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The theropod that wasn’t: an ornithopod tracksite from
the Helvetiafjellet Formation (Lower Cretaceous)
of Boltodden, Svalbard
JØRN H. HURUM1,2, PATRICK S. DRUCKENMILLER3, ØYVIND HAMMER1*,
HANS A. NAKREM1 & SNORRE OLAUSSEN2
1
Natural History Museum, University of Oslo, PO Box 1172, Blindern, 0318 Oslo, Norway
2
The University Centre in Svalbard (UNIS), PO Box 156, 9171 Longyearbyen, Norway
3
Department of Geosciences, University of Alaska Museum, University of Alaska Fairbanks,
907 Yukon Drive, Fairbanks, AK 99775, USA
*Corresponding author (e-mail: ohammer@nhm.uio.no)
Abstract: We re-examine a Lower Cretaceous dinosaur tracksite at Boltodden in the Kvalvågen
area, on the east coast of Spitsbergen, Svalbard. The tracks are preserved in the Helvetiafjellet Formation (Barremian). A sedimentological characterization of the site indicates that the tracks
formed on a beach/margin of a lake or interdistributary bay, and were preserved by flooding. In
addition to the two imprints already known from the site, we describe at least 34 additional, previously unrecognized pes and manus prints, including one trackway. Two pes morphotypes and
one manus morphotype are recognized. Given the range of morphological variation and the presence of manus tracks, we reinterpret all the prints as being from an ornithopod rather than a theropod, as previously described. We assign the smaller (morphotype A, pes; morphotype B, manus) to
Caririchnium billsarjeanti. The larger (morphotype C, pes) track is assigned to Caririchnium sp.,
differing in size and interdigital angle from the two described ichnospecies C. burreyi and C. billsarjeanti. The occurrence of a quadrupedal, small to medium-sized ornithopod in Svalbard is puzzling, considering the current palaeogeographical reconstructions and that such dinosaur tracks
have mainly been described from Europe but not North America.
Gold Open Access: This article is published under the terms of the CC-BY 3.0 license.
Globally, only a small number of sites preserve
evidence of dinosaurs that lived at polar latitudes.
In the Arctic, skeletal remains and footprints of
Jurassic and Cretaceous dinosaurs are known from
Alaska, Canada, Siberia and Svalbard (Gangloff
2012). The first indisputable evidence that dinosaurs
inhabited the palaeo-Arctic was discovered in 1960
at Festningen, in western Spitsbergen, Svalbard.
These discoveries consist of ornithopod dinosaur
tracks in a Lower Cretaceous (Barremian –Aptian)
sandstone unit of the Helvetiafjellet Formation
(Lapparent 1960, 1962). New tracks were subsequently discovered when the same locality was
revisited in the early 2000s (Hurum et al. 2006).
Other Spitsbergen dinosaur tracks from the same
formation were also reported at Hanaskogdalen
and Ullaberget, in the doctoral work of Ivar Midtkandal (Midtkandal et al. 2007), and at Olsokneset,
described in a popular paper by Smelror et al.
(2006).
In 1976, two tracks were discovered in eastern Spitsbergen in the Helvetiafjellet Formation at
Boltodden in the Kvalvågen area (Fig. 1), which
were described as belonging to a medium-sized
theropod by Edwards et al. (1978). In 2012 and
2014, we revisited the Boltodden site and, during
the course of our field investigations, discovered
numerous other individual footprints and at least
one trackway. Based on pes morphology and the
presence of several manus imprints, we interpret
the new finds, as well as two previously described
tracks, as being made by an ornithopod and not a
theropod. Here, we describe the new tracks and
also provide, for the first time, a detailed palaeoenvironmental context for the site.
Ornithopod ichnotaxonomy has been in a state of
flux. Of large ornithopod ichnotaxa, eight Barremian and nine Aptian ichnogenera have been
described worldwide (Dı́az-Martı́nez et al. 2015).
In their recent review of large ornithopod dinosaur
tracks, Dı́az-Martı́nez et al. (2015) only considered
three genera valid. Iguanodontipus in the Berriasian – Valanginian, Caririchnium in the Berriasian – Albian and, finally, Hadrosauropodus in the
From: Kear, B. P., Lindgren, J., Hurum, J. H., Milàn, J. & Vajda, V. (eds) 2016. Mesozoic Biotas of
Scandinavia and its Arctic Territories. Geological Society, London, Special Publications, 434, 189 –206.
First published online January 6, 2016, http://doi.org/10.1144/SP434.10
# 2016 The Author(s). Published by The Geological Society of London.
Publishing disclaimer: www.geolsoc.org.uk/pub_ethics
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J. H. HURUM ET AL.
dda
(b)
Kva
lhov
(a)
len
190
80°
50
0
100
10
Nordaustlandet
Kvalhovden
79°
344
Ny-Ålesund
Spitsbergen
Hanaskogdalen TS
78° Festningen TS
Longyearbyen
Edgeøya
Ullaberget TS
Boltodden TS
77°
Svalbard
TS
Olsokneset TS
100 km
Boltodden
Sporodden
500 m
Fig. 1. (a) Map of Svalbard showing the study area at Boltodden in the Kvalvågen area and other tracksites (TS)
described from Spitsbergen. Outcrops of the Adventdalen Group (Jurassic– Cretaceous) are shown in a darker shade
(simplified: cf. Dallmann et al. 2002). (b) The Boltodden tracksite and the Kvalhovden stratigraphic reference site.
Aptian– Maastrichtian. From this review, it follows
that all large ornithopod tracks from the Barremian
are of the genus Caririchnium. Four ichnospecies
of Caririchnium are known (Dı́az-Martı́nez et al.
