HUMUS SUBSTANCES AND SOIL STRUCTURE
31
ROCZNIKI GLEBOZNAWCZE – SOIL SCIENCE ANNUAL
Vol. 63 No 3/2012: 31–36
DOI 12.2478/v10239-012-0030-3
ERIKA TOBIAŠOVÁ, JURAJ MIŠKOLCZI
Slovak University of Agriculture, Department of Soil Science
HUMUS SUBSTANCES AND SOIL STRUCTURE
Abstract: In this study, the soil structure of two soil types (Haplic Chernozems and Eutric Fluvisols) in four ecosystems (forest,
meadow, urban and agro-ecosystem) with dependence on humus substances were compared. The stability of dry-sieved and waterresistant macro-aggregates and micro-aggregates with a dependence on the proportion of humus substance fractions was determined.
Quantity of humus substances influenced mainly water-resistant aggregates. A positive correlation was recorded between size fraction of 2–3 mm and contents of humus substances (P < 0.01; r = +0.710) and fulvic acids (P < 0.05; r = +0.634), and negative
correlation between size fraction of 0.5–1 mm and contents of humus substances (P < 0.05; r = -0.613) and fulvic acids (P < 0.01;
r = -0.711). Humic acids influenced mainly the formation of dry-sieved aggregates and fulvic acids played an important role in
micro-aggregate formation. The quality of humus substances influenced more intensively the formation of dry-sieved aggregates.
There were positive correlations between optical parameters of humus substances and humic acids and larger dry-sieved aggregates
(3–7 mm) and negative correlations with smaller (0.5–3 mm). The highest proportions of larger size of water-resistant aggregates (1–
20 mm) were in forest ecosystem, but smaller (0.25–1 mm) agreggates were dominated in agro-ecosystem.
Keywords: Humus substances, Soil aggregates, Ecosystems, Haplic Chernozems, Eutric Fluvisols
humus substances and other macromolecules, which
are naturally resistant against microorganisms activiOrganic matter is considered an essential element ty or are physically protected inside the aggregates
in the formation of aggregates [Šimanský 2011; Zey- [Theng et al. 1989]. The subjects of this study are: i)
tin and Baran 2003], and contrast formation of ag- assessment of the impact of humus substances on the
gregates contributes to the stabilization of soil orga- formation of soil aggregates; ii) comparison of soil
nic matter through physical protection within aggre- structure in ecosystems on Haplic Chernozems and
gates [Balabane and Plante 2004]. Relation between Eutric Fluvisols.
soil structure and organic matter is dynamic. The degree of organic matter decomposition affects the forMATERIALS AND METHODS
mation of soil aggregates and their stability [Bonde
et al. 1988. The stability of soil aggregates thus deLocalities of soil sampling are situated in Danube
pends not only on quantity, but also quality of orga- Lowland. Geological substrates of this area are Neonic matter inputs [Tisdall and Oades 1982]. Soil struc- gene clays, sands and gravels, which are in most areture of natural ecosystems is different from the soil as covered with loess and loess loam. Along the river
structure of agro-ecosystems [Šimanský and Zaujec Váh and Nitra are fluvial sediments. The average
2009; Zaujec and Šimanský 2003]. Natural ecosys- annual temperature in the studied localities is 9.8°C
tems accumulate in the surface layer of soil more and average sum of rainfall per year is 570 mm. In
particulate organic matter in soil aggregates and also drier areas of the Danube Lowland oak forests are
organic matter in the much more stabile fractions [Fre- preserved and along the river Váh floodplain forests.
ixo et al., 2002]. Higher concentration of organic car- In vegetation of agro-ecosystems cereals, especially
bon and higher intensity of mineralization is often Zea mays, Triticum aestivum, Hordeum vulgare are
associated with fractions of macro-aggregates. By dominated; there are also Beta vulgaris, Helianthus
contrast, organic carbon in micro-aggregates is more annuus and Brassica napus var. napus. The experiphysically protected and therefore a higher content ment included two soil types – Haplic Chernozems
of biochemical recalcitrant fraction leads to the for- and Eutric Fluvisols and four ecosystems – forest,
mation of stabile micro-aggregates and lower inten- meadow, urban and agro-ecosystem. The soil samsity of decay inside the aggregates [Six et al. 2000]. ples for determination of the quantity and quality of
Stabile organic compounds in soil are represented by soil organic matter and soil structure were taken from
INTRODUCTION
http://versitaopen.com/ssa oraz http://versita.com.ssa
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32
E. TOBIAŠOVÁ, J. MIŠKOLCZI
In Haplic Chernozem more stabilized organic substances dominated, as reflected in a higher proportion of
smaller aggregates, which include more stabile component and vice versa in Eutric Fluvisols less stabile,
so we also recorded a higher proportion of larger aggregates. According to Roberson et al. [1991] different fractions of organic matter participate on the formation and stabilization of aggregates. As organic
matter is gradually stabilizing some binds break down
and new create, thus larger aggregates may be by time
to break down into smaller, in which organic matter is
more stabilized. Therefore, higher content of smaller
aggregates was recorded in Haplic Chernozem and larger in Eutric Fluvisols. In the case of water-resistant
aggregates significantly higher proportion of fractions
from 0.25 to 0.5 mm was in Haplic Chernozems.
