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Pedoweathering and mineralogical change in cryosols in an ultra-continental climate (Central Yakutia, Russia).

INTRODUCTION

Soils are closely related to the parent materials they are formed from and thus to Earth geodynamic processes. A second most influential factor of soil formation is that of climate and of the climate-induced biota. Currently, the global soil science community is in a process of flux because of new challenges and the responses required. Thus, the overall needs of mankind urgently require knowledge of soil behaviour induced by global change and have resulted in the development of large international projects involving new soil surveys and related in-depth studies. For example, projects such as the "Digital Soil Map of the World" are to be based on soil properties (Sanchez et al., 2009) and the "Universal Soil Classification" embraces information on soils gathered at a new level of investigation (Golden et al., 2010). Both of these projects need information on soils of large areas that are not well known from previous periods of soil survey. One such territory is Central Yakutia located in the Central Yakutia plain at an altitude of less than 400 m. Pedogenesis in this permafrost-affected zone has taken place in the cold ultra-continental climatic conditions that are sufficiently different from those of more humid climates in which permafrost-affected soils are wide spread (Kimble, 2004). That is why the study of permafrost-affected soils in such specific conditions should enrich essentially the general understanding of pedogenic processes (e.g. pedo-weathering) in the area of cold soils.

The properties, genesis, and classification of soils of Central Yakutia have been documented generally in Russian (Gerasimov, 1963; Elovskaya, 1987; Ivanova, 1971; Sokolov, 1991; Desyatkin et al., 2009). The soils named "Palevye (Pale)" following the Russian Classification are calcareous and mostly formed on the loess-like substrate. An attempt to determine the position of these soils in a "Classification and diagnostic system of Russian soils" (2004) based on morphology, analytical characteristic, and clay mineralogy has been made recently (Desyatkin et al., 2011). Nevertheless many aspects of soil genesis, and especially mineralogy, are still poorly known for the very specific and vast region of Siberia. The goal of this paper is to investigate the nature and distribution of the clay minerals in several permafrost-affected soils of Central Yakutia, to elucidate the specific soil processes involved and to consider any differences there may be with soils from similar landscapes.

OBJECTS AND STUDY LOCATION

The studied soil profiles are situated in Central Yakutia with GPS coordinates at 61-62[degrees]N and 129-133[degrees]E (Fig. 1). Geologically, this territory consists of Pleistocene river terraces overlain by predominately calcareous loess-like material. The climate is sharply continental. Mean annual air temperatur e is -10 to -11[degrees]C, but with great seasonal contrast: the mean monthly temperature in July is +18 - +19[degrees]C and in January -35 - -45[degrees]C. Extreme temperatures are +38[degrees]C and -64[degrees]C. The mean annual precipitation is 210-220 [micro]m, which is less than potential evapotranspiration (250-300 mm). However, the perennial variation of precipitation is high and wet years may have >300 mm. Central Yakutia is a territory with continuous permafrost at depths of 150-250 m. The thawing depth is from 0.5 to 2.5 m depending on the substrate and the landscape. The permafrost is a very important source of moisture making possible forest growth (Sugimoto et al., 2002), here dominated by larch (Larix cajanderi), pine (Pinus sylvestris) and birch (Betula platyphilla) with a small admixture of spruce (Picea obovata).

Several dozens of soil profiles were excavated and described and four of the most representative were sampled for the study of clay mineralogy. The studied "Palevye (Pale)" soils, classified according to World Reference Base for Soil Resources (2006), are represented by Pit 10-03 of Cambic Calcic Cryosol (Siltic, Magnesic): AO (0-6 cm)--Bw (6-22 cm) Bk(f) (22-65 cm); Pit 18-03 of Cambic Calcic Cryosol (Siltic, Luvic): O (0-3 cm)--A (3-7 cm)--AE (7-15 cm)--Bt (15-41 cm)--Bk(f) (41-91 cm); Pit 1-07 of Cambic Turbic Cryosol (Reductaquic): AO (0-10 cm)--Bw (10-20 cm)--[Bw.sub.@] (20-57 cm)--[Bk.sub.@] (57-75 cm)--[Bkg.sub.@]f (75-100 cm); and Pit 2-07 of Cambic Calcic Turbic Cryosol: O (0-4 cm)--AO (49 cm)--Bwh (9-19 cm)--[Bw.sub.@] (19-44 cm)--[Bk.sub.@] (44-114 cm)--[Bkf.sub.@] (114-124 cm).