2015): C. magnificum is found in Berrasian –Albianaged deposits of Brazil and Spain; C. kortmeyeri is
only known from the Aptian –Albian of Canada;
C. billsarjeanti is from the Aptian of Switzerland;
and C. lotus is known from the Barremian–Albian
of China and Spain (for a discussion, see Dı́az-Martı́nez et al. 2015). In the Aptian, only one Hadrosauropodus species is known, H. kyoungsookimi,
which is found in Korea.
Geological setting
The Barents Sea platform and its exposed part, Svalbard, are located on the NW corner of the Eurasian
continental plate (Fig. 1). In the Early Cretaceous,
Svalbard was situated at 63 –668 N (Torsvik et al.
2012). The Mesozoic basin fill in the western margin of the Barents Platform was deposited within
the Mesozoic Atlantic rift system (Faleide et al.
2008). In contrast, the Triassic –Lower Cretaceous
basin fill in Svalbard and the western platform
areas were deposited in a subsiding epicontinental
sag basin (Steel & Worsley 1984; Faleide et al.
2008; Worsley 2008; Midtkandal & Nystuen 2009;
Glørstad-Clark et al. 2010). Although these areas
experienced no major extensional or compression
tectonics, the deposition of the Mesozoic basin fill
was controlled by faulting, halokenesis in some
basins, volcanism, and the vertical movement and
tilting of major structural elements (Steel & Worsley 1984; Grogan et al. 1999, 2000; Glørstad-Clark
et al. 2010; Anell et al. 2014; Senger et al. 2014).
The nearly 2 km-thick Middle Jurassic – Early
Cretaceous Adventdalen Group is dominated by
mudstone and heterolithic fine-grained sandstone–
mudstone (Steel & Worsley 1984; Mørk et al.
1999). The Adventdalen Group is subdivided into
four formations (Mørk et al. 1999). The Bathonian–Valanginian Agardhfjellet Formation, like its
offshore counterparts in the Barents Sea, the Fuglen
and Hekkingen formations, was deposited under
conditions with a low sediment supply and periodic
high organic production in an inner- to outer-shelf
environment (Dypvik et al. 1991). The overlying
Valanginian–Hauterivian Rurikfjellet Formation
consists of inner-shelf mudstone passing upwards
into prodelta/lower shoreface/distal delta-front
environments and defines a large-scale regressive
unit (Gjelberg & Steel 1995). The overlying Helvetiafjellet Formation, in which the dinosaur tracks are
found, is a sandstone-dominated Barremian–early
Aptian unit, up to 155 m thick. It was deposited
in fluvial, deltaic, tidal and paralic environments
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AN ORNITHOPOD TRACKSITE IN SVALBARD
(Gjelberg & Steel 1995; Midtkandal & Nystuen
2009). Finally, the uppermost formation of the
group is the Aptian –Albian Carolinefjellet Formation, which is more than 1200 m thick and consists
of shallow shelf sandstones and offshore mudstones
with scattered carbonate beds (Maher et al. 2004).
In the Early Cretaceous, the sediment source
area in Svalbard and the western Barents Sea was
towards the north or NW (Steel & Worsley 1984;
Gjelberg & Steel 1995; Midtkandal & Nystuen
2009). This drainage pattern is linked to the opening
of the Amerasian Basin (Lawver et al. 2002;
Golonka et al. 2003; Dörr et al. 2012) and associated
volcanism (Senger et al. 2014 and references
therein). The sudden influx (i.e. forced regression:
Gjelberg & Steel 1995) of the SE-directed fluviodeltaic Helvetiafjellet Formation above the distal
clastic deposits of the Rurikfjellet Formation is an
obvious response to uplift in the north (Steel &
Worsley 1984; Gjelberg & Steel 1995; Midtkandal
& Nystuen 2009). The presence of bentonites, a
change from mature quartz arenites to the sudden
appearance of lithic or arkosic arenites, interbedded
lava flows and emplacement of intrusive basalts
(Edwards 1979; Maher et al. 2004; Corfu et al.
2013; Senger et al. 2014) reflect volcanism during
deposition of the Helvetiafjellet Formation. Data
from Svalbard and the northern Barents Sea, including Franz Josef Land, suggest short-lived volcanism
around the Barremian–Aptian transition (Corfu
et al. 2013). The erosive boundary at the base of
the Helvetiafjellet Formation atop the underlying
Rurikfjellet Formation is interpreted as a response
to forced regression and incision (Gjelberg & Steel
1995; Midtkandal & Nystuen 2009). No Upper
Cretaceous sediments have yet been recorded in
Svalbard.
Correlation and age of the succession and
dinosaur tracks
Until recently, the Barremian age of the Helvetiafjellet Formation was inferred from stratigraphic
relationships and plant fossils (Grøsfjeld 1992;
Mørk et al. 1999). Apart from plant fragments, macrofossils are scarce. A recent U –Pb zircon date from
a bentonite in a core (well DH 3, Adventdalen)
returned an age of 122.8 + 0.4 Ma (Corfu et al.
2013), which indicates an earliest Aptian age. The
bentonite occurs near the middle part of the Helvetiafjellet Formation. Alternatively, recent palynological studies suggest a Barremian age for the
entire formation, and an early Aptian flooding surface (Fig. 2a) above the Helvetiafjellet Formation
(Midtkandal pers. comm.). The basal part of the
Helvetiafjellet Formation in central Spitsbergen is
a subaerial unconformity surface: that is, a sequence
191
boundary (Midtkandal & Nystuen 2009). The formation thickens towards the south and SE (Parker
1967), without any systematic change in the amount
of marine facies associations (Gjelberg & Steel
1995). This suggests higher accommodation space
to the south and SE. The formation was sourced
from the NW and had the main drainage system orientated towards the SE (Gjelberg & Steel 1995;
Midtkandal & Nystuen 2009). Although biostratigraphic resolution is poor, the interpreted incised
valley fill and aggrading nature of the lower part
of the formation (Nemec 1992; Gjelberg & Steel
1995; Midtkandal & Nystuen 2009) suggest nearchronostratigraphic correlation between eastern
and western Spitsbergen.
