K R Y ST Y N A KONECKA-BETLEY
FO SSIL SOILS OF LATE PLEISTO C EN E
D EV ELO PED FROM LOESSES
Departm ent o f So il S cien ce , W arsaw Agricultural U n iversity
INTRODUCTION
Fossil soils in quaternary and older formations are of basic stratigraphie importance. They determine breaks in the sedimentation of loesses. Climate and vegetation changes are documented and transformation of ecosystems of these time periods are also characterized by those soils.
The basis for distinguishing paleopedons is characterized by some definite pedogenic traits in aeolian and other sediments, which should be traced spatially in the landscape. Variability of these traits under different environ mental conditions becomes a basis for distinguishing several soil types within one catena. The latter can be put in order spatially in the so-called soil mosaics.
The course of soil-forming processes should be documented by the results of biophysico-chemical and micromorphological studies performed by the methods applied at present in soil science, including methods determining the age of the mineral substrate or organic matter. For comparative purposes with present soils and spatial correlation determination, fossil soils should be (according to recommendations of the Commission for Paleopedology IN- QUA) assigned to taxonomic units in accordance with a national or internatio nal classification system while applying the valid horizon designations.
BASIC LOESS PROFILES
Diagnostic types and horizons of fossil paleopedons of the Late Pleistocene were recognized and distinguished on the basis of investigation results of the
following outcrops: Sandomierz-Chobrzany environs, Złota and Żurawica [Konecka-Betley 1974; Konecka-Betley, Straszewska 1977]; environs of Ka zimierz Dolny on Vistula-Kwaskowa Góra, Góra Trzykrzyska [Konecka-Bet
ley, Maruszczak 1976]; Kraków-Zwierzyniec I [Chmielewski, Ko
necka-Betley, Madeyska 1977]; Kraków-Spadzista II [Konecka-Betley 1987a]; Sandomierz [Konecka-Betley, Czępińska-Kamińska, Zagórski 1986], Łopatki [Konecka-Betley 1991] and Polanów Samborzecki and other outcrops - unpublished materials. The pedostratigraphy of the above outcrops, based on the results of chemical and micromorphologic investigation, has allowed for the presentation of a synthetic loess profile in this work (Fig.l).
COM PLEX OF SOILS
OF TH E EEMIAN AND LATE VISTULIAN INTERG LA CIAL Several series of loesses can be found throughout Poland [Maruszczak 1986; Harasimiuk, Maruszczak, Wojtanowicz 1988; Jersak 1988], viz.: older loesses belonging to the previous cool stage and younger loesses lain in the last cool Vistulia n. Among these forms, the occurrence of fossil soil of differentage rank were found. At the bottom of the Vistulian series of loesses, fossil forest eemian soils developed from older loess. It is covered [Konecka-Betley 1987b] with a soil complex with younger fossil soils of Late Vistulian [Konecka-Betley, Maruszczak 1976; Konecka-Betley, Straszewska 1977; Konecka-Betley etal. 1986]. On glacial areas, such a soil is developing, first of all, from organic formation, most often from gytia, peats and organic silts.
Interglacial fossil forest soil is characterized by a well-formed Eet-luvic lessivage horizon and the lack A horizon, poor in free iron and small colloidal fraction as well as by a well-developed and thicker diagnostic argillic-Bt horizon, often with superficial gleization symptoms. This horizon has an enriched colloidal fraction and substantial free iron. In the Eet, Bt and С horizons of this soil, minerals of the smectite group prevail, at a smaller content of il lite. The diagnostic Bt horizon developed as a consequence of lessivage is documented by a well-formed fluvial plasma of the vosepic type filling the soil pores partially or fully. Also plasma destruction, outwash of pores, and displa cement of colloidal clay to secondary deposition occurred. Plasma destruction should be connected with frost phenomena occurring in the destruction of soil lessivé or in a later period when epigenetic periglacial structures were “rooted" in middle younger loess. Plasma transforms in some outcrops in a non trans parent plasma of the isotonic type as a consequence ot later displacement of iron and manganese at the interglacial end. Also, much younger plasma of the cristic type formed as a consequence of the displacement of secondary carbo nates from overlying loesses can be found at times. In the С horizon, loess remains almost unchanged by the soil-forming processes.
