Zawartość różnych form związków próchnicznych w glebach rdzawych bielicowanych i w bielicy, wytworzonych z piasków wodnolodowcowych

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R O C Z N IK I G L E B O Z N A W C Z E T. X X V , D O D A T E K , W A R S Z A W A 1974

F R A N C IS Z E K K U Ż N IC K I, P IO T R S K Ł O D O W S K I1

C O N T E N T OF V A R IO U S F O R M S O F H U M U S C O M P O U N D S

IN P O D Z O L IZ E D R U S T Y SO ILS A N D P O D Z O L ,

D E V E L O P F R O M F L U V IO G L A C IA L S A N D S

Institute fo r Economical Geodesy, Soil Science Laboratory,

W arsaw Technical U niversity

The investigating comprise five profiles developed from hydroglacial

sands of the Baltic glaciation, three profiles of which (1, 2 and 3) are

situated in the Kurpiowska plain, on the territory of Myszyniecka Forest

and two profiles <4 and 5) on the territory of Piska Forest in the

Mazurian Lake-land.

The profiles 1, 2 and 3 have been established northwards Ostrołęka,

within the reach of the Poznań stage esiker covering the Leszno stage

sediments, while the profiles 4 and 5 are situated within the reach of

the Poznań stage near the outer embankment of frontal moraine [1, 8, 15].

In the esker field sediments, along with the taking away distance from

glacier by water, the grain size gradually decreases and mineral com

position becomes poorer (profiles 1, 2, 3 as compared with profiles

4 and 5) [1].

The podzolization degree of soils developed from esker sands is affect

ed by many factors, and, above other things, by the age of parental

formations and their mineral composition as w ell as by the transport of

material determining its segregation. A n important role in the podzoliz

ation process play water conditions on which depend the organic matter

transformations and the mobilization of mineral elements. O f the esker

sands with finer material and strongly rinsed dunes are formed more

readily and from them weakly formed soils develop, which can undergo

podzolization in further evolution stages. From sands with coarser ma

terial, richer in minerals, from weakly formed soils podsolized rusty

soils are developing, further evolution of which in the direction of typical

soils is running rather slow. Rusty soils, distinguished in the

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1 8 6

F. Kuźnicki, P. Skłodowski

tics of Polish soils in the class of podzol-earths as a type and podzolized

rusty soils as a subtype, comprise weakly podzolized soils, developed

mainly from sands of different origin. In morphological aspect rusty soils

do not reveal any podzolization features, while podzolized rusty soils

distinguish themselves with very w eak podzolization degree [1, 2, 9, 16].

From the viewpoint of physicochemical properties, considerable differen

ces occur between rusty and podsol soils, justifying the correctness of

separating in the systematics of these soils the above two typological

units [16].

The aim of the present work was to investigate, whether any differ

ences exist between podzolized rusty soils (leptic podzols after F A O )

and podzols with regard to the content of different forms of humus com

pounds, or in other words whether is possible to regard the content of

different humus compound forms in these soils as one of the criteria

enabling separation of these two units. The method of organic matter

analysis according to Duchaufour and Jacquin, applied in the work, was

described several times in previous works of the same authors concern

ing content of humus compounds in these soils, and therefore no special

commentary is needed [4, 10].

IN V E S T IG A T IO N R E S U LTS

Am ong 22 profiles, described and analyzed in every detail, samples

from the genetic horizons of five most characteristic forest soil outcrops

were taken for investigations. In the profile 1 representing podzol devel

oped from loose esker sand humus compound forms in the А 0, А ХА Ъ A s

and B h horizons w ere analyzed, while in the profiles 2, 3, 4 and 5,

representing podzolized rusty soils developed from loose esker sand,

humus compound forms in the samples taken from the A 0, A XA 2 and B r2

horizons were comprised with the analysis. From the physico-chemical

properties point of 2 acid reaction in upper horizons, considerable exchan

geable and hydrolytic acidity and a low saturation degree with basic

cations (below 20%) increasing along with the profile depth.

W ith regard to mineral composition they are sands of the fraction

of 0.2-0.06 onm, unusually variable and rich in heavy minerals. Mineral

composition of heavy fraction of the samples analyzed leads to the

presumption that the source of the majority of elements would constitute

crystalline rocks carried aw ay by the glacier [1].

