GEOLOGICA CARPATHICA, OCTOBER 2008, 59, 5, 461—487
www.geologicacarpathica.sk
Paleoenvironment of the Early Badenian (Middle Miocene)
in the southern Vienna Basin (Austria) – multivariate
analysis of the Baden-Sooss section
JOHANN HOHENEGGER
1
, NILS ANDERSEN
2
, KATALIN BÁLDI
1
, STJEPAN ĆORIĆ
3
,
PETER PERVESLER
1
, CHRISTIAN RUPP
3
and MICHAEL WAGREICH
4
1
Department of Paleontology, University of Vienna, Althanstrasse 14, A-1090 Vienna, Austria; johann.hohenegger@univie.ac.at
2
Leibniz Laboratory for Radiometric Dating and Stable Isotope Research, Christian-Albrechts-University, D-24118 Kiel, Germany
3
Geological Survey of Austria, Neulinggasse 38, A-1030 Vienna, Austria
4
Department of Geodynamics and Sedimentology, University of Vienna, Althanstrasse 14, A-1090 Vienna, Austria
(Manuscript received December 13, 2007; accepted in revised form June 12, 2008)
Abstract: Multivariate latent structure methods were used to determine environmental factors that influenced the distribu-
tion of magnetic susceptibility, calcium carbonate, organic carbon, stable oxygen and carbon isotopes, ichnofossils, calcar-
eous nannoplankton and benthic as well as planktonic foraminifera in the 102 m long section of late Early Badenian age
(Middle Miocene, Upper Lagenidae Zone) cored at Baden-Sooss for scientific investigations. Five factors ‘temperature’,
‘eutrophication’, ‘water stratification’, ‘oxygen-rich particulate organic material’ and ‘surface productivity’ controlled the
variables to different degrees. The tectonically unaffected deeper part of the section (38 m to 102 m) started with a short
warm period possibly characterizing environmental conditions of the preceding Lower Lagenidae Zone. A long ‘warm’
period from 78 m to 92 m followed the first temperature decline between 92 m and 100 m. Increased terrestrial input
caused by intensified weathering through seasonal changes characterized warm periods. The subsequent long ‘colder’
period between 49 m and 78 m is distinguished by increased oxygen depletion, mixed water masses and dysoxic bottom
conditions preferring carbonate and organic carbon production as well as inbenthic foraminifera. The following ‘warm’
period with decreasing oxygen depletion is abruptly finished between 36 m and 38 m in the sedimentary record through
tectonic deformation. In the following period, ‘colder’ water conditions dominated interrupted by short warmer intervals,
finally tending to warmer water at the top of the cored interval (8 m to 16 m). Although intermediate temperatures pre-
vailed in the youngest period, oxygen depletion remained relatively high after obtaining the maximum in the previous
period. This increase in oxygen depletion toward the top of the section is reflected in rising
δ
13
C isotope values together
with decreasing temperatures, thus following – just after the Miocene ‘Monterey’ excursion – the slight global cooling
trend between —14.7 and —13.9 Myr preceding the main Middle Miocene cooling period.
Key words: Miocene, Badenian, Vienna Basin, paleoenvironment, paleoclimate, multivariate analyses.
Introduction
A core was drilled for scientific investigations at the Badenian
stratotype locality (Cicha et al. 1975; Papp & Steininger
1978), the former clay pit Baden-Sooss (Fig. 1), to shed light
on the stratigraphic position and environmental conditions
during sedimentation of the Middle Miocene “Badener Tegel”
(Baden Group) using a multidisciplinary approach. Based on
corresponding cycles in magnetic susceptibility, organic car-
bon and calcium carbonate content, correlation with orbital
cycles was possible. Using the absence of the index fossil
Helicosphaera waltrans and presence of the planktonic fora-
minifer Orbulina universa as stratigraphic tie points (Abdul
Aziz et al. 2008), cross-correlations between orbital cycles
and cycles in magnetic susceptibility enable precise dating of
the section between —14.379 ± 0.001 and —14.142 ± 0.009 Myr
(Hohenegger et al. 2008). The influence of environmental pa-
rameters obtained by investigations of magnetic susceptibility
(Selge 2005), sedimentology, clay mineralogy and geochem-
istry (Wagreich et al. 2008), ichnology (Pervesler et al. 2008),
paleoecology of benthic (Báldi & Hohenegger 2008) and
planktonic foraminifera (Rupp & Hohenegger 2008) together
with calcareous nannoplankton (Ćorić & Hohenegger 2008) is
summarized and inter-correlated. Precise dating allows corre-
lation with global climate changes (Zachos et al. 2001; Hol-
bourn et al. 2007).
Environmental indicators
Several parameters dependent on environmental gradients
could be defined in the Baden-Sooss section by detailed inves-
tigations. All these parameters were included in a comprehen-
sive analysis to reconstruct the paleoenvironment during
deposition of sediments in the Badenian Sea at the western
border of the southern Vienna Basin. The following environ-
mental variables were related to depth (age) in the section:
Anisotropic magnetic susceptibility (AMS)
Magnetic susceptibility was measured along the whole
cored section at 5 cm spacing, resulting in 1797 measurements
462
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
(for details see Selge 2005; Wagreich et al. 2008). These mea-
surements displayed significant periodic variations that could
be decomposed into a set of four significant cycles with period
lengths of 40 m, 23 m, 14 m and 11 m for the tectonically un-
affected part of the section from 40 m to 102 m (Hohenegger
et al. 2008: fig. 5). The high negative correlation with CaCO
3
and organic carbon (Hohenegger et al. 2008: table 1) together
with similar period numbers and lengths of the three variables
(Hohenegger et al. 2008: fig. 5) led to the idea of comparing
the four significant period lengths with orbital cycles. Correla-
tion between different sequences of orbital cycles and the
three cycles of magnetic susceptibility, CaCO
3
and organic
carbon at Baden-Sooss indicates that they correspond with the
100 kyr eccentricity, 41 kyr obliquity, 23 kyr and 19 kyr preces-
sion cycles (Hohenegger et al. 2008: table 3).
The major variations of magnetic susceptibility can be
found through combining the four decomposed sinusoidal
functions into a compound function (Fig. 2a). This function
shows a clear differentiation of the upper (6 m to 40 m) from
the deeper part of the cored section (40 m to 102 m). Period
lengths are shorter in the upper part and distances between
the three main peaks differ significantly (Fig. 2a). Shorter
periods in the upper part of the sequence are caused by the
loss of section through tectonic deformation recognizable as
small-scale fault planes (Wagreich et al. 2008). The three
main peaks in magnetic susceptibility are equated with orbit-
al 100 kyr eccentricity peaks. They result from a higher input
of detrital magnetic components, i.e. hematite, through sea-
sonal differences, caused by increased eccentricity and
obliquity influencing solar radiation (insolation), precipita-
tion, evaporation and wind systems (Selge 2005). Although
oscillations in magnetic susceptibility are intensified in the
upper part of the section showing higher amplitudes
(Fig. 2a), the mean level is significantly lower than in the
deeper part of the section (Hohenegger et al. 2008: table 2).
This can be interpreted as a generally higher, but less vary-
ing sedimentary input in the deeper part of the section. While
the rate of sedimentary input was on average lower in the up-
per part of the section, it was intensive during periods of de-
tritus input (Fig. 2a). The lower mean susceptibility is also
documented in the significant correlation with age as ex-
pressed by depth in the cored sequence (Table 1).
Calcium carbonate
Percentages of CaCO
3
were measured in the tectonically
unaffected deeper part of the section (40 m to 102 m) in
20 cm intervals, resulting in 310 measurements (Khatun
2007). Twenty-two overview samples where taken including
six samples for the upper part of the section between 6 m and
40 m (Fig. 2b). Oscillations in the deeper part of the section
could be decomposed into four sinusoidal functions with pe-
riod lengths identical to those of magnetic susceptibility and
organic carbon (Fig. 2b). The high negative correlation be-
Fig. 1. a – Tectonic map of
the Vienna Basin and location
of the studied borehole Baden-
Sooss. b – Schematic sedimen-
tological log of the borehole
Baden-Sooss (after Hohenegger
et al. 2008).
463
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
Fig. 2. a – Magnetic susceptibility, fit by sinusoidal regression based on power spectra. b – Percentages of calcium carbonate, fit by sinuso-
idal regression based on power spectra. c – Percentages of organic carbon, fit by sinusoidal regression based on power spectra. d – Estimated
water depth, 95% confidence intervals, fit by linear regression and by sinusoidal regression based on power spectra. Grey and white bands indi-
cate periods obtained by moving averages of magnetic susceptibility.
tween calcium carbonate and magnetic susceptibility sup-
ports the idea of an opposite reaction to environmental con-
ditions (Hohenegger et al. 2008). During periods of high
detrital sedimentary input expressed in peaks of magnetic
susceptibility, calcium carbonate content as a result of shell
production (mainly planktonic and benthic foraminifera and
calcareous nannoplankton) is low (Wagreich et al. 2008).
Productivity of planktonic organisms is high in colder water
indicating that peaks in calcium carbonate coincide with
minima in orbital eccentricity and obliquity (Hohenegger et
al. 2008). Although calcium carbonate content varies oppo-
sitely to magnetic susceptibility intensity, it also shows a
significant decrease from the lower to the upper part of the
section (Table 1).
Organic carbon
The sample set used for the investigation of calcium carbon-
ate was also used to measure percentages of organic carbon
(Khatun 2007). The organic carbon content is low throughout
the entire section (Fig. 2c) decreasing upwards (Table 1;
Wagreich et al. 2008). Periods of oscillation coincide between
organic carbon and CaCO
3
(Fig. 2c) but with a significant 3.2 m
phase difference to CaCO
3
(Hohenegger et al. 2008: fig. 6). Al-
though correlation with magnetic susceptibility is negative, it is
less significant than CaCO
3
due to the later onset of periods, e.g.
phase differences (Hohenegger et al. 2008: table 1). Similar to
magnetic susceptibility and CaCO
3
the decrease of organic car-
bon content with time is significant (Table 1).
464
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
cor
e de
pth
magn
etic
suscep
tibi
lit
y
calciu
m carb
onat
e
organi
c carb
on
hydr
oge
n inde
x
δ
13
C G
lob
igerin
oides
trilo
bus
δ
18
O G
lob
igerin
oides
trilo
bus
δ
13
C G
lo
big
erin
a
bull
oides
δ
18
O G
lo
big
erin
a
bull
oides
δ
13
C Ho
eglu
ndin
a
elegan
s
δ
18
O Hoe
glu
ndin
a
elegan
s
δ
13
C U
vig
erin
a
grill
i
δ
18
O Uv
ig
eri
na
grilli
∆δ
18
O
c
o
rre
la
ti
on
1
–0
.156
–0
.1
59
–0
.275
–0
.387
0.
26
2 0
.17
9 0.
20
7
0.