The dinosaur tracks at Boltodden are situated
in the lower part of the Helvetiafjellet Formation
(Fig. 2) and therefore are likely to be Barremian in
age or close to the Barremian –Aptian boundary,
similar to most of the other reported dinosaur tracks
from the formation (Heintz 1963; Hurum et al.
2006; Midtkandal et al. 2007).
Facies of the succession with the
dinosaur tracks
The succession at Boltodden that includes the dinosaur tracks is subdivided here into lower and upper
units, informally defined as Unit A and Unit B,
respectively (Fig. 3). Based on correlations with
nearby Kvalhovden, these units belong to the basal
part of the Helvetiafjellet Formation. Units A and
B can also be correlated with the subdivision
given by Onderdonk & Midtkandal (2010), who
subdivided the Helvetiafjellet Formation at Kvalhovden into seven numbered units and interpreted
their facies associations. We also adopt these subdivisions and their general interpretations for the
Boltodden locality. At Kvalhovden, Unit 1 and
Unit 2 consist of displaced slide blocks with fluvial,
braided stream-deposited sandstone overlain by
coastal floodplain deposits, similar to the facies
association that is normally seen at the base of the
formation all over central Spitsbergen (Edwards
1979; Gjelberg & Steel 1995; Midtkandal & Nystuen 2009). Unit 3 is a mixture of collapse scar fill
and delta-front facies associations. Unit 4, with its
mouth bar progradation, can also be seen as small
clinoforms (Fig. 2a). Overlying this, Unit 5 is a
16 m-thick sandstone-dominated section interbedded with thin mudstone and coal beds that is interpreted as being part of progradational delta plain.
Unit 6 is 6 m thick and represents a renewed
mouth bar progradation. The final unit, Unit 7, represents near-shore facies and is the transition to the
overlying conformable open shelf mud deposits of
the Carolinefjellet Formation. Nemec et al. (1988)
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192
J. H. HURUM ET AL.
Fig. 2. (a) Well-exposed outcrop of the Helvetiafjellet Formation along the sea cliff at Kvalhovden, facing east. The
summit is 344 m above sea level. The subdivision of units is from Onderdonk & Midtkandal (2010). (b) Overview
of Boltodden, looking towards the west. The helicopter has landed on the top surface of Unit B. (c) Medium- to
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AN ORNITHOPOD TRACKSITE IN SVALBARD
m
8
193
FS
7
(Kvalhovden Unit 4)
Boltodden Unit B
5
4
coaly shale
FS
East northeastward prograding
mouth bar
3
Legend:
Parallel or slightly
inclined bedding
2
Trough
cross bedding
Coarsening upward unit
Dinosaur foot prints
Roots
(Unit)
(Kvalhovden Unit 2)
Ripples
FS
TS
Boltodden Unit A
Planar
cross bedding
Unit as defined at Kvalhovden
(Onderdonk and Midtkandal 2010)
1
Crevasse channel
reworked in
upper part
Crevasse splay
0
Coastal plain
Helvetiajellet Formation
Barremian/Early Aptian
6
Lower delta plain/Mouth bars/ Embayment
Eastward
prograding
mouth bar
Mud- vf f m c vc
stone Sandstone
Fig. 3. Sedimentological log through the lower middle part of the Lower Cretaceous Helvetiafjellet Formation at
the Boltodden tracksite (see Fig. 2a for the proposed stratigraphic position) showing lithologies, sedimentary and
biogenic structures, and interpretations of depositional environments. TS, transgressive surface; FS, flooding surface.
interpreted the uppermost part of the formation as
barrier bar deposits.
Unit A (probably Unit 2 at Kvalhovden) at
Boltodden is 1.8 m thick and consists of two prominent sandstone beds. The lower sandstone bed (0–
1 m in Fig. 3) consists of a coarsening-upwards succession from mudstone to trough cross-stratified
medium- to coarse-grained sandstone with rootlets
(Fig. 2e). The trough axis varies from 160 –3408
to 170–3508. Decimetre-scale slump scar and convolute bedding are observed laterally. A thin silt –
mudstone bed caps this bed. A sharp basal boundary
is seen in the overlying 70 cm-thick (1–1.8 m in
Fig. 3), box-shaped trough cross-stratified mediumgrained sandstone with an upper horizontal to
slightly inclined laminated part with coarsergrained sandstone. The dinosaur footprints are seen
on the surface of this bed (Figs 3 & 2d). Laterally,
Fig. 2. (Continued) coarse-grained, poorly sorted sandstones with 2D dunes interpreted as an eastwards-prograding
mouth bar. Upper part of the lower coarsening-upwards unit in Unit B (see Fig. 3). (d) Sandstone bed showing
medium-grained cross-stratified sandstone in the lower part passing up into a horizontal laminated, medium- to
coarse-grained upper part. The dinosaur tracks occur at the top surface of this bed. Upper crevasse splay in Unit A. The
stick is 70 cm long. (e) A 1 m-thick coarsening-upwards unit from siltstone at the base to low-angle trough
cross-stratified medium-grained sandstone above with rootlets (arrow), interpreted to be crevasse splay deposits. Lower
crevasse splay in Unit A.
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194
J. H. HURUM ET AL.
the lower sandstone bed in Unit A is downfaulted
with no striation or slickensides, suggesting a largescale slump scar. This interpretation is consistent
with Unit A being laterally equivalent to the
slump blocks in Unit 1 or Unit 2 at Kvalhovden.
