thermometer” because they are interpreted as mineral phase changes controlled by temperature and pressure. Previous studies (e.g., Niu et al., 2002; Suetsugu et al., 2009) showed that the MTZ is thin (hot) beneath the Society hotspot. However, the spatial resolution of the previous results is poor because of the sparse data in the region. We will study the thermal structure in the MTZ by mapping the topography of the mantle discontinuities with considerably better spatial resolution by receiver function analysis (e.g., Owens and Crosson, 1988). This should help in determining whether the presumed mantle plumes ascend through the MTZ. The OBEM data will be analyzed with a three-dimensional magnetotelluric method (Tada et al., 2011) to obtain the electrical conductivity structure down to the MTZ beneath the Society hotspot. Electrical conductivity is sensitive to temperature and composition (including the degree of mineral hydration) in a different manner from seismic velocities. Simultaneous use of BBOBSs and OBEMs could provide information on the elastic properties and electrical conductivities in the mantle, respectively, which would enable separate determination of the thermal and compositional characteristics of the mantle plumes (e.g., Fukao et al., 2004).

4. Seismic and Tsunami Records of the 2010 Chilean Earthquake

During the observation period, the Chilean earthquake (Mw8.8) occurred off the coast of Chile (35.846°S, 72.719° W) on February 27, 2010, which provided a unique opportunity to observe seismic waves and tsunamis triggered by the earthquake. Figures 5(a) and 5(b) show seismograms recorded for approximately one day at station SOC8, where BBOBSs, OBEMs, and DPGs were in operation. On the vertical and horizontal components, the surface waves circling the Earth several times were clearly observed. Approximately 10 h after the arrival of the first seismic wave, we observed a tsunami signal lasting for 5–6 h on the DPG sensor (Fig. 5(c)). Interestingly, we observed an electromagnetic (EM) signal simultaneously with the pressure signals, of which OBEM and DPG waveforms are similar (Figs. 5(d) and (f)), thus indicating that the EM signal was also caused by the Chilean tsunami. It is theoretically well understood that the movement of electrically-conductive ocean water in an ambient geomagnetic field induces secondary EM fields in the oceans (Sanford, 1971). However, until recent advances in high-precision measurement of the EM fields enabled the seafloor and island measurement of the tsunami signals (Manoj et al., 2011; Toh et al., 2011), this type of research was restricted by the low-signal tsunami EM levels. The EM measurement enables the evaluation of tsunami propagation direction and particle motion of the seawater, which could not be obtained from the pressure measurement. This is the first array observation of the EM field caused by a tsunami. We will be able to track the tsunami waves over eastern French Polynesia by analyzing the data from the TIARES network, which will enable the study of detailed tsunami propagation and its interaction with bathymetry.
Figure 5
Fig. 5

19 h records of (a) vertical component, (b) horizontal component, and (c) water pressure of the 2010 Chilean earthquake. R1, R2, … and G1, G2, … denote successive arrivals of Rayleigh and Love waves, respectively, which circled the Earth’s surface. Bottom three panels: (d) EW component, (e) NS component, and (f) vertical component of 3-h geomagnetic records of the tsunami generated by the earthquake (black). The corresponding water pressure record (red) is superimposed.

Declarations

Acknowledgments

The deployment of the seafloor instruments was performed as a part of the SORA 2009 research cruise by JAMSTEC. We are grateful to Captain Masaharu Akamine and the crew of R/V MIRAI for the installation cruise, Captain Vaimoana Opeta, ship-owner Arnaud Le Morvan, and the crew of the Tahitian fishing boat Fetu Mana for the recovery cruise. Their devoted effort led to the success of the TIARES observation. This work is supported by a Grant-in-Aid for Scientific Research (19253004) from the Japan Society for the Promotion of Science. We are also thankful to the French government for allowing the deployment of instruments in the French Polynesian seafloor and particularly to Pr. Pierre Mery, Délégation Régionale à la Recherche et à la Technologie in French Polynesia for his efficient and kind support. INSU CNRS funded the marine operation of UEB-IUEM with the participation of DT-INSU and J. F. D’Eu from CNRS. We thank two anonymous reviewers for improving the manuscript.