51
7
0.
77
9
0.
46
7
–0
.3
93
0.
31
5
–0
.1
25
si
gn
if
ic
a
n
ce
0.
00
0
0.
0
0
2
0.
00
0
0.
00
4
0.
01
4
0
.06
7 0.
15
0
0
.00
3
0.
00
0
0
.00
0
0.
02
6 0.
06
3
0.
15
4
co
re
d
ept
h
num
be
r 47
9
47
8
31
6
31
6
47
71 7
1
27
27
77
73
25 25
69
c
o
rre
la
ti
on
–0
.1
56
1
–0
.4
57
–0
.2
36
–0
.1
86
0.
01
3
–0
.259
–
0.
083
–
0.
309
–0
.442
–0.
35
5
–0
.4
13
0.
10
0
–0
.0
48
si
gn
if
ic
a
n
ce
0.
0
0
0
0.
0
0
0
0.
00
0 0.
10
6
0.
45
7
0
.01
5 0.
34
1
0
.05
8
0.
00
0
0
.00
1
0.
02
0 0.
31
6
0.
34
6
m
agn
et
ic
su
sc
ep
ti
b
il
it
y
num
be
r
47
8
47
8
31
6
31
6 47
71
7
1
27
2
7
77
73
25 25
69
c
o
rre
la
ti
on
–0
.1
59
–0
.457
1
0.
40
7 0.
01
3
–0
.0
16
0.
25
8 –0
.0
28
–0.
44
6
0.
17
2
0.
26
3
0.
90
7 –0
.5
38
0.
12
3
si
gn
if
ic
a
n
ce
0.
0
0
2
0.
00
0
0.
00
0 0.
46
5
0.
45
5
0
.03
4 0.
47
9
0
.18
8
0.
10
7
0
.02
8
0.
00
6 0.
13
5
0.
19
8
calciu
m
c
arb
on
at
e
num
be
r
31
6
31
6 31
6
31
6 47
51
5
1
6
6
54
53
6 6
50
c
o
rre
la
ti
on
–0
.2
75
–0
.236
0.
40
7
1
0.
38
7
0.
02
7
0.
02
5 –0
.7
20
–0.
47
8
0.
03
4
0.
28
8 0.
01
7
–0
.3
63
–0
.275
si
gn
if
ic
a
n
ce
0.
0
0
0
0.
00
0
0.
0
0
0
0.
00
4
0.
42
5
0
.43
0 0.
05
3
0
.16
9
0.
40
3
0
.01
8 0.
48
7
0.
24
0
0.
02
7
organ
ic
carb
on
num
be
r
31
6
31
6
31
6
31
6
47
51
5
1
6
6
54
5
3
6
6
50
c
o
rre
la
ti
on
–0
.3
87
–0
.1
86
0.
01
3
0.
38
7
1
0.
08
7 0
.08
9
–
–
–0
.1
34
0
.09
9
–
–
0.
03
2
si
gn
if
ic
a
n
ce
0.
0
0
4 0.
10
6
0.
4
6
5
0.
00
4
0.
29
1
0
.28
8
–
–
0.
19
4
0
.26
2
–
–
0.
42
2
hy
dr
og
en
in
de
x
num
be
r
47 47
47
47 47
42 4
2
0
0
44
4
4
0
0
41
c
o
rre
la
ti
on
0.
26
2 0.
01
3
–0
.0
16
0.
02
7
0.
08
7
1
0.
10
3
0.
55
9 0
.11
4
0.
30
5
0.
39
0 0.
24
4
0.
69
6 –0
.1
48
si
gn
if
ic
a
n
ce
0.
0
1
4 0.
45
7
0.
4
5
5 0.
42
5
0.
29
1
0
.19
6
0.
00
3
0
.30
3
0.
00
6
0
.00
1 0.
13
7
0.
00
0 0.
11
3
δ
13
C
Glob
ig
e
ri
n
o
ide
s
tr
il
obu
s
num
be
r
71
71 51
51 42
71
7
1
23 2
3
68
6
7
22
22
69
c
o
rre
la
ti
on
0.
17
9
–0
.259
0.
25
8
0.
02
5 0.
08
9 0.
10
3
1
0.
46
7
0.
53
4
0.
49
0
0.
57
6
0.
82
3
0.
66
2
0.
59
3
si
g
n
if
ic
anc
e 0.
0
6
7
0.
01
5
0.
0
3
4
0.
43
0 0.
28
8 0.
19
6
0.
01
2
0
.00
4
0.
00
0
0
.00
0
0.
00
0
0.
00
0
0.
00
0
δ
18
O
Gl
o
b
ig
e
ri
n
o
id
e
s
tr
il
obu
s
num
be
r 71
71
51
51
42
71 7
1
23
23
68
67
22
22
69
c
o
rre
la
ti
on
0.
20
7 –0
.0
83
–0
.0
28
–0
.7
20
–
0.
55
9
0.
46
7
1
0.
22
6 0.
27
2
0.
42
2 0.
32
3
0.
52
2 0.
23
6
si
g
n
if
ic
anc
e
0.
1
5
0 0.
34
1
0.
4
7
9 0.
05
3
–
0.
00
3
0
.01
2
0
.12
8
0.
09
4
0
.02
8 0.
06
7
0.
00
5 0.
14
5
δ
13
C
Gl
ob
ig
e
ri
n
a
bu
ll
o
ides
num
be
r 27
27
6
6
0
23
2
3
27
2
7
25
2
1
23
23
22
c
o
rre
la
ti
on
0.
51
7 –0
.3
09
–0
.4
46
–0
.4
78
.(
a)
0.
11
4
0.
53
4 0.
22
6
1
0.
72
1
0.
70
6
0.
72
0
0.
78
5 0.
10
7
si
gn
if
ic
a
n
ce
0.
0
0
3 0.
05
8
0.
1
8
8 0.
16
9
–
0.
30
3
0
.00
4 0.
12
8
0.
00
0
0
.00
0
0.
00
0
0.
00
0 0.
31
8
δ
18
O
Gl
o
b
ig
e
ri
n
a
bu
llo
id
e
s
num
be
r
27 27
6
6
–
23
2
3
27
2
7
25
21
23
23
22
c
o
rre
la
ti
on
0.
77
9
–0
.4
42
0.
17
2
0.
03
4
–0
.1
34
0.
30
5
0.
49
0 0.
27
2
0.
72
1
1
0.
75
8
0.
96
0
0.
59
4 –0
.0
57
si
gn
if
ic
a
n
ce
0.
0
0
0
0.
00
0 0.
1
0
7
0.
40
3 0.
19
4
0.
00
6
0
.00
0 0.
09
4
0
.00
0
0
.00
0
0.
00
0
0.
00
1 0.
32
1
δ
13
C
H
o
eglu
n
d
in
a
ele
g
a
n
s
num
be
r
77
77 54
54 44
68
6
8
25
2
5
77
73
25
25
68
c
o
rre
la
ti
on
0.
46
7
–0
.355
0.
26
3
0.
28
8 0.
09
9
0.
39
0
0.
57
6
0.
42
2
0.
70
6
0.
75
8
1
0.
60
2
0.
93
8 –0
.1
49
si
gn
if
ic
a
n
ce
0.
0
0
0
0.
00
1
0.
0
2
8
0.
01
8 0.
26
2
0.
00
1
0
.00
0
0.
02
8
0
.00
0
0.
00
0
0.
00
2
0.
00
0 0.
11
4
δ
18
O
H
o
e
g
lundi
n
a
el
eg
a
n
s
num
be
r
73
73
53
53 44
67
67
21
21
73 7
3
21
21
67
c
o
rre
la
ti
on
–0
.3
93
–0
.413
0.
90
7 0.
01
7
–
0.
24
4
0.
82
3 0.
32
3
0.
72
0
0.
96
0
0.
60
2
1
0.
55
3
0.
66
7
si
gn
if
ic
a
n
ce
0.
0
2
6
0.
02
0
0.
0
0
6 0.
48
7
–
0.
13
7
0
.00
0 0.
06
7
0
.00
0
0.
00
0
0.
00
2
0.
00
2
0.
00
0
δ
13
C
U
viger
in
a g
ri
ll
i
num
be
r
25
25
6 6
0
22
2
2
23
23
25
2
1
25
25
22
c
o
rre
la
ti
on
0.
31
5 0.
10
0
–0
.5
38
–0
.3
63
–
0.
69
6
0.
66
2
0.
52
2
0.
78
5
0.
59
4
0.
93
8
0.
55
3
1
0.
15
8
si
g
n
if
ic
anc
e
0.
0
6
3 0.
31
6
0.
1
3
5 0.
24
0
–
0.
00
0
0
.00
0
0.
00
5
0
.00
0
0.
00
1
0
.00
0
0.
00
2
0.
24
2
δ
18
O
U
vi
g
er
in
a g
ril
li
num
be
r 25
25
6
6
0
22
22
23
23
25
21
25 25
22
∆δ
18
O
c
o
rre
la
ti
on
–0
.1
25
–0
.0
48
0.
12
3
–0
.2
75
0.
03
2
–0
.1
48
0.
59
3 0.
23
6 0
.10
7
–0
.0
57
–0.
14
9
0.
66
7 0.
15
8
1
si
g
n
if
ic
anc
e 0.
1
5
4
0.
34
6
0.
1
9
8
0.
02
7
0.
42
2
0.
11
3
0
.00
0 0.
14
5
0
.31
8
0.
32
1
0
.11
4
0.
00
0 0.
2
4
2
num
be
r 69
69
50
50 41
69
6
9
22
2
2
68
6
7
22 22
69
Table 1:
Correlation
matrix
(Pearson’s
correlation
coefficients)
betwee
n
environmental
variables
of
the
complete
core.
Significant
cor
relations
marked
by
grayish
background.
465
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
cor
e d
epth
magn
etic
suscepti
bili
ty
calci
um ca
rbon
ate
orga
nic
carb
on
hydr
oge
n in
dex
δ
13
C Glob
ige
rin
oide
s
tril
ob
us
δ
18
O G
lo
big
erin
oide
s
tril
ob
us
δ
13
C Glob
ige
rin
a
bu
lloi
des
δ
18
O Gl
ob
ig
eri
na
bu
lloi
des
δ
13
C H
oeg
lun
din
a
eleg
ans
δ
18
O H
oeg
lundi
na
eleg
ans
δ
13
C U
vig
erin
a
gril
li
δ
18
O U
vig
erin
a
gril
li
∆δ
18
O
co
rre
la
ti
o
n
–0
.249
–
0.
113
–
0.
022
–
0.
064
0.
05
4 –
0.
178
–
0.
076
–0
.160
0.
18
0 –
0.
114
–0
.036
–
0.
370
–0
.592
–
0.
151
si
gn
if
ic
an
ce
0.
02
4
0.
19
0 0.
44
1 0.
33
7
0.
37
5 0.