W hile discussing the investigation results the content both of free

(light) fraction and bounded (heavy) fraction must be taken into account.

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Content of various form s of humus compounds... ₁₈₇

T a b l e

1

Content of free fraction and bounded fraction in the organic matter of soils

Locality Profile No.Horizon

Sam pling depth cm

Weight per cent in relation to analyzed sample Total

С % of С content in relation to soil In % of total С free frac tion bounded frac tion % free frac tion bounded frac tion free frac tion bounded frac tion Budy Prywatne, profile 1 Ao A1A2 a2 Bh +0-5 0-3 5-15 16-28 78.89 18.67 2.66 7.14 2 1 .1 1 87.33 97.34 92.86 29.874 5.382 0.292 1.538 29.726 4.946 0.102 0.690 0.148 0.436 O.I9O 0.848 99.50 91.89 35.82 44.86 0.50 8.11 64.18 55.14 Budy Prywatne, profile 2 Ao A1A2 Br +0-4 0-5 10-30 91.28 15.19 2.30 8.72 84.81 97.70 37.085 3.339 0.318 36.945 2.649 О.О34 0.140 О.49О 0.284 99.65 85.33 10.68 0.35 14.67 89.32 Łodziska, profile 3 Ao A1A2 Br +0-4 0-7 7-20 76.39 10.13 4.61 23.61 89.87 95.39 33.400 2.859 0.451 33.236 2.519 0.II5 0.164 0.340 0.336 99.51 88.10 25.49 О.49 11.90 74.51 Wiartel, profile 4 Ao A1A2 Br 0-4 4-8 15-30 80.06 25.59 3.34 19.94 74.41 96.56 35.162 6.796 1.018 34.989 6.267 0.338 О.17З О.529 0.680 99.50 92.22 33.20 0.50 7.78 66.80 Szeroki Bór, profile 5 Ao A1A2 Br 0-3 3-10 20-40 91.96 13.32 2.13 8.04 86,68 97.87 35.662 3.195 0.649 35.533 2.600 0.161 O.I29 0.595 ‘0.488 99.60 82.35 24.80 0.40 17.65 75.20

Free fraction, as compared with bounded one consists usually of weaker

polymerized humus compounds [4, 5, 10].

The total С content in the A 0 horizon of all profiles is fairly high,

varying within the limits of 30-37%. Bounded fraction (0.4-0.5% in relation

to total C) plays inconsiderable role as compared with freee fraction

(about 99% in relation to total C). The humification degree in this

horizon is low one (8-10%), while the residuum (R) content, constituting

non-extracted free fraction part of organic matter is high, exceeding

90% С (in per cent of total C). As it is evident from the above data,

the upper organic matter layer A 0 in all the profiles investigated could

be determined as so-called raw humus-mor. The total С content in the

humus-eluvial horizon А гА 2 is high in all profiles (2.9-6.8%), at which

a significant role plays also free fraction (82-92% in relation to total C).

The humification degree in this horizon shows rather wide fluctu

ations (18-40%).

Significant differences with regard to both total С and humus com

pound forms occur between the B h horizon of podzol and the B T horizon

of podzolized rusty soils.

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Content of different humus compound forms in soils determined in the organic matter fractions /4/ T a b l e 2 £

00

С fractioning in % of total ( Locality . Käme of soil Pro fi le No. Ho rizon Samp ling depth cm С free fraction bounded fraction % 1st extraction . II nd extraction _R I St extraction U n d extraction Illrd extraction Hu mines P1 H1 F2 H2 *3 H3 P4 H4 F5 H5 H Budy Prywatne Iron-Humus Podsol 1 W k 2 4 +0-5 0-3 5-12 16-18 29.874 5.382 0.292 1.538 4,26 5.57 3.04 11.05 2.72 6.02 9.46 13.98 1.51 4.29 6.76 3.51 1.00 5.31 0.68 3.71 90.01 70.70 15.88 12.61 0.16 3.47 35.47 24.58 0.02 0.50 4.39 5.72 0.02 1.45 9.12 1.10 0.02 0.84 4.05 4.42 0.02 0.63 5.40 0.86 0.01 0.83 4.73 4.68 0.25 0.39 1.02 13.78 Budy Prywatne

