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In present investigation the quartz surface grain micromorphology was studied on the 0.25-0.5 mm sand fraction. The complex of 13 quartz surface microtextures of mechanical and chemical origin was observed, which had been described previously in many studies (Krinsley, Doornkamp, 1973; Higgs, 1979). They are, angular and rounded outlines, conchoidal fractures, straight steps, fracture plates, parallel striations, straight and curved scratches and grooves, V-shaped indentations, upturned plates, oriented etch pits, adhering particles, solution pits and crevasses (Alekseeva, 2003). The special combination of these microtextures allowed conclusions to be made about the likely transport histories of the clastic grains (Higgs, 1979; Krinsley, Donahue, 1968; Krinsley, Doornkamp, 1973). The analysis of surface micromorphology of quartz grains from studied sediments allowed separating the three main grain groups: A) The mostly subangular grains show the prevalence of conchoidal fractures, fracture plains and straight steps, which are the result of the weathering processes or glacial transport (Krinsley, Doornkamp, 1973; Fig. 1-A). A considerable number of grains with such a suite of surface textures have more rounded outlines, V- shaped indentations and curved grooves overprinted on their surfaces and indicate that these quartz grains were transported by water either prior to, during, or after the glacial transport. B) The subrounded and rounded grains show the presence of small conchoidal fractures, V-shaped indentations, straight and curved grooves and scratches, which are considered to be the product of high-energy fluvial transport in coastal or riverine settings (Higgs, 1979; Fig. 1-B). C) The grains with subrounded and rounded outline, small conchoidal fractures, upturned plates and dish-shaped concavities were formed during the aeolian transport (Krinsley, Doornkamp, 1973; Fig. 1-C). The sediments of different origin show the difference in the content of quartz grains of the groups mentioned. The grains with water transport traces absolutely dominate in alluvial sediments. Grains from weathered rocks and aeolian material appear in glacial sediments. Fluvial-glacial sediments vastly have processed the moraine deposits and differ from them by bigger contents of grains with traces of water processing that can be explained by the existence of more dynamic conditions during the glacier retreating. The lacustrine sediments between two moraine layers contain a lot of aeolian grains. The cover loams deposits inherit the composition of glacial sediments; the increasing of the contents of grains with traces of water conversion in contrast with moraine was observed. 20
Fig.1. Micromorphology of quartz grains from the Pleistocene sediments in the Upper Oka River Basin: А – grains formed as a result of glacial transport; B – grains with the traces of water reworking; C – grains with the traces of wind reworking; D – adhering clays particles as a result of diagenesis; E – traces of cryogenetic weathering. D Commonly present on the majority of studied grains, are adhering clays particles forming accumulations of different thickness both on the exposed grain surfaces and within the fracture planes and depressions (Fig. 1-D). They are perhaps the result of diagenesis (Krinsley, Doornkamp, 1973). Solution pits and crevasses are probably the result of in situ chemical weathering. The content of grains with such surface features increases in cover loams deposits and can be explained by the activity of soil processes. Many grains carry the traces of cryogenic weathering, which is reflected in the presence of fresh conchoidal fractures on the grains surface (Rogov, 2000; Fig. 1-E). 21
Page 2 and 3: PHYSICS, CHEMISTRY AND BIOGEOCHEMIS
Page 4 and 5: IN MEMORIAM Dr Ludmila Petrovna Kor
Page 6 and 7: magnetic (ferrimagnetic) oxides, ma
Page 8 and 9: educed water activity, would favour
Page 10 and 11: In this paper AT sorption by surfac
Page 12 and 13: were obtained with clay content, pH
Page 16 and 17: Hence, the micromorphology suggests
Page 18 and 19: As the indicators of soil aeration
Page 20 and 21: Stomatal diffusive resistance of th
Page 22 and 23: indicators of soil aeration conditi
Page 24 and 25: REFERENCES 1. 2. 3. 4. 5. 6. 7. 8.