Unit A is interpreted as two stacked interdistributary bay deposits, as crevasse splays within a
lower-delta or coastal-plain facies association. The
lower sandstone bed with a defined coarseningupwards trend and rootlets suggest a more distal
crevasse splay, while the sharp-based upper 70 cmthick sandstone bed might suggest a more proximal facies (i.e. crevasse channel: Elliott 1974).
The horizontal to slightly laminated, somewhat
coarser-grained sandstone in the upper part of the
70 cm-thick sandstone bed is here suggested to be
reworked crevasse channel deposits, probably by
sedimentation in the upper flow regime, most likely
on a beach/margin of a lake or interdistributary
bay. The 70 cm-thick sandstone bed is overlain by
a mudstone lamina that defines the base of the first
prograding mouth bar of Unit B (Fig. 2c). We therefore suggest that the dinosaurs were walking on a
beach, probably within an interdistributary bay or
lake, and the tracks were preserved by mud from
a flooding event.
Unit B corresponds to units 3 and 4 at Kvalhovden, where Unit 3 consists of an approximately
10 m-thick mudstone unit followed by a 20 mthick Unit 4, which has three defined coarseningupwards (Cu) units. The thick mudstone Unit 3 at
Kvalhovden is missing at Boltodden, and Unit B
consists only of two well-defined Cu units. The
lower Cu unit (1.7– 3.9 m in Fig. 3) consists of mudstone laminae followed by ripple-laminated finegrained sandstone at the base, then a horizontal
bedded fine-grained sandstone that passes upwards
into large-scale ENE-migrating high-angular planar
cross-stratified medium- to coarse-grained sandstone, occasionally with tangential bottom sets. The
top set has an erosive boundary to the high-angular
planar sets and consists of a more low-angular crossstratified sandstone with a similar grain size. The
lower Cu unit is interpreted to represent mouth bar
progradation. Upper low-angular cross-strata probably result from a shift in drainage: for example, as an
avulsion of the distributary or crevasse channel.
The upper Cu unit (3.9–8.1 m in Fig. 3) has a
nearly 2 m-thick mudstone in the lower part intersected by very-fine-grained ripple-laminated sandstone in the upper part. Coaly mudstone is seen
near the base. The sandstone in the upper 2 m is
fine to medium grained with a low-angular planar
cross-stratification, and is much better sorted than
the first Cu units at 1.7–3.9 m in Figure 3. This
Cu unit is also interpreted as mouth-bar progradation, but thicker mudstone and finer grain size
with better sorting suggest a more distal facies,
probably developed into a deeper standing body of
water. The uppermost 0.4 m of this Cu unit shows
horizontal laminated well-sorted fine-grained sandstone, suggesting that the mouth bar was capped
by a beach. This upper Cu unit is capped by shale
representing a new flooding surface. Apart from
the thick delta-front mudstone of Unit 3 in the profile, presented by Onderdonk & Midtkandal (2010),
the Unit B section at Boltodden follows their interpretation of mouth-bar progradation. Unit 3 varies in
thickness at Kvalhovden from missing to more than
50 m owing to the position of the underlying sliding
blocks. Unit 3 is missing on the intact horst blocks.
Unit B, which here is interpreted as two prograding mouth bars, might also be interpreted as two parasequences (Van Wagoner et al. 1988).
Methods
The tracks were mapped using a combination of
techniques. The coordinates of the tracks were
recorded using a Leica total station (theodolite and
laser range finder). Each track was photographed
with a scale bar and magnetic compass, then outlined with chalk and photographed again. Using
Adobe Illustrator, the photographs were scaled,
rotated, translated and traced to produce the overview map (see later).
For photogrammetry, between 12 and 17 photographs were taken of each track from different positions in azimuth and altitude. The images were
combined into a 3D model using the free photogrammetry software Autodesk 123D Catch, converted to a 3D ASCII point-cloud file in Meshlab,
then imported into the free GIS software QGIS
v. 2.4 (QGIS Development Team 2014). The point
cloud was gridded (interpolated to a regular grid)
to produce an elevation map, and contoured. Additional morphometrics were measured directly in
the field. Past v. 3.02 (Hammer et al. 2001) was
used for reduced major axis (RMA) regression,
and for plotting and analysing compass directions.
Use of size-class terminology follows Marty
(2008) and Dı́az-Martı́nez et al. (2015).
Description of the tracks
A total of 36 clearly defined footprints were documented at the Boltodden site, including two pes
morphotypes, one manus morphotype, and one pes
and manus trackway (Table 1). Medium-sized tridactyl pes prints with associated manus prints are
the most common morphotype, and larger tridactyl
tracks are less common. The prints are preserved
as true tracks with varying degrees of erosion.
Some of the tracks show partial collapse of sand
into the print from along the sides, which influences
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AN ORNITHOPOD TRACKSITE IN SVALBARD
195
Table 1. Details of tracks shown in Figure 5
Track
number
Width
(cm)
Area 1
1
2
3
24
25
36
20
20
33
Pes
Pes
Pes?
?
19
?
20
22
28
20
Pes
Pes
Pes
Pes
Area 2
8
35
41
Pes
9
?
?
Pes?
Area 3
10*
11*
12*
13
14*
15
16
17*
18
19
c. 30
33
31
11
13
25
?
?
28
28
c. 24
30
26
11
12
24
?
?
31
25
Pes
Pes
Pes
Manus
Manus
Pes
Manus
Manus
Pes
Pes
20
21*
22
?
9
c. 36
?
11
c. 30
Manus
Manus
Pes?
23
24
25
?
7
7
?
10
11
Pes?
