Pollen records of 11 profiles from Wendland in northern Germany

1) Ingesamt 11 Profile aus sechs Mooren und Seen im Gebiet des Hannoverschen Wendlandes wurden pollenanalytisch untersucht. Die Ablagerungen umfassen den Zeitraum vom Beginn der Älteren Tundrenzeit bis zur Gegenwart. 2) Die Waldgeschichte des Hannoverschen Wendlandes weist teils Merkmale der atlantisch geprägten Gebiete Nordwestdeutschlands, teils solche des kontinental beeinflußten nordostdeutschen Raumes auf und nimmt damit eine Zwischenstellung ein. 3) Die Kiefer wandert zu Beginn der Allerödzeit ein, d.h. später als im mecklenburgisch-märkischen Gebiet und im mitteldeutschen Trockengebiet. Im Verlauf der Allerödzeit bildeten sich hier wie dort lichte Kiefern-Birken-Wälder aus. 4) In der Jüngeren Tundrenzeit fand zunächst nur eine geringe Auflichtung der Wälder statt, und die Kiefer überwog weiterhin. Erst im späteren Verlauf dieser stadialen Phase breitete sich die Birke aus und verdrängte die Kiefer. Der späte Rückgang der Kiefer stellt eine Parallele zu der Entwicklung in Südostmecklenburg und in der Altmark dar. Die Abgrenzung dieser Phasen in der Jüngeren Tundrenzeit ist durch eine 14C-Datierung gesichert. 5) Noch im Atlantikum ähneln die Diagramme aus dem Gartower Talsandgebiet im Osten des Wendlandes in ihren hohen Kiefernanteilen denen der Sandergebiete in Brandenburg. Die Diagramme aus dem Moränengebiet des westlichen Wendlandes schließen dagegen mehr an die der östlichen Lüneburger Heide und des Hamburger Gebietes an. Dieser Unterschied wird auf edaphische Unterschiede zurückgeführt. 6) Seit dem frühen Subboreal glich auch die Vegetation des Gartower Gebietes mehr den buchenarmen Waldgesellschaften auf sauren Sandböden, wie sie im atlantischen Westen vorkommen. Die Kiefern sind fast ganz aus dem Waldbild verschwunden, wobei der rasche Rückgang zu Beginn des Subboreals sicher zu einem wesentlichen Teil vom Menschen beeinflusst worden ist. Die anschließende kiefernarme Zeit dauerte im gesamten Wendland bis zum Beginn der Kieferaufforstungen in der Neuzeit. 7) In allen untersuchten Diagrammen ist etwa seit dem Subboreal eine Besiedlung nachzuweisen. Diese muß im Osten des Wendlandes intensiver gewesen sein als im Westen. Es lassen sich Phasen geringer und intensiver Besiedlung nachweisen. 8) Seit Beginn des Subboreals ist das Waldbild schon so stark vom Menschen beeinflusst, dass die Ausbreitungsgeschichte der Laubwaldarten nicht ohne Berücksichtigung der Siedlungsphasen diskutiert werden kann. Besonders im Westen bestand eine ausgedehnte Lindenphase, die durch eine Siedlungszeit (Bronzezeit) beendet wurde. Beim folgenden Rückgang der Siedlungsintensität breitet sich bevorzugt die Hainbuche aus, die dann bei der nächsten Besiedlungsphase (Eisenzeit) zurückging. Erst danach erfolgte die maximale Rotbuchenausbreitung, die nur im Westteil des Wendlandes bedeutende Ausmaße zeigte, während im Ostteil rot- und hainbuchenreiche Eichenwälder entstanden. 9) Seit Beginn der mittelalterlichen Besiedlung ist dann der Eingriff des Menschen so stark gewesen, dass die edaphisch bedingten Unterschiede zwischen Moränen- und Sandergebieten im Pollenspektrum verwischt wurden. Sowohl die buchenreichen Wälder des westlichen als auch die buchenarmen Wälder des mittleren und des östlichen Teilgebietes müssen zu fast reinen Eichenwäldern geworden sein. 10) Calluna-Heiden sind im östlichen Wendland schon in vorgeschichtlicher Zeit nachzuweisen. Im Mittelalter und in der Neuzeit treten sie im gesamten Wendland auf. Etwa im 18. und 19. Jahrhundert war die Ausdehnung der Heideflächen am größten. Erst danach wurden sie im Zuge der Kiefernaufforstungen bis auf geringe Reste verdrängt. 11) Während in der spätglazialen Vegetation Juniperus auftritt, ist der Wacholder sowohl in vorgeschichtlicher als auch in geschichtlicher Zeit - im Gegensatz zur Lüneburger Heide - wohl niemals ein Bestandteil der anthropogenen Calluna-Heiden gewesen.

