Philippine Sea Plate motion since the Eocene estimated from paleomagnetism of seafloor drill cores and gravity cores
© 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 2010
Received: 28 April 2009
Accepted: 22 April 2010
Published: 6 August 2010
Current models of Philippine Sea (PHS) Plate motion assume a general and large northward shift since the Eocene. In order to constrain better the age and amount of this northward shift, we have conducted a paleomagnetic study on drill and gravity cores, respectively, taken from the seafloor of the northern part of the PHS Plate. The core samples consist of sedimentary rocks or semi-consolidated sediments, and their ages, as estimated from microfossils and strontium isotope ratios, range from the Eocene to late Miocene. The results of stepwise alternating-field and thermal demagnetization experiments revealed that 19 sections at 17 sites out of 58 sections at the 29 sites examined yielded mean paleomagnetic directions with a 95% confidence limit (α95)of <25°, and 14 sections at 13 sites have α95 < 15°. An estimation of the amount of the northward shift at each site was obtained from the difference between the paleolatitude and the present latitude. This estimation revealed that the northern part of the PHS Plate was located near the equator at 50 Ma and that the majority of the northward shift took place between about 50 and 25 Ma. Very little northward movement occurred after 15 Ma. Based on our data, together with the available paleomagnetic information suggesting clockwise rotation of about 90° since the Eocene and the requirements from geometry with the surrounding plates, we present a model in which the PHS Plate rotated 90° clockwise between 50 and 15 Ma on the Euler pole near 23°N, 162°E, although it is impossible to specifically determine the Euler pole position.
The history of PHS Plate motion is not yet well understood. At the present time, the PHS Plate is a small plate, and there is no hotspot track that documents plate motion. Furthermore, most of the plate is submerged, rendering it difficult to construct a virtual geomagnetic pole (VGP) path using fully oriented paleomagnetic samples. Paleomagnetic data are available for islands along the eastern margin of the plate, such as the Ogasawara (Bonin) islands, Guam, Saipan, and Palau (Kodama et al., 1983; Haston et al., 1988; Haston and Fuller, 1991), for eastern Indonesia, which occupies the southernmost part of the PHS Plate (Hall et al., 1995a, b), and for drill cores of the Ocean Drilling Program (ODP) Leg 126 from the northern part of the IBM Arc (Koyama et al., 1992). However, a VGP path could not be constructed because of the possibility for local movement in the tectonically active regions and limited age distribution. Therefore, with the exception of the eastern and southern margins, paleomagnetic data on the PHS Plate are limited to data obtained from the cores of the Deep-Sea Drilling Project (DSDP) in the 1970s taken from the West Philippine Basin, Shikoku and Parece Vela Basins, and Daito Ridge (Louden, 1977; Kinoshita, 1980). However, the quality of these data may not be high enough by modern standards because (1) these cores were drilled by a rotary core barrel and, as such, they may have been physically disturbed and (2) complete demagnetization experiments were not conducted. Nevertheless, the paleomagnetic data on the PHS Plate that are available show a general and large northward shift of the plate since the Eocene. These data have been incorporated into models of PHS Plate motion which also generally assume a large northward movement since the Eocene (e.g., Seno and Maruyama, 1984; Hall et al., 1995a, b, c; Hall, 2002), but the distance of the movement and variation in speed over time have not yet been well documented. ODP recently occupied again the West Philippine Basin at a single site (Site 1201), but the paleomagnetic data failed to continuously track PHS Plate motion because of the occurrence of large hiatuses (Shipboard Scientific Party, 2002).
We have conducted a paleomagnetic study of drill cores and gravity cores newly taken from the northern part of the PHS Plate in order to better constrain the age and amount of the northward shift. We present a model of PHS Plate motion using these newly acquired data.
2. Samples and Measurements
Drill cores of consolidated sediment taken with a deep-sea Boring Machine System (BMS) (Matsumoto and Sarata, 1996; Matsuda et al., 2004) of R/V Hakurei-maru No. 2 were used in this study. The BMS can drill through rocks down to a maximum depth of 20 m below the seafloor by remote operation from the vessel through an armored cable and take cores 47 mm in diameter. Drilling was conducted at topographic highs with no or little unconsolidated sediment cover. The drilling sites were chosen based on the strength of acoustic reflection from the seafloor and were distributed on the Kyushu-Palau Ridge, Amami Plateau, Daito Ridge, Oki-Daito Ridge, Okinawa Rise (Urdaneta Plateau), and the northeasternmost part of the Parece Vela Basin (Fig. 1). Short semi-consolidated sediment cores taken with a gravity corer were also included in this study.