Podzolized rusty soil

2 A°A +0-4 0-5 10-30 37.085 3.339 0.318 3.19 4.58 1.89 1.93 9.13 3.14 1.38 2.04 2.83 1.60 4.70 0.31 91.55 64.87 2.51 0.07 6.23 46.54 0.00 0.18 11.63 0.00 0.81 11.63 0.00 0.54 4.09 0.01 1.53 10.38 0.00 0.48 4.40 0.27 4.91 0.65 Lodziska

3 A°A Bp +0-4 0-7 7-20 33.400 2.859 0.451 3.96 5.14 10.64 2.48 4.72 1.11 0.97 2.31 3.99 1.42 1.89 1.55 90.68 74.04 8.20 0.18 6.85 47.89 0.01 0.70 2.88 0.01 0.07 5.99 0.01 0.56 5.54 0.02 0.73 5.5^ 0.02 0.70 5.12 0.24 2.29 1.55 Wiartel

Podzolized rusty söil

4 a°a2 Br 0-4 4-8 15-30 35.162 6.796 1.018 2.21 1.43 10.02 2.68 1.53 5.11 1.39 2.13 4.12 1.39 4.99 3.54 91.83 82.14 10.41 0.17 3.99 32.32 0.02 0.79 6.68 0.01 0.34 5.50 0.01 0.38 3.34 0.08 0.47 9.63 0.01 0.56 4.22 0.20 1.25 5.11 Szeroki Bór

5 An

Bi

0-3 3-10 20-40 35.662 3.195 0.649 2.59 6.73 2.00 2.80 10.98 5.85 1.09 2.00 2.93 1.10 2.13 3.70 92.02 59.53 10.32 0.09 8.89 48.84 0.01 1.19 4.01 0.03 0.12 2.00 0.01 1.88 5.24 0.03 1.53 5.24 0.02 1.28 6.32 0.21 2.74 3.55

Explanation of the symbols: F^ fulvic acids in free fraction E1 humic acids in free fraction

1st extraction F^ fulvic acids in bounded fraction 11^ humic acids in bounded fraction

U n d extraction

Fg fulvic acids in free fraction H0 humic acids in free fraction

U n d extraction F^ fulvic acids in bounded fraction humic acids in bounded fraction

Illrd extraction

F^ fulvic acids in bounded fraction Ня humic acids in bounded fraction

extraction R residuum of the non-extracted free fraction part

H "humines" - unsoluble part of bounded fraction after 3 extractions 1st extraction by means of the Na^PgO^

lind extraction by means of the Na^PgOr, 117rd extraction 0.1 К NaOH solution

NagSO^ solution with pH»7 solution with pH=9*8

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T a b l e

3

Sumary content of different organic compound forms in particular fractions and the values characteristic for humification

