_UDK 551.583.7:911.52(434)"63":902.67_
Documenta PraehistoricaXXXV (2008)
Holocene paleoclimatic and paleohydrological changes
in the Särret basin, NW Hungary
Pal Sümegi1, Sändor Gulyäs1, Gergo Persaits1
1 University of Szeged, Department of Geology and Paleontology, Hungary
sumegi@geo.u-szeged.hu
ABSTRACT - According to detailed sedimentological and paleontological analyses carried out on sam-
ples taken from the Särret-Nädasdladäny core-profile, a complete environmental history of a neotec-
tonic depression was drawn. The sequence is composed of fluvial-lacustrine and marshland deposits
which started to accumulate during the Late Glacial and culminated at the beginning of the Holo-
cene. The highly characteristic changes in the biofacies were linked to changes in the lithofacies with-
in this sequence. A transition in the dominance of moving water species, observable initially in la-
custrine species preferring well-lit, well-oxygenated conditions was observed. Eventually, the littoral
and eutrophic lacustrine species, as well as marsh-dwellers, became dominant in the profile, mark-
ing the emergence of uniform peat land in the Särret Basin.
IZVLEČEK - S pomočjo sedimentoloških in paleontoloških analiz vzorcev iz vrtine Särret-Nädasdla-
däny lahko sestavimo popolno okoljsko zgodovino te neotektonske depresije. Zaporedje sestavljajo
rečni, jezerski in močvirski depoziti, ki se začnejo v poznem glacialu in se nadaljujejo v začetek holo-
cena. Zelo značilne spremembe v fosilnih zbirih lahko povežemo s spremembami v sedimentaciji.
Na začetku prevladujejo vrste, ki živijo v tekoči vodi, te pa kasneje zamenjajo vrste, ki živijo v jezeru,
v dobro osvetljenih vodah z dovolj kisika. Kasneje postanejo pogostejše obalne in evtrofične kot tudi
močvirske vrste, ki zaznamujejo nastanek šote v kotlini Särret.
KEY WORDS - paleohydrology; paleoecology; mollusks; Holocene; Särret
Introduction
Quaternary geological and malacological investiga-
tions in the neotectonic basin of the Sarret started
as early as the beginning of the 20th century (Kor-
mos 1909). The region, with an area of approxi-
mately 120km2 located at the interface of the Mezo-
föld and the Transdanubian Mid-Mountains, occupies
a neotectonic basin (Loczy 1913; Cserny 2000) with
a NE-SW trend which developed at the end of the
Quarternary (Dömsödi 1977) and infilled with Qua-
ternary deposits of great thickness. Although a large
portion of the peat was destroyed, compacted and
suffered pedogenesis as a result of drainage (from
1825 onwards), according to the quarter-malacolo-
gical investigations initiated by Tivadar Kormos
(1909), Holocene deposits of great thickness are still
preserved in the area under investigation.
The region of the Sarret came into the focus of Hun-
garian paleo-environmental and stratigraphic re-
search via the detailed quarter-malacological investi-
gations carried out by Endre Krolopp and Levente
Fuköh from the 1970s onwards (Fuköh-Krolopp
1986; Fuköh 1977; Krolopp 1972). Furthermore, co-
rings with continuous undisturbed samples in the
area near Nadasladany and Sarkeszi in the Sarret
region (Fig. 1), and the sedimentological, isotope-
geochemical, geochemical, pollen analytical and
quarter-malacological investigations carried out as
part of a Hungarian-British Joint Scientific Coopera-
tion in 1995, meant a major breakthrough in the
stratigraphic and paleo-environmental study of the
area (Willis et al. 1996; Cserny 2000). The findings
of the detailed chronological, lithostratigraphical
and biostratigraphical analyses of these core sam-
ples are presented in this paper.