From drill cores of the BMS, we selected a core piece longer than ∼10 cm (called a ‘section’ in this paper) for the paleomagnetic measurements. Each section was not oriented azimuthally, but the relative declination within it can be discussed. Two cubic specimens of about 2 cm each side were cut from each horizon with a diamond saw, and a total of eight or more specimens were obtained from each section. Samples from the gravity cores were in the form of cubes, about 7 cm3 each, and were taken by inserting plastic cubes into half-split core surfaces or by gouging with a special apparatus made of stainless steal. Paleomagnetic measurements were carried out for 55 sections at 26 sites of BMS cores and three sites of 1- to 2-m-long gravity cores.
Summary of core sections from which paleolatitudes were obtained.
Depth in core (mbsf)
NN7-15 (3.6–11.8) (N)
NP24 (27.2–30.0) (N)
NP24 (27.2–30.0) (N)
NP25 (23.3–27.2) (N)
NP25 (23.3–27.2) (N)
NP24–25 (23.3–30.0) (N)
NN11–20 (0.3–8.2) (N)
NN5–6 (11.8–14.9) (N)
NP23 (30.0–32.4) (N)
NP23–24 (27.2–32.4) (N)
NP23 (30.0–32.4) (N)
NP23–24 (27.2–32.4) (N)
E.-M. Eocene (42.6–52.6) (F)
Daito 401 Seamount
NP16 (39.7–42.5) (N)
Daito 3316 Seamont
P12–14 (37.9–42.6) (F)
Oki-Daito 432 Seamount
P12–14 (37.9–42.6) (F)
Iwoto Trough SE
NN9 (9.8–10.6) (N)
NN9 (9.8–10.6) (N)
Age control of the core sections is based on calcareous nannofossil biostratigraphy, planktonic foraminiferal biostratigraphy, or strontium isotope (87Sr/86Sr) stratigraphy (Table 1). The sections of the paleomagnetic measurements are at the same depths as, or nearby to the horizons of microfossil analyses or isotope measurements, or they are between two horizons of age determination. The ages of the studied samples range from the Eocene to late Miocene. The timescale of Gladstein et al. (2004) was used in this study. It is difficult to determine sedimentation rates, and thus it was not possible to judge that secular variations in the geomagnetic field could be averaged out for the depth intervals of 10–20 cm of each section. However, sedimentation slow enough for averaging out secular variations is expected in general from the pelagic environment of the study area and the distribution of the drilling sites on topographic highs.
The analyses revealed that since the Eocene, the studied area has moved in a northward direction by as much as ∼25° in latitude. The present northern part of the PHS Plate was located near the equator at ∼50 Ma. The majority of the movement took place between the Eocene and Oligocene (at approx. 50–25 Ma), and the movement since the middle Miocene, ∼15 Ma, is small. The average northward velocity component obtained from the linear least square fitting to the data before ∼20 Ma is approximately 8.0 cm/year, when only the sites of higher reliability with α95 < 15° are included in the calculation. The section 8.75–8.90 mbsf at the KP357 Seamount was excluded for the reason that secular variation could not be averaged based on its lithology, namely, tuff.