Locality Profile Ho. Gene tic hori zon Sam pling depth cm Total С

С of fulvic and humic acids and of humines of total С

H:F rdtio Humifi cation degree C:N ratio

% of С content in particular fractions in relation to soil

free

fraction bounded fraction free fraction bounded fraction

Fi+F2 H1+H2 _2+Fg w 5 humines H R Fi+F2 H1+H2 _^+f£ h,+h + 5 huminei H 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 Budy Prywatne Profile 1 Ao a1A2 a2 Bh +0-5 о-з 5-15 16-28 29.874 5.382 0.292 1.538 5.77 9.86 9.80 14.56 3.72 11.33 10.14 17.69 0.20 5.55 49.99 26.54 0.50 2.17 13.17 14.82 0.25 0.39 1.02 13.78 0.65 0.87 0.40 0.64 9.99 29.30 84.12 87.39 29.3 20.1 13.4 26.3 26.889 3.805 0.047 O.I94 1.724 О.5З1 О.О29 0.224 1.113 0.610 0.030 0.272 0.061 О.299 0.148 0.408 0.011 0.116 0.039 0.228 0.076 0.021 0.003 0.212 Budy Prywatne Profile 2 Ao A1A2 Br +0-4 0-5 10-30 37.085 3.339 0.318 4.57 6.62 4.72 3.53 13.83 3.45 0.08 8.56 68.55 0.00 1.20 20.12 0.27 4.91 0.65 0.76 0.99 0.32 8.45 35.13 97.49 29.8 20.3 1З .5 33.953 2.166 0.008 1.683 0.221 O.OI5 1.309 0.462 0.011 0.033 0.286 0.218 0.006 0.040 0.064 0.101 0.164 0.002 Łodziska Profile 3 Ao A1A2 Br +0-4 0-7 7-20 33.400 2.859 0.451 4.93 7.45 14.63 3.90 6.61 2.66 0.21 7.65 59.42 0.04 1.96 13.54 0.24 2.29 1.55 0.77 0.57 0.22 9.32 25.96 91.80 33.6 19.7 18.1 30.286 2.117 0.037 1.647 O.2I3 0.066 1.303 0.189 0.012 0.067 O.219 0.268 0.016 0.056 0.061 0.081 0.065 0.007 Wierteł Profile 4 Ao A1A2 Br 0-4 4-8 15-30 35,162 6.796 1.018 3.60 3.56 14.14 4.07 6.52 8.65 0.26 4.80 47.45 0.04 1.73 14.24 0.20 1.25 5,11 1.06 0.99 0.30 8.17 17.86 89.59 30.4 20.9 15.8 32.29О 5.582 0.106 1.266 0.242 0.144 I.433 0.443 0.088 O.O9O 0.326 0.483 0.012 0.118 0.145 O.O7 I 0.085 О.О52 Szeroki Bór Profile 5 Ao A1A2 Br о-з з - ю 20-40 35.662 3.195 0.649 3.68 8.73 4.93 3.90 13.11 9.55 0.15 10.56 56.08 0.04 4.35 15.57 0.21 2.74 3.55 1.03 0.86 0.20 7.98 40.47 89.68 З2.9 24.5 12.5 32.817 I.902 0.067 1.314 0.279 О.О32 1.402 0.419 0.062 0.049 0.369 0.364 O.OO5 0.139 0.101 0.075 0.087 0.023 00

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190

F. Kuźnicki, P. Skłodowski

In the B h horizon the total С content amounts to about 1.5% while

in the B r horizon the total С content varies within 0.3-1.0%. Bounded

fraction prevails in either case over free fraction, particularly in podzol

ized rusty soils. In the B h horizon the free fraction content is almost

twice higher than in the B r horizon.

Very interesting differences are observed between the content of

fulvic acids in free and bounded fraction in the B h and B T horizon.

In free fraction the content of fulvic acids of the first extraction in

the B h horizon is usually higher than in the B r horizon while in bounded

fraction is inversely: fulvic acids of the first extraction show a consid

erable predominance in the B r horizon as compared with the B h horizon.

Simultanously it ought to be noted that in the B h horizon several teen

times more humines are contained than in the B r horizon. It proves a far

advanced condensation and stabilization of humus compounds under in

fluence of iron hydroxids and aluminium in the B h horizon of podzol as

compared with the B r horizon of podzolized rusty soils [3, 5, 7, 9].

A significant difference between the B h and the B r horizon occurs in

the H :F ratio, amounting in the B h horizon to 0.64 and in the B r horizon

fluctuating within 0.20-0.32. In either case fulvic acids prevail over humic

ones, the percentage of humic acids in the B h horizon of podzol being,

however, 2-3 times higher than in the B r horizon of podzolized rusty soils.

On the whole it can be stated that the organic matter evolution in

podzol is more advanced than in podzolized rusty soils, what is connected

with the totality of ecologic conditions.

The C :N ratio in the A 0 horizon of podzolized rusty soils is somewhat

higher than in podzol. In the A XA 2 horizon of these both typological

units no significant differences in this respect can be noted, while in

the B h horizon this ratio is much higher as compared with the B r horizon,

what is connected with higher content of most mobile fulvic acids of the

first extraction with a low specific gravity in free fraction of this horizon

as w ell as with higher total С content. The residuum (R) content in the

B h horizon is usually higher than in the B T horizon.

The investigations explain the role of humus in the podzolization

process. The soil podzolization degree depends to a considerable extent

on percentage and of particular humus compound forms and their inter

relation. The investigations of К o n o n o w a [7] and other authors [3. 5,

14] have proved that organic substances remaining in acid solutio upon

precipitation of humic acids, known under the name of fulvic acids,

distinguish themselves with complicated structure.

Many authors [6, 11] have proved that in these acids, among others,

carboxylic, phenolic and other groups are contained.

