Gleysols on sandy deposits of the Litorina Sea underlain by Histosol formations of Ancylus Lake age in western Estonia/Antsulusjarve-aegsetel soomuldadel lasuvatel Litoriinamere liivadel kujunenud gleimullad Laane-Eestis.
INTRODUCTIONOne of the prime interests of natural scientists around the Baltic Sea is to detect the environmental changes in the shifting coast of the sea basin. Already since the Stone Age people have adapted themselves to the fluctuating sea level. It means that terrestrial processes during different stages of the Baltic Sea have great geological, pedogenetic, and archaeological importance. During the last few years we have studied several multisequal soil sections in the area of ancient human settlements in western Estonia. The development of Histosols and/or Molli-Histic Gleysols on calcareous till as well as on Baltic Ice Lake sediments during the Yoldia stage have been reported (Reintam & Moora 1998; Reintam et al. 2001). Automorphic Podzols and Arenosols have developed of sandy deposits of Ancylus and/or Litorina stages on the top of many outcrops. The lowermost part of the Lemmejogi outcrop became the first section, at least in Estonia, which was sampled directly from the top of strongly gleyed till (Reintam et al. 2001). The Paikuse and Pulli outcrop sections were the first ones which had pedological interpretations (Reintam & Moora 1998) in addition to the geologist's indefinite qualification as "organic sediments".
This paper deals with the materials concerning contemporary gleyic formations of different age on Litorina fine sand underlain by peats on Ancylus silty sediments. The presence of bisequal hydromorphic soil profiles, some of which developed more than 7000 BP and others within the past centuries or even during the last decades, has become possible due to the relatively low altitude and permanently high level of the groundwater table.
MATERIAL AND METHODS
Site, topography, geology, and sampling
The main stages in the Baltic Sea history have been known since the beginning of the last century, but have never been properly defined as stratigraphical units whose boundaries between different water bodies are time transgressive. In this paper the boundary between the Baltic Ice Lake and the Yoldia Sea is given as 10 300 yr BP, between the Yoldia Sea and the Ancylus Lake 9300 yr BP, between the Ancylus Lake and the Litorina Sea 8000 yr BP, and between the Litorina Sea and the Limnea Sea 4000 yr BP (Raukas 1997).
Two pits in similar topographical and geological situation were chosen for detailed investigation (Table 1). Both of them have archaeological significance. The first site (Figs 1 and 2) was located in the courtyard of the modern Lihula Central Townstore (58[degrees]41'N, 23[degrees]48'E) at an altitude of 14.86 m a.s.l. Asphalt and gravel covered a 52-cm layer of silty Anthrosol, which evidently had been transported from some other place at the time of village restoration about 1300. A Eutric Gleysol profile (Fig. 3a), which developed after the Litorina regression, began at an altitude of 14.34 m a.s.l., and a Molli-Histic Gleysol, which developed during Late Ancylus time, started at an altitude of 13.60 m a.s.l. Calcareous reworked till with limestone gravel and pebble material begins at an altitude of 13.39 m a.s.l. Probably that till was reworked during the deep Yoldia Sea regression, however, Ancylus Lake activity cannot be excluded. A thin layer of highly compacted fine sand seems to have accumulated in the nearshore zone of Ancylus Lake before the start of terrestrial paludification. The underlying peat contains residues of woody material.
The second pit was excavated on the Island of Saaremaa (Figs 1 and 4) between the villages of Ilpla and Reo (58[degrees]19'N, 22[degrees]40'E) near a gravel quarry which was exhausted in 1976. On the basis of a large-scale soil map (Fig. 5) compiled in 1987-1988, it is possible to conclude that a Eutri-Gleyic Arenosol profile formed on fine Litorina Sea sand and is only about 24 years old as it tends to be developed during the time after the retreat of the Litorina Sea. This profile covers a problematic thin Fluvisol formation underlain by a Histosol on an Ancylus sandy deposit (Fig. 3b). Silurian limestone lies at a depth of 155 cm and is overlain by a coarse sandy layer (12 cm) containing both calcareous gravel and shingle from limestone bedrock.
The [sup.14]C data from the outcrop allow us to specify the time of the maximum Litorina Sea transgression in the precincts of Ipla-Reo Kilbumagi but also the age of the Konnu Stone Age settlement (Fig. 4) located nearby. Artifacts from the settlement belong to the Early Neolithic Period. The amount of charcoal collected during the excavations of the settlement in 1976-1978 was not sufficient for analysis. Settlement history is really a special field of geographic research. Archaeologists, whose research is based on material finds, cannot describe the formation and development of their forefathers in the Prehistoric Period without involving palaeogeographic disciplines. Pedologic information plays an important role in the study of the development of natural environments in the past.