Palynology on sediment profile Tso Kar in Ladakh

Palynological investigation of a 410 cm long core section from Tso Kar (33°10'N, 78°E, 4527 m a.s.l.), an alpine lake situated in the arid Ladakh area of NW India at the limit of the present-day Indian summer monsoon, was performed in order to reconstruct post-glacial regional vegetation and climate dynamics. The area was covered with alpine desert vegetation from ca. 15.2 to 14 kyr BP (1 kyr=1000 cal. years), reflecting dry and cold conditions. High influx values of long-distance transported Pinus sylvestris type pollen suggest prevailing air flow from the west and northwest. The spread of alpine meadow communities and local aquatic vegetation is a weak sign of climate amelioration after ca. 14 kyr BP. Pollen data (e.g. influx values of Pinus roxburghii type and Quercus) suggest that this was due to a strengthening of the summer monsoon and the reduced activity of westerly winds. The further spread of Artemisia and species-rich meadows occurred in response to improved moisture conditions between ca. 12.9 and 12.5 kyr BP. The subsequent change towards drier desert-steppe vegetation likely indicates more frequent westerly disturbances and associated snowfalls, which favoured the persistence of alpine meadows on edaphically moist sites. The spread of Chenopodiaceae-dominated vegetation associated with an extremely weak monsoon occurred at ca. 12.2-11.8 kyr BP during the Younger Dryas interstadial. A major increase in humidity is inferred from the development of Artemisia-dominated steppe and wet alpine meadows with Gentianaceae after the late glacial/early Holocene transition in response to the strengthening of the summer monsoon. Monsoonal influence reached maximum activity in the Tso Kar region between ca. 10.9 and 9.2 kyr BP. The subsequent development of the alpine meadow, steppe and desert-steppe vegetation points to a moderate reduction in the moisture supply, which can be linked to the weaker summer monsoon and the accompanying enhancement of the winter westerly flow from ca. 9.2 to 4.8 kyr BP. The highest water levels of Tso Kar around 8 kyr BP probably reflect combined effect of both monsoonal and westerly influence in the region. An abrupt shift towards aridity in the Tso Kar region occurred after ca. 4.8 kyr BP, as evidenced by an expansion of Chenopodiaceae-dominated desert-steppe. Low pollen influx values registered ca. 2.8-1.3 kyr BP suggest scarce vegetation cover and unfavourable growing conditions likely associated with a further weakening of the Indian Monsoon.

Age determination and pollen profile of sediment core Trentelmoor, Peine, northern Germany

The filling up of the lake which existed in the basin of the Trentelmoor (40 km E of Hannover, Germany) - in Preboreal times was finished 2000 years ago. Since then fen vegetation has covered the former lake's surface. The postglacial development of the vegetation follows the pattern which is typical of Central Europe. However, due to the poorness of the soils around the Trentelmoor, the frequencies of some tree species differ. Beech for example never reached - for the benefit of oak - that importance which this tree species usually gains on better soils. Human impact becomes recognisable in the upper Neolithic for the first time. The area has been settled continuously, but with changing intensities, throughout the last 3000 years. When the manuscript of this paper went to press the results of two radiocarbon age determinations only were completed. An additional three determinations were completed somewhat later. See the accompanying table for results.