Material and methods
Sampling was carried out with the help of a Living-
stone piston corer, following the so- called 'overlap-
ping' method. Cores were halved lengthwise after
having been transported to the lab, to suit the needs
of different analytical approaches. The terminology
and symbols of Troels-Smith (Troels-Smith 1955),
internationally accepted for unconsolidated sedi-
ments, were used to describe the lithology.
Radiocarbon measurements were carried out on 7
samples derived from the peat layers, the inwashed
charcoals and flue-ash horizons in the Light Isotope
Laboratory of the Nuclear Research Center at the
Hungarian Academy of Sciences in Debrecen. The
methodology and techniques presented in Hertelendi
et al. (1989) were followed for the digestion and
measurements. In addition, these 3 samples were
analyzed with AMS in the Isotope Laboratory of Ox-
ford University (Willis 1997). Radiocarbon dates
were utilized to determine the lithostratigraphy and
chronological units with the help of the results of
geochemical, pollen analytical and malacological
analyses. They were also utilized to determine the
rate of deposition in the sedimentary basin (Fig. 2).
The results of pollen analysis were used as input in
comparative biostratigraphy. In order to gain an ex-
pansive picture of the paleo-environment, pollen
data published earlier by Katherine Jane Willis (Wil-
lis 1997) have been utilized.
Samples collected from layers
between 8-12cm were washed
through a mesh screen for mol-
lusks. The work of Sümegi and
Krolopp (2002), Meijer (1985),
Ložek (1964) was utilized to de-
termine and put the species into
paleo-ecological groups according
to their temperature tolerance,
recent biogeographic affinity and
distribution, as well as their hu-
midity and vegetation cover pre-
ferences. Both the dominance va-
lues of the species found and the
ratio of paleo-ecological and re-
cent biogeographical groups,
along with the results of the ra-
diocarbon measurements and the
lithostratigraphy, were depicted on graphs with
Psimpoll software (Bennett 1992).
Lithological and lithostratigraphical findings
Three major lithostratigraphic units were identified
in the undisturbed, continuous core of the 398cm
deep borehole (Fig. 2). The first unit, located be-
tween depths of 398 and 268cm, is made up of al-
ternating layers of fine laminated silt, gravelly sand
and sandy gravel. According to the radiocarbon data,
the development of these silty intercalations must
have taken place between 13 000-11000 BP, at the
end of the Pleistocene.
The next sedimentary unit is located between depths
of 268 and 164cm. This horizon is composed of
white, grayish-white, calcareous muds, with a carbo-
nate content ranging between 80-90%. The majority
of the carbonates are derived from biomicritic pel-
lets secreted by the Chara vegetation and calcareous
oogonia. This sequence must have been deposited in
a relatively shallow, well-lit lacustrine system, with
eutrophic conditions prevailing at the bottom. This
lacustrine phase, characterized by the deposition of
calcareous marls, must have existed between 11000
and 9000 BP in the area.
From a depth of 164cm, there is a sudden decrease
in the carbonate content, accompanied by a promi-
nent increase in the organic content. The distribu-
tion of organic matter is not homogenous and by no
means dispersed, but resembles a downward flame-
like structure made up of the remnants of peat fern
(Thelypterispalustris). All this points to the emer-
gence of individual floating mats, which must have
Fig. 1. The area of the Sarret catchment basin, with the Sarret-Nadas-
dladany borehole (I.) marked.
Fig. 2. Palaeo-ecological results of the Särret-Nädasdladäny I core sequence.
united and closed within a period of 100-200 years.
A recent analogy for the development of such float-
ing mats is known from Lake Velencei, situated NE
of the area of the Sarret (Balogh 2000).
No samples were taken from the surface down to a
depth of 48cm and no radiocarbon measurements
were taken for this part of the profile. The emer-
gence of floating mats can be placed between 8500-
8700 BP, while the development of a unified closed
peat horizon must be younger than 8500 BP. Peat
formation must have been quite significant even at
6500 BP as well, according to the radiocarbon data.
The results of malacological analysis
Some 4785 specimens belonging to 41 species have
come to light from the core. Three major malacolo-
gical zones have been identified with the help of sta-
tistical analyses on the data (Fig. 2.).
