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IN KAHRAMANMARAS PROVINCE, TURKEY Recep Gündoğan, Kadir Yılmaz Sutcu Imam University, Faculty of Agriculture, Department of Soil Science, Kahramanmaras, Turkey ABSTRACT Morphological, and selected physical and chemical properties of five pedons on four landscape positions (summit, shoulder, backslope, and toeslope) were examined to evaluate the effect of landscape position and parent material on soil properties. Parent material of soils on summit and shoulder was Upper Miocene formation consist of marl, sandy and conglomeratic layers rich in carbonate. Soils on the backslope and toeslope developed on non-calcareous Pliocene mixed deposits. The soil on the marl layer had 10 YR hue and loamy clay texture, massive structure and vertic features. Soils on sandy and conglomeratic layers had 7.5YR hue, weak-to-moderate granular or subangular structure. The soil on the backslope had clayey-skeletal, 5 YR hue and medium-to- coarse subangular structure. The soils on the toeslope had 7.5 YR hue, clay texture and vertic features. pH values ranged 6.8-7.86 and the soil on the backslope had the lowest pH value. Soil properties such as soil color and texture were influenced parent material and landscape positions. INTRODUCTION Hillslopes are classified into summit, shoulder, backslope, footslope and toeslope (Ruhe,1975).These landscape positions can greatly influence hydrological, and pedological processes (Hall,1983). The effects of topography on pedogenesis have been known for a long time and soil-landscape relationships have been widely used to study soil genesis (Jenny,1941; Birkeland,1984; Fanning and Fanning,1989; Hall and Olson,1991). Walker et al.(1968) reported that backslope soils were most affected by erosion and footslope soils showed higher clay and organic matter content. Malo et al. (1974), and Ovalles and Collins (1986) stated that there was significant relations between landscape positions and soil properties. Soil-landscape relationships could often be hidden by parent material ( Stolt et al.,1993). The knowledge of the degree of parent material uniformity is essential in pedogenesis studies. Parent material unconformities were attributed to the stratification in parent rocks resulting in variability in particle size or mineralogy, or to litologic discontinuities resulting from colluvial, alluvial or eolian additions (Brewer,1976). The objective of this study was to determine the effects of topography and parent material on soil properties. This approach was successfully used in determining uniform mapping units for soil survey (Brigss and Shishira,1975) and for soil management and soil productivity determinations (Chartres,1982; Stone et al, 1985). MATERIALS AND METHODS Site Description : The study site is located in Kahramanmaraş Province, Turkey, approximately 15 km west of Kahramanmaras city. Five representative pedons were selected to study from four different landscape positions: i) summit, ii) shoulder iii) backslope, and iv) toeslope. Morphological characteristics of soil profiles were identified using the Soil Survey Staff (1993). Geology of the study area consists of Upper Miocene-age clay, sand and conglomerate layers covered with various depths of non-calcareous Pliocene-age mantle. Upper Miocene layers exposed at the faults edge because they were uplifted and inclined with 12-14° angle by tectonic (Önalan,1986, Gül,1987). Therefore, tectonic plays a significant role in current morphology of the study area. Climate in the study area is characterized by dry and hot summers and warm and wet winters. The annual average precipitation is 710 mm. Monthly mean temperature ranges from -2 °C in January to 17 °C in July, with mean annual value of 8 °C (Kaya,1996). Soil moisture regime is xeric and soil temperature regime is thermic (Tigem,1991). Soils were classified as Inceptisol and Vertisol (Gündogan et al., 1998). Laboratory Methods : Soil samples were air dried and passed through a 2-mm sieve. Particle size distribution was determined by Bouyoucos hydrometer method (Bouyoucos,1962). Soil pH was measured in saturated samples (Richards,1954). Organic C was determined by Walkley-Black wet oxidation method (Allison,1965). Carbonate content was determined by using Shiebler calcimeter method (Allison and Moodie,1965). RESULTS AND DISCUSSIONS Morphological properties : The soils (P1, P2) on the summit, and P3 on the shoulder developed from Upper Miocene deposits rich in carbonate. These deposits consist of marl, sandy and conglomeratic layers. P4 and P5 pedons are described on the backslope and toeslope respectively, and developed from non-calcareous Pliocene mixed deposits. A summary of morphological properties of soils is listed in table 1. Soil depth varies from 45 cm to 110 cm. P2, P3 and P4 pedons have weak-to-moderate granular or subangular structure. Structure of P4 pedon is much stronger than that of the other pedons. The effect of parent material on structure and solum depth is more than the effect of landscape position. Structure has not developed in P1 and P5 pedons. The soil have cracks. While P1 pedon have 10 YR hue, P2 and P3 pedons 7.5 YR hue, oxidizing and well drained condition prevail in these pedons du to their coarse texture. P4 and P5 pedons on the backslope and toeslope have 5YR or 7.5 YR respectively, and lower value (<4) and chroma (>3). Similar colour pattern observed in a Entisol-Alfisol-Vertisol catena by weitkamp et al.