AMS radiocarbon dates and pollen analysis from Zugspitzplatt

On the strongly karstified and almost unvegetated surface of the Zugspitzplatt, at an altitude of about 2290 m in the Wettersteingebirge, there is a doline within which over a period of several thousand years a bed of fine loess-like sediment, almost 1m thick, has accumulated. Notwithstanding the situation of this locality far above the present tree-line, this infill contains quantities of pollen and spores sufficient for pollen analysis without use of any enrichment techniques. Despite poor pollen preservation, it was possible to date the basal layers of this profile on the basis of their pollen assemblages. AMS dating (7415 ± 30 BP) has confirmed that the oldest sediments were laid down during the early Atlantic period, the time of the thermal optimum of the Holocene. At least since that time this site has never been overridden by a glacier. The moraine associated with the Löbben Oscillation between 3400 and 3100 BP - here represented by the so-called Platt Stillstand (Plattstand) - did not quite reach the doline. A diagram shows known Holocene glacial limits. The composition of the pollen assemblages from the two oldest levels with high pollen concentrations strongly suggests that the distance between the doline and the forest was much less during the Atlantic than at present.

Pollen and macroremains from profiles from site Osterholz and Elm

The biostratigraphic classification of the Pleistocene in north-western and central Europe is still insufficiently known, in spite of numerous geological and vegetation-history investigations. The question is not even clear, for example, how often a warm-period vegetation with thermophilous trees such as Quercus, Ulmus, Tilia, Carpinus etc could develop here. In past years, on the basis of several geological and vegetation-history findings, suspicion has often been expressed that some of the classical stages of the Pleistocene could include more warm periods than heretofore assumed, and as a result of recent investigations the period between the Waal and Holstein interglacials seems to include at least two warm periods, of which the Cromer is one. This paper contributes to this problem. The interglacial sediments coming from the Elm-Mountains near Brunswick and from the Osterholz near Elze - both within the limits of the German Mittelgebirge - were investigated by pollen analysis. In both cases a Pinus-Betula zone and a QM zone were found. The vegetation development of the Pinus-Betula zone is characterized in both sequences by the early appearance of Picea. Because of strong local influence at the Osterholz a detailed correlation is difficult. However, vegetation development at the time of the QM zone at both sites was similar; it is especially characterized by the facts that Ulmus clearly migrated to the site earlier than Quercus and was very abundant throughout this time. Furthermore, both diagrams show very low amounts of Corylus. The interglacial of the Osterholz shows in addition to the above; a Carpinus-QM-Picea-zone in which Eucommia reaches a relative high value and in the upper of which Azolla filiculoides was also found. The similarity of vegetation development justifies acceptance of the same age for the occurrences. A comparison of the vegetation development at the Elm and the Osterholz with those of the Eem, Holstein, Waal, and Tegelen warm periods as well as with all the Cromer sites so far investigated shows that only a correlation with the Cromer Complex is possible. This correlation is supported by the geologic relations in the Osterholz (the deposit is overlain by Elster till). Therefore the till-like material with Scandinavian rock fragments underlying the deposit at Elm is of particular interest. The 'Rhume' interglacial beds at Bilshausen, only 60 km south of Osterholz, is also assigned to the Cromer complex, but the two deposits cannot be of the same age because the vegetation development differs. Therefore the Cromer complex must include at least two warm periods. Further conclusions about the relative stratigraphic position of these two occurrences and correlations of other Cromer sites are at this time not possible, however.

