NORWEGIAN JOURNAL OF GEOLOGY
MAS 14C-Doting of Glacigenic Sediments
59
AMS radiocarbon dating of glacigenic
sediments with low organic carbon content- an
important tool for reconstructing the history of
glacial variations in Norway
Lars Olsen, Klaas Van der Borg, Bjørn Bergstrøm, Harald Sveian,
Stein-Erik Lauritzen & Geir Hansen
Olsen, L., Van der Borg, K., Bergstrøm, B., Sveian, H., Lauritzen, S.-E. & Hansen, G.: AMS radiocarbon dating of glacigenic sediments with low orga­
nic carbon content- an important tool for reconstructing the history of glacial variations in Norway. Norsk Geologisk Tidsskrift, Vol.
Trondheim 200 l. ISSN
0029-196X.
In this paper we present and examine a comprehensive series of dates
(> 200), which underpins a
81, pp. 59-92.
new reconstruction of ice-sheet fluctuations
along nine transects extending from inland to the coast in Norway. Sediments with low organic content dominate the dated materials, particularly
from the inland sites, some of which may have a marine origin. Consequently, the new dates reported here, include mainly 14C-dates of bulk orga­
nic sediment samples. The geochronology of sites located in coastal areas is mainly based on shell dates. A considerable number
(> 100) of previ­
ously published dates are also employed, both as 'control dates' for the new synthesis, and as components of the overall geochronological data
base. The data base also includes I4C-dates of bones and calcareous concretions, U/Th-dates of speleothems and calcareous concretions, and
TL/OSL-dates of wind-blown and water-lain sand. Brief reference is also made to relative age estimates based on amino acid analyses and correla­
tion using magnetostratigraphy. The accuracy and precision of the chronology is
exarnined
on a millennium scale. The dates give ranges of ages
which provide a coherent chronology of tl!e stratigraphic succession and of the main events, which span the Middle to Late Weichselian interval.
Olsen, L. 1, Van der Borg, K. 2, Bergstrøm, B. 1, Sveian, H. 1, Lauritzen, S.-E. 3 & Hansen, G.4; l) Geological Survey ofNorway, N0-7491 Trondheim, 2)
University of Utrecht, R./. Van de Graaff laboratorium, P. O.Box 80.000, 3508 TA Utrecht, The Netherlands, 3) Geo/. Inst., University of Bergen, A/legt.
41, N0-5007 Bergen & 4) Surface Geochemical Services AS, P. O. Box 1257 Vika, N0-0111 Oslo, Norway.
Corresponding author: Lars Olsen (e-mail: [email protected])
Keywords: AMS-14 C analysis, geochronological methods, Quaternary stratigraphy, glacial variations, glacial curves
lntroduction
Previous studies of glacial oscillations in Norway have
focused on coastal and offshore areas, where the availa­
bility of fossiliferous marine sediments has made it pos­
sible to establish a fairly detailed chronology. A major
problem with inland areas is the limited number of
good-quality dates. As a result, most attempts to recon­
struct the history of Weichselian glacial variations prior
to the Late Glacial Maximum (LGM), with the ice
retreat further than to the Younger Dryas ice margin,
have been rather speculative and based on poorly-defi­
ned chronologies.
In this paper, we present new and review old
geochronological data on the Middle and Late Weichse­
lian Norwegian tills and sub-/inter-till deposits, inclu­
ding many radiocarbon dates of sediments with low
organic carbon content. We also examine the quality of
data derived by the various dating methods. The wider
regional implications of the data, including their
geochronological range and resolution, are assessed in a
separate section, with relevant palaeoenvironmental and
palaeoclimatic data added in Appendix B. Glacial his­
tory interpretations, with curves of glacier fluctuations
in onshore Norway during the Middle and Late Weichse­
lian based on the new data, are presented in an accompa­
nying paper (Olsen et al., this volume).
The aim of the present paper is to combine results
derived from various dating methods and traditional
stratigraphical methods to construct a detailed geochro­
nological framework for ice-sheet fluctuations in Nor­
way 1 5 to 40 ka BP. This is done on the basis of: (l) the
dating of deposits with low organic content using well­
established methods and (2) age estimates derived by a
range of methods as a means of assessing the reliability
of dates obtained by a single method, particularly the
AMS-14C dating of bulk organic sediment samples.
Sediment samples and stratigraphical data have been
gathered from many parts of the country, mainly along
nine transects extending from the inland area to the
coast (Fig. l), as part of the programme of stratigraphical
mapping of Quaternary deposits by the Geological Sur­
vey of Norway. We also include published data, particu­
larly from the areas covered by transects 3 and 8.
60
NORWEGIAN JOURNAL OF GEOLOGY
L. Olsen et al.
SW DEN
no.
2
3
4
5
6
7
on rna
Leirelva, Varanger Peninsula
Pa
Sk' llbekken, Pasvik
Ar
s
A
Gry
Hl
T
u
Bo
A
KJ
Gr
R
Lu
Komagelva, - " Leirhola/Lauksundet, Arnøy
Sar ejohka, Finnmarksvidda
Øvre Æråsvatn. Andøya
Storelva, Grytøya
Mågelva 11, Hlnnøya
Gaves in Kjøpsvik, Tysfjord
Urdalen
Bogneset, Melø y
Asmoen,- "
-
Kjelddal, - " Grytåga, Fauske
Fiskelauselva, Grane
Hattfjelldal
Si
Sitter, Nord-Flatanger
N
Tv
Namsen, Namdal
Langstrandbakken,\flkna
Ø. Tverråga, Lierne
B
Blåfellelva,-"-
Se
Reinåa*, Se lb u
Stærneset, - " -
Se
G
F
Between
K
8and9
Jæren
E
Hh
4
5
6
7
8
9
10
11
Luktvatnet, Vefsn
Ha
La
1
2
3
12
13
Risvasselva, - " -
Fi
Skj
9
no.
V
V
8
9, west
Slte name
Grytdal, B udal
Flora, Tydal
Skjonghelleren (cave), Møre
Hamnsundhelleren cave
Kollsete, Sogn og Fjordane
14
15
16
17
18
19
20
21
22
24
23
25
26
Elgane, Jæren
E ersund
27
H
Herlandsdalen
H
Rundhaugen
28
29
30
H
Sk
O
Ro
L
L
Fo
Fo
Passebekk
Skjeberg
31
32
33
Dokka
Rokoberget
Mesna, Lillehammer
Stampesletta, -
"
-
Gråbekken, Folldal
Folldal
34
35
36
Fig. l: Map showing location of sites (dots) for which 14C dates were obtained for this study. Also indicated are sites with comparable informa­
tion (open circles) reported in published or unpublished sources, the western margin of the Scandinavian ice sheet during the Weichselian
maximum (LGM) and the Younger Dryas (YD) stadia� transects for the glaciation profiles, positions of the major ice-stream channels on the
continental shelf, and specific sites (indicated by letters and closed circles with crosslines) referred to in the inset list of sites and in Appendix A.
NORWEGIAN jOURNAL OF GEOLOGY
The relative importance of the individual dating met­
hods in this compilation, in terms of the number of loca­
lities for which dates have been derived, is illustrated in
Figure 2. The frequency distribution indicates that the
geochronological interpretations are based mainly on
the AMS-14C dating of sediment samples, with a signifi­
cant amount of data obtained by the 14C-dating of shells
and other organic materials. Age estimates derived by
other methods are limited in number, but may be quali­
tatively important.
Published dates with finite 14C-ages, generally rejected
or suspected to be in error due to sample contamination,
are not included in the data base (Tables 2-5), except in a
few cases where new data are available to re-assess the
dates. For example: in Table 4, the Gråmobekken gyttja
sand, originally dated to c. 32 000- 37 000 14C-yr BP by
Thoresen & Bergersen (1983), with new data published
by Bergersen et al. (1991), Lauritzen (1991) and Olsen et
al. (1996); and the Gamlemsveten soll, earlier dated to c.
20 000 14C-yr BP by J. Mangerud (pers. comm. 1981),
with new data published by Nesje et al. (1988), Vorren et
al. (1988) and Møller et al. (1992).
Sediments facies and depositional
environments
Methods
Standard procedures for stratigraphical studies of till
and waterlain sediment have been followed in most
cases (see e.g. Olsen et al. 1996). In addition, in order to
detect Ce-deficiency in sediments, which is an indicator
of the marine depositional environment (Roaldset
1980), the content of La and Ce were determined using
X-ray fluorescence (XRF) and Inductively coupled
plasma spectroscopy (ICP). The analyses, performed on
the fractions < 2 J..Lm and < 63 J..Lm, were carried out at
the Geological Survey of Norway, Trondheim. The ICP
method is considered to reduce the risk of distortions
caused by the addition of "pre-Quaternary" elements
derived from the dissolution of rock fragments. Cen/Ce
- ratios have been calculated following the procedure
described by Roaldset (1980), where Cen represents the
normalized numerical values of Ce, i.e. the numerical
values of Ce achieved from XRF or ICP analysis correc­
ted relative to a scale where La is set to 100, and �
represents an average value of Cen calculated specifically
for each region studied.
Sediment facies and depositional environments
Reconstruction of ice-sheet fluctuations in Norway is
based on complex stratigraphic sequences which include
a variety of sediment facies originating from a range of
depositional environments. The most frequent and
qualitatively most important of these are illustrated in
NAS 1"C-Dating
of Glacigenic Sediments
61
Numberot
localities
30
25
20
15
10
shell
sed.
Olher
Fig.2: Frequency distribution of types of age estimates included in
this study. In most cases age estimates based on any t:Llting method
used are available for only one stratigraphical unit at each locality,
but AMS-14C dating of sediments are generally available for more
than one unit (at maximum, from six stratigraphical units at one
locality). For explanation of the abbreviations, see the main text.
Table l. Sediments deposited in proglacial environments
occur in a majority of the localities. The glaciolacustrine
sediment facies A and Bl are mainly represented by sub­
facies a) of laminated day, silt and sand, alternating with
sub-facies b) of massive day, silt or sand, whereas the
glaciofluvial sediment facies B2 indudes several sub­
facies of sand and gravd, respectively. These sediment
facies types (A, Bl, B2) are the most frequent facies in
our data base for the inland areas (Fig. 3). In coastal
areas the glaciomarine facies Dl and D2, as well as
marine facies G, are the most frequent sediment types.
Facies Dl and D2 are represented by massive, as well as
laminated day, silt and sand, and indude various
amounts of dropstones (pebbles, cobbles). Syngenetic
deformation may occur. Facies G is also represented by
massive and laminated day, silt and sand, but dropstones
are rare or not present.
Glaciomarine sediment facies Cl and C2, which are
similar to facies Dl and D2 in grain-size distribution and
structures and are recorded at high altitudes in inner
fjord valleys at some 20 localities, are qualitatively
important because they indicate both certain (C2) and
62
NORWEGIAN jOURNAl OF GEOLOGY
L. Olsen et al.
Table
l
Sediment facies
Proglacial;
A
B
Bl
B2
c
Cl
C2
D
Sedimentary environment
Dl
E
F
G
Ice-dammed lake; mainly
glaciolacustrine
laminated sand, silt & clay
Proglacial;
lee-lake; mainly laminated
glaciolacustrine
sand, silt & cl'!Y_
Proglacial;
Various kinds of deposits;
glaciofluvial
Proglacial;
mainlysand
Uplifted above lateglacial & Holo-
glaciomarine
cene marine limit; silt & clay,
Proglacial;
As Cl, but with marine
with clasts; no marine fossils
glaciomarine
Proglacial;
glaciomarine
02
Comments
Table 1: Sediment facies and
depositional environment infer­
red from the studied sections.
For examples of stratigraphic
successions, see Appendix A.
fossils (shells, dinofl�).
Lower than lateglacial & Holocene marine limit; silt & clay,
with clasts; no marine fossils
Proglacial;
As Dl, but with marine
glaciomarine
fossils (shells, dinotlag.).
Fluvial
Lacustrine
Marine
Mainly grave! & sand
Silt & fine sand
All sites are from onshore
areas and therefore uplifted
compared to the present
sea-leve!; silt & clay
H
Terrestrial organic env.
Gyttja, peat, etc.
I
Aeolian environment
Sand
J
Other subaerial conditions
Subaerial cave environment;
pedogenesis, etc.
probable (Cl) high contemporary relative sea-levels (see
next paragraph), in turn indicating substantial glacial
isostatic depression of the land.
High relative sea-levels
The occurrence of pre-Holocene marine sediments at
localities situated far landward and much higher than the
present sea-level have a high significance, especially those
which lie well above the lateglacial marine limit. Only
three such sequences containing marine macrofossils
(shells) and five with marine microfossils (foraminifera,
dinocysts, algae) have been found so far, though a num­
ber of other sequences may contain trace quantities of
preserved marine fossils. Residues of relict marine orga­
nisms were extracted to establish whether waterlain sedi­
ments that lack obvious marine fossils accumulated
under marine conditions, and the content of La and Ce
has also been measured. Additional parameters (e.g. C/N­
ratios, Cl, Br) also used to detect a possible marine influ­
ence will be discussed in a later report (Olsen, in prep.).
Ce-deficiency in marine sediments
The Ce-deficiency of confirmed and inferred marine
organic-bearing sediments is clearly indicated in Fig. 4,
where the Ce/Ce - ratio is plotted against ()13C for
marine and terrestrial sediments. All 26 samples of the
confirmed and the inferred marine sediments show
Ce/Ce values lower than 1 .0, whereas most of the terres­
trial sediments have values higher than 1 .0 (Fig. 4, and
Olsen et al., this volume). However, an overlap in values
is expected due to probable variation in the content of
material of marine versus terrestrial origin, and variation
in the concentration and distribution of heavy minerals
with lanthanides in the sediments. Plots of the majority
of the samples for which a marine origin is inferred are
in the same area as the fossil-bearing sediments of con­
firmed marine origin (Fig. 4), and we take this to indi­
cate that Ce-deficiency, in combination with ()13C, is
generally a fairly good indicator of marine sediments
from mixed assemblages of materials.
Geochronological methods
The crucial requirement for the success of this project,
which is reported here and in the companion paper
(Olsen et al., this volume), was to find a dating method
suitable for testing the timing of individual glacial or
interstadial events. Repeated glacial advances lead to the
removal of older surficial material, and discontinuous
sedimentary records. A method was therefore needed to
provide age estimates for basal parts of lodgement tills,
and for any underlying glaciolacustrine and glaciofluvial
sediments, and which typically have low organic content.
AMS '"C-Dating
NORWEGIAN JOURNAl OF GEOLOGY
We have assumed that what is eroded from one place is
quickly redeposited at another, and that erosion nor­
mally proceeds from the top of each sedimentary unit.
Because there was very little likelihood of finding macro­
fossils spanning the time range 15-40 ka BP at most of
localities, especially in inland areas, we have focused on
14C-dating of sediment samples where major organic
components are assumed to originate from contempo­
rary living organisms (plants, animals, e.g. hird drop­
pings), and contemporary soil, including recycled older
soil components. The policy adopted was to date a suffi­
cient number of samples from each lithological unit.
Thus potential age distortions due to resedimentation of
organic C from older strata would be minimized. The
aim was to demonstrate consistency of data in order to
overcome the general scepticism felt towards bulk sedi­
ment dating compared with macrofossil dating (e.g.
Tornqvist et al. 1992, Heimens et al. 1996). Dates of bulk
sediment samples obtained from proglacial units associ­
ated with an advancing glacier, represent the most
important input data in our glacial reconstructions.
These are considered likely to give the most accurate ages
of sediment deposition and of the associated phase of ice
Sedimentary
facies
4
8
Number of localities
12
16
20
24
28
A
81
82
C1
C2
01
02
E
F
G
H
Considered
ærtain
Possible
J
Fig. 3: Frequency distribution of the most frequently occurring sedi­
ment facies represented in the sub-till sediments in our study. Most of
the sediment facies (A, Bl, C, D, F & G) are dominated by clay, silt
and fine sand, and most of these are inferred to represent proglacial
environments (A-D). For description of sedimentary environment,
see Table l.
of Glac igenic Sediments
63
Ce - 'contenr and S 13C of 47 sediment samples:
(XRF,
ICP)
Ce/Ce
1.5
1.0
.QPossible marine, bul
• wilh no recorded marine fossils
* wilh marine lossils (shells, dinoflag)
·=�) only terrestrial input
�
��� - - -��:A ��- -
� ------���
---------
�
• •
--
�-
.
��#
.
0.5
-110
-115
-do
S13C rei. to PDB
-2�
Fig. 4: Ce 'content' (expressed as Cenf{& ratio) and o13C of 47 selec­
ted sediment samples. See the main text for description of calculation
procedure for Cen!S:&. The assignments marine, possible marine and
terrestrial sediments follow the criteria given in the figure caption to
Fig. 5. Note that all the samples with a certain or inferred significant
input of marine sediments have a Cenfs;& ratio of c. 1.0 or less, which
indicate sediments depleted in Ce.
.
advance. Corresponding dates from sediments laid down
by a retreating glacier would tend to be slightly too old,
and in some cases could reflect the age of the preceding
ice advance or interstadial since the sediments are likely
to contain recycled organic carbon (e.g. Sutherland
1980). However, even in these cases, only a very small
component of carbon derived from contemporary living
organisms would be needed to bring the calculated age
dose to the real age of the sediment deposition (e.g. Ols­
son 1974, Olsson & Possnert 1992). Ice-retreat contexts
therefore provide the second-most important set of age
estimates used to reconstruct the regional glacial history.
Further constraints on dating accuracy are provided
by 'control'-dating of separate organic fractions of some
samples, by correlation and 14C-dating using other
materials, such as shells, plant macrofossils, bones and
calacareous concretions, as well as other dating methods
(TL, OSL, U/Th, amino acid analyses, palaeomagnetic
measurements). Evaluation of dating precision is based
on tests of reproducability (replicates).
AMS radiocarbon dating of bulk sediment
som ples
Field-sampling focused on homogeneous fine-grained
sediment units (clay - clayey silt) of sediment facies A,
Bl, Cl, C2, Dl, D2 and G (p. 5) with no visible traces of
oxidation, root penetration, or fissures favouring the cir­
culation of particulate matter through water seepage.
Dark grey to bluish grey unoxidized sediments were
sampled in an attempt to reduce the likelihood of secon­
dary input of dissolved and (especially) particulate mat­
ter. Contamination from bacteria growth (e.g. Wohlfarth
64
NORWEGIAN JOURNAL OF GEOLOGY
l. Olsen et al.
Table 2
Locality
Transect
no.
