K. K O N E C K A -B E T L E Y
D IS T R IB U T IO N A N D T R A N S F O R M A T IO N S O F O R G A N IC M A T T E R IN F O SSILE SO ILS A M O N G LO ESSES
Institute of Soil Science and A gricu ltu ral Chemistry, A gricu ltu ral U niversity of W arsaw
One of the criteria of isolation of fossile soils among loess sediments are mineral horizons w ith accumulated organic matter. They distinguish themselves morphologically as grey or dank-grey and sometimes «browned layers, often of a considerable thickness. However, their thickness and total content of organic carbon proves neither their organic matter trans formation, nor its genesis and age.
To determine the changes and distribution of organic matter age in fossile soils of different age developed from loess, the fractioned analysis of organic matter was carried out b y the method of D u c h a u f o u r and J a c q u i n [1]. According to this method light (free) and heavy (bounded) fractions of organic matter w ere isolated. In particular fractions (light 'and heavy) fulvic and humic acids w ere isolated, at determination of carbon content in them. In the residue after light fraction isolation, the content of carbon (so-called residuum) as w ell as carbon in unsoluble part of heavy fraction in so-called humines were determined.
For the investigation o f organic compounds 3 profiles of polygenetic fossile soils from the Sandomierz Upland [5, 9]— Złota, Żurawica and Chobrzany, defined by many authors as soil complexes (2, 3, 4) have been chosen.
Genetic horizons characteristic for contemporary soils can be isolated morphologically in these soils, but they w ere formed in various periods of warm er interstadials and interglacials under different plant commun ities, separated from one another with cold phase— the period of a new loess blowing up.
A t Żurawica and Chobrzany, beside soil complexes, there occurs younger soil from the Stillfried I (Pandof) interstadial w eakly formed, with very low organic matter content (Tables 1, 2, 3) developed from
Carbon content in different fractions of organic matter of soil
T a b l e 1
Locality Horizon Depth cm Weight percent in relation to total Total С %
For cent of carbon in relation to soil In per cent of total С Age light frac tion heavy frac tion light frac tion heavy frac tion light frac tion heavy frac tion
Złota A1 150-160 0,65 99.35 0.705 0.195 O.51O 27.65 72.35 Stillfried A
175-185 0.62 99.38 ( 0:588 0.16? 0.421 28.40 71.60 PK II and III
A3B 200-210 0.39 99.61 0o284 O.O5O О.234 17.67 82.33
st 235-245 0.24 99.76 0.150 0.002 0.148 1.33 98.67
Żurawica / V 295-300 0.28 99.72 0.196 0.0C5 0.191 2.55 97.45 Stillfried В FK I 361-371 0.38 99.62 0.456 0.099 0.357 2 1 .7 1 78.29 Stillfried A 371-400 0.55 99*45' 0.392 0.114 0.278 29.IO 70,90 PK II and III
A5 400-415 0.40 99.60 0.263 O.O9O 0.173 34.23 65.74
Bt 437-448 0.02 99.98 0.133 0.002 O.I3I 1.50 98.50
Chobrzany /Ад/ 220-230 0.20 99.80 0.222 0.004 0.218 1.20 98.20 Stillfried В PK I A1 360-386 0.57 99.43 О.394 0.163 O.23I 41.40 58. GO Stillfried A a1a5 386-400 0.33 99.67 0,231 0.093 О.13З 40.25 59.75 PK II and III
400-413 0.17 99.83 0.118 O.OO5 0.115 4,24 95.76
The analyses were carried out by Dr. P.Skłodowski, for which the author expres.oes him her gratitude
20 8 K o n e c k a -B e tl e y
ik i G le b o z n a w c z e
Content of different forms of organic compounds determined by the method of Ph. Duchaufour and F. Jacquin
T a b l e 2 Locality Depth cm Total С %
Carbon distribution in % of total carbon
light fraction heavy fraction
1 st extraction U n d extraction
■0 1 st extraction U n d extraction Ilird extraction humines