The first zone is located between depths of 398 and
270cm. According to sedimentation rates, this hori-
zon must have developed between 13 000-11 000
BP. The ratio of species with a preference for mov-
ing water habitats is above 50% in this horizon (e.g.:
Valvata psicinalis, Lithoglyphus naticoides, Pisi-
dium amnicum, Unio cf. crassus). Specimens of
the Boreal Gyraulus riparius and Valvata pulchella
have come to light from this part of the profile alone.
One of the major characteristics of this horizon is
the collective appearance of aquatic species expan-
ding during the colder phases of the Pleistocene, be-
coming restricted at the beginning of the Holocene
(Valvatapulchella, Bithynia leachi, Gyraulus ripa-
rius), and the aquatic species starting their expan-
sion during the Holocene (Lithoglyphus naticoides,
Bithynia tentaculata). This collective appearance of
mollusks preferring milder climatic and colder cli-
matic periods at the end of the Pleistocene and the
beginning of the Holocene can be regarded as one
of the most characteristic features of the Quarter-
nary malacofauna of the Carpathian basin. (Willis et
al. 1995; Sümegi 2004). Fauna of the same age and
composition have been identified from the areas of
the Tapolca basin, the Jaszsag, the bedrock horizon
of the Vörös marshland of Csaszartöltes, and the
sandpit of Töszeg (Hertelendi et al. 1993). On the
basis of these fauna horizons, we may assign the col-
lective appearance of the species Valvata pulchella
and Lithoglyphus naticoides between 12 000-9000
BP in the Carpathian Basin.
The results of the pollen analysis from the malaco-
logical samples (Willis 1997) also seem to corrobo-
rate the findings of the radiocarbon measurements
(Fig. 2).
The neotectonic depression of the Sarret was sur-
rounded by gallery, forest-like, forest-steppe taiga,
characterized by a dominance of birch (Betula) mi-
xing with conifers of common pine (Pinus silves-
tris), spruce (Picea), fir (Abies), juniper (Juniperus)
and grasses (Graminea), carices (Cyperaceae) at
the time. Although regarding the extension of the se-
dimentary basin of the Sarret (80-120 km2) (Jacob-
son-Bradshaw 1981), we may assume that the pol-
len composition of the profile reflects the composi-
tion of the vegetation on a wider, regional scale (Me-
zoföld, Bakonyalja, Bakony) and not only the adja-
cent marginal vegetation of the depression.
The second malacological horizon is located between
depths of 270-167cm. The majority of species with
a moving-water habitat preference, like Valvata pul-
chella, Gyraulus riparius, Lithoglyphus naticoides,
Lymnaea stagnalis, Pisidium amnicum, Unio cf.
crassus, became restricted. On the other hand, the
rheophilous species Valvata piscinalis managed to
survive. Moreover, there was a significant increase
in the proportion of this latter species, which has be-
come a prevailing element of this local malacologi-
cal zone. However, it must be noted that there was
a definite decrease in the size of the specimens col-
lected from the calcareous muds compared to those
from the preceding zone. According to data and ob-
servations on the recent malacofauna, as well as the
Quaternary malacofauna deriving from several pro-
files in the Nyirseg and Lake Balaton, the gastropod
species Valvata piscinalis successfully copes with
environmental transformations like that from a flu-
vial to a lacustrine habitat, surviving in the littoral
surf zone, where moving water supplies a sufficient
amount of dissolved oxygen. It is in this malacologi-
cal zone that the species Lymnaea peregra (f. ova-
ta), Physa fontinalis, Gyraulus albus, Sphaerium
corneum, and Bithynia tentaculata appear and gra-
dually become dominant. Besides these strong chan-
ges in the aqueous fauna, the amphibic species Cary-
chium minimum and Succineas also show up in
this horizon. All these changes seem to imply the de-
velopment of a relatively shallow, 1-3m deep, well-
lit, but eutrophication at the bottom lacustrine en-
vironment, characterized by mild water temperatu-
res and alkaline pH during the growth season in the
area under investigation. The higher ratio of littoral
elements implies the proximity of our sampled pro-
file to a singular littoral surf zone.
