Geomorphic Development of the Ota River Lowland, Southern Part of the Fukuroi City, Shizuoka Prefecture, Japan

The Ota River Lowland is located in the middle part of the Tokai region, Central Japan, extending about 20km from north to south and 12km from east to west. The Lowland is mainly composed of muddy deposits which are carried by the Ota River. The purpose of this paper is to clarify the formative proc...

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Published inKikan chirigaku Vol. 47; no. 2; pp. 103 - 118
Main Author WATANABE, Fumihiko
Format Journal Article
LanguageEnglish
Published Sendai The Tohoku Geographical Association 1995
Japan Science and Technology Agency
Online AccessGet full text
ISSN0916-7889
1884-1252
DOI10.5190/tga.47.103

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Abstract The Ota River Lowland is located in the middle part of the Tokai region, Central Japan, extending about 20km from north to south and 12km from east to west. The Lowland is mainly composed of muddy deposits which are carried by the Ota River. The purpose of this paper is to clarify the formative process of the Ota River Lowland. This study is based on the analysis of data from boring, the results of radiocarbon dating, the distribution of archaeological remains, the distribution of the Jori grid-system, and old maps. The sediments of the Ota River Lowland are divided into six units: the basal gravel layer (BG), the lower silt and clay layer (LC), the middle sand layer (MS), the middle silt and clay layer (MC), the upper sand layer (US), and the upper silt and clay layer (UC). The basal gravel layer is considered to represent the river bed gravel in the Last Glacial Age. The lower silt and clay layer was deposited under a low salinity environment and is divided into silt and clay. The silt layer contains a small quantity of shell and the clay layer contains a little humus. The middle sand layer is contrasted to the Holocene Basal Gravel Bed (HBG). The HBG was named by Endo et al. (1982), and indicates the basal gravel layer of the Holocene deposits. The middle silt and clay layer contains a large quantity of shell which shows that the depositional environment was affected greatly by marine water. The upper sand layer is the marine deposits, containing a little biotite, pyrite and magnetite, and is supposed to represent the deposit which is carried by the Tenryu River. The upper silt and clay layer is composed of humic silt and clay, and is considered to have been deposited in a sedimentary environment of backmarsh. In conclusion, the geomorphic development of the Ota River Lowland during the latest Pleistocene to the present is summarized as follows. 1) In the latest Pleistocene, the Ota River Lowland was developed in the former fluvial valley formed by the lowest sea level of the Last Glacial Age. Afterward, the former fluvial valley was drowned by transgression, and was filled with silt and clay (about 20, 000-10, 000 years ago). 2) About 10, 000 years ago, the sea level dropped because of the cold climate episode and the fluvial sand accumulated in the drowned valley again. 3) In the early Holocene, the sea level rose rapidly. As a result, the Ota River Lowland became a bay. After the culmination of the post glacial sea level rise, the sea level remained stable. At this time, the sediments of the Tenryu River drifted into the bay of the Ota River Lowland, and closed the bay mouth (about 10, 000-6, 000 years ago). 4) The closed bay became a brackish, swampy lagoon (about 6, 000-1, 900 years ago). 5) In the late Yayoi period, the sea level rose again and the sea water flowed into the middle part of the Ota River Lowland (about 1, 900-1, 700 years ago). 6) By the seventh century, the Jori grid-system was enforced and the sea level dropped again. However, the water area was left in the southern part of the Ota River Lowland as before (about 1, 700-1, 300 years ago). 7) The water area disappeared owing to the Hoei earthquake in 1707 (about 300 years ago).