In some outcrops, the organic matter horizon of interglacial soil lessivé can be expected in the lowest part of humus horizons younger soil (Fig.l). This part
Fig. 1. Schem atic loess section:
I - Iithostratigraphy - letters sym bols: LM - younger loesses; n - lowest; d - lower; s - middle; g - upper; GJ - interglacial soil; Gi - interstadial soil; GH - holocene soil;
II - pedostratigraphy - 1 - humus horizon; 2 - leaching horizon; 3 - illuvial horizon; 4 - parent material loess; 5 - gley horizon; 6 - vistulian deposits; 7 - eemian deposits
of the horizon contains 0.44% of organic carbon. The Ch:Cf ratio here remains below I, while the content of humic carbon is low, amounting to only 8%, which indicates a low value in the colloidal fraction. Low ratio of humic to fulvic acids in this horizon is related to the Eet and Bt horizons and not to overlying younger chernozems. Micromorphology proves that organic matter usually occurs in the form of weakly developed mullicol. Also, small ferrugi nous concretions of spherical shape can be found.
The interglacial eemian soil was developed under forest vegetation [Menke 1982; Maruszczak 1986]. The pollen diagrams for the Eemian Interglacial [Jastrzębska-Mamelka 1985; Mamakowa 1986; Tobolski 1986], allow the tracing of the plant succession changes in the course of the whole interglacial, by which typological transformations of the soils are documented. The deve lopmental cycle of interglacial soils on loesses is as follows: initially, weakly formed brown soils, leached brown soils and typical grey-brown soils (lessivés), gleyed and superficially gleyed soils. From the ecological viewpoint the primary coniferous forest sites transformed in climatic optimum of the interglacial into multi-species deciduous forests, then in the younger part of the interglacial, into spruce-fir-pine forests and finally, into pine forests with an increasing share of herbaceous vegetation.
SOILS DEVELOPED FROM THE YOUNGER (LOWEST) LOESS The cooling of the climate and a rapid development of the grassy-herbaceous vegetation defines the limits between older and younger Vistulian loesses. The first cooling of Vistulian is characterized by the recession of woody plants and by a distinct increase in the share of herbaceous vegetation, particularly of grasses and sedges. In central Poland the shrubby tundra predominates [Ja- strzębska-Mamełka 1985], while on loess areas, in southern Poland cool steppe prevails with distinct continental climate symptoms. At that time, the accumu lation of organic matter began. Upon warming up in the Amersfoort (or jointly Amersfoort and Brörup), it transformed in consequence of pedological proces ses into rather thick, sometimes bipartite chernozem or into a charnozem which is not fully developed, and not connected genetically with Eemian soil. Con trary to the horizon A of interglacial soil lessivés, the horizons A of Vistulian chernozem (Fig. 1 ) developed directly above the Eemian soil surface, - called Avl and Av2-ones, contain 0.60-0.55% organic carbon. In the Avl horizon, humic acids predominate, the Ch:Cf ratio lying above 1 and even reaching 2 [Konecka-Betley et al. 1986]. In the Av2 horizon, a slight predominance of tulvic acids occurs, the Ch:Cf ratio decreasing to below 1. The above pedolo gical data confirm the bipartite of chernozems and are connected with repeated rapid encroachment in the climatic optimum of interstadial of woody vegeta tion.
Organic matter in chernozem Avl and Av2 horizons occurs in the form of well-humified mullicol with a small amount of silasepic plasma, mainly in the Av2 horizon. Also, large calcite crystals are to be found in some pores, while among clayey minerals, illite predominates. The diagnostic horizon for cher nozem soils that developed from younger lowest Vistulian loess is the A mollic humus accumulation horizon. It is proposed for the above two soils: Eemian and Late-Vistulian chernozems, called up to now "soil complex”, to assume the name of soil association as a superior pedostratigraphic unit [Konecka-Bet ley 1987b].