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Content of various form s of humus compounds., ₁₉₁

play a significant role in the podzolization process, constitutes a separate

question, requiring a special study.

The results of the authors’own investigations prove that the organic

matter transformations in podzolized rusty soils are running differently

than in podzol, what probably is connected with drier soil climate of this

typological unit. The hypothesis can be put that in rusty soils physical

and chemical weathering of rocky material distinctly revails over biolo

gical one. It is to stress, however, that rusty soils assigned in the

Systematics of Polish Soils to the podzol-earth class [16] do not constitute

any uniform group. The differences occuring between proper and pod

zolized rusty soils result from the mineral composition of parental rooks

and the totality of ecological conditions [16].

On the whole it can be concluded that the origin of sands as parental

formations of the soils investigated exerts a decisive influence on soil

podzolization degree, depending to a considerable extent on organic

mater transformations.

R EFERENCES

[1] B i a ł o u s z S.: W p ły w m orfogenezy P ojezierza Mazurskiego na kształtowanie

się gleb. W arszawa 1970 (doctor’s thesis).

[2] B o r o w i e c S.: Zagadnienia gleboznaw czo-siedliskow e W olińskiego Parku N a

rodowego. W arszawa 1969, P W R iL .

[3] B r u c k e r t S., J a c q u i n F.: Contribution a l ’étude de la condensation des

composés organiques au cours de l ’hum ification en m ilieu podzolique. E xtrait

du ».Bulletin de l ’Ecole Nationale Supérieure Agronom ique de N an cy” . 13, 1971,

1, 28-35.

[4] D u c h a u f o u r P., J a c q u i n F.: Nouvelles recherches sur l ’extraction et le

fractionnem ent des composés humiques. E xtrait du „B ulletin de l ’Ecole N a

tionale Supérieure Agronom ique de N ancy” . 8, 1, 1966, 24.

[5] D u c h a u f o u r P.: Processus de form ation des sols (Biochim ie et Geochimie).

C.R.D.P. Nancy 1972, s. 182.

[6] K o n e c k a - B e t l e y K . : Zagadnienie żelaza w procesie glebotwTórczym. Rocz.

glebozn. 19, 1968, 1.

[7] К o n o n o w a М. М.: Substancje organiczne gleby, ich budow-a, właściwości

i m etody badań. W arszawa 1968, P W R iL , s. 391.

[8] K o n d r a c k i J.: G eografia fizyczna Polski. W arszawa 1965, PW N .

[9] K u ź n i c к i F., B i a ł o u s z S., R u s i e c k a D., S k ł o d o w s k i P.: Charak

terystyka procesu bielicowania w glebach w ytw orzonych z piasków w yd m o

w ych Puszczy Kam pinoskiej. Rocz. glebozn., 1973.

[10] K u ź n i c k i F., S k ł o d o w s k i P.: Przem iany substancji organicznej w n ie

których typach gleb Polski. Rocz. glebozn. 19, 1968, 1, 3-25.

[11] M u s i e r o w i c z A., Próchnica Gleb. W ydanie I I uzupełnione. W arszaw a 1964,

P W R iL , s. 106.

[12] P r u s i n k i e w i c z Z., N o r y ś k i e w i c z B.: Zagadnienie w ieku bielic na

wydm ach brunatnych m ierzei Św iny w św ietle analizy palynologicznej i

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dato-192

F. Kuźnicki, P. Skłodowski

w ania radiow ęglem С 14. Zesz. nauk. Uniw. M. Kopernika w Toruniu, z. 14,

G eografia V, 1966, 75-88.

{13] P r u s i n к i e w i с z Z., Bitum iny w próchnicy glebow ej. Rocz. glebozn., 21,

1970, 2, 525-530.

[14] P o s n e r A. M., T h e n g В. G. G., W a k e J. R. H.: The extraction of

soil

organic m atter in relation to hum ification. Trans.

9th. Congr. Int. Soil Sei.

Soc., t. 2, 1968. s. 153.

[15] R ó ż y c k i S. Z.: Plejstocen Polski środkowej. W yd. II. W arszaw a 1972, P W N ,

s. 315.

[16] System atyka gleb Polski. Opracowanie zbiorow e K om isji Genezy, K la sy fik a cji

i K a rto g ra fii Gleb P T G . Rocz. glebozn. 25, 1973, 1.