The morphological description and the sampling of both profiles were carried out in a traditional soil science way (FAO 2006) to the depth of calcareous till and/or underlying limestone. Holocene stratigraphy was established by Raukas et al. (1995). Microimpactites with an age of over 7000 [sup.14]C yr BC were discovered at Ilpla-Reo, which may have originated from the explosion that generated the meteoritic craters at Kaali (Fig. 4).
Analyses
Analytical techniques on air-dry soil were carried out by a research assistant Raja Kahrik in the laboratories of the Department of Soil Science and Agrochemistry, Estonian University of Life Sciences (former name Estonian Agricultural University). Fine earth with grain size less than 2 mm was used. Samples for the determination of particle size were treated with sodium pyrophosphate to break down aggregates. Sands were sieved and fractions finer than 0.05 mm were determined by pipette analysis (Pipette Apparatus Table Model 7 Samples). Total chemical analysis was carried out after alkaline fusion treatment. Iron and aluminium were ascertained by means of sulphosalicylic acid and aluminone, respectively; alkaline earths, potassium, and sodium were determined by flame photometry. Carbonates were determined acidometrically for recalculation of measurement data. The results obtained are expressed for ignited noncalcareous material (Arinushkina 1970; van Ranst et al. 1999). Previously the reliability of these techniques was verified by atomic absorption spectrometry.
Cation exchange capacity (CEC) and exchangeable bases were measured by percolation of a sample with ammonium acetate at pH 7.0 and expressed in cmol [kg.sup.-1]. The total amounts (g [kg.sup.-1]) of organic carbon and nitrogen were measured by the Tyurin and Kjeldahl volumetric methods, respectively (Ponomareva 1957). The Anne' method (van Ranst et al. 1999) is equivalent to the Tyurin method used. The group and fractional compositions of humus were measured by the alternate acid-alkaline treatment according to the volumetric method of Tyurin-Ponomareva (Ponomareva 1957). The results are expressed as a percentage of organic carbon. Group composition represents humic acids (H.a.), fulvic acids (F.a.), and humins known as the insoluble residue. Humic and fulvic acids altogether are humus acids. The fractions within the groups are the following: 1a--free fulvic acids (only within the group of fulvic acids); 1--humic and fulvic acids bound with mobile [Fe.sub.2][O.sub.3] and [Al.sub.2][O.sub.3]; 2--humic and fulvic acids bound with Ca and Mg; 3--humic and fulvic acids bound with immobile sesquioxides and clay.
The humic : fulvic ratio is an integral parameter of the maturity and mobility of humus as well as of humicity (>1) and/or fulvicity (<0.7). The ratio of the first to the second fraction demonstrates the relationship of the brown humic-fulvic complexes, bound with mobile sesquioxides, to the grey (black) complexes bound with alkaline earths. Decalcification with 0.05 M sulphuric acid represents a part of humus fractination, which permits determination of the second and the third fractions as well as the hydrolysate of 0.5 M sulphuric acid by extracting humus substances from the crystal structure of clay minerals (Ponomareva 1957). Dithionite-extractable (total nonsiliceous) iron, oxalate-extractable iron, aluminium, and silica were measured after Coffin and Tamm, respectively; iron activity was calculated after Schwertmann (van Ranst et al. 1999). The pH of both water and I M KCl suspensions (1:2.5) was measured potentiometrically with the pH-meter Jenway 3071. The specific surface area (SSA) was measured after Puri and Murari using water absorption from the steam-saturated atmosphere above 41% sulphuric acid (Kitse & Rooma 1984). The results are expressed as [m.sup.2] [g.sup.-1].
The soils were named according to the World Reference Base for Soil Resources (FAO 2006). Requirements for the accuracy of sampling, laboratory techniques and measurements were satisfied as for any reference profile (Batjes & van Engelen 1997).