H F1 % F2 i:2 F3 H3 F4 H4 F5 H5 Złota 150-160 175-185 200-210 255-245 0.705 0.588 0.284 0.150 1.42 I.70 1.76 1.28 1.36 1.76 0.23 0.68 1.06 7.37 8.67 9.22 17.30 15.99 3.87 1.33 19.72 23.61 31.69 33.53 6.24 5 .9I 2.75 8.00 8.65 6.97 8.10 6.67 8.51 12.41 8.10 4.00 13.52 11.22 14.79 20.67 6.81 9.88 12.68 16.00 8.80 5.40 4.24 10.00 Żurawica 295-300 361-371 371-400 400-415 437-448 0.196 0.456 0.392 0.263 0.133 0.44 1.02 I.52 0.66 I.27 1.19 0.88 0.28 I.52 4.60 9.69 11.40 2.55 15.13 16.84 18.63 1.50 32.14 20.83 23.72 26.60 39.10 9.69 7.67 2.04 5.04 9.77 11.73 9.З7 11.73 10.64 15.80 5.10 4.58 9.18 9.12 8.27 16.84 10.96 10.97 8.36 7.52 16.55 9.87 8.16 4.18 9.02 5.62 14.71 5.10 5.80 0.02 Chobrzany 220-230 360-385 386-4-00 400-413 0.222 0.394 0.231 0.118 I.27 0.86 1.01 0.87 О.29 О.43 11.67 8.22 1.80 27.16 29. S 7 4.24 40.99 25.63 23.14 45.22 9.01 5.84 4.30 9.З2 15.76 6.85 7.79 14.41 4.95 5.5З 6.49 7.63 15 .5 1 4.51 3.97 5.03 9.90 4.04 4.50 8.47 4.08 6.55 4.76 7.65
Fx - fulvic acids in the light fraction Ist ortracti0 - humic acids in the light fraction HagSO^ , pH 7 F2 - fulvic acids in the light fraction U n d oxtracti Hg - humic acids in the light fraction pH 9.8 F^ - fulvic acids in the heavy fraction 1st ©xtractio H^ - humic acids in the heavy fraction Na^SO^ , pH 7 H - humines, unsoluble part of the heavy fraction of orga
remained after three consecutive extractions
n NaJP?07+ F4 - fulvic a H^ - humic ac on Na^P20? , *5 - fulvic a - humic ac n Na4?2°7+ R - residuum, matter nie matter cids in tł ids in the .cids in tl ids in the non-extre le heavy fraction > heavy fraction ю heavy fraction 1 heavy fraction icted part of the li
U n d ез pH 9. Ilird € 0.1 N 1 ght fractJ ctraction ] ,8 ixtraction laOH LOn of org ^a4F2°7 * anic Distr ib uti on an d tr an s fo rm a tio n of o rg an ic m a tte r 2 0 9
Total content of different forms of organic compounde in particular fractions and the values characterizing humification
T a b l e J Locality Sampling depth cm Total С %
С of ful vie and humic acids and humines in % of total С 1 H+F ratio Humifi cation degree «
С percentage in particular fractions in relation to С in soil
light
fraction heavy fraction light fraction 1 heavy fraction V ?2 Hl +H2 W y5 H3+H4+H5 humines . H R Fl +F2 Hl +H2 V V 5 huminesH Złota 150-160 175-185 200-210 235-245 0.705 0.588 0.284 0.150 I.70 2.38 2.82 8.65 10.03 10.96 41.99 42.00 54.58 60.67 21.56 26.20 23.5I 28.00 8.80 3.40 4.24 10.00 0.69 0.82 0.60 0.46 82.70 84.01 96.13 98.67 0.122 0.094 0.011 0.002 0.012 0.014 0.008 0.061 -0.059 0.031 0.296 0.247 0.155 O.O9I 0.152 0.154 0.067 0.042 0.062 0.020 0.012 0.015 Żurawica 295-300 361-371 371-400 400-415 437—448 0.196 0.456 0.392 0.263 0.133 1.32 I.30 3.04 5.22 10.96 12.59 60.71 41.66 46.42 39.60 62.32 31.12 21.92 19.38 16.34 27.06 5.62 14.71 5.10 3.80 9.02 0.51 0.63 0.64 0.59 О.43 97.45 84.87 83.16 81.37 98.50 O.OO5 0.069 0.066 0.049 0.002 0.006 0.005 0.008 0.024 0.043 0.033 O.II9 O.I9O , 0.182 0.120 0.083 0.061 0.100 0.076 0.043 0.036 0.011 0.067 0.020 0.010 0.012 Chobrzany i 22О-23О 36О-З86 386-400 400-413 0.222 0.394 0.231 0.118 1.56 I.29 12.68 9.09 70.26 36.79 39.90 62.71 23.86 15.46 15.09 25.42 4.08 6.35 4.76 7.63 0.34 0.73 0.59 0.40 98.20 72.84 65.80 95.76 0.004 0.107 0.069 0.005 0.006 0.003 O.O5O 0.021 0.156 0.145 О.О92 О.О74 0.053 0.061 0.035 О.ОЗО 0.009 О.О25 0.011 O.OO9 21 0 K * K o n e c k a -B e tl e y
younger carbonated loess. Loess of the polygenetic soils w here upper part corresponds with the Stillfried II and III (Am ersfort and Brörup) inter stadial and lower part— with the Eems interglacial, is decalcified.
