• Journal of The Korean Society of Grassland and Forage Science
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• v.14 no.1
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• pp.57-63
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• 1994

We use a variety of methods to determine the optimum time for havesting corn for silage. In addition, adequate dry matter for silage must be considered along with maturity stage. The objective of this study was to evaluate using the kernel milk line to determine when to harvest com for silage in 1992 on the Livestock Experimental F m , Keiymung Junior College at Keongsan, Keongsangbukdo. Four hybrids were field grown and com plants were harvested at various stages of kernel development so that kemel milk line movement could be analyzed whilc the corn was in the premature stages. As the plants approached maturity, the ears were collected from each of the hybrids and the position of the milk line wa5 noted. Then the whole plants were chopped and the content of DM was determined. The milk line was a readily identifiable feature of maturing com kemels. We focused on the five development \tage\. The fint was "soft dough". The second was "dent". The third wa, "75% milk". and the fourth wa5 "half milk". The half milk occurs when the milk line is positioned falf way down the kemel face. and the final stages win "no milk", milk disappearance as indicators of physiological maturity in maix. Milk free stage of the kemel occurred from I to 3 days prior to black layer having developed. The range for harvesting com for silage occurs a kemels mature from 75% milk to no milk. Position of milk line was easy to see. and can be used as a visible indicator to determine com matunty stage\ and whole plant dry matter. Whole plant dry matter increased with advancing maturity. averaged over hybrids it was 24.1, 25.6. 28.5. 34.6 and 39.0% at soft dough, dent, 75% milk. half milk and no milk. Milk line was more usehl indicator in monitoring corn maturity prior to physiological maturity.ing corn maturity prior to physiological maturity.

• Journal of the Korean association of regional geographers
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• v.4 no.2
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• pp.49-64
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• 1998

Bing-gye valley(Kyongbuk Province, South Korea) is well known as a tourist attraction because of its meteorologic characteristics that show subzero temperature during midsummer. Also, there are some interesting geomorphic features in the valley area. Therefore, the valley is worth researching in geomorphology field. The aim of this paper is to achieve two purposes. These are to clarify geomorphic features on talus within Bing-gye valley area, and to infer the origin of Bing-gye valley. The main results are summarized as follows. 1) The formation of Bing-gye valley It would be possible to infer the following two ideas regarding the formation of Bing-gye valley. One is that the valley was formed by differential erosion of stream along fault line, and the other is that the rate of upheaval comparatively exceeded the rate of stream erosion. Especially, the latter may be associated with the fact that the width of the valley is much narrow. Judging that the fact the width of the valley is much narrow, compared with one of its upper or lower valley, it is inferred that Bing-gye valley is transverse valley. 2) The geomorphic features of talus (1) Pattern It seems to be true that the removal of matrix(finer materials) by the running water beneath the surface can result in partly collapse hollows. Taluses are tongue-shaped or cone-shaped in appearance. They are $120{\sim}200m$ in length, $30{\sim}40m$ in maximum width. and $32{\sim}33^{\circ}$ in mean slope gradient. The component blocks are mostly homogeneous in size and shape(angular), which reflect highly jointed free face produced by frost action under periglacial environment. (2) Origin On the basis of previous studies, the type of the talus is classified into rock fall talus. When considered in conjunction with the degrees of both weathering of blocks and hardness of blocks, it can be explained that the talus was formed under periglacial environment in pleistocene time. (3) The inner structure of block accumulation I recognize a three-layered structure in the talus as follows: (a) superficial layer; debris with openwork texture at the surface, 1.3m thick. (b) intermediate layer: small debris(about 5cm in diameter) with fine matrix(including humic soil), 70cm thick. (c) basal layer: over 2m beneath surface, almost pure soil horizon without debris (4) The stage of landform development Most of the blocks are now covered with lichen, and/or a mantle of weathering. It is believed that downslope movement by talus creep well explains the formation of concave slope of the talus. There is no evidence of present motion in the deposit. Judging from above-mentioned facts, the talus of this study area appears to be inactive and fossil landform.