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• W2068036009 abstract "In their recent paper, Takahashi and Saito (1997) summarize current thinking regarding the development of the Kanto Syntaxis in Central Japan. The basic model they present is that since the late middle Miocene, the end-on orientated Izu–Bonin Ridge island arc on the Philippine Sea Plate has effectively been punching a southeast–northwest-orientated deformation front into the Honshu Arc in Central Japan. This model builds upon previous works by Matsuda (1979), Amano (1986, 1991), Niitsuma (1989) and Otsuki (1990) to name but five. This latest version utilizes paleomagnetic, sedimentologic and biostratigraphic information and makes key assumptions regarding the relative motion of the Philippine Sea Plate and the Japan Arc. It is the latter element that we consider problematic in particular with regards to the pre-Pliocene development of the Kanto Syntaxis. Paleomagnetic declination offsets observed in Miocene rocks in the Chichibu Basin (Hyodo & Niitsuma 1986) and the Uchiyama Area (Takahashi & Watanabe 1993), east Kanto Syntaxis, are considered to record collision events in the late middle Miocene and the late Miocene. The sedimentological studies of Amano (1986, 1991) on trough-fill marine sediments with interbedded conglomerates in the South Fossa Magna are used as evidence for four (two additional) collision events. Nannofossils and foraminifers recovered from those marine sediments are used to date the collisions. Combining all of this information, it is argued that the Kushigatayama and Misaka Blocks arrived in the syntaxis at 12 and 9–7 Ma, respectively (recorded paleomagnetically and sedimentologically). The later arrival of the Tanzawa (5–3 Ma) and Izu Blocks (1 Ma onwards) appears not to have induced any deformation in the eastern Kanto Syntaxis (paleomagnetic data in Takahashi & Nomura 1989) but is represented by triggered conglomerate deposition. A key element in the Kanto Syntaxis model is the relative convergence of the Philippine Sea Plate and the Honshu Arc for the middle Miocene–Present, and specifically the position of the Izu Peninsula and subducted along-strike equivalents of the Izu–Bonin Ridge (SIBR). Takahashi and Saito (1997) propose a punctuated linear accretion of the SIBR fragments based upon the assumption that the Philippine Sea Plate has been converging northwest with Japan at 3.4 cm/year since the late middle Miocene (12 Ma). Because the Kanto Syntaxis model is based partially upon paleomagnetic data, it is perhaps worth considering new, largely paleomagnetic-based, information relevant to the Miocene motion between the Philippine Sea Plate and the Honshu Arc. Fortunately for plate tectonic modeling in the region, the effects of the Japan Sea (Jolivet et al. 1995; Takahashi & Saito 1997) and Shikoku Basin (Taylor 1992) spreading can be ignored because these events terminated a few million years prior to the Kushigatayama Block collision at 12 Ma. Therefore, the Philippine Sea Plate motion is the principal factor in the convergence equation. Numerous attempts have been made to calculate the present day motion of the Philippine Sea Plate relative to Eurasia (Fitch 1972; Karig 1975; Ranken et al. 1984; Huchon 1986; Seno et al. 1987), all locating the Euler pole to the northeast of Japan. The most recent effort by Seno et al. (1993) positioned the Euler pole at 48.2°N, 157.0°E with a rotation rate of 1.09°/million years (clockwise). Using geological arguments, Seno et al. (1993) extrapolated the current convergence motion of the plate back into the Pliocene. The major problem facing geologists trying to evaluate the Philippine Sea Plate’s pre-Pliocene motion is the fact that it is both isolated from the mid-ocean ridge reference frame and does not possess a suitable hot spot trace. However, it has been recognized for some time that the plate had moved northwards and that it underwent clockwise rotation (Louden 1977; Otsuki 1990; Haston & Fuller 1991), but no one had proposed a precise estimate of the plate’s Euler pole(s) and rotation vector(s). Recently, new paleomagnetic data from the southern part of the Philippine Sea Plate have been obtained (Ali & Hall 1995; Hall et al. 1995a) which has enabled the motion of the plate to be established more precisely (Hall et al. 1995b). The Miocene Euler pole was positioned much further south than its present day location at 15°N 160°E, with 34° clockwise rotation taking place between 25 and 5 Ma. Hall et al. (1995b) showed also that the new model could account for the paleomagnetic inclination shifts obtained from Deep Sea Drilling Project/Ocean Drilling Program (DSDP/ODP) and onland sites on the northern half of the plate and practically all of the declination offsets obtained from the eastern margin of the plate (Mariana and Bonin Islands). The few anomalous offsets, for example between some similar age formations in the Bonin Islands, were attributed to local block rotation within the forearc region. Also, the model offered a relatively simple explanation of the Cenozoic development of the Australia–Philippine Sea Plate boundary and the source of the ophiolitic and arc fragments embedded in the North New Guinea Orogen (Ali & Hall 1995). Hall et al. (1995b) chose the Eurasia– Philippine Sea Plate Euler poles and rotation amounts of: 5–0 Ma, 48.2°N 157.0°E, 5.45° clockwise (based on Seno et al. 1993); 25–5 Ma, 15°N 160°E, 34° clockwise; 40–25 Ma, no motion; 50– 40 Ma, 10°N 150°E, 50° clockwise. In the light of this new information, we have calculated the position of the