From the ecosystems (Table 1) the highest content of organic matter was in forest ecosystem, but its
quality was the highest in the agro-ecosystem, which
is mainly the result of the impact of tillage on organic substances stabilization and application of manure, which also contains humus substances with a high
degree of polycondensation [Nannipieri 1993]. Larger fractions of dry-sieved aggregates (3–20 mm) had
the higher proportion in the urban ecosystem and vice
versa smaller fractions (0.25 to 3 mm) dominated in
the forest ecosystem. These are aggregates, whose
stability have been changing over the change of soil
RESULTS AND DISCUSSION
moisture; due to this situation can be evaluated as
Higher content of total carbon and nitrogen and positive. According to Tisdall and Oades [1982] in canarrower C:N ratio was in Eutric Fluvisols than in se of temporary and unstable aggregates mainly poHaplic Chernozems (Table 1). In soil profile of Eu- lysaccharides, roots and fungal hyphae are binding
tric Fluvisols higher soil moisture was, due to the agents. Larger aggregates had higher proportion in
carbon contents were also higher here compared with the meadow ecosystem. In an urban and also meadow
dry Haplic Chernozems. The close relationship be- ecosystems grass vegetation was, so the formation of
tween soil organic carbon content and soil moisture larger aggregates was conditional mechanically by
were also recorded by Alvarez and Lavado [1998], plant roots. The greater stabilization of aggregates is
Meersmans et al. [2008] and Tobiašová [2010]. Co- in the natural ecosystem, due to this reason a higher
nversely quality of organic substances assessed on content of smaller aggregates was here compared to
the basis of the carbon of humic acids carbon to car- urban ecosystem, which is confirmed by the study
bon of fulvic acids ratio (CHA:CFA) and colour coeffi- Barreto et al. [2009]. They also showed on a higher
cients of humus substances (QHS) and humic acids degree of aggregation under natural vegetation.
(QHA) were higher in Haplic Chernozems than in
The forest ecosystem had the highest proportion of
Eutric Fluvisols. Dry conditions in Haplic Cherno- the fraction of humic acids bound with divalent cazems contributed to higher stabilization of organic tions, and also the fractions of dry-sieved aggregates
matter, which confirmed the results of Denef et al. of size from 0.25 to 3 mm was dominated here and
[2002]. Higher proportion of humic acids was in Ha- from the water-resistant conversely the larger ones.
plic Chernozem, especially of fraction of humic acids
Formation of aggregates is influenced by the stabound with divalent cations. In the case of dry-sie- bility of soil organic matter. In the case of dry-sieved
ved aggregates (Table 2) in Haplic Chernozems gre- aggregates fractions larger than 3 mm were in negaater proportion of smaller aggregates from 0.25 to 5 tive correlation with the stability of organic matter
mm was, while in the Eutric Fluvisols there were lar- and vice versa aggregates smaller than 3 mm was
ger 5–20 mm aggregates. This may be caused just by in positive (Table 3). Less stabilized organic matter
a different quality of organic matter inputs in soil. supported production of larger aggregates, while more
the humus horizon in three replications. From the
chemical properties, organic carbon by wet combustion according to the Tyurin method [Orlov and
Grišina 1981], fractional composition of humus substances according to the Ponomarevova and Plotnikova method [1975], the optical properties of humus
substances [Orlov and Grišina 1981] were determined. From the physical properties, soil structure – drysieved macro-aggregates, water-resistant macro-aggregates according to the Baksejev method and micro-aggregates according to the Kaèinský method
[Hraško 1962], index of aggregate stability [Henin et
al. 1969], the coefficient of vulnerability [Valla et al.