Our observation that the majority of the northward movement of the PHS Plate occurred before ∼25 Ma is consistent with the geology of the Japanese Islands. The collision of the IBM Arc against the Southwest Japan Arc is considered to have started at about 15 Ma, and the location of the collision has not moved significantly since then (e.g., Amano, 1991; Takahashi and Saito, 1999). This result indicates that the direction of the PHS Plate motion since 15 Ma should be almost northward, perpendicular to the strike of the Nankai Trough in the collision zone. Because the formation of the volcanic front of the Southwest Japan Arc in the Quaternary indicates the arrival of the edge of the PHS Plate slab under the front at the depth of about 110 km (Kimura et al., 2005), the length of the subducted slab is estimated to be about 380 km, which amounts to a movement of ∼3.5° in terms of latitude. Such a small amount is close to the uncertainty of paleomagnetism and consistent with the result showing little northward shift since ∼15 Ma. At the present time, the PHS Plate motion relative to Eurasia is northwestward, with a velocity of approximately 3 cm/year at the easternmost part of the Nankai Trough (Seno et al., 1993; Kato et al., 1998), but the direction changed to the current direction at about 3 Ma or later (Nakamura et al., 1984; Jolivet et al., 1989; Yamazaki and Okamura, 1989). Thus, the direction for the last 15 Ma can be regarded as north on average. It is assumed that the PHS Plate did not show any large northward movement during the spreading of the Shikoku Basin, which occurred from ∼27 to 15 Ma (Okino et al., 1994). This assumption is based on the lack of geological evidence for a collision of the IBM Arc at any place along the Nankai Trough when the IBM Arc migrated from the location of the Kyushu-Palau Ridge to its present position associated with the opening of the Shikoku Basin.
Easterly deflected paleomagnetic directions of up to ∼90° in the Eocene have been reported from the eastern and southern margin of the PHS Plate (Kodama et al., 1983; Haston et al., 1988; Haston and Fuller, 1991; Koyama et al., 1992; Hall et al., 1995a, b). According to the compilation by Haston and Fuller (1991), the paleomagnetic declinations obtained from the eastern margin of the PHS Plate can be summarized as D = 105.3° ± 12.6° and 91.7° ± 16.9° in the Eocene from the Bonin Islands of Chichijima and Anijima, respectively; D = 43.0° ± 12.5° in the lower Eocene from Saipan; D = 68.4° ± 12.8° in the middle Oligocene from Palau; D = 66.1° ± 11.1° in the middle Oligocene from Guam; D = 54.5° ± 17.4° in the lower Miocene from Palau; D = 30.7° ± 8.4° in the middle Miocene from Saipan. Declinations of 85.7° ± 15.9° at 47±3 Ma, 39.1°±19.5° at 40±2 Ma, and ∼40° from 27 to 33 Ma have been reported in eastern Indonesia (Hall et al., 1995a). Kodama et al. (1983) suggested that the easterly deflected declinations from the Bonin Islands are due to local tectonic rotations associated with left-lateral strike-slip faults. However, it would be better to consider that the entire PHS Plate rotated clockwise because all islands show concordant rotations (Haston and Fuller, 1991). In addition, the skewness of magnetic anomalies in the West Philippine Basin also suggests a similar clockwise rotation (Louden, 1977; Shih, 1980). The compilation of the then available paleolatitude data from the PHS Plate by Koyama et al. (1992, figure 11) revealed a tendency for the range of paleolatitude distribution to decrease with increasing age and a decrease in the mean paleolatitude, suggesting that the site distribution was originally close to E-W in low latitudes and then changed to N-S. This scenario is consistent with the clockwise rotation of about 90°.
Hall et al. (1995a, b, c proposed a model in which the PHS Plate rotated clockwise by 34° between 25 and 5 Ma around the Euler pole at 15°N, 160°E, by 50° between 50 and 40 Ma around the pole at 10°N, 150°E, and no rotation between 40 and 25 Ma. Sdrolias et al. (2004) further limited the period of the younger rotation to be between 15 and 5 Ma. However, these models are inconsistent with the PHS Plate motion towards north along the Nankai Trough since 15 Ma deduced from the collision of the IBM Arc against the Southwest Japan Arc mentioned above. Furthermore, based on the volcanic activity in southwestern Japan, the subduction of the hot Shikoku Basin lithosphere beneath the Southwest Japan is considered to have occurred between 17 and 12 Ma concurrently from Kyushu to central Japan just west of the IBM Arc collision zone (Kimura et al., 2005). There is no evidence that the area subducted by the hot Shikoku Basin gradually extended eastward with time, which is predicted from the model proposed by Hall and others. In addition, magnetic anomaly skewness of the Shikoku Basin supports no significant rotation since ∼20 Ma (Chamot-Rooke et al., 1989). The model of Hall and others predicts small or no northward motion between 40 and 25 Ma around the Daito Ridge, with the majority of the northward drift occurring before and after this period of time (Hall et al., 1995c). However, our observation suggests rather rapid northward motion between 40 and 25 Ma (Fig. 3). The model of Hall and others is based mainly on the paleomagnetic data from eastern Indonesia, which is a tectonically active region, and it strongly depends on the results from a single locality mean at about 40 Ma (Hall et al., 1995a, b). Hence, we consider that this model may not be well constrained.