D IS C U S S IO N OF R E S U LT S
On the whole, it can be stated that in all the horizons of fossile soils the heavy fraction of organic matter (Table 1), bounded with mineral particles, plays more important role as compared with light, so-called free fraction. The light fraction content is higher in horizons with higher organic carbon content. Light fraction of organic matter in total C% in the A t horizon of the Chobrzany profile constitutes about 40% of total C, what can prove a shorter period of the A 1 horizon formation, perhaps in the Ems interglacial + Am ersfort interstadial or in the Amersfort interstadial only.
The content of the light and heavy fraction and of the so-called residuum are correlated with humification degree (Table 3) of organic matter.
In the fossile soil horizons with higher organic matter content its transformation is not so far advanced as in the contemporary soils occur ring on the areas built of loess [7, 8], where the heavy (bounded) fraction content, expressed in total C%, can reach up to 90%.
A considerable organic carbon content in A 1 horizons of polygenetic soils, in the so-called residuum, i.e. non-extracted part of light fraction of organic matter proves either specific climatic conditions, less favour able for the humification process or shorter period of the occuring changes in organic matter of this genetic horizon.
Perhaps a part of free, non-humified organic matter underwent a certain diagenesis in this horizon and was consequently conserved.
A ll fossile soils characterize themselves «with a relatively low carbon content in humines, constituting an unsoluble part of the heavy fraction ('bounded with mineral part of soil), particularly the soil horizons (A j) of soil from the Stillfried I (Pandorf) interstadial. The highest content of humines is in the B t horizons of soils from the Eems interglacial, what proves the occurrence of higher quantities of difficultly soluble complex humus— clay compounds.
The occurrence of higher colloidal clay content in the B t horizons was confirmed by the determination of granulometric composition as w ell as b y the micro-morphologic investigations [5].
It is to stress that in the contemporary chernozem and brown soils there occurs 3-4 fold higher content of humines than in the investigated fossile soils [6, 7, 8].
212 K. K onecka-B etley
The humification degree is closely correlated with the organic matter content and ewolution: the most strongly humified organic matter occurs in the B t horizons (the oldest horizon of polygenetie soil) and in the (A j) horizons from the Pandorf interstadial (the lowest content of accumulated organic residues). Low humification degree, below 80, occurs in hums horizons of soils originating probably from two interstadials, i.e., poly- genetic soils at Złota and Żurawica. A t Chobrzany it is still less, amount ing even to 65, what proves specific conditions of this soil formation under influence or forest-interglacial vegetation and to much less extent under influence or without any influence of interstadial vegetation with a considerable percentage of herbaceous plants.
A particular attention deserves the ratio between humic and fulvic acids, maintaining in all the soils investigated within the limits of 0.34-0.82 (Table 3). It proves that in fossile soils, even chernozems the content of fulvic acids prevails over that of humic acids. The former predominate in the heavy fraction and are extracted mainly in the first extraction.
A ll the results obtained prove that the organic matter transformations in fossile soils, despite its fixing in the B t horizons with mineral particles, advanced not particularly for (predominance of fulvic over humic acids as the compounds with more complicated structure) and underwent some checking.
The organic matter transformations in the fossile soil profiles investi gated throw also the light upon the totality of eeologic conditions of the formation of these soils. On the whole it can be stated basing on the fractioned humus in the soils in question, principally in the soil com plexes, that their formation conditions were not favourable for forming typical chernozems of the steppe zone; on the other hand, they are more approximated to the conditions of development of not fully formed cher nozems or forest grey soils. Of it the predominance of fulvic acids in the heavy fraction, a considerable residuum content and a low H :F ratio (Złota, Żurawica) can bear the evidence. Low er humification degree of the interstadial A 1 horizons in the profile at Chobrzany (the depth of 360-400 cm) as well as higher residuum content as compared with humus horizons of the remaining profiles proves on the one hand somewhat lower decomposition degree of resh organic matter and a different plant community, probably of the forest vegetation, on the other. In particular horizons of the profile the total content of carbon is lower than in the remaining ones and the organic matter transformations are less distinctly marked, w hat is conformed by lower percentage of humic acids of the Illrd extraction in the heavy fraction (Table 3). From the typologie view point the properties of this soil are approximated to those distinguished
on the area of soils lessives, without any secondary overlapping the upper horizons of the later chernozem process.