08
8 0.
28
3
0.
25
0 0.
22
4 0.
19
7
0.
39
6 0.
05
9
0.
00
4 0.
13
1
wa
te
r d
epth
num
be
r
63
63 46 46
37 59 59
20 20 58
56 19
19 57
co
rre
la
ti
o
n
0.
52
8 –0
.1
50
–0
.1
56
–0
.0
38
–0
.0
47
0.
15
3
0.
00
5
0.
02
7
0.
69
0
0.
61
9
0.
52
2 –0
.0
86
–0
.2
06
–0
.288
si
gn
if
ic
an
ce
0.
00
0
0.
10
1 0.
12
8 0.
39
2
0.
38
8 0.
13
1 0.
48
6
0.
45
7
0.
00
1
0.
00
0
0.
00
0 0.
37
1 0.
21
4
0.
01
7
inbe
nthi
c fo
ra
m
ini
fe
ra
num
be
r
74
74 55 55
39 56 56
19
19
58
55 17 17
54
co
rre
la
ti
o
n
–0
.255
0.
51
2 –0
.0
92
0.
25
0 0.
14
9
–0
.1
69
–0
.467
–
0.
036
–0
.371
–0
.637
–0
.478
–0
.545
–
0.
315
–0
.223
si
gn
if
ic
an
ce
0.
01
4
0.
00
0 0.
25
2
0.
03
3
0.
18
3 0.
10
6
0.
00
0 0.
44
2
0.
05
9
0.
00
0
0.
00
0
0.
01
2 0.
10
9
0.
05
2
ox
yphyl
ic
fo
ra
m
ini
fe
ra
num
be
r
74
74 55
55 39
56
56 19
19
58
55
17 17
54
co
rre
la
ti
o
n
0.
29
0
–0
.464
0.
31
0 0.
09
9 0.
15
6 0.
10
1 0.
20
8
0.
09
4
0.
46
1
0.
45
1
0.
45
3 0.
38
8 0.
02
8
0.
05
1
si
gn
if
ic
an
ce
0.
00
6
0.
00
0
0.
01
1 0.
23
6
0.
17
1 0.
23
0 0.
06
2
0.
35
1
0.
02
4
0.
00
0
0.
00
0 0.
06
2 0.
45
7
0.
35
8
abunda
nc
e be
nth
ic
fo
ra
m
in
ife
ra
num
be
r
74
74
55 55
39 56 56
19
19
58
55 17 17
54
co
rre
la
ti
o
n
–0
.442
0.
25
3 0.
05
2 0.
09
1 0.
24
1
–0
.1
69
–0
.490
–
0.
319
–0
.568
–0
.638
–0
.502
–0
.775
–0
.515
–
0.
090
si
gn
if
ic
an
ce
0.
00
0
0.
01
5 0.
35
2 0.
25
3
0.
07
0 0.
10
6
0.
00
0 0.
09
1
0.
00
6
0.
00
0
0.
00
0
0.
00
0
0.
01
7 0.
25
9
di
ve
rs
it
y b
enth
ic
fo
ra
m
in
ife
ra
num
be
r
74
74 55 55
39 56
56 19
19
58
55
17
17 54
co
rre
la
ti
o
n
0.
01
3
0.
38
0 –0
.1
75
–0
.332
–0
.544
–
0.
303
–
0.
132
–0
.682
–
0.
337
–0
.388
–0
.4
06
–0
.5
61
–0
.6
17
0.
19
6
si
gn
if
ic
an
ce
0
.4
7
1
0.
01
1 0.
18
7
0.
04
2
0.
00
5 0.
06
2 0.
25
6
0.
06
8 0.
25
7
0.
02
1
0.
02
0 0.
09
5 0.
07
0
0.
16
8
di
ve
rs
it
y p
lan
kt
on
ic
fo
ra
m
in
ifi
er
a
num
be
r 36
36 28
28
21 27 27
6
6
28
26 7
7
26
co
rre
la
ti
o
n
–0
.468
–0
.568
0.
58
1 0.
22
3 0.
26
7
–0
.1
76
0.
38
9 0.
67
4
0.
80
7 –0
.0
38
0.
11
1
0.
84
5 0.
65
3
0.
36
8
si
gn
if
ic
an
ce
0.
00
2
0.
00
0
0.
00
1 0.
12
7
0.
12
1 0.
19
0
0.
02
2 0.
07
1
0.
02
6 0.
42
4
0.
29
5
0.
00
8 0.
05
6
0.
03
2
abunda
nc
e pla
nk
to
ni
c
fo
ra
m
in
ife
ra
num
be
r
36
36
28 28
21 27
27 6
6 28
26
7 7
26
co
rre
la
ti
o
n
–0
.165
0.
55
2 –0
.0
57
–0
.2
60
–0
.3
17
0.
13
7
–0
.571
–
0.
093
–0
.862
–0
.472
–0
.572
–
0.
534
–
0.
214
–0
.205
si
gn
if
ic
an
ce
0
.1
6
9
0.
00
0 0.
38
7 0.
09
1
0.
08
0 0.
24
7
0.
00
1 0.
43
0
0.
01
4
0.
00
6
0.
00
1 0.
10
8 0.
32
2
0.
15
7
w
arm
wat
er p
lan
kt
on
ic
fo
ra
m
in
ife
ra
num
be
r 36
36 28 28
21 27
27 6
6
28
26 7
7
26
co
rre
la
ti
o
n
–0
.232
–0
.5
67
0.
18
0 0.
27
0
0.
45
4 –0
.1
94
0.
46
7
0.
20
6 0.
72
6 0.
17
4
0.
35
0 0.
53
9 0.
30
5
0.
24
4
si
gn
if
ic
an
ce
0
.0
8
6
0.
00
0 0.
18
0 0.
08
3
0.
01
9 0.
16
6
0.
00
7
0.
34
8 0.
05
1 0.
18
8
0.
04
0 0.
10
6 0.
25
3
0.
11
5
co
ld
er
w
at
er p
lan
kt
on
ic
fo
ra
m
in
ife
ra
num
be
r 36
36 28 28
21 27
27 6
6
28
26 7
7
26
co
rre
la
ti
o
n
0.
31
9
–0
.234
0.
19
5
–0
.116
–0
.2
96
0.
06
9
0.
50
0 0.
01
8
0.
46
3
0.
33
6
0.
35
1 –0
.0
73
–0
.0
71
0.
43
2
si
gn
if
ic
an
ce
0.
00
0
0.
00
0
0.
00
1
0.
03
2
0.
03
6 0.
30
2
0.
00
0 0.
46
7
0.
01
1
0.
00
3
0.
00
3 0.
37
4 0.
37
6
0.
00
0
ic
hnofa
br
ic
t
ype
1
num
be
r
37
1
37
0
25
4
25
4
38 58
58 24
24
64
60 22 22
56
co
rre
la
ti
o
n
0.
17
9
0.
12
6 –0
.0
36
0.
28
6
0.
28
3
0.
25
8 0.
13
2
0.
00
7 0.
11
8 0.
18
9
0.
26
9 –0
.2
51
0.
09
8
–0
.1
55
si
gn
if
ic
an
ce
0.
00
0
0.
00
8 0.
28
3
0.
00
0
0.
04
2
0.
02
5 0.
16
2
0.
48
7 0.
29
2 0.
06
7
0.
01
9 0.
13
0 0.
33
1
0.
12
8
ic
hnofa
br
ic
t
ype
6
num
be
r
37
1
37
0 25
4
25
4
38
58 58
24 24 64
60 22 22
56
co
rre
la
ti
o
n
0.
34
6
–0
.3
47
0.
06
9
–0
.0
03
–0
.2
94
0.
21
0 0.
01
8
0.
52
0
0.
81
2
0.
42
7 0.
31
0
0.
85
2 0.
53
3
–0
.0
81
si
gn
if
ic
an
ce
0.
00
0
0.
00
0 0.
28
2 0.
48
9
0.
13
5 0.
19
4 0.
47
2
0.
14
5
0.
02
5
0.
02
7 0.
10
5
0.
01
6 0.
13
8
0.
37
4
Co
cc
ol
ith
u
s pel
a
g
icu
s
num
be
r
10
2
10
2
72 72
16 19 19
6
6
21 18
6 6
18
co
rre
la
ti
o
n
0.
55
8 0.
11
8
–0
.318
–0
.293
–0
.4
35
0.
11
4 –0
.2
50
–0
.4
11
–0
.0
94
0.
34
8
0.
44
9 –0
.6
32
0.
13
0
–0
.489
si
gn
if
ic
an
ce
0.
00
0
0.
11
9
0.
00
3
0.
00
6
0.
04
6 0.
32
1 0.
15
1
0.
20
9 0.
43
0 0.
06
1
0.
03
1 0.
08
9 0.
40
3
0.
02
0
re
wo
rk
ed
na
nno
pla
nk
to
n
num
be
r
10
2 10
2
72
72
16 19 19
6
6
21
18 6
6
18
Table 1:
Continued.
466
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
wate
r d
epth
inbe
nthic fo
ram
ini
fer
a
oxyphy
lic fora
min
ifer
a
abunda
nce
benth
ic
fora
min
ife
ra
dive
rsi
ty b
enthi
c
fora
min
ife
ra
dive
rsi
ty p
lankt
on
ic
fora
min
ifie
ra
abunda
nce
plankto
nic
foramin
ifera
warm w
ater p
lan
kto
nic
foramin
ifera
colder w
ater p
lan
kton
ic
foramin
ifera
ichno
fab
ric
type
1
ichno
fab
ric
type
6
Cocc
olith
us pe
la
gic
us
rewor
ked
nanno
plankto
n
co
rre
la
ti
o
n
–0
.249
0.
52
8
–0
.255
0.
29
0
–0
.4
42
0.
01
3
–0
.468
–
0.
165
–
0.
232
0.
31
9
0.
17
9
0.
34
6
0.
55
8
si
gn
if
ic
an
ce
0.
02
4
0.
00
0
0.
01
4
0.
00
6
0.
00
0 0.
47
1
0.
00
2 0.
16
9 0.
08
6
0.
00
0
0.
00
0
0.
00
0
0.
00
0
co
re
d
epth
num
be
r
63
74
74
74
74 36
36 36 36
37
1
37
1
10
2
10
2
co
rre
la
ti
o
n
–0
.113
–
0.
150
0.
51
2
–0
.464
0.
25
3
0.
38
0
–0
.568
0.
55
2
–0
.567
–0
.234
0.
12
6
–0
.3
47
0.
11
8
si
g
n
if
ic
a
n
ce
0.
19
0
0.
10
1
0.
00
0
0.
00
0
0.
01
5
0.
01
1
0.
00
0
0.
00
0
0.
00
0
0.
00
0
0.
00
8
0.
00
0 0.
