Geographical Review of Vol. 69 (Ser. B), No. 2, 134-143, 1996

Recent Studies on the Late Quaternary Landform Evolution of Riverine Coastal Plains in Japan

Masatomo UMITSU Department of Geography, Nagoya University, Chikusa, Nagoya 464-01, Japan

Abstract: Recent studies on the evolution of Japanese riverine coastal plains and sea-level changes in the late Quaternary are reviewed. Studies on the landforms and sediments of the plains have been done in many riverine coastal plains using various research techniques. Landforms and sediments of the riverine coastal plains have changed remarkably since the last glacial maximum. Several studies have clarified the paleogeography of the plains, and also pointed out that the landform evolution of the plains has been influenced by minor fluctuations of sea-level changes in the late Holocene.

Key words: late Quaternary, Holocene, landform evolution, riverine coastal plain, sea-level change

ten by Ota et al. (1982, 1990), Yonekura and Ota Introduction (1986), Ota and Machida (1987), Iseki (1988), Oya et al. (1988), Umitsu (1991), and so on. The There are a number of small coastal plains aim of this paper is to review papers on the both on the Pacific and coasts of subject which have been published mainly in the Japanese, islands; they develop not only the last decade. along sandy coasts but also in the regions of lower reaches of rivers. These coastal plains are Characteristics and Environmental Set termed riverine coastal plains in this paper. tings of Japanese Riverine Coastal Plains According to Thom (1982) and Woodroffe (1990), these plains can be classified into river Most Japanese plains are depositional plains dominated and wave-dominated coastal plains that consist of Pleistocene uplands and Holo fr om the viewpoint of their formative settings. cene alluvial lowlands. Pleistocene uplands There are few tide-dominated coastal plains in occupy large areas in the Kanto, Mikawa, and Japan. Stratigraphic studies of the sediments of Tokachi plains etc., and Holocene alluvial the coastal plains indicate that there have been lowlands occupy a large area in the Ishikari, considerable changes in landforms since the Niigata, and Nobi plains, etc. Most Pleistocene last glacial maximum. These changes have uplands in Japan were formed as marine or resulted from postglacial sea-level changes. fl uvial terraces during the last interglacial and Many studies have been carried out on both last glacial periods. sea-level changes and landform evolution of Kubo (1990) examined in detail the landforms the riverine coastal plains in Japan. Studies on of the Kanto plain, where the metro sediments and landforms of Japanese coastal politan area is located. She reviewed studies on plains are mainly conducted by physical geog the evolution of the Pleistocene uplands and raphers and Quaternary geologists. The stratig upland-dissected valleys in the plain, and also raphy and chronology of Holocene sediments of presented the evolution of the Tokyo Lowland riverine coastal plains allow reconstruction of in prehistoric and historic times. the ways in which landforms have responded to Sediments of the present riverine coastal sea-level changes in the past. plains have been deposited in, and over, valleys Several review papers on the late Quaternary formed by the last glacial maximum under low evolution of Japanese riverine coastal plains sea-level conditions. Deposition and landform and sea-level changes have already been writ evolution of the riverine coastal plains com Late Quaternary Evolution of Coastal Plains 135