The problem of typology of these soils seems to be still open one, as in every case they can represent different development stages, depending on duration of soil-forming process under different plant communities.
REFERENCES
[1] 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 Su périeure Agronom ique de N an cy” 8, 1966, 1.
[2] J e r s a k J.: L a stratigraphie des loess en Pologne concernant plus particu lièrem ent le dernier étage froid. Biul. peryglac. 20, 1969, P W N , 99-132.
[3] M a r u s z c z a k H.: Zagadnienie k lasyfikacji lessów w Polsce. Przew odn ik sympozjum krajow ego: L itologia i stratygrafia lessów w Polsce. W ydawn. geolog. 1972, 17-29.
[4] K o n e c k a - B e t l e y K.: Poziom y diagnostyczne śródlessowych gleb kopal nych Polski południowo-wschodniej. Przew odn ik sympozjum krajow ego: L ito logia i stratygrafia lessów w Polsce. W arszawa, W ydawn. geolog., 1972, 30-36. [5] K o n e c k a - B e t l e y K., S t r a s z e w s k a K.: Charakterystyka gleb kop al
nych W yżyn y Sandomierskiej (poziom y diagnostyczne). Typescript, 1972. [6] 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, 32-25.
[7] K u ź n i c k i F., K o n e c k a - B e t l e y K., K o w a l k o w s k i A., B i a ł o u s z St.: Geneza i typologia gleb Polski Środkowej. P rzew od n ik konferencji te re nowej zjazdu naukowego, 1970, s. 40 (Typescript).
[8] K u ź n i c k i F., S k ł o d o w s k i P.: Zawartość różnych form zw iązków próch nicznych w rędzinach w porównaniu z innym i typam i gleb. Rocz. glebozn. (in print).
[9] International Association on Quarternary Research, V lth Congress (IN G U A ) From the Baltic to the Tatras. P W N , Łódź 1961, s. 104.
К. К О Н ЕЦ К А-Б ЕТЛ Е Й Р А З М Е Щ Е Н И Е И П Р Е О Б Р А З О В А Н И Е О Р Г А Н И Ч Е С К О Г О В Е Щ Е С Т В А С Р Е Д И Л Е С С О В Ы Х Ф О С С И Л Ь Н Ы Х П О Ч В Институт почвоведения и агрохимии Варшавксой сельскохозяйственной академии Р е з ю м е В настоящем труде исследовано размещение и преобразования органичес кого вещества средилёссовых ф оссильн ы х почв Сандомерской возвышенности с целью определения одного из критериев типологии этих почв и совокуп ности экологических условий их образования. П олучен ны е результаты свидетельствуют о том, что преобразования орга нического вещества (определенного по методу Дюш офура и Ж акэна) в ком плексах ф оссильн ы х почв, несмотря на его связь в горизонтах Bt с м инераль
214 K. K onecka-B etley ными частицами, не продвинулись особенно далеко (преобладание ф ульвоки слот над гуминовыми кислотами как более слож ны м и соединениями) и бы ли задер ж аны в известны х пределах. О продвижении эволюции этих почв может свидетельствовать высшая и ли низшая степень гумификации органического вещества связанного с расти тельны м и соообществами в отдельны х интерстадиалах и в интерглациале. В общем можно заклю чать, что условия образования почв, в первую очередь почвенны х комплексов (Ш тильф рид А. — P K I I и I I I ) не благоприятствовали образованию типичных черноземов степной зоны ; они более приближ ались к условиям образования неполны х черноземов или лесны х сероземов. K. K O N E C K A -B E TLEY L A D IS L O C A T IO N E T LE S T R A N S F O R M A T IO N S DE L A S U B S T A N C E O R G A N IQ U E DES SO LS F O S S IL E S E N T R E LE S LO ESS Institut de Pedologie et Chim ie Agricole,
U niversité Agronom ique de Varsovie R é s u m é
Dans l ’ouvrage présent on a étudié la dislocation et les transformations de la substance ogranique des sols fossiles entre les loess du plateau de Sandomierz, dans le but d’établir un des critères de la typologie de ces sols et l ’ensemble des conditions écologiques de leur origine (pédogenese).