RESULTS AND DISCUSSION
Organic matter
The lack of any mollic and/or histic formation on both calcareous till and limestone bedrock (Figs 3a and 3b) demonstrates that the sites studied were dry land of islands or islets during the regressions of the Baltic Ice Lake and the Yoldia Sea. In the Pre-Boreal about 9300 BP thin silty-sandy sediments of the Ancylus Lake transgression covered till at Lihula and the limestone in the Ilpla-Reo area. The Histosol profile is dated to 7732 [+ or -] 118 BP (Tln-2554) in the lower part and 7368 [+ or -] 68 BP (Tln-2558) in the upper part of the histic horizon at Ilpla-Reo, and to 7459 [+ or -] 56 BP (Tln-2731) for wood within peat at Lihula. If we suppose that shallow water of Ancylus Lake rapidly retreated from islet-like bedrock and till hillocks, the duration of hydromorphic pedogenesis there must have been at least 2000 years until Litorina transgression once again buried soils under a sandy carpet. The Late Ancylus pedogenesis in the Boreal Chronozone resulted in the formation of Eutric Histosols during about two millennia or even for some hundred years less. The average annual increment in organic carbon appears to be about 10-11 g [m.sup.-2] [yr.sup.-1] in the layer of 25-35 cm, being about 3-4 times higher in the upper part of the histic horizon than in the lower one. This situation is quite similar to that in Molli-Histic Gleysols of Pre-Ancylus stages (Reintam et al. 2001).
The [R.sub.2][O.sub.3]-humic humus, saturated with alkaline earths, is also characteristic of molli-histic epipedons of Late Ancylus-Early Litorina age (Tables 2 and 3). Although the total amount of organic carbon is a little less at Lihula, there are no differences in the principal composition of humus between the two sites. Only Ca-humic-fulvic complexes are better preserved in the high groundwater conditions at Lihula. This is also reflected in the composition of decalcinate. In spite of large differences in the age of Gleysols (Table 2 modern soil, Table 3 Limnea age soil) and total amount of organic carbon, the composition of humus is quite similar. Based on previous studies of several other soil units, we conclude that the main qualitative characteristics of humus status form during early stages of pedogenesis. Further quantitative development appears to result in only negligible changes in qualitative properties. Therefore saturated [R.sub.2][O.sub.3]-humic-fulvic humus of different-aged Gleysols is preserved even in the conditions of an increase in total solubility and impoverishment in decalcinate (Table 3). A similar result occurs in the striped Fluvic formation at a depth of 85-92 cm (Table 2). Organic matter seems to have accumulated here in shallow brackish water of the Litorina Sea (enriched in exchangeable [Na.sup.+], Table 4), however, there are no differences in humus composition compared to those above. Only the C:N ratio is extremely large.
[FIGURE 1 OMITTED]
[FIGURE 2 OMITTED]
[FIGURE 3 OMITTED]
[FIGURE 4 OMITTED]
[FIGURE 5 OMITTED]
The colluvial material deposited at Lihula appears to be from mollic epipedons of Rendzinas of calcareous till origin from the neighbouring areas. It is possible that part of the calcium both in decalcinate (Table 3) and the exchangeable complex (Table 4) of underlying layers could have originated from this material as a result of the weathering of carbonates and leaching of products.
Exchange properties and texture
Against the background of neutral to slightly alkaline reaction, the accumulation of organic carbon resulted in an increase in the specific surface area as well as in cation exchange capacity (Table 4).
The temporal influence is absent in the development of exchange properties of modern and Limnea-age Gleysol. Everywhere the impact of organic matter is prevalent. Calcium is the dominant exchangeable cation.
Pedogenetic textural differentiation is lacking in all Ancylus and Post-Ancylus sediments (Table 5). Common uniformity is also characteristic of the covering Anthrosol of silty sandy till origin. Textural stratification of Post-Ancylus sandy material tends to be due to the coastal activities during its formation at a depth of 107-117 cm at Lihula, but possibly also at a depth of 127-143 cm in the region of Ilpla--Reo. The weathering of sand particles is weak in the top of the uppermost Gleysol profiles, especially within the modern profile at Ilpla-Reo, as a result of which only a slight accumulation of clay and silt can be found.
The simple uniformity of exchange properties and texture of different-aged Gleysols and mineral subsoils of Histosols confirm the former generalization that no pedogenetic differentiation takes place under aquic groundwater regimes and the layering of the solum depends on former geologic conditions and sedimentation.
Chemical characterization
Practically the same can be said about the chemical properties (Tables 6 and 7). Slight accumulation of nonsiliceous substances has taken place in the horizons of organogenic origin as well as in the Bw-horizons of the weathering of sand-size alumosilicates (Table 6). The only exception is once again the coastal layer at a depth of 107-117 cm at Lihula. Naturally, iron activity has increased everywhere in the topsoil, but is quite high throughout both underlying Molli-Histic profiles. Amorphous aluminium is low due to the high pH value and base saturation. The amount of amorphous silica can be explained with the gleying in the conditions of alkaline reaction.