AbstractList The Ota River Lowland is located in the middle part of the Tokai region, Central Japan, extending about 20km from north to south and 12km from east to west. The Lowland is mainly composed of muddy deposits which are carried by the Ota River. The purpose of this paper is to clarify the formative process of the Ota River Lowland. This study is based on the analysis of data from boring, the results of radiocarbon dating, the distribution of archaeological remains, the distribution of the Jori grid-system, and old maps. The sediments of the Ota River Lowland are divided into six units: the basal gravel layer (BG), the lower silt and clay layer (LC), the middle sand layer (MS), the middle silt and clay layer (MC), the upper sand layer (US), and the upper silt and clay layer (UC). The basal gravel layer is considered to represent the river bed gravel in the Last Glacial Age. The lower silt and clay layer was deposited under a low salinity environment and is divided into silt and clay. The silt layer contains a small quantity of shell and the clay layer contains a little humus. The middle sand layer is contrasted to the Holocene Basal Gravel Bed (HBG). The HBG was named by Endo et al. (1982), and indicates the basal gravel layer of the Holocene deposits. The middle silt and clay layer contains a large quantity of shell which shows that the depositional environment was affected greatly by marine water. The upper sand layer is the marine deposits, containing a little biotite, pyrite and magnetite, and is supposed to represent the deposit which is carried by the Tenryu River. The upper silt and clay layer is composed of humic silt and clay, and is considered to have been deposited in a sedimentary environment of backmarsh. In conclusion, the geomorphic development of the Ota River Lowland during the latest Pleistocene to the present is summarized as follows. 1) In the latest Pleistocene, the Ota River Lowland was developed in the former fluvial valley formed by the lowest sea level of the Last Glacial Age. Afterward, the former fluvial valley was drowned by transgression, and was filled with silt and clay (about 20, 000-10, 000 years ago). 2) About 10, 000 years ago, the sea level dropped because of the cold climate episode and the fluvial sand accumulated in the drowned valley again. 3) In the early Holocene, the sea level rose rapidly. As a result, the Ota River Lowland became a bay. After the culmination of the post glacial sea level rise, the sea level remained stable. At this time, the sediments of the Tenryu River drifted into the bay of the Ota River Lowland, and closed the bay mouth (about 10, 000-6, 000 years ago). 4) The closed bay became a brackish, swampy lagoon (about 6, 000-1, 900 years ago). 5) In the late Yayoi period, the sea level rose again and the sea water flowed into the middle part of the Ota River Lowland (about 1, 900-1, 700 years ago). 6) By the seventh century, the Jori grid-system was enforced and the sea level dropped again. However, the water area was left in the southern part of the Ota River Lowland as before (about 1, 700-1, 300 years ago). 7) The water area disappeared owing to the Hoei earthquake in 1707 (about 300 years ago).
Author WATANABE, Fumihiko
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References_xml – reference: 森脇広 (1979): 九十九里浜平野の地形発達史. 第四紀研究, 18, 1-16.
– reference: 江坂輝彌 (1982): 縄文土器文化研究序説. 六興出版.
– reference: 海津正倫 (1976): 津軽平野の沖積世における地形発達史. 地理学評論, 49, 714-735.
– reference: Sakaguchi, Y., Kashima K. and Matsubara A. (1985): Holocene marine deposits in Hokkaido and their sedimentary environments. Bulletin of the Department of Geography University of Tokyo, 17, 1-17.
– reference: 渡辺誠・磯谷和明 (1981): 磐田市御殿・二之宮遺跡の自然遺物. 磐田市教育委員会編: 御殿・二之宮遺跡発掘調査報告書I. 磐田市, 74-75.
– reference: 杉原荘介 (1977): 日本農耕社会の形成. 吉川弘文館.
– reference: 鹿島薫・長澤良太・宮崎隆 (1985): 静岡県菊川平野における完新世の海水準変動に関する資料. 第四紀研究, 24, 45-50.
– reference: 静岡県教育委員会 (1979): 静岡県遺跡地図. 静岡県.
– reference: 谷岡武雄 (1963): 平野の地理. 古今書院.
– reference: Endo, K., Sekimoto K. and Takano T. (1982): Holocene stratigraphy and paleoenvironments in the Kanto Plain, in relation to the Jomon Transgression. Institute of Natural Sciences College of Humanities and Sciences, Nihon University, Earth Sciences, 17, 1-16.