In Palau and Saipan, the easterly deflected declinations were observed in the lower to middle Miocene as well as in the Eocene and Oligocene (Haston and Fuller, 1991). This observation contradicts our model. On the other hand, the declinations of Palau and Saipan require significant rotation of the PHS Plate since the middle Miocene, which is inconsistent with the geology of the Japanese Islands, as mentioned above. The data from Palau and Saipan may have been affected by local tectonic movement because these islands belong to tectonically active regions, but further studies are needed to resolve the inconsistency.
Our model is consistent with the paleomagnetic data from eastern Indonesia in predicting the southward motion of eastern Indonesia between the Eocene and Oligocene. Although the amount of the southward motion depends on the unknown opening direction of the West Philippine Basin, eastward or westward (in the geometry at 50 Ma), it can explain the paleolatitude data of Hall et al.(1995a, b) at least qualitatively. Queano et al. (2007) reported paleomagnetic data from the North Luzon, northern Philippines which indicate an ∼7° northward movement of this region since ∼15 Ma. At the present time, this region is separated from the PHS Plate by the East Luzon Trough-Philippine Trench subduction zone, but it may have been a part of the PHS Plate before 3–5 Ma (Queano et al., 2007). The latitude of the Euler pole position of the PHS Plate since 15 Ma is required to be similar to that of the collision zone between the IBM Arc and Southwest Japan based on the lack of significant movement of the collision zone, but it is difficult to constrain its longitude. If it is to the east of the collision zone and not very far from the PHS Plate, a northward motion of the PHS Plate larger than that at the Nankai Trough (∼3.5° for the last 15 Ma) is predicted at the North Luzon due to the larger distance from the Euler pole, which is consistent with the observation.
The samples used in this study were collected under the project “Deep Sea Survey Technology for Natural Resources in Japan ”conducted by the Japan Oil, Gas and Metals National Corporation. We thank Emi Kariya and Etsuko Usuda for their help with the measurements and the members of the Paleogeodynamics research group of the Geological Survey of Japan, AIST, for helpful discussions. Comments from Jason R. Ali and two anonymous reviewers improved the manuscript.
- Amano, K., Multiple collision tectonics of the South Fossa Magna in Central Japan, Modern Geol., 15, 315–329, 1991.Google Scholar
- Arason, P. and S. Levi, The maximum Likelihood solution for inclination-only data, Eos Trans. AGU, 87(52), Fall Meet. Suppl., Abstract GP21B–1312, 2006.Google Scholar
- Chamot-Rooke, N., K. Tamaki, and K. Kobayashi, Deskewed magnetic profiles of the Shikoku Basin and the past kinematics of the Philippine Sea Plate, Eos Trans., 70, 1365–1366, 1989.Google Scholar
- Deschamps, A. and S. Lallemand, The West Philippine Basin: An Eocene to early Oligocene back arc basin opened between two opposed subduction zones, J. Geophys. Res., 107, doi:10.1029/2001JB001706, 2002.