Chemical composition appears to be quite homogeneous among the different-aged sediments (Table 7). Slight impoverishment in iron of all weathered gley(ic) horizons is due to the mobilization of ferrous compounds during the gleying and the seasonal fluctuation of the groundwater table. No traces of illuvial and/or in situ accumulation of sesquioxides are observed. Layer differences of alkaline earths are explained by the specifics of Holocene sediments. Molecular ratios repeat the chemical uniformity of the Holocene and contemporary Gleysol formations.
CONCLUSIONS
Archaeological, palaeogeographical, and stratigraphical information is of great importance to study the trends and rates of pedogenesis and the evolution of soils. Gleysol formation during the Holocene on different-aged aqueous sediments is highly uniform and dependent on the composition and layer structure of parent sediments. As a result of hydromorphic humus accumulation, the large amount of active organic matter as the driving force for pedogenesis tends to create a rapid increase in the specific surface area and exchange properties but preserves the stable textural-chemical properties of the sandy-silty deposits from the Ancylus stage up to modern times.
ACKNOWLEDGEMENTS
We would like to thank Raja Kahrik for her contribution in laboratory analyses, Ester Jaigma for the linguistic revision of the manuscript, Priit Perm and Tambet Kikas for their collaboration in the final design of the digital soil map, and Kersti Siitan for the technical formation of Figs 1, 2, and 4. Our sincere thanks belong to Dr. Richard W. Arnold and Prof. Hans-Peter Blume for their valuable advice, useful comments, and recommendations to improve the manuscript.
Received 29 July 2008, accepted 24 September 2008
REFERENCES
Arinushkina, E. V. 1970. Handbook for Soil Chemical Analyses. University Press, Moscow, 487 pp. [in Russian].
Batjes, N. H. & van Engelen, V. W. P. 1997. Guidelines for the Compilation of a 1: 2 500 000 SOTER Database (SOYEUR Project). Report 97/06, International Soil Reference and Information Centre. Wageningen, 68 pp. [FAO] Food and Agriculture Organization. 2006. World Reference Base for Soil Resources 2006 A Framework for International Classification, Correlation and Communication. World Soil Resources Reports, 103. FAO, Rome, 142 pp.
Kitse, E. & Rooma, I. 1984. Mullateaduse laboratoorne praktikum [Laboratory practice in soil science]. Estonian Agricultural Academy, Tartu [in Estonian].
Ponomareva, V. V. 1957. To the method for the study of soil humus after I. V. Tyurin's scheme. Pochvovedenie (Soviet Soil Science), 8, 66-71.
Raukas, A. 1997. Evolution of the Baltic Sea. In Geology and Mineral Resources of Estonia (Raukas, A. & Teedumae, A., eds), pp. 268-274. Estonian Academy Publishers, Tallinn.
Raukas, A., Saarse, L. & Veski, S. 1995. Revised Holocene stratigraphy in Estonia. Proceedings of the Estonian Academy of Sciences, Geology, 44, 201-210.
Reintam, L. & Moora, T. 1998. Development of pedogenesis on aqueous deposits within the Holocene in West Estonia. Proceedings of the Estonian Academy of Sciences, Geology, 47, 108-129.
Reintam, L., Raukas, A., Kleesment, A., Moora, T. & Kahrik, R. 2001. Podzolization in aeolian sands, underlain by Gleysol formation, during nine millennia in southwestern Estonia. Proceedings of the Estonian Academy of Sciences, Geology, 50, 254-281.
Van Ranst, E., Verloo, M., Demeyer, A. & Pauwels, J. M. 1999. Manual for the Soil Chemistry and Fertility Laboratory. Analytical Methods for Soils and Plants. Equipment and Management of Consumables. University of Ghent, Gent, Belgium, 243 pp.
