<?xml version="1.0" encoding="UTF-8"?><xml><records><record><source-app name="Biblio" version="7.x">Drupal-Biblio</source-app><ref-type>17</ref-type><contributors><authors><author><style face="normal" font="default" size="100%">Ortiz, I.</style></author><author><style face="normal" font="default" size="100%">Simón, M.</style></author><author><style face="normal" font="default" size="100%">Dorronsoro, C.</style></author><author><style face="normal" font="default" size="100%">MartÄ±n, F.</style></author><author><style face="normal" font="default" size="100%">GarcÄ±a, I.</style></author></authors></contributors><titles><title><style face="normal" font="default" size="100%">Soil evolution over the Quaternary period in a Mediterranean climate (SE Spain)</style></title><secondary-title><style face="normal" font="default" size="100%">Catena</style></secondary-title></titles><keywords><keyword><style  face="normal" font="default" size="100%">Buried soils</style></keyword><keyword><style  face="normal" font="default" size="100%">climatic changes</style></keyword><keyword><style  face="normal" font="default" size="100%">Pleistocene</style></keyword><keyword><style  face="normal" font="default" size="100%">Relict soils</style></keyword><keyword><style  face="normal" font="default" size="100%">Soil development</style></keyword></keywords><dates><year><style  face="normal" font="default" size="100%">2002</style></year><pub-dates><date><style  face="normal" font="default" size="100%">2002///</style></date></pub-dates></dates><urls><web-urls><url><style face="normal" font="default" size="100%">http://www.sciencedirect.com/science/article/pii/S0341816201001941</style></url></web-urls></urls><volume><style face="normal" font="default" size="100%">48</style></volume><pages><style face="normal" font="default" size="100%">131 - 148</style></pages><language><style face="normal" font="default" size="100%">eng</style></language><abstract><style face="normal" font="default" size="100%">Palaeosols in the Granada Basin (SE Spain) have been studied in two different situations: surface soils on geomorphically stable surfaces since the Early Pleistocene with younger pedogenic overprinting and buried soils on unstable surfaces from the Middle –Late Pleistocene on which successive erosional – depositional episodes have alternated with pedogenic episodes. For each soil clay and iron accumulation indices, the Fet + Al t /Si t ratio, clay mineralogy and micromorphological features were used to estimate the degree of soil development. From the Early to the early Late Pleistocene, the main pedogenic processes were the leaching of carbonates, weathering, illuviation and rubification, which resulted in Bt horizons with red colours, clay texture, clay coatings and kaolinite neoformation. The degree of weathering and the development of these Bt horizons varied over time, and the soils that formed on the surfaces from the Early Pleistocene show strongest weathering and development. However, after their formation, there were periods in which they were partially truncated and recalcified, resulting in polygenetic soils. The different degrees of development of the buried soils during the last 474,000 years indicate that the wettest warm period was stage 7 and the driest, stage 5. Stages 9 and 11 must have had climates with intermediate wetness. Since the clay accumulation and iron oxide accumulation indices, the differences in Fet + Al t /Si t ratio between Bt and C horizons, the extent of kaolinite neoformation and the micromorphological features of the soils formed during stage 7 are all similar to the surface soils that formed on Early Pleistocene deposits, these features cannot be used to date surfaces older than 242,000 BP. By contrast, the soils that formed during stage 7 and later periods show different extents of development and thus can be used for the approximate dating of landforms.</style></abstract></record><record><source-app name="Biblio" version="7.x">Drupal-Biblio</source-app><ref-type>17</ref-type><contributors><authors><author><style face="normal" font="default" size="100%">Ortiz, I</style></author><author><style face="normal" font="default" size="100%">Simón, M</style></author><author><style face="normal" font="default" size="100%">Dorronsoro, C</style></author><author><style face="normal" font="default" size="100%">MartÄ±n, F</style></author><author><style face="normal" font="default" size="100%">GarcÄ±a, I</style></author></authors></contributors><titles><title><style face="normal" font="default" size="100%">Soil evolution over the Quaternary period in a Mediterranean climate (SE Spain)</style></title><secondary-title><style face="normal" font="default" size="100%">Catena</style></secondary-title></titles><keywords><keyword><style  face="normal" font="default" size="100%">Buried soils</style></keyword><keyword><style  face="normal" font="default" size="100%">climatic changes</style></keyword><keyword><style  face="normal" font="default" size="100%">Pleistocene</style></keyword><keyword><style  face="normal" font="default" size="100%">Relict soils</style></keyword><keyword><style  face="normal" font="default" size="100%">Soil development</style></keyword></keywords><dates><year><style  face="normal" font="default" size="100%">2002</style></year></dates><volume><style