Komagelva
Komagelva
Komagelva
Komagelva
l
(conta. l
Leirelva
(conta.)1
(conta.)l
l
(conta.)l
Leirelva
Leire!va
Leirelva
l
Leirelva
l
l
Leirelva
(conta.)l
Skjellbekken
Skjellbekken
Kroktåa
Mågelva
Urdalen
Urdalen
Meløy
Kjelddal I
Kjelddal Il
Grytåga
Okshola
Okshola
Sjønstå
Risvasselva
Luktvatnet
Luktvatn et
Luktvatnet
Grane,N.
Grane,F.
Grane,F.
Grane,F.
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Hattfjelldal
Slettåsen
Slettåsen
Røssvatnet
Røssvatnet
Langstr.bak.
Øyvatnet
Øyvatnet
Øyvatnet
Gartland
Gartland
Gartland
Namsen
Namsen
Namsen
Namsen
Domåsen
Domåsen
Namskogan
Rognbuelva
Ø. Tverråga
Nordli
Blåfjellelva I
Blåfjellelva Il
Blåfjellelva
Blåfjellelva
Blåfjellelva
Blåfjellelva
Il
Il
Il
Il
Blåfjellelva Il
l
l
3
3
3
3
4
4
4
4
(subgl.)4
(subgl.)4
4
4
(conta.) 5
5
(conta.) 5
5
5
5
5
5
5
5
5
5
5
(conta.)5
5
(conta.) 5
5
(conta.)5
5
(conta.) 5
(conta.)5
5
5
5
6
6
6
(conta.)6
6
6
(conta.) 6
(conta.) 6
6
6
6
(conta.)6
(conta.)6
6
(conta.)6
6
6
6
(conta.)6
(conta.)6
(conta.)6
(conta.)6
(conta.)6
(conta.) 6
Field no.
501 -89
501 -89
5 1 9-89
5 1 9-89
507-89
507-89
5 1 2-89
5 12-89
5 1 3-89
5 1 3-89
16-94
1 8-94
7.-98
1-8-98
20.-98
2 1 .-98
14.-98
16.-98
18.-98
9.-96
94-0060
94-0058
23.-96
10.-96
5.-95
5.-95
5.-95
94-0030
1 .-040991
3.-040991
94-003 1
1 . -28069 1
2.-28069 1
3.-28069 1
10.-95
1 1 .-95
10.-95
10.-95
1 1 .-95
1 1 .-95
1 3.-95
13.-95
14.-95
14.-95
12.-95
1 2.-95
94-0020
94- 002 3
1 .-97
8.-95
8.-95
8.-95
9.-95
9.-95
9.-95
20.-95
1 5.-95
16.-95
17.-95
5.-97
6.-97
53-94
10.-97
3.6.-90
2.-90
2.-95
2.-95
3.-95
2.-95
3.-95
3.-95
Lab.no.
UtC 1 795
UtC 1 796
UtC 3458
UtC 3459
UtC 1 797
UtC 1 798
UtC 1 799
UtC 1 800
UtC 3460
UtC 346 1
UtC 4039
UtC 4040
ute 7394
UtC 7456
UtC 8458
UtC 8459
UtC 8456
UtC 8457
UtC 8 3 1 3
UtC 5557
UtC 3470
UtC 3457
UtC 5467
UtC 5558
UtC 4868
UtC 4715
UtC 4796
UtC 3467
UtC 22 1 5
UtC 22 1 6
UtC 3466
UtC 22 12
UtC 22 1 3
UtC 22 14
UtC 4720
UtC 472 1
UtC 4802
UtC 4803
UtC 4804
UtC 4805
UtC 4807
UtC 4808
UtC 4809
UtC 48 10
UtC 4806
UtC 4722
UtC 3468
UtC3469
UtC5974
UtC 4800
UtC 4 7 1 8
UtC 4870
UtC 4871
UtC4719
UtC 480 1
UtC 4725
UtC48 1 1
UtC 48 1 2
UtC 48 1 3
UtC 5975
UtC 5976
UtC 3465
UtC 5986
UtC 3464
UtC 1380
UtC 3463
UtC 47 1 1
UtC 4712
UtC 47 1 3
UtC 4793
UtC 4794
UtC 4866
Fraction
Weight
INS
SOL
INS
SOL
INS
SOL
!NS
SOL
SOL
!NS
LOI
TC
1 .40%
1 .40%
1 .86%
0 . 1 0%
0 . 1 0%
2 . 1 0%
2 . 1 0%
4. 1 0%
4. 10%
3.61 o/o
0.22%
0.22%
0.20%
0.20%
TOC
!NS
!NS
!NS
!NS
!NS
!NS
!NS
!NS
!NS
!NS
INS
INS
C 03
INS
SOL
!NS
DCM
INS
INS
INS
INS
INS
INS
INS
lNS
INS
SOL
DCM
SOL
DCM
!NS
DCM
INS
DCM
DCM
INS
INS
INS
INS
Hexane
INS
SOL
SOL
INS
DCM
C 03
Hexane
INS
INS
INS
INS
INS
INS
INS
INS
INS
SOL
INS
INS
DCM
DCM
SOL
1 .00 mg
0.34mg
0.68mg
0.53mg
0.53 mg
0.33 mg
1 .57mg
1 .88 o/o
0.23mg
1 .26mg
0.8 1 mg
2.26%
l . l 5%
1 .08 o/o
1 .44 o/o
1 .02 o/o
0.23%
0.07%
0.34 o/o
0. 14%
1 .23 o/o
1 .35 o/o
1 .65 o/o
2.40mg
2.02mg
1 .06mg
0.77 mg
1 .52mg
1 .30mg
2.40mg
1 .44mg
2. 1 7mg
0.55 mg
1 .23 mg
2.3 1 mg
0 . 1 0%
0.08 o/o
0.50 o/o
1 .40 o/o
1 .03 o/o
0 . 1 3 o/o
1 .04 o/o
0 . 1 0%
1 .72 o/o
1 .75mg
1.31 mg
0. 1 1 mg
0. 1 8mg
2.32mg
0.95mg
2.32 mg
2.03 mg
1.33mg
1 .36mg
0.20 o/o
o/o
o/o
o/o
o/o
0.63 o/o
0.05
0.20
0.90
0. 1 5
4.01 o/o
0.09 o/o
0.87 o/o
0.85 o/o
0.04 o/o
0.04 o/o
d13C
16 420
1 5 370
14 380
8 660
15 0 1 0
10 550
17 290
1 7 1 10
18 680
14 570
34 000
25 860
13 950
1 3 890
20 470
27 580
17 700
18 880
24 858
35 400
1 1 580
1 1 790
9 470
36 800
14 690
30 600
5 477
26 400
28 000
19 500
29 400
27 300
30 500
25 700
28 060
25 370
25 980
13 370
25 780
1 1 310
26 720
1 1 740
23 500
6 472
5 376
34 900
3 1 000
1 90
140
140
120
160
1 00
1 70
160
1 70
1 10
600
280
90
140
1 10
220
80
100
161
500
90
1 00
50
600
1 30
300
47
400
500
200
500
600
600
600
220
1 70
240
1 00
240
70
280
70
240
48
41
400
500
190
140
140
120
160
100
1 70
160
1 70
1 10
600
280
90
140
1 10
220
80
100
161
500
90
1 00
50
600
130
300
47
400
500
200
500
600
700
600
220
1 70
240
100
240
70
280
70
240
48
41
400
500
-18.0
29700
500
500
*
18 700
19 340
2 2 330
10 790
1 6 250
28 000
6 460
8 141
1 6 1 10
18 580
18 020
14 7 1 0
1 4 120
28 700
10 220
17 830
41 000
2 2 220
8 1 80
14 1 80
1 3 090
4 612
5 880
8 260
500
500
150
150
140
190
200
50
60
120
140
1 70
1 70
220
400
130
190
2000
240
110
90
80
41
50
1 10
-27.6
-2 1 . 1
-24.6
-29.5
-23.3
-29.5
-8.9
-29.9
-21. 3
-2 1 .9
•
0.72 o/o
2.50 o/o
1 .66 o/o
0. 1 6mg
1 . 1 8mg
1 .93mg
0.80mg
0.90mg
0. 12mg
0.58 o/o
1 .40 o/o
0.03 o/o
0.02 o/o
0.40%
+l· 1sd
-27.8
-27.3
-25.4
-25.7
-26.6
-25.9
-25.7
-23.5
-24.2
-24.5
-29. 1
-26.3
-20
-20.4
-28.4
-25.9
-25.4
-24.8
-24.5
-6.1
- 1 1 .5
- 1 6.6
- 14.3
-21
-25.7
- 1 6. 1
-29.2
-20.1
-2 1 .35
-20.98
-20.3
-23.02
- 1 9.42
- 1 9. 18
-24.5
-22.8
-25
- 3 1 .9
-27.2
- 3 1 .4
-22.6
-31
- 1 8.2
- 3 1 .4
-30.1
- 1 0.6
- 1 9.5
*
0.03 o/o
C14-yrs.
- 1 9.2
•
-23.5
-25.0
-23 . 1
-27.4
- 1 9.2
- 1 9.5
-30. 1
-29.2
-27.8
ISO
1 50
140
1 90
200
50
60
120
140
1 70
1 70
220
400
1 30
1 90
3000
240
1 10
90
80
41
50
1 10
ANIS "C-Oating
NORWEGIAN JOURNAL OF GEOLOGY
Locality
Thmsect
no.
Blåfjellelva II
6
Blåfjellelva II
Humm., Sve.
Sitter
Sitter
Sitter
Sitter
Myrvang
Myrvang
Myrvang
Reinåa
Rein åa
Rein åa
Rein åa
Reinåa
Rein åa
Stærneset
Stærneset
Flora
Flora
Flora
Flora
Flora
Flora
Flora
Flora
Flora
Flora
Flora
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Grytdal
Kollsete, S/F
Skjeberg
Skjeberg
Herlandsdal.
Herlandsdal.
Herlandsdal.
Passebekk
Passebekk
Passebekk
Rokoberget
Rokoberget
Dokka, K.
Dokka, K.
Mesna, Lh.
Mesna, Lh.
Mesna, Lh.
Stampesletta
Stampesletta
Gråbekken
Folldal
Folldal
Folldal
Folldal
6
Field no.
9
1 7.-96
1 8.-96
1 . -92
7.-95
7.-95
29-9 1
7.-95
6.-95
6.-95
6.-95
1 . -96
2.-96
3.-96
4.-96
5.-96
6.-96
7.-96
8.-96
8.-97
16.-97
1 9.-97
20.-97
2 1.-97
22.-97
23.-97
24.-97
25.-97
26.-97
27.-97
4.-95
4.-95
4.-95
1 1 .-96
12.-96
13.-96
14.-96
1 5.-96
16.-96
2.-97
3.-97
4.-97
18.-97
2.-87
2.-87
9
2-10/9-94
9
3-10/ 9-9 4
14.-97
1 1.-97
12.-97
13.-97
Lab.no.
19 7 1 0
l iO
l iO
20 040
1 00
1 00
22 070
2 1 1 50
12 480
30 200
5 010
1 6 770
14 350
5 770
28 700
1 6 850
19 880
3 1 600
29 280
30 900
18 820
25 240
17 800
15 920
17 800
13 420
16 700
15 620
14 7 1 0
1 9 600
1 9 050
18 000
14 5 1 0
38 500
12 860
7 670
39 500
37 200
4 1 800
23 700
25 300
28 400
lO 560
13 5 1 0
1 8 970
22 490
19 480
1 6 770
32 000
28 300
23 250
28 600
2 1 000
1 0 600
47 000
33 800
18 900
26 800
36 1 00
1 70
1 30
70
400
90
1 90
90
50
300
90
1 60
400
260
300
li O
1 80
400
260
400
200
220
200
200
280
1 20
400
90
700
200
50
800
600
1 000
200
260
300
80
80
I SO
1 80
200
1 90
300
240
1 70
300
400
240
1 70
130
70
400
90
190
90
50
300
90
1 60
400
260
300
li O
1 80
400
260
400
200
220
200
200
280
120
400
90
700
200
50
800
600
l i OO
200
260
300
80
80
I SO
180
200
4000
3000
800
200
400
700
200
400
1.-270991
UtC2217
7.-97
7a. - 9 1
UtC 604 1
TUa••
UtC 1965
UtC 4723
UtC 4724
UtC 4709
UtC 4710
UtC 4792
(conta.) 9
(subgl.) 9
9.-270991
1.-290991
9
7.-270991
9
1 8.-95
19.-95
1.-95
1.-95
1.-95
9
9
9
(conta.) 9
+1- Isd
-2 1 . 1
4.-2 70991
1.-210391
Cl4-yrs.
-21.4
-29.1
-23.7
-26.4
-28.3
-29.6
-24.6
-24.9
-28.8
- 1 8.2
- 1 7.5
- 1 7.4
- 16. 1
-15.1
- 16 . 1
- 1 5.6
- ! I. l
9
(conta.) 9
9
9
9
dl3C
TOC
INS
INS
INS
SOL
INS
DCM
INS
SOL
DCM
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
SOL
DCM
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
SOL
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
INS
SOL
INS
C 03
C 03
INS
SOL
DCM
4.-89
9
9
TC
INS
9
9
Wl
UtC 5566
9
9
Weight
65
UtC 5565
UtC 4814
UtC 47 1 7
UtC 4799
UtC 2 103
UtC 4869
UtC 4716
UtC 4797
UtC 4798
UtC 5549
UtC 5550
UtC SSSI
UtC 5552
UtC 5553
UtC 5554
UtC SSSS
UtC 5556
UtC 5977
UtC 5978
UtC 5979
UtC 5980
UtC5981
UtC 5982
UtC 5983
UtC 5984
UtC 6042
UtC 5985
UtC 6043
UtC 4714
UtC 4867
UtC 4795
UtC 5559
UtC 5560
UtC 5561
UtC 5562
UtC 5563
UtC 5564
UtC 6038
UtC 6039
UtC 6040
UtC 6046
UtC 1801
UtC 1 802
UtC 4728
UtC 4729
UtC 6045
UtC 6044
UtC 5987
UtC 5988
UtC 1962
UtC 1 963
UtC 22 1 8
UtC 3462
UtC 1964
Sweden; 6
7
(conta.) 7
7
(conta.) 7
7
(conta.) 7
(conta.) 7
7
7
7
7
7
7
7
7
7
7
7
(conta.) 7
7
7
(conta.) 7
7
7
7
(conta.) 7
7
(conta.) 7
(conta.) 7
7
7
7
7
7
7
(conta.) 7
(conta.) 7
7
8
Fraction
of Glacigenic Sediments
2.22 mg
2.0 1 mg
0.67 mg
0.08%
0.07%
0.70%
0.60%
0.70%
0. 1 8 mg
1 .06 mg
0.84 mg
1.33 mg
0.05%
1 .30%
1.13%
1.58%
0.90%
0.82%
0.70 o/o
0.44 o/o
0.75 o/o
0.77%
*
•
•
•
•
•
•
•
•
2.26 mg
O. !O mg
1 .28 mg
0.89 o/o
0.89%
0.03 o/o
0.66 o/o
0.66 o/o
0.70 o/o
0.62 o/o
0.98%
0.02 o/o
0.04 o/o
*
•
- 1 9.9
-26.2
-29.8
- 1 9.4
- 19.2
-20
-20.8
-20.4
-20.5
•
•
-23.8
•
2.20%
2.20 o/o
2.33 mg
2.38 mg
0.42 o/o
0.43 o/o
0. 1 6%
0.01 o/o
0.0 1 o/o
5.20
2.70
1 .07
1 .20
o/o
o/o
o/o
o/o
1.60 o/o
0.20 o/o
1.60%
0.45%
1 .20%
2.31 mg
2.28 mg
1 .26 mg
0.75 mg
1.0 1 mg
0.20%
0.07%
5.60 o/o
5.40%
0.28%
0.25%
0.22%
1.06%
0.23 o/o
0.22%
1.80%
-29.6
-28.7
-28.4
-28.4
-29.3
-29.4
•
•
-30.4
-29.6
-29.75
-30.2
-25.4
-2 4. 95
-27.5
•
-26.9
-20.7
-20.7
-22.2
-26.2
-30.3
c.
190
300
240
1 70
300
400
240
900
800
31500
700
700
16 030
100
1 00
••
16 000
32 300
4 1 300
36 300
26 260
23 260
7 960
••
500
500
900
1000
500
600
220
220
160
160
60
60
d13C: ratio 1 3C / 1 2C in per mil with respect to PDB-reference.
•
: Estimated d l 3C-value.
••
: Numbers not available; preliminary report (S. Gulliksen, pers. comm. 1995) .
Table 2: AMS-14C dates of sediments (in situ or redeposited in till) organized with resped to location and transed (listed from north to south);
for transed number and position, see Fig. l. The list includes 136 dates; 4 of these are of calcareous concretions. 'Weight'= weight of graphite
used for measurements. The abbreviation 'conta.' indicates contamination by young carbon, and 'subgl.' indicates subglacially deposited sedi­
ments. Neither of these two sets of dates is used in the data-base for the glaciation profile constructions (Olsen et al., this volume).).
66
L.
Olsen et al.
NORWEGIAN JOURNAL OF GEOLOGY
et al. 1998) was prevented by storing the air-dried sam­
ples in a cold room with a temperature of 0-4 °C.
Some 136 dates were measured at the Accelerator
Mass Spectrometry (AMS) facility at the University of
Utrecht (Table 2), which uses a 6 MV Van de Graaff tan­
dem accelerator (Van der Borg et al. 1997). Five fractions
of the sediments- which had a low (0.1-6 o/o TOC) orga­
nic content - were dated. The different fractions (and
numbers) were (l) the insoluble residual fraction (INS;
99), (2) the NaOH-soluble fraction (SOL; 18), (3) the
dichlormethane-extracted fraction (DCM; 13) and (4)
the hexane-extracted fraction (Hexane; 2), and (5) the
C03-fraction of calcareous concretions (C03 ; 4). Grap­
hite targets were used for the AMS analysis in all cases.
Possible fractionation effects, which may occur in
samples containing less than 0.3 mg carbon were correc­
ted for, and additional uncertainty introduced by this
procedure was taken into account in calculating of the
final error range (Alderliesten et al. 1998). We have con­
fidence in the results, except for the very small samples
for which it is difficult to assess the relative importance
of contamination. However, as discussed below, the
amount of carbon (mg C) used for measurements seems
to be more critical for the effect of contamination (parti­
cularly by young carbon) than the carbon content in the
sediment and the overall sample size.
Sample preparation
INS and SOL fractions
A standard alkali-acid-alkali treatment was used to
remove contamination by humic acids and carbonate.
The INS fraction, which may contain a persistent small
portion of humics, is the residue that is retained after
standard alkali-acid-alkali treatment, whereas the SOL
813C of 117 sediment samples:
No.