– reference: 大庭正八 (1983): 袋井市域の地形と地質. 袋井市編: 袋井市史 通史編. 袋井市, 5-51.
– reference: 千田昇 (1987): 大分平野西部の完新世における地形発達. 地理学評論, 60, 466-480.
– reference: 松原彰子 (1984): 駿河湾奥部沖積平野の地形発達史. 地理学評論, 57, 37-56.
– reference: 柴田稔 (1987): 地理的環境. 浅羽町教育委員会編: 権現山遺跡. 浅羽町, 5-13.
– reference: 鈴木正男 (1976): 過去をさぐる科学. 講談社.
– reference: 平野吾郎 (1974): 見性寺貝塚調査における二, 三の問題. 磐田市教育委員会編: 遠江見性寺貝塚の研究. 磐田市, 45-53.
– reference: 永井義博 (1987): 結語. 袋井市教育委員会編: 鶴松遺跡II. 袋井市, 42-59.
– reference: 藤本潔 (1990): 松島湾岸谷底平野における後期完新世海水準微変動の連続的復元. 地理学評論, 63, 629-652.
– reference: 加藤芳郎 (1985a): 坂尻遺跡をめぐる地形・地質学的背景. 静岡県教育委員会編: 一般国道1号袋井バイパス埋蔵文化財発掘調査報告書坂尻遺跡. 静岡県, 1-12.
– reference: 袋井市 (1983): 袋井市史 通史編. 袋井市.
– reference: 吉岡伸夫 (1983): 縄文時代の袋井市域. 袋井市編: 袋井市史 通史編. 袋井市, 109-133.
– reference: 平井幸弘 (1987): サロマ湖の湖岸・湖底地形と完新世後半のオホーツク海の海水準変動. 東北地理, 39, 1-15.
– reference: 加藤芳郎 (1962): 出土貝類について. 磐田市教育委員会編: 西貝塚. 磐田市, 16-17.
– reference: 松本秀明 (1984): 海岸平野にみられる浜堤列と完新世後期の海水準微変動. 地理学評論, 57, 720-738.
– reference: 井関弘太郎 (1975a): 沖積層基底礫層について. 地学雑誌, 84, 247-264.
– reference: 市原寿文 (1967): 遠江石原貝塚の研究. 静岡大学人文学部人文論集, 18, 25-44.
– reference: 経済企画庁 (1965): 表層地質図5万分の1磐田・掛塚, 土地分類基本調査. 経済企画庁.
– reference: 鶴見英策ほか (1983): 南関東・東海地域広域変動地形調査. 建設省国土地理院.
– reference: 市原寿文 (1978): 大畑遺跡の立地環境. 袋井市教育委員会編: 袋井市大畑遺跡1977年度の発掘調査. 袋井市, 5.
– reference: 西村嘉助 (1957): 条里以後の地形変化. 広島大学文学部紀要, 11, 132-145.
– reference: 井関弘太郎 (1975b): 沖積世後期の海水準変化と遺跡の地形環境. 考古学と自然科学, 8号, 39-52.
– reference: Matsuda, I. (1974): Distribution of the recent deposits and buried landforms in the Kanto Lowland, Central Japan. Geographical Reports of Tokyo Metropolitan University, 9, 1-36.
– reference: 千田昇・松本秀明・小原真一 (1984): 陸前高田平野の沖積層と完新世の海水準変化. 東北地理, 36, 232-239.
– reference: 石野博信・岩崎卓也・河上邦彦・白石太一郎編 (1991): 古墳時代の研究 第6巻 土師器と須恵器. 雄山閣.
– reference: 大平明夫 (1992): 完新世における新潟平野北東部の地形発達史. 地理学評論, 65, 867-888.
– reference: 加藤芳郎 (1985b): 土橋遺跡をめぐる地形・地質学的背景, 袋井市教育委員会編: 土橋遺跡基礎資料編. 袋井市, 11-25.
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