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Identification of Prospective Geosites That Show Features of the Active Continental Margin in Eastern Kii Peninsula, Southwest Japan

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Identification of Prospective Geosites That Show Features of the Active Continental Margin in Eastern Kii Peninsula, Southwest Japan Acta Geoturistica, vol. 8 (2017), nr. 1, 19-31 DOI 10.1515/agta-2017-0003 Identification of prospective geosites that show features of the active continental margin in eastern Kii Peninsula, Southwest Japan 1* 2 DOROTA SUZUKI and HIDEO TAKAGI 1 Research Institute for Science and Engineering, Waseda University, Tokyo 169-8050, Japan 2 Department of Earth Sciences, Faculty of Education and Integrated Arts and Sciences, Waseda University, Tokyo 169-8050, Japan * ( corresponding author e-mail: [email protected]) ABSTRACT The eastern Kii Peninsula exhibits a variety of rock outcrops, fossils, and other geological features that illustrate the formation history of the Japanese Islands. This work aims to describe the geotourism potential of the region based on the significant rock exposures, and sets out the basis for establishing geosites in this region in the future. Geologically important sites have been selected, together with places of unique history and culture within the northern part of the eastern Kii Peninsula, including the Ise and Toba areas. The results of this study include a detailed description of the geology and history of the region, together with an evaluation of the relative value of each selected locality as a geosite. Proper development and promotion of the proposed sites would make the sites available for education and tourism, and provide opportunities for suitable development and the popularization of geological knowledge. Key words: Kii Peninsula, Ise Jingu Grand Shrine, MTL, geosite INTRODUCTION (JGN) in December 2016, 8 of which are also recognized members of the UNESCO The Japanese Islands were a part of the Global Geopark Network (GGN). Asian continent until the opening of the Since the establishment of the JGN in Japan Sea during the Early–Middle 2008, a number of large disasters have Miocene (c. 20−15 Ma). This led to the damaged Japanese geopark areas; e.g., development of the islands that currently volcanic eruptions in Kirishima Geopark in form an active subduction-related arc– 2011, and many landslides caused by heavy trench system at the junction of four major local rains in Aso Geopark in 2012 and in plates: the Pacific and Philippine Sea Izu-Oshima Geopark in 2013．The recent oceanic plates, and the Eurasian and North Kumamoto Earthquake damaged Aso American continental plates. The complex Geopark in 2016. The Sanriku coastal areas geological history of the islands formation of NE Japan were affected by the is reflected in a remarkable diversity of destructive tsunami caused by the 2011 geological elements whose variety and Tohoku earthquake, and were subsequently character offer substantial potential for incorporated into the Sanriku Geopark in geotourism. Publication of the first list of 2013, which provides an excellent example 100 geosites in Japan has resulted in a great of using the recognition afforded by expansion of Japanese geoparks and a geosites to assist with reconstruction and growing interest in geotourism. The current disaster prevention. list includes 120 sites, with 43 areas in the The eastern Kii Peninsula (Fig. 2) country certified as national geoparks contains a range of geological features © 2017 Dorota Suzuki and Hideo Takagi. This is an open access article licensed under the Creative Commons Attribution-NonCommercial-NoDerivs License (http://creativecommons.org/licenses/by-nc-nd/3.0/). 19 Acta Geoturistica, vol. 8 (2017), nr. 1, 19-31 illustrative of an active continental margin Asian continent (130−85 Ma) produced a formed by plate subduction, such as large volume of granitic magma that accretionary complexes and high-pressure intruded the pre-Cretaceous accretionary metamorphic rocks, as well as offering complexes and thermally metamorphosed outstanding local culture and historical surrounding rocks, forming the low-P/T elements. Increasing knowledge about the metamorphic rocks of the Abukuma geology of the region may open new metamorphic belt (~110 Ma) and the Ryoke opportunities for geotourism development, metamorphic belt (100−90 Ma; Suzuki, et with potential accompanying economic al., 1996). benefits. This paper aims to identify several The Median Tectonic Line (MTL), a significant locations for geosites in the Ise major fault zone separating the Ryoke and and Toba areas (Suzuki, 2014), and to Sanbagawa metamorphic belts, formed determine the quality and accessibility of initially as a normal fault that presumably each site with respect to geotourism affected the emplacement of older Ryoke potential that is currently unfulfilled, with granitic rocks (Okudaira and Suda, 2011) most of the significant geological sites and juxtaposed the low-P/T Ryoke being poorly known. metamorphic belt against the high-P/T Sanbagawa belt at c. 60 Ma (Takagi et al. 2010). These two belts are commonly BRIEF GEOLOGICAL HISTORY OF described as forming a paired metamorphic