Loit Reintam (a), Tanel Moora (b), and Anto Raukas (c)
(a) Department of Soil Science & Agrochemistry, Estonian University of Life Sciences, Kreutzwaldi 1, 51014 Tartu, Estonia; loit.reintam@emu.ee
(b) Institute of History, Tallinn University, Ruutli 6, 10130 Tallinn, Estonia
(c) Institute of Ecology, Tallinn University, Narva rant. 25, 10120 Tallinn, Estonia; anto.raukas@mail.ee
Table 1. General characterization of the pits
Location Material Horizon and Colour
depth, cm
Lihula Debris fill, [A.sub.tierrie], 10YR2/2
till 0-52
58[degrees]41'N, Limnea Sea A 52-68 10YR2/2
fine sand
23[degrees]48'E Bw 68-78 10YR4/3
IG 78-108 10YR7/3
Beach gravel IIG 108-126
Ancylus-age, AH 126-137 10YR1/1
peaty
Very compact IIIG 137-147 5G5/1
sand
Calcareous > 147
till
Ilpla-Reo Litorina Sea A 0-8 10YR2/1
sand
58[degrees]19'N, Bwg 8-24 10YR6/2
22[degrees]40'E Cg 24-45 10Y8/1
CG 45-69 10Y8/1
ACa 69-85 10Y7/2
IIG 85-92 5GY4/3
Ancylus-age, H3 92-117 N1.5/0
peaty AH 117-127 10YR2/2
Ancylus-age IIIG 127-143 5GY6/3
sand
Gravelly IVG 143-155
shingle sand
Limestone > 155
Location Characteristics Thickness, cm
Lihula Debris fill, 52
anthric
58[degrees]41'N, Mollic, weakly 16
rooted
23[degrees]48'E Slightly cambic 10
Quicksand, grey 30
Coarse gravelly 18
sand
Molli-histic 11
Silty, aleuritic 10
Under groundwater
Ilpla-Reo Mollic, well- 8
rooted
58[degrees]19'N, Rusty, weakly 16
cambic
22[degrees]40'E Whitish-grey, 21
fine
Striped, silty 24
stripes
Humously striped 16
Plastic clay, 7
steely grey
Molli-histic 25
Mollic, clayey 10
Fine silty sand 16
Coarse, calcareous 12
Table 2. Composition of organic matter in percentage of organic carbon,
Ilpla-Reo, Island of Saaremaa
Characteristics Horizon and depth, cm
Modern soil Litorina
A 0-8 Bw 8-24 IIG 85-92
Organic C, g 81.0 1.9 12.2
[kg.sup.-1]
of soil
Nitrogen, g 4.2 0.2 0.2
[kg.sup.-1]
of soil
C:N 19.3 9.5 61.0
Humic acids
1 8.3 11.2 4.8
2 6.1 7.9 0.0
3 5.2 6.7 15.6
Total 19.6 25.8 20.4
Fulvic acids
1a 4.9 18.6 0.7
1 2.9 0.0 5.3
2 7.3 25.2 0.0
3 3.8 0.0 11.7
Total 18.9 43.8 17.7
Hydrolysate of 0.5 5.4 8.3 10.7
M [H.sub.2][S0.sub.4]
Total soluble 43.9 77.9 48.8
Insoluble residue 56.1 22.1 51.2
Humic : fulvic 1.04 0.59 1.15
ratio
1st fraction: 0.84 0.34 10.10
2nd fraction
Decalcinate, g
[kg.sup.-1]
Fe 7.3 1.5 2.9
A1 1.6 0.9 0.9
Ca 0.7 0.4 19.6
Characteristics Horizon and depth, cm
Ancylus age, 7732 [+ or -] 118-7368
[+ or -] 68 BP
H3 92-105 H3 105-117 AH 117-127
Organic C, g 337.9 93.3 33.1
[kg.sup.-1]
of soil
Nitrogen, g 17.9 4.1 2.1
[kg.sup.-1]
of soil
C:N 18.9 22.8 15.8
Humic acids
1 9.0 6.8 3.8
2 5.2 15.6 5.0
3 9.7 11.3 22.9
Total 23.9 33.7 31.7
Fulvic acids
1a 3.7 6.2 7.0
1 0.1 0.1 0.0
2 4.7 9.6 14.4
3 2.7 5.1 8.9
Total 11.2 21.0 30.3