Pollen profiles from three former lakes in the Lake Garda area

1. Late glacial and postglacial sediments from three former lakes in the Lake Garda area (Southern Alps) were investigated. 2. The pollen diagram from Bondone (1550 m) shows an older phase rich in NAP. A younger one corresponds with the Younger Dryas time according to two radiocarbon determinations. In the Preboreal no climatic deterioration could be found. 3. At first plants, which are nowadays typical for snow-ground, pioneer and dwarf shrub associations, immigrated into the surroundings of Bondone. In Alleröd times larch and pine appeared as the first trees. At the beginning of the Preboreal dense forest existed in that region. During the Alleröd timber line was at about 1500 m. 4. In the pollen diagrams from Saltarino (194 m) and Fiavè (654 m) an oldest period rich in NAP is followed by two stadial and two interstadial phases. Tree birches and larches immigrated during the oldest interstadial phase. 5. In the case of Saltarino and Fiavè only a preliminary dating could be made. A correlation seems to be possible with diagrams published by Zoller as well as with the diagram of Bondone. Discrepances in dating, which arise then, are discussed. According to the two possibilities of dating the youngest stadial is synchronous either with the so-called Piottino stadial or the Younger Dryas time. Consequently the oldest interstadial phase of Saltarino corresponds either with the Bölling or with a pre-Bölling interstadial. The last possibility seems to be more probable. 6. In the southern part of the Lake Garda area reforestation was preceded by a long shrub phase mainly with Juniperus. At about 650 m there was a period with Pinus mugo and only with a small amount of Juniperus before reforestation. A phase with Betula nana well known from areas north of the Alps could nowhere be found. 7. In the area under study larch appeared as the first tree. Lateron it has been the most important constituent of the forests near timber line. Birch, which plays an important role as a pioneer tree in Denmark - for instance at the transition of the pollen zones III/IV - as well as in Southern Germany during Bölling time, was of less importance at the southern border of the Alps. In that area the spreading of Pinus occurred very early causing dense forests. 8. During the last stadial phase (probably Younger Dryas time) dense forests with Pinus and Larix existed at 650 m. In the lower part of the Lake Garda area, however, both thermophilous trees as Quercus and herbs frequently occurred. This leads to the conclusion that during this time tree growth was limited by dryness in lower altitudes of the border of the Southern Alps. Pinus and Juniperus, however, do not show higher values in this period, a fact which cannot yet be explained. 9. A list of plants, which were found in the sediments, is compiled. Helodium lanatum, Dictamnus albus, Mercurialis cf. ovata, Buxus, Cerinthe cf. minor, Onosma, Anthericum and Asphodelus albus are findings, which are of special interest for the history of the flora of that region.

Lithology and pollen record of various sediment profiles of postglacial age from Bavaria, Germany

(Einleitung) Im süddeutschen Jungmoränengebiet wurden während der letzten 25 Jahre verschiedene vegetationsgeschichtliche Arbeiten durchgeführt, die der Untersuchung der Späteiszeit galten. Die wichtigsten von ihnen stammen von G. Lang (1952), A. Bertsch (1961), H. Müller (1962) und H. Schmeidl (1971). Ohne Zweifel müssen die dabei gewonnenen Ergebnisse in anderen Landschaften des nördlichen Alpenvorlandes überprüft und verschiedene Probleme weiterhin verfolgt werden, wie z. B. das der Definition und Umgrenzung der Bölling-Zeit und der Älteren Tundrenzeit s. str. und die Abhängigkeit der Vegetationsentwicklung von der Meereshöhe. Die vorliegende Studie ging auch auf die Notwendigkeit zurück, die spätglazialen Ablagerungen bei dem Tonwerk Kolbermoor nahe Rosenheim, einer der klassischen Stätten der Quartärforschung im nördlichen Alpenvorland, einer vegetationsgeschichtlichen Neubearbeitung zu unterziehen. Die Untersuchungen wurden auf benachbarte Seen, den Sims-See und den Hofsrätter See, ausgedehnt, da die Ergebnisse von Kolbermoor faziell beeinflußt schienen (Niedermoore) und an limnischem Material überprüft werden mußten.

Age determination and pollen profile of sediment core Voulkaria 1966, Greece

Lake Voulkaria is situated in northwestern Greece in the Prefecture of Etoloakarnania, 6 km SW of the city of Vonitsa and 10 km east of the northern tip of the island of Levkás (Leukás, Lefkada). The lake is separated from the Ionian Sea on the West by a narrow limestone ridge ca 10 m high and has a size of 940 ha. An almost continuous fringe of Phragmites surrounds the open water. This reed bank is up to 500 m wide along the southern shore of the lake. Water depth is low, predominantly less than 2 m. In the south-eastern part of the lake a maximum depth of 3.1 m was measured in September 1997.

