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Kadir Yılmaz, Recep Gündoğan, Ali Rıza Demirkıran Kahramanmaraş Sütçü Imam University, Faculty of Agriculture, Department of Soil Science, Kahramanmaras-Turkiye ABSTRACT Kahramanmaraş province, Turkey, has significantly variability in climate, vegetation, topography, and parent material type. Different combinations of soil formation factors have been observed in the study area. This study was conducted to characterise soils widely found in Kahramanmaraş and classify them according to criteria in Soil Taxonomy. pH values ranged from 7.06 to 8.33. Cation exchange capacity (CEC) of soils ranged from 20 to 180 cmol kg-1 and base saturation were very high. Carbonate content increased with depth and reached to 50 % in some profiles. Smectite was dominant clay mineral and followed by illite, kaolinite, paligorskite and vermikulite respectively. Pedogenesis of soils had been affected by parent material, climate and topography. The soils were classified as Typic Haplocambid, Typic Humaquept, Typic Haplargid, Vertic Haploxerept, Aridic Haploxeroll, Typic Petrocalcid, Lithic Haploxeralf, Aquic Haploxerert, Typic Haplohemist and Mollic Xerofluvent according to the Soil Taxonomy. INTRODUCTION Kahramanmaraş Province is located in the East Mediterranean Region of Turkey. Mediterranean and Continental climate conditions are dominated. Landscape is characterised by steep bedrock hills and cliffs of limestone, sandstone and metamorphic rocks, and nearly level depression plains (Pamir and Tolun, 1968). Soils are classified as Red-Mediterranean, Red-Brown-Mediterranean, Brown, Red-Brown, Non-Calcareous-Brown, Brown-Forest, Non-Calcareous-Brown-Forest, Chestnut, Alluvial, Colluvial and Organic great soil groups according to modified system of Baldwin et al. (1938). Red-Mediterranean and Red-Brown-Mediterranean soils developed on limestone and conglomerate. These soils were rich in carbonate and had 2.5 YR and 5 YR hue. While Chestnut soils occurred on upland, Brown and Red-Brown soils occurred on the lowland of northern area. These soils had 7.5 YR and 10 YR hue and high carbonate content. Non-Calcareous-Brown and Non-Calcareous-Brown-Forest soils formed over non-calcareous parent materials on upland had reddish B horizon due to Fe-rich illuvial clay and sesquioxides. Alluvial and Colluvial soils occurred in the depression plains of the southern and northern study areas and narrow valleys (Topraksu, 1973). Organic soils developed on the muck at local depression in the southern region (Tigem, 1991). The soils on the study area were not entirely classified according to Soil Taxonomy as well as other provinces of Turkiye. Some researchers such as Senol and Dinç (1986), Durak (1989), Ekinci (1990) and Cangir and Ekinci (1995) studied to classify the great soil groups in some regions of Turkiye. The purpose of this study was (i) to determine some physical, chemical and mineralogical properties of soil pedons representing great soil groups in Kahramanmaraş Province, (ii) to classify them according to Soil Taxonomy (Soil Survey Staff, 1998) and (iii) to describe and evaluate genesis of soils, in these semi-arid and arid regions of Turkiye. MATERIALS and METHODS Kahramanmaraş is located in the East Mediterranean of Turkey. It lies between 370 11' and 380 36' North, and between 360 15 and 370 42' East and covers about 1450 km2. The area is generally hilly, and elevation ranges 450 to 3081 m above mean sea level (msl). The study area has two climatic regions: The Continental and Mediterranean Climate Regions. The Continental climate region has been dominate in northern area with monthly mean temperature ranges from -0.4 Co in December to 23 Co in July, with mean annual value of 10.3 Co. The average annual precipitation is about 386 mm. The southern area has Mediterranean climate. The total annual precipitation is about 710 mm, most of this occurs in winter, December through April. The mean annual temperature is 16.5 oC, and monthly mean temperature ranges from 4.5 oC in January to 28 oC in August (Kaya, 1996). The soils in the northern area has mesic soil temperature and aridic moisture regime. The soils on the central and the southern area have thermic temperature regime and xeric moisture regime. Aquic moisture regime appears in the local depression area in the southern area (Tigem, 1991). Geology of study