METHODS

pH-values were measured potentiometrically in [H.sub.2]O with a soil:water ratio of 1:2.5. Extraction and content of soil organic matter (C) was determined by the wet combustion method of Tyurin. In the upper horizons: AO enriched by decomposed soil organic matter and O loss on ignition was determined. The forms of soluble iron in the <1 mm fractions were obtained by using the dithionite-citrate-bicarbonate method (Mehra and Jackson, 1958) and in the non-calcareous horizons by extraction with oxalate (Jackson et al., 1986). The carbonate presence was identified in the field by adding some drops of 10 % HCl to the samples. The <1 mm fraction of the soils were obtained by gentle grinding and disaggregation with subsequent dry sieving. Carbonates in calcareous samples were dissolved by 9 % acetic acid.

The <1 [micro]m fractions from soil horizons were separated by sedimentation and decantation, followed by dispersion by addition of a few drops of ammonia as a peptizing agent. The mineralogical composition of the <1 [micro]m soil fractions was investigated using a DRON-2 X-ray diffractometer with CoKa radiation and a monochromator in the diffracted beam. Pretreatment of the <1 [micro]m fractions included (i) saturation with Mg; (ii) ethylene glycol solvation; and (iii) heating at 550[degrees]C for 3 h. The samples studied by X-ray diffraction were also investigated by FTIR spectroscopy. FTIR spectra in the 400-4000 [cm.sup.-1] range were obtained using a Tensor 27 spectrometer (Bruker) with a resolution of 4 [cm.sup.-1] in ambient air and at room temperature. Spectra were recorded in the transmission mode using KBr pellets. The KBr and clay samples were heated in a furnace overnight at 105[degrees]C to minimize adsorbed water, and 1 mg of sample and 300 mg of KBr thoroughly mixed, pressed to a transparent pellet and their IR spectra recorded.

RESULTS

PHYSICOCHEMICAL PROPERTIES AND TEXTURE.

The studied soils are characterized by high soil organic matter contents, represented by raw humus, in the topmost O, AO, and A horizons and by relatively low soil organic matter contents in the mineral horizons. The pH values in the profiles change from acidic in the upper horizons (4.0-5.6), to weakly acidic to slightly alkaline in the middle horizons (6.0-7.7) and to alkaline in the basal horizon (8.0-8.5). Based on the relative proportions of dithionite--and oxalate-soluble iron, the studied soils could be split into two groups: (i) Pits 10-03, 18-03, and 2-07 with extremely low content (<0.6%) of dithionite-soluble iron and (ii) Pit 1-07 with much higher content (1.40-1.74 %). This higher amount is reflected by the more reddish color of both the substrate and the soil and could be explained by an admixture of pre-Quaternary material. In the soils of the first group most of the dithionite-extractable iron could be accounted for by amorphous + poorly crystallized (oxalate extractable) iron, especially in Pit 2-07 which is characterized by a relatively low clay content. In Pit 1-7, there is a slightly pronounced accumulation of oxalate extractable iron in the AO and Bw horizons.

The profiles have developed on a loess-like substrate apart from the Cambic Calcic Turbic Cryosol (Pit 2-07) which is characterized by a more sandy texture. The distribution of the clay size fraction is somewhat irregular, particularly in Pits 1-07 and 2-07, and in the lower horizons of Pit 18-03. These irregularities are most likely due to textural variation in the parent material. The clay content in Pit 10-03 shows no variation with depth. In the Pit 18-03 a well pronounced texture differentiation is detected both by morphological features and clay distribution. It is likely related to exchanging sodium ([Na.sub.+]), as this soil has 10% of exchanging sodium (Desyatkin et al., 2011) and is named "Solodic Pale soil" according to the local classification (Desyatkin et al., 2009).

MINERALOGY

The minerals identified in the clay fractions of all profiles are as follows: (i) chlorite, (ii) illite or interlayer-cation-deficient mica (Rieder et al., 1998), (iii) smectite and / or mixed-layer smectitic minerals with a high [greater than or equal to] 50 % amount of expandable layers, (iv) mixed-layer minerals with a small amount of expandable layers, (v) kaolinite, and (vi) quartz.

Chlorite identification is based on the 001 and 003 basal reflections at 14.0-14.2 [Angstrom] and 4.75 [Angstrom] respectively that are stable after ethylene glycol solvation and showing a slight contraction of the 001 peak to 13.8 [Angstrom] after 550[degrees]C treatment.