Hydrolysate of 0.5 6.4 6.1 5.3
M [H.sub.2][S0.sub.4]
Total soluble 41.5 60.8 67.3
Insoluble residue 58.5 39.2 32.7
Humic : fulvic 2.13 1.60 1.05
ratio
1st fraction: 0.92 0.27 0.20
2nd fraction
Decalcinate, g
[kg.sup.-1]
Fe 3.7 3.5 4.0
A1 0.2 1.9 2.0
Ca 0.6 0.1 11.3
Mg 0.2 0.1 1.7
Table 3. Composition of organic matter in percentage of organic carbon,
Lihula, Laane County
Characteristics Horizon and depth, cm
Covering Terric Anthrosol Limnea
(14.86 m above sea level) age *
0-13 13-26 26-52 A 52-68
Organic C, g 36.9 27.7 27.7 12.3
[kg.sup.-1]
of soil
Nitrogen, g 2.4 4.4 2.0 0.9
[kg.sup.-1]
of soil
C:N 15.4 6.3 14.3 13.7
Humic acids
1 8.7 8.3 9.6 11.2
2 9.9 14.0 10.0 20.0
3 4.3 8.6 6.2 4.7
Total 22.9 30.9 25.8 35.9
Fulvic acids
1a 2.8 2.1 2.1 11.4
1 6.2 10.4 11.2 7.0
2 4.9 6.0 4.9 15.0
3 7.7 4.6 4.9 5.9
Total 21.6 23.1 23.1 39.3
Hydrolysate of 0.5 M 10.1 12.7 8.2 6.2
[H.sub.2][S0.sub.4]
Total soluble 54.6 66.7 56.1 81.4
Insoluble residue 45.4 33.3 43.9 18.6
Humic : fulvic 1.06 1.34 1.17 0.91
ratio
1 st fraction: 1.01 0.94 1.40 0.52
2nd fraction
Decalcinate (g kg)
Fe 0.5 0.2 0.4 0.6
A1 2.4 1.6 2.8 0.0
Ca 21.7 16.0 20.7 7.0
Mg 23.3 22.9 24.4 3.5
Characteristics Horizon and depth, cm
Ancylus age 7459 [+ or -] 56 BP
(13.6 m above sea level)
AH 126-131 AH 131-137
Organic C, g 154.7 47.2
[kg.sup.-1]
of soil
Nitrogen, g 7.5 3.7
[kg.sup.-1]
of soil
C:N 20.6 12.8
Humic acids
1 14.2 17.7
2 8.9 14.1
3 8.1 6.8
Total 31.2 38.6
Fulvic acids
1a 1.3 1.6
1 3.3 4.4
2 6.4 9.5
3 2.8 2.8
Total 13.8 18.3
Hydrolysate of 0.5 M 3.5 2.5
[H.sub.2][S0.sub.4]
Total soluble 48.5 59.2
Insoluble residue 51.5 40.8
Humic : fulvic 2.26 2.10
ratio
1 st fraction: 1.14 0.93
2nd fraction
Decalcinate (g kg)
Fe 1.7 1.1
A1 6.3 3.1
Ca 12.4 4.9
Mg 3.6 2.0
* Eutric Gleysol on Litorina sand.
Table 4. pH, exchange properties, and specific surface area (SSA)
Location Soil Horizon and [pH.sub.H20]
depth, cm
Ilpla-Reo Eutri-Gleyic A 0-8 6.7
Arenosol
Bw 8-24 7.0
C 24-45 7.1
[C.sub.stratif.] 7.7
45-69
Fluvisol? ACa 69-85 7.5
IIG 85-92 7.2
Molli-Histic H3 92-105 6.1
Gleysol
(Histosol) H3105-117 6.7
AHG 117-127 7.4
IIIG 127-143 7.8
IVG 143-155 7.4
Lihula Terric Anthrosol [A.sub.terric] 0-13 7.4
(14.86 m a.s.l.) [A.sub.terric] 13-26 7.4
[A.sub.terric] 26-39 7.4
[A.sub.terric] 39-52 7.3
Eutric Gleysol A 52-68 7.2
(14.34 m a.s.l.) Bw 68-78 7.5
G 78-93 7.9
IG 93-107 8.0
107-117 7.9
IIG 117-126 7.9
Molli-Histic (A)H 126-131 6.9
Gleysol
(13.6 m a.s.l.) AH 131-137 7.1
IIIG 137-147 7.8
Location Soil [pH.sub.KCI] [Ca.sup.2+] [Mg.sup.2+]
cmol [kg.sup.-1]
Ilpla-Reo Eutri-Gleyic 6.5 52.31 3.27
Arenosol
6.6 3.03 0.13
6.7 2.71 0.09
7.5 19.36 0.24
Fluvisol? 7.5 19.75 0.20
7.1 32.95 0.99
Molli-Histic 5.8 85.26 6.63