The analyzed biological zone must have emerged be-
tween 11 000 and 9000 BP. That is, the End-Pleisto-
cene, Early Holocene mesotrophic lake phase must
have emerged as early as 11 000 BP in the Sarret de-
pression, and this correlates well with the develop-
mental history of the sub-basins of the neotectonic
depression of Lake Balaton (Tapolca Basin, Kis-Bala-
ton) and the ponds located at the Danube-Tisza Inter-
fluve (Cserny-Nagy-Bodor 2000). This calcareous
mud horizon of Sarret yielded some harpoons assu-
med to be of Mesolithic Age, according to archeolo-
gical data (Marosi 1935; 1936a; 1936b; Nemeskeri
1948; Makkay 1970). Thus the calcareous muds
identified in the Nadasladany borehole may be cor-
related with a period of the Mesolithic.
According to palynological data, there was also signi-
ficant change in the composition of the vegetation
parallel with the emergence of this malacological ho-
rizon (Willis 1997). There was a shift in the advance
of deciduous trees, in contrast to the formerly domi-
nant conifers, namely birch (Betula), oak (Quercus),
elm (Ulmus), and hornbeam (Carpinus). Neverthe-
less, the ratio of common pine (Pinus silvestris) re-
mained significant. This latter factor might be stron-
gly related to the ability of the Sarret sedimentary
basins to act as a regional pollen trap in the area.
Thus pollen from the common pine woodlands,
being extensive in the Bakony Mts. at the beginning
of the Holocene, might also have been transported
into and accumulated in the sedimentary basin of
the Sarret from greater distances. To put it another
way: the basin must have preserved pollens origina-
ting from several regions characterized by different
natural endowments and highly varying plant paleo-
associations (coniferous remnant woodlands, the co-
oler basins and valleys of the Bakony Mts., deciduous
woodlands, the Bakony Mts. including the foothill
area, open loess and dolomite steppe areas, the do-
lomite cliffs of the foothill area of the Bakony, with
high relief, the area of the Mezoföld).
There was a complete turnover in the malacofauna
at the final stage of calcareous mud deposition and
the initiation of peat formation in the area of Sarret-
Nadasladany. Species with a moving water habitat
preference completely disappeared, giving way to
the extensive, Holarctic still water species. The gas-
tropod Valvata cristata is the dominant form in this
part of the profile. However, species preferring a
well-lit, well-oxygenated lacustrine habitat (Physa
fontinalis, Lymnaea peregra f. ovata, Sphaerium
corneum) also completely disappeared when peat
formation began. The increase in the proportions of
marsh-dwellers (Acroloxus lacustris, Planorbis pla-
norbis, Anisus leucostoma), and the littoral, amphi-
bic Succineas (Succinea oblonga, Oxyloma elegans)
indicate a change in the environment and lithology.
The malacological data are in close correlation with
changes in the sedimentary layers, the emergence of
floating mats and the appearance of a wet, terres-
trial-like habitat wedged into the lacustrine environ-
ment. Such island-like patches of floating mats was
observed on the Nagy-Mohos floating mat of Kallo-
semjen at the end of the 1980s. According to the fin-
dings of investigations on the recent malacofauna,
the underwater areas of the floating mats are inha-
bited by the gastropod species of Valvata cristata,
Planorbis planorbis and Anisuses. While the surfa-
ces located above the water such as wet reed, ferny
and bulrush areas are populated by Succineas and
Carychium minimum in large quantities, the com-
position of the malacofauna of the recent floating
mats of Kallosemjen is highly similar to that of the
floating mat phase observed in the borehole of Sar-
ret-Nadasdladany.