menced with the postglacial sea-level rise. Osaka River, respectively. The age of the basal Typical Japanese riverine plains consist of gravel bed of the paleo-river channel in the alluvial fans, floodplains, and deltas from the Sakuragawa lowland, northeast of Tokyo, is inner to coastal regions in that order (Oya et al. estimated at 2.4-2.2ka (Suzuki et al. 1993). 1988). However, considerable variation in land This age is slightly older than those given in form is observed between the individual river previous studies. me coastal plains. There are plains without Sea-level changes during the late glacial deltas, plains with broad flood plains, and plains period are still poorly understood. Sediments in which alluvial fans occupy the entire plain. of the period in buried, channels of riverine Large dunes or sandy barriers also develop coastal lowlands are sandy and have a relati along the shoreline of the Tsugaru, Akita, vely high N-value (indicator of the hardness of Shonai, and Niigata plains which located along sediments). Sea levels of the early Holocene the coast of the Sea of Japan. Rows of beach reported in various sites are around -30 to ridges are typically recognized in the Kuju-kuri -50m (Ota et al . 1982, 1990). plain, eastern Japan. Similar rows of beach In the Kanto plain, an unconformity and the ridges are also recognized in the Ishikari, deposition of a conspicuous sandy bed are Yufutsu, and Sendai plains in north and north recognized between the contact of the Pleisto eastern Japan. In general, relatively large cene and Holocene sediments in the riverine plains develop in regions where the land tended coastal plains. These sandy sediments were to subside during the late Quaternary. called the Holocene basal gravel bed (HBG) by A special issue of the Geographical Review of Endo et al. (1982), and they are considered to be Japan on "Fluvial and Coastal Plains in Japan" sediments that were deposited in the period of was published in 1989. Several papers on the Younger Dryas. fl uvial plains (Oya and Kim 1989, Nakayama A slow rise of sea level in the early Holocene and Toyoshima 1989), coastal landforms was reported by Matsushima (1987) and Endo (Fukumoto 1989), coastal sand dunes (Naruse et al. (1989) in the Kanto plain, eastern Japan. 1989), maritime coastal (Hirai 1989) and The period of slow transgression continued barriers in the coastal lowlands (Matsubara until approximately 8,500-8,300yr BP. After 1989) were included in that issue. that period, the sea level rose rapidly and reached a high stand in the middle Holocene Holocene Sea-level Changes in Japan around 7,000-6,000 yr BP. In many places, the sea level during that period is reported to have As a detailed review of studies of sea-level been 2-3m higher than present level (Ota et al. changes in Japan has already been written by 1982, 1990). The highest sea level in the Izu Umitsu (1991), only a brief reference to several Peninsula, which is located on the Philippine recent studies is made here. There are many Sea Plate, however, was recognized at 2,000 -3 opinions about the lowest sea-level during the ,000yr BP (Ota et al. 1986, Taguchi 1993). last glacial maximum: -80m (Oshima 1982, This is considered to be due to the difference in 1990); -95•}3m (Saito et al. 1989) ; -100m tectonic setting between the Philippine Sea and

(Fujii 1990); -127•}30m (Oba 1988); -140m the Pacific Ocean Plates. Marked uplift is evi (Iseki 1977) and so on. Many studies, however, dent on the Boso, Muroto, and other peninsulas regard the level around -100m as the sea-level along the Pacific Ocean and Japan Sea coasts. at that time (Ota and Omura 1991, etc.). The height of middle Holocene marine terraces The extensions of paleo-river valleys formed in these regions was several meters higher than during the last glacial maximum have been the present sea level (Ota and Machida 1987). recognized in various places such as Tokyo and In particular, it was more than 20 meters higher Osaka bays and the continental shelves around in the Boso Peninsula (Frydle 1982). the Japanese islands. The buried paleochannel Minor fluctuations and temporal sea-level under the bottoms of Tokyo and Osaka bays falls after the middle Holocene are reported on are called the paleo-Tokyo River and paleo the Okhotsk coast (Maeda 1984, Sakaguchi et 136 Masatomo Umitsu al. 1985, Hirai 1987), the Inland Sea coast ments including the courses of paleochannels in (Naruse et al. 1984), the Chita Peninsula (Maeda the plain. et al. 1983), etc. In many places, minor sea-level Studies on the landform evolution and sedi falls are recognized around 4.500 and 3,000 ments of the riverine coastal plains of the Kanto 2,000yrs BP, and they are called middle Jornon plain during the Holocene were done by Endo small regression (Ota et al. 1982) and Yayoi et al. (1982, 1987, 1989), Ando (1986, 1988), regression (Ariake Bay Research Group 1965), Ando et al. (1987, 1990), Matsushima (1987), respectively. Kosugi (1989), etc. Most of the studies involved reconstruction of the Holocene depositional Evolution of River-dominated Riverine environments of the riverine coastal plains, and Coastal Plains in Japan determining the extent of marine transgres sion through diatom analysis. These studies Many studies on the sedimentary environ clarified more detailed landform evolution and ments and landform evolution of riverine environmental change in comparison to previ coastal plains have been done based on the ous studies. examination of drilling logs and detailed fossil Based on diatom analysis (Kosugi 1985, 1986, analysis of sediments. Detailed study on the 1988), Kosugi (1989) clarified the evolution of basal topography of the Holocene and latest the Oku- which expanded to the Pleistocene sediments in the Kanto plain was north of the Tokyo lowland during the postgla conducted by Endo et al. (1988). They also cial transgression (Figure 1). Evolution of the discussed the mode of deposition of the sedi region was classified into three stages: (1) trans