11
9
m
agn
et
ic
susc
epti
bil
it
y
num
be
r 63
74
74
74
74
36
36
36
36
37
0
37
0
10
2
10
2
co
rre
la
ti
o
n
–0
.022
–
0.
156
–
0.
092
0.
31
0 0.
05
2
–0
.1
75
0.
58
1 –0
.0
57
0.
18
0
0.
19
5 –0
.0
36
0.
06
9
–0
.318
si
g
n
if
ic
a
n
ce
0.
44
1 0.
12
8 0.
25
2
0.
01
1 0.
35
2
0.
18
7
0.
00
1 0.
38
7 0.
18
0
0.
00
1 0.
28
3
0.
28
2
0.
00
3
ca
lciu
m
ca
rb
on
at
e
num
be
r 46
55
55
55 55
28
28 28 28
25
4
25
4
72
72
co
rre
la
ti
o
n
–0
.064
–
0.
038
0.
25
0 0.
09
9 0.
09
1
–0
.3
32
0.
22
3
–0
.2
60
0.
27
0
–0
.116
0.
28
6 –0
.0
03
–0
.293
si
g
n
if
ic
a
n
ce
0.
33
7
0.
39
2
0.
03
3 0.
23
6 0.
25
3
0.
04
2 0.
12
7 0.
09
1 0.
08
3
0.
03
2
0.
00
0 0.
48
9
0.
00
6
or
ga
ni
c ca
rb
on
num
be
r 46
55
55 55 55
28
28 28 28
25
4
25
4
72
72
co
rre
la
ti
o
n
0.
05
4
–0
.0
47
0.
14
9 0.
15
6 0.
24
1
–0
.5
44
0.
26
7
–0
.3
17
0.
45
4
–0
.296
0.
28
3 –0
.2
94
–0
.435
si
g
n
if
ic
a
n
ce
0.
37
5 0.
38
8 0.
18
3 0.
17
1 0.
07
0
0.
00
5 0.
12
1 0.
08
0
0.
01
9
0.
03
6
0.
04
2 0.
13
5
0.
04
6
hy
dr
og
en
in
de
x
num
be
r
37
39 39 39 39
21
21 21
21
38
38 16
16
co
rre
la
ti
o
n
–0
.1
78
0.
15
3 –0
.1
69
0.
10
1 –0
.1
69
–0
.3
03
–0
.1
76
0.
13
7 –0
.1
94
0.
06
9
0.
25
8 0.
21
0
0.
11
4
si
g
n
if
ic
a
n
ce
0.
08
8 0.
13
1 0.
10
6 0.
23
0 0.
10
6
0.
06
2 0.
19
0 0.
24
7 0.
16
6 0.
30
2
0.
02
5 0.
19
4
0.
32
1
δ
13
C
G
lobi
ge
ri
n
o
id
es
t
ril
o
b
u
s
num
be
r
59
56 56 56 56
27
27 27 27 58
58 19
19
co
rre
la
ti
o
n
–0
.0
76
0.
00
5
–0
.4
67
0.
20
8
–0
.490
–
0.132
0.
38
9
–0
.571
0.
46
7
0.
50
0 0.
13
2
0.
01
8
–0
.2
50
si
g
n
if
ic
a
n
ce
0.
28
3
0.
48
6
0.
00
0 0.
06
2
0.
00
0 0.
25
6
0.
02
2
0.
00
1
0.
00
7
0.
00
0 0.
16
2
0.
47
2
0.
15
1
δ
18
O
Glo
b
ig
er
in
oi
de
s
t
ril
o
b
u
s
num
be
r 59
56
56 56
56 27
27
27
27
58 58
19
19
co
rre
la
ti
o
n
–0
.1
60
0.
02
7
–0
.0
36
0.
09
4
–0
.3
19
–0
.6
82
0.
67
4
–0
.0
93
0.
20
6 0.
01
8 0.
00
7
0.
52
0
–0
.4
11
si
g
n
if
ic
a
n
ce
0.
25
0 0.
45
7 0.
44
2 0.
35
1 0.
09
1
0.
06
8 0.
07
1 0.
43
0 0.
34
8 0.
46
7 0.
48
7
0.
14
5
0.
20
9
δ
13
C
G
lobi
ge
ri
n
a
bu
ll
o
id
es
num
be
r
20
19 19 19 19
6
6
6
6
24 24
6
6
co
rre
la
ti
o
n
0.
18
0
0.
69
0 –0
.3
71
0.
46
1
–0
.568
–
0.337
0.
80
7
–0
.8
62
0.
72
6
0.
46
3 0.
11
8
0.
81
2 –0
.0
94
si
gn
if
ic
an
ce
0
.2
2
4
0.
00
1 0.
05
9
0.
02
4
0.
00
6 0.
25
7
0.
02
6
0.
01
4 0.
05
1
0.
01
1 0.
29
2
0.
02
5 0.
43
0
δ
18
O
Glo
b
ig
er
in
a
bu
ll
o
id
es
num
be
r 20
19 19
19
19 6
6
6 6
24 24
6 6
co
rre
la
ti
o
n
–0
.114
0.
61
9
–0
.637
0.
45
1
–0
.638
–0
.388
–
0.
038
–0
.4
72
0.
17
4
0.
33
6 0.
18
9
0.
42
7 0.
34
8
si
gn
if
ic
an
ce
0
.1
9
7
0.
00
0
0.
00
0
0.
00
0
0.
00
0
0.
02
1 0.
42
4
0.
00
6 0.
18
8
0.
00
3 0.
06
7
0.
02
7 0.
06
1
δ
13
C
H
o
eg
lu
n
d
in
a
e
le
g
an
s
num
be
r 58
58
58
58
58
28
28
28 28
64 64
21 21
co
rre
la
ti
o
n
–0
.036
0.
52
2
–0
.478
0.
45
3
–0
.502
–0
.4
06
0.
11
1
–0
.572
0.
35
0
0.
35
1
0.
26
9 0.
31
0
0.
44
9
si
gn
if
ic
an
ce
0
.3
9
6
0.
00
0
0.
00
0
0.
00
0
0.
00
0
0.
02
0 0.
29
5
0.
00
1
0.
04
0
0.
00
3
0.
01
9 0.
10
5
0.
03
1
δ
18
O
H
o
eg
lundi
n
a
e
le
g
an
s
num
be
r 56
55
55
55
55
26
26
26
26
60
60 18
18
co
rre
la
ti
o
n
–0
.370
–
0.
086
–0
.5
45
0.
38
8
–0
.775
–
0.561
0.
84
5 –0
.5
34
0.
53
9 –0
.0
73
–0
.2
51
0.
85
2 –0
.6
32
si
g
n
if
ic
a
n
ce
0.
05
9
0.
37
1
0.
01
2 0.
06
2
0.
00
0 0.
09
5
0.
00
8 0.
10
8 0.
10
6 0.
37
4 0.
13
0
0.
01
6 0.
08
9
δ
13
C
U
vig
er
in
a gr
il
li
num
be
r 19
17
17 17
17 7
7 7 7
22
22
6 6
co
rre
la
ti
o
n
–0
.592
–
0.
206
–
0.
315
0.
02
8
–0
.5
15
–0
.6
17
0.
65
3
–0
.2
14
0.
30
5
–0
.0
71
0.
09
8
0.
53
3
0.
13
0
si
gn
if
ic
an
ce
0.
00
4 0.
21
4 0.
10
9 0.
45
7
0.
01
7
0.
07
0 0.
05
6 0.
32
2 0.
25
3 0.
37
6 0.
33
1
0.
13
8
0.
40
3
δ
18
O
U
vi
g
er
in
a gr
il
li
num
be
r
19
17 17 17
17
7
7 7 7
22
22
6
6
co
rre
la
ti
o
n
–0
.151
–0
.2
88
–0
.2
23
0.
05
1 –0
.0
90
0.
19
6
0.
36
8 –0
.2
05
0.
24
4
0.
43
2 –0
.1
55
–0
.0
81
–0
.489
si
gn
if
ic
an
ce
0
.1
3
1
0.
01
7 0.
05
2 0.
35
8 0.
25
9
0.
16
8
0.
03
2 0.
15
7 0.
11
5
0.
00
0 0.
12
8
0.
37
4
0.
02
0
∆δ
18
O
num
be
r 57
54 54 54 54
26
26 26 26
56 56
18
18
Table 1:
C
ontinued
from
the
previous
pages.
467
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
Table 1:
Continued
from
the
previous
pages.
wate
r d
epth
inbe
nthic fo
ram
in
ife
ra
oxyph
ylic f
ora
minif
era
abun
danc
e be
nthic
fora
min
ife
ra
dive
rsi
ty b
enthi
c
fora
min
ife
ra
divers
ity p
lan
ktonic
fora
min
ifie
ra
abun
danc
e pla
nkton
ic
fora
min
ife
ra
warm
water
pla
nk
ton
ic
fora
min
ife
ra
cold
er w
ate
r plan
kton
ic
fora
min
ife
ra
ichn
ofab
ric t
yp
e 1
ichn
ofab
ric t
yp
e 6
Coccol
ithu
s pe
la
gicu
s
rew
orke
d
nann
op
lankto
n
co
rr
el
atio
n 1
0.
38
1
–0
.0
50
–0
.0
30
0.
00
4 0
.00
9
–0
.1
92
–0
.1
16
0.
12
1
–0
.1
01
0.
12
3 0.
31
1
0.
28
8
si
gn
if
ic
an
ce
0.
00
1 0.
35
3 0.
40
9 0.
48
9 0
.48
3
0.
16
4 0.
27
8 0.
27
0 0.
24
0 0.
19
4 0.
11
2
0.
13
1
wa
te
r d
epth
num
be
r 63
60
60 60 60 28
28 28 28 51 51 17
17
co
rre
la
ti
o
n
0.
38
1
1
–0
.401
0.
26
2
–0
.463
–
0.
168
–0
.281
–0
.3
10
0.
03
9 0.
07
5 0.
08
7
0.
44
6
0.
45
5
si
gn
if
ic
an
ce
0.
00
1
0.
00
0
0.
01
2
0.
00
0 0
.17
5
0.
05
7
0.
03
9 0.
41
4 0.
29
2 0.
26
1
0.
02
4
0.
02
2
inbe
nthi
c fo
ra
m
ini
fe
ra
num
be
r
60 74
74
74
74 33
33
33 33 56 56
20
20
co
rre
la
ti
o
n
–0
.050
–0
.401
1
–0
.322
0.
47
9 0
.26
0
–0
.1
61
0.
36
1 –0
.2
65
–0
.3
55
0.
10
2
–0
.688
–
0.
252
si
g
n
if
ic
a
n
ce
0.
35
3
0.
00
0
0.
00
3
0.
00
0 0
.07
2
0.
18
6
0.
01
9 0.
06
8
0.
00
4 0.
22
7
0.
00
0 0.