SOILS DEVELOPED FROM LOWER YOUNGER LOESS The second post-Eemian stadial is characterized by cool and moist climate with the vegetation in the first phase of park tundra and in the second phase of woodless tundra, simultaneously with blowing of the younger lower loess. The vegetation is not particularly rich. Soil developed from this loess contains 0.22% of organic carbon and is distinctly rich in fluvial acids, the Ch:Cf ratio being below 1. Under a weakly developed A horizon, grey-bluish gleying is found and a shallowly decarbonated horizon as well wich confirms weakly marked pedogenesis. This horizon is not colloidally enriched, nor is there enrichment in free iron. A weakly developed silasepic plasma, sometimes calcite plasma and big manganese-ferruginous concretions (typical for super ficial gleization) occur in these profiles. Soil is cut by ice wedges reaching the Bt horizon in the Eemiàn soils. It is a rather weakly-developed, superficially gleyed soil. The second warming after the Eemian interglacial, being cooler and of higher moisture content than the first one, in which the above soil was finally formed, am be correlated with the Odderade interstadial [Tobolski
1986].
SOILS DEVELOPED FROM M IDDLE YOUNGER LOESS Middle younger loess began to accumulate under cool and rather moist continental climate conditions. This loess contains more calcium carbonate. In its upper section, soi 1 with a more advanced degree of development was formed most probably under tundra vegetation with groups of trees. In connection with the occurrence of permafrost in the substrate and with solifluction, no thicker A horizon was found in situ. Nevertheless, an intensive weathering documented by décalcification, mobilization, and some accumulation of iron in the forming Bbr cambic horizon took place. Micromorphology indicates the displacement of the mineral material from the A horizon to the secondary deposit. Plasma of the cristic type and large calcite crystals as well as small ferruginous-man- ganese concretions with embedded quartz grains can by encountered in it. Plasma of the silasepic type and sometimes weakly formed lattisepic and skelsepic plasma occurs in the Bbr horizon which formed in situ, although this horizon was cut with ice wedges. This is an initial phase of soil plasma separation, but without displacement.
Carbon in this horizon in the Spadzista Krakow outcrop [Konecka-Betley 1987a] dated by 14C were found to be 32000±2000 Y.B.P. Organic matter in this soil is characterized by the prevalence of fulvic acids, a Ch:Cf ratio lying below 1, and the carbon content amounting to 0.20-0.36%. This is a perigla- cially transformed brown soil, most probably an arctic one, which can be on the basis of dating connected with the Denakamp interstadial. The same outcrop revealed a l4C date of 42100± 14000 (Gr. N-7135) Y.B.P., which, although the soil was not investigated, can correlate possible with the Hengelo or
Moer-shoofd interstadial Konin-Maliniec I. [Kozarski 1981]. Results of thermolu- minescentie datings (TL) of the same soil carried out by Prószyńska-Bordas, Prószyński and Stańska-Prószyńska [1989] at Polanów Samborzecki are simi lar, namely 30±5 and 40.5±4 ka P.B. (the latter date unpublished).
SOILS DEVELOPED FROM UPPER YOUNGER LOESS Worsening climatic conditions were responsible for the repeated blowing of upper younger loess. This is typical loessial deposit of considerable thick ness, strongly carbonatic, the top of which lies at present on the surface. Within this loess, the occurrence of a weakly marked fossil soil, strongly transformed periglacially has been documented. Organic matter from this horizon was dated by 4C [Konecka-Betley 1987a], among other things, for 21000±90 (Ly- 2542)Y.B.P. This proves a slight warming trend in the period of the youngest loess sedimentation, probably of the phase rank. In the stratigraphie scheme presented by Buraczyński etal. [1984], the bipartite of the upper younger loess is marked as well. However, the stratigraphie position of this initial soil has still not been established. It is perhaps connected with Konin-Maliniec II horizons from the Wielkopolska plain [Kozarski 1981], after which the widest spreading of continental glaciation ensued.