Ф. КУЗЬН И Ц КИ , П. СКЛОДОВСКИ

С О Д Е Р Ж А Н И Е Р А З Л И Ч Н Ы Х Ф О Р М Г У М У С Н Ы Х С О ЕДИ Н ЕН И Й

В Р Ж А В Ы Х П О Д З О Л Е Н Н Ы Х П О Ч В А Х И В П О Д ЗО ЛЕ

О Б Р А З О В А Н Н Ы Х ИЗ В О Д Н О Л Е Д Н И К О В Ы Х П Е С К О В

Институт хозяйственной геодезии,

Почвоведческая лаборатория,

RapmaBCKO^ï

П олитехники

Р е з ю м е

Вы деленны е в Систематике почв П ольш и в классе подзолоземов рж авые

почвы как тип и рж авы е подзоленны е почвы как подтип охватывают слабо

оподзоленные почвы, образованные главным образом из песков разного про

исхождения. Ц елью настоящего труда я в ля лось определение, сущ ествую т ли

по отношению к содержанию разны х форм гум усны х соединений различия

м еж ду ржавыми подзоленными почвами и подзолами.

В проф иле 1 представительным д ля подзола образованного из р ы хлого

зандрового песка анализировали формы гум усны х соединений в горизонтах

Л 0, A i A 2 , A z и

Bh, а в п р оф и ля х 2, 3, 4 и 5 представительны х для рж авы х

подзоленны х почв образованных из ры хлого зандрового песка проводили ана

ли зы форм гум усны х соединений [4] в образцах

отобранных из горизонтов

Л о , A i A 2 и

В

г

3. Существенные различия по отношению к содержанию как

общего С так и форм гум усны х соединений наблюдаются м еж ду горизонтом B h

подзола и горизонтом В т

рж авы х подзоленны х почв. В горизонте Bh содер

ж ание общего С составляет около 1,5%, а в горизонте Вг содержание этого э л е

мента колеблется в пределах 0,3-1,0%. В обоих случ а я х связанная фракция

преобладает над свободной фракцией. В горизонте Вп в сравнении с горизонтом

В г содержание свободной фракции почти два раза выше. Наблюдаются также

разницы меж ду содержанием ф ульвоки слот в свободной и связанной фракции

горизонта Вп в сравнении с горизонтом В т. В свободной фракции содержание

ф ульвок и слот первой эстракции в горизонте Bh выше, чем в горизонте В т, в

связанной ж е фракции наоборот: содержание ф ульвоки слот первой экстракции

гораздо выш е в горизонте В г, чем в горизонте B h.

Одновременно в горизонте Bh содержится по сравнению с горизонтом В т

несколько раз больш е гумин. Это свидетельствует о далеко продвинутой кон

В г — рж авый горизонт.

(9)

Content of various form s of humus compounds.,

193 денсации и стабилизации гум усны х соединений под влиянием гидроокиси ж е

леза и алюмия в горизонте В а подзола. Существенное различие м еж ду гори

зонтом Вн и горизонтами В г наблю дется такж е в соотношении H : F, составля

ющем в горизонте В h 0,64, а в горизонтах В т

0,20-0,32. Участие гуминовых ки

слот в горизонте Bh 2-3 раза выше, чем в горизонтах В т.

В общем можно констатировать, что эволюция органического вещества

в подзоле продвинута дальш е, чем в рж авы х подзоленны х почвах, что связано

с совокупностью экологических условий.

Соотношение С : N гораздо выше в горизонте B h, чем в В г, что в свою

очередь связано с высшим содержанием в этом горизонте наиболее подвиж ны х

ф ульвок и слот первой экстракции, с низким удельн ы м весом, содержащ ихся

в свободной фракции, а такж е с высшим содержанием общего С.

Р езульта ты исследований приводят к заключению, что изменения органи

ческого вещества в рж авы х подзоленны х почвах происходят иначе, чем в под

золе, что по всей вероятности связано с более сухим почвенным климатом этой

типологической единицы. М ож но ф ормулировать гипотезу, что в рж авы х по

чвах ф изическое и химическое выветривание скального ’материала превышает

биологическое выветривание.