Pollen and macroremains from four profiles from site Samerberg 1

Pollen and macrofossil analysis of lake sediments revealed the complete development of vegetation from Riss late-glacial to early Würm glacial times at Samerberg (12°12' E, 47°45' N, 600 m a.s.l) on the northern border of the Alps. The pollen bearing sediments overlie three stratigraphic units, at the base a ground-moraine, then a 13 m thick layer of pollen free silt and clay, and then a younger moraine; all the sediments including the pollen bearing sediments, lie below the Würm moraine. The lake, which had developed in an older glacial basin, became extinct, when the ice of the river Inn glacier filled its basin during Würm full-glacial time at the latest. One interglacial, three interstadials, and the interdigitating treeless periods were identified at Samerberg. Whereas the cold periods cannot be distinguished from one another pollenanalytically, the interglacial and the two older interstadials have distinctive characteristics. A shrub phase with Juniperus initiated reforestation and was followed by a pine phase during the interglacial and each of the three interstadials. The further development of the interglacial vegetation proceeded with a phase when deciduous trees (mainly Quercus, oak) and hazel (Corylus) dominated, though spruce (Picea) was present at the same time in the area. A phase with abundant yew (Taxus) led to an apparently long lasting period with dominant spruce and fir (Abies) accompanied by some hornbeam (Carpinus). The vegetational development shows the main characteristics of the Riss/Würm interglacial, though certain differences in the vegetational development in the northern alpine foreland are obvious. These differences may result from the existence of an altitudinal zonation of the vegetation in the vicinity of the site and are the expression of its position at the border of the Alps. A greater age (e.g. the Holsteinian) can be excluded by reason of the vegetational development, and is also not indicated at first sight from the geological and stratigraphical data of the site. Characteristic of the Riss/Würm vegetational development in southern Germany - at least in the region between Lake Starnberg/Samerberg/Salzach - is the conspicuous yew phase. According to absolute pollen counts, yew not only displaced the deciduous species, but also displaced spruce preferentially, thus indicating climatic conditions less favourable for spruce, caused by mild winters (Ilex spreading!) and by short-term low precipitation, indicated by the reduced sedimentation rate. The oldest interstadials is bipartite, as due to the climatic deterioration the early vegetational development, culminating in a spruce phase, had been interrupted by another expansion of pine. A younger spruce-dominated period with fir and perhaps also with hornbeam and beech (Fagus) followed. An identical climatic development has been reported from other European sites with long pollen sequences (see chapter 6.7). However, different tree species are found in the same time intervals in Middle Europe during Early Würm times. Sediments of the last interglacial (Eem or Riss/Würm) have been found in all cases below the sediments of the bipartite interstadial, and in addition one more interstadial occurs in the overlying sediments. This proves that Eem and Riss/Würm of the north-european plain resp. of the alpine foreland are contemporaneous interglacials although this has been questioned by some authors. The climax vegetation of the second interstadial was a spruce forest without fir and without more demanding deciduous tree species. The vegetational development of the third interstadial is recorded fragmentary only. But it has been established that a spruce forest was present. The oldest interstadial must correspond to the danish Brørup interstadial as it is expressed in northern Germany, the second one to the Odderade interstadial. A third Early Würm interstadial, preserved fragmentarily at Samerberg, is known from other sites. The dutch Amersfoort interstadial most likely is the equivalent to the older part of the bipartite danish Brørup interstadial.