• Matine<><ganic ......
O Poeslblemorlneoog.lnjd
I?J Terrestrlal material
liD�="*
El co fraction
�§_: SubgiacMtJ depoeltion
•.
·5
Fig.S: Frequency distribution oflJ13C values obtained from all sam­
ples with availablelJ13C data in the data-base. The assignments l)
marine, 2) possible marine and 3) terrestrial sediments are based on
l) occurrence of marine fossils, 2) waterlain sediments and lack of
evidence of damming conditions (ice or bedrock/sediment thres­
holds) and 3) all other cases.
fraction is that remaining after the final alkali extraction.
After combustion of the organic carbon samples, the
obtained C02 gas was routinely separated from S02 with
KMn04• For details of the method, see van der Borg et
al. (1997) and Alderliesten et al. (1998).
DCM and hexane fractions
The DCM and hexane extractions were carried out at Geo­
lab Nor AS, Trondheim. The sediment was air-dried, in an
effort to minimize the loss of volatile compounds, and dis­
solved for 3 hours at 90 °C in dichlormethane (DCM), or
alternatively using hexane as a solvent (SOXTEC extrac­
tion system). Activated copper was used to remove eie­
mental sulphur from the solution. The extract was then
rotavapored using a centrifugal machine and air-dried.
Gas chromatography analysis (GCA)
Hydrocarbons from six selected DCM-extracted fractions
were identified by GCA using a Dani 8500 GC. This has a
10 m WCOT fused silica column of 0.27 mm internal
diameter and 1.20 !liD fllm thickness (Chromopack
Inc.). The temperature settings of the column were 50 °C
as initial temperature, and 10 °C/min as heating rate up
to 310 °C, which was kept during 15 minutes. The detec­
tors were standard FIDs. External standards were used
for calibration, and an internal standard was used for the
quantification.
Generally, the samples had equal composition, but
they showed a different distribution of components
(Hansen 1996):
a) Saturated hydrocarbons, mainly (C14-C32) n-alkanes
were present in small amounts. Some unsaturated
hydrocarbons were occasionally detected.
b) Aromatic hydrocarbons (3-rings) were found in rela­
tively large amounts.
c) Variable amounts of polyaromatic hydrocarbons
were detected, though these were generally in large
amounts.
d) The unresolved complex mixture (UMC - heavy and
often strongly polar compounds of sulphur, nitrogen
and oxygen) varied markedly in importance between
the samples.
The DCM -extractable organic material in the samples
turned out to be mainly of terrestrial origin. All the com­
pounds recorded are typical of higher plants, pollen,
spores, algae, etc.
The hexane-extracted fractions
Based on comparisons with many sediment samples of
sea-bed origin, the hexane-extracted fractions are
thought to contain organic components derived mainly
from marine environments.
Af./o..S '"C-Oat ing of Glacigenic Sed iments
NORWEGIAN jOURNAL OF GEOLOGY
'l
o
•
D
�
Terrestrial material
O
C03
Marine organic input
Possible marine organic input
(]]]
rn
•
•
1
�
Subgladal deposition
a
h lon
a
•
C03 - bearing bedrock
•
•
n
1
�
•
•
•
q
�
. . .
,n
�
o
a
� ai
Hexane
ct on
�a i
. . . 1
�
•
R
Fl
,
�·
.•
� �
�
·
��,1�M-���-"·��·�·�·�·���· ��
'lr��
�.,··�
w�
i ��
- ��
·
· �
· �
· �
� ·��
· �
·· ·
o
�
�
�
�
�
�·
'Terrestrial'
67
organic samples of the INS fractions peak at -19 o/oo, but
record a wide range of ol3C-values. Whereas most marine
organic samples have ol3C-values distinct from those of
terrestrial samples, marine plankton from cold waters
with an abundant supply of C02, and some marine fatty
acids and lipids, can record ol3C-values dose to those
typical of terrestrial samples- i.e. -26 to -29 o/oo (e.g. Druf­
fel et al. 1986). Some marine algae are probably also com­
monly depleted in oBC, as shown for example from stu­
dies on algal silt from Andøya, northern Norway (Vorren
et al. 1988). This is in accord with the ol3C-values of the
two samples of the hexane fraction, which supposedly
contain mainly marine organic components.
Protocol and screening of accurate dates
613C rei. lo PDB
Fig.�: Frequency distribution offPC values obtained from different
organic fractions of samples obtained from different materials.
co3- fraction of calcareous concretions
Carbondioxyde was extracted from calcareous concreti­
ons (2.9 - 5.6% carbon) and used for analysis (Table 2).
The dating protocol employed in this study has several
steps in which questionable dates can be identified and
eliminated. The low organic content typical of the bulk
sediment samples requires special consideration. Most of
the samples record loss-on-ignition values (WI) of 5.2%
or less, total carbon content (TC) of 5.6 % or less, and
total organic carbon values (TOC) of 1.8 % or less. The
distribution and range of organic content measures in the
majority of the samples is indicated in Fig. 7, which shows
(l) all LOI, TC and TOC data, (2) TOC only, after removal
of all samples which show distinct traces of groundwater
oxidation, and (3) TOC only, where samples with < O.l %
No.
The 813C-analysis
The range of f,l3C-values (relative to PDB) of bulk orga­
nic sediment samples obtained from 'marine' sediments
are typically -15 to -22 o/oo, whereas those from 'terres­
trial' samples are -20 to -32 o/oo (Fig. 5). This accords with
the majority of other investigations (e.g. Brown 1986,
Chen & Pollack 1986, Druffel et al. 1986). In order to
assess the possibility of contamination by inert carbon
secreted from 'old' carbonates, the values of the samples
taken from areas with carbonate-rich bedrock are indi­
cated (Fig. 5). These values show a wide spread of o1 3C
values and do not, in general, indicate a significant con­
tamination from old carbonates since the carbonate
rocks in Norway have much more positive 813C values
ranging from -10 o/oo to+ 8.4 o/oo (Veizer & Hoefs 1976,
Trønnes & Sundvoll 1995, Melezhik et al. 1997, 1999).
The different o13C-distributions of the various sample
fractions (Fig. 6) could indicate the influence of different
source materials. The residual (INS) fractions of terrestrial
samples are characterized by the two maxima, i.e. one at
f,13C approx. -30 %o and another at 813C approx. -24
o/oo. The DCM fractions have values dose to approx. -30
o/oo, corresponding to the more negative of the two INS
maxima, whereas the SOL-fractions record a broader
f,13C-range, between the two INS maxima. The marine
=
=
No.
10
,.
3
No.
10
0.5
1.0
1.5
2.0
%TOC
2
0.5
10
1.0
1.5
% Total organic cartlon (TOC)
2.0
1
2
3
% Organic content (LOI. TC & TOC)
Fig. l: Frequency distribution of organic content in samples from the
dated sediments. l - Organic content from loss-on-ignition (LOI),
total carbon (TC) and total organic carbon (TOC); 2 & 3- TOC
after different steps of refinement in the screening and selection of
sediments to be dated and used in our geochronological data-base.
See the main text for further details.
L Olsen et al.
68
[il
D
No.
Contaminated by young C
l nnn l!L .
l.� JS
14
15
5
o
:
N�
N
2
o
No
�
i
5
o
o
:
E:l Considered to be insignificantly contaminated
Subglacial deposition
1
3
N
NORWEGIAN JOURNAL OF GEOLOGY
o
'
5
10
15
10
,
On
10
i
10
hl
15
10
,
15
20
20
i
20
. � t::l
15
i
15
20
i
20
25
!!a�
25
30
35
45
40
* SOL;
IIOiuble fnlcllon
i
30
i
35
i
40
i
45
* OCM;
' lerT8etrlal ' fradlon
i
25
i i. i li'.i••
30
35
40
i
• • •c
45
* Hexane;
•
i
25
i
30
•
i
25
i
30
ka BP ( 1 4 c - yr)
marine • fraction
i
35
i
40
i
45
co3 - Iraction
[calc. concrøtions]
, la
, la
i
35
40
45
Fig.B: AMS-14C dates ofdifferentfractions from the studied sediments.
organic content and showing weak traces of groundwater
oxidation have been omitted (8 dates). After sample scree­
ning, (Fig. 7:3), 25 o/o of the remaining data-sets still have
low organic content (O.l o/o organic carbon).
The major sources of possible old carbon contami­
nants are: l) graphite, 2) 'old' organic-bearing sediments,
and 3) dissolved carbonate from calcareous bedrock (e.g.
Fowler et al. 1 986). Based on XRD analysis of parallels to
50 of the dated samples, neither graphite nor coal were
detected in any of these at an approx. 3 o/o detection level;
and for the 6 samples where quartz also was absent, grap­
hite and coal were not detected at a O.l o/o detection level.
In addition, based on the microscopic and stereoscopic
examination of more than 100 samples from the dated
sediments during foraminifer, pollen and macro-plant
analysis, numerous plant remains but almost no graphite
or coal fragments were detected. Contamination by this
source is therefore considered to be insignificant (e.g.,
graphite and coal sum to less than 2 o/o of the bulk micro­
and macrofossil 'sediment' fraction). Dissolved carbonate
from calcareous bedrock is also thought to be of only
minor importance (see p. 1 1 ). However, the low TOC/TC­
ratios (0.2-0.3; Table 2) for the bulk sediment samples may,
in some cases, result from significant amounts of carbo­
nate C derived from dissolved C02 from the contempora­
neous atmosphere. In combination with carbon from a
small component of dissolved old carbonate and recycled
humic comple:xes, this may give an apparently 'old' age
(reservoir effect) of the groundwater (or lake water) and
the bulk organic fractions. The ages of terrestrial plant
remains, which are the main constituents of most of the
bulk organic sediments sampled in this study, are not
intluenced by such older carbon. Contamination by pri-
mary input of carbon from old organic-bearing sediments
(by redeposition) is more difficult to evaluate, though it
may have a significant effect on samples from same degla­
ciation sediments. On the other hand, the sampling and
storage procedures will have reduced the potential for con­
tamination befare, during and after sampling, by the secon­
dary input of carbon. For these reasons, the remaining
samples of low organic content have not been rejected, alt­
hough we acknowledge that the same absolute amount of
carbon contamination would affect these samples much
more than those with a higher organic carbon content (e.g.
Olsson 1973, 1974, 1986, Olsson & Possnert 1992).
A further screening resulted in the rejection of sam­
ples that were susceptible to the secondary input of par­
ticulate matter through water penetration or by other
means. Thus sandy sediments and other sediments sho­
wing even the faintest traces of oxidation were omitted,
which eliminated four of the dates.
The DCM and hexane-extracted fractions are suppa­
sed to consist mainly of terrestrial and marine organic
carbon components, respectively (Hansen 1 996). Only
two hexane fraction-measures are available (Fig. 8), and
neither of these can be easily rejected on general consi­
derations since the dated sediments in both cases are
only overlain by a single till, and this till is derived from
the last regional ice advance (after 16 ka BP; Olsen
1997a) . This is contrary to the DCM and SOL fractions
where all 1 3 of the DCM -fraction dates and most of the
1 8 SOL-fraction dates are rejected because of clear con­
tamination by young carbon. This conclusion is based
on the fact that all of these samples were taken from
No.
10
A
14C - AMS
l
15
20
25
31 dateo al mar1ne
moØuoc-ia
30
35
l
40
45 ka BP
Fig.9: All dates ofsediments and shells in our data-base (Dec. 1999) after
rejection ofsamples ofquestionable dating quality. See the main textfor a
description of the screening procedure ofdates accepted in our data-base.
AMS 14(-Doting of Glocigenic Sed iments
NORWEGIAN JOURNAL OF GEOLOGY
Table 3
Locality
Kroktåa, Hinnøya
Storelva, Grytøya
Mågelva, Hinnøya
Mågelva, Hinnøya
Mågelva, Hinnøya
Mågelva, Hinnøya
Meløya, Meløy
Skavika,
aret
Stamnes,
øya
Bogneset I, Aniøya
Bogneset l, Åmøya
Bogneset l, Åmøya
Bogneset l, Åmøya
Bogneset l, Åmøya
Bogneset Il, Am øya
Storvika, Gildeskål
Skogreina, Meløy
Skogreina, Meløy
Skogreina, Meløy
Stigen, Meløy
Åsmoen, Ørnes
Åsmoen, Ørnes
Mosvollelva, Ørnes
Djupvika, Ørnes
Vargvika, Meløy
Gamrnalrnunnåga, M.
Ytresjøen, Meløy
Ytresjøen, Meløy
Vassdal ferry quay
Vassdal, Meløy
Holmåga, Meløy
Sandvika, Meløy
Neverdalsvatnet, Meløy
Nattmålsåga, Meløy
Fonndalen, Meløy
Aspåsen, Meløy
Oldra, Meløy
Oldra, Meløy
Oldra Il, Meløy
Kjelddal l, Meløy
Kjelddal Il, Meløy
Geitvågen, Bodø
Bestemorenga, Bodø
Osan, Soløyvatn., Bodø
Hestbakken, Bodø
Sandjorda, Bodø
Grytåga, Fauske
Grytåga, Fauske
Bringslimarka, Fauske
Røsvik, Sørfold
Røsvik, Sørfold
Røvika, Fauske
Gongskardet, Fauske
Holstad, Fauske
Finneid grave) pit
Seljåsen, Sørfold
Kinesmoen, Sørfold
Grønåsen, Fauske
Sjønstå, Fauske
�
Straumfors, Rana
Granmoen, Altemark
Øyjorda, Rana
Hundkjerka, Hommelstø
Hundkjerka, Hommelstø
Hundkjerka, Hommelstø
Langstrandbakken
Sitter, Flatanger
Myrvang, Trøndelag
Osen, Trøndelag
Osen, Trøndelag
Osen, Trøndelag
Reveggheia, Osen
Gjevika, Osen
Follafoss, Trøndelag
Follafoss, Trøndelag
Transect
Field no.
Lab. no.
3
3
3
3
3
3
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
4
6.-98
1 . -98
I-2-98
I-3-98
I-4-98
I-5-98
1 3 . -98
M6-92
MS-92
M4-92
2.-6/6-93
11-6/7-94
III-6/7-94
IV-6/7-94
1 . - 1 7/6-94
2.- 14/9-95
1 .- 5/6-93
3.-5/6-93
2.-5/6-93
1 9.-98
M7-92
05.06.93
08.07.94
M8-92
M3-92
M2-92
22.-98
23.-98
1 .-6/6-93
M I -92
1 1 .-98
12.-98
1 . - 7/7-94
1 . - 1 4/9-95
2 1 .-96
1 .-27/7-95
2.-30/9-93
1 .-20/7-95
3.-20/7-95
1 5.-98
1 7.-98
08.06.93
2 1 .08.94
24.-96
26.-96
27.-96
1 9.-96
20.-96
1 . - 1 7/8-93
1 . - 1 5/9-95
2.-1 5/9-95
1 .-24/9-93
1 . - 1 6/6-93
1 . - 1 7/6-93
1 . - 1 0/9-94
1 . - 1 2/9-94
22.-96
1 .-25/8-93
1 . - l l /9-94
UtC 7350
UtC 7345
UtC 7346
UtC 7347
UtC 7348
UtC 7349
UtC 8310
T- 10798
T- 10541
T- 10540
TUa-947
TUa- 1 239
TUa- 1 240
TUa- 1241
T- I I 784
UtC 4727
TUa-743
TUa-946
TUa- 1 092
UtC 83 14
TUa-567
TUa-744
TUa- 1094
T- 10543
T- 10797
T- 10539
UtC 83 1 5
UtC 83 16
TUa-944
T- 10796
UtC 8308
UtC 8309
T- I I 785
T- 12567
UtC 5465
TUa- 1 386
TUa-745
TUa- 1385
TUa- 1387
UtC 83 1 1
UtC 83 12
TUa-945
TUa- 1095
UtC 5468
UtC 541 2
UtC 54 13
UtC 5463
UtC 5464
T- I I404
T- 12565
T- 1 2566
TUa-942
TUa- 1096
TUa-943
TUa- 1097
TUa- 1098
UtC 5466
T- I I405
TUa- 1388
UtC 7351
TUa- 1099
ute 83 1 7
TUa- 1093
T- I I 786
T- I I 787
T- 12564
UtC 4726
UtC 54 14
T- I I 96 1
T- I I 963
TUa- 1238
T- l l 960
T- l l962
TUa- 1 260
TUa- 1261
no.
4
4
4
5
5
5
6
6
6
7
7
7
7
7
7
7
10.-98
l a-3/6-93
24.-98
4.-6/9-94
1 .-6/9-94
2.-6/9-94
1 . - 1 4/7-95
1 . - 1 7/7-95
28.-96
2.-8/10-94
4.-( 1 7-9 1 )
5.-22/9-94
1 .-6/9-91
2.-6/9-91
1 .-20/5-92
2.-21/5-92
Mollusc shell
One shell fragment
One shell fragment
One shell fragment
One shell fragment
One shell fragment
One shell fragment
One shell fragment
Div. species
Div. species
Div. species
Div.
Arctica islandica, a.o.
Div.
Arctica islandica, a.o.
Mya
One shell fragment
Div. species
Div. species
Div. species
One shell fragment
Hiatella arctica
Macoma, a.o.
Fragm. of one species
Macoma calcarea
Div. species
Hiatella, Mya, Macoma
Fragm. of o ne species
One shell fragment
Div. species
Div. species
One shell fragment
One shell fragment
Chlamys islandica
Div. species
Fragm. of o ne species
Div. species
Div. species
Mya truncata
One shell fragment
One shell fragment
One shell fragment
Div.
One species
Div.
Div.
Div.
Fragm. of one species
Div.
Mya, Macoma
Div. species
Div. species
Div.
Nuculana, a.o.
Nuculana, a.o.
Anomia
Macoma calcarea
Div.
Mya
One shell fragment
One shell fragment
Balanus
One shell fragment
Div. species
Div.
Div.
Div. species
One shell fragment
Div.
