DOI chapter:
Grenzgänger, traders and the last hunter-gatherers of the North European Plain
DOI chapter:Bauerochse, Andreas; Leuschner, Hanns Hubert: Neolithic colonisation of the southwestern Dümmer basin (NW Germany) – evidence from palaeobotanical data
DOI Page / Citation link:https://doi.org/10.11588/diglit.66745#0049
48
Neolithic colonisation of the southwestern Dummer basin (NW Germany) - evidence from palaeobotanical data
samples from trees with different morphology. Trees
with a diameter of less then 20 cm and stumps were
not sampled. All samples were cut with a chain saw.
The preparation of the samples followed standard
procedures (e.g. described by Leuschner 1994; for a
detailed description of the preparation see Leuschner
et al. 2007, 185-186). The tree ring series have been
cross-dated and the matches statistically evaluated by
calculating the coefficient of parallel variation and
/-values (Bailee/ Pilcher 1973).
Results
At the bottom of the diagram, the presence of pol-
len from pine (Pinus sylvestris) and alder (Alnus
glutinosa) presents a picture of a mosaic of wet de-
pressions and drier sites poor in nutrients, covered
by pines and species of the mixed oak forest (mainly
oaks). Increasing pollen of peatland species and the
decrease of the pine curve in the course of the lower
centimetres of the diagram show increasing wetness
and paludification (Fig. 2). Almost at the same time
when the first trackway, PR 31 (Fig. 3), was built,
pollen of herbs and emerging anthropogenic indica-
tors (after Behre 1981) mark an increasing human
impact in the area. Dendrochronological data from
the trackway timbers document its construction in
4629 BC at the latest, and following maintenance for
at least 100 years (Fig. 4; cf. Achterberg et al. 2015).
Partly built directly on the mineral ground, its
construction reflects the beginning of the paludifica-
tion, showing a number of features indicating soft
and muddy subsoil. A multilayered substructure and
a superstructure - up to about 5 m wide - partly fixed
by longitudinal stems put laterally across the construc-
tion and pierced with dowels, stabilised its position
(Fig. 3).4 The timbers were cut in four felling episodes,
starting at 4629 BC, 4614 BC, 4590 BC, and 4538 BC,
all of which coincided with times when the trees were
characterised by growth depressions (Fig. 4). However,
we have merely 36 timbers dated, out of which only six
were completely preserved to include the waney edge
(Fig. 4; Achterberg et al. 2015), and so we cannot be
sure whether our data cover the entire period during
which the trackway was used.
The remains of a further trackway, Pr 36, situated
about 100 m west of Pr 31, demonstrate the presence
of a second corduroy road conserved at the basis of
the mire (Fig. 5). Like Pr 31, the construction dates
4 Metzler 1993; 2003; Bauerochse/Metzler2001; cf. Heu-
muller et al., this volume.
to the early Neolithic. Radiocarbon data spanning the
periods 4220-4040 calBC (5170 ± 60 BP, Hv 25659),
4040-3930 calBC (5310 ± 50 BP, Hv 25660), and
4070-3760 calBC (5100 ± 60 BI> Ki 4619) classify
the construction (cf. Bauerochse/ Metzler 2001,
tab. 1; Bauerochse et al. 2012, 150).
Some metres east of Pr 31 and situated in the peat
about 50 cm above, two more trackways, Pr 34 and
Pr 35, were preserved. From its technical features, Pr 34
was similar to trackway Pr 31: a wooden construc-
tion made of a lengthwise substructure covered by a
superstructure made of pine stems laying laterally. For
stabilisation stems were put longitudinally at the edges
of the superstructure, fixed by oak dowels stuck in the
ground (Fig. 6; Bauerochse/Metzler2001; Metzler
2003). All dendrochronological data - all coming from
the dowels - show the same felling year: 3798 BC.
Next to Pr 34 the remains of Pr 35 were pre-
served; a few planks and two rows of oak piles stuck
in the peat in a distance of about 50 cm presumably
formed a narrow footbridge or landing stage (Fig. 6).
Dendrochronological data from the oak piles date its
construction to 3701 BC (cf. Bauerochse et al. 2012;
Achterberg et al. 2015). Pollen of floating leaf plants
like pondweed (Potamogeton), pond lily (Nuphar),
and water lily (Nyphaea) document the temporary
expansion of the lake from the beginning of the 4th mil-
lennium BC onwards (cf. Fig. 2; Bauerochse/Metz-
ler 2001). Pollen samples taken from a core some
200 m north of the excavation site demonstrate the
existence of a lake in the immediate vicinity already
since the Atlantic period. Probably it was this lake
that expanded as a consequence of a rising ground
water level and flooded the area.
Drier conditions during the second half of the 4th
millennium BC caused the lake to disappear before, at
the transition to the 3rd millennium, pines germinated
and formed a bog forest (Figs. 2; 8). Buried pines, ex-
cavated when cutting peat, demonstrate this process,
which started about 3050 BC.
From about 2930 BC a change in growth patterns
(depressions of the annual growth rings) again displays
a change in site conditions. According to the dendro-
datings trackway Pr 32 was built in 2909 BC and was
maintained subsequently over a period of about 20
years (Fig. 7). For these years distinct growth depres-
sions (c. 2885-2860 BC), followed by a period without
any evidence of tree growth (c. 2860-2850 BC), display
a period of wetter conditions (Fig. 8). Approximately at
the same time, emerging spores of peat mosses (Sphag-
num) indicate initial raised bog growth (Fig. 2).