14
2
ox
yphyl
ic
fo
ra
m
ini
fe
ra
num
be
r 60
74 74
74
74 33
33
33 33
56 56
20 20
co
rre
la
ti
o
n
–0
.030
0.
26
2
–0
.322
1
–0
.1
45
–0
.2
81
0.
23
3
–0
.3
95
0.
24
9 0.
20
3
–0
.1
90
0.
40
9 0.
14
6
si
g
n
if
ic
a
n
ce
0.
40
9
0.
01
2
0.
00
3
0.
10
9
0
.05
6
0.
09
6
0.
01
1 0.
08
1 0.
06
7 0.
08
0
0.
03
7 0.
27
0
abunda
nc
e be
nth
ic
fo
ra
m
in
ife
ra
num
be
r 60
74
74
74 74
33
33
33 33 56 56
20 20
co
rre
la
ti
o
n
0.
00
4
–0
.463
0.
47
9 –0
.1
45
1
0.
20
1 0.
05
2
0.
34
2 –0
.1
02
–0
.1
90
–0
.0
22
–0
.563
–
0.
309
si
g
n
if
ic
a
n
ce
0.
48
9
0.
00
0
0.
00
0 0.
10
9
0
.13
2
0.
38
8
0.
02
6 0.
28
5 0.
08
0 0.
43
5
0.
00
5 0.
09
2
di
ve
rs
it
y b
enthi
c
fo
ra
m
in
ife
ra
num
be
r 60
74
74 74 74
33
33
33 33 56 56
20 20
co
rre
la
ti
o
n
0.
00
9 –0
.1
68
0.
26
0 –0
.2
81
0.
20
1
1
–0
.386
0.
55
4
–0
.6
37
0.
03
7
–0
.2
75
0.
21
0
0.
28
4
si
g
n
if
ic
a
n
ce
0.
48
3 0.
17
5 0.
07
2 0.
05
6
0.
13
2
0.
01
0
0.
00
0
0.
00
0 0.
41
9 0.
06
4 0.
20
1
0.
12
6
di
vers
it
y p
lan
kt
on
ic
fo
ra
m
in
ifi
er
a
num
be
r
28
33 33 33 33 36
36
36
36 32 32 18
18
co
rre
la
ti
o
n
–0
.1
92
–0
.2
81
–0
.1
61
0.
23
3
0.
05
2
–0
.386
1
–0
.420
0.
65
2 0.
21
6
–0
.3
75
0.
01
5
–0
.746
si
g
n
if
ic
a
n
ce
0.
16
4 0.
05
7 0.
18
6 0.
09
6 0.
38
8
0
.01
0
0.
00
5
0.
00
0 0.
11
8
0.
01
7 0.
47
7
0.
00
0
abunda
nc
e pla
nk
to
ni
c
fo
ra
m
in
ife
ra
num
be
r
28
33 33 33 33
36
36
36
36 32
32 18
18
co
rre
la
ti
o
n
–0
.116
–0
.310
0.
36
1
–0
.395
0.
34
2
0.
55
4
–0
.420
1
–0
.888
–
0.
220
–
0.
035
–
0.
276
–0
.123
si
g
n
if
ic
a
n
ce
0.
27
8
0.
03
9
0.
01
9
0.
01
1
0.
02
6
0
.00
0
0.
00
5
0.
00
0 0.
11
3 0.
42
5 0.
13
4
0.
31
3
w
arm
wat
er p
lan
kt
on
ic
fo
ra
m
in
ife
ra
num
be
r 28
33
33
33
33
36
36 36
36
32 32 18
18
co
rre
la
ti
o
n
0.
12
1 0.
03
9
–0
.2
65
0.
24
9
–0
.1
02
–0
.637
0.
65
2
–0
.888
1
0.
11
9 –0
.0
33
0.
09
3
–0
.1
83
si
g
n
if
ic
a
n
ce
0.
27
0 0.
41
4 0.
06
8 0.
08
1 0.
28
5
0
.00
0
0.
00
0
0.
00
0
0.
25
7 0.
42
8 0.
35
7
0.
23
3
co
ld
er
w
at
er p
lan
kt
on
ic
fo
ra
m
in
ife
ra
num
be
r
28
33 33 33 33
36
36
36 36
32
32 18
18
co
rre
la
ti
o
n
–0
.1
01
0.
07
5
–0
.3
55
0.
20
3
–0
.1
90
0
.03
7
0.
21
6
–0
.2
20
0.
11
9
1
–0
.0
98
0.
10
8
0.
04
0
si
g
n
if
ic
a
n
ce
0.
24
0
0.
29
2
0.
00
4 0.
06
7 0.
08
0 0
.41
9
0.
11
8 0.
11
3
0.
25
7
0.
03
0 0.
14
5
0.
34
6
ic
hnofa
br
ic
t
ype
1
num
be
r 51
56
56 56 56 32
32 32 32
37
1
37
1 98
98
co
rre
la
ti
o
n
0.
12
3
0.
08
7
0.
10
2 –0
.1
90
–0
.0
22
–0
.2
75
–0
.375
–
0.
035
–
0.
033
–0
.098
1
–0
.035
0.
28
0
si
g
n
if
ic
a
n
ce
0.
19
4 0.
26
1 0.
22
7 0.
08
0 0.
43
5 0
.06
4
0.
01
7 0.
42
5 0.
42
8
0.
03
0
0.
36
8
0.
00
3
ic
hnofa
br
ic
t
ype
6
num
be
r
51
56 56 56 56 32
32 32 32
37
1 37
1
98
98
co
rre
la
ti
o
n
0.
31
1
0.
44
6
–0
.688
0.
40
9
–0
.5
63
0
.21
0
0.
01
5
–0
.2
76
0.
09
3 0.
10
8
–0
.0
35
1
0.
51
9
si
g
n
if
ic
a
n
ce
0.
11
2
0.
02
4
0.
00
0
0.
03
7
0.
00
5 0
.20
1
0.
47
7 0.
13
4 0.
35
7 0.
14
5
0.
36
8
0.
00
0
Co
cc
ol
ith
u
s pe
la
g
icu
s
num
be
r 17
20
20
20
20 18
18 18 18 98 98
10
2
10
0
co
rre
la
ti
o
n
0.
28
8
0.
45
5 –0
.2
52
0.
14
6 –0
.3
09
0.
28
4
–0
.7
46
–0
.1
23
–0
.1
83
0.
04
0
0.
28
0
0.
51
9
1
si
g
n
if
ic
a
n
ce
0.
13
1
0.
02
2 0.
14
2 0.
27
0 0.
09
2 0
.12
6
0.
00
0 0.
31
3 0.
23
3 0.
34
6
0.
00
3
0.
00
0
re
wo
rk
ed
na
nno
pla
nk
to
n
num
be
r 17
20 20 20 20 18
18 18 18 98
98
10
0 10
2
468
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
In the deeper part of the section, high organic carbon con-
tent comes mainly from terrestrial plant material as is shown
by Rock Eval pyrolysis. The Hydrogen Index (HI; Espitaliè
et al. 1977) is low and more typical of type III kerogen
(Wagreich et al. 2008). Correspondence of HI with the or-
ganic carbon cycle (Table 1) corroborates the increase of or-
ganic carbon originating from marine photosynthetic
organisms during periods of high productivity.
Paleowater-depth
Estimation of paleowater-depth is based on foraminifera
and performed in two ways. First, the Plankton/Benthos-ratio
in the modified form of Van der Zwaan et al. (1990) was used
to estimate the depth in meters (Báldi & Hohenegger 2008).
This method indicates that the water depth oscillated strongly
in the deeper part of the section. The average water depth
would have been around —600 m, with a minimum of —211 m
and a maximum of —863 m. In the upper part of the section
there would have been a strong shallowing to —117 m water
depth at 10 m in the section core depth, suddenly sinking to
—404 m water depth at 8.4 m (see Báldi & Hohenegger 2008:
fig. 2a). These oscillations of inferred water depth are at least
partly an artefact of the restricted ecological conditions of
the shallow and marginal Badenian Sea, e.g. cold water in-
gressions leading to a strong increase in planktonic foramin-
iferal numbers. Their abundance is strongly correlated with
the estimates of water depth (r = 0.98; p(t
0
) = 2.58E-53). We
conclude that depth estimation of the Badenian Sea in the
Vienna Basin using the method of Van der Zwaan et al.
(1990) is biased and is merely a reflection of plankton abun-
dance during cooler periods.
For paleowater-depth estimate we used the method of Ho-
henegger (2005) based on depth ranges of benthic foramin-
ifera and extended by the inclusion of species abundance
where l
j
is the geometric mean of the distribution borders,
d
j
the depth range and n
j
the abundance of the j
t h
species (see
Báldi & Hohenegger 2008). This transfer function depends on
depth ranges of benthic species, which for extant species are
based on modern ranges and for extinct species estimated by
comparison with ranges of the morphologically most related
living species. This estimate must not be understood as point
estimation, but represent intervals within 95% confidence lim-
its (Hohenegger 2005). Diversity, abundance or species num-
ber of benthic foraminifera could also influence the estimated
depth gradients. Testing dependencies by multiple regression
confirms the highly significant independence of this method
from the variables abundance, species number and diversity.
Power spectral analysis demonstrates significant oscilla-
tions [p(random) = 0.0066] in these depth estimations (Ham-
mer & Harper 2005). Therefore, they could be fitted by
sinusoidal regression (Fig. 2d). Since independence of this
estimation from benthos diversity and abundance has been
tested, these oscillations can be interpreted as sea-level
changes with a maximum difference of 75 m (Fig. 2d).
Additionally, linear regression was used to test for depen-
dence on depth (age) in the section. The regression
indicates a significant [p(t
0
) = 0.0334] decrease in water-
depth related to depth in the stratigraphic sequence. Figure
1d shows the confidence interval (—206 m to —323 m water
depth) at the deepest sample (102 m) shallowing to an inter-
val width from —172 m to —320 m water depth at the highest
sample (8 m). The mean trend of water depth in the section is
from —265 m to —246 m, indicating a weak but significant
shallowing tendency of + 19 m (Fig. 2d).
Stable isotopes
The tests of planktonic and benthic foraminifera from 78
samples were used to obtain
δ
18
O- and
δ
13
C-ratios. Stable
isotopes were measured on Globigerinoides trilobus, a typi-
cal warm water planktonic foraminifer (Li et al. 1999). It is
abundant in the deeper part of the section, becoming rare in
the upper part. Therefore, additional measurements were per-
formed on the abundant Globigerina bulloides in samples
from the upper part of the section that indicate cooler waters
(Rupp & Hohenegger 2008). Hoeglundina elegans, an
epibenthic foraminifer with an aragonite test was used to de-
termine the stable isotope composition of bottom water.