2000], index of crusting and critical contents of soil
organic matter according to Pieri [Lal and Shukla
2004] were determined. The obtained results were
analyzed using statistical software Statgraphic Plus.
In addition to basic descriptive statistical indicators
for the evaluation of the relevance of various factors
on the observed parameters, multi-factorial analysis
of variance (ANOVA) was used. Differences between variants were assessed by Tukey test for significance level P<0.05. To determine interdependencies,
correlation analysis was used. Minimum significant
correlation coefficient was determined on the level
of significance P<0.05 and P<0.01.
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HUMUS SUBSTANCES AND SOIL STRUCTURE
33
TABLE 1. Average values of soil organic mater parameters in soil types and ecosystems
Factors TO C
NT
C:N
CHA:CFA Q HS
Q HA
HA 1
HA 2
HA 3
SHA
[mg×kg–1]
FA 1a FA 1
FA 2
FA 3
SFA
[%]
Soil type
HC
EF
21 370
22 030
2272
2503
9.87
8.46
0.82
0.69
3.71
4.67
3.54
4.02
5.40
4.36
13.73 11.40
9.56 11.81
30.49 4.20
25.74 4.60
7.91
7.96
2.54
3.74
7.08
7.35
21.73
23.65
19 0 5
2549
2 6 15
2484
9.47
10 . 4 1
8.27
8.51
1.11
0.84
0.62
0.47
3.26
4.39
4.08
5.05
3.37
3.67
3.89
4.18
5.54
4.81
4.92
4.25
11.78 12.69
15.06 9.16
6.93 14.36
12 . 8 1 10 . 2 1
29.95
29.04
26.20
27.27
9.81
9.44
6.38
6.12
1. 3 3
2.96
1. 8 7
6.42
8.16
8.46
6.61
5.64
23.72
25.43
19.13
22.48
Ecosystem
AL
FE
ME
UE
18 0 8 0
25 930
21 620
2 1 18 0
4.44
4.58
4.28
4.31
Explanations: HC – Haplic Chernozems, EF – Eutric Fluvisols, FE – forest ecosystem, AL – agro-ecosystem, ME – meadow ecosystem, UE – urban
ecosystem, TOC – total organic carbon, NT – total nitrogen, C:N – carbon and nitrogen ratio, CHA:CFA – humic acids carbon and fulvic acids carbon
ratio, QHS – colour coefficient of humus substances, QHA – colour coefficient of humic acids, HA 1 – fraction of humic acids free and bound with
mobile R2O3, HA 2 – fraction of humic acids bound with Ca2+, HA 3 – fraction of humic acids bound with mineral particles of soil and with stabile
R2O3, SHA – sum of humic acids, FA 1a – free aggressive fulvic acids, FA 1 – fraction of fulvic acids free and bound with mobile R2O3,
FA 2 – fraction of fulvic acids bound with Ca2+, FA 3 – fraction of fulvic acids bound with mineral particles of soil and with stabile R2O3, SFA – sum
of fulvic acids.
TABLE 2. Average contents of air dry and water-stable macro-aggregates in soil types and ecosystems
Factors
2–7 mm
D
7–5 mm 5–3 mm 3–1 mm 1–0.5 mm 0.5–0.25 mm 3–2 mm 2–1 mm 1–0.5 mm 0.5–0.25 mm <0.25 mm
D
D
D
D
D
W
W
W
W
W
[%]
Soil type
HC
EF
7.93
12.80
20.68
25.46
28.16
26.73
26.31
23.15
9.84
7.18
3.29
2.44
11.30
11.66
13.60
12 . 9 4
11.99
10.76
10 . 4 7
7.57
16 . 3 9
6.78
11.41
6.23
9.74
14.09
21.29
18.06
24.29
28.64
25.28
25.87
29.08
29.55
26.95
29.36
22.23
20.38
10.08
12.15
7.32
4.49
2.85
4.59
2.52
1.51
2.18
19 . 7 2
10.08
13.94
12 . 2 6
17.32
14 . 8 8
8.62
20.78
9.96
8.56
6 . 18
22.98
4.52
7.60
0.98
14 . 2 9
5.90
18 . 6 6
7.50
Ecosystem
AL
FE
ME
UE
Explanations: HC – Haplic Chernozems, EF – Eutric Fluvisols, FE – forest ecosystem, AL – agro-ecosystem, ME – meadow ecosystem, UE – urban
ecosystem, D – dry-sieved macro-aggregates, W – water-resistant macro-aggregates.