Macoma calcarea
Macoma calcarea
One shell fragment
Macoma calcarea
Macoma calcarea
One shell fragment
One shell fragment
Weight
dl3C
Cl4-yrs. +/-
*
1 2 430
41 660
l l 270
l l 680
I l 060
45 560
38 200
l l 865
12 420
32 100
40 025
35 940
28 355
38 090
I I I65
l i l lO
38 545
37 730
38 060
1 2 200
28 355
12 520
29 075
10 430
1 2 450
> 44.800
28 720
35 500
35 280
30 6 1 0
9 059
1 2 600
12 520
l l 975
l l 990
36 455
32 5 1 0
33 040
33 975
35 800
3 3 700
l l l40
I I 560
9 890
Il 770
10 ISO
41 460
9 670
9 710
9 625
9 670
9 755
9 870
10 245
10 585
9 445
9 540
9 560
8 1 95
2.06 mg
2.3
8 413
1 .69 mg
1.8
2.12 mg
2.02 mg
2.14 mg
2.07 mg
2.57 mg
1 .98 mg
0.5
*
0.3
*
*
0.7
2.7
*
*
*
*
*
*
*
*
-6. 1
*
*
*
1 .98 mg
I.l
*
*
*
*
*
*
2 . 1 8 mg
2 . 1 9 mg
0.4
1.9
2 . 1 6 mg
1 .95 mg
1.8
0.3
*
*
*
*
0.66
*
*
*
*
2.36 mg
2.06 mg
1 .4
-l
*
*
l . l4
1 .86
- 1 .6
0.78
0.84
*
*
*
*
*
*
*
*
0.55
*
*
*
*
*
*
2.5
- 1 .35
*
*
*
*
*
*
*
8 330
9 220
46 340
8 665
9 1 20
36 950
12 490
12 070
I l 615
12 000
39 140
12 035
12 325
46 905
47 565
di 3C: ratio 1 3C/ !2C in per mil with respect to PDB-reference.
: Estimated d ! 3C-value.
*
Table 3: Radiocarbon dates (conv. and AMS) of marine mollusc shells, organized with respect to location and transect, as in Table 2. The
numerical ages are reduced by a reservoir age of 440 years. The list includes 75 dates.
69
lsd
80
1 500
80
70
70
2400
700
60
105
2600
965
1455
430
1675
105
80
835
735
710
60
235
85
370
185
195
240
600
575
3950
39
60
205
155
60
530
395
315
515
600
400
80
90
70
60
70
900
50
85
70
130
75
75
80
80
100
60
l iS
75
49
85
50
1 620
125
I lO
2700
70
60
95
125
2425
230
215
4020
4680
70
l. Olsen et al.
sediments lying below till of at least early lateglacial age.
Thus all dates from this group with measured ages
younger than 15 ka BP must be contaminated by young
carbon, and may therefore be excluded.
An interesting observation from a screening of the
SOL-fraction dates is that all dates that are considered to
be too young based on stratigraphic position result from
measurements of low amounts of C ( < 0.90 mg C; Table
2). All SOL-fraction dates used further in this study are
therefore based on material with a weight > 0.90 mg C. A
similar screening of data has been reported by, e.g., Bar­
nekow et al. (1998) and Gulliksen et al. (1998), who used
"well over l mg C" and > 0.60 mg C, respectively, as the
amount of material used for their AMS measurements.
The last screening step is based on interpretations of
stratigraphy and depositional environment. Samples obtai­
ned from sediments inferred to be of subglacial origin (sub­
glacial channels etc.), are unlikely to contain the remains of
contemporary living organisms or, if they do, this compo­
nent is likely to be small compared to older resedimented
organics. Such samples are therefore also rejected.
From the original 136 dates, only 93 survive the scre­
ening procedures, and (Fig. 9), the majority of these were
obtained from INS-fractions (82 dates). Accompanying
these are some 31 (> 15 ka BP) of a total of 75 dates of
marine mollusc shells (Fig. 9; and Table 3), which are
used in part as dating control for bulk sediment dates
but also as the main basis for the chronology of the gla­
cial history befare 15 ka BP in the coastal areas.
Dating control
In cases where shells were found in the same package of
sediment units (dated unit plus overlying and underly­
ing units), their 14C-dates are a direct control of the bulk
sediment dates, although they may represent different
ages if sediment redeposition has occurred. The
geochronology of the local glacial history of some areas
is mainly based on shell dates. In these cases, by campa­
ring the results with regional events where the chrono­
logy has been established using bulk sediment samples,
shell dating may provide an indirect age control. Amino
acid analysis of shells, luminescence-dating (TL and
OSL) of sand grains, 14C-dating and U/Th-dating of cal­
careous concretions, U -series dating of speleothems, and
palaeomagnetic stratigraphy may also provide some
dating control, either directly or indirectly.
Radiocarbon dates of shells
Radiocarbon dating of shells by decay counting was car­
ried out at the University of Trondheim (T-prefix, Table
3), whereas the AMS was performed at the University of
Uppsala, with graphite targets prepared in Trondheim
(TUa), and at the University of Utrecht (UtC). For details
of the laboratory procedures adopted at the universities of
Trondheim, Uppsala and Utrecht, see Gulliksen & Thom-
NORWEGIAN JOURNAL OF GEOLOGY
sen (1992), Thomsen & Gulliksen (1992), Possnert (1990)
and Van der Borg et al. (1997), respectively.
TL and OSL dating of sediments
Luminescence dating was not included in this study, but
some previously-published TL and OSL dates (Table 4),
are considered to be 'control' dates. These include dates
of feldspars from glaciofluvial and glaciolacustrine fine
sand, and quartz grains from aeolian deposits. For details
of the methods and results, see Mejdahl (1988, 1990,
1991), Bergersen et al. (1991), Larsen & Ward (1992),
Mejdahl & Christiansen (1994) and Olsen et al. (1996).
U/Th - dating of calcareous concretions
Uranium - thorium dating (U/Th) of 4 samples of calca­
reous concretions were carried out at the University of
Bergen. Some additional U -series dates of calcareous
concretions and speleothems (Table 4), from caves in
North Norway are also included (Lauritzen 1991, 1995,
Lauritzen et al. 1996, Nese 1996, Nese & Lauritzen 1996,
Lauritzen, unpublished material 1998). For details of the
laboratory methods, see Lauritzen ( 1995).
Amino acid measurements of shells
Amino acid racemization (AAR) ratios (D-alloisoleucine/
L-isoleucine ratios, denoted alle/ Ile) of shell samples
were analysed at the University of Bergen by V. Clausen
Hope and H.P. Sejrup. Eleven samples were measured, the
objective being to distinguish shells dating to between 35
000 - 45 000 yr old and those of Early Weichselian or
older age, which is beyond the range of the radiocarbon­
method. This led to the identification and exclusion of 4
pre-Middle Weichselian samples (Table 5). For details of
the analytical and preparation procedures see Miller &
Brigham-Grette (1989).
Palaeomagnetic measurements (PM)
Remanent magnetism of samples from five localities was
measured at the University of Bergen under the supervi­
sion of R. Løvlie. Possible excursions were recorded at
two of these localities (Løvlie & Ellingsen 1993, Løvlie
1994). We have also included palaeomagnetic data from
cave sediments from W. Norway and N. Norway in aur
data base, details of which, as well as of the methods
employed, can be found in Larsen et al. (1987) and Valen
et al. (1996, 1997).
Table 4: (next page) Various datesfrom different published sources, used
in the reconstruction of the glacial history and as 'control' dates. For com­
parison between cal yr and 14C yr, see the main text. The dated part of the
bones is collagen. *) Dates used only tentatively because amino acid ratios
ofshells from the same unit indicate a possibly older age. (m) = multiple
fragments; and (s) = single fragment. The table includes 100 dates.
Nlo5 14C·Dating of Glacigenic Sediments
NORWEGIAN jOURNAl OF GEOlOGY
71
Table 4
No. Lab. refr.
Material
l
2
3
4
5
6
7
8
9
• 1o
sand,gl.fluvial (sub-till)
s-silt, gl.Jacus. (sub-till)
s-silt, gl.lacus. (sub-till)
gyttja silt; INS (sub-till)
wood; Salix? (sub-till)
sand,gl.fl.-gl.Iacustrine
sand,gl.fl. -gl.lacustrine
shell (in till) ; (m)
shell (m), gl.m. (sub-till)
shell (in till) ; (m)
shell (in till); Mya trun.
shell (in till); Mya trun.
shell; Mya truncata
shell
shell
foraminifera
algal silt; SOL
algal silt; INS
macro algae
algal silt; SOL
algal silt; INS
algal silt; INS
algal silt; SOL
algal silt; INS
gyttja; SOL
gyttja; SOL
silty gyttja, gl.lacustrine
silty gyttj a, gl.lacustrine
shell (in till); Mya trun.
shell (m)
bone; Ursus Maritirnus
bone; Ursus Maritirnus
bone; Ursus Maritirnus
bone; Canis Lupus
bone of seal
bone; Ursus Maritirnus
calcareous
concretions
calc. concretions
calc. concretions
calc. concretions
calc. concretions
calc. concretions
shell (in till); Mya trun.
shell (in till) ; Mya trun.
shell (in till); Mya trun.
shell (in till)
shell (in till)
shell (in till); Mya trun.
shell; Mya truncata
soil; bulk org. fraction
bone (m)
bone (m)
bone (m)
speleothem
speleothem
speleothem
speleothem
bone (s); Phoca sp.
bone (m); Plautus alle?
bone (m);
bone (s);
gyttja; SOL
foraminifera; E. excavat.
foraminifera; E. excavat.
foraminifera; E. excavat.
shell (in till/silt-sand)
shell (in till/silt-sand)
shell (in till)
forarninifera; E. excavat.
foraminifera; E. excavat.
palaeosol; SOL
silt, glaciomarine, INS
R-93380 1
R-94380l a
R-94380 lb
Ua-3 19
UtC- 1392
R-823820a
R-823820b
TTT-2377
11
T12 AAL 877A
13 Ua-1043
14 Ua- 1337
15 BAL 1 780
16 BAL 1 785
17 T- 1 775A
18 T- 1 775B
19 T-558 1
20 T-4791A
21
T-479 1B
22 T-5278B
23 T-4793A
24 T-4793B
25 T-8559A
26 T-8558A
27 T-8029A
28 T-8029B
29 T-3942
30 Ua-20 16
31
TUa-436
32 TUa-488
33 TUa-485
34 TUa-489
35 TUa-487
36 TUa-346
37 ULB 846 ULB 863
38 T-12093
39 T-12092
40 T-12089
41 T- 12090
42 T- 12091
43 T-2670
*44 T-4004
45
46 T-8071
47 T-7281
*48 T-2657
49 AAL-568
50 T51
T-5 1 56
52 T-5593
53 (8 dates)
54 el 83044
55 el 83142
56 el 8322 1
57 el 83307A
58 TUa-806 1
59 TUa-806
60 (5 dates)
61
(8 dates)
62 T- 132 1 1
63 TUa64 TUa( 1 1 ratios)
65
66 T-3423B
67 T-922
68 T-3422B
69
70
71 T-2380
72 UtC- 1963
Method
OSL
OSL
TL
Age, cal.yr BP
Age, l4C-yr BP
Locality
Refr.
1 7 000+/-2000
26 000+/-3000
26 000+/-3000
14 500+/-2000
22 000+/-2500
22 000+/-2500
37 100+/-1600
> 45 000
33 000+/-3500
37 000+/-4000
c. 27 000
c. 30 000
40 600+2 1 00/-1 700
41 900+2800/-2 100
< 44 000
17 940+/-245
> 40 000
c. 22 000
c. 22 000
18 100+/-800
19 100+/-270
17 800+/-230
17 910+/-820
18 950+/-280
18 950+/-1090
19 100+/-670
20 780+/-540
18 820+/-200
19 650+/- 180
21 800+/-410
2 1 520+/- 150
39 1 50+900/-800
33 560+/- 1 150
20 1 10+/-250
20 2 1 0+/- 130
22 500+/-260
3 1 160+/-300
39 365+/-640
41 1 20+1480/- 1 250
several dates:
17 000 - 36 000
23 345+/- 145
29 360+/-255
31 9 1 0+/-335
32 470+/-325
46 560+2700/-2000
34 330+ 1630/- 1410
42 400+ 1280/- 1 1 1 o
Early Weichselian
41 500+ 3 1 30/-2240
26 940+/-670
35 700+/ - 1 100
Eemian/Late Saalian
20 000+/29 600+/-800
32 800+/-800
Komagelva
Leire!va
Leirelva
Sargejohka
Sargejohka
Kautokeino
Kautokeino
Lauksundet
Leirhola
Kvalsundet
Slettaelva; unit C l
Slettaelva; C 1 -C2
Bleik (overconsolidated sediments)
Bleik ( overconsolidated sediments)
Endletvatnet
Endletvatnet
Æråsvatnet
Æråsvatnet
Æråsvatnet
Æråsvatnet
Æråsvatnet
Æråsvatnet
Øv. Æråsvatnet
Øv. Æråsvatnet
Øv. Æråsvatnet
Øv. Æråsvatnet
Bøstranda, Langøya
Cave; Trenyken
Cave; Kjøpsvik
Cave; Kjøpsvik
Cave; Kjøpsvik
Cave; Kjøpsvik
Cave; Kjøpsvik
Cave; Kjøpsvik
Cave; Kjøpsvik
Olsen et al. 1996
Olsen et al. 1996
Olsen et al. 1996
Olsen, 1988; Olsen et al. 1996
Olsen 1995, 1 998
Olsen 1 988; Olsen et al. 1996
Olsen 1988; Olsen et al. 1996
Andreassen et al. 1985
Andreassen et al. 1985
Vorren et al. 1981
Vorren et al. 1981
Vorren et al. 1981
Møller et al. 1 992
Møller et al. 1992
Møller et al. 1992
Møller et al. 1992
K.D. Vorren, 1978
K.D. Vorren, 1 978
Vorren et al. 1 988
Vorren et al. 1988
Vorren et al. 1988
Vorren et al. 1988
Vorren et al. 1 988
Vorren et al. 1 988
Alm 1993
Alm 1993
Alm 1993
Alm 1993
Rasmussen 1984
Møller et al. 1992
Nese & Lauritzen 1996
Nese & Lauritzen 1996
Nese & Lauritzen 1996
Nese & Lauritzen 1996
Nese & Lauritzen 1996
Nese & Lauritzen 1996
Nese & Lauritzen 1996
Cave; Rana
Cave; Rana
Cave; Rana
Cave; Rana
Cave; Rana
Vassdal
Svellingen, Frøya
Svellingen, Frøya
Ertvågøya
Kortgarden
Eidsvik
Eidsvik
Gamlemsveten
Skjonghelleren; G
Skjonghelleren; G
Skjonghelleren; G
Skjonghelleren; G
Skjonghelleren; G
Skjonghelleren; G
Skjonghelleren; K
Harnnsundhelleren
Harnnsundhelleren
Hamnsundhelleren
Hamnsundhelleren
Kollsete
Elgane; unit 3
Elgane; unit 3
Elgane; unit 3
Foss-Eigeland; EID
Oppstad; unit Q
Oppstad; unit Q
Oppstad; unit N/0/A
Høgemork; unit 3
Vatnedalen
Rokoberget
S.-E. Lauritzen, unpubl.
S.-E. Lauritzen, unpubl.
S.-E. Lauritzen, unpubl.
S.-E. Lauritzen, unpubl.
S.-E. Lauritzen, unpubl.
Rasmussen 1981
Aarseth l990
Aarseth 1990
Pollestad 1992
Pollestad 1990
Mangerud et al. 1981
Mangerud et al. 1981
J. Mangerud, pers.comm. 1981
Larsen et al. 1987
Larsen et al. l987
Valen et al. 1995
Larsen et al. 1987
Larsen et al. 1987
Larsen et al. 1987
Larsen et al. l987
Valen et al. 1996
Valen et al. 1996
Valen et al. 1996
Valen et al. 1996
Aa & Sønstegaard 1997, in prep.
Janocko et al. 1998
Janocko et al. 1 998
Janocko et al. 1998
Andersen et al. 1991
Andersen et al. 1991
Andersen et al. 1987
Andersen et al. 198 7
Andersen et al. 1987
Blystad 1981
Rokoengen et al. 1993
14C-AMS
14C-AMS
TL
37 000+/-5000
41 000+/-5000
TL
14C
14C
Mya t./ Aic. i. >
14C
14C
AAR; alle/Ile > (total= 0.071 ) >
14C-AMS
14C-AMS
AAR; alle/Ile > (total = 0.055) >
AAR; alle/Ile > (total = 0.047) >
14C
14C
14C
14C
14C
14C
14C
14C
14C
14C
14C
14C
14C
14C-AMS
14C
14C
14C
14C
14C
14C
20 000 U!Th
40 000
14C
14C
14C
14C
14C
14C
14C
AAR; alle/Ile > (total= 0. 127) >
14C
14C
14C
AAR; alle/Ile > (total= 0.22) >
14C
14C
14C
14C
range of dates:> 28 900 - 34 400
25 900+/-1 800
29 900+/- 1 800
U-series
27 900+/- 1200
23 900+/- 1200
U-series
28 000+/-2000
32 000+/-2000
U-series
55 700+/-4000
51 700+/-4000
U-series
24 387+/-960
14C-AMS
24 555+/ -675
14C-AMS
range of dates:> 27 580 - 3 1 045
14C-AMS
range of dates:> 29 745 - 3 1 905
14C-AMS
43 800+3700/-2500
14C
34 820+ 1 1 65/- 1 020
14C-AMS
33 480+ 1 520/- 1 280
14C-AMS
AAR; alle/Ile > average: 0.05 > Mid Weichselian age
31 330+ 700/-640
14C
41 300+6200/-3500
14C
38 600+ 1600/- 1 300
14C
AAR; alle/Ile > (hyd = 0.055) > Mid Weichselian age
AAR; alle/Ile > (hyd = 0.05 1 ) > Mid Weichselian age
35 850+/ 1 1 80/- 1040
14C
33 800+800/-700
14C-AMS
72
L
Olsen et al.
NORWEGIAN JOURNAl OF GEOlOGY
Table 4, continuation
No. lab. refr.
73
74
75
76
77
78
UtC- 1962
PM072842
PM072842
PM072842
PM072842
79
R-90330 1
80
RRRR-897005
R-897006
PM072843
R-8970 1 0
T-3556A
T-3556B
81
82
83
84
85
86
87
88
Material
Method
clay-silt, gl.marine, !NS
bone; mamrnoth scapula
bone; mammoth scapula
bone; mammoth scapula
bone; mammoth scapula
soil weathering and
fossil ice wedge
sand, aeolian
sand, aeolian
sand, aeolian
sand, aeolian
sand, gl.fluv.
sand, gl.tluv.
bone (s); mammoth
sand, gl.tluv.
gyttja sand; SOL
gyttja sand; !NS
1 4C-AMS
Age, cal.yr BP
14C
U/Th
U!Th
U!Th
corr. of strata to
adjacent areas
TL
TL
TL
TL
TL
TL
U-series
TL
1 4C
14C
42 400+/-500
52 300+/-900
53 900+/-900
probably Middle
Weichelian age:
37 400+/-4000
39 300+/-4000
40 000+/-5000
40 000+/-7000
32 000+/-3000
54 000+/-5000
45 300+/-2900
<42 000+/-4000
Age, 14C-yr BP
Locality
Refr.