Figure 1. Fossil diatom assemblages in the paleo Oku-Tokyo Bay at 5,500yr BP (Kosugi, 1989). Late Quaternary Evolution of Coastal Plains 137 gressive stage (10,000-6, 500yr BP); (2) maxi Holocene sediments in the Hiroshima plain mum transgression (6,500-5,300yr BP); and (3) using FeS2 analysis, and pointed out that regressional stage (5,300yr BP-present). He Holocene sea-level changes in the region con also presented the Holocene relative sea-level sisted not of one cycle with transgression and curve and paleogeographical maps of the regression stages but 2 cycles with a temporary region at 9,500, 5,500 and 4,500yr BP. regression stage between two transgressive Based on diatom and pollen analyses, Endo et stages. Studies on the marine limit using FeS2 al. (1987, 1989) discussed the landform evolu analysis were also carried out by Nakai et al. tion and vegetational change in a riverine (1982), Sadakata et al. (1988), and Sato (1989). coastal plain, and they pointed out that these Nakai et al. (1982) discussed the environmental physical environmental changes did not all and sea-level changes in the Nagoya port region occur independently of each other, but in part based on analyses of the C/N ratio and ƒÂ13C, due to mutual interaction. and recognized colder and lower sea-level peri Further studies on the evolution of landforms od and a warmer and higher sea-level period in and the deposition process of the Holocene sedi the Holocene. Sadakata et al. (1988), and Sato ments in riverine coastal plains with references (1989) also used FeS2 analysis together with to the postglacial transgression have been diatom analysis and reconstructed the late carried out in the Rikuzentakata plain (Chida et Holocene sea-level records in small riverine al. 1984), Akita plain (Geological Research coastal plains. Group of Akita University on the Nihonkai A study on the depositional sequence of the Chubu Earthquake in 1983 1986), Nobi plain was done by Umitsu (1990). He lowland (Matsushima 1987), Nobi plain (Figure classified the Holocene sedimentary sequence 2, Umitsu 1992), Fukuyama plain (Ono 1988), into the following stages: slow transgressive Izumo plain (Hayashi 1991), Hiroshima plain stage (10,000-8,500yr BP); rapid transgressive (Shiragami 1985), Buzen Yukuhashi plain stage (8,500-6,500yr BP); aggradational stage (Chida 1985), Miyazaki plain (Nagaoka et al. (6,500-5,500yr BP); and progradational stage 1986), etc. (5,500yr BP-present) which includes minor In particular, Shiragami (1985) analyzed the regressional stages during the periods of 5,000

Figure 2. Idealized Holocene stratigraphy and sedimentary model of the delta, central Japan (Umitsu, 1992). 138 Masatomo Umitsu