present-day northern end of the Izu–Bonin Ridge at 2.5 million-year intervals back to 15 Ma (Fig. 1). Also drawn in Fig. 1 is the position of the SIBR at 12.5 Ma. We assume it formed a belt ~ 120 km wide and was a linear extension of the present-day Izu–Bonin Ridge. We consider this a reasonable assumption because the Izu–Bonin–West Mariana Ridge today forms a > 2500-km linear feature south to 23°N. Also, Takahashi and Saito (1997) assume a linear trend along the Izu–Bonin Ridge-SIBR. In addition, we have calculated the position of an Izu-Bonin Ridge-SIBR using the Seno et al. (1993) current convergence model back to 12.5 Ma (Fig. 1). Those authors would almost certainly not support extending their model into the late and middle Miocene, for example they might point out the problem in explaining the subduction history of the Philippine Sea Plate along its western boundary, but it is an assumption implicit in the model of Takahashi and Saito (1997). Plate tectonic model for the Central Japan–Philippine Sea Plate region (based on the CGNW/UNESCO 1990 chart sheet 2). Note the 12.5-Ma backtracked positions of the Izu–Bonin Ridge using the plate motion models of (i) Hall et al. (1995b) and (ii) Seno et al. (1993). Note the position of the ‘subducted’ Izu–Bonin Ridge (SIBR), which in both models is well away from the Kanto Syntaxis at this time. Numbers 2.5, 5, 7.5, 10, 12.5 and 15 (Ma) indicate the position of the present-day northern end of the Izu–Bonin Ridge at various times. Also shown are the 25°N, 35°N, 133°E and 143°E graticules. In both reconstructions the SIBR is a significant distance away from the Kanto Syntaxis in the late middle Miocene. The model of Hall et al. (1995b) places the SIBR ~ 300 km to the west-southwest of the Kanto Syntaxis. For comparison, if we use the Seno et al. (1993) current convergence model (which should not be used), then the western edge of the Izu–Bonin Ridge intersects the Japan margin > 400 km to the north-northeast (Fig. 1). It is interesting to note that the Hall et al. model moves the SIBR close to the Kanto Syntaxis at ca 7.5 Ma. However, convergence between the Philippine Sea Plate and the Japan Arc at that time was much less than it is today (at that time, the motion vector of Philippine Sea Plate relative to the Nankai Trough was subparallel). Therefore, transferring SIBR fragments into the syntaxis at about this time would be possible, although the mechanism might not be buoyant detachment from a subducting plate but could have involved strike–slip faulting. In the early Pliocene, the change of the Philippine Sea Plate motion relative to the Japan Arc would have developed the Kanto Syntaxis in the classic manner as described by Takahashi and Saito (1997). We recognize clearly that the late middle to end Miocene (as well as the Pliocene–Recent) portion of the Kanto Syntaxis deformation model is based upon paleomagnetic and sedimentologic–biostratigraphic observations. However, we have examined their root information sources and can find no compelling arguments indicating that alternative interpretations to both suites of data cannot be developed. With regard to the sedimentological evidence, on the basis of their coarse clast size and inferred rapidity of deposition, Amano (1991) (which is the key information source cited by Takahashi & Saito 1997) suggested that the conglomerates within the Fujikawa Group of the South Fossa Magna represented four separate collisions of four different blocks of the ‘proto Izu–Bonin Arc’. Figure 4 of Kitazato (1997) provides data that put the study of Amano (1991) into a wider geographical perspective and show the lithostratigraphy and chronostratigraphy for the whole of the area of the inferred Izu–Bonin Ridge collision in central Honshu. At ca 5 Ma, conglomerates appear widespread across the area (in four of the sections). Prior to that, conglomerates are restricted solely to the Fujikawa region and even within that area appear not to be as widespread as one would expect (Amano 1991; Fig. 5). The possibility that the Miocene conglomerates may have been generated by other processes such as extension and graben formation related to the bending of the arc (but perhaps beyond the resolution of the available paleomagnetic data for Central Honshu) should be explored. Thus, before a complete understanding of the pre-Pliocene history of the Kanto Syntaxis can be assumed, the basic geometric problem related to Philippine Sea Plate Izu-Bonin Ridge–Honshu Arc motion needs to be appreciated fully. Current convergence models extended back into the Miocene are incompatible with the known geology, the paleomagnetic and the geophysical information from the Philippine Sea Plate and its bordering regions. Moving the Philippine Sea Plate around the western Pacific prior to the Pliocene, in a way that satisfies those observations, requires a quite different Euler pole position(s) and rotation rate(s) to those of the present day. Using the most recently published Miocene Philippine Sea Plate motion information, the earliest age of entry of the SIBR fragments to the Kanto Syntaxis (from the west-southwest) is in the latest Miocene. Strike–slip faulting, rather than buoyant detachment, may have been the way in which the arc pieces were transferred at that time. In future, we hope to add to discussions of the region in a more positive way." @default.
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• W2068036009 title "Miocene intra‐arc bending at an arc–arc collision zone, central Japan: Comment" @default.
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