When preserved, aragonite tests show the original isotope
composition of the surrounding water, while calcite of fossil
tests can be affected by even weak diagenesis altering the
oxygen isotope composition (Sharp 2007). Comparing
δ
18
O
isotopes of the aragonite and calcite test walls, enrichment
relative to the equilibrium value for calcite has been noticed
(Grossmann 1984). Because H. elegans is rare in the upper
part of the section as a result of the strong increase of in-
benthic foraminifera, stable isotopes were also measured on
the inbenthic Uvigerina grilli. Here,
δ
13
C ratios are influ-
enced by the microhabitat, where the decomposition of sedi-
mentary organic matter correlated to sediment depth and
food supply leads to depletion of
δ
13
C (e.g. Rohling &
Cooke 1999).
Oxygen isotopes
The
δ
18
O of G. trilobus significantly increases (Table 2) in
the deeper part of the section from —1.82 at 102 m to —1.32 at
40 m (Fig. 3a) demonstrating minor oscillations (residuals =
0.28) that are negatively correlated with magnetic suscepti-
bility (Table 2).
δ
18
O-values are stable in the upper part of
the section, varying with a standard deviation (SD) of 0.35
around the mean of —1.61. Negative correlations with mag-
netic susceptibility are close to being significant (Table 2).
Oxygen isotopes in G. bulloides behave dissimilarly to G.
trilobus in the upper part of the section (Fig. 3a). Starting
with low values of —1.85 at 40 m depth that are close to those
of G. trilobus (—1.94), a rapid increase to 0.61 at 34.8 m is
followed by oscillations (SD = 0.22) around a mean of 0.64
(Fig. 3a). The high correlation between
δ
18
O-values of both
planktonic species is evident in their parallel fluctuations
(Fig. 3a). Both vary with magnetic susceptibility (Table 2).
(
)
[
]
(
)
∑
∑
=
=
=
=
⋅
=
k
j
j
k
j
j
j
j
j
j
j
d
n
d
n
l
depth
1
1
/
/
/
41
.
244
201
.
0
−
⋅
=
depth
core
depth
water
mean
469
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
The strong difference but parallel reaction in
δ
18
O may be in-
terpreted as an ontogenetic effect in G. bulloides (Kroon &
Darling 1995), because juveniles of that species calcify in
deeper water and later migrate to shallower waters (Spero &
Lea 1996; Bemis et al. 1998). However, more recent isotope
investigations indicate a deeper habitat of G. bulloides
throughout its life cycle (Chiessi et al. 2007). Thus the coinci-
dence of
δ
18
O-values in G. trilobus and G. bulloides at 40 m
could be the result of mixed water masses, as is suggested by
the high
δ
18
O of —0.92 in G. trilobus at 42 m (Fig. 2e).
Oxygen isotopes of the epibenthic H. elegans demonstrate
an independence from depth in the deeper part of the section
(Table 2), weakly varying (SD = 0.223) around a mean of
1.81. In this part of the section, oscillations of the
δ
18
O are
highly negatively correlated with magnetic susceptibility
(Table 2; Fig. 2b). After a strong increase between 40 m and
35 m, the few
δ
18
O measurements are close to the mean value
of 2.13 (SD=0.14). According to the few measurements in the
upper part of the section, the negative correlation (r= —0.357)
with magnetic susceptibility is insignificant (Table 2). For a
better resolution of benthic
δ
18
O in the upper part of the sec-
tion, stable isotopes were measured on the inbenthic species
U. grilli. Regression analysis of
δ
18
O between U. grilli and
H. elegans confirms a linear relationship. The 95% confi-
dence interval for the slope of the regression (b =0.947) in-
cludes the value of 1 which would indicate identical
relations, while the intercept of 0.582 falls within the confi-
dence limits of 0.78 + 19 ‰ for enriched
18
O in aragonite
Fig. 3. a – Stable oxygen isotopes of planktonic foraminifera. b – Stable oxygen isotopes of benthic foraminifera. c – Stable carbon iso-
topes of planktonic foraminifera. d – Stable carbon isotopes of benthic foraminifera. e – Absolute differences in stable oxygen isotopes be-
tween planktonic and benthic foraminifera. Grey and white bands indicate periods obtained by moving averages of magnetic susceptibility.
470
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
Table 2:
Correlation
matrix
(Pearson’s
correlation
coefficients)
betwee
n
environmental
variables
of
the
deeper
core
(lower
left
triang
le
matrix)
and
the
upper
core
(upper
right
triangle
matrix).
Significant
correlations
marked
by
grayish
background.
core
depth
mag
net
ic
susc
ep
tib
ilit
y
calc
ium ca
rbon
ate
orga
nic
car
bon
hyd
roge
n in
dex
δ
13
C G
lo
bige
rinoi
des
trilob
us
δ
18
O Globi
gerin
oid
es
trilob
us
δ
13
C G
lobi
gerin
a
bull
oides
δ
18
O Gl
obigerin
a
bull
oides
δ
13
C H
oeg
lund
ina
eleg
an
s
δ
18
O Ho
eg
lund
ina
eleg
an
s
δ
13
C U
vig
eri
na
gril
li
δ
18
O Uv
ig
erin
a
gril
li
∆δ
18
O
co
rr
e
lat
io
n
1
0.
02
9 –
0.178
0.
388
–
0.
20
7 0.
14
2
0.
20
7
0.
517 0
.174
0.
60
2
–0
.393
0
.315
–0.47
3
si
g
n
if
ic
a
nc
e
–
0.
35
3
0
.35
1
0.
1
9
5
–
0
.15
0
0.
2
4
0
0.
15
0
0.
0
03 0
.183
0.
00
1
0
.02
6 0.
0
6
3
0.
00
8
co
re
de
p
th
num
be
r
3
1
1
\1
69
16
9 7
7
1
2
7
27 27
27
29
25
25
25
25
co
rr
e
lat
io
n
–0
.0
56
1
–0
.203 0
.327
–
0.
355
–0
.2
81
–0.08
3 –
0.309
–0
.4
96
–0.04
9
–0
.413
0
.100
–0.31
7
signi
fi
c
a
n
c
e
0
.162
–
0.
3
31
0
.237
–
0.
0
34
0.
0
7
8
0.
34
1
0
.05
8
0.
0
0
3
0.
40
8
0
.02
0 0.
3
1
6
0.
06
1
m
agn
et
ic
su
sc
ep
ti
b
ilit
y
num
be
r 31
0
31
0\
1
6
9
7
7
1
27
27 27
27
29 25
25
25 25
co
rr
e
lat
io
n
–0
.1
50
–0.45
2
1
0.
656
–
–0
.397
0.
551
–0.02
8 –
0.446
0.
806
–0.28
1
0.
90
7 –0
.5
38
0.
81
3
si
gn
if
ic
an
c
e
0
.004
0.
00
0
–
0.
0
5
5
– 0
.18
9
0.
1
0
0
0.
47
9
0
.18
8
0.
0
2
6
0.
32
4
0
.00
6 0.
1
3
5
0.
02
5
ca
lc
iu
m ca
rb
on
at
e
num
be
r
3
10
31
0
31
0\
7
7
1 7
7
6 6
6 5
6
6 6
co
rr
e
lat
io
n
–0
.3
45
–0.25
1
0.
421
1
–
–0
.214 0
.068
–0.72
0 –
0.478 –
0.0
08
–0.27
9
0.
01
7
–0
.3
63
0.
02
4
signi
fi
c
a
n
c
e
0
.000
0.
00
0
0.
0
00 –
–
0.
3
23
0
.442
0.
05
3
0
.16
9
0.
4
9
4
0.
32
5 0
.48
7 0.
2
4
0
0.
48
2
or
ga
nic
c
ar
b
on
num
be
r
3
10
31
0
31
0
31
0\
7
1 7
7
6 6
6
5
6
6 6
co
rr
e
lat
io
n
–0
.3
87
–0.18
6
0.
013
0.
387
1
–
– –
–
– – –
–
–
signi
fi
c
a
n
c
e
0.
0
0
4
0.
10
6
0
.46
5
0.
0
0
4
–
–
– –
–
– – –
–
–
hy
d
ro
ge
n
i
n
de
x
num
be
r
47
47
4
7
47
4
7
\1
1
1 0
0
0 0 0
0
0
co
rr
e
lat
io
n
0.
303
–0.23
6
0.
047
–0
.0
02
0.
08
7
1
0.
321
0.
55
9 0
.11
4 0.
18
0
0.
47
2 0
.24
4
0.
696
–0.06
2
signi
fi
c
a
n
c
e
0.
0
2
2
0.
05
9
0
.38
0
0.
4
9
6
0.
29
1
–
0
.051
0.
00
3 0
.30
3
0.
1
9
5
0.
01
0 0
.13
7
0.
0
0
0
0.
38
5
δ
13
C
Globi
ge
ri
n
o
id
e
s
tr
il
o
b
us
num
be
r
45
45
4
5
45
42
45\
2
7
27
23 23
25
24 22
22 25
co
rr
e
lat
io
n
0.
469
–0.24
8 0.
230
0.
069
0.
08
9
–0
.081
1
0.
46
7
0.
534
0.
792
0.
72
9
0.
82
3
0.
662
0.
71
3
signi
fi
c
a
n
c
e
0
.001
0.
05
0 0
.06
4
0.
3
2
6
0.
28
8 0
.29
8
–
0.
01
2
0.
0
04
0
.000
0.
00
0
0
.00
0
0
.000
0.
00
0
δ
18
O
Gl
ob
ig
e
ri
n
oi
de
s
tr
il
o
b
u
s
num
be
r
45
45 4
5
45
42
4
5
45\
2
7
23
23
25
24
22
22
25
co
rr
e
lat
io
n
–
–
–
–
– –
–
1
0.
226 0
.272
0.
42
2 0
.32
3
0.
52
2 0.
23
6
si
g
n
if
ic
a
nc
e
–
–
–
–
– –
–
–
0
.12
8
0.
0
9
4
0.
02
8 0
.06
7
0.
0
0
5
0.
14
5
δ
13
C
G
lobi
g
e
ri
n
a
bu
ll
o
id
e
s
num
be
r
0
0
0
0
0 0
0
0
\27
2
7
25
21 23
23 22
co
rr
e
lat
io
n
–
–
–
–
– –
–
–
1
0.
721
0.
70
6
0.
72
0
0.
78
5 0.
10
7
si
g
n
if
ic
a
nc
e
–
–
–
–
– –
–
– –
0
.000
0.
00
0
0
.00
0
0.
0
0
0
0.
31
8
δ
18
O
G
lo
b
ige
rin
a
bu
ll
oi
de
s
num
be
r
0
0
0
0
0 0
0
0
0\
2
7
25
21
23
23 22
co
rr
e
lat
io
n
0.
705
–0.37
2 0.
152
–0
.0
95
–0.13
4
0.
394
0.
614
– –
1
0.
80
2
0.
96
0
0.
594
0.
34
4
signi
fi
c
a
n
c
e
0
.000
0.
00
5 0
.15
2
0.
2
6
1
0.
19
4
0.