Only a few years later, in the middle of the 28th
century BC, conditions became drier again, and from
Neolithic colonisation of the southwestern Dummer basin (NW Germany) - evidence from palaeobotanical data
samples from trees with different morphology. Trees
with a diameter of less then 20 cm and stumps were
not sampled. All samples were cut with a chain saw.
The preparation of the samples followed standard
procedures (e.g. described by Leuschner 1994; for a
detailed description of the preparation see Leuschner
et al. 2007, 185-186). The tree ring series have been
cross-dated and the matches statistically evaluated by
calculating the coefficient of parallel variation and
/-values (Bailee/ Pilcher 1973).
Results
At the bottom of the diagram, the presence of pol-
len from pine (Pinus sylvestris) and alder (Alnus
glutinosa) presents a picture of a mosaic of wet de-
pressions and drier sites poor in nutrients, covered
by pines and species of the mixed oak forest (mainly
oaks). Increasing pollen of peatland species and the
decrease of the pine curve in the course of the lower
centimetres of the diagram show increasing wetness
and paludification (Fig. 2). Almost at the same time
when the first trackway, PR 31 (Fig. 3), was built,
pollen of herbs and emerging anthropogenic indica-
tors (after Behre 1981) mark an increasing human
impact in the area. Dendrochronological data from
the trackway timbers document its construction in
4629 BC at the latest, and following maintenance for
at least 100 years (Fig. 4; cf. Achterberg et al. 2015).
Partly built directly on the mineral ground, its
construction reflects the beginning of the paludifica-
tion, showing a number of features indicating soft
and muddy subsoil. A multilayered substructure and
a superstructure - up to about 5 m wide - partly fixed
by longitudinal stems put laterally across the construc-
tion and pierced with dowels, stabilised its position
(Fig. 3).4 The timbers were cut in four felling episodes,
starting at 4629 BC, 4614 BC, 4590 BC, and 4538 BC,
all of which coincided with times when the trees were
characterised by growth depressions (Fig. 4). However,
we have merely 36 timbers dated, out of which only six
were completely preserved to include the waney edge
(Fig. 4; Achterberg et al. 2015), and so we cannot be
sure whether our data cover the entire period during
which the trackway was used.
The remains of a further trackway, Pr 36, situated
about 100 m west of Pr 31, demonstrate the presence
of a second corduroy road conserved at the basis of
the mire (Fig. 5). Like Pr 31, the construction dates
4 Metzler 1993; 2003; Bauerochse/Metzler2001; cf. Heu-
muller et al., this volume.
to the early Neolithic. Radiocarbon data spanning the
periods 4220-4040 calBC (5170 ± 60 BP, Hv 25659),
4040-3930 calBC (5310 ± 50 BP, Hv 25660), and
4070-3760 calBC (5100 ± 60 BI> Ki 4619) classify
the construction (cf. Bauerochse/ Metzler 2001,
tab. 1; Bauerochse et al. 2012, 150).
Some metres east of Pr 31 and situated in the peat
about 50 cm above, two more trackways, Pr 34 and
Pr 35, were preserved. From its technical features, Pr 34
was similar to trackway Pr 31: a wooden construc-
tion made of a lengthwise substructure covered by a
superstructure made of pine stems laying laterally. For
stabilisation stems were put longitudinally at the edges
of the superstructure, fixed by oak dowels stuck in the
ground (Fig. 6; Bauerochse/Metzler2001; Metzler
2003). All dendrochronological data - all coming from
the dowels - show the same felling year: 3798 BC.
Next to Pr 34 the remains of Pr 35 were pre-
served; a few planks and two rows of oak piles stuck
in the peat in a distance of about 50 cm presumably
formed a narrow footbridge or landing stage (Fig. 6).
Dendrochronological data from the oak piles date its
construction to 3701 BC (cf. Bauerochse et al. 2012;
Achterberg et al. 2015). Pollen of floating leaf plants
like pondweed (Potamogeton), pond lily (Nuphar),
and water lily (Nyphaea) document the temporary
expansion of the lake from the beginning of the 4th mil-
lennium BC onwards (cf. Fig. 2; Bauerochse/Metz-
ler 2001). Pollen samples taken from a core some
200 m north of the excavation site demonstrate the
existence of a lake in the immediate vicinity already
since the Atlantic period. Probably it was this lake
that expanded as a consequence of a rising ground
water level and flooded the area.
Drier conditions during the second half of the 4th
millennium BC caused the lake to disappear before, at
the transition to the 3rd millennium, pines germinated
and formed a bog forest (Figs. 2; 8). Buried pines, ex-
cavated when cutting peat, demonstrate this process,
which started about 3050 BC.
From about 2930 BC a change in growth patterns
(depressions of the annual growth rings) again displays
a change in site conditions. According to the dendro-
datings trackway Pr 32 was built in 2909 BC and was
maintained subsequently over a period of about 20
years (Fig. 7). For these years distinct growth depres-
sions (c. 2885-2860 BC), followed by a period without
any evidence of tree growth (c. 2860-2850 BC), display
a period of wetter conditions (Fig. 8). Approximately at
the same time, emerging spores of peat mosses (Sphag-
num) indicate initial raised bog growth (Fig. 2).
Only a few years later, in the middle of the 28th
century BC, conditions became drier again, and from