TABLE 3. Correlations between soil organic mater parameters and dry-sieved and water-resistant macro-aggregates
Dry- sieved macro- aggregates
Water- resistant macro- aggregates
2–7 mm 7–5 mm
5–3 mm
3–1 mm
1–0.5 mm 0.5–0.25 mm 3–2 mm
2–1 mm
1–0.5 mm 0.5–0.25
mm
- 0.255
- 0.076
- 0.253
- 0.078
+ 0.408
- 0.708**
- 0.028
+ 0.361
-0.579*
- 0.115
- 0.497
+0.518
+0.172
+ 0.499
- 0.347
+0.011
+0.778** +0.754**
+ 0.239
+0.212
+ 0.052
- 0.209
- 0.513
+ 0.443
- 0.341
-0.535*
+0.211
CHA:CFA - 0.094
Q HS
+ 0.260
Q HA
+ 0.220
- 0.523
+0.575*
+0.591*
- 0.365
+ 0.395
+ 0.532
+ 0.485
-0.596*
-0.565*
+ 0.452
-0.568*
-0.678**
+ 0.278
- 0.337
- 0.511
+0.119
+ 0.255
+ 0.074
+0.719** +0.222
-0.565*
-0.657*
-0.594*
- 0.449
+ 0.397
-0.739**
- 0.471
HA 1
HA 2
HA 3
SHA
+0.019
-0.603*
+ 0.037
-0.657*
- 0.469
-0.616*
+ 0.253
-0.726**
- 0.446
- 0.131
+0.197
- 0.194
+0.158
+0.822**
- 0.461
+0.661**
+0.512
+0.606*
- 0.300
+0.698**
+ 0.449
+ 0.398
- 0.068
+0.606*
- 0.192
+ 0.049
+ 0.001
- 0.014
+ 0.470
+0.170
- 0.083
+ 0.347
+0.173
+ 0.432
- 0.242
+ 0.373
+ 0.404
+0.199
+ 0.054
+ 0.443
FA 1a
FA 1
FA 2
FA 3
SFA
- 0.277
- 0.179
- 0.166
- 0.391
-0.559*
+ 0.084
- 0.520
- 0.048
- 0.006
+ 0.309
+ 0.288
- 0.495
+ 0 . 2 14
+ 0.291
+ 0.201
- 0.105
+ 0.372
+ 0.292
- 0.052
+ 0.454
- 0.098
+0.536*
- 0.078
+ 0.001
+0.178
+0.151
+0.611*
- 0.261
+ 0 . 3 18
+ 0.261
+ 0.389
- 0.187
+0.113
+0.171
+0.197
- 0.297
+ 0.307
+0.147
- 0.499
- 0.044
- 0.326
+ 0.302
+ 0 . 19 7
- 0.463
+ 0.024
-0.532*
+ 0.291
+ 0.028
-0.623*
- 0.297
TO C
NT
C:N
- 0.384
-0.602*
+ 0.269
Explanations: * P < 0.05, ** P< 0.01; TOC – total organic carbon, NT – total nitrogen, C:N – carbon and nitrogen ratio, CHA:CFA – humic acids
carbon and fulvic acids carbon ratio, QHS – colour coefficient of humus substances, QHA – colour coefficient of humic acids, HA 1 – fraction of
humic acids free and bound with mobile R2O3, HA 2 – fraction of humic acids bound with Ca2+, HA 3 – fraction of humic acids bound with mineral
particles of soil and with stabile R2O3, SHA – sum of humic acids, FA 1a – free aggressive fulvic acids, FA 1 – fraction of fulvic acids free and
bonded with mobile R2O3, FA 2 – fraction of fulvic acids bound with Ca2+, FA 3 – fraction of fulvic acids bound with mineral particles of soil and
with stabile R2O3, SFA – sum of fulvic acids.
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34
E. TOBIAŠOVÁ, J. MIŠKOLCZI
stabilized, especially humus substances supported the
formation of aggregates of smaller fractions, which
is consistent with the theory of Six et al. [2000].