According to radiocarbon data, peat formation, re-
sulting in a transformation of the lacustrine environ-
ment, began around 9000 BP in the area under in-
vestigation, being active even at 6000 BP. Peat for-
mation must have continued even after that. How-
ever, because of the presence of mixed, disturbed
layers, no samples were taken from the surface to a
depth of 48cm.
The composition of pollens also underwent a sharp
and strong change at the beginning of peat forma-
tion, with a sudden increase in the proportions of
fern (Pteridophyta), and grass (Gramineae) pollens,
including water plants (e.g. float-grass - Glyceria).
All these changes are closely linked to the develop-
ment and evolution of floating mats in the area. The
inwash and transportation of pollens of local flowe-
ring plants into the basin was dominant during this
time, as reflected in the composition of pollens and
spores. The question is, however, what might have
caused the transformation of the basin from a regio-
nal pollen trap into a local one? It seems that the
conditions favoring pollen entrapment must have
changed in the basin as a result of the development
of floating mats also changing the entrapment capa-
city. According to investigations carried out, this hori-
zon can be characterized by the quickest rate of de-
position. The underlying factor must have been the
rapid horizontal and vertical growth and expansion
of floating mats. According to the analyses of plant
remains, the majority of the spores within this hori-
zon come from peat fern (Thelypteris palustris), one
of the most important floral elements in floating
mats. As a result of the relatively rapid growth in the
local vegetation, and the rapid accumulation and de-
position of their spores, along with rapid sedimenta-
tion, prevented the large-scale accumulation of re-
gional, distant pollens transported into the basin.
These pollens appear only subsequently in the pro-
file in this horizon.
Following the development of floating mats, the rate
of deposition decreased, accompanied by a stall in
peat formation increasing the pollen entrapment
ability of the Sarret sedimentary basin and enabling
the entrapment of regional pollens as well. As a re-
sult of this, larger amounts of pollen from oak (Quer-
cus), elm (Ulmus) hazel (Corylus), and grasses (Gra-
mineae) could have accumulated. According to the
pollen composition, a mixing of pollens deriving
from a forest steppe or closed woodland existing in
the neighborhood in a milder phase (with a trans-
portation direction from the Bakony and Vertes Mts.)
and an open steppe area (Mezoföld, loess steppes)
was identified. The early appearance of cereal pol-
lens in the Sarret-Nadasdladany section (6000 calBC)
seems to be in good agreement with the appearance
of the Early Neolithic communities and the emer-
gence of productive societies in the Carpathian ba-
sin (Hertelendi et al. 1998).
Summary
According to the detailed sedimentological and pa-
laeoontological analyses carried out on samples ta-
ken from the Sarret-Nadasdladany core-profile, a
complete environmental history of a neotectonic de-
pression have been drawn. The sequence is compo-
sed of fluvial-lacustrine and marshland deposits
which started to accumulate during the Late Glacial.
Paleo-associations determined with the help of ma-
lacological data form a line of successions, with the
first fluvial phase appearing as early as 13 000-
11 000 BP. The infant neotectonic depression cha-
racterized by fluvial conditions must have been sur-
rounded by open, gallery-like mixed taiga vegeta-
tion. At a greater distance, a more open, cold, conti-
nental forested steppe covering the loess and dolo-
mite surfaces can be reconstructed.
Around 11 000 BP the depression was inundated, re-
sulting in the emergence of a well-lit, but eutrophi-
cation at the bottom lacustrine environment, char-
acterized by a water depth of 3m in the deepest
parts of the depression. There was a change in the
vegetation around the depression at about 10 000
uncalBP, characterized by the emergence of decidu-
ous woodland in the area. A substantial amount of
pollen grains from the pinewoods surviving in the
cold relict spots in more distant, mountainous re-
gions, accumulated during the Early Holocene. The
lake was surrounded by extensive cattail and reed-
beds, as well as sedge tussocks, at the time fringed
by hardwood and softwood gallery forests and de-
ciduous woodland. These conditions survived for
some one thousand years, suggesting that the rate of
infilling (0.31 mm/year) roughly equalled that of the
rate of subsidence (11 000-9000 uncalBP).