Illite is recognized by peaks at the 001 and 002 basal reflections at 10.0 [Angstrom] and 5.0 [Angstrom] respectively that remain stable after ethylene glycol and heat treatments.

Highly smectitic clays are identified by the response to ethylene glycol solvation whereby a peak at ~14 [Angstrom] in the Mg-saturated air-dry state shifts to a fundamental 001 spacing of [greater than or equal to] 17 [Angstrom]. As the 002 reflection at 8.49 [Angstrom], which is characteristic of a pure smectite (montmorillonite or beidellite) mineral, is not detected it is probable that the expandable phase represents a random mixed-layer structure with a non-expandable phase such as illite. The high background towards the low angle side of the 17 [Angstrom] peak is typical of a random mixed-layer illite-smectite structure where the smectite layers exceed 50% (Reynolds, 1980).

Mixed-layer clays with minor proportions of smectite or vermiculite layers are recognized by the asymmetries of the 10.0 [Angstrom] illite and 14 [Angstrom] chlorite peaks on XRD patterns of Mg saturated and heated samples respectively and suggest the presence of random mixed layer structures (Figs. 2, 3). Kaolinite is recognized by its 001 reflection at 7.14 [Angstrom] which disappears after heating at 550[degrees]C. The identification is confirmed by FTIR spectroscopy data that enables kaolinite to be identified in the presence of chlorite. IR spectroscopy is a sensitive method for the detection of kaolinite (Delvaux et al., 1989). The absorption bands near 3700 [cm.sup.-1] (the vibration of inner surface OH groups), 3627 [cm.sup.-1] (the stretching vibration of inner OH groups), 914 [cm.sup.-1] (bending vibration of inner OH groups), 540 [cm.sup.-1] (Si-O-Al bending vibrations), and 470[ cm.sup.-1] (Si-O-Si bending vibrations) all indicate the presence of kaolinite (Madejova and Komadel, 2001; Pentrak et al., 2009).

Quartz is identified by its characteristic XRD peaks at 3.34 and 4.26 [Angstrom] and by its most typical IR absorption band doublet at 800-780 [cm.sup.-1] (Hlavay et al., 1978; Madejova and Komadel, 2005) (Fig. 2).

DISTRIBUTION OF CLAY MINERALS

Using the above criteria, the distribution of the various clay minerals within the profiles of the Cryosols studied may now be summarized as follows:

Cambic Calcic Cryosol (Siltic, Magnesic) (Pit 10-03). There is little difference in the clay mineralogy of the Bw and Bk(f) horizons, both being characterized by mixed-layer smectite (most likely probably illite-smectite and probably chloritesmectite), chlorite, illite, kaolinite and quartz.

Cambic Calcic Cryosol (Siltic, Luvic) (Pit 18-03). The essential clay mineralogy of this soil, particularly in the two B horizons, is rather similar to that described above, but clear differences are found in both the A and AE horizons. Thus the intensity of the diffraction peak (001) for the smectitic mineral is much diminished in the AE horizon while in the A horizon it practically disappears. The same is true of the 14.2 [Angstrom] chlorite peak which in the A horizon appears to be replaced by a weak 12 [Angstrom] peak in the Mg-saturated state. The intensities of both the illite and kaolinite basal reflections are also severely diminished in the A horizon.

Cambic Turbic Cryosol (Reductaquic) (Pit 1-07). The clay mineralogy of the four B horizon samples, ranging in depth from 10 to 100 cm, are essentially similar to each other and to that of the B horizons of the soils just described. A mixed-layer smectitic clay (probably interstratified illite-smectite) is the dominant mineral with subsidiary amounts of chlorite, illite, kaolinite, and trace amounts of quartz. There is a clear change, however, in the upper AO horizon with a marked decrease in the content of the expandable smectitic clay, as well as a reduction in the amount of chlorite as indicated by the barely perceptible 13.8 [Angstrom] peak after heating at 550[degrees]C accompanied by weak diffraction maxima in 10 to 14A region. It is noted too that the 10A indicative of illite becomes progressively weaker in the Bw horizons and is barely detectable in the AO horizon.

Cambic Calcic Turbic Cryosol (Pit 2-7).The same trends are found in this soil although it is notable that the expandable smectitic phase persists throughout the profile and into the AO horizon where it remains the dominant clay mineral. Both illite and chlorite are severely reduced in the AO horizon compared with the underlying Bwh horizon.