Gleysol
(Histosol) 6.5 66.32 4.86
7.0 42.84 1.98
7.4 21.69 0.40
7.2 20.69 0.23
Lihula Terric Anthrosol 7.2 21.70 3.08
(14.86 m a.s.l.) 7.1 20.65 2.86
7.0 20.65 2.97
6.8 17.59 2.54
Eutric Gleysol 7.1 15.61 2.04
(14.34 m a.s.l.) 7.3 4.08 0.54
7.6 1.18 0.24
7.6 0.82 0.17
7.4 3.94 0.74
7.4 1.37 0.26
Molli-Histic 6.7 46.39 13.63
Gleysol
(13.6 m a.s.l.) 6.6 23.84 8.36
7.4 6.43 0.79
Location Soil [K.sup.+] [Na.sup.+] CEC
cmol [kg.sup.-1]
Ilpla-Reo Eutri-Gleyic 0.18 0.32 56.18
Arenosol
0.01 0.00 3.17
0.00 0.00 2.80
0.02 0.00 19.62
Fluvisol? 0.00 0.00 19.95
0.10 0.02 34.04
Molli-Histic 0.15 0.80 92.84
Gleysol
(Histosol) 0.09 0.32 71.60
0.10 0.09 45.01
0.04 0.00 21.13
0.03 0.00 20.96
Lihula Terric Anthrosol 0.96 0.32 26.06
(14.86 m a.s.l.) 1.20 0.37 25.08
1.52 0.37 25.51
1.40 0.37 21.90
Eutric Gleysol 1.04 0.03 18.73
(14.34 m a.s.l.) 0.27 0.12 5.01
0.10 0.08 1.61
0.08 0.05 1.11
0.24 0.13 5.03
0.09 0.06 1.79
Molli-Histic 1.44 0.13 61.59
Gleysol
(13.6 m a.s.l.) 1.68 0.72 34.61
0.36 0.12 7.70
Location Soil SSA
[m.sup.2]
[g.sup.-1]
Ilpla-Reo Eutri-Gleyic 105
Arenosol
9
7
12
Fluvisol? 6
23
Molli-Histic 420
Gleysol
(Histosol) 141
72
13
10
Lihula Terric Anthrosol 86
(14.86 m a.s.l.) 89
96
77
Eutric Gleysol 52
(14.34 m a.s.l.) 19
5
4
19
5
Molli-Histic 259
Gleysol
(13.6 m a.s.l.) 118
10
Table 5. Granulometric composition, g [kg.sup.-1]
Location Soil Horizon and Fractions,
depth, cm [mirco]m
2000-500
Ilpla-Reo Eutri-Gleyic A 0-8 13
Arenosol Bw 8-24 4
C 24-45 4
[C.sub.stariff]. 5
45-69
Fluvisol? ACa 69-85 1
IIG 85-92 8
Molli-Histic H3 92-105 0
Gleysol H3105-117 0
(Histosol) AHG 117-127 9
IIIG 127-143 33
IVG 143-155 9
Lihula Terric [A.sub.terric] 113
Anthrosol 0-13
(14.86 m a.s.l.) [A.sub.terric] 13-26 105
[A.sub.terric] 26-39 115
[A.sub.terric] 39-52 99
Eutric Gleysol A 52-68 118
(14.34 m a.s.l.) Bw 68-78 54
G 78-93 32
IG 93-107 25
107-117 * 485
IIG 117-126 35
Molli-Histic AH 126-131 133
Gleysol
(13.6 m a.s.l.) AH 131-137 58
IIIG 137-147 15
Location Soil Fractions, [mirco]m
500-250 250-50 50-2 <2
Ilpla-Reo Eutri-Gleyic 99 680 184 24
Arenosol 30 954 12 0
14 964 15 3
25 916 37 17
Fluvisol? 8 954 37 0
18 934 216 27
Molli-Histic 0 0 0 0
Gleysol 0 0 0 0
(Histosol) 51 601 316 23
129 620 202 16
50 593 348 0
Lihula Terric 272 484 131 0
Anthrosol
(14.86 m a.s.l.) 239 483 174 0
243 405 225 12
285 442 171 0
Eutric Gleysol 241 514 93 34
(14.34 m a.s.l.) 147 771 10 18
58 901 5 4
75 887 11 2
173 295 47 0
195 755 15 0
Molli-Histic 196 436 225 10
Gleysol
(13.6 m a.s.l.) 88 550 220 84
18 781 158 28
Table 6. Content of pedogenetic nonsiliceous substances, g [kg.sup.-1]
Location Soil Horizon and Total non-
depth, cm siliceous
Fe
Ilpla--Reo Eutric A 0-8 2.8
Arenosol
Bw 8-24 2.2
C 24-45 0.9