Manus
Manus
In line with print 18, next in sequence?
missing ‘heel’
Split by crack
Furthest back in trackway?
Questionable track, not included in the
study
Simple oblong shape
Roundish
Reniform
Area 4
26
27
28
28
24
25
26
c. 22
24
Pes
Pes
Pes
Missing ‘right’ toe
Poorly defined
Hard to define toes
4
5
6
7
Length
(cm)
Type
Area 5 – Edwards et al. (1978) tracks
29
28
?
30
29
30
31
12
9
32
28
26
33
26
26
Pes
Pes
Manus
Pes
Pes
34
35
36
Manus
Manus
Manus
11
12
?
10
9
?
Comments
Three distinct claw impressions
Like track 1
Questionable track, not included in the
study
Only two toes visible
Poorly preserved
Only two toes visible
Only two toes visible
Morphotype
A
A
A
A
A
A
Large ornithopod; clear print; part of ‘left’
toe covered
Dimensions uncertain, simple oblong
shape
C
Dimensions uncertain; right foot
Left foot
Right foot
A
A
A
B
B
A
B
B
A
A
Between prints 11 and 12
Approximate measure
Dimensions uncertain
Dimensions uncertain; behind print 10
Good track with clear metatarsal pad
Associated with pes 29 and 32
Clear track
Deep; small but with good claw
impressions; ‘heel’-sliding?
Not as well defined
C
B
B
A
B
B
A
A
A
A
A
B
A
A
B
B
B
*Part of the same trackway.
the overall morphology of the tracks, particularly
the terminal digit shape. No skin impressions were
noted. All of the tracks are preserved on the same
horizon: however, the track-bearing surface is only
partly eroded into view and the central area of the
mapped site (Figs 4 & 5) remains covered by
sandstone (Fig. 4). It is likely that many of the shallow rounded depressions found on the track horizon
are also prints, but they lack clearly defined foot
characteristics such as toes or a triangular shape.
Some of these even show spacing and alignment
expected with a trackway. Their preservation may
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196
J. H. HURUM ET AL.
Fig. 4. Aerial photograph of the tracksite at Boltodden, Kvalvågen. The main trampled areas (A1– A5: see the text)
lie in the same stratigraphic horizon and are separated by an area of relatively smooth sandstone surface in the
centre of the picture.
be a result of erosion or, alternatively, they may represent undertracks (for a discussion of the variation
in ornithopod tracks, see Santos et al. 2012).
Clearly discernable individual prints (mapped
in Fig. 5) occur in five areas: Area 1 lies in the
SW and includes six relatively small pes imprints;
Area 2 is a single large pes imprint along with one
other large poorly defined print at the north end of
the site; Area 3 is in the centre of the study site,
and includes eight larger pes imprints, a number of
relatively small circular manus imprints and a number of indistinct depressions; Area 4 has three pes
imprints; and Area 5 is at the eastern end, and has
four large pes and four manus imprints. The two previously described prints (Edwards et al. 1978) are
represented here by tracks 30 and 32. Widths and
lengths are plotted in Figure 6a. The rose plot of
clearly orientatable tracks (n ¼ 15) is shown in
Figure 6b. The directions are not randomly distributed (Rao’s test for uniform circular distribution,
U ¼ 200, p ¼ 0.002) but bimodal, pointing either
to the north or the south.
Morphotype A
We mapped 19 tridactyl pes tracks of this morphotype. All 19 prints are of similar size and are
wider than long (mean width, 26.9 cm; mean
length, 24.7 cm: see Table 1). The pes tracks in
Area 1 are identical in morphology to those of
areas 3–5. Digit III is consistently longer than digits
II and IV. The individual digits are broadly triangular in outline and symmetrical in shape. The terminal digit morphology varies from U-shaped to
V-shaped. Distinct claw impressions appear present
in track 32, while a more blunt claw impression next
to it in track 30 is more commonly seen (Figs 7 & 8).
However, it is likely that soft-sediment deformation
and erosion influenced the original shape. Phalangeal pads are weakly discernable on some prints.
The interdigital angle varies from 328 to 408, and
total divarication ranges from 628 to 828. The metatarsophalangeal pad impression is usually distinct,
and is posteriorly rounded (Fig. 6, track 12) to
straight (Fig. 6, track 1), or even weakly bilobed
(Fig. 6, track 11).
Morphotype B
We documented 12 manus tracks that are associated
with the pes tracks of morphotype A (e.g. Fig. 6,
track 30 & Fig. 9). (Additional manus prints were
also observed in Area 1 but were not measured or
mapped owing to an incoming tide during the field
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AN ORNITHOPOD TRACKSITE IN SVALBARD
7
197
8
N
9
Area 2
6
19
12
14
5
20
16
11
Area 3
4
18
25
10
23
15
24
13
Area 5
17
3
31
27
28
21
36
34 32
26
2
36
Area 4
29
30
33
35
≈
1
0
6
Total station
Area 1
-1
≈
2
7
4
5
≈
1
-2
≈
-3
≈
≈
-4
-12
-11
-10
-9
-8
-7
-6
-5
-4
-3
≈
-2
-1
0
1
2
3
4
m
Fig. 5. Detailed map of clearly defined footprints at the Boltodden site, with the sea to the south and SW. A
probable trackway is marked in red/grey. Tracks 3 and 22 were excluded from the study (see Table 1).
(a)
N
(b)
35
8
11
12
30
Width
10
19
25
2
1
15
27
26
32
30
18
2
33
28
20
5
n = 15
15
15
20
25
30
Length
35
40
Rao’s U = 200, p = 0.002
Fig. 6. (a) RMA regression of length (L) v. width (W ) of pes tracks. W ¼ 0.75L + 7.8; R 2 ¼ 0.60; p ¼ 0.0005,
n ¼ 16. (b) Rose plot of the directions of orientatable tracks.
