The Arakawa Lowland is located in the central part of the Kanto Region. The authors reconstructed the Holocene environmental changes in the upper part of Arakawa Lowland based on analysis of boringlogs, fossil diatom assemblages, and radiometric datings. The relationship between the shoreline location and the distribution of shell mounds was also analyzed. The results can be summarized as follows.
Stratigraphic examination showed a buried valley lying below the Arakawa Lowland, dissecting the buried Tachikawa Terrace at the later maximum stage of the Last Glacial Age. The width of the buried valley is 2.5-3.5km and the level of the valley floor is from -10 to -20m a. s. l. in this area. At the early stage of the Holocene transgression, fluvial (fresh water) sediments were deposited on the lowland. At about 8, 600y. B. P., when the sea-level rose to around -15m a. s. l., the environment of inner bay expanded into this area due to the rise in sea level. The inner bay environment expanded inland and reached to the furthest point at about 8, 300y. B. P. This condition continued till about 6, 800y. B. P. After about 6, 300y. B. P., the inner bay sediments were overlaid by fluvial (fresh water) sediments. Around 5, 500y. B. P., the inner bay environment ceased to exist in this area.
The expansion of the inner bay area at around 8, 300y. B. P., as seen by the fossil diatom assemblage, extended east of the center of the lowland (Fig. 1). Some branches of rivers, such as the Iruma River, the Koaze River, the Oppe River and the Ichinokawa River, flow into the Arakawa River. These supply a great deal of sediment to the lowland. Therefore the inner bay environment did not expand to the west side of the lowland. Furthermore, the molluscan of shell mounds, situated on the uplands, included Corbicula japonica, Crassostrea gigas, Anadara (Tegillarca) granosa, and Meretrix lusoria: such marine-brackish water molluscan shells were found in the Hirakata Shell Mound situated on the Oomiya Upland, while fresh water molluscan shells were found at the Kosenba Shell Mound situated on the Musashino Upland. These molluscan shell compositions of shell mounds coincide with the shoreline location indicated by diatom assemblages.

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In order to investigate the correspondence between areal distributions of vegetation units and micro-landform units, vegetation is comprehended by physiognomy as units that have own form and area. A vegetation unit comprehended in this way is named a “vegetation patch”.
The study area is one of the third order stream's basins, about 0.45km² in area and about 180m in relative height, in the Takadate Hills situated in south of Sendai. This area is covered with secondary forest but not any afforestation area. Distribution of vegetation patches are compared with those of micro-landform units distinguished by form and topographic location and delineated by breaks of slopes. Woody plant composition of every vegetation patch differs from each other. Boundaries of vegetation patches coincide in many places with the breaks of slopes. This means that each vegetation patch is located on an own condition represented by soil profile, which is distributed in correspondence with micro-landform unit. As a result, landform, soil and vegetation show a catenary arrangement. However, the vegetation patch corresponding to the soil hydrologic environment and ground-surface stability of the crest slope and the upper sideslope is not spread in some cases on a lower part of upper sideslope. The fact indicates that more active surface processes occur on a lower part of upper sideslope than the rest of upper sideslope.

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This paper reviews studies of British internal migration since the 1980s. During the wide economic and political fluctuations of the era, the main themes had been: how migration responded to disequilibrium in local labour markets; how the British housing system related to labour immobility; and how different experiences of different socioeconomic groups affected the migration behaviour of each group.

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In this paper, the author discusses the change of local sea-level pressure system in Central Japan from January 18 to 21, 1991, by using the hourly observation data of sea-level pressure.
After the passage of synoptic-scale cyclone, at around 09 JST (Japan Standard Time) on 18, local low-pressure areas in the southeast of the mountainous areas in Central Japan are generated, where local cyclones are formed. On the evening of 18, a local high-pressure area in the northwest of the mountainous areas in Central Japan is generated, where the local anticyclone is formed.
From January 19 to 20, the local sea-level pressure system shows the diurnal change. Not only the nocturnal local anticyclone but also the daytime local cyclone are generated even in winter. That is, on the evening of 19, the local anticyclone centered at Takayama is generated. At around 06 JST on 20, it is most developed, but before noon it declines. Then the local cyclone centered at Matsumoto is generated and most developed at around 15 JST. On the evening of 20, the local anticyclone is again generated.
However, in spite of the daytime heating, the local cyclone is not immediately generated and developed. Thus the heating and cooling on the surface of Central Japan cannot merely cause this diurnal change.

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