4,500yr BP and 3,000-2,000yr BP. of beach ridges in five coastal plains including Studies on small estuarine coastal lowlands the Sendai and Ishinomaki plains in north were also done by Ota et al. (1985, 1986), eastern Japan. Tose studies confirmed that the Matsubara et al. (1986), Fujimoto (1990, 1993), origin of beach ridges found in these coastal and Sawa et al. (1994) based on the analysis of plains are convex parts of the Holocene upper molluscs and/or microfossils. They clarified sand which were formed by Holocene sea-level the sedimentary environments, paleogeogra fl uctuations. Four rows of beach ridges can be phy, and sea-level changes of the region in the seen in these coastal plains, and the similarity middle and late Holocene. in the formative period of each beach ridge range was pointed out. Each row of beach Evolution of Wave-dominated Coastal ridges (BR-I, BR-I', BR-II, and BR-III) was Plains in Japan formed in the periods of 5,400-4,500 yr BP, 3,300-3,000yr BP, 2,800-1,700yr BP, and 800 Most Japanese wave-dominated coastal plains yr BP-present, respectively (Matsumoto 1984, are characterized by rows of beach ridges and 1985). sand dunes. Matsumoto (1984, 1985) clarified Rows of beach ridges are also recognized in the evolution and period of formation of rows small riverine coastal plains. Shiragami (1983)

Figure 3. Geomorphological map of the Sarobetsu plain (Ohira, 1995). 1. 2. mountains, hills and terraces 3. alluvial fan 4. peatland 5, coastal sand dune ridge 6. floodplain (partly lower peatland) 7. natural levee 8. abondoned river channel Late Quaternary Evolution of Coastal Plains 139

Figure 4. Chronology of Holocene palaeoen vironmental changes in the Sarobe tsu plain (Ohira, 1995). A: river channel side B: peatland near a river channel C: peatland far from a river channel D: coastal sand dune ridges E: relative sea-level changes in the F: paleoclimate 1. lagoon 2. floodplain 3. peatland 4. coast al barrier 5. sand dune ridges 6. soil 7. peat 8. shell

examined the number of beach ridges in rela secondary barrier formation are considered to tion to geological conditions along the western coincide with the minor sea-level regression in coast of Island. He concluded that the middle and late Holocene, which are also three rows of beach ridges are developed in seen in other coastal plains. regions where the geology consists of relatively Matsubara (1992) discussed the relationship soft rocks, coastal terraces are well developed, between human activity and landform evolu and the gradient of paleochannel of the last tion of the barriers. She pointed out that the glacial maximum is relatively gentle. There are initial stage of human activity coincided with one or two rows of beach ridges in regions the period when the area around the Megazuka where the geological conditions differ from archaeological site changed from a lagoon to a those mentioned above. back-swamp due to the construction of coastal Studies on the evolution of coastal plains barrier II (ca. 4,000yr BP), and that the initial with conspicuous coastal barriers were carried stage of human settlement coincided with the out in regions along the coast of period when the formation of coastal barrier III (Matsubara 1984, 1988, 1989), the northeast was completed (ca. 2,000 yr BP). Niigata plain (Ohira 1992), and the Sarobetsu Based on diatom analysis, Ohira (1992) stud plain (Ohira 1995), and others. Matsubara ied the Holocene sedimentary environments (1989) reconstructed the Holocene landform on the northeastern Niigata plain. He recon evolution and sedimentary environment of five structed the Holocene landform evolution of lowlands including Ukishimagahara, and the the region and pointed out that there was a Kano River, lowlands based on the period of strong sediment supply between analysis of foraminifera. According to Ma 5,400-4,800yr BP. Further study was con tsumbara (1984), coastal barriers in this region ducted by Ohira (1995) on the landform evolu are classified into primary barrier formed tion of the Sarobetsu plain in , north during the Holocene transgression and second ern Japan (Figure 3). He discussed the evolu ary barrier that developed after the transgres tion of peatland in relation to the late Holocene sion seaward of the primary barrier. Formation environmental change, and noted that forma of the primary barrier started 8,000yr BP, and tion and expansion of peatland in the Sarobetsu the secondary barrier developed and closed a plain were closely related to the late Holocene mouth of inland areas in periods 5,000-4,000yr minor sea-level fall in the periods ca. 4,500 BP and 3,000-2,000yr BP. These two periods of 4,000 yr BP (Figure 4), and active fluvial condi 140 Masatomo Umitsu