4
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198
J. H. HURUM ET AL.
Fig. 7. Photographs of selected tracks, orientated with magnetic north towards the top, except for tracks 1 and 8,
which have north towards the bottom. The arrow for track 30 points to a manus imprint (track 36). Track numbers
are as in Figure 5 and Table 1.
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AN ORNITHOPOD TRACKSITE IN SVALBARD
199
Fig. 8. Photogrammetric elevation maps of the tracks shown in Figure 7. Elevations in cm above the lowermost
point are shown on selected contours. Note the reversal of north for track 1. Track numbers are as in Figure 5 and
Table 1.
visit.) They are round to oval in shape, consistent in
size and are slightly wider than long (mean width,
10.4 cm; mean length, 10.2 cm: see Table 1). Digit
impressions were not observed. The manus tracks
are placed in front of the pes morphotype A tracks,
best seen in tracks 11 + 14 (Figs 5 & 9b), 30 + 36
(Figs 5, 7, 8 & 9a) and 33 + 34 (Fig. 5).
Track morphotype C
We recognize a second pes morphotype based on
track number 8 (Figs 5 & 7), and a similar sized,
but poorly preserved track number 9. Track 8 is
considerably larger, about 25% longer than the
rest of the morphotype A pes imprints at Boltodden,
and is also longer than wide (width, 35 cm; length,
41 cm). Although track 8 appears to have a smaller
total divarication angle than morphotype A, this is in
part due to part of the imprint of ‘left’ toe being covered by sediment, making it appear more narrow
than it really is (Table 1). Morphotype C is similar
in shape to the tracks described from the Festningen
locality by Lapparent (1960, 1962) and Hurum et al.
(2006): however, it is smaller in overall size (the
Festningen tracks average (width × length) 62 ×
63 cm, this single track being (width × length)
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200
J. H. HURUM ET AL.
Fig. 9. (a) Some tracks in Area 5, with track numbers as in Figure 5 and Table 1. Tracks 36 and 31 are interpreted
as manus imprints. The ruler is 63 cm long. (b) A pes (track 11) and manus (track 14) pair in Area 3. (c) Interpreted
manus imprint in Area 3 (track 14). Magnetic north is towards the top. (d) Elevation map of track 14.
35 × 40 cm). The posterior margin of the distal
metatarsal impression is nearly straight as in the
Festningen tracks, referred to as a ‘quadrangular
heel pad’ in Castanera et al. (2013a). The angles
between the toes are about 308, about 58 less than
in the Festningen tracks (Hurum et al. 2006).
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AN ORNITHOPOD TRACKSITE IN SVALBARD
Probable trackway
Pes tracks 10, 11 and 12 (morphotype A) are of similar size, are orientated in the same direction, and are
spaced in a manner consistent with them being part
of a trackway. In addition, manus track 14 is found
in the expected position relative to track 11. Tracks
17 and 21 (manus) may also be part of this trackway.
The distance from track 10 (right pes) to track 12
(right pes) gives a stride length (SL) of 125 cm.
The pace length (PL) is then SL/2 ¼ 62.5 cm. The
mean foot length (FL) of tracks 11 and 12 is
28 cm, giving a PL/FL ratio of 2.3.
Discussion
Barremian climate of Svalbard
The succession with the dinosaur tracks is part of the
Helvetiafjellet Formation in central Spitsbergen,
interpreted as an overall paralic deposit (Midtkandal
& Nystuen 2009). Identified facies associations
include braided stream, distributary channels, interdistributary bay, delta/coastal plain with coal beds,
mouth bar, barrier bar, tidal estuary, lagoon and
transgressive shoreline (Steel & Worsley 1984;
Nemec et al. 1988; Gjelberg & Steel 1995; Midtkandal & Nystuen 2009).
The Early Cretaceous has been regarded as one
of the warmest periods in the Phanerozoic. However, being situated at 63 –668 N latitude (Torsvik
et al. 2012), the Early Cretaceous climate of Svalbard is suggested to be seasonally variable. Based
on studies from the Lower Cretaceous in the Sverdrup Basin, which was then situated further north
of Svalbard (i.e. c. 758 N: Wynne et al. 1988; Torsvik et al. 2012), the climate changed from semi-arid
and seasonal in the Late Jurassic and Valanginian to
humid and cool in the Late Valanginian (Galloway
et al. 2013). The common occurrence of glendolites
(calcite pseudomorphs of ikaite, a hydrated calcium
carbonate phase associated with near-freezing water
temperatures: Selleck et al. 2007) in some of the
units in the Rurikfjellet and Carolinefjellet formations (Mørk et al. 1999; Price & Nunn 2010; Dypvik
& Zakharov 2012) also suggests a relatively cool
climate in the Early Cretaceous of Svalbard.
However, there is also evidence for a warm climatic regime during deposition of the Helvetiafjellet Formation. The flora known for the formation
includes gingkos and conifers (Heintz 1963; Harland & Kelly 1997), and occasionally thick bituminous coal seams with underlying seatearth (fireclay)
with rootlets also occur in the Helvetiafjellet Formation (Nemec 1992). Together with abundant fossilized tree trunks and dinosaurs (ornithopod tracks)
in Svalbard (Hurum et al. 2006), this suggest a wellvegetated and humid environment. In addition, the
201
common occurrence of kaolinite as both a porefilling mineral and in kaolinite beds may point to a
warm or, at least, seasonally warm climate. The
lower part of the Helvetiafjellet Formation sandstone consists of white kaolinitic quartz arenites,
shifting to grey to greenish lithic arenites in the
upper part. This shift in composition is related to
the influx of volcanic fragments (Edwards 1979).