area consists of metamorphic and sedimentary rocks including schist, serpentine, limestone, sandstone, marl, conglomerate, and alluvial and colluvial deposits. There are locally found basalt rocks in the study area. Maquis and coniferous forests are dominant vegetation including pinus, cedrus abiece essp. But quercous and juniperus can also be found especially in the northern region. The plains and uplands in the southern and northern regions are mainly consisted of cultivated farmlands. METHODS Thirteen pedons were selected for characterisation that represent each great soil group in Kahramanmaraş Province. All soil pedons were described and sampled according to standard procedures (Soil Survey Staff, 1993). Soil samples were air dried, crushed, sieved through 2-mm sieve, and reserved for subsequent analysis. Particle size distributions were determined by hydrometer method (Bouyoucus, 1951). pH was determined with glass electrode in saturated soil after 4-h equilibration period. Electrical conductivity were measured in saturated samples (Richards, 1954). Exchangeable cations were extracted from the soil by 1N amonium acetate at pH 7.0, and than extractions were analysed by an atomic absorption spectroscopy (Jackson, 1969). Cation exchange capacity (CEC) was determined by the amonium saturation method at pH 7.0 (Soil Survey Staff, 1993). Organic carbon was determined by Walky-Black wet oxidation method (Allison, 1965). The total carbonate contents were measured using scheibler calcimeter (Allison and Moodie, 1965). Clay samples (<2 um) selected from surface and subsurface horizons were treated with Citrate Bicarbonate Ditionite (CBD) to remove free oxides and prepared for XRD analysis using the method described by Jackson (1969). Clay fractions were saturated with K and Mg and than clay minerals were identified using X-Ray diffractometer (XRD). Soils were classified according to Soil Taxonomy (Soil Survey Staff, 1998). RESULTS and DISCUSSION Soil Morphology, and Physical and Chemical Properties : The classification and landscape positions of soils studied are showed in Table 1. Cambic horizon and ochric epipedon are commonly found in the studied pedons. Argillic horizon, mollic and histic epipedons are rarely found. Petrocalcic horizons were found especially in the northern area. The main pedogenic processes were calcification, clay illuviation, transfomation such as clay formation and soil colours, and petrocalcic horizon formation. Vertic and redoximorphic features were observed in some pedons. Table 2 shows the morphologic characteristics of soils. All pedons have slightly alkaline reaction, pH 7.1-8.3, and very high base saturation. The organic matter contents were found between 0.20 and 3.48 % in the soils formed on inorganic parent materials. Organic matter contents in Histosol were reached to 66.81 %. (Table 3). Entisols, P13, developed from alluvial sediments. Colours were 10 YR hue. Entisols had very weak, fine, granular in the surface, and massive or single grain in the subsurface horizon. Textures varied from loam to clay. Organic mater content varied between 0.93 and 0.15 % and irregularly distributed within profile. This is associated with sediment stratigraphy. CEC ranged from 25.4 to 34.8 cmol kg-1. Inceptisols developed from coluvium, basalt and limestone (P2, P4 and P12), Colours varied from 2.5 YR and 7.5 YR hues, related sesquioxids accumulation. P2 had 2.5 Y hue, associated with perched water. Soils had moderate, medium granular or subangular blocky structure in surface horizons and weak, coarse blocky or moderate, medium subangular blocky structure in subsurface horizons. All pedons had high clay content. Many researchers reported that soils on the limestone and basalt rocks Southern Turkey, had fine textures (Ergene, 1963; Topraksu, 1973; Kapur et al., 1986; Senol and Dinç, 1986). But only P4 and P12 had vertic features. Because smectite is dominate in these soils (Table 4). Mollisol developed from mica schist (P5) had sandy loam texture. Colour was 2.5 Y hue, and related to the parent material Structure was weak, fine granular in surface horizons and structurless in C horizons.  