From the humus substances there were humic
acids, which were in a positive correlation with the
aggregates of size 0.5–3 mm, in particular, a fraction
of humic acids bound with divalent cations (Ca2+,
Mg2+), with whose they form humates, which are
small water soluble. Therefore they have importance
in the aggregation process, when they create a thin
layer on the surfaces of mineral particles, which act
as binding agents in case of smaller aggregates. The
stabilization of organic substances in the case of smaller aggregates also occurs through their bonds with
the clay fraction [Jastrow 1996]. Such a bond is more
stabile and more resistant against decomposition activity of soil organisms. Organic matter in smaller
aggregates is protected through the inhibition of carbon oxidation [Hernanz et al. 2002]. In larger fractions of aggregates a greater proportion has sand fraction and in smaller aggregates fraction of clay. Organic matter, which is part of larger aggregates, is largely composed of particulate organic matter and there are also structural substances, which subject rather the process of mineralization than the stabilization. In the case of aggregate fraction of 0.25–1 mm
a positive correlation with the fraction of fulvic acids
bound with monovalent cations was found.
Formation of aggregates was strongly influenced
not only by the quantity of humic acids, but also their
quality (Table 3). From the individual fractions positive influence on their stability, fraction of humic
acids bound with divalent cations had. The more stabilized humic acids were, the higher proportion of
aggregates from 0.5 to 3 mm was.
In case of narrower C:N ratio in soil organic matter, higher proportion of 3–7 mm aggregates was and
in case of wider C:N ratio larger proportion of smaller 0.25–1 mm aggregates was. Rate of nitrogen mineralization is higher, thus over time the ratio of C:N
extends to what also the results of Gregorich et al.
[2003] showed. This also indicates the presence of
fresh organic matter in the larger aggregates.
In the case of water-resistant aggregates (Table 1)
correlation between the quality of humus substances
and water-resistant aggregates of size <2 mm was
observed. In case of the CHA:CFA ratio this correlation was positive and in the case of colour coefficients was negative. The higher the contents of nitrogen, fulvic acids fractions of free and bound
with R2O3 were, the smaller the content of water-resistant 0.25-0.5 mm aggregates was. Tisdall and Oades
[1982] describe as permanent aggregates these, on
whose formation degraded aromatic humus substances in connection with polyvalent metal ions, which
are strongly bound to clay particles participate.
Micro-aggregates (Table 4) had a higher proportion in Haplic Chernozems (16.39%) than in Eutric
Fluvisols (6.78%). It also shows on a higher proportion of stabile organic substances in the formation of
smaller aggregates. According to Bedrna et al. [1968]
in this case it can be the formation of micro-aggregates not only by adsorption on the surfaces, but also
by diffusion of humus substances into interlayer spaces of clay minerals lattice. Aggregate fraction of 0.010.05 mm had higher proportion in Haplic Chernozems and all other fractions had higher contents in
Eutric Fluvisols. The higher the total organic carbon
and wider C:N ratio were, the higher proportion of
micro-aggregates of fraction 0.01–0.05 mm was (Table 5). This fraction was also in negative correlation
with fraction of fulvic acids bound with divalent cations (r =-0.691, P>0.01). From the ecosystems this
fraction of micro-aggregates had the highest proportion in the forest ecosystem, in which the highest input of organic matter with a wider C:N ratio and higher content of fulvic acids were. Therefore, in these
conditions micro-aggregates of size from 0.01 to 0.05
mm will have the highest proportion.
Overall, in the case of micro-aggregates fulvic
acids play important role. Negative correlation was
recorded between the proportion of micro-aggregates of size <0.001 mm and a content of free fulvic
acids and bound with mobile R2O3 (r =- 0.594, P>
0.05) and positive correlation with a fraction of fulvic acids bound with divalent cations (r= 0.622,
P>0.05). Rehák and Janský [2000] described the formation of smaller micro-aggregates (<0.01 mm) as a
result of cohesion forces, which are the result of a
large number of contact points and surfaces in voluTABLE 4. Average contents of micro-aggregates in soil types and
ecosystems
Factors 2–0.25 0.25–0.05 0.05–0.01 0.01–0.001 <0.001
mm
mm
mm
mm
mm
[%]
Soil types
HC
EF
16.48
20.78
16.33
21.06
50.26
35.49
13.68
17.55
3.25
5.12
22.06
20.92
24.71
7 . 10
38.04
47.21
43.94
42.32
18.13
11.85
13 . 9 4
18.98
4.37
3.28
4.06
5.04
Ecosystem
AL
FE
ME
UE
17.42
16.76
13.77
26.58
Explanations: HC – Haplic Chernozems, EF – Eutric Fluvisols,
FE – forest ecosystem, AL – agro-ecosystem, ME – meadow ecosystem,
UE – urban ecosystem.