tions were seen in the period of ca. 3,000-2,000 Lake (Akagi et al. 1993). yr BP under a cool and humid climate. Ohira et al. (1994) discussed the evolution of peatland in small estuarine plains located along Evolution of Maritime Coastal Lakes in the shores of , northern Japan. They Japan concluded that the formation and evolution of peatland is closely related to middle and late Many studies on the late Quaternary en Holocene sea-level fluctuations. vironmental changes of maritime coastal lakes have been done in (Ikeya et al. Concluding Remarks 1990), and Shinji lakes (Tokuoka et al. 1990), Kasumigaura Lake (Saito et al, 1990), etc. Recent studies on the evolution and landform Most of these maritime coastal lakes are consid formation of riverine coastal plains in Japan ered to have evolved from former inlets that have been carried out with reference to late expanded inland during the postglacial marine Quaternary sea-level changes. In particular, transgression, and are not yet infilled by sedi studies conducted during the last decade have ments. Studies on the lake-floor landforms and characteristically based their discussions and sea-level changes in the maritime coastal lakes explanations of late Holocene landform evolu have been carried out by Hirai (1983, 1987, tion on the minor sea-level fluctuations of the 1989). late Holocene. There are many places, however, Hirai (1989) classified the landforms of lake where the minor sea-level fluctuations have not side terraces and littoral shelves of Japanese yet been examined. Furthermore, the influence maritime coastal lakes, and discussed land of local tectonics, climatic changes, and sedi forms and sea-level changes in the middle and ment supply during the late Holocene should late Holocene. He concluded that two terraces also be examined more in detail. To this end, on the lakeside lowlands were formed at two future research will need to incorporate region different high lake-water levels 6,000yr BP and al comparisons and examination of the land 4,000-3,000yr BP, and that littoral shelves that form evolution of riverine coastal plains. indicate low-water levels were formed in times Acknowledgments of low water in 4,500yr BP, 3,000-2,000yr BP, and in the 16-17th centuries. I would like to express my thanks to Mr. T. R. Ikeya et al. (1990) conducted an interdiscipli Hashimoto of Sydney University for his assistance in the correction of English in my manuscript. nary study, including geology, sedimentology, (Received Jan. 31, 1996) geography, geochemistry, paleontology, biolo (Accepled May 25, 1996) gy, archeology, and pedology, on the formation and evolution of Lake Hamana during the References Holocene. The results of analyses of the sedi ments revealed the following six stages in rela Akagi, S., Toyoshima, Y., Hoshimi, K., and Tanimura, tion to global sea-level changes: a period of M. 1993. Geoenvironment and geologic history of gradual rise of the sea level 10,000-9,000 yr BP; lake Koyamaike, Tottori prefectre. The Memoirs of the Geological Society of Japan, 39:103-116. (JE) a period of rapid rise of the sea level 9,000 Ando, K. 1986. Holocene paleoenvironments and the 6,000yr BP; a period of a stable high sea level highest sea-level based on the diatom assem 6,000-3,500yr BP; a period of falling sea level blages in Minuma Lowland, Saitama Prefecture. 3,500-2,800yr BP; a period of stable low sea Daiyonki-kenkyu (The Quat. Res. ), 23: 165-174. level 2,800-1,000yr BP; and a period of rising (JE) sea level from 1,000yr BP-present. Paleogeogra Ando, K. 1988. Marine clay deposits on the US phical maps of Lake Hamana 10,000, 6,000, (Holocene upper sand bed) in Arakawa lowland, Saitama Prefecture. Daiyonki-kenkyu (The Quat. 3,000, and 1,800yr BP were also drawn in the Res.), 27: 139-151. (JE) study. Further studies on the evolution of mari Ando, K., and Fujimoto, K. 1990. Radiocarbon ages time coastal lakes in the Holocene were done on obtained from upper limit of marine deposits in Kamo Lake (Kobayashi et al. 1993) and Koyama Arakawa lowland and problems for recogni Late Quaternary Evolution of Coastal Plains 141

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