F. K U Ź N IC K I, Р. S K Ł O D O W S K I

C O N T E N U DE D IF F É R E N T E S F O R M E S DES CO M PO SÉS H U M IQ U E S

D A N S LES SO LS OCRES PO D Z O L IQ U E S ET D A N S LE P O D Z O L,

FO RM ÉS DE S A B LE S F L U V IO G L A C IA U X

L ’Institut de Géodesie Économique

Laboratoire pédologique, de l ’Ecole Polytechnique à Varsovie

R é s u m é

Les sols ocres distingués comme un type au Système des Sols de Pologne, en

classe des sols podzolisés et des sols ocres podzoliques comme un sous-type, com

prennent des sols faiblem ent podzolisés, formés, surtout de sables de diverse genèse.

L e but de l ’ouvrage ci-dessus a été d’établir s’il y avait des différences entre les

sols ocres podzoliques et les podzols dans le contenu de différentes form es de

composés humiques. A u p ro fil 1 représentant le podzol form é de sable de sandre

on a analysé des form es de composés humiques aux horizons A 0, A 1A ll A 2 et B h,

aux profils 2, 3, 4 et 5 représentant des sols ocres podzoliques form és du sable de

sandre on a execute des analyses des form es des composés humiques [4] dans des

échantillons pris des horizons A 0, A XA 2 et B r 4. Des différences essentielles par

rapport au contenu aussi bien de C total que des form es des composés humiques

existent entre l ’horizon B h du podzol et des horizons B T des sols ocres podzoliques.

A l ’horizon B h le contenu de C total est environ 1,5%, aux horizons Br le contenu

de C total oscille entre 0,3-1,0%.

Dans les deux cas la fraction liée prévaut sur la fraction libre.

A l ’horizon Bh en comparaison avec des horiz. B r le contenu libre est presque

deux fois plus grand. I l y a des différences entre le contenu d’acides fulviques

dans la fraction lib re et liée à l ’horizon B h en comparaison avec des horizons B r.

* B r — l ’horizon ocre. Roczniki G lebozn aw cze — 13

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194 F. Kuźnicki, P. Skłodowski

Dans la fraction libre le contenu d’acides fulviques de la l ère extraction à l ’h o

rizon Bh est plus haut que celui aux horizons Br, cependant dans la fraction fix é e

il y a un phenomène contraire: des acides fulviques de la l ère extraction prévalent

considérablement aux horizons B r en comparaison avec l ’horizon

Bn-En même temps l ’horizon B h contient baucoup plus d’humines que les horizons

Br.

Cela prouve une condensation avancée et une stabilisation des composés hu

miques sous l ’influence des hydroxydes ferriques et d’aluminium à l ’horizon Bh

du podzol. C ’est la proportion H : F (qui est: à Bh — 0,64 et aux horizons B r —

0,20-0,32) qui constitue la différen ce essentielle entre l ’horizon Bh et des horizons*

Br.

En général on peut constater que l ’évolution de la substance organique du

podzol est plus avancée que celle des sols ocres podzoliques ce qui est liée avec

l ’ensemble de conditions écologiques.

La proportion C : N est beaucoup plus haute à l ’horizon B h qu’aux horizons Br

ce qui résulte à son tour d’un plus grand contenu dans cet horizon d’acides fu l

viques de la l ère extraction, plus mobiles et d ’un bas poids spécifique compris

dans la fraction libre et aussi avec un plus grand contenu de C total.

Des résultats de ces recherches on peut déduire que les changements de la

substance organique dans les sols ocres podzoliques s’accomplissent autrement que

dans le podzol ce qui se lie probablem ent avec un clim at de sol plus sec de cette

unité typologique.

On peut form uler l ’hypothèse que dans les sols ocres la décomposition physique

et chimique du m atériel rocheux surpasse nettement la décomposition biologique.

F. K U Ż N IC K I, P. S K Ł O D O W S K I

G E H A L T V E R S C H IE D E N E R H U M U S V E R B IN D U N G S F O R M E N

IN DEN A U S D EN F L U V IO G L A Z IA L S A N D E N E N T W IC K E L T E N

P O D S O L IE R T E N R O S T IG E N BÖ D EN U N D P O D S O L

Institut für Wirtschaftsgeodäsie,

Bodenkundliches Laboratorium , Technischer Hochschule in W arszawa

Z u s a m m e n f a s s u n g

Die in der System atik der Böden Polens in der Klasse von Podsolerden als

ein T yp abgesonderten rostigen Böden (Rosterden) und als ein U ntertyp abgeson

derten podsolierten rostigen Böden (Podsol-Rosterden) umfassen schwach pod-

solierte, hauptsächlich aus Sanden verschiedener H erku nft entiw ckelten Böden.