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HUMUS SUBSTANCES AND SOIL STRUCTURE
TABLE 5. Correlations between soil organic mater parameters
and micro-aggregates
Micro- aggregates
2- 0.25
mm
0.25- 0.05 0.05- 0.01 0.01- 0.0- <0.001
mm
mm
01mm
mm
- 0.422
- 0.246
- 0.275
- 0.179
- 0.143
- 0.122
+0.744** - 0.462
+ 0.406 - 0.237
+0.585* - 0.374
- 0.223
+ 0.054
- 0.416
CHA:CFA +0.062
Q HS
+ 0.252
Q HA
+0.216
+ 0.294
- 0.272
+ 0.005
- 0.181
- 0.123
- 0.377
- 0.141
+0.165
+ 0.308
+0.010
+ 0.256
+ 0.207
HA 1
HA 2
HA 3
SHA
- 0.318
+ 0.030
-0.536*
- 0.511
+ 0.236
- 0.006
+ 0.021
+0.119
+ 0.336
+0.115
+ 0.249
+ 0.468
- 0.363
- 0.173
+ 0.249
- 0.173
- 0.383
- 0.157
- 0 . 18 0
- 0.487
FA 1a
FA 1
FA 2
FA 3
SFA
+ 0.205
- 0.440
+ 0.300
- 0.258
+ 0 . 2 14
+0.139
+ 0.435
+0.154
+ 0.021
+ 0.427
- 0.203
+ 0.307
-0.691**
+ 0.505
- 0.303
- 0.211
- 0.348
+0.140
- 0.482
- 0.364
+ 0.398
-0.594*
+0.622*
- 0.288
+ 0.247
TO C
NT
C:N
Explanations: * P < 0.05, ** P< 0.01; TOC – total organic carbon, NT –
total nitrogen, C:N – carbon and nitrogen ratio, CHA:CFA – humic acids
carbon and fulvic acids carbon ratio, QHS – colour coefficient of humus
substances, QHA – colour coefficient of humic acids, HA 1 – fraction of
humic acids free and bound with mobile R2O3, HA 2 – fraction of humic
acids bound with Ca2+, HA 3 – fraction of humic acids bound with mineral particles of soil and with stabile R2O3, SHA – sum of humic acids,
FA 1a – free aggressive fulvic acids, FA 1 – fraction of fulvic acids free
and bound with mobile R2O3, FA 2 – fraction of fulvic acids bounded
with Ca2+, FA 3 – fraction of fulvic acids bound with mineral particles
of soil and with stabile R2O3, SFA – sum of fulvic acids.
me unit, and sodium or electrolytes contribute to increasing of cohesion. Through this mechanism just a
fraction of free fulvic acids bound with mobile R2O3
could participate in the formation of smaller microaggregate factions.
CONCLUSIONS
1. Proportion of larger dry-sieved macro-aggregates
(>3 mm) was in negative correlation with the stability of organic substances and contrast, smaller
macro-aggregates (<3 mm) in positive correlation.
Quantity and quality of humic acids, in particular
those, which are bound with divalent cations, was
in positive correlation with the aggregates of size
0.5-3 mm.
2. Proportion of water-resistant aggregates of size
fraction <2 mm was in positive correlation with
the ratio of humic acids carbon to fulvic acids carbon and in negative correlation with colour coefficients. The higher the proportion of fulvic fractions of free and bound with R2O3 was the smaller
water-resistant aggregates content of size fraction
0.25–0.5 mm was.
3. In case of micro-aggregates negative correlation
between the proportion of size fraction <0.001 mm
35
and a fulvic acids of free and bound with mobile
R2O3 was recorded and positive correlation with
fulvic acids bound with divalent cations.
4. In the forest ecosystem micro-aggregate fraction
of size from 0.01 to 0.05 mm was dominated and
also the content of smaller dry-sieved macro-aggregates fractions (0.25–3 mm) was the highest,
and on the other hand larger fractions (3-20 mm)
had the highest proportion in the urban ecosystem.
In Haplic Chernozems a higher proportion of smaller dry-sieved macro-aggregates (0.25–5 mm)
were, while in Eutric Fluvisols larger macro-aggregates (5–20 mm) were dominated.
Acknowledgements
The work was financially supported by project
VEGA 1/0300/11 and VEGA 1/0237/11.
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Erika Tobiašová
Tr. A. Hlinku 2, 949 01 Nitra, Slovak Republic
[email protected]
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