P1, P3, P6, P7 and P8 classified as Aridisols. P3 pedon developed on the serpentine had 2.5 Y hue. P1, P6 and P7 pedons developed on the marl had 10 YR hues. P8 pedons developed on the limestone had 5 YR hue. Soil colours related to clay content of parent material. Because higher clay content in the parent material decreased oxidation. Many researchers reported that soils formed on the limestone or conglomerate more redder than one on the marl in the arid and semi arid region of Turkiye (Akalan, 1963; Topraksu, 1973; Köy Hizmetleri, 1990 ). P3 had argillic horizon, P6 and P8 had petrocalcic horizon and other pedons had cambic horizon as diagnostic horizons. Clay illuviation in P3 and formation of petrocalcic horizon in P6 and P8 are not associated with the present climatic conditions (Fanning and Fanning, 1989; Kapur et al. 1990; Sancho et al., 1992; Atalay, 1996). In general, they had moderate, medium granular structure in surface horizons, moderate medium or fine subangular blocky in subsurface horizons. Pedon 9 developed over shale classified as an Alfisol. The soil colour was not changing through profile and was 2.5 Y hue. Clay content is increasing thorough the soil profile, and while it is 16.8 % in the Ap horizon, clay content reaches to 22.8 % in the Bt horizon (8 cm to 19 cm). Field observations (clay coatings on ped surfaces and around pores) and clay increase was sufficient for argillic horizon definition. Coarse and medium texture of this profile helped clay illuviation (Fanning and Fanning, 1989). Bt and BC horizons had moderate medium subangular blocky structure and A horizon had weak fine platy structure. Vertisol (P10) pedon ranged from 64.7 %to 85.0 %. The soil had massive structure. The shrinking and swelling of clay minerals accompanying drying and wetting cycles, will not allow to form a stable structure. The rupture and slippage of soil masses in the diagonal directions as a result of the great swelling pressures developed in these soils when the are wetted causes structure disturbance (Fanning and Fanning, 1989; Buol et al. 1997). Matrix colour was 5 Y hue, and very low chroma (<2). Low chroma is related to poor drainage conditions. This soil also had 0.15 % total salt in depth between 25 cm and 150 cm. Histosol (P11) pedons are found locally in the study area. These soils have high organic matter content. This soil had sligthly alkaline reaction, about pH 7.6. CEC varied from 92.9 to 182.7 cmol kg-1 and base saturation was high. Organic mater characteristic resulted in these properties. Organic matter had eutropic characteristic, associated with environment condition in where they had developed (Dinç et al., 1993).  Clay Mineralogy : Many researchers reported that smectite is the dominant silicate mineral in arid and semi arid region of Turkey (Ergene, 1963; Gülçur, 1964; Gürel,1985; Kapur et al., 1991). These similar results were found in this study. According to X-ray diffraction analysis (Table 4), smectite is the dominant silicate minerals in the soils (P1, P3, P4, P9, P10, P12) and illite occurs as the second dominant clay mineral in these soils (P2, P5). In addition, the soil samples have given peaks that indicative of paligorskite, kaolinite and vermiculite. The other pedons have smectite, illite, kaolinite, paligoskite and vermiculite in the same propotions P6, P7, P8 and P11) CONCLUSIONS Soils in Kahramanmaras Province show that pedogenic processes are strongly depending on the parent materials and the climatic conditions. Especially, there were significantly relation between soil colours and parent materials. While soils derived from marl had 10 YR hue, other parent material rich in carbonate such as limestone and conglomerate had 5 YR or 7.5 YR hue. The leaching of carbonate and clay in the central and southern province were more than elsevere. Argillic horizon and petrocalcic horizon formation was not related with the present arid climate conditions on the northern province. Topography was an important factor in pedogenesis. The profiles which were formed on slopy areas were influenced by moderate and severe erosion. Therefore, these soils had very shallow soil depths. The soils which formed on depression topography had insufficient drainage and salinity problems. While smectite is the dominant silicate minerals, illite occurs as the second dominant clay mineral in these soils. Soils had vertic features associated with smectite clay mineral.   ACKNOWLEDGEMENTS The authors thank İsmet KÖKSAL and Asuman NALBANTOĞLU for help with laboratory studies. REFERENCES Akalan İ. (1963). 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