47 000+4000/-3000
45 400+ 1 500/- 1200
Rokoberget
Sæter, Søre Ål
Sæter, Søre Ål
Sæter, Søre Ål
Sæter, Søre Ål
Øv. Åstbrua
(sub-till sediments)
Sorperoa
Sorperoa
Sorperoa
Sorperoa
Fåvang
Fåvang
Fåvang
Haugalia
Grå( mo)bekken
Grå(mo)bekken
Rokoengen et al l 993
Heintz 1974
Idland 1992
Idland 1992
Idland 1992
Haldorsen et al 1992
38 400+/-500
48 300+/-900
49 700+/-900
< glacial adv. after
early M.W. interst.
33 400+/-3000
35 300+/-3000
36 000+/-4000
36 000+/-6000
28 000+/-3000
50 000+/-4000
41 300+/-3000
< 38 000+/-4000
37 330+640/-590
32 520+650/-590
situ or redeposited material in till), selected for dating
include:
Discussion with evaluation of dates
Possible sources ofthe dated organic matter
Based on microscopic and stereoscopic examination
of parallels to most of the dated bulk-organic sedi­
ment samples, we consider terrestrial plant remains to
be the main organic component in most cases. This
also applies to the sediments where a certain marine
organic component is detected. However, exact num­
bers for the distribution of the different organic com­
ponents are not available, and possible origins of the
organic matter in the waterlain sediments ( either as in
l) the remains of contemporary marine or lacustrine
organisms,
2) the remains of contemporary terrestrial organisms,
3) airborne organic particles of contemporary living
organisms from remote sites,
4) resedimented organic matter from older sediments or soils,
5) secondary (post-burial) organic matter delivered by
cryoturbation, bioturbation, water transportation
(particulate or dissolved), or other processes.
Table 5
No.
m a.s.l.
Species
HYD
40
Mya trun.
I-97
40
Mya trun.
Mågelva
11-97
155
Mya trun.
BAL 3366B
Mågelva
II-97
155
Mya trun.
3
BAL 3377
Mågelva
3 - 1 9/8-97
ISO
Mya/Hia.
4
BAL 3388
Harstad
AL 9700 1
Dislocated
5
BAL 3389
Sto reiva
AL 97004
1 10
Mya trun.
6
BAL 3390
Store!va
AL 97003
lOS
Arc./Mya?
7
BAL 3391
Sto reiva
AL 97007
115
Mya?
8
BAL 3392
Skogreina
05.06.93
lO
Mya?
9
BAL 3393A
Vassdal
1 - 1 1 1 0-92
5
BAL 3393B
Vassdal
1 - 1 / 1 0-92
5
10
BAL 3394
2 - 1 / 1 0-92
20
11
BAL 3395
Gammelmunnåga
Bogneset
4-25/8-96
8
0.035
0.033
0.032
0.032
0.028
0.043
0.04
0.035
0.034
0.048
0.042
ND
0.0 1 5
0.08 1
0.08
0 . 1 47
0 . 1 49
0. 1 44
0.13
0 . 1 58
0. 1 54
0.022
0.02 1
0.02 1
0.0 1 5
0. 1 1 3
0. 1 1 5
0 . 1 05
0.095
l
2
Lab. refr.
Location
Field no.
BAL 3365A
Harstad
I-97
BAL 3365B
Harstad
BAL 3366A
Bergersen et al. 1991
Bergersen et al l991
Bergersen et al. 1991
Bergersen et al. 1991
Myklebust 1992
Myklebust 1992
Idland 1992
Myklebust 1992
Thoresen & Bergersen 1983
Thoresen & Bergersen 1983
Are. is!.
Cardium
edule
Cardium
edule
Mya
Are. is!.
Table 5: Amino acid racemization ratios and inferred age of dated shells.
f\verage/
Probable age based
on the AAR ratios
std. dev..
FREE
A�rage/
std. dev.
0.034
0.00 1
0.03 1
0.002
0.187
0.183
0. 1 55
0. 146
0. 1 85
0.003
0. 1 5 1
0.005
Lateglacial age
0 .042
0.002
0.035
0.00 1
0.045
0.004
0.0 1 5
0 . 1 95
0. 1 76
0. 1 56
0 . 1 47
0. 1 75
0.22 1
ND
0. 1 86
0.0 1 3
0. 1 52
0.005
0 . 1 98
0.033
Lateglacial age
0.08 1
0.00 1
0.148
0.00 1
0.137
0.0 1
0 . 1 56
0.003
0.022
0.00 1
O.D l 8
0.004
0. 1 1 4
0.00 1
0.296
0.28 1
0.435
0.43
0.4 1 5
0.402
0.36
0.361
ND
ND
ND
ND
0.382
0.407
0.276
0.27
0.289
0.0 1 1
0.433
0.004
0.409
0.009
0.361
0.00 1
O. l
0.007
Lateglacial age
Lateglacial age
Lateglacial age
Postglacial age
Mid Weichselian
age
Eemian age
Eemian age
Early Weichselian Eemian age
Postglacial age
Postglacial age
0.395
0.0 1 8
0.273
0.004
Early Weichselian Eemian age
Mid Weichselian
age
AM5 '"C·Dating of Glacigenic Sediments
NORWEGIAN JOURNAL OF GEOLOGY
C4C- age± 1a):
Legend
Test dates:
o
1!1
IV
Ill
{
Control dates:
INS, 14C
SOL, 14C
�
,.....__..._.
,__c__,
Sheii,14C
Tl/OSL (recalculated to14C-yr)
Calcareous concretion, 14C
Palaeomag. excursion
Bone, 14C of colagen
� Bone, U[fh-dating
(recalculated to 14C-yr)
,__p__,
,__ø__,
,_e....
,__B--l�
15
-Lillehammer;
INS: silt. Control: till
- L.angstrandbakken;
lNS: silt. Control: tili
14
- Sargejohka;
13
INS: gyttja, silt. Control: lill
12
- Sitter;
INS: tili. Control: tili/sand
o
11
-Grylaga;
tili
10
- Gråbekken;
sand -silt
9
-Folldal;
sand- silt
CJ
8
11
73
o
-l.eirelva;
sand· silt
li!
-Sitter;
7
till
D
6
o
5
o
4
o
il
-Myrvang;
silt
o
- Kroktåa;
tili
(]
- Mågelva:
tili
o
l
l
illii
l,
.._
,
-
Mesna;
sand -silt
- Fiskelauselva;
silt
l
- Komagelva;
sand- silt
•
10
do
ds
5o
Fig. l 0: Fifteen examples of test- and 'control' dates used in this study; see also Ta ble 6. Four groups of dates are shown: I - Con trol dates from
the same unit (as the test dates) or from correlated units from nearby sites; Il- Test dates and/or control dates resedimented from older units;
III- Control dates from younger units; and N- Control dates derivingfrom older units. Note that only the examples in group I include test
dates and control dates which are directly comparable in age. See the main textfor correction of cal yr to 14C yr, and for further details.
We consider that a combination of sources l, 2 and 3
will introduce only minor age-deviations. The products
of contemporary living organisms will probably contri­
bute similarly to the radiocarbon date, on average, in
each region, except for possible unusual cases of extra­
ordinarily high fractionation, hardwater or reservoir
age effects (e.g. Barnekow et al. 1998). The similarity in
ages for the ice advances and retreats in the different
regions studied (p. 22)(Fig.l), exclude serious age-dis­
tortions in most cases. The same applies to contamina­
tion through resedimentation (4) or post-burial alter­
ation (5), though these are more diffi.cult to evaluate.
However, we think that our approach has reduced the
likelihood of post-burial contamination by particulate
material coarser than medium to coarse silt. We also
consider that the risk of post-burial contamination by
dissolved organic matter is reduced because of the low
permeability of the dated, homogeneous fine-grained
sediments, coupled with the exclusion of samples with
traces of oxidation.
The effects of resedimentation by older organic
matter (4) may, however, occasionally be detected. In
the simplified log from Hattfjelldal, presented by Olsen
( 1997a), a sequence of reversed ages with depth is evi­
dent. This suggests that organic matter in the glacial­
glaciofluvial sequence has been eroded from progressi­
vely deeper/older strata, to be redeposited in reversed
order of age.
74
NORWEGIAN JOURNAL OF GEOLOGY
L. Olsen el al.
The accuracy and precision of the datesf
B
A
Number of sats
of repticates
Age-deviations
%
No.
.
.
±6
±4
±2 -
-
8 -
±8
•
.
l
l
l
3
4
n=2
6 -
.
.
.
.
.
.
.
r--
4-
2-
Number of replicates
Il
l
l
:::4.5%
5-6%
2:9%
Age-deviations (±}
Fig. 1 1: Dating precision indicated as age deviations from the mean
age � each set of 1 4 sets of replicate dates; A - Dots representing each
set of replicates, and B - Histogram which shows, for instance, that 9
of 1 4 sets of replicate dates have a datingprecision with age deviati­
ons � 4.5 %, and that 13 of 14 such sets ofdates have a datingpreci­
sion with age deviations � 6%.
Incorporation of a significant amount of recent orga­
nic matter during sample storage (5) is thought to be
unlikely in the samples employed in this study because
NaOH-insoluble fractions only were used as a basis for
the glacial curve constructions, and any recent organic
growths would be mainly alkali-soluble. In the cases of
other sediment fractions of low organic C content and of
terrestrial macrofosslls, however, such input during stor­
age may lead to serious contamination by young carbon
(Wohlfarth et al. 1998).
Redeposited older organic matter derived from older
solls may occasionally be encountered, and in such cases
the accuracy of the radiocarbon ages is reduced. Conside­
rably radiocarbon dating of solls and buried solls has been
attempted with variable degrees of success for more than
30 years (Campbell et al. 1967a, b, Scharpenseel & Becker­
Heidmann 1991, Martin & Johnson 1995, Wang et al.
1996). Generally it is concluded that radiocarbon ages of
organic matter in soll increase with depth and time, but
will eventually reach a steady state which is a function
mainly of regional climate (Wang et al. 1996). Therefore,
radiocarbon dating of organic matter in buried soll could
overestimate the age of burial by as much as the steady­
state age of the soll. In an attempt to unravel this problem,
Wang et al. (1996) also found that the steady-state ages of
organic matter for three solls were at least 5 000-10 000
years at 20 cm depth, and even higher in deeper parts of
the profiles. This degree of 'aging' could not be established
during the short intervals avallable between each Middle
to Late Weichselian burial episode in Norway. Conse­
quently, we consider the effects of any input of older soll­
material in the sediments to be no more serious, but pro­
bably of a simllar scale, to that attributable to the inwash
of older organic matter, which is generally thought to be
insignificant in most Weichselian sediments in Norway.
The type of dating methods, material dated, palaeocli­
matic data and other parameters used to reconstruct the
regional glacial history are indicated in Table 5 and Fig. 2
(see also Appendix B). 14C and AMS- 14C dating of sedi­
ments are the most important dating methods used in
our reconstructions, the focus being on INS fractions
because they seem to be much less sensitive to contami­
nation by younger material through groundwater than
SOL and DCM fractions. This observation is not surpri­
sing, because the fine-grained material selected for
dating would prevent infiltration by particulate matter,
and only the dissolved organics can easlly migrate
through these sediments. The INS fraction is not parti­
culary prone to contamination by dissolved matter in
contrast to the SOL and DCM fractions. We think that
all the DCM fractions, which mainly are derived from
dissolved organic matter, are seriously contaminated by
young carbon or were derived almost entirely from infil­
tration of Holocene organic material into the sub-till
sediments. Hence, all dates obtained using DCM- extrac­
ted material are rejected.
All the sediment samples considered in this study
were obtained from locations that are situated above the
present-day groundwater level, occasionally near steep
groundwater gradients and surface water draining
through the sediments. The SOL fraction in such sedi­
ments is clearly less likely to yield reliable age estimates
than simllar fractions obtained from low altitude basins
where the generally slow groundwater flow makes the
SOL fraction less vulnerable to groundwater contamina­
tion. This is one reason why the SOL fraction is the pre­
ferred dating fraction for sediments in such terrain posi­
tions. Another reason for dating the SOL fraction in pre­
ference to the INS fraction, is that the latter may occasio­
nally include particles of graphite or old organic matter
which may be resistant to moderate pedogenetic disinte­
gration processes (see e.g. Olsson 1974, Paus 1982, Vor­
ren et al. 1988, Gulliksen et al. 1998).
The accuracy of ages obtained for INS fractions
depends on the depositional environment and sediment
type. Based on microscopic and stereoscopic examination
of samples from most of the dated sediments we assume
that the predominant organic component of the INS
fraction is derived from contemporary plants and ani­
mals, inter-mixed with resedimented soll matter from the
surrounding terrain. In unusual cases where the latter
component is extraordinary high, or in the very few cases
where a major part of the plant remains may derive from
limnic plants, the radiocarbon ages of the INS fraction
may be seriously influenced by older carbon (reservoir
effect). The rate of influx of soll material is probably grea­
ter during an ice advance phase, than during a retreat
phase, due to increased solifluction rates during stadial
periods. In a few cases we have attempted to test the accu­
racy of INS fraction dates by independent measures
(Table 6 & Fig. 10), such as, for example, dating of shell
NORWEGIAN JOURNAL OF GEOLOGY
NilS
Table6
Locat ion
Sediment
Test, 14C-yr BP
Control, yr BP
l
Kornagelva
sand- silt
16 420+/-190; !NS
OSL: 17 000+/-2000;
2
Fisklauselva
silt
28 000+/-500; INS
Palaeomag. excursion,
29 400+/-500; !NS
L ak e Mungo(?) , age;
No.
14C: 14 500+/-2000
14C: c. 28 000
3
Mesna
sand- silt
3 1 500+/-700; !NS
see Table 4, nos. 79-82
Mågelva l
36 100+900/-800; !NS
4
til!, with re-
13 890+/-140; !NS
14C: 11 680+/-70 (shell)
5
Kroktåa
til!, with re-
13 950+/-90; !NS
14C: 12 230+/-80 (shell)
6
Myrva ng
silt, with re-
16 770+/-190; INS
14C: 12 070+/-60 (shell)
sed. org.
Sitter
til!, with re-
14 350+/-90; SOL
7
sed. org.
sed. org.
75
Minimum difference in %
(+l- l std.)
(+l- 2 std.)
o
o
o
o
o
o
13
11
corr. unit, TL-dates,
sed. org.
30 200+/-400; INS
'"C-Dating of Glocigenic Sediments
12
8
27
22
14
9
12
o
6
o
34
28
7
2
13
40
7
shell from correlated
units; 14C:
36 950+/-2700
39 140+/-2425
8
Leire!va
sand- silt
17 290+/-170; INS
TL : 26 000+/-3000;
14C: 22 000+/-2200
18 680+/-170; SOL
OSL: 26 000+/-3000;
26 260+/-220; !NS
14C: 22 000+/-2200
calc.concretion,
9
Folldal
sand- silt
23 260+/-160; SOL
14C: 36 300+500/-600
lO
Gråbekken
sand- silt
32 520+650/-590; INS
calc. concretion,
37 330+640/-590; SOL
14C: 41 300+900/-1000
11
Grytåga
till, with re-
35 400+/-500; !NS
shell
12
Sitter
til!, with resed. org.
21 150+/-130; !NS
14C: 41 460+/-900
shell in overlying unit;
12 480+/-70; SOL
14C: 12 490+/-70
13
Sargejohka
gyttja silt
35 .000+/-1600; INS
Palaeomag. excursion
sed. org.
o
in overly ing unit; L ak e
Mungo?, age:
14C: c. 28 000
14
Correlated unit;
TL : 37 000 - 41 000;
14
Langstrand-
15
Lillehammer
silt
18 700+/-500; !NS
14C: 33 000 - 37 000
shell from underlying
silt
31 500+/-700; INS
unit, 14C: 36 950+/-2700
mammoth scapula from
bakk en
32 300+/-500; !NS
36 l 00+900/-1000; !NS
o
75
corr. underly ing unit,
14C: 45 400+ 1500/-1200
See al so Table 4 , nos.
75-77.
20
Table 6: Comparison of sediment test dates and other dates ('control') from either the same or an adjacent correlated unit. TL, OSL and U-series
ages are given in cal yr BP and corrected to 1 4cyr BP. Dates 1 -3 represent group I in Fig. 1 0, where as dates 4-1 1 , 12-1 3 and 1 4-15 represent
groups Il, Ill and N, respectively.
material obtained from the same stratigraphical hori­
zons. The difficulty with such an approach is that the
shells may have been redeposited, and thus be derived
from a different source to that of the INS fraction.
For direct comparison of all age estimates, those not
based on the radiocarbon method were corrected to the
14C-yr timescale using a simplified (and converted)
version of the CALIB 3.0 computer program (Stuiver &
Reimer 1993) for ages up to c. 22 000 cal yr. The radio­
carbon ages of older dates were estimated by subtrac­
ting 4000 yr from the original values. This accords
approximately with other comparisons up to c. 45 000
cal yr between cal (U-series dating and varve chrono­
logy) and 14C timescales based on the dating of speleot­
hems, corals and terrestrial macrofossils (e.g. Vogel
1983, Bard et al. 1993, Hercman & Lauritzen 1996,
Vogel & Kronfeld 1997, Kitagawa & van der Plicht
1998).
In the three cases where dates using independent met­
hods have been obtained from the same or age-equivalent
units the ages overlap at+/- lcr (Fig. 10, group I). Sedi­
ment dates and 'control' dates in such cases are conside­
red to give an accurate age of the sediment unit. By con­
trast, in eight tests (group Il) where at least one of the
dates (test or 'control') seem to have been redeposited
from older units, four are from till, where both the test
and the 'control' dates must therefore retlect redeposited
organics. Mean differences of 14-18 o/o and 8-11 o/o bet­
ween the test and 'control' dates of group Il are calculated
from average ages at+/- lcr and+/- 20", respectively.
76
Table 7
No.
l
NORWEGIAN JOURNAL OF GEOLOGY
l. Olsen et al.