Lithology, age determination and pollen records of five profiles for nothern Bavaria, Germany

Palynological investigations in northeastern Bavaria (Bavarian Vogtland, Fichtelgebirge, Steinwald) reveal the Late Glacial and Postglacial history of the regional vegetation. Radiocarbon data in comparison with those from the neighbouring regions (Rhön, Oberpfälzer Wald, Bavarian Forests) show a time lag in the development of the arboreal vegetation due to migration processes. The Fichtelgebirge is the southernmost part ofnortheastern Bavaria where the early Alleröd period (pollen zone IIa) is characterised by a dominance of birch forests. Hazel reached maximal values around 8000 BP in the area from the Fichtelgebirge to the Bavarian Forests, e.g. about 600 years earlier than in the more northern Rhön mountains. For spruce there is a considerable time lag between the Bavarian Forests and the Fichtelgebirge. Spruce spreading started in the Fichtelgebirge during the older part of the Atlantic period (pollen zone VI). At the same time, spruce already was the dominant tree in the Bavarian Forests. During the younger part of the Atlantic period (pollen zone VII) spruce and mixed oak forest tree species frequently occurred in the Fichtelgebirge. At the end of pollen zone VI, spruce came to dominance. At the same time, the immigration of beech started. During the Subboreal period (pollen zone VIII), spruce remained being a dominant member in the forests and at the end of pollen zone VIII, fir began to spread rapidly. During the first part of the Subatlantic period (pollen zone IX) spruce, beech, fir and pine formed the mountainous forests in the Fichtelgebirge. In the area of the Bavarian Vogtland, however, fir was a dominant forest tree during pollen zone IX, while spruce and beech played a less important role. During the 12th century, human colonisation started in the area of the Fichtelgebirge. This is 400 years later as in the area of the Rhön mountains. Indicators for earlier forest clearances are rare or absent.

Lithology and palynology of profiles from three low mountain ranges in northern Germany

Im Fichtelgebirge, im Harz und in der Rhön wurden die spätglazialen und frühpostglazialen Ablagerungen von vier Mooren in 625-805 m Meereshöhe pollenanalytisch hinsichtlich von Makrofossilien (Samen, Früchte) und stratigraphisch untersucht. 1. Nur im Fichtelgebirge konnte in 625 m Höhe ein vollständiger Spätglazialablauf aufgedeckt werden. Es handelt sich dabei um einen ehemaligen kleinen See südlich Fichtelberg, der wahrscheinlich durch Tieftauen eines begrabenen Firn- oder Schneefeldes entstand. Betula pubescens wurde kontinuierlich vom Ende der Älteren Tundrenzeit bis zum Boreal nachgewiesen. Auf nahe Vorkommen von Kiefern darf man seit IIb (Jüngere Allerödzeit) schließen, sie wurden aber durch die Jüngere Tundrenzeit, während der es noch zu Solifluktionserscheinungen kam, von ihren höher gelegenen Standorten wieder verdrängt. Die allerödzeitlichen Birken- bzw. Birkenkiefernwälder müssen in diesen Höhen noch licht oder parkartig gewesen sein. Verbreitet waren Rasengesellschaften, die hauptsächlich aus Gramineen und Artemisia bestanden. Auch Beutla nana und Pollen von Ephedra cf. distachya wurden nachgewiesen. In der Seelohe (770-780 m) ist nur der Ausklang einer waldarmen Zeit, offensichtlich der Jüngeren Tundrenzeit, erfaßt. Großreste von Bäumen fehlen. 2. Im Oberharz (Radauer Born, 800 m) wurde nur ein kurzes Stück der Jüngeren Tundrenzeit aufgedeckt. Großreste von Bäumen fehlen hier ebenfalls. Aus dem Praeboreal stammt der erst fossile Nachweis von Betuala nana im Oberharz. Die Zwergbirke wächst auf dem Moor noch heute und gilt hier als Eiszeitrelikt. 3. Eine Datierung der spätglazialen Ablagerungen vom Roten Moor in der Rhön ist zur Zeit nur mit Vorbehalt möglich. Zwar wurde hier der Laacher Bimstuff gefunden, er ist jedoch umgelagert und unmittelbar über dem Tuffhorizont befindet sich eine Schichtlücke. Wahrscheinlich zeigt die Bimsstuffschicht aber doch noch den Allerödhorizont an. 4. Während der Jüngeren Tundrenzeit dürfte im Fichtelgebirge die Waldgrenze bei etwas 600 m gelegen haben. Das bedeutet gegenüber der heutigen Waldgrenze eine Erniedrigung um rund 700 m. Am Schluß der Älteren Tundrenzeit lag die Waldgrenze wahrscheinlich wie in der Allerödzeit höher als 600-650 m, aber unter 800 m. 5. Pollenkörner der Ericalen sind in den Ablagerungen aus dem Harz wesentlich häufiger als in den anderene Gebieten. Häufungen von Ericalen-pollen sind besonders für Spätglazialablagerungen solcher Gebiete charakteristisch, die heute im subozeanischen oder ozeanischen Klimabereich liegen (Niederlande, Irland). 6. Während sich die Bodengegensätze in der heutigen Vegetation der drei Untersuchungsgebiete sehr deutlich bemerkbar machen, wurden keine nennenswerten Unterschiede im spätglazialen Pollenniederschlag der drei Mittelgebirge gefunden. Vermutlich erfolgte die Auswaschung der Nährstoffe aus den an sich nährstoffkräftigen Granitverwitterungsböden während der Späteiszeit nicht so rasch, wie es heute der Fall ist. Die Niederschlagsmengen dürften geringer und das Klima weniger humid gewesen sein. 7. In der Liste der spätglazialen Pflanzen überwiegen die Arten mit borealzirkumpolarer Verbreitung. Arktisch-alpine Arten treten zurück. Kontinentale und subatlantische bzw. subozeanische Arten sind etwa gleich stark vertreten.