face="normal" font="default" size="100%">48</style></volume><pages><style face="normal" font="default" size="100%">131-148</style></pages><language><style face="normal" font="default" size="100%">eng</style></language><abstract><style face="normal" font="default" size="100%">Palaeosols in the Granada Basin (SE Spain) have been studied in two different situations: surface soils on geomorphically stable surfaces since the Early Pleistocene with younger pedogenic overprinting and buried soils on unstable surfaces from the Middle –Late Pleistocene on which successive erosional – depositional episodes have alternated with pedogenic episodes. For each soil clay and iron accumulation indices, the Fet + Al t /Si t ratio, clay mineralogy and micromorphological features were used to estimate the degree of soil development. From the Early to the early Late Pleistocene, the main pedogenic processes were the leaching of carbonates, weathering, illuviation and rubification, which resulted in Bt horizons with red colours, clay texture, clay coatings and kaolinite neoformation. The degree of weathering and the development of these Bt horizons varied over time, and the soils that formed on the surfaces from the Early Pleistocene show strongest weathering and development. However, after their formation, there were periods in which they were partially truncated and recalcified, resulting in polygenetic soils. The different degrees of development of the buried soils during the last 474,000 years indicate that the wettest warm period was stage 7 and the driest, stage 5. Stages 9 and 11 must have had climates with intermediate wetness. Since the clay accumulation and iron oxide accumulation indices, the differences in Fet + Al t /Si t ratio between Bt and C horizons, the extent of kaolinite neoformation and the micromorphological features of the soils formed during stage 7 are all similar to the surface soils that formed on Early Pleistocene deposits, these features cannot be used to date surfaces older than 242,000 BP. By contrast, the soils that formed during stage 7 and later periods show different extents of development and thus can be used for the approximate dating of landforms.</style></abstract></record><record><source-app name="Biblio" version="7.x">Drupal-Biblio</source-app><ref-type>17</ref-type><contributors><authors><author><style face="normal" font="default" size="100%">Wijmstra, T A</style></author></authors></contributors><titles><title><style face="normal" font="default" size="100%">The place of the Tenagi Philippon in the Pleistocene stratigraphical sequence</style></title><secondary-title><style face="normal" font="default" size="100%">Zeitschrift der Deutschen Geologischen Gesellschaft</style></secondary-title></titles><keywords><keyword><style  face="normal" font="default" size="100%">climatology Greece (Macedonia)</style></keyword><keyword><style  face="normal" font="default" size="100%">Flora</style></keyword><keyword><style  face="normal" font="default" size="100%">Pleistocene</style></keyword><keyword><style  face="normal" font="default" size="100%">prairie-zone</style></keyword></keywords><dates><year><style  face="normal" font="default" size="100%">1972</style></year></dates><publisher><style face="normal" font="default" size="100%">Schweizerbart'sche Verlagsbuchhandlung</style></publisher><pub-location><style face="normal" font="default" size="100%">Stuttgart</style></pub-location><volume><style face="normal" font="default" size="100%">123</style></volume><pages><style face="normal" font="default" size="100%">565-566</style></pages><language><style face="normal" font="default" size="100%">eng</style></language><abstract><style face="normal" font="default" size="100%">From an analysis of a 120 m section in Eastern Macedonia a sequence steppe and forest phases became evident. By C14 analysis it could be proved that during the stadial phases within the Weichselian an open Artemisia-Chenopodiaceae steppe existed in the area. On the other hand during the interstadials, shrub steppe phases in which pine and oak were present, existed in the area. During the interglacials forest was found. In these forests a Carpinus-Ulmus belt was succeeded by a Pinus nigra-Abies zone. In this zone the presence of Ericaceae is of importance (WIJMSTRA 1969). It became also clear from the analysis of this section that the glacial phases were equally long, but in each glacial the development of the Vegetation sequence and consequently of the climate was different. It was possible to establish the position of the Holstein interglacial either at a depth between 78 and 70 m or between 62 and 62.5 m. In this interglacial the presence of Pterocorya is worth mentioning, also Buxus and Myrtus were found in this interval. In the first phase between 87 and 105 m a series of three humid zones existed. In these zones Carpinus and Ulmus were important constituents of the Vegetation. These zones were found separated by long dry periods when the forest was dominated by Pinus nigra, Pinus heldreichii and evergreen oaks from the group Quercus ilex/coccifera. In this dry type of forest frequently naturally buming lead to open places. On these open places at first an Artemisia-Chenopodiaceae Vegetation was present.</style></abstract></record></records></xml>