From the upper younger loess, the sedimentation of which was most probably completed around 13500 Y.B.P., on the loess areas soils of the chernozem and brown-earth type were formed under vegetation of natural ecosystems. These soils occur at present on the surface, still they have a late Pleistocene base.They are relict soils transformed, in many cases, periglacially and anthropogenically, and are not modern Holocene soils. As early as the late Pleistocene, weathering, brown soils lessivés, or superficially gleyed soils, depend ing on relief and décalcification of area, began to develop. Certain areas, mainly on plateaus, transformed into chernozems, in which organic matter developed finally in Preboreal and Boreal periods [Jersak 1988]. A prevalence of humic acids over fulvic acids, the Ch:Cf ratio of over 1 and sometimes even over 3, were found in these soils. The humification degree, however, is somewhat lower in these soils as compared to early-Vistulian chernozems, as a relict chernozems lie steadily under the given vegetation.
In soils lessivés or superficially gleyed soil lessivés of the late-Pleistocene bases, the character of organic matter and the micromorphologic properties are similar to older interglacial soils, though weaker marked sometimes. In the Neoholocene, these soils were transformed, mainly under the effect of human activity, which manifest, among other things, through organic carbon loesses increases in phosphorus content.
Spatial variability of the soil cover among loess formations, both relict and fossil ones, has been found. In such eases, soil complexes called “catenas” are encountered, most often among various soil groupings. Distinguishing catenas is based upon the recognition of particular pedons forming rows in
pedomor-phologic profiles. The occurrence of many soil types in one catena depends, first of all, on the area relief, water conditions, cryogenic phenomena, and quantitative-qualitative geochemical differentiation of the initial material. The site elements mentioned are overlapped with the action of vegetation.
CONCLUSIONS
Soil-forming processes in loesses of the Lite Pleistocene documented by geochemical and micromorphological indices allowed for the recognition of diagnostic horizons of interloessial fossil soils of different age rank as:
1. For interglacial soils, the argillic — Bt is diagnostic and to a lesser degree, the luvic-Eet horizon; for interstadial soils - the cambic poor developed Bbr and special mollic-A horizons are diagnostic.
2. Definite horizons and their succession in profiles created a basis for distinguishing soil types of different developmental degree.
3. All the investigations (both field and laboratory) made it possible to document the occurrence of five interstadial soils jointly those occurringon the surface, with Late-Pleistocenic bases as well as a very well formed interglacial Eemians soil developed from older loess.
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K. K on eck a-B etley
GLEBY KOPALNE PÓŹNEGO PLEJSTOCENU WYTWORZONE Z LESSÓW Katedra G leb ozn aw stw a SG G W w W arszaw ie
STRESZCZENIE
Przedstawiono pedostratygrafię kilku odsłon ięć lessów vistulianskich i starszych południow o- w schodniej Polski. Poziom y diagnostyczne dla kopalnych paleopedonów rozpoznano i w yd zielon o na podstawie badań fizykochem icznych, m ikrom orfologicznych, palynologicznych oraz nielicznych datowań 14C i TL. Stw ierdzono w spągu vistulianskiej serii lessów kopalną glebę z interglacjału eem sk iego, w ytw orzoną z lessu starszego poprzedniego piętra ziem nego z dobrze wykształconym poziom em diagnostycznym Bt argil lic. Przykrywa ją zespół gleb kopal nych m łodszych, i nterstadial- nych, w ytw orzonych z lessów vistulianskich. Jako diagnostyczne dla gleb m łodszych w ydzielono: poziom próchniczny m ollic i słabo w ykształcony poziom wietrzenia B b r -c a m b ic .
Prof. dr Krystyna Konecka-Betley Departm ent o f Soil Science
Warsaw Agricultural IJniversily-SGGW 02-528 Warszawa, Rakowiecka 26/30, Poland