Material
Age; 14C-yr BP
Average; 14C-yr BP
Precision
Hattfj elldal,
sand-
(+/- 6%)
silt-
28 080+127 300+126 720 +125 980+/28 700+/30 900 +129 280+/31 600+141 800 +/38 500+137 200+139 500 +/17 800+/IS 920+/17 800+/16 700+115 620 +119 600+/19 050+/18 000+/17 110+/18 680 +l28 000 +/29 400 +/19 900 +120 040 +111 790 +111 580 +/14 710 +/14 120+/25 370 +123 500 +119 880 +/16 850+l23 700 +125 300 +1-
26 500 +1- 1500
n=4
30 200 +l-1500
(+/- So/o)
39 500 +/- 2300
(+/- 6%)
16 850 +1- 950
(+/- 6%)
16 150 +/-550
( +/- 3.5%)
18 800 +/-800
(+/-4.5%)
17 900 +/- 800
(+/- 4.5%)
28 700+/- 700
( +/- 3%)
19 900 +/-200
(+/-lo/o)
11 685+l- !OS
(+/-lo/o)
14 415+/-295
( +/-2%)
24 500 +/- 1000
( +/-4%)
18 350 +l- 1550
(+l-9%)
24 500+1- 800
(+/- 3.5%)
Location
gravelly
sand
2
Reinåa,
sand-
n=4
tillsandtill
3
Grytdal,
sand-
n=4
tillsilt-
till
4
Flora I,
till-
n=3
silt sand-
Flora Il,
till-
n=2
Flora III,
till
silt sand-
n=3
silt sand-
Leirelva, SOL
silt
silt-
n=2
silt
Grane, F.,
n=2
Blåfjellelva II,
siltsilt-
n=2
silt
Okshola,
silt sand-
n=2
till
5
6
7
8
9
lO
till
11
Domåsen,
silt sand
silt sand-
12
n=2
Hattfjelldal Il,
silt sand
till-
n=2
silt
ReinåaIl,
silt sand -
n=2
silt sand
Grytdal Il,
till-
n=2
silt
13
14
The 'control' dates in two of the tests in group Il
( Gråbekken and Folldal) were obtained from calcare­
ous concretions, which are likely to yield 'old' ages
because of dissolved carbonate (hardwater effect). If it
is assumed that the test and 'control' dates of gro up Il
may, in several cases, be based on materials of mixed
ages, then the accuracy may be greater than expressed
above. Based on these preliminary tests (Fig. 10), it is
conduded that the accuracy of the sediment dates is
hetter than 15 o/o at+/- 1cr and hetter than 10 o/o at+/2cr. However, because relatively few dates based on a
few dating methods are available to support the exer­
cise at each site, it is the regional consistency of data
(assuming that the major regional events have similar
age; see p. 22) which provides the best indication of the
accuracy of the dating. The combination of regional
stratigraphy and dated stadials and interstadials simply
does not give enough available time, considering the
time needed for multiple major ice-growth and ice­
retreat intervals, for the low accuracy of the dates wit­
hin the 40-15 ka BP interval (Fig. 12). Further discus­
sion on this topic can be found below and in Olsen et
al. (this volume).
Table 7: Replicates ofAMS-14C
dates (mainly the INS fradion)
from one unit or a succession of
stacked closely spaced units of
a/most the same age and gene­
sis.
Dating precision
The dating precision or reproducability of the INS frac­
tion ages could be tested by comparing replicates of
dates obtained from some 14 sediment units or successi­
ons that are dosely associated with respect to genesis,
time and space. The results show a good precision
(Table 7, and Fig. 11), with 13 of the 14 replicates within
a 6 o/o deviation.
Statistical treatment of the new dates
The new dates presented here and used for reconstruc­
tion of the history of ice-sheet fluctuations (Olsen et al.,
this volume), have been given a statistical evaluation
using a standard Student t-test (Table 8 ) . The critical
values of the Student t-function are obtained from a sta­
tistical table of Student t-distribution published by Fis­
her & Yates ( 1948 ) . Data sets 1-4 represent the dates from
the four major interstadials which occurred during the
45-15 ka BP interval (Olsen 1997 ) . Similar groups of
dates with approximately the same mean ages (c. 16-18,
25-28, 33-35 and 41-45 ka BP) appear in Fig. 9, which
ANIS '"C·Dating of Glac igenic Sediments
NORWEGIAN JOURNAL OF GEOLOGY
Table 8
� (Trofors
(Bulk
organic sediment dates)
16 420±190
17 290±170
17 no±160
18 680±170
20 470±no
17 700±80
18 880±100
19 500±200
18 700±500
19 340 + 150
n1 =40
!lt
Stt1
interstadial)
= 18 698
Sn1 = 218
22 330±150
16 250±190
16 no±120
18 580±140
18 020±170
17 830±190
22 220±240
19 no± no
20 040±100
22 070 + 170
21 150±130
19 600±280
16 770±190
19 050±120
18 000±400
16 850± 90
19 880±160
18 970±150
18 820±no
22 490±180
17 800±400
19 480±200
15 920±260
16 770±190
17 800±400
21 000±400
16 700±220
18 900±200
15 620 + 200
19 090 + 100
Confidence leve!= 99 % �a=0.01
� L 1 = t112a * Sn1=2.708 * 218 = 590
� 'True' mean age of set l = 18 698 (±590)
5n.l (Hattfjelldal interstadial I)
(Bulk
29 280±260
30 900±300
38 500±700
37 200±600
32 000±300
33 800±800
36 100±900
31 500±700
32 300±500
36 300±500
31 600±400
!13 = 33 982
�
Sn3 = 1n6
(Hattfjelldal interstadial Il)
(Bulk organic sediment dates)
25 860±280
27 580±220
24 858±161
26 400±400
28 000±500
27 300±600
25 700 + 600
n2 =27
28 700±300
28 600±300
25 240±180
26 800±400
23 700±200
26 260±220
25 300±260
23 260±160
28 400±300
(shell dates)
28 300±240
28 355±430
23 250 + 170
28 355 + 235
Confidence leve!= 99 % �a=0.01
n2 =26 431
� Lz = t112a * Sn2=2.77 l * 312 = 865
� 'True' mean age of set 2=26 431 (±865)
28 060±220
25 370±170
25 980±240
25 780±240
26 720±280
23 500±240
28 000 +200
Sn2 =312
�n1+590 <n2 -865
� Significant difference at 99 % confidence leve!.
('pre-Hattfjelldal' interstadial)
�
organic sediment dates)
34 000±600
35 400±500
36 800±600
30 600±300
29 400±500
30 500±600
34 900±400
31 000±500
29 700±500
28 700±400
30 200±400
35100± 1600
n3 =44
(shell dates)
38 200±700
35 500±600
40 025±965
35 280± 575
36 455± 530
38 545±835
37 730±735
38 060±710
28 720±240
32 510±395
32 100±2600
35 940±1455
30 610±3950
38 090±1675
39 140±2425
33 040±315
33 975±515
35 800±600
33 700±400
36 950±2700
29 075±370
(Bulk
organic sediment dates)
(shell dates)
41 000±240
41 300±900
41 800±1000
n4 = n
39 500±800
47 000±4000
14 =43 645
� L4 = t112a * S114=3.169 * 2487 = 7881
�'True' mean age of set 4 = 43 645 (±7881)
S14= 2487
41 660±1500
46 340±1620
45 560±2400
46 905±4020
47 565 +4680
41 460±900
Confidence leve!= 99 % �a=0.01
�n3+3013 >J4-7881
� Possible insignificant difference at 99 % confidence leve!.
Additional statistical evaluation:
The confidence interval for the difference between the mean
ages (n3 and14) of the two data sets3 and4 is:
Confidence leve!= 99 % �a=0.01
L= Z112a * ..J (Sfi4+ S114); and 99 % confidence leve!
� = t112a * Sn3=2.700 * ln6 = 3013
�'True' mean age of set3 = 33 982 (±3013)
� L=2.57
�n2 +865 <n3-3013
� Significant difference at 99 % confidence leve!.
77
�a=0.01 and Z112a = 2.57
*
..J ( 1116+ 2487) = 154
� (14- !13-L) < (11 4- ll3 ) < (14- !13+L)
� 9355 < 9663 < 9817
� The difference in mean ages between data sets3 and 4 is
also significant at 99 o/o confidence leve!.
�
Table 8: Statistical evaluation of dates based on Student t-distribution. Critical values of tfor 1/2a and n-1 degrees offreed om, after Fisher & Yates
(1 948). a is the risk-of-err or leve� (1 -a.)lOO% is the confidence leve� n is the number ofdates,J1 is the mean, S is the standard error ofthe mean, L is
theconfidenæ interva� and Z112a is a given number (e.g., 1.64fora=0. 1 0; or 90% confidence leve� and 2.57 ra=O.Ol; or 99% confidenæ level).
shows a histogram of the same dates, independent of
stratigraphy and stratigraphic correlations. This implies
that the statistical treatment of the four interstadial data
sets are also based on a statistically sound and (almost)
independent basis. The stratigraphic correlations are
considered to be of only minor significance for this sta­
tistical treatment, because the differences in mean ages
between the different groups of dates are larger before
(Fig. 9) than after introduction of correlations as a tool
for separation of data in sets 1-4.
The first step of calculations shows that the diffe­
rences in mean ages of data sets 1-3 are all significant
at a 99 % confidence level. The confidence intervals at
this level for data sets 3 and 4 are overlapping, which
indicates that the difference between their mean ages
may be insignificant. However, the additional statisti­
cal evaluation (Table 8) shows that the difference in
mean ages between these data sets is also significant at
a 99 % confidence level. Consequently, the comparison
of dates based on Student t-distribution shows signifi­
cant differences in mean ages of all represented inter­
stadials.
StratJgrap � y and stratigraphical
cons1derahons
Generalizecl stratigraphy
A generalized stratigraphy of the Middle and Late
Weichselian of Norway is illustrated in Fig. 12. The stra­
tigraphical model includes five main units of tills alter­
nating with waterlain sediments. Units 3 - 10 represent
the interval 15 - 45 ka BP on the basis of all available
dates. The generalized stratigraphy is based on more
78
l. Olsen et al.
NORWEGIAN JOURNAl OF GEOlOGY
lnterstadials
(14C-ages)
Stratigraphical model
Unit
1
2
C.13 ka BP
3
4
5
6
7
8
C. 39 ka BP
9
Cl-Si S
G
D
Transect number
(Consistency)
and
No. of transects
ice advances
9
1,2,3,4,5,6, 7,8, 9
1,2,3,4,5,6, 7,8, 9
1,2,3,4,5,6, 7,8, 9
1,2,3,4,5,6, 7,8, 9
9
9
9
1,2,3,4,5,6, 7,8, 9
9
3
1
4-5
6-7
1
3, 7,8(?}, 9
1, 3,4(?), 5,6, 7, 9
1
l
l
9
V
'Bø Iling
interstadlal'
IV
9
N
=
40
6-7
Range (92%)
7-8
Ill
5-7
Range (100%)
6-8
11
6-8
Range (1 00%)
1 (?), 2(?), 3(?), 4(?),6(?), 7,8, 9
3-8
l
3(?), 6(?), 7,8, 9
3-5
Range (100%)
1,
1, 3(?),4,5,6, 7,8, 9
5
5
1'
1
1
5-7
3(?),4,5, 7 ,8(?), 9
N
1' 3(?}, 4,5, 6(?}, 7,8, 9
1
1' 3(?),4,5,6(?), 7, 8, 9
Cl
=
Clay
Si
=
Silt
S = Sand
1
6-8
G = Grave!
D
16-21 ka
=
=
27
23.3- 28.7 ka
N
=
44
28.7-40 ka
N
=
14
40-47 ka
Diamicton, mainly basal till
Fig. 12: Outline of the generalized regional stratigraphy representing the interval l 0-1 5 to 40-45 ka BP. The chronology refers to 14C-yr. Unit l
may include several subunits of tills and waterlain sediments, and is supposed to represent all lateglacial stadial and interstadial events after c.
12.3 ka BP. Unit 2 represents the first regional lateglacial ice-retreat phase recorded in onshore positions along the coast ofNorway. Unit 3
represents the second major ice-advance (LGM 2) during the Late Weichselian. Units l, 2 & 3 occur along all nine transects. Unit 4 represents
the ice retreat between the two major ice advances during the Late Weichselian. So far, this unit has not been recorded along transect 2. Unit 5
represents the Last Glacial Maximum (LGM l). It is probably represented along all transects, but as unit 4 is lacking along transect 2, unit 5
cannot be proper/y distinguished from the overlying unit 3. Units 6, 7 & 8 also occur along most transects, whereas units 9 & l O are considered
less well-dated and more tentative/y correlated, with the exception of transects 7, 8 & 9 where these units are dated more accurately.
than 100 localities spread over most parts of Norway.
Almost 50 of these localities, with representatives from
all nine transects (Fig. 1), are included as examples in
Appendix A, and 3 1 of these are presented in simplified
stratigraphic logs (Appendix A). The localities, compri­
sing excavated sections, cores and exposures along rivers
and roads, are grouped in Appendix A according to their
occurrence along each of the nine transects from distal
(left) to proximal (right), and are presented from north
to south.
Regional overview
There is a strong regional consistency with ages based on
more than 300 dates (all included in our extended data
base) in the stratigraphic scheme depicted in Fig. 12 and
Appendix A. The major ice advances I- IV of the inter­
val 15- 45 ka BP are represented by glacial sediments in
at least six of the nine transects, except for ice advance I
(dated to c. 40 ka BP), which is less pronounced in our
data. However, ice advance I may also be represented, at
NORWEGIAN JOURNAl OF GEOLOGY
least indirectly, in more than the two areas west of the
main watershed where 40 ka-aged glacial deposits are
recorded (i.e. along transects 7 and 8). Evidence of a very
high relative sea-level along transect 9, during deposition
of unit 8 at Herlandsdalen, Passebekk, and Mesna, and at
Rokoberget c. 233 m a.s.l. (Olsen & Grøsfjeld 1999; late­
glacial marine limit c. 190 m a.s.l.; at this site where the
sediments are depleted in Ce and contain some marine
dinotlagellate cysts; see Appendix B-7), indicates signifi­
cant glacial isostasy and the occurrence of an extensive
ice-body corresponding to unit 9. Till recorded for this
glacial episode, called the Mesna Till, occurs at Lilleham­
mer (Olsen 1985). This suggests that a significant ice
advance at c. 40 ka BP may also have occurred in south­
eastern Norway. The same argument with high 'relative'
sea-level may be made for stratigraphic evidence for sites
along transects 3, 4, 5 and 6, which indicates that this ice
advance, at least south of Vestfjorden (Fig. 1), may have
been a very extensive one. The intervening interstadial
episodes also seem to be equally well represented over the
region as a whole. At least two of the four interstadials are
represented at more than 60 o/o of the sites. Proxy palaeo­
climatic and palaeoenvironmental data and other charac­
teristics from some of these interstadials are included in
Appendix B. The consistency of the regional stratigraphy
gives clear constraints for the ages and duration of events
in the generalized stratigraphic model (Fig. 12), and thus
constrains the accuracy of the dates utilized.
Summary and conclusions
Radiocarbon dating with AMS of sediments with a low
organic carbon content is the most important geochro­
nological method employed in this work. Quaternary
geological mapping and correlation have provided a
range of pre-lateglacial sediments available for dating in
this study of Middle and Late Weichselian ice-sheet tluc­
tuations in Norway. This implies that all dates evaluated
and used here have a minimum age of 13-15 ka ( 14C) BP,
which have been used as a reference age to evaluate the
effect of possible contamination by young carbon.
Terrestrial macro plant remains, formed in equili­
brium with the atmosphere, which would be preferred for
dating in order to avoid reservoir effects, were not avai­
lable in most cases. An attempt has been made to over­
come the disadvantages of possible contamination of
sediments which have a low organic carbon content, by
the careful screening of samples, and, where possible,
comparing a number of dates from the various lithologi­
cal units. Emphasis is placed on age estimates obtained
from fine-grained sediments (p. 18) using INS fractions
(most dates > 15 ka BP) because these appear to be much
less liable to contamination by younger organic material
than SOL and DCM fractions, especially for samples taken
well above the local groundwater table. All DCM-extrac­
ted samples, and all SOL fractions with small amounts of
AMS '"COating
of Glacigenic Sediments
79
material ( < 0.90 mg C) used for AMS measurements are
seriously contaminated by young carbon (dates < 13 ka
BP), and therefore should not be used for reconstruction
of glacial variations. Two dates based on hexane fractions,
also obtained from sediments lying well above the present
groundwater table, seem to be uncontaminated by young
carbon, and may therefore provide reliable ages.
There is a noticeable scarcity of radiocarbon dates of
shells, which may retlect a general scarcity of shells in the
age range 15-27 ka BP (Fig. 9) on the Norwegian main­
land. Dissolution by moderately concentrated acidic
meltwater from melting sea-ice, together with their
removal by glacial erosion, are possible explanations for
this effect (Olsen et al., this volume). Thus the bulk orga­
nic sediment dates are particularly important for the
reconstruction of the glacial history of Norway during
this period.
14C-dates of bulk sediment samples and macro algae
from waterlain sediments from Andøya, northern Nor­
way, show a difference between INS and SOL fractions
that is normally less than 5 o/o, and less than 8 o/o, in
extreme cases (K.D. Vorren 1978, T.O. Vorren et al. 1988,
Alm 1993). The data from sediments located well above
the local groundwater level reported here occasionally
show much larger age deviations {10-30 o/o) between the
INS and SOL fractions. However, in all these cases the
SOL-fraction dates result from measurements of very
small (< 0.90 mg C) amounts of carbon.
The data reported here, which include a number of
'control' dates based on a variety of dating methods,
enable the accuracy of bulk sediment dates to be asses­
sed. The accuracy of the INS fractions in particular is
relatively high (less than 10-15 o/o deviation between test
and 'control' dates). The precision of replicate dates has
also been shown to be fairly high. However, the number
of high-quality 'control' dates for establising dating
accuracy is low (Fig. 10). The strongest argument for the
overall reliability of the bulk sediment dates rests on the
high regional consistency in the dates of well-documen­
ted lithological and stratigraphic changes and geological
events along the nine transects in our model. However,
the relevance of this argument is based on the assump­
tion of consistency in the timing of regional glacial
events. If these events were not fairly contemporaneous,
then our strongest argument for dating quality is less
valid. The combination of stratigraphy and geochrono­
logy based on various dating methods for the age-inter­
val 15-40 ka (14C) BP does, however, constrain the accu­
racy of the age estimates of the different events, such that
no single regional glacial event is likely to be, in any case,
more than 2000-3000 yr outside the estimated age range
(Fig. 12). This is also supported by the statistical evalua­
tion based on Student t-test of all new dates presented
here, which show significant differences in mean ages of
all represented pre-lateglacial interstadials, at a 99 o/o
confidence level (Table 8). Further examination of these
results and hypotheses as well as the timing of events
during the Middle and Late Weichselian in Norway is
80
NORWEGIAN JOURNAL OF GEOLOGY
L. Olsen et al.
now in progress in a new project (NORPAST 19992002), which has participants from several universities
and research institutions (Larsen et al. 1998).
The glacial variations during the Middle and Late
Weichselian in Norway, based on the chronology inclu­
ded here are shown to be semi-cyclic in character, inclu­
ding very rapid changes which imply glacier instability
during most of the age interval. These are the main
conclusions which are further dealt with in the accompa­
nying paper (Olsen et al., this volume).
