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CONCEPTS AND MORPHOLOGY OF HYDROMORPHISM IN SOILS Stahr K. The concept of gleysation related with the influence of groundwater is as old as modern soil science. However, soon it was evident, that a simple uniform concept will not be able to explain all morphological features that appear with hydromorphism or reductomorphism. Therefore Kubiena in his visionary approach for a natural soil system in Central Europe used the water regime for the subdivision of soils at the highest level. He separated submerged soils under the influence of full time or part time flooding from the semiterrestric or ground water influenced soils and the most important division of terrestrial soils. Within the terrestrial soils, he included soils with stagnant meteoric water. The later decision caused many problems and was criticized by quite a few scientists. However, the modern approach for example by WRB combining gleyic and stagnic properties, does cause even more confusion and hinders the separation of two major different groups of pedogenic processes. Using iron and manganese oxides as colouring and diagnostic features, it was elaborated, that with ground water influence these oxides are generally precipitated on the walls of macropores that is on the external site of aggregates. On the other hand, stagnant water pushes the same oxides into the internal matrix of the aggregates, resulting in mottling and the formation of concretions. This concept is world-wide applicable, however it has its limits. One limit, which has also significant ecological consequences, is the wet or reduction bleaching, which may occur with ground water in the subsoil or with stagnant water in the topsoil and results in the export of the iron and manganese compounds from the whole horizon or even the soils. Other limitations do occur in the morphology, if very sandy or heavy clay texture is present or under saline, carbonatic or sulfidic conditions. For all these conditions, the concept has to be modified, if not totally reassessed. There are at least two more cases, which have to be taken into account, when hydromorphism/ reductomorphism should be covered by soil science in full. The one case existing mainly in lowland situation is the overlapping of ground water influence from below and stagnant water from above. In those cases often an impermeable soil layer or soil horizon separates those regimes, but at least is semi-permeable allowing to combine the features. Another very complicated situation is envisaged, if stagnant or ground water influence is combined in sloping areas with a dominant lateral water flow and consequently the expression of morphological features along the slope more than within the profile. These approaches will be discussed systematically in the forthcoming paper. 140
HYDROPHYSICAL CHARACTERISTICS OF POROUS BODY AS IN- PUT DATA FOR WATER TRANSPORT MODELS Walczak R. T., Sławiński C., Witkowska-Walczak B. ABSTRACT The water retention, saturated and unsaturated hydraulic conductivity coefficients are the basic hydrophysical characteristics of the soil. The correct determination of those characteristics is indispensable to obtain the required accuracy of the used models of water transport in soil profile. Therefore, the methods of measurement and estimation of these characteristics are extensively developed. DETERMINATION OF STATIC WATER RETENTION CURVE The dependence between soil water potential and soil water content, called the soil water retention curve (Fig.1), is a basic hydrophysical soil property. The static soil water retention curve is determined in Richards chambers or on the sandygypsum blocks. It is determined for the state of thermodynamic equilibrium which is obtained after the specific time. 2 1 Fig. 1. An exemplary of static water retention curve for loamy (1) and sandy (2) soils. DETERMINATION OF HYDRAULIC CONDUCTIVITY COEFFICIENT AND DYNAMIC RETENTION CURVE Unsaturated hydraulic conductivity is one of the most important physical soil characteristics. Applying TDR techniques [2, 3, 6] and the instantaneous profile method (IPM) the measurement of hydraulic conductivity coefficient k(ψ) and also dynamic retention curve θ(ψ) has become much faster and effective. It was demonstrated, that this method gives accurate results for various initial and boundary 141
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Jan Gliński, Grzegorz Józefaciuk,
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CONTENTS PART A: GAS EXCHANGE Revie
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SOIL - PLANT - ATMOSPHERE AERATION
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In single observations, rates of N
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than in the night while CH 4 uptake
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Pumpanen et al. (2003b) measured wi
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5. Liikanen A 2002. Greenhouse gas
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EFFECT OF SOIL TILLAGE AND COMPACTI
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Cumulative CO 2 (kg C ha -1 ) 600 F
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Soil depth (mm) 0 20 40 60 80 Diffu
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METHANE Main suppliers to the atmos
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3. Emission of N 2 O is higher from
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30. Kusa, K., Sawamoto, T., Hatano,
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GAS EMISSION FROM WETLANDS Stępnie
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ater retention capacity in the chan
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zone, while in Nadrybie lake the le
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Eh 350 300 250 mV 200 150 100 50 0
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Table 1. Sources and sinks of atmos
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Fig. 1. Quasi - equilibrium methane
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Fig. 5. Concentration of nitrous ox
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drooxygenology, such subbranches as
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Fig. 3. Soil microbial respiration
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NITROUS OXIDE EMISSION FROM SOILS W
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N2O-N [mg kg -1 ] 100 80 60 40 20 0
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7. McKenney, D.J., C.F. Drury, and
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AERATION STATUS OF SOIL AND ENZYME
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Catalase is heme-containing enzyme
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8. Deng S., Dick R. Sulfur oxidatio
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The number of profiles representing
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tics (Stępniewski et al., in press
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MICROBIAL ECOLOGY OF SOIL POROUS ME
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The bulk of non-rhizosphere soil is
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RELATIONS The relations between soi
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23. Mamilov A.Sh., Byzov, B.A. Zvya
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silts. The content of C org in the
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Table 2. Continued Location Day of
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5 o C Eh (mV 400 300 200 100 1A 1B
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STRUCTURE FORMATION AND ITS CONSEQU
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when water content differences are
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authors stated that O 2 gradients i
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strength of the already existing st
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source of transforming DNA for Acin
Page 86 and 87: THE BIOCHEMISTRY OF THE RHIZOSPHERE
Page 88 and 89: der field conditions r-strategists
Page 90 and 91: 22. Tarafdar JC and Jungk A 1987. P
Page 92 and 93: ics behavior have been published (K
Page 94 and 95: Activity of dehydrogenase (DHA) was
Page 96 and 97: The rather small concentration of A
Page 98 and 99: The effect of the pesticide dosage
Page 100 and 101: METHANOTROPHIC ACTIVITY OF COAL MIN
Page 102 and 103: GC TESTS Air-tight bottles (60 ml)
Page 104 and 105: dumping. For older rock samples, af
Page 106 and 107: SOIL - PLANT - ATMOSPHERE AERATION
Page 108 and 109: - properties of plant surface and c
Page 110 and 111: mination, should be considered.The
Page 112 and 113: Considering a possibility of detect
Page 114 and 115: SURFACE PROPERTIES OF SOILS AND THE
Page 116 and 117: clay content the latter processes p
Page 118 and 119: der alkaline treatment the silica o
Page 120 and 121: COMPACTION EFFECTS ON SOIL PHYSICAL
Page 122 and 123: suming and expensive regression-bas
Page 124 and 125: CROP RESPONSE Roots A characteristi
Page 126 and 127: CONCLUSIONS Alterations in the aggr
Page 128 and 129: 27. Keller, T., Arvidsson, J., Dawi
Page 130 and 131: MONITORING OF POROUS MEDIA PROCESSE
Page 132 and 133: - temperature: semiconductor, therm
Page 134 and 135: This is the reason why the optimisa
Page 138 and 139: conditions applied to the soil samp
Page 140 and 141: ESTIMATION OF THE HYDROPHYSICAL CHA
Page 142 and 143: Fig. 6. Scheme of EURO-ACCESS-II mo
Page 144 and 145: The experimental field is located a
Page 146: Nannipieri Paolo Ostrowska Aneta Os
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