On Kong Karls Land, the sandstones of the Helvetiafjellet Formation are unconsolidated and have
probably never exceeded a burial temperature of
60 –708C (Larssen et al. 1993). Here, a claystone
bed within arkosic arenite is dominated by kaolinite,
suggesting soil profile processes that have leached
unstable minerals. Although kaolinite soil profiles
are often associated with warm climates, recent
work has shown that kaolinite soil profiles probably
also form in cooler temperate climates with seasonal
growth during warm months (Sheldon & Tabor
2009). Although the kaolinite bed in Kong Karls
Land does not represent a complete preserved kaolinitic soil profile typically associated with a tropical
climate, it might suggest at least a seasonally warm
climate during deposition of the Helvetiafjellet
Formation in Svalbard. Finally, we have plotted
occurrences of Cretaceous coal directly from the
database of Boucot et al. 2013 (Fig. 10) that indicate
a particularly high latitude for the Cretaceous northern wet belt coal, stretching to 77–788 N instead of
the more typical 608 N.
The tracks
Edwards et al. (1978, pp. 940– 941) described two
of the tracks at the locality (tracks 30 and 32 in
this paper) as ‘apparently made by a large carnosaurian dinosaur’ and attributed them to the Middle
Jurassic theropod Megalosaurus due to the presence
of sharp claw impressions. Thulborn (1990, pl. 10)
refigured one track (our track number 32) and
described it as:
A theropod footprint attributed to Megalosaurus, in the
Lower Cretaceous of Kvalvågen, Spitsbergen; about
23 cm wide. This is an unusually broad and short
print, but has unmistakable indications of the claws.
Thulborn (1990) further suggested a list of possible
characters discerning ornithopod and theropod
tracks, noting that theropod footprints tend to be
longer than wide, have V-shaped tapering digits,
possess narrow toe and claw prints, less widely
divergent digits than typical ornithopods, and a
V-shaped rear half of the footprint.
In considering the Boltodden tracks, most characteristics of the pes indicate that they are, in fact,
made by an ornithopod. In particular, the tracks are
consistently wider than long, and the digit impressions are relatively broad and short when compared
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202
J. H. HURUM ET AL.
Fig. 10. Occurrences of coal in the Early Cretaceous, based on Boucot et al. (2013). FJL, Franz Josef Land; SVB,
Sverdrup Basin.
to most unequivocal theropod tracks. Also, where
preserved, the metatarsophalangeal joint impressions are broadly rounded and not narrowly Vshaped, as noted by Thulborn (1990). The primary
reason that the Boltodden prints had been attributed
to a theropod rest solely on the presence of sharp
claw impressions (Edwards et al. 1978). We interpret this morphology to be a taphonomic artefact
of soft-sediment deformation, whereby watersaturated sand partially collapsed at the tracking surface, resulting in distortion at the distal end of the
digits and producing an artificially narrow toe outline, including a sharp claw-like morphology. The
high moisture content of the sediment is inferred
from the depositional setting, which was probably
a beach (see earlier). As noted elsewhere (Milan &
Bromley 2006; Jackson et al. 2009; Razzolini
et al. 2014), collapse and flow of sediment with a
high moisture content can significantly alter track
morphology, resulting in erroneous conclusions
regarding the trackmaker and other interpretations
based on morphology.
Castanera et al. (2013b) recently discussed the
problems of discerning ornithopod and theropod
tracks, noting that the association of pes prints
with manus prints (which are easily overlooked)
can also provide important evidence in support of
an ornithopod trackmaker. Our field investigations
indicate that many of the morphotype A tracks,
including those described in Edwards et al. (1978),
are also associated with small, round to oval prints
that we interpret as manus tracks. Collectively,
overall print morphology and the presence of
manus prints provide unequivocal evidence that
the main Boltodden trackmaker was a mediumsized ornithopod. Finally, we do not believe that a
subset of prints could be from a theropod given
that all morphotype A prints are morphologically
consistent and lack any indication of a posteriomedially orientated hallux. The Boltodden site provides yet another example of mistaken identity,
where ornithopod tracks had previously been misinterpreted as having been made by theropods (Romilio & Salisbury 2011; Castanera et al. 2013b).
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AN ORNITHOPOD TRACKSITE IN SVALBARD
The Boltodden tracks of morphotype A are all
made by a small to medium-sized ornithopod that
was at least facultatively quadrupedal. A number
of different ornithopod ichnotaxa are known from
the Cretaceous (Lockley et al. 2014; but see Dı́azMartı́nez et al. 2015). The Boltodden tracks are
similar to those attributed to Caririchnium Leonardi, 1984, a quadrupedal trackway of comparable
size known from numerous sites globally, including
the Lower Cretaceous of Brazil, Colorado, the USA
(Thulborn 1990, fig 6.32d) and several localities in
Europe (Castanera et al. 2013a, b; Garcı́a-Ortiz &
Pérez-Lorente 2014 and references therein). The
Boltodden tracks are most similar to Iguanodontipus Sarjeant et al., 1998, and particularly I. billsarjeanti Meyer & Thuring, 2003 from the Aptian of
Switzerland, now referred to Caririchnium billsarjeanti (Dı́az-Martı́nez et al. 2015). The ichnospecies
C. billsarjeanti has a tridactyl pes wider than long,
with a length of 28 –35 cm, and an interdigital angle
of 30 –358, very similar to the Boltodden prints. The
pace length of 62.5 cm is also consistent with C.
billsarjeanti (62 –72 cm: Meyer & Thuring 2003),
partly strengthening the interpretation of tracks
10– 12 as a trackway. In addition, the manus prints
associated with C. billsarjeanti are similar in size,
morphology and placement, being located anterior
to the apices between digits III and IV (Meyer &
Thuring 2003). Lockley & Wright (2001) discussed
the position of the manus relative to the pes in quadrupedal ornithopod tracks and concluded that this
varies even within trackways. This is also true for
the Boltodden tracks. We therefore refrain from
categorizing left and right tracks in our material.