DISCUSSION

Based on the above data the loess-like substrate of Central Yakutia is enriched in chlorite in comparison with the loess-like parent material of European Russia, where a "hydromica-smectite" composition has been reported (Gradusov, 2000). Despite their close mineralogical similarities, the studied soils illustrate some possible scenarios relating to the processes involved in the distribution of clay minerals in soil profiles affected by permafrost. The possibility of pedogenic weathering of clay minerals in Cryosols has been recently illustrated by a study of such soils in much colder conditions in ice-free areas of Admiralty Bay, King George Island (Simas et al., 2006).

Little mineralogical change can be observed in the B horizons of the Cambic Calcic Cryosol (Siltic, Magnesic) (Pit 10-03) over a depth of 6 to 65 cm. This may be explained by the neutral--alkaline pH values of these horizons and strongly suggests that all the clay minerals identified have been simply inherited from the loess-like parent material. It is of interest, however, that a pronounced vermiculitization of illite has been observed even in non-acidic arctic tundra Gelisols of Northern Alaska (Borden et al., 2010), although these soils formed in more moist conditions compared with the Cryosols of Yakutia. An additional factor that may be relevant to the weak differentiation of the clay minerals in some of the studied profiles is that the high content of the fine size fraction, enriched in phyllosilicates, tends to make any change unnoticeable.

In the Cambic Turbic Cryosol (Reductaquic) (Pit 1-07) there is a decrease in the smectitic phase in the more acidic upper horizons, as well as a decrease in the chlorite content. The transformation of illite and chlorite to randomly interstratified illite-smectite and chlorite-smectite respectively in circum-neutral to weakly acidic conditions has been documented for permafrost-affected soils Kriozems (Cryosols) formed in the cold, continental, climate of the Kolyma Lowland, North-East Siberia, as has the extremely weak intensity of chemical weathering of the Yedoma deposits (Alekseev et al., 2003).

In the upper part of the Cambic Calcic Turbic Cryosol (Pit 2-07) both illite and chlorite appear to decrease significantly. These upper horizons are acidic and may well have been affected by the vegetation community, especially mosses and lichens which are abundant on the surface of this soil. The overall proportion of the smectitic phase may possibly reduce in the upper horizons, as suggested by a decrease in intensity of the peak at ~14 [Angstrom] in the Mg-saturated sample although there is little corresponding decrease in the intensity of the peak at 17 [Angstrom] after glycol treatment. Significant losses of chlorite and mica, as well as the appearance of smectitic phases, have been reported in a soil formed in cold climatic conditions (Egli et al., 2003; Mavris et al., 2010). Thus, the presence of smectitic phase in the acidic upper horizons bearing in mind the decrease of shares of illite and chlorite can be explained by those minerals transformations.

More pronounced chlorite weathering is shown in the mildly acidic upper horizons of Cambic Calcic Cryosol (Siltic, Luvic) (Pit 18-03). The higher pH value of the upper horizon is in a good agreement with the influence of the vegetation community which is represented by grasses and herbs without an admixture of moss. In this profile, an eluvial morphology is evident, with clay material being translocated down the profile to yield a distinct Bt horizon. As it was mentioned above, these features could relate to the presence of [Na.sup.+] on the cation exchange complex, as documented by Desyatkin et al. (2011). On the other hand, the weathering in the upper horizons of the profile suggests the influence of more acidic conditions than indicated by current pH values. Solution chemistry may however be determined by a cyclical process relating to inherited carbonate in the parent material, with dissolved carbonate migrating downward in wet seasons and upward toward the freezing front in autumn.

It is evident that the clay mineralogy of the Cryosols investigated has been significantly affected to various degrees during the process of soil formation, particularly in the upper, more acidic horizons. These changes affect the dominant smectitic phase, illite and chlorite, all of which have been inherited from the loess-like parent material. The smectitic phase, whose X-ray characteristics are entirely consistent with random mixed-layer illitesmectite and probably chlorite-smectite where the proportion of smectite layers is [greater than or equal to] 50 %, is relatively unaffected in the Cambic Calcic Cryosol of Pit 10-03.