Biostratigraphical investigations of Lago d'Averno, near Naples

Remains of diatoms, molluscs, ostracods, foraminifera and pollen exines preserved in the sediments of Lago d'Averno, a volcanic lake in the Phlegrean Fields west of Naples, allowed us to reconstruct the changes in the ecological conditions of the lake and of the vegetation around it for the period from 800 BC to 800 AD. Lago d'Averno was at first a freshwater lake, temporarily influenced by volcanic springs. Salinity increased slowly during Greek times as a result of subsidence of the surrounding land. Saline conditions developed only after the lake was connected with the sea by a canal, when Portus Julius was built in 37 BC. The first post-Roman period of uplift ended with a short freshwater phase during the 7th century after Christ. Deciduous oakwoods around the lake was transformed into a forest of evergreen oaks in Greek times and thrived there - apparently almost uninfluenced by man - until it was felled, when the Avernus was incorporated into the new Roman harbour in 37 BC, to construct a shipyard and other military buildings there. Land-use was never more intense than during Roman times and weakest in Greek and Early Roman times, when the Avernus was considered a holy place, the entrance to the underworld.

Lithology and pollen record of 4 profiles from the Bavaria, southern Germany

Palynological investigations of sediments from northern Bavaria (Rhön, Grabfeld, Lange Berge) reveal the Late Glacial and Postglacial history of the regional vegetation. The older sedirnents were found in the Rhön (Schwarzes Moor) and date back into the Bölling Period. At the end of that period pine spread into the Grabfeld. In both areas Lacher Tuff has been found. A radiocarbon date of 10,300 BP was found for the Late Glacial - Postglacial transition and one of 9300 BP for the Preboreal - Boreal transition. Hazel reached its highest values in the Rhön around 7,400 BP. During the Atlanticum a deciduous mixed oak forest covered the Rhön and Grabfeld regions. Beech dominated since the Subatlanticum. In the Lange Berge region, however, a mixed forest with Fagus, Picea, Pinus and Abies developed. In the Rhön first anthropogenic influence was found during the Latene Period. The boundary between zone IX and X has been dated at 820 A.D., and the start of extensive forest clearances at 1000 A. D. A culmination of landuse was found for the Medieval Period. At the end of that period however the Rhön was deserted. New forest clearances started around 1500 A.D., but were interrupted by the 'Thirty Years War'. Afterwards the Rhön got its present appearance.