The main difference noted between C. billsarjeanti
and the Boltodden prints is seen in the more pronounced claw impressions of some of the latter:
however, this is interpreted as a taphonomic artefact, as discussed above. Caririchnium kortmeyeri
(Amblydactylus kortmeyeri Currie & Sarjeant,
1979) have pointed digits that may be interpreted
as claw impressions, but no associated manus tracks.
Castanera et al. (2013b, p. 11) recently noted
that ‘quadrupedality inferred from trackways is
scarcely documented for medium-sized ornithopods
in the Late Jurassic –Early Cretaceous worldwide,
except in Europe’. This makes the Boltodden tracks
very interesting from both a locomotory and palaeobiogeographical perspective. First, the tracks
establish that facultative quadrupedality was present in these small to medium-sized ornithopods,
which have an estimated hip height of approximately 1 m (morphotype A), following Alexander
(1976). Secondly, the tracksites were located at
between 638 and 668 N in the Barremian when Svalbard was most probably isolated from mainland
Europe and possibly Greenland/North America
(Hurum et al. 2006; Torsvik et al. 2012). The
203
presence of dinosaurs in Svalbard at this time suggests at least intermittent terrestrial connectivity
between Svalbard and a larger landmass to the
west (Greenland/North America). That the tracks
are clearly from a quadrupedal ornithopod, and
thus more like European forms, is puzzling. One
possibility is that quadrupedal ornithopods were
more widespread across Greenland/North America
at this time than recognized but poorly represented
by body or trace fossils, which seems likely to be
at least partly true. Alternatively, a potential route
of terrestrial connectivity that is not currently recognized by tectonic and palaeogeographical reconstructions permitted dispersal between Svalbard
and Europe. Either way, the presence of dinosaur
footprints in Svalbard indicates that they become
widely distributed at high palaeolatitudes during
the Cretaceous.
The large pes track of morphotype C (number 8
on Figs 5 & 7) is smaller than the tracks from the
same horizon on the Festningen locality on the western side of Svalbard, but considerably larger than
the other tracks at the Boltodden locality. In a
review of iguanodontid tracks, Sarjeant et al. (1998,
p. 200) stated that the ornithopod tracks from Festningen are morphologically distinct from other
iguanodontid tracks but were made by a similar,
albeit different, trackmaker. They diagnosed Iguanodontipus as:
Tridactyl pedal imprints of a dinosaur, semidigitigrade,
all three digits being of similar length. Central digit
(III) directed forward and approximating to an equilateral triangle in shape. Digits II and IV directed almost
laterally; they are somewhat less broad and have the
form of isosceles triangles with rounded to sub-acute
distal ends. Posterior of sole smoothly curved or very
slightly flattened. Claws not defined. Trackway narrow: stride long.
Dı́az-Martı́nez et al. (2015, p. 23) left only the species Iguanodontipus burreyi in the genus and
emended the diagnosis to:
Tracks belonging to Iguanodontipodidae with a small
heel impression that is rounded, centered and narrow
(as wide as the width of the proximal part of the digit
III impression); long, narrow digit impressions with
sharp distal ends.
This fits well with the morphology of the morphotype C track, but measurements of Iguanodontipus
burreyi indicate that the length and width of the
tracks varies from 23 to 30 cm and the interdigital
angles from 358 to 508 (Sarjeant et al. 1998).
The Boltodden track morphotype C is larger than
this (35 × 41 cm), and has a narrower interdigital
divarication (308). This suggests two alternatives.
It may represent a juvenile individual of the ichnotaxon described from Festningen (Hurum et al.
2006) or indicate the presence of a new ornithopod
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204
J. H. HURUM ET AL.
taxon in the Barremian of Svalbard. Given that we
currently have only a single well-preserved track
and that it seems unlikely to have multiple coexisting species of medium-sized ornithopods in
the Barremian of Svalbard, we refrain from naming
a new taxon and, instead, refer this to Caririchnium
sp., which is currently the only valid ornithopod ichnogenus recognized during this interval (Dı́az-Martı́nez et al. 2015).
Conclusion
The Barremian tracksite at Boltodden, Svalbard
presents an important high-latitude dinosaur tracksite, which we reinterpret as made by ornithopods
rather than a theropod, as previously described. The
ornithopod prints were formed while the animals
walked along a lake margin or on a beach within
an interdistributary bay. Mud deposited from river
flooding or raised water/sea level preserved the
tracks. We assign the tracks of the smaller (A, B)
morphotype to to Caririchnium billsarjeanti and
refer the larger morphotype (C) to Caririchnium sp.
Both morphotypes appear to be morphologically
distinct from the tracks at Festningen, in western
Spitsbergen. The occurrence of a quadrupedal,
small to medium-sized ornithopod in Svalbard is
puzzling, considering the palaeogeography and that
such dinosaur tracks have mainly been described
from Europe, but not from North America.
This study was funded by LoCrA (Lower Cretaceous clastic wedges, an under-explored play in the Arctic), initiated
by the University of Stavanger and the University Centre in
Svalbard (UNIS) in cooperation with the University of
Bergen; the University of Nebraska at Omaha; the University of Texas at Austin, the Institute for Geophysics; the
Lomonosov Moscow State University; the University of
Oslo; and the University of Copenhagen.
We are grateful to reviewers Anthony Romilio and
Diego Castanera for useful comments.
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