In the upper horizons of the Cryosols of Pits 1-07 and 2-07 there is a distinct reduction in the expandability of the smectitic phase, whereas in the Cambic Calcic Cryosol of Pit 18-03 the relative proportion of the smectitic phase is markedly reduced in the AE horizon and it seemingly disappears in the A horizon. Loss of expandability of smectitic clays is often observed in the acidic upper horizons of soils developed under a cool humid climate, such as Podzols and Brown forest soils, in Europe and North America (Wilson et al., 1984; Wilson, 1999). Generally, this feature is attributed to the introduction of non-exchangeable hydroxy- Al into the interlayer space so inhibiting both the swelling capacity and the ability to contract to 10A after heat treatment of the smectitic clay. Interlayering proceeds most effectively at pH values between ~4.4 to 5.6, which is within the range of the pH values of the uppermost horizons of the Cryosols from Pits 1-07 and 2-07, but where pH falls below 4.3 then the hydroxyl-Al converts to the [Al.sup.3+] ion. Another explanation of decrease of expandable phase portion is its partial dissolving in the upper acidic horizons. In the Cryosol from Pit 18-03, however, it is apparent that the smectitic phase is absent from the A horizon and is much decreased in quantity in the AE horizon. Although these features might be explained by the decomposition of the smectitic phase, another possibility is that the clay has been eluviated down the profile to accumulate in the underlying Bt horizon. This might be a more likely explanation bearing in mind the mildly acidic character of the topmost horizon (pH 5.6) and the alkaline reactions of those underlying it (pH 7.5-8.5).

With regard to the changes noted in the illite and chlorite components of the <1[micro]m fractions, similar changes have been noted too in Podzolic and Brown forest soils in Europe and North America. Illite normally loses interlayer potassium and converts to a mixed layer dioctahedral illite-vermiculite in the upper acidic horizons of such soils or even to illitesmectite as it was shown for soils of Yedoma deposits (Alekseev et al., 2003) and it seems that this is a likely explanation for the loss of illite in the upper horizons of the Cryosols. The situation with regard to chlorite is more problematical as complete decomposition of the clay mineral occurs in some soils (Bain, 1977), which is not surprising bearing in mind its susceptibility to acid dissolution in the laboratory, whereas in other soils it has been proposed that the mineral forms interlayered and mixed-layer clays (De Coninck et al, 1983; Righi et al, 1993). Although there is not enough evidence to decide upon these two possibilities, it is of interest that there seems to be no relationship between intensity of chemical weathering and increase of oxalate extractable iron. The non-systematic distribution of this form of iron in the soils of Yakutia has also been noted by Ivanova (1971).

In conclusion, the clay mineralogy and the specific clay mineral changes noted in the permafrost-affected soils studied here are determined by the interaction of the various soil forming factors first identified by Dokuchaev in the 19th century. The preponderant factor in this case is parent material as it seems almost certain all the clay minerals identified have been inherited from the underlying loess-like deposit. However, the continental climatic conditions and the vegetation communities have combined to create acid conditions in the upper parts of the soil profiles and this has brought about change in the nature and distribution of the clay minerals within the soil profiles. A seasonal migration of dissolved carbonates from and to the parent material at the base of the profiles during spring and autumn may also have influenced the pH distribution within the Cryosols.

CONCLUSION

The clay mineralogy of the fine size fractions (<1[micro]m) of a set of Cryosols in north east Siberia is characterized by the dominant occurrence of a highly smectitic phase (most likely mixed-layer illite-smectite and probably chlorite-smectite), subordinate illite and chlorite, and with traces of kaolinite. All these minerals have been inherited from the loess-like parent material. Pedogenesis has brought about change in the more acidic upper horizons, including a marked reduction in the expandability of the smectitic phase, possibly accounted for by the introduction of non-exchangeable hydroxy-Al into the interlamellar space or partial dissolving of smectitic phase, and a reduction in relative contents of both illite and chlorite. Illite has been at least partially transformed to a mixed-layer illite-vermiculite (smectite), whereas chlorite has either been completely decomposed or has transformed to a mixed-layer expandable component. In one profile, the smectitic mineral appears to be absent from the upper horizon, suggesting that it may have been completely decomposed. An alternative explanation is that it has been eluted or translocated down the profile to accumulate in a Bt horizon.

ACKNOWLEDGEMENTS

The authors are grateful to the reviewers for helpful suggestions and very useful remarks.