(eds.): Late Quaternary Stratigraphy in the Nordic Countries
150,000 - 1 5,000 BP . Striae 34, l 03- 1 08.
Blystad, P. 198 1 : An inter-til! organic sediment of Early or Middle Weich­
selian age from Setesdal, southwestern Norway. Boreas 10,363-367.
Brown, R. H. 1986: t4C depth profiles as indicators of trends of di­
mate and t4C/ 12C ratio. Radiocarbon 28,350-357.
Campbell, C. A., Paul, E.A., Rennie, D. A. & McCallurn, K. J. 1967a:
Factors affecting the accuracy of the carbon dating method of the
analysis to soil humus studies. Soil Science l 04, 8 1 -84.
Campbell, C.A., Paul, E.A., Rennie, D. A. & McCallum, K. J. 1967b:
Applicability of the carbon-dating method of analysis to soil
humus studies. Soil Science 104,217-227.
Chen, Y. & Polach, H. 1986: Validity of 14C ages of carbonates in sedi­
ments. Radiocarbon 28, 4 64 - 4 72.
Acknowledgements. - This paper reviews the results of several years of
regional Quaternary geological mapping, of stratigraphical fieldwork
and numerous AMS-14C dating programmes financed by the Geological
Survey of Norway. T he Research Council of Norway (NFR) has provi­
ded financial support for the dating of some shell material. T he radio­
carbon dating of bulk sediment and mollusc shell samples have been
carried out at the universities of Utrecht (The Netherlands), Trondheim
(Norway) and Uppsala (Sweden), and some U/Th- dates, amino acid
measurements and palaeomagnetic measurements were provided by the
University of Bergen (Norway). John Lowe,Atle Nesje, Goran Possnert
and Wojtec Nemec have refereed the manuscript. Irene Lundqvist has
made the drawings and John Lowe and David Roberts have corrected
the English text. We are grateful to all these institutions and persons for
their valuable assistance. T his paper is a contribution to project 5.3.3 in
the NORPAST (Past Climates of the Norwegian Region) project, a colla­
boration between Norwegian geo- and biological institutions, suppor­
ted by NFR.
Druffel, E. R. M., Honja, S., Griffin, S. & Wong, C. S. 1986: Radiocar­
bon in particulate matter from the eastern sub-arctic Pacific
Ocean: evidence of a source of terrestrial carbon to the deep sea.
Radiocarbon 28, 397-407.
Fisher, R.A. & Yates, F. 1 948: Statistical Tables for Biological,Agricultu­
ral and Medical Research. 3rd ed., Oliver and Boyd, Edinburgh.
Pollestad, B. A. 1 990: Eide 1 320 IV, kvartærgeologisk kart - M 1 :50
000 (med beskrivelse). Norges geologiske undersøkelse.
Pollestad, B. A. 1992: Halsa 1 42 1 III, kvartærgeologisk kart- M 1 :50
000 (med beskrivelse). Norges geologiske undersøkelse.
Fowler, A. J., Gillespie, R. & Hedges, R. E. M.
1 986:
Radiocarbon
dating of sediments. Radiocarbon 28, 44 1 -450.
Gulliksen, S., Birks, H. H., Possnert, G. & Mangerud, J. 1 998: A calen­
dar age estimate of the Younger Dryas - Holocene boundary at
Kråkenes, western Norway. The Holocene 8, 3,249-259.
Gulliksen, S. & Thomsen, M. S. 1992: Examination of background
contamination levels for gas counting and AMS target preparation
in Trondheim. Radiocarbon 34,312-317.
Haldorsen, S., Rappol, M., Sønstegaard, E. & Henningsmoen, K. 1992:
Interstadials and glaciotectonic deformations in Åstdalen, southeas­
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Appendix A
Regional stratigraphic data
LGM
position
Transect
Outer
coastline
Mountai ns,
watershed
..
..
1:
2:
3:
4:
l
5:
l
l
l
l
\
\
\
\
\
6:
l
\
'
'
'
'
7:
'
'
'�-----i��----�
8:
9:
/
,
'
'
,
,
'
'
,
,
,
Younger Dryas
(ice margin position)
Scale:
o
200
400 km
Appendix A- 1 : Stratigraphic
sites projected on to their asso­
ciated transects. For location of
transects, see the main text
(Fig. 1). The numbers refer to
the sites with stratigraphic suc­
cessions which are shown as
simplified lags in Appendix A2. True lengths of transects
according to the map, Fig. l,
are indicated. Note that no
sites from the continental shelf
are included here.
AMS '<IC-Doting of Glacigenic Sediments
NORWEGIAN jOURNAL OF GEOLOGY
F I N N M A R K , e ast
1
2
L e ire lva
Si
l Tra n u c t 1 l
G
S
S kje l lb e k k e n ,
P a s v lk
G
0
.. . t 8 . 4
.
.\
. .
.·
·
Si
S
m ·•·• • •.
G
O
..
·
TR O M S - F IN N M AR K , w est
l Tra n u c t 2 l
X
3
K o m a g e lv a
Si
c.1 26
••
5
'
.17
t
S
G
D
ooo
BP
yr
c. 2 8 0 m a . a . l .
4
Le irh o la/
Lau ks u n d e t •
s
Si
a.s.l.
10
'
'
M?
Si
m
'
1
S a rg e jo h k a
m a.a.l.
34
1 7 .2 k a
83
o
G
..-.....-_ �
30
c===--�
�P.
37
�-
!llf 1 2 3
�
R iver b e d
TRO M S
6
N O R D LA N D
Ø v re Æ r å s v a t n
7
( c o m p o s ite ; c o r i n g )
m
Om
l.
3 4 ..".,,6--'-='=='
a s
l Tra n s e et 3 l
Si S G D
<::>
c::t
..
.··
32
10
..·
31
,-,-"CC..,..�r-
-
C>
S o l u b le
fra c t i o n
&
�
Si S
•
c. 1 02
Q
(:::) ·�
Oo
•
=
•
G D
-
2
m a .s .l .
. ���-:'
'
27 ,580
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8
10
•
�
�
12
te • D . 0 8
20
tra c t l o n
alonea
1 3
R iv e r
1 2
K j e ld d a l
( c o m p o s it e )
N O R D LA N D
,;,
•
A
B o g n eset
Si S G O
1 1
m
8 ·1
l.
75
J- �
·�
Åsm oen
-1
Si S G O
ø2
� ..
-·
c=-=,..."_
12
10
- - . ..
e,
T
c ..
J.
24 8 15 8
/
/
.. .. .. .. . .. .. . .. ..
/
.. .. .. _
·-­
.. .. .. ..
.. ..
c . 5 1 5 m a.a.l.
_ _ ,1 :5
t t
. ..
-r:... ... ..\...
33,200
Si S G O
��i�;o.J•�oi-::;:'� - -- R iv o r b o d ,
w ater l v l
B e d ro c k
.__
ø
om
.. ..
om
. . :::·��::.·:.:::
/::
/
1 4
••) A rof/ca J•ll ndlca,
tra g m
• • • • • •• • • • • •
R is v a s s e lv a ,
S u l itje l m a
G ry t å g a ,
V a l n e s fl o r d
m
1 Tra n s e c t 4 1
1 O
\
·------- ---- ·-····--6
�a" �? M
.. -fii':iiil ..
l n a o l u b le
G ra v e l
Om
a .a . l .
c. 1 4D m
U rd a l e n
M å g e lv a 1 1
? - - ,.. . . .. .. .. .. .. . .. .. .. .. .. . .. .. .1..
C)
33
8
S to r e l v a
9
:
M arine m o ll u 1 c a h e l l
F is k e l a u s e l v a
S1 S G O
1 5
om
A iv l f b e d ,
w ater leve l
H a ttfje l l d a l
Si S G O
.. .. 2
e n ta
H l
.
at M o l l u a c a h e l l ,
m a l n ly frag m e n ts
H
11
H a ttfje l l d a l
i n t e rs t a d ia l l
B e d rock
a
.
H a tlfje l ld a l
i n t e rs ta d la l l l
Trofors
l n t e rs ta d la l
LG M
L
..t
G la c i a l
l Tra n s e c t
5
l
Hl
e
10
M a xlm u m
(exte n s i o n )
AppendixA-2: Examples ofsimplified logs from sites located along all nine transects indicated o n the map, Fig. l, and in Appendix A-l. The
logs are arranged from distal (left) to proximal (right) position and from north to south. Note that dates are shown as ka BP (i. e., time-scale in
14C-yr, except those indicated as TL/OSL dates which are shown in cal yr) along transects l and 2, and as 14C-yr BP along all other transects.
Most 14C-dates are based on the INS fractions (B; and dates without a letter attached), A indicates the SOL fraction.
84
L Olsen et al.
NORWEGIAN JOURNAL OF GEOLOGY
T R Ø N D E LA G
1 6
m
l Tra n sect s i
18
L a n g s t ra n d b a k k e n ,
Vikna
N a m se n
S1 S G D
o m
c . 1 G 4 m a .a . L
2O
0 m
22
B l å fje l l e l v a
(S e c tlon 11)
Si S G O
c.
470
m a .s .l .
S tæ r n e s e t ,
S e lbu
23
F l o ra , S e l b u
24
M Ø R E , coast
25
S k j o n g h e l le r e n
(cave)
lrra n s e c t a i
26
H a m n s u n d h e l l e re n ( c a v e ) ,
c o m p o s il e s t r a t i g ra p h y
m
2 4 400
2 4 ,8 0 0
�
�
S i S ilt
S= S a n d
G
G ra v e t
D = O ia m icton
{ naund
{ Åin und
...... ,
D a ting of b o ne
•)
•
•
B o n e s in u n d e rlying
unit due to
cryoturbalion/
b iotu r b a ti o n
Ham
i n te rs l a d i a l
in leralad ial
'
'
1 000 yr
BP
...... ,
'
'
W eathered rocks
&
b e d ro c k
s w - N O R W AY
27
o m
J æ r e n u p la n d s ( H ø g jæ r e n )
E lg a n e - 1 , 2
...... ,
'
'
'
......
...... ....
'
...... ,
rytd a l ,
Bu dal
G
'
Si S G O
10
20
30
/
ANIS 14C-Dating of Glacigenic Sed iments
NORWEGIAN JOURNAl OF GEOLOGY
O P P LA N D - H E D M A R K
36
F o lld a l
lrra n s e c t ø l
35
G rå b e k k e n , F o lld a l
( G r å m o b e k k e n)
Si S G D
o m
c.
11) U /T h -a g e o f c a l c a re o u s
\
sao
m .. .. . 1 .
c o n c re t i o n
(T h c o n t 8 m i n a t e d )
34
S ta m p e s le t t a ,
L ill e h a m m e r
B e d ro c k
SiS G D
O m
**)
I n f o r m a t l o n fro m
3 0 - 4 0 m d e p th
a f t e r T h o rn e n &
B e rg e rs e n ( 1 9 8 3 )
Leg end
D ia m ic to n ( i n c a v e s )
T i li
G ra v e l
Sand
31
P e lite
S k je b e r g
D e form a ti o n
D ia m ic to n
G ra v e l
O m
Sand
Si
S i lt
E n v i ro n m e n t
M a rine
Te
Te r r e s tria l
D e fo r m a ti o n o r
lc e - rto w d l r e c t l o n
...,__
O e f o r m a t io n o r f a b ric
S tr i a t i o n
N
W�B
B U S K E R U D - VE STFO LD - TE LE M A R K
ITra n s e c t 9 , w est l
s
8
29
28
m
• •
.. i
, ",. ,,. .. ,. , .
N um edal
l
242
234
230
.. .. . .. •
S1 S G O
.. . .. •
_._._ .. .
·-··
238
Rundhaug"
St S G D
.. .. .. · ·
\ ·· ·
.
. �.::
•••
--: 1 -i1!�E, // /
V
p
�-�ii-121J:o
:Ll
:
· -
�
�
"
'
/
/
......
//
2
��� -:..
_r::a.
; '" :
4
�
-
_
��-r··
�
. .. . .
'" �i�
30
.,
.
. ..
. . .. .. .
.
m
.I .L
,328
.. .. .. .
270
Passe bekk,
N u m edal
Si S G O
--
•••
- -
..
�:;-:-� �
- �- - - - - - - - - - -
�
M"
'
250
85
1 000
BP
.. .. .. .. .. ..
..
yr
.. .. .. .. ...
· ·· ····· ·
•
• • • • • • • ••
... _ _ _
•••
.
---..... ....... __ _ _
-
20
. ..
86
.&.,
L
.�. A3
Ttansect L ocati on & reference
no.
l
l
l
2
Komagelva
(Olsen e t al. 1 996)
Le1relva
(Olsen et al. 1 996)
Skjellbekken, Pasvlk
(Olsen, unp ubl. )
3
Lauksundet, Arnøya
(Andreassen et al. 1985)
Le1rhola, Arnøya
(Andreassen et al. I985)
Slettaelva
(Vorren e t al. l98 1 )
Sargejohka
(Olsen 1 988, O lse n
e t a l. 1 996)
Kautokemo
(O lse n 1988, O lse n
& Often 1 996)
Bleik,
(Mø lle r e t . 1 992)
�vre Ærasvatnet
(A lm 1 993)
Ærasvatnet
( T.O . Vorre n e t al.
1988)
Endletvatnet
(K.D. Vorre n 1 978)
Storelva, (irytøya
3
Magelva, Hmnøya
3
�ave, Kjøpsvik
(L auri tze n e t al.
1 996)
Bo neset I & Il
(O sen, in p rep . )
2
2
2
2
3
3
3
3
4
4
4
4
5
5
NORWEGIAN JOURNAl OF GEOlOGY
Olsen et al.
And�r
�
,
(jt åga
(O sen, i n prep.)
Risvasselva
(Olsen, in prep.)
�aves, Rana
(Lauritzen, pers.
comm. 1998)
l1unakJerka
_
(Olsen,
unpubl.)
Fis!<Jauselva
(O lse n 1 997 a)
Str. uni ts
3
4
3
4
3, 5
6
7
8
3, 5
3, 5, 7
8
3, 5, 7
8?
3, 5, 7
8
6
6
6
6
6&7
7
Hat t9elldal &
Slettåsen
(O lse n 1 997 a,
i n p rep. )
Langstrandbakken,
Vik na
�_:;tre Tverråga
(O lse n e t a l.,
in prep.)
Gran, Nor�1
(O lse n e t al.,
i n p rep.)
l)ellelva I & Il
(Olsen e t a l.,
in p rep.)
Sitter, J:ilatanger
��
Sæterelva, Osen
(Olsen & Riiber,in prep.)
14C
B2
!NS, SOL
A
INS, SOL
B2
!NS
B2
!NS
TL
X
OSL
U-ser.
AA ratio
Pal. Mag.
X
Ce-deficiency (0.88)
X
Ce- de f. (0.90)
shell, resed.
X
D2/G
X
X
E/F
Comments
shel l
shell, pollen, resed.
X
x (um t 7)
!NS,
macro
Lake Mungo? ( c. 28 ka BP)
p olle n, palaeosol
3, 5, 7
8
B l /B2
4
6?, 8?
4
D2
D2
B l /F
3.
4
D2/G
SOL, INS,
macro
p olle n, algae
D2/G
SOL, INS
pollen
A/C2
X
3
4
3, 5, 7, 9
lO
3, 5, 7, ':1
lO
4
8, l O
3, 4., 5
6
7
8
9?
5, 7
8?
3, 5, 7
8
6
8
JO?
j, 5, 7, 9
lO
3
4
5
6
7
5
Fa cies
8
3
4
5
6
7
8
3
4
5, 7
8
3
4
5, 7
3, 5, 7
8
9, lO
3
4
5, 6, 7
3
4
5, 7
8
3, 5, 7
8
(A/C2)
su)>aenal
su bae ri al
X
SOL, INS,
macro
X
X
D2/G
X
X
D2
X
B l /B2
INS
B2
!NS
!NS
B2/C I
D l /B2
!NS
X
A
!NS
Bl
B l /E/F
!NS
A
!NS
Dl
Bl/DI/G?
Dl
X
re se d. she ll, di nofl ag.
re se d. she ll, di nofl ag.
she ll, di nofl ag.
X
resed. shell, ce-aet. ( 0.94)
Ce-def., re se d. (0.93)
calc. concretlons
calc. concre ti ons
calc. concre ti ons
�g�
!NS
!NS
!NS
INS
D2/G
bones, calc. concretwn
bones, calc. concre ti on
X
!NS
C0 3
B2/Cl
X
x, JNS
A
su!'aena!
su bae ri al
su bae ri al
NBI
she ll
shell, resed. l umt l O)
X
X
X
A
!
s�el , torammitera
shell
pollen, msects
X
X
V l !B2
D2/G
D2/G
re se d.
X
!NS
!NS
X
re se d. she ll
X
reworked org. (unit 8 )
re se d. org.
p olle n, Ce- de f. (0.93),
p os si ble mari ne algae
pollen, Ce- de f. (0.94)
she ll, re se d. (u ni t 8)
re se d. org. (u ni t lO)
rewo�kea org. (umt 4),
di nofl ag.
rew orke d org. ( u ni t 8 )
shell, resed. l umt 8)
NORWEGIAN JOURNAl OF GEOlOGY
Thmsect Location & reference
no.
7
7
7
Reinåa, Selbu
Stærneset, Selbu
tjrytdal, tjauldal
Str. units
3
4
hiatus
6
7
8
3
Flora, Selbu/Tydal
8
SkJonghelleren
(Larsen et al. 1987)
8
8
8
8
8
9
9
9
19
9
9
9
9
9
19
9
Hamnsundhelleren
(Valen e t al. 1998)
Gamlemsveten
( J. Mangerud, pers.
comm. l981)
K_ortgard�n
(Pollestad 1990)
Skorgenes, Vestnes
(Larsen & Ward
1992)
Kollsete, Sogndal
(Aa & Sønstegaard
1 997, in prep.)
S�jeberg, Halden
(Olsen 1995, 1998)
Herlandsdalen,
Numedalen
Passebek!<,
Numedalen
Kokoberget
(Rokoengen et al.
1993)
Dokka
(Olsen 1995, 1998)
Stampesletta,
Lillehammer
(Olsen 1995, 1998)
Mesna, Llilehammer
(Olsen 1985, 1995,
1 99 8 )
�
Sorperoa, Vinstra
(Ber ersen et al.
1991
Gr�( m��ekken,
, (Thoresen &
Folldal
Bergersen 1983)
OJUpd_alsbekken,
Folldal
(Thoresen &
Bergersen 1983)
Folldal
(Olsen, unpubl.)