- Duncan, R. A. and D. A. Clague, Pacific plate motion recorded by linear volcanic chains, in The Pacific Ocean, edited by A. E. M. Nairn, F. G. Stehli, and S. Uyeda, 89–121, The Ocean basin and margins, vol. 7A, Plenum Press, 1985.Google Scholar
- Gladstein, F., J. Ogg, and A. Smith, A Geologic Time Scale 2004, 589 pp., Cambridge University Press, Cambridge, 2004.View ArticleGoogle Scholar
- Hall, R., Cenozoic geological and plate tectonic evolution of SE Asia and the SW Pacific: computer-based reconstructions, model and animations, J. Asian Earth Sci, 20, 353–431, 2002.View ArticleGoogle Scholar
- Hall, R., J. R. Ali, C. D. Anderson, and S. J. Baker, Origin and motion history of the Philippine Sea Plate, Tectonophysics, 251, 229–250, 1995a.View ArticleGoogle Scholar
- Hall, R., J. R. Ali, and C. D. Anderson, Cenozoic motion of the Philippine Sea Plate: Paleomagnetic evidence from eastern Indonesia, Tectonics, 14, 1117–1132, 1995b.View ArticleGoogle Scholar
- Hall, R., M. Fuller, J. R. Ali, and C. D. Anderson, The Philippine Sea Plate: Magnetism and reconstructions, in Active Margins and Marginal Basins of the Western Pacific, edited by Taylor, B. and J. Natland, AGU Geophys. Monogr., 88, 371–404, 1995c.View ArticleGoogle Scholar
- Haston, R. B. and M. Fuller, Paleomagnetic data from the Philippine Sea plate and their tectonic significance, J. Geophys. Res., 96, 6073–6098, 1991.View ArticleGoogle Scholar
- Haston, R., M. Fuller, and E. Schmidtke, Paleomagnetic results from Palau, West Caroline Islands: A constraint on Philippine Sea plate motion, Geology, 16, 654–657, 1988.View ArticleGoogle Scholar
- Hickey-Vargas, R., Basalt and tonalite from the Amami Plateau, northern West Philippine Basin: New Early Cretaceous ages and geochemical results, and their petrologic and tectonic implications, Island Arc,14, 653–665, 2005.View ArticleGoogle Scholar
- Hilde, T. W. C. and C.-S. Lee, Origin and evolution of the West Philippine Basin: A new interpretation, Tectonophysics, 102, 85–104, 1984.View ArticleGoogle Scholar
- Huang, J. and D. Zhao, High-resolution mantle tomography of China and surrounding regions, J. Geophys. Res., 111, B09305, doi:10.1029/2005JB004066, 2006.Google Scholar
- Ishizuka, O., J.-I. Kimura, Y. B. Li, R. J. Stern, M. K. Reagan, R. N. Taylor, Y. Ohara, S. H. Bloomer, T. Ishii, U. S. Hargrove III, and S. Haraguchi, Early stages in the evolution of Izu-Bonin arc volcanism: New age, chemical, and isotopic constraints, Earth Planet. Sci. Lett., 250, 385–401, 2006.View ArticleGoogle Scholar
- Iwamoto, H., M. Yamamoto, N. Seama, K. Kitada, T. Matsuno, Y. Nogi, T. Goto, T. Fujiwara, K. Suyehiro, and T. Yamazaki, Tectonic Evolution of the Central Mariana Trough, Eos Trans., 83, 2002 Fall Meeting Suppl., 2002. 502Google Scholar
- Jolivet, L., P. Huchon, and C. Rangin, Tectonic setting of Western Pacific marginal basins, Tectonophysics, 160, 23–47, 1989.View ArticleGoogle Scholar
- Kato, T., Y. Kotake, S. Nakao, J. Beavan, K. Hirahara, M. Okada, M. Hoshiba, O. Kamigaichi, R. B. Feir, P. H. Park, M. D. Gerasimenko, and M. Kasahara, Initial results from WING, the continuous GPS network in the western Pacific area, Geophys. Res. Lett., 25, 369–372, 1998.View ArticleGoogle Scholar
- Kimura, J.-I., R. J. Stern, and T. Yoshida, Reinitiation of subduction and magmatic responses in SW Japan during Neogene time, Geol. Soc. Am. Bull., 117, 969–986, 2005.View ArticleGoogle Scholar
- Kinoshita, H., Paleomagnetism of sediment cores from Deep Sea Drilling Project Leg 58, Philippine Sea, Init. Rep. DSDP, 58, 765–768, 1980.Google Scholar