Page 26 and 27: Table 1. Breakdown of numbers and t
Page 28 and 29: MORPHOLOGICAL AND PHYSICOCHEMICAL P
Page 30 and 31: conditions, existing at the first p
Page 32 and 33: INFLUENCE OF TEMPERATURE ON WATER P
Page 34 and 35: moisture % 100 90 80 70 60 50 40 so
Page 36 and 37: STATE OF MICROBIAL COMMUNITIES IN M
Page 38 and 39: million cells/g soil 25 20 15 10 5
Page 40 and 41: THE INFLUENCE OF COMPOSITION AND PR
Page 42 and 43: days grew faster than on substrate
Page 44 and 45: SOIL SALINITY AND CLIMATE CHANGES I
Page 46 and 47: POROUS STRUCTURE OF NATURAL BODIES
Page 48 and 49: These nonuniform classification sys
Page 50 and 51: Mercury intrusion data are plotted
Page 52 and 53: METHOD AND MATERIALS The shear stre
Page 54 and 55: wheat flour NaCl salt fine milk Fig
Page 56 and 57: The shear experiments revealed two
Page 58 and 59: Variable charge of mineral surfaces
Page 60 and 61: 3. Huffaker RC and Wallace A 1958 P
Page 62 and 63: Q V (pH)/N t = α(pH) = n ∑ i= 1
Page 64 and 65:
REFERENCES 1. De Wit, J.C.M, Van Ri
Page 66 and 67:
BM - biomass; NM - necromass; MM -
Page 68 and 69:
thousand times at the absence of co
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. m 131.5 131.0 I Height above sea
Page 72 and 73:
SEASONAL VARIABILITY OF SOIL WATER
Page 74 and 75:
The mean difference (MD) and the ro
Page 76 and 77:
Acknowledgement This paper presents
Page 78 and 79:
1992; Selim 1999). The relative imp
Page 80 and 81:
1.0 C rel 0.5 0.0 v=0.7 D=3.28 v=0.
Page 82 and 83:
1.0 a b C rel 0.5 0.0 0 1 2 3 0 1 2
Page 84 and 85:
Comparison of before- and after-pul
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provides the accessibility of catio
Page 88 and 89:
MODEL RESEARCH ON FORMATION OF SYNT
Page 90 and 91:
The analysis of the specific surfac
Page 92 and 93:
PHOSPHATE-INDUCED CHANGES IN THE SP
Page 94 and 95:
According to the data of Table 1, t
Page 96 and 97:
MINERAL-ORGANIC COMPOUND OF SOILS:
Page 98 and 99:
RESULTS AND DISCUSSION An analysis
Page 100 and 101:
INTRODUCTION CHEMICAL DEGRADATION O
Page 102 and 103:
of organic particles and their elec
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HNO 3 -extractable form is very clo
Page 106 and 107:
Results demonstrated that Pb and Cd
Page 108 and 109:
tion was measured using the Tjurina
Page 110 and 111:
OUTPUT FLUXES OF LEAD IN FOREST ECO
Page 112 and 113:
Regional data on Pb concentrations
Page 114 and 115:
DEVICE FOR EVALUATION OF THE RAPE P
Page 116 and 117:
SPECTROSCOPIC COMPARISON OF HUMIC A
Page 118 and 119:
ehavior of sequentially extracted H
Page 120 and 121:
MODERN MONITORING SYSTEMS FOR THE M
Page 122 and 123:
The control of the measurement syst
Page 124 and 125:
ASORPTION AND SURFACE AREA OF SOILS
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Nm xCBET N = ( 1− x BET − )[ 1+
Page 128 and 129:
According to this, when x/N (1-x) i
Page 130 and 131:
POTENTIAL OF AZOLLA CAROLINIANA TO
Page 132 and 133:
The decrease of Pb(II) and of Cd(II
Page 134 and 135:
12. 13. 14. 15. 16. Piechalak, A.,
Page 136 and 137:
Kloc, 2001]. Nitrogen adsorption is
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This is worth noting that the lower
Page 140 and 141:
N ( h) 1 2 γ ( h) = [ ( ) ( )] ( )
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Exemplary spatial distributions (sa
Page 144 and 145:
This is worth noting that significa
Page 146 and 147:
adsorbed chemicals to microorganism
Page 148 and 149:
were detected in the untreated soil
Page 150 and 151:
0.4 1000 Moisture [Vol.] 0.3 0.2 0.
Page 152 and 153:
NITROUS OXIDE EMISSION FROM SOILS W
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N2O-N [mg kg -1 ] 100 80 60 40 20 0
Page 156 and 157:
LITERATURE 1. 2. 3. 4. 5. 6. 7. 8.
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where v(t) - CO 2 production rate;
Page 160 and 161:
carbon was involved mainly into mic
Page 162 and 163:
Demkin Vitaliiy DrSc Dmitrakov Leon
Page 164 and 165:
Priputina Irina PhD Rudko Tadeusz P
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