Les résultats obtenus (on appliquait la méthode de Duchaufour et de Jaquin) prouvent que les transformations de la substance organique dans les ensembles de sols fossiles-bien qu elle soit liée dans des n iveau x B t avec les parties m i nérales — ne sont pas trop avancées (supériorité des acides fulviques sur des acides humiques — composés plus compliqués) et elles ont subi un certain en rayage.
Un (plus grand ou plus petit) degré d’hum ification de la substance organique, se reliant avec les ensembles des plantes dans les interstades ou un interglacial, marque un degré d’évolution de ces sols.
En général, on peut constater que les conditions de la genèse des sols et surtout des complexes de sols n’étaient favorables pour la form ation des chernozems ty piques dans la zone de steppe, mais par contre, ailes s’approchent des conditions de form ation des chernozems peu évolués (peu profonds) ou des sols gris forestiers.
K. K O N E C K A -B E TLEY
V E R T E IL U N G U N D V E R W A N D L U N G E N DES O R G A N IS C H E N STO FFES DER F O S S IL E N LÖ SSB O D E N
Institut fü r Bodenkunde und Agrikulturchem ie, Landw irtschaftliche U n iversität zu W arszawa
Z u s a m m e n f a s s u n g
In der vorliegenden A rb eit waren die Verteilung und Verwandlungen des organischen Stoffes in den fossilen Lössböden des Sandom ierz Hügellandes unter sucht, um ein der T yp ologiek riterien dieser Böden zu finden und die Gänze von ökologischen Bedingungen der Entwicklung derselben zu ermitteln.
D ie erhaltenen Ergebnisse wiesen daraufhin, dass die Verw andlung des o r ganischen Stoffes (bestim m t nach der M ethode von Duchaufour und Jacquin) in den K om plexen von fossilen Böden, trotz der Verbindung derselben in den B t-H o rizonten m it mineralischen Teilchen, nicht besonders w e it fortgeschritten seien (ein Ü bergew icht der Fulvosäuren über Huminsäuren als mehr kom plizierten V er bindungen) sowie einer gewissen Hemmung unterliegen.
Ü ber den Evolutionsfortschriftt dieser Böden kann höherer oder kleinerer H um ifizierungsgrad des m it den Pflanzengesellschaften in einzelnen Interstadialen und in dem In terglazial verbundenen organischen Stoffes zeugen.
Im allgem einen kann man feststellen, dass die vorhandenen Bildungsbeding ungen der Böden, und in erster L in ie der Bodenkom plexe (S tillfried A. — P K I I und I I I ) die Bildung von typischen Tschernosemen der Steppenzone nicht b e günstigen, dagegen sie sich m ehr den Bildungsbedingungen der unentwickelten Tschernoseme oder grauer W aldböden nähern.
K. KO NE CK A -B E TLEY
R O Z M IE S Z C Z E N IE I P R Z E M IA N Y S U B S T A N C J I O R G A N IC Z N E J W S R O D LE S S O W Y C H G L E B A C H K O P A L N Y C H
Instytut G leboznawstwa i Chem ii Rolnej A kadem ii Rolniczej w W arszaw ie
S t r e s z c z e n i e
W niniejszej pracy badano rozm ieszczenie i przem iany substancji organicznej śródlessowych gleb kopalnych W yżyn y Sandom ierskiej, w celu ustalenia jednego z k ryteriów typologii tych gleb i całokształtu w arunków ekologicznych ich p o wstawania.
Otrzym ane w yn ik i świadczą, że przem iany substancji organicznej (wykonane metodą Duchaufoura i Jacquin) w kompleksach gleb kopalnych, mim o powiązania ich w poziomach B t z częściami m ineralnym i, nie poszły zbyt daleko (przew aga kwasów fu lw ow ych nad kwasam i hum inowym i — zw iązkam i bardziej złożonym i) i uległy zahamowaniu.
O stopniu ew olu cji tych gleb świadczy w iększy lub m niejszy stopień hum ifikacji substancji organicznej, w iążący się z zespołami roślinnym i w poszczególnych in ter- stadiałach oraz w interglacjale.
O gólnie można stwierdzić, że warunki powstawania gleb, głów nie kom pleksów glebow ych (S tillfried A. — P K I I i I I I ) nie sprzyjały powstawaniu typowych czar- noziem ów strefy stepowej, natomiast nawiązują bardziej do warunków powstawania czarnoziem ów niedokształconych lub szarych gleb leśnych.
D o c . d r hab. K r y s t y n a K o n e c k a -B e t le y In s ty t u t G le b o z n a w s t w a i C h e m ii R o ln e j A R W a rsz a w a , ul. R a k o w ie c k a 26