- Kirschvink, J. L., The least-squares line and plane and the analysis of paleomagnetic data, Geophys. J. R. Astron. Soc., 62, 699–718, 1980.View ArticleGoogle Scholar
- Kodama, K., B. H. Keating, and C. E. Helsley, Paleomagnetism of the Bonin Islands and its tectonic significance, Tectonophysics, 95, 25–42, 1983.View ArticleGoogle Scholar
- Koyama, M., S. M. Cisowski, and P. Pezard, Paleomagnetic evidence for northward drift and clockwise rotation of the Izu-Bonin forearc since the early Oligocene, Proc. ODP Sci. Results, 126, 353–370, 1992.Google Scholar
- Louden, K. E., Paleomagnetism of DSDP sediments, phase shifting of magnetic anomalies, and rotations of the West Philippine Basin, J. Geophys. Res., 82, 2989–3002, 1977.View ArticleGoogle Scholar
- Matsuda, N., H. Tsuchiya, K. Matsumoto, N. Saito, and M. Endo, Development and operation of deep-sea boring machine system by operating group on the deep-sea boring machine system, Shigen-to-Sozai, 120, 425–430, 2004 (in Japanese with English abstract).View ArticleGoogle Scholar
- Matsumoto, K. and S. Sarata, Development of Deep-sea Boring Machine System, Shigen-to-Sozai, 112, 1015–1020, 1996 (in Japanese with English abstract).View ArticleGoogle Scholar
- Nakamura, K., K. Shimazaki, and N. Yonekura, Subduction, bending and eduction. Present and Quaternary tectonics of the northern border of the Philippine Sea plate, Bull. Soc. Géol. Fr., 26, 221–243, 1984.View ArticleGoogle Scholar
- Okino, K., Y. Shimakawa, and S. Nagaoka, Evolution of the Shikoku Basin, J. Geomag. Geoelectr., 46, 463–479, 1994.View ArticleGoogle Scholar
- Okino, K., Y. Ohara, S. Kasuga, and Y. Kato, The Philippine Sea: New survey results reveal the structure and the history of the marginal basins, Geophys. Res. Lett., 26, 2287–2290, 1999.View ArticleGoogle Scholar
- Queano, K. L., J. R. Ali, J. Milsom, J. C. Airchison, and M. Pubellier, North Luzon and the Philippine Sea Plate motion model: Insights following paleomagnetic, structural, and age-dating investigations, J. Geophys. Res., 112, B05101, doi:10.1029/2006JB004506, 2007.Google Scholar
- Sdrolias, M., W. R. Roset, and R. D. Muller, An expression of Philippine Sea plate rotation: the Parece Vela and Shikoku Basins, Tectonophysics, 394, 69–86, 2004.View ArticleGoogle Scholar
- Seno, T. and S. Maruyama, Paleogeographic reconstruction and origin of the Philippine Sea, Tectonophysics, 102, 53–84, 1984.View ArticleGoogle Scholar
- Seno, T., S. Stein, and A. E. Gripp, A model for the motion of the Philippine Sea Plate consistent with NUVEL-1 and geological data, J. Geophys. Res., 98, 17941–17948, 1993.View ArticleGoogle Scholar
- Sharp, W. D. and D. A. Clague, 50-Ma initiation of Hawaii-Emperor bend records major change in Pacific Plate motion, Science, 313, 1281–1284, 2006.View ArticleGoogle Scholar
- Shih, T.-C., Marine magnetic anomalies from the West Philippine Sea: Implications for the evolution of marginal basins, in The Tectonic and Geologic Evolution of Southeast Asian Seas and Islands, edited by Hayes, D. E., AGU Geophys. Monogr., 23, 49–76, 1980.View ArticleGoogle Scholar
- Shipboard Scientific Party, Site 1201, Proc. ODP, Init. Reps., 195, 1–233, doi:10.2973/odp.proc.ir.195.104.2002, 2002.Google Scholar
- Takahashi, M. and K. Saito, Miocene intra-arc bending at an arc-arc collision zone, central Japan: Reply, Island Arc, 8, 117–123, 1999.Google Scholar
- Yamazaki, T. and Y. Okamura, Subducting seamounts and deformation of overriding forearc wedges around Japan, Tectonophysics, 160, 207–229, 1989.View ArticleGoogle Scholar
- Yamazaki, T. and R. J. Stern, Topography and magnetic vector anomalies in the Mariana Trough, JAMSTEC J. Deep Sea Res., 13, 31–45, 1997.Google Scholar