0
04
0.
0
0
0
– –
–
0.
00
0
0
.00
0
0
.001
0.
04
6
δ
13
C
Hoe
g
lun
d
ina
el
eg
a
n
s
num
be
r
48
48 4
8
48
44
43
43 0
0
48\
2
9
25
25
25
25
co
rr
e
lat
io
n
0.
182
–0.59
6
0.
358
0.
30
2 0.
09
9
0.
254
0.
596
– –
0.
631
1
0.
60
2
0.
93
8 0.
06
2
signi
fi
c
a
n
c
e
0
.108
0.
00
0
0.
0
06
0.
0
1
8
0.
26
2
0.
0
50
0
.000
–
–
0.
0
0
0
–
0
.00
2
0.
0
0
0
0.
38
7
δ
18
O
H
o
e
g
lun
d
in
a
el
eg
a
n
s
num
be
r 48
48
48
48
44
43
43 0
0
48 48
\2
5
21
21 24
co
rr
e
lat
io
n
–
–
–
–
– –
–
– –
–
–
1
0.
553
0.
66
7
si
g
n
if
ic
a
nc
e
–
–
–
–
– –
–
– –
–
–
–
0
.002
0.
00
0
δ
13
C
U
v
ig
e
rin
a g
ril
li
num
be
r
0
0
0
0
0 0
0
0 0
0
0
0\
2
5
25
22
co
rr
e
lat
io
n
–
–
–
–
– –
–
– –
–
–
–
1
0.
15
8
si
g
n
if
ic
a
nc
e
–
–
–
–
– –
–
– –
–
–
–
–
0.
24
2
δ
18
O
U
v
ig
e
rin
a
g
ri
ll
i
num
be
r
0
0
0
0
0 0
0
0 0
0
0
0
0\
25
22
∆δ
18
O
co
rr
e
lat
io
n
0.
39
2 –0.04
6
0.
058
–0
.2
34
0.
03
2
–0
.134
0.
624
– –
0.
30
6 0.
00
7
– –
1
signi
fi
c
a
n
c
e
0.
00
4 0.
38
2
0
.35
4
0.
0
6
3
0.
42
2
0
.19
3
0
.000
–
–
0.
0
2
3
0.
48
1
–
–
–
num
be
r
44
44 4
4
44
41
4
4
44 0
0
43 43
0
0
44
\2
5
471
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
Table 2:
Continued.
cor
e d
epth
magn
etic
suscep
tib
ili
ty
calciu
m carb
onat
e
organ
ic c
arb
on
hydrog
en in
dex
δ
13
C G
lobi
geri
no
ide
s
tril
ob
us
δ
18
O G
lob
ig
erin
oides
tril
ob
us
δ
13
C G
lobi
geri
na
bull
oid
es
δ
18
O Glo
big
eri
na
bull
oid
es
δ
13
C Hoe
glundi
na
eleg
an
s
δ
18
O H
oeg
lun
din
a
eleg
an
s
δ
13
C U
vig
erin
a g
ril
li
δ
18
O U
vig
erin
a gri
lli
∆δ
18
O
co
rr
el
at
io
n
–0
.209 –
0.
17
6 –0.
03
2
–0.
07
1
0.
054
–0
.0
36
–0
.040
– –
0.
06
4 0.
19
4
– –
–0
.2
21
si
g
n
ifi
ca
nc
e
0
.09
5
0
.13
6 0.
42
2
0.
3
2
9
0.
3
7
5
0.
4
1
5
0.
40
6
–
–
0
.35
3 0.
12
4
–
–
0.
0
9
4
wa
te
r d
ep
th
num
be
r
4
1
4
1
41
41 37 38
38
0
0
3
7
37
0
0
37
co
rr
el
at
io
n
0.1
59 –
0.
10
0 –0.
11
7
–0.
14
3
–0
.0
47
0.
068
0.
005
– –
0.
29
0 0.
16
6
– –
–0
.0
33
si
gnif
ican
ce
0.1
32
0.2
4
4
0
.2
0
7
0
.159
0
.388
0
.343
0
.4
88
–
–
0
.03
6 0.
15
6
–
–
0.
4
2
3
inbe
nth
ic
for
am
inife
ra
num
be
r
5
1
5
1
51
51 39 38
38
0
0
3
9
39
0
0
37
co
rr
el
at
io
n
–0
.551
0.4
41
–0.
02
6
0.
192
0.
149
–0
.3
03
–0
.491
– –
–0
.8
26
–0.
60
1
– –
–0
.3
19
si
gnif
ican
ce
0.0
00
0
.00
1 0.
42
7
0.
0
8
8
0.
1
8
3
0
.032
0
.0
01 –
–
0
.00
0
0.
00
0 –
–
0
.027
oxy
ph
ylic
fora
m
inif
er
a
num
be
r
51
5
1
51
51 39
38
3
8
0
0
39
39 0
0
37
co
rr
el
at
io
n
0.0
34
–0
.3
59
0.
32
5
0.
08
5 0.
15
6 0.
05
9 0.
16
1
– –
–0
.0
20
0.
25
6
– –
0.
263
si
gnif
ican
ce 0.4
07
0
.00
5
0.
01
0
0.
2
7
8
0.
1
7
1
0.
3
6
3
0.
16
7
–
–
0
.45
3 0.
05
8
–
–
0.
0
5
8
abu
ndanc
e be
nt
hi
c
for
am
in
if
er
a
num
be
r 5
1
51
51
51 39 38
38
0
0
3
9
39
0
0
37
co
rr
el
at
io
n
–0
.395
–0
.0
23
0.
06
7
0.
152
0.
241
–0
.0
33
–0
.374
– –
–0
.3
22
–0.
18
6
– –
–0
.1
96
si
gnif
ican
ce
0.0
0
2
0.4
3
8
0.
32
0
0
.143
0
.070
0
.421
0
.0
10 –
–
0.0
2
3
0.
12
8 –
–
0
.123
di
ve
rs
it
y be
nt
hi
c
for
am
in
if
er
a
num
be
r
51
51
51
51
39
38
38
0
0
39
39
0
0
37
co
rr
el
at
io
n
0.3
66
0.3
50
–0.
18
3
–0.
34
6
–0
.5
44
0.
015
–0
.168
– –
–0
.0
71
–0.
38
0
– –
0.
089
si
gnif
ican
ce
0.0
3
3
0.0
4
0
0.
18
5
0
.042
0
.005
0
.474
0
.2
40 –
–
0.3
8
3
0.
04
9 –
–
0
.359
di
ve
rs
it
y p
lan
kt
on
ic
for
am
in
if
er
a
num
be
r
26
26
26
26
21
20
20
0
0
20
20
0
0
19
co
rr
el
at
io
n
–0
.286
–0
.4
58
0.
54
3
0.
505
0.
267
–0
.2
89
0.
30
7
– –
–0
.2
49
0.
45
7
– –
0.
090
si
gnif
ican
ce
0.0
7
8
0.0
0
9
0.
00
2
0
.004
0
.121
0
.108
0
.0
94 –
–
0.1
4
4
0.
02
1 –
–
0
.357
abu
ndanc
e plank
toni
c
for
am
in
if
er
a
num
be
r
26
26
26
26
21
20
20
0
0
20
20
0
0
19
co
rr
el
at
io
n
0.1
8
7
0.3
7
8
–0.
02
6
–0.
3
0
9
–0
.3
1
7
0
.246
–
0
.656
– –
–0
.1
8
7
–0.
72
6
– –
–0
.4
4
2
si
gnif
ican
ce
0.1
8
0
0.0
2
8
0.
45
0
0
.063
0
.080
0
.148
0
.0
01 –
–
0.2
1
4
0.
00
0 –
–
0
.029
w
ar
m
w
at
er p
lan
kt
on
ic
for
am
in
if
er
a
num
be
r
26
26
26
26
21
20
20
0
0
20
20
0
0
19
co
rr
el
at
io
n
–
0
.401
–0
.3
9
0
0.
11
0
0
.396
0
.454
–0
.3
0
6
0.
55
4
– –
0.0
2
9
0.
65
5
– –
0
.338
si
gnif
ican
ce
0.0
2
1
0.0
2
4
0.
29
7
0
.023
0
.019
0
.094
0
.0
06 –
–
0.4
5
1
0.
00
1 –
–
0
.079
co
ld
er
w
at
er p
lan
kt
on
ic
for
am
in
if
er
a
num
be
r
26
26
26
26
21
20
20
0
0
20
20
0
0
19
co
rr
el
at
io
n
0.7
3
9
–0
.2
8
7
0.
19
9
–0.
1
1
4
–0
.2
9
6
0
.132
0.
64
9
– –
0.7
4
0
0.
53
4
– –
0
.539
si
gnif
ican
ce
0.0
0
0
0.0
0
0
0.
00
1
0
.036
0
.036
0
.226
0
.0
00 –
–
0.0
0
0
0.
00
0 –
–
0
.001
ic
hn
ofabri
c t
yp
e 1
num
be
r
249
248
248
24
8
38
35
35
0
0
38
38
0
0
34
co
rr
el
at
io
n
0.0
1
4
–0
.0
7
8
–0.
02
1
0
.272
0
.283
0
.231
0.
28
7
– –
0.3
1
2
0.
36
7
– –
–0
.0
4
7
si
gnif
ican
ce
0.4
1
2
0.1
1
0
0.
37
3
0
.000
0
.042
0
.091
0
.0
47 –
–
0.0
2
8
0.
01
2 –
–
0
.397
ic
hn
ofabri
c t
yp
e 6
num
be
r
249
248
248
24
8
38
35
35
0
0
38
38
0
0
34
co
rr
el
at
io
n
0.1
4
9
–0
.3
1
1
0.
09
4
–0.
0
0
3
–0
.2
9
4
0
.344
0.
14
7
– –
0.0
1
5
0.
31
2
– –
0
.157
si
gnif
ican
ce
0.1
0
9
0.0
0
4
0.
22
0
0
.490
0
.135
0
.105
0
.3
01 –
–
0.4
7
9
0.
12
8 –
–
0
.296
Cocco
li
th
u
s p
el
a
gi
cu
s
num
be
r
70
70
70
70
16
15
15
0
0
15
15
0
0
14
co
rr
el
at
io
n
0.3
6
7
0.1
2
8
–0.
25
9
–0.
3
5
7
–0
.4
3
5
0
.447
0.
09
6
– –
0.4
6
0
0.
23
4
– –
0
.301
si
gnif
ican
ce
0.0
0
1
0.1
4
6
0.
01
5
0
.001
0
.046
0
.048
0
.3
67 –
–
0.0
4
2
0.