Z w eck der vorliegenden A rb e it w ar nachzuprüfen, ob hinsichtlich des Gehaltes

verschiedener Humusverbindungsformen irgendw elche D ifferen zen zwischen p od

solierten rostigen Böden und Podsols bestehen.

Im P ro fil 1, von welchem ein aus dem losen Sandersand entwicketes Podsol

vertreten war, wurden die Humusverbindungsform en in den Horizonten A 0, A

i

A 2,

A 2 und B h, in den P ro file n 2, 3, 4 und 5 degagen, vertrebar fü r die aus losem

Sandersand entwickelten podsolierten rostigen Böden, wurden die Hum usverbin

dungsformen in den aus den Horizonten A 0, A i A z und Br entnommenen Proben [4],

a n a lysiert5.

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Content of various form s of humus compounds... ₁₉₅

S ignifikante D ifferen zen in Bezug auf den Gehalt der sowohl Gesamtkohle

als auch der Hum usverbindungsform en treten zwischen dem B^-Horizont des P od -

sols und dem B r-H orizont von podsolierten rostigen Böden auf. Im B^-Horizont

beträgt der G esam t-C-G ehalt ca 1,5%, im Br-H orizont dagegen schwankt dieser G e

halt innerhalb 0,3-1,0%. In beiden Fällen überw iegt die verbundene Fraktion die

freie Fraktion. Im Bn-Horizont ist der Gehalt der freien Fraktion fast doppelt

hoher im V ergleich m it dem Br-Horizont.

Est bestehen auch D ifferen zen zwischen dem G ehalt an Fulvosäuren in der

freien und verbundenen Fraktion im B h-H orizont im Vergleich m it dem B r-H ori

zont. In der freien Fraktion übersteigt der Gehalt von Fulvosäuren der I. Extraktion

im Bh-Horizont diesen im Br-Horizont, während in der verbundenen Fraktion um

gekehrt, und zw ar: der Gehalt von Fulvosäuren der I. Extraktion im B r-H orizont

im V ergleich m it dem Bh-Horizont wesentlich höher ist.

G leichzeitig sind im B h-H orizont wesentlich höhere M engen von Huminen im

Vergleich im dem B r-H orizont enthalten. Dies zeugt über eine w e it fortgeschrittene

Kondensation und Stabilisierung der Humusverbindungen unter dem Einfluss der

Eisenhydroxyde und Alum inium im B^-Horizont des Podsols. Eine signifikante

D ifferen z zwischen dem Bh- und Br-H orizont tritt auch im H : F -V erhältnis auf,

das im B^-H orizont 0,64 und im Br-H orizont 0,20-0,32 beträgt. Der A n te il der

Huminsäuren im B^-H orizont ist 2-3 m al höher als im Br-Horizont.

Im allgem einen kann man feststellen, dass die Evolution des organischen

Stoffes im Podsol m ehr fortgeschritten als in den podsolierten rostigen Böden ist,

was m it der Gänze von ökologischen Bedingungen im Zusammenhang steht.

Das С : N -V erhältnis ist wesentlich höher im B^-Horizont im Vergleich m it

dem B r-Horizont, was m it höherem Gehalt der beweglichsten Fulvosäuren

der

I. Extraktion m it niedrigem spezifischen G ew icht in der freien Fraktion w ie auch

m it höherem G esam t-C-G ehalt verbunden ist.

Die Untersuchungsergebnisse wiesen darauf, dass die Verwandlungen des o r

ganischen Stoffes in podsolierten rostigen Böden im V ergleich m it dem Podsol

anders verlaufen, was wahrscheinlich m it dem trockeneren Bodenklim a dieser

typologischen Einheit verbunden ist. Man kann die Hypothese stellen, dass in den

rostigen Böden die physikalischen und chemischen V erw itteru n g des Felsm aterials

die biologische V erw itteru n g deutlich übersteigt.

F. K U Ż N IC K I, P. S K Ł O D O W S K I