The infilling of the basin intensified between 9000-
6500 uncal BP, with the sedimentation rate exceed-
ing 0.8 mm/year. There is a marked change in the
pollen composition here, characterized by the ap-
pearance of taxa indicating arable farming and stock-
breeding. The close correlation between the appea-
rance of taxa reflecting a production economy, and
the acceleration of the sedimentation rate, most cer-
tainly indicate the presence of human settlements
around Lake Sarret during the Early Neolithic, resul-
ting in increased erosion rates. As a result of human
activities, paludification of the lake was accelerated,
and from 6500 uncalBP onwards led to the emer-
gence of stable marshland with floating mats.
REFERENCES
BALOGH M. 2000. A lapok rendszerezese. (Systematiza-
tion of swamps). In E. Szurdoki (ed.), Tözegmohäs elöhel-
yek Magyarorszägon: kutatäs, kezeles, vedelem. (Sphag-
num biotops in Hungary: research, handling, protect)
CEWEEB Munkacsoport, Miskolc: 57-65.
BENNETT K. D. 1992. PSIMPOLL - A quickBasic program
that generates PostScript page description of pollen dia-
grams. INQUA Commission for the study of the Holocene:
working group on data handling methods. Newsletter 8:
11-12.
CSERNY T. 2000. Komplex földtani kutatasok hazai tava-
kon, lapokon es mocsarakon. (Komplex geological resear-
ches on Hungarian lakes, swamps and marshes). In E.
Szurdoki (ed.), Tözegmohäs elöhelyek Magyaroszägon:
kutatäs, kezeles, vedelem. (Sphagnum biotops in Hun-
gary: research, handling, protect) CEWEEB Munkacsoport,
Miskolc: 27-41.
CSERNY T., NAGY-BODOR E. 2000. Limnogeological inves-
tigations on Lake Balaton, In E. Gierlowski-Kordesch, K.
Kelts (eds.), Lake Basins Through Space and Time.
AAPG Studies in Geology 46: 605-618.
DÖMSÖDI J. 1977. A Fejer-megyei Sarret talajjavitö anya-
gai (tozeg, lapföld, lapi mesz). (Materials for soil amelio-
ration from the Sarret of Fejer country (peat, lime-mud)).
Agrokemia es Talajtan, 26: 331-350.
FÜKÖH L. 1977. A Fejer-megyei Sarret Mollusca faunajanak
biosztratigrafiai vizsgalata. (Biostratigraphical investiga-
tion on Mollusc fauna of Sarret in Fejer-country). Soosiana
5: 17-26.
HERTELENDI E., CSONGOR E., ZÄBORSZKY L., MOLNÄR I.,
GÄL I., GYÖRFFY M., NAGY S. 1989. Counting system for
high precision C-14 dating. Radiocarbon 31:399-408.
HERTELENDI E., LOKI J., SÜMEGI P. 1993. A Hay-tanya
melletti feltaras retegsoranak szedimentolögiai es sztrati-
grafiai elemzese. (Sedimentological and stratigraphical
examination of the profile at the Hay-tanya). Acta Geo-
graphica, Geologica et Meteorologica Debrecina 30-
31: 65-75.
HERTELENDI E., KALICZ N., RACZKY P., HORVÄTH F., VE-
RES M., SVINGOR E., FUTO I., BARTOSIEWICZ L. 1996. Re-
evolution of the Neolithic in eastern Hungary based on ca-
librated radiocarbon dates. Radiocarbon 37:239-244.