[C.sub.stratif] 0.4
45-69
Fluvisol? ACa 69-85 0.7
IIG 85-92 0.6
Molli-Histic H3 92-105 2.3
Gleysol
(Histosol) AH3105-117 1.7
AHG 117-127 1.6
IIIG 127-143 0.3
IVG 143-155 0.3
Lihula Terric [A.sub.terric] 0-13 4.7
Anthrosol
(14.86 m a.s.l.) [A.sub.terric] 13-26 3.6
[A.sub.terric] 26-39 3.9
[A.sub.terric] 39-52 3.6
Eutric Gleysol A 52-68 3.6
(14.34 m a.s.l.) Bw 68-78 2.5
G 78-93 1.2
IG 93-107 0.8
107-117 * 6.4
IIG 117-126 2.2
Molli-Histic AH 126-131 7.0
Gleysol
(13.6 m a.s.l.) AH 131-137 7.7
IIIG 137-147 5.4
Location Soil Amorphous Iron
Fe A1 Si activity,
%
Ilpla--Reo Eutric 2.7 0.6 0.9 96
Arenosol
0.5 0.4 0.9 23
0.2 0.3 0.3 22
0.3 0.2 1.4 75
Fluvisol? 0.7 0.3 0.1 100
0.5 0.4 0.9 83
Molli-Histic 2.2 0.3 0.6 96
Gleysol
(Histosol) 1.6 0.9 0.8 94
0.3 0.7 0.4 19
0.1 0.5 0.8 33
0.2 0.2 0.3 67
Lihula Terric 1.4 0.1 1.4 72
Anthrosol
(14.86 m a.s.l.) 3.6 0.1 0.6 100
3.4 0.1 1.0 87
3.1 0.1 0.9 86
Eutric Gleysol 1.8 1.7 0.3 50
(14.34 m a.s.l.) 2.3 1.2 0.0 92
0.3 0.1 0.3 25
0.3 0.3 0.4 38
3.1 0.1 0.6 48
0.6 0.0 0.5 27
Molli-Histic 6.9 0.3 1.2 99
Gleysol
(13.6 m a.s.l.) 3.6 0.2 1.5 47
2.4 0.1 1.5 44
Table 7. Chemical composition of Eutric Arenosol on Litorina sands
underlain by Molli-Histic Gleysol of Ancylus age, g [kg.sup.-1] of
ignited noncalcareous material
Constituents Modem Eutri-Gleyic Arenosol, cm Fluvisol?, cm
A Bw C C 45-69 ACa JIG
0-8 8-24 24-4 stratified 69-85 85-92
Si 391.5 401.5 472.2 393.9 399.2 399.3
Fe 15.9 7.5 8.1 10.1 8.7 17.4
Al 47.5 40.2 38.8 40.3 38.4 47.1
Ti 2.0 1.2 1.0 1.3 1.6 2.1
P 2.6 1.8 3.2 1.5 2.6 2.8
Ca 40.3 7.3 7.3 47.7 68.3 96.3
Mg 8.5 2.8 2.4 7.1 7.6 13.4
K 21.3 16.5 15.9 15.8 16.5 19.2
Na 5.5 7.0 6.0 5.8 6.7 5.0
Mn 0.2 0.2 0.2 0.6 0.5 0.6
Si/Fe+Al 6.84 8.81 10.66 8.41 9.04 6.94
Si/Fe 49.24 106.72 116.30 78.16 91.98 45.86
Si/Al 7.86 9.60 11.74 6.70 10.03 8.18
At/Mg 4.97 7.01 12.83 5.04 4.49 3.13
Constituents Ancylus-age Mollic Gleysol, cm
AHG IIIG IVG
117-127 127-143 143-155
Si 404.5 417.3 392.1
Fe 20.1 12.3 14.6
Al 49.9 45.8 43.7
Ti 3.0 1.7 2.3
P 2.6 2.9 2.3
Ca 87.4 177.2 157.5
Mg 16.5 14.3 17.1
K 20.5 20.4 17.6
Na 4.9 3.8 2.6
Mn 1.2 0.3 0.3
Si/[Fe.+A1 6.55 7.78 5.34
Si/Fe 40.24 67.75 38.47
Si/Al 7.82 8.79 6.20
At/Mg 2.69 2.85 2.27
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| Author: | Reintam, Loit; Moora, Tanel; Raukas, Anto |
|---|---|
| Publication: | Estonian Journal of Earth Sciences |
| Article Type: | Report |
| Geographic Code: | 4EXES |
| Date: | Dec 1, 2008 |
| Words: | 5548 |
| Previous Article: | Karksilepis parva gen. et sp. nov. (Chondrichthyes) from the Burtnieki Regional Stage, Middle Devonian of Estonia/Karksilepis parva gen. et sp. nov.... |
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