14C
B2/Cl?
INS
Ce-def.(0.87)
Bl/Cl?
INS
Ce-def.(0.72)
B2/Cl?
INS
A/B2/Cl?
4
5
6
7
A(Cl)
3
A/B2
A(Cl)
Bl/Cl/Dl
lO
Bl/Cl/Dl
4
2,6
7
A/Cl
subaerial
A(subgl.)
subaerial
A(subgl.)
subaerial
A \SUb&J-)
subaenal
A(subgl.)
subaerial
subaenal
3
8
9
lO
5.
6
7
8
4?
3, 5
"C-Doting of Glacigenic Sediments
Facies
4
5
6
8
9
7
AMS
TL
OSL
U-ser.
AA ratio
Pal. Mag.
IN:>
Comments
reworked org. (umt 4)
Ce-def.(0.83)
reworked org.(unit 6)
INS
INS
INS
INS
INS
INS
INS
INS
IN::.
INS
Ce-def.(0.88)
reworked org.(unit 6)
Ce-def.(0.87)
reworked org.(unit 8)
Ce-def.(0.53)
reworked org.(unit lO)
Ce-def. ( 0.77)
X
X
X
X
X
X
X
bones, speleothems
Lake Mungo(c. 28 ka BP)
LaChamp(c. 40-42 ka BP)
speleothems
bones(from unit 6 & 8)
Lake Mungo(c. 28 ka BP)
X
block held, soll, bulk org.
X
shell, resed. ( umt 6!)
6?
D2/G
lO?
B2/Dl
B2/Dl
4,6?
lO
A
AlF
INS
x;SOL
4
Dl
INS
6
7
8
Bl/Cl
INS
INS
INS
Ce-def.(0.79)
reworked org.(unit 8)
Ce-def. ( 0.36)
4
5,6,7
A(Cl)
INS
INS
Ce-def.(0.77)
resed. org. (unit 8),
Ce-def. ( 0.97)
C2
Cl/C2?
INS
INS
pollen, Ce-def.(0.66),
dinoflag.
4
5
6?
Bl/B2
INS
INS
4?
5, 7
8
3
A(subgl.)
3, 5, 7?
8, 9?
3, 5?
3
5
3
8
3, 5, 6, 7
8
lO
3
3
Cl
A/Cl
Bl
Bl/Cl?
87
X
hiatus between units 6 & lO
pollen
SOL
INS
reworked org.(unit 6),
Ce-def. ( 0.98)
umt 4?, clastlc dyke from
contact between units 3 & 5.
reworked org.(unit 8)
4?
A (subgl.)
!NS
urnt 4!, dasbc dyl<e from
contact between units 3 & 5/7
8
9
8
9?
Bl/Dl?
INS
Ce-def. (0.93)
5, 7
10?
3, 5, 7 .
4?,6
8
3, 5, 7 .
4?,6
8
9?
3, 5, 7?
4?,6
8?
X
subaenal
A
B2/E
x;SOL,INS
X
X
calc. concretions
pollen, calc. concret.
pollen, resed.(unit 8)
A
B2/E
A
B2/E
aeolian sand
INS,SOL,
C03
pollen, resed.(unit 8?),
calc. concretions 9?
AppendixA-3: Localities (sites) with generalized stratigraphic units, sedimentfacies, utilized dating methods and comments on dating, corre­
lation and indicators of climate and environment. For numerical ages ofdates, see the main text, Tables 2, 5 & 6. For location of transects, stra­
tigraphic framework and sediment facies, see the main text, Figs. l & 12 and Table l .
88
L Olsen et al.
NORWEGIAN JOURNAl OF GEOlOGY
Appendix B
Palaeodimatic and palaeoenvironmental data
Numberof
localities
Appendix B-3: (next page)
Magnetic susceptibility from the stratigraphic successions at Sarge­
johka (A), Blåjjellelva (B), Mesna (C), Grytdal (D), Folldal (E),
with all curves plotted in the same diagram (F; after Olsen 1997b).
All curves are based on c. 500 gram samples. Numerical ages are
based on AMS- 14 C dates ofsoils and correlated sediments.
15
10
5
Appendix B-1: Frequency distribution ofpalaeoclimatic and palaeoen­
vironmental indicators used in this study. Most indicators are available
from only one or two stratigraphical units at each site, but shells occur
quite commonly in several units, e.g. at Bogneset, northern Norway
(see Appendix A), where shells occur in 5 different stratigraphic units.
,...,-,'
' '
,
,.
l
'
\
l
l
l
l
l
,'
l
l
l
l
,•
...'
--
,'
',,
l
l
: ...
2·!
.... l
-"'
mm/year
1500 .-------�--�A�
... �
\
l
l
\
\
\
l
l
'
\
1000
500
1
�
5
o
Appendix B-2: Map with location of modern soil and paleosol sites
referred to in this study. Names ofsites are: * = Pasvik (Jour modern
soil sites), 2= Sargejohka, 3= Blåjjellelva, 4= Støren (modern soil site),
5= Grytdal, 6= Folldal, and 7= Mesna (modern and paleosol site).
After Olsen (1997b).
� 400 600
100
[X8- XcJ
X
200
[10-a Sl]
300
[X8- X el
x
400
[1 o-s Sl]
500
600
Appendix B-4: (A) Suggested approximately linear relationship bet­
ween modern rainfall (precipitation) and pedogenic magnetic sus­
ceptibility ofyoung soils from single sites (open eireles) and averaged
value from several sites (closed circle). (B) Similar curve based on
more comprehensive data from-loess soils in the temperate zones
around the world. Inferred from data in Maher & Thompson
(1995). XB and X c are explained in Appendix B-8. After Olsen
(1997b).
-
-
-
150
G5
158
G4
228
G3
234
G2
G1
ma.s.l.
M
W
lntertil
Tdl
Til!
Til!
oediments
lntertill
Till
TiR
o
\
l
(
l
l
l
.
200
G2,
indicated
.
therefore different
curves as
position of the
sediments and
stratigraphic
The two alternatives
include different
24 ka BP.
(11) younger !han
ka, and
of section
(l) c. 25
.
two age alternatives
of the watertain
intertill sediments
Note·
l & 11 represent
100
�
... I"C-AMsl
�37-42 ka BPI
��
�
li
1\
1 \
l \
1
1l
1
�
l
\ l
l 11
l
l
l1
\:'C"..
" .. ...
l \
\
\
P1.2?
P1.
P1 .1
50
_",.,......,
units)
400
l
l '���� l
..
300
250
X (1 o-s Sl
Grytdal, S-Trøndelag
L Paleosols
f
200
units)
er..�\�'\�\' tsl��-F= ::::::::;;;:-::-��l
...,..
Sand
el
��
Sand/grave
·
100
X (10-5 Sl
Sargejohka, Finnmark
260
D
A
..
til!
&
o
P1.1
50
100
X (10-5 Sl-
l
E
F3
i
!:e
*
*
liD
lill
�
l"'
m
F2
F
·--
P1.2
l
_!!lo
...
o
150
units)
��""år> l
l
l
l
l
200
5
4
3
2
l lom
li
l1 :
200
Carbonate
concretions
(disk tonns)
- ...;,;�
*
1983)
& Bergersen
(after Thoresen
Fl= =�
X (1 o-s Sl
100
50
Folldal
� Riwrlevel /normal stand
.
'}. �
Till
[!,
.
·'
:
a� r (/�
18
10
150
units)
Blåfjellelva, Lierne
[�11 '����::1 se- '""l
6 .r_
·.v
B
c
i'P3'
300
units)
=
-
200
400
Paleosol correlated
wilh regional
paleosol Pi
l
l
l#
l
l
Alt.ll
C lJ E
l
1
l
l
l
l
l
l l
l It
l
Alt.lt
l
1
l A
/
�
----. ...-_
...
___
_
[lee- l li
L��::Lhhll o/L .':·-l·-·- · - · - ·
and
cover
lill
ment]
lake
environ*
and
lee­
rover
(lee­
'
�('e :
l
l
E
100
'Pi'
P0 = Modem soil
X (1 o-s Sl 200
100
r
MAGNETIC SUSCEPTIBILITY
113uried �e
x (1 o-s Sl units)
soils ka BP0
50
150
Til!,
oxidised
o
Mesna, Lillehammer
CIO
-o
�
'"
(])
"'
3'
(/l
(])
c...
(\'
<»
Q...
G)
a
ci5'
CC
()"'
5"
o
c
�
�
o
m
G)
o
-n
�
""z
o
c
m
�
G)
5>
z
z
o
90
l.
Olsen et al.
...
l�
...
_
NORWEGIAN jOURNAL OF GEOLOGY
B-5
Location&
Material
Environment
Sargejohka
Gyttja silt
Terrestrial fluvial lacustrine
Algal silt
Marine
reference
%LOI,TC
AP-unident.
-NAF%
Inferred climate,
characteristic vegetatiori
1.2 (LOI)
20-0-80
12-13 (LOI)
5-o-95
Subarctic tundra,treeless vegetation,but dwarf birches occur
frequently. Grasses and sedges
dominate. Wormwood (Artemisia)
reaches 5o/o.
High Arctic climate in the younger
part, Middle to Low Arctic, with
Betula nana,Ericales,Rubiaceae,
etc. in the older part.
Maritime Middle Arctic (Oxyria,
Cyperaceae) to continental Low
Arctic climate (Artemisia, Betula n.)
Organic content;
orTOC
(Olsen et al.
1996}
Transect2
N.Æråsvatnet
(Vorren et al.
1988)
Jransea 3
Bogneset
(Olsen,in prep.)
Hiatus
Algal silt
Silt
Marine
3-4 (LOI)
10-0-90
(preliminary results)
Glaciomarine
Maritime Subarctic conditions,
with scattered trees (Betula sp.).
Transect4
Hattfjelldal
(Olsen,in prep.)
Silt - sand
Gl.fluv. gl.lac.; possible
marine influence
1.4 (TC)
(some resed.
pollen)
(Ce-def., marine
TranseaS
Kollsete
(Aa & Sønstegaard 1997)
Rokoberget
(Rokoengen et
al. 1993}
Silt - sand
Gyttja
Sandysilt
Hiatus
Clayeysilt
Transect9
algae?)
Gl.fluv. - fluv. gl.lac. - lac.,
marine influ.?
Gråbekken
(Gråmobekken;
Thoresen&
Bergersen 1983)
Djupdalsbekken
(Thoresen &
Bergersen 1983)
Folldal
(Olsen,in prep.)
Clay-silt/
sand!
grave!
Glaciolac./
glaciofluv.
Till,with
resed. org.
Resed. material:
Gl.lac. - gl.fluv.
Clay- silt
Transect9
Øv.Astbrua
gravel pit
(Haldorsen et
al. 1992)
Transea9
1.7 (TC)
> 90 o/o NAF,some
resed. or longtrans-
2.7 (LOI)
ported tree-pollen
8.5-31.5-60
3.0(LOI)
13-20-67
3 .0 (LOI)
30 - O-70; some
resed. or longtransported tree-pollen.
10-o-90
Glaciolacustrine
0.2(TOC)
Mainly resed. pollen
Silt - sand
Gl.lac.
0.2 (TOC)
Similar as at Djupdalsbekken
Soil
Subaeril cond.,
weathering and
permafrost
Gl.lac.
No organics found
Plant macrofossils
up to 2 cm length
recorded
(preliminary results)
Subarctic tundra,scattered trees,
decid. & conif. trees,some ferns.
Subarctic - Arctic tundra,dom. by
dwarf birches and grasses. July temp.
at !east 3-4'C lower than today.
Subarctic climate,tundra conditions
combined with seashore vegetation,
dominated by grass.
Similar as the younger part
1.8 (LOI)
Sand!
siltyclay
(preliminary results)
Subarctic tundra,treeless vegetation,but dwarf birches occur
frequently. Grasses and sedges
dominate. Isolated areas with fems.
60-14-26;
(some resed.
pollen)
Gl.lac. - lac.
Gl.lac. gl.marine (Cedef. & dinocvsts l
Gl.lac. gl.marine (?)
33- 33- 33;
40-O -60; mosses
and twigs of Salix
are found
Subarctic climate,open tundra veg.,
scattered birches. Mainly herbs, as
Poaceae,Artemisia ( 6%}, Thalictrum and Cyperaceae.
Slightlydifferent, with more wet
conditions and much more shrubs
than at Gråbekken.
(preliminary results)
Ice-free interval,
assigned age, BP
Sargejohka inter-
stadial;
35 000>45 000 14C-yr
"Andøya interstadial";
18 000-18 500;
19 000-19 500;
and20 00021 000 14C-yr
(Øv.Æråsvatnet ;
Alm,1993)
''Alesund interstadial";
28 000-39 000
l4C-yr
Hattfjelldal interstadialll;
24 000-27 000
14C-yr
HattfjeUdal interstadiall;
30 000->35 000
14C-vr
"Bø interstadial";
c. 43 500>50 000 14C-yr
Rokoberget interstadial, y. part;
c. 34 000 14C-yr
Rokoberget interstadial, o. part;
c. 47 000 14C-vr
Gråmo bekken
interstadial;
c.32 00040 000 14C-yr
Gråmo bekken
interstadial, o. part;
>40 000?
"Hattfjelldal interstadialll ";
24 000 -27 000
(preliminary results)
Gråmobekken
interstadial, o. part;
locality.
Permafrost conditions with ice
wedge formation,proximity to a
glacier in both ends of the interval
>40 000?
Øv. Astbrua inter-
As at the closelying Djupdalsbekken
Open,treeless tundra vegetation
dominated by grass. Dwarf birches
occur commonly. Artemisia up to 12%.
stadial2;
Mid Weichselian.
Øv. Åstbrua inter-
stadiall;
>48 000, probably
early Mid Weichs.
Appendix B-5: Middle and Late Weichselian interstadials (> 15 ka BP) in Norway, with examples ofpalynomorph data (pollen & spores)
expressed as AP versus NAP, and a preliminary interpretation of the climatic conditions..
MN5
NORWEGIAN JOURN1L OF GEOLOGY
Å
..1!.
"CDating of Glacigenic Sediments
91
l
B-6
Dinotlagellates
Samplenos.
1-6/7-94
Operculodinium
centrocap_um
Protoperidinium spp.
(cf. P. conicoides)
Protoperidinium spp.
Spiniferites spp. indet.
Bitectatodinium
tepikiense
Peridinium
faeroense
1-2/10-92
%of normalized average
3B-2/10-92
2
l
4
40.4 o/o
49.8 o/o
11
38
O o/o
2
1.9 o/o
O o/o
O o/o
o
3
dinoflaK. cysts
o
l
97
Sum, dinocysts
7
18.522
385
410
1194
16.761
19.009
5.130
677
8
9
88
27
2
4
3
53
c.36 000
c. 40 000
915
Productivity (no. of dino-
l cysts per gram dry sed.)
Other microfossils:
Foraminifera
Pollen
Spores
90
l
l
l
c. 32 000
100 o/o
9
2
7
c.38 000
8.0 o/o
l
12
49
4
2.180
Sum, markers
14C-ages(shell, from
3A-2/10-92
94
Unidentified
Dry material (grams)
2-2/10-92
Age range:
28,000-
c. 28,000
the same se d. samples)
40,000 BP
Appendix B-6: Palynomorphs, mainly dinoflagellates recorded in the Middle and Late Weichselian sediments at Bogneset, Amøya, North Nor­
way. The number of dinoflagellate cysts and other microfossils are indicated. 14 C-ages ofshells are included.
�,..;.,. B-l
Dinoflagellates
Operculodinium
centrocarpum
Protoperidinium spp.
(cf. P. conicoides)
Protoperidinium spp.
Spiniferites spp. indet.
Bitectotodinium
tepikiense
Peridinium
faeroense
Unidentified
dinojlag. cysts
Sum, dinocysts
Sum, markers
Dry material (grams)
Productivity (no. of dino-
l cysts per gram dry sed.)
Sitter
1-11/7-95
from the same sed.)
Oldra
1-20/7-95
72
4
l
5
Rokoberget
2-27/9-91
Rokoberget
4-11/3-90
Namsen
2-10/10-95
Grytdal
1-15/10-96
2
l
l
2
77
o
9
1220
2
l
4
l
124
87
870
825
1.955
1.455
1.314
9.667
8.499
630
o
78
46
19
Other microfossils:
Foraminifera
Marine algae
Pollen
Spores
14C-ages(INS or shell,
Sitter
1-17/7-95
2
>2
2
some
10.296
2 1.632
l
3
c.21 000
l
l
c.30 000
c.33 000
(shell)
11
27
c. 34 000
8
2
c. 47 000
c. l8 500
12
c.39 500
14C-yr BP
Appendix B-7: Palynomorphs, mainly dinoflagellates recorded in the Middle and Late Weichselian sediments from selected sites in Norway.
The number of dinoflagellate cysts and other microfossils are indicated. 14 C-ages ofsediments (and o ne shell) are included.
92
L Olsen et al.
NORWEGIAN jOURNAL OF GEOLOGY
Appendix 8-8
Site
Pasvik
Støren
L ill ehammer
Sargejohk a
L ierne
L ierne
Grytdal
Grytdal
Folld al
Folld al
Folld al
L illehammer
Soil
pO
pO
pO
pl
pl.l
p1.2
pl.l
p1.2
pl.l
p1.2
p1.3
pl
Period
Holocene
Holocene
Holocene
Sargejohka i. s.
Trofors i. s.
Hattfjelld al i. s. I
Hattfjelld al i. s. Il
Hattfjelld al i. s. I
Trofors i. s.
Gråmobekken i. s.
pre-Gr åm. i. s.
Gråmobekken i. s.
Age, ka BP
lO
XB-XC
Precipitation, mm/year
Palaeodata
Today
250
540 -700
500
9
470
1000- 1300
500- 1000
700-800
9
300
700-850
>35
300
650- 830
300
17- 21
130
280-365
300 -500
30-40
60
125 -175
300-500
24- 28
115
255-320
500- 1000
30-37
65
145 - 190
500- 1000
17- 21
80
175-225
300-500
26 -36
40
90- 125
300 - 500
>36
100
220 -285
300-500
31-36
100
220 -285
700- 800
Appendix B-8: Annual mean precipitation inferred from magnetic susceptibility (X) in paleosols (buried
soils). Although local variations may occur due to variations in topography, parent material, etc., an appro­
ximately linear relationship is assumed between annual mean precipitation and increase in magnetic sus­
ceptibility in different soils (mainly podsols). Basic suppositions are particularly the relationship between
the modern soil and precipitation in Pasvik (4 sites), Støren (l site) and Lillehammer (l site). XB= maxi­
mum X in the soil B horizon, and X c = minimum or average X in the soil C horizon. After Olsen (1997b).