JACOBSON G. L., BRADSHAW R. H. W. 1981. The selection
of sites for palaeovegetational studies. Quaternary Re-
search 16: 80-96.
KERNEY M. P., CAMERON R. A. D., JUNGBLUTH J. H. 1983.
Die Landschnecken Nord- und Mitteleuropas. P. Parey,
Hamburg-Berlin.
KORMOS T. 1909. A Fejer-megyei Sarret geolögiai mültja
es jelene. (Geological past and present of the Sarret in Fe-
jer-country) In L. Löczy (ed.), A Balaton tudomänyos ta-
nulmänyozäsänak eredmenyei 1.1. (Results of the study
of Balaton lake). Paleontolögiai Függelek 1: 66.
KROLOPP E. 1972. Negyedidoszak. (Quarter) In A. Ronai,
F. Szentes (eds.), Magyaräzö Magyarorszäg 200.000-es
földtani terkepsorozatähoz. 34. Szekesfehervar. (Me-
moir to the 1:200.000 scale geological map series of Hun-
gary 34. Szekesfehervar).
LOŽEK V. 1964. Quartermollusken der Tschechoslowa-
kei. Rozpravy Üstavu ustedniku geologichkeho 31. Praga.
LOCZY L. 1913. A Balaton tö tudomänyos vizsgälatänak
eredmenyei. (Results of the study of Balaton lake). Mag-
yar Földrajzi Tarsasag Balaton Bizottsaganak kiadvanya.
Budapest: 617.
MAKKAY J. 1970. A kokor es rezkor Fejer megyeben. In
Fitz J. (ed.), Fejer megye törtenete az öskortöl a honfo-
glaläsig. Fejer megye törtenete I. Szekesfehervar: 9-52.
MAROSI A. 1935. Öskokori szigony Mentöpusztaröl. Sze-
kesfeherväri Szemle: 75-76.
1936a. Kormeghatarozo adatok a csor-merftopusztai
oskori csontszigonyhoz. Szekesfeherväri Szemle: 40-
42.
1936b. A szekesfehervari muzeum oskori csontszigo-
nya. Archaeolögiai Ertesitö 49: 83-85.
MEIJER T. 1985. The pre-Weichselian nonmarine mollus-
can fauna from Maastricht-Belvedere (Southern Limburg,
the Netherlands). Mededelingen Rijks Geologische Dienst
39: 75-103.
NEMESKERI J. 1948. A mezolithikus kultura uj nyomai
Magyarorszagon. Termeszettudomäny 3:221-222.
SÜMEGI P. 2004. The results of paleo-environmental re-
construction and comparative geoarcheological analysis
for the examined area. In P. Sümegi, S. Gulyas (eds.), The
geohistory of Bätorliget Marshland. Archaeolingua Press.
Budapest: 301-348.
SÜMEGI P., KROLOPP E. 2002. Quartermalacological ana-
lyses for modeling of the Upper Weichselian palaeoenvi-
ronmental changes in the Carpathian Basin. Quaternary
International 91:53-63.
TROELS-SMITH J. 1955. Karakterisering af lose jordater.
Danmarks Geologiske Undersogelse, ser. IV.
WILLIS K. J. 1997. The Impact of Early Agriculture upon
the Hungarian Landscape. In J. Chapman, P. Dolukhanov
(eds.), Landscapes in Flux Central and Eastern Europe
in Antiquity. Oxbow Books. Oxford: 93-207.
WILLIS K. J., SÜMEGI P., BRAUN M., TOTH A. 1995. The
Late Quaternary Environmental History of Batorliget, N.E.
Hungary. Palaeoclimatology, Palaeoecology, Palaeogeo-
graphy 118:25-47.
1996. Flora, fauna and human impact changes in
the Western part of Hungary at Lateglacial/Postgla-
cial transition. Manuscript, Cambridge University, Sub-
department of Quaternary Sciences.
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