Authors’ Affiliations

(1)
Japan Agency for Marine-Earth Science and Technology, Institute for Research on Earth Evolution, Yokosuka, Kanagawa, Japan
(2)
The Earthquake Research Institute, the University of Tokyo, Tokyo, Japan
(3)
UEB, IUEM, CNRS, France
(4)
Laboratoire Geosciences du Pacifique Sud, Université de Polynésie Française, Tahiti, French Polynesia
(5)
Laboratoire de Geophysique, CEA, Tahiti, French Polynesia

References

  1. Araki, E. and H. Sugioka, Calibration of deep sea differential pressure gauge, JAMSTEC-R, 9, 141–148, 2009.View ArticleGoogle Scholar
  2. Fukao, Y., T. Koyama, M. Obayashi, and H. Utada, Trans-pacific temperature field in the mantle transition region derived from seismic and electromagnetic tomography, Earth Planet. Sci. Lett., 217, 425–434, 2004.View ArticleGoogle Scholar
  3. Garnero, E. J., Heterogeneity of the lowermost mantle, Ann. Rev. Earth Planet. Sci., 28, 509–537, 2000.View ArticleGoogle Scholar
  4. Larson, R. L., Latest pulse of Earth: Evidence for a mid-Cretaceous super-plume, Geology, 19, 547–550, 1991.View ArticleGoogle Scholar
  5. Manoj, C., S. Maus, and A. Chulliat, Observation of magnetic fields generated by tsunamis, Eos Trans. AGU, 92, 13–14, 2011.View ArticleGoogle Scholar
  6. Niu, F., S. C. Solomon, P. G. Silver, D. Suetsugu, and H. Inoue, Mantle transition-zone structure beneath the South Pacific Superswell and evidence for a mantle plume underlying the Society hotspot, Earth Planet. Sci. Lett., 198, 371–380, 2002.View ArticleGoogle Scholar
  7. Nolasco, R., P. Tarits, A. Chave, and J. H. Filloux, Magnetotelluric imaging of the Tahiti Hot Spot, J. Geophys. Res., 103(30), 287–309, 1998.Google Scholar
  8. Owens, T. J. and R. S. Crosson, Shallow structure effects on broadband teleseismic P waveforms, Bull. Seismol. Soc. Am., 78, 96–108, 1988.Google Scholar
  9. Peterson, J., Observations and modeling of background seismic noise, U.S. Geol. Surv. Open-File Rept. 93-322, U.S. Geological Survey, Albuquerque, New Mexico, 1993.Google Scholar
  10. Ritsema, J. and H. J. van Heijst, Seismic imaging of structural heterogeneity in Earth’s mantle: Evidence for large-scale mantle flow, Sci. Prog., 83, 243–259, 2000.Google Scholar
  11. Sanford, T. B., Motionally induced electric and magnetic fields in the sea, J. Geophys. Res., 76(15), 3476–3492, doi:10.1029/JC076i015p03476, 1971.View ArticleGoogle Scholar
  12. Shiobara, H., K. Baba, H. Utada, and Y. Fukao, Ocean bottom array probes stagnant slab beneath the Philippine Sea, Eos Trans. AGU, 90, 70–71, 2009.View ArticleGoogle Scholar
  13. Suetsugu, D., H. Shiobara, H. Sugioka, G. Barruol, F. Schindele, D. Reymond, A. Bonneville, E. Debayle, T. Isse, T. Kanazawa, and Y. Fukao, Probing South Pacific mantle plumes with ocean bottom seismographs, Eos Trans. AGU, 86, 429–435, 2005.View ArticleGoogle Scholar
  14. Suetsugu, D., T. Isse, S. Tanaka, M. Obayashi, H. Shiobara, H. Sugioka, T. Kanazawa, Y. Fukao, G. Barruol, and D. Reymond, South Pacific mantle plumes imaged by seismic observation on islands and seafloor, Geochem. Geophys. Geosyst., 10, Q11014, doi:10.1029/2009GC002533, 2009.View ArticleGoogle Scholar
  15. Tada, N., K. Baba, H. Utada, W. Siripunvaraporn, and M. Uyeshima, Importance of treating seafloor topography in inversion of 3-D marine MT data, Abstract, the 2011 EGU General Assembly, EGU2011–2874, 2011.Google Scholar
  16. Toh, H., K. Satake, Y. Hamano, Y. Fujii, and T. Goto, J. Geophys. Res., 116, B02104, doi:10.1029/2010JB007873, 2011.Google Scholar

Copyright

© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2012

Advertisement