(1996).They conclude that the movement Fe is restricted its low solubility and remained in profile, the greater solubility of Mn leads to its removal from upper slope sites and its subsequent transport to lower slope soils. There are common pebbles and cobbles on the surface and within profile in the P3 and P4 pedons which is due to the movement of fine particles from upslope to downslope by erosion. Many researchers reported that upper slopes were affected from erosion (Walker et al., 1968; Birkeland,1984;Deniel et al. 1985).  Physical and Chemical Properties : Physical and chemical properties of soils are given in table 2. Soil textures vary from sandy loam to clay. Clay increase in P1 pedon located on the summit is related to the marl layer of Upper Miocene formation. P4 pedon has less clay content than P5 pedon due to transportation of fine particles from backslope to toeslope. Soil pH values range from 6.87 to 7.86 and P4 pedon has the lowest pH value probably due to the parent material that derived from quartzite. Organic matter content ranges from 2.12 % to 0.06 % and decreases with depth in all pedons. The increase in carbonate content with depth in P1, P2 and P3 pedons is associated with the carbonate leaching. Lesser amount of carbonate in P4 and P5 pedons could be related to capillary rise and movement by runoff from upslope to downslope. Harper (1957) and Glinka (1963) had explained carbonate accumulation by capillary rise as well in their study.  CONCLUSIONS The soils formed on the Upper Miocene deposits are rich in carbonate and the soils formed on Pliocene deposits are non-calcareous. The soils on the summit and shoulder formed on the Upper Miocene deposits are rich in carbonate and have 10 YR or 7.5 YR hue. Soils formed on the marl layer had lower value and finer texture than that of the other soils formed sandy and conglameratic layer. Soils on the backslope and toeslope formed on non-calcareous deposits have 5 YR or 7.5 YR hue. Fine particles translocated by water from upslope to downslope, therefore, backslope soils had less clay content and coarser particles compared to toeslope soils. The findings of this study proved that the distribution of soil properties varies as a function of parent material and landscape position. However, parent material was dominant on the soil properties compared to landscape position. REFERENCES Allison L.E., Moodie C.D. (1965). Carbonate:Volumetric Calcimeter Method. In C. A, Black (ed), Methods of Analysis. Agronomy Monographs No: 9, Part 2. American Society Agronomy, Madison, Wisconsin, USA., p 1389-1392. Allison L.E. (1965). Organic Carbon: Walkley-Black Method. In C. A, Black (ed), Methods of Analysis. Agronomy Monographs No: 9, Part 2. American Society Agronomy, Madison, Wisconsin, USA., p 1367-1378. Birkeland P.W. (1984). Soils and Geomorphology. Oxford University Press, New York, p. 372. Bouyoucos G.J., (1962). Hydrometer Method Improved For Making Particle Size Analyses of Soils, Agron. Jour., 54, 464-465. Brewer R. (1976). Fabric and mineral analysis. Chapter 4: calculation soil formation. Krieger Publ., New York. Briggs D.J., Shishira E.K. (1975). Soil Variability in geomorphologically defined survey units in the Albudeite of Murcia Province, Spain. Catena suppl. 6: 69-84. Chartres C.J. (1982). The use of landform-soil associations in irrigation soil surveys in Northern Nigeria. J. Soil Sci. 33:317-328. Deniels R.B., Giliam J.W., Cassel D.K. and Nelson L.A. (1985). Soil erosion class and landscape position in the North Caroline Piedmont. Soil Sci. Soc. Am. J. 49: 1991-995. Glinka K.D. (1963). Treatise on soil science (translated from the Russian). Israel Program for Scientific Translations, Jerusalem. Gül M.A. (1987) Kahramanmaras Yöresinin Jeolojisi ve Petrol Olanaklari, TPAO Rapor No:2359, Ankara. Gündoğan R., Yılmaz K., Gürel N., Bodur M. N., Demirkıran A. R., Köksal İ., Şerbetç H. (1998). KSÜ. Afşar Kampusu Topraklarının Etüd ve Haritalaması, KSÜ Araştırma Fonu Projesi (Yayınlanmamış), Kahramanmaras. Hall G.F.(1983). Pedology and Geomorphology. In : L.P. Wilding, N.E. Smeck, and G.F. Hall (Eds.). Pedogenesis and Soil Taxonomy. I. Concepts and Interactions. Elsevier, Amsterdam. Hall G. F., Olson C.G. (1991). Predicting Variability of soils from landscape models. (In Spatial variabilities of soils and landforms, ed. Mauhaach, M.J., and Wilding, L. P.), SSSA Special Publication Number :28, p. 9-24. Harper W.G. (1957). Morphology and genesis of Calsisols. Soil Sci. Soc. Am. Proc. 21: 40-424. Janny H.(1941). Factors of soil formation, McGraw-Hill, New York,281 p. Kaya, F. (1996). Kahramanmaraş Ilinin Iklim Özellikleri, Yüksek Lisans Tezi (Basılmamıs), K.S.U. Sosyal Bilimler Enstitüsü, Kahramanmaraş, 144 s. Malo D.D.,. Worcester B.K, Cassel D.K., Matzdorf K.D. (1974). Soil-landscape relationships in a closed drainage system., Soil Sci.Soc. A m. Proc. 38:813-817. 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Effect of erosion and landscape position on the productivity of Piedmont soil. Soil Sci. Soc. Am. J. 49: 987-991. Walker P. H., Hall G.F., Protz R. (1968). Soil trends and variability across selected landscapes in Iowa. Soil Sci. Soc. Am. Proc. 32: 987-991. Weitkamp W.A, Graham R.C, Anderson M.A., Amrhein C. (1996). Pedogenesis of a vernal pool Entisol-Alfisol-Vertisol catena in southern California. Soil Sci. Soc. Am. J. 60: 316-323. |