DOI: 10.13168/AGG.2013.0047

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Sofia N. LESSOVAIA (1) *, Sergey V. GORYACHKIN (2), Roman V. DESYATKIN (3) and Matrena V. OKONESHNIKOVA (3)

(1) St. Petersburg State University, Faculty of Geography and Geoecology, V.O., 10 line, 33, St. Petersburg, 199178, Russia, +7-812-3233913

(2) Institute of Geography, Russian Academy of Sciences, Staromonetny per.29, Moscow, 119017 Russia, + 7-495-9593786,

(3) Institute of Biological Problems of the Cryolithozone, Siberian Branch, Russian Academy of Sciences, pr. Lenina 47, Yakutsk, 667891 Russia, +7-4112-335690

* Corresponding author's e-mail: lessovaia@yahoo.com

(Received March 2013, accepted May 2013)

Table 1 Some properties of the studied soils.

Horizon, depth (cm)          pH        <1[micro]m     LI     C
                         [H.sub.2]O        (%)       (%)    (%)

Pit 10-03, Cambic Calcic Cryosol (Siltic, Magnesic)

AO (0-6)                    4.0           --        93.2    --
Bw (6-22)                   7.0          22.9        --    2.1
Bk(f) (22-65)               8.0          22.9        --    1.3

Pit 18--03, Cambic Calcic Cryosol (Siltic, Luvic)

A(3-7)                      5.6           8.2              3.4
AE (7-15)                   7.5          11.9        --    0.9
Bt (15-41)                  7.6          26.2        --    0.5
Bk(f) (41-91)               8.5          18.5        --    0.4

Pit 1-07, Cambic Turbic Cryosol (Reductaquic)

AO (0-10)                   4.8          23.4        --    4.3
Bw (10-20)                  6,0          26.6        --    1.3
[Bw.sub.@] (20-57)          7.3          32.1        --    0.5
[Bk.sub.@] (57-75)          8.3          22.9        --    0.5
[Bkg.sub.@]f (75-100)       8.1          32.3        --    0.4

Pit 2-07, Cambic Calcic Turbic Cryosol

O (0-4)                     5.0           --        49.4
AO (4-9)                    4.4          11.1       27.5
Bwh (9-19)                  6.3           7.8        --    1.4
[Bw.sub.@] (19-44)          7.7          11.1        --    0.2
[Bk.sub.@] (44-114)         8.0          15.6        --    0.3
[Bkf.sub.@] (114-124)       8.2          12.3        --    0.2

                           [Fe.sub.2][O.sub.3]
Horizon, depth (cm)
                           d       o      o/d
                              (%)

Pit 10--03, Cambic Calcic Cryosol (Siltic, Magnesic)

AO (0-6)                 --      --      --
Bw (6-22)               0.58    0.32    0.55
Bk(f) (22-65)           0.31     --      --

Pit 1803, Cambic Calcic Cryosol (Siltic, Luvic)

A(3-7)                  0.44    0.33    0.75
AE (7-15)               0.53    0.26    0.49
Bt (15-41)              0.56    0.26    0.46
Bk(f) (41-91)           0.33     --      --

Pit 1-07, Cambic Turbic Cryosol (Reductaquic)

AO (0-10)               1.51    0.71    0.47
Bw (10-20)              1.74    0.51    0.29
[Bw.sub.@] (20-57)      1.55    0.21    0.13
[Bk.sub.@] (57-75)      1.40     --      --
[Bkg.sub.@]f (75-100)   1.63     --      --

Pit 2-07, Cambic Calcic Turbic Cryosol

O (0-4)                  --      --      --
AO (4-9)                0.35    0.25    0.71
Bwh (9-19)              0.34    0.28    0.82
[Bw.sub.@] (19-44)      0.28    0.22    0.78
[Bk.sub.@] (44-114)     0.27     --      --
[Bkf.sub.@] (114-124)   0.29     --      --

Abbreviations and notes: d--dithionite and o--oxalate extractable
[Fe.sub.2][O.sub.3] '-'--no data available; <1 [micro]m--content of
particle size <1 [micro]m in the <1 [micro]m fraction; LI--loss on
ignition; C--soil organic matter, %
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Title Annotation:ORIGINAL PAPER
Author:Lessovaia, Sofia N.; Goryachkin, Sergey V.; Desyatkin, Roman V.; Okoneshnikova, Matrena V.
Publication:Acta Geodynamica et Geromaterialia
Article Type:Report
Geographic Code:4EXRU
Date:Oct 1, 2013
Words:5265
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