THE JAPANESE ISLANDS belt system (Miyashiro, 1961). Cretaceous–Paleogene accretionary The core of Japan’s basement geology complexes are exposed in the Shimanto belt developed from the off-scraping of and in the eastern Hokkaido (Hidaka and sedimentary cover from oceanic plates Tokoro) belts. Back-arc spreading in the subducting along the Asian continental Shikoku Basin (19−15 Ma) caused the margin over the past 500 Myr, resulting in opening of the Japan Sea, accompanied by the episodic development of accretionary volcanism (e.g., Kano et al., 1991). complexes stepping progressively farther Continued rifting of the Shikoku Basin seaward over time. Phases of accretion are during the Miocene led to eastward well preserved from the Permian, Jurassic, migration of the Philippine Sea plate, Cretaceous and Paleogene periods, bringing the Izu–Bonin Arc into contact alternating with episodes of tectonic erosion with central Honshu, with which it collided (Fig. 1; e.g.; Isozaki et al., 2011). Parts of after c. 17 Ma (Sako and Hoshi, 2014). The the Paleozoic accretionary complexes were spreading that formed the Japan Sea metamorphosed under high-P/T conditions produced a 30°–40° anti-clockwise rotation to generate the metamorphic rocks of the of Northeast Japan (Hoshi and Takahashi, Renge belt (~350−280 Ma; Tsujimori and 1999) and clockwise rotation of Southwest Itaya 1999), the Suo belt (~220 Ma; Japan by ~45° to its present position at ~15 Tsutsumi et al., 2000), and the Chizu belt Ma, consistent with a ‘double-door’ model (~180 Ma; Shibata and Nishimura, 1989). for the opening of the Japan Sea (Otofuji et Cretaceous accretionary complexes were al. 1994). Between these two blocks of the metamorphosed, forming the high P/T Japanese Islands, a large basin structure Sanbagawa belt in the Late Cretaceous (e.g., (Fossa Magna) developed, which was filled Miyashita and Itaya, 2002) and the highest- by a thick sequence of Neogene sediments grade rocks in the Kamuikotan zone (145– and volcaniclastics. The Itoigawa–Shizuoka 100 Ma; Shibakusa and Itaya, 1992). Tectonic Line (ISTL) is the western Subduction of the Izanagi-Kula and bounding fault of the Fossa Magna (e.g., Pacific plates beneath the former eastern Takeuchi, 2004). 20 Acta Geoturistica, vol. 8 (2017), nr. 1, 19-31 Fig. 1 Post-Jurassic tectonic development of the Japanese Islands (after Maruyama, 1997; Taira, 2001; Isozaki et al., 2011). AC: accretionary complex, ISTL: Ito–Shizuoka Tectonic Line, K-PR: Kyushu–Palau Ridge, MTL: Median Tectonic Line, NAP: North America Plate. Since the Quaternary, the Japanese island at the east side of Kii Peninsula, the arc system has been strongly compressed northern and eastern parts of which are by westward to northwestward subduction studied here, is a product of oceanic plate of the Pacific plate and the Philippine Sea subduction. In this area, the eastward- plate. Arc–arc collision and further trending belts of variably metamorphosed accretion of the Izu–Bonin Arc to the Jurassic–Cretaceous accretionary Honshu arc after 15 Ma has resulted in complexes and associated igneous rocks are intensive deformation of central Honshu dissected by faults, illustrating the (e.g., Takahashi, 1994). Deep subduction of dynamism of the formation of the Japanese the Philippine Sea plate at the Nankai Islands. Trough has formed a frontal accretionary The Upper Cretaceous Ryoke granites in prism to the Southwest Japan forearc (e.g., the north of this region are juxtaposed Hayman et al., 2012). The western side of against schists of the Sanbagawa the MTL is currently active, and metamorphic belt along the Median accommodates dextral motion. Tectonic Line (MTL). The precise location of this ENE–WSW striking fault has recently been confirmed in the region GEOLOGY OF THE STUDY AREA (Suzuki et al., 2015). The surface trace of the MTL starts to bend gradually eastward The geology of Shima Peninsula located as it crosses the peninsula into the Chubu 21 Acta Geoturistica, vol. 8 (2017), nr. 1, 19-31 region, as a result of the middle Miocene (c. Chichibu belts by the Gokasho–Arashima 15 Ma) to recent collision of the Izu–Bonin Tectonic Line (G–A Line), a group of faults arc with the Honshu arc. within serpentinite mélange. The G–A Line The Sanbagawa metamorphic belt is is considered to represent the extension of distributed continuously across the region the Kurosegawa Terrane, which comprises to the south as the Mikabu greenstone unit, lenticular bodies of pre-Jurassic sediments which includes large ultramafic bodies. To and metamorphic rocks with serpentinite the southeast of the Mikabu unit, the (Saka et al., 1988). The southern margin of Chichibu belt, composed mainly of Jurassic the Chichibu belt is defined by the Butsuzo accretionary complexes with Cretaceous Tectonic Line, along which the sedimentary forearc basin deposits, extends parallel to sequences of the Chichibu belt are thrust the MTL. These sedimentary sequences are over the Cretaceous Shimanto belt to the divided into the Northern and Southern south (Kato & Saka, 2006). Fig. 2 Geological map of the Ise and Toba areas (compiled from the 1:200,000 geological map “Ise”, after Nishioka et al., 2010).
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