20
0 –
–
0
.148
rewor
ke
d
na
nn
op
la
nk
to
n
num
be
r
70
70
70
70
16
15
15
0
0
15
15
0
0
14
472
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
Table 2:
Continued
from
the
previous
pages.
wate
r d
epth
inbe
nthic fo
ram
ini
fera
oxyphy
lic fo
ramin
ife
ra
abunda
nce be
nthic
foramin
ifera
dive
rsi
ty be
nthic
foramin
ifera
dive
rsi
ty pl
ankto
nic
foramin
ifi
era
abunda
nce pl
ankto
nic
foramin
ifera
warm w
ater p
lan
kton
ic
foramin
ifera
colder w
ater p
lan
kton
ic
foramin
ifera
ichno
fabr
ic t
ype
1
ichno
fabr
ic t
ype
6
Cocc
olith
us pe
la
gicu
s
rew
orke
d
nanno
plankto
n
co
rre
la
ti
o
n
–0
.175
0.
39
7 0.
26
0 0.
14
4 0.
07
9
–0
.0
27
–0
.2
32
0.
019
–0
.10
6
0.
35
1
0.
52
8 0.
00
5
0.
42
8
si
g
n
if
ic
a
n
ce 0.
21
2
0.
02
7 0.
11
0 0.
25
1 0.
35
7
0.
46
8
0.
246
0.
478
0.
3
7
8
0.
0
0
0
0
.00
0 0.
48
8
0.
00
7
core d
ep
th
num
be
r 2
3
24 24 24 24
11 11
11 11
123
1
2
3 33
33
co
rre
la
ti
o
n
–0
.077
–
0.
312
0.
61
9
–0
.681
0.
67
7 0.
36
8
–0
.789
0.
817
–0
.78
7
–0
.288
0.
52
9
–0
.302
0.
34
4
si
g
n
if
ic
a
n
ce 0.
36
3
0.
06
9
0.
00
1
0.
00
0
0.
00
0 0.
13
3
0.
002
0.
001
0.
0
0
2
0.
0
0
1
0.
0
0
0
0.
04
4
0.
02
5
m
agn
et
ic su
sc
ep
ti
bi
lit
y
num
be
r 2
3
24
24
24
24 11
11
11
11
123
12
3
33
33
co
rre
la
ti
o
n
–0
.5
79
–0
.4
58
0.
11
6
0.
85
0 –0
.3
17
–0
.9
98
–0
.3
20
–0
.0
31 –0
.13
5
0.
08
5 –0.1
13
–0
.8
91
0.
05
9
si
g
n
if
ic
a
n
ce
0.
11
4 0.
21
9 0.
42
6
0.
03
4 0.
30
2
0.
02
0
0.
396
0.
490 0.
4
5
7
0
.42
8 0
.40
5
0.
15
0 0.
48
1
ca
lc
iu
m
ca
rb
on
at
e
num
be
r 6
5
5
5 5
3 3
3 3
7
7
3
3
co
rre
la
ti
o
n
–0
.720
–
0.
541
0.
84
1 0.
37
5 0.
28
8
–0
.9
98
–0
.2
02
–0
.1
53 –0
.01
3
0.
14
8
0.
61
1
–0
.9
66
–0
.1
48
si
gn
if
ic
an
ce
0.
05
3 0.
17
3
0.
03
7 0.
26
7 0.
31
9
0.
01
9
0.
435
0.
451 0.
4
9
6
0
.37
6 0
.07
3
0.
08
4 0.
45
3
or
ga
ni
c ca
rb
on
num
be
r
6 5
5 5 5
3 3
3 3
7
7
3
3
co
rre
la
ti
o
n
–
– – – –
– –
– –
–
–
–
–
si
g
n
if
ic
a
n
ce
–
– – – –
– –
– –
–
–
–
–
hy
d
ro
ge
n i
nd
ex
num
be
r
1
1 1 1 1
1 1
1 1
1
1
1
1
co
rre
la
ti
o
n
–0
.3
88
0.
03
3
0.
00
6
–0
.0
63
–0
.2
50
–0
.6
05
0.
304
0.
111 0.
16
9
–0.0
62
0
.26
3
0.
37
7 0.
31
6
si
gn
if
ic
an
ce
0.
03
7
0.
44
7
0.
49
0
0.
39
9
0.
15
1 0.
05
6
0.
232
0.
396 0.
3
4
4
0
.38
6 0
.10
7
0.
26
6 0.
30
2
δ
13
C
G
lobi
ge
ri
n
o
id
es
tr
il
obu
s
num
be
r
2
2
19 19 19 19
8
8
8
8
24
2
4
5
5
co
rre
la
ti
o
n
–0
.2
78
0.
19
9
–0
.435
0.
50
0
–0
.760
–
0.
171
0.
662
–0
.4
83 0.
36
5
0.
18
2
–0.0
33
0.
71
1 0.
33
7
si
g
n
if
ic
a
n
ce 0.
10
5
0.
20
7
0.
03
1
0.
01
5
0.
00
0 0.
34
2
0.
037
0.
112 0.
1
8
7
0
.19
8 0
.43
9
0.
08
9 0.
29
0
δ
18
O
Glo
b
ig
er
in
oi
de
s
t
ril
obu
s
num
be
r 2
2
19
19
19
19 8
8 8
8
24
2
4
5
5
co
rre
la
ti
o
n
–0
.1
60
0.
02
7
–0
.0
36
0.
09
4
–0
.3
19
–0
.6
82
0.
674
–0
.0
93 0.
20
6
0.
01
8 0
.00
7
0.
52
0
–0
.4
11
si
g
n
if
ic
a
n
ce
0.
25
0
0.
45
7
0.
44
2
0.
35
1
0.
09
1 0.
06
8
0.
071
0.
430 0.
3
4
8
0
.46
7 0
.48
7
0.
14
5 0.
20
9
δ
13
C
G
lobi
ge
ri
n
a
bu
ll
oi
des
num
be
r
2
0
19 19 19 19
6
6
6
6
24
2
4
6
6
co
rre
la
ti
o
n
0.
18
0
0.
69
0 –0
.3
71
0.
46
1
–0
.568
–
0.
337
0.
807
–0
.8
62 0.
72
6
0.
46
3 0.
11
8
0.
81
2 –0
.0
94
si
g
n
if
ic
a
n
ce 0.
22
4
0.
00
1 0.
05
9
0.
02
4
0.
00
6 0.
25
7
0.
026
0.
014 0.
0
5
1
0.
0
1
1
0.
2
9
2
0.
02
5 0.
43
0
δ
18
O
G
lob
ig
er
in
a
bu
ll
oi
d
es
num
be
r 2
0
19 19
19
19 6
6
6 6
24
2
4
6 6
co
rre
la
ti
o
n
–0
.113
0.
48
9
–0
.556
0.
53
3
–0
.801
–
0.
610
0.
797
–0
.7
16
0.
74
9
0.
39
1 –0.0
81
0.
78
7 –0
.6
38
si
g
n
if
ic
a
n
ce 0.
31
2
0.
01
7
0.
00
7
0.
00
9
0.
00
0 0.
05
4
0.
009
0.
023
0.
0
1
6
0.
0
2
4
0.
3
4
6
0.
03
2 0.
08
6
δ
13
C
H
o
eg
lu
n
d
in
a
el
eg
an
s
num
be
r 2
1
19
19
19
19 8
8
8
8
26
2
6
6 6
co
rre
la
ti
o
n
–0
.207
0.
57
4 –0
.3
11
0.
38
2
–0
.6
95
–0
.3
96
0.
523
–0
.5
02 0.
60
2
0.
39
3 0
.11
6
0.
64
3
0.
99
8
si
g
n
if
ic
a
n
ce 0.
19
8
0.
01
0 0.
12
0 0.
07
2
0.
00
1 0.
21
8
0.
143
0.
155 0.
1
0
3
0
.03
5 0
.30
4
0.
27
8
0.
01
8
δ
18
O
H
o
eg
lund
in
a
el
eg
a
n
s
num
be
r 1
9
16 16 16
16
6 6
6 6
22
2
2
3
3
co
rre
la
ti
o
n
–0
.370
–
0.
086
–0
.5
45
0.
38
8
–0
.775
–
0.
561
0.
845 –0
.5
34
0.
53
9 –0.0
73
–0.2
51
0.
85
2 –0
.6
32
si
g
n
if
ic
a
n
ce 0.
05
9
0.
37
1
0.
01
2 0.
06
2
0.
00
0 0.
09
5
0.
008 0.
108
0.
1
0
6 0
.37
4
0
.13
0
0.
01
6 0.
08
9
δ
13
C
U
vi
g
er
in
a
gr
il
li
num
be
r 1
9
17
17 17
17 7
7 7
7
22
2
2
6 6
co
rre
la
ti
o
n
–0
.5
92
–0
.2
06
–0
.3
15
0.
02
8
–0
.5
15
–0
.6
17
0.
653
–0
.2
14 0.
30
5
–0.0
71
0
.09
8
0.
53
3 0.
13
0
si
gn
if
ic
an
ce
0.
00
4 0.
21
4 0.
10
9 0.
45
7
0.
01
7 0.
07
0
0.
056
0.
322 0.
2
5
3
0
.37
6 0
.33
1
0.
13
8 0.
40
3
δ
18
O
U
vig
er
in
a gr
il
li
num
be
r
1
9
17 17 17
17
7 7
7 7
22
2
2
6
6
co
rre
la
ti
o
n
–0
.2
09
–0
.2
66
–0
.3
27
0.
24
7 –0
.3
98
0.
22
8
0.
35
1
–0
.0
98 –0
.11
2
–0.2
39
–0.2
59
–0
.1
61
–0
.5
69
si
g
n
if
ic
a
n
ce
0.
18
9
0.
15
1
0.
10
0
0.
16
9
0.
05
7 0.
31
1
0.
220
0.
417 0.
4
0
6
0
.14
2 0
.12
2
0.
42
0 0.
21
6
∆δ
18
O
num
be
r
2
0
17 17 17 17
7
7
7
7
22
2
2
4
4
473
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
wate
r d
epth
inb
en
th
ic f
oramin
ife
ra
oxyp
hy
lic f
ora
minif
era
ab
undanc
e be
nthic
for
am
in
ife
ra
div
ers
ity
benthi
c
for
am
in
ife
ra
div
ers
ity
pla
nkto
nic
for
am
in
ifie
ra
ab
undanc
e pla
nk
to
nic
for
am
in
ife
ra
war
m wa
ter p
la
nkt
on
ic
for
am
in
ife
ra
cold
er w
ate
r plan
kton
ic
for
am
in
ife
ra
ichnof
abri
c ty
pe 1
ichnof
abri
c ty
pe 6
Coccol
ithu
s pe
lagicu
s
rew
orke
d
nanno
plankto
n
co
rr
el
atio
n 1
0.46
5 0.
05
7
–0
.0
8
4
0.
06
6
0.
61
8
–0
.6
2
0
0.
62
1 –0
.4
8
5
0.
04
5 –0
.3
0
4
–0
.1
1
7
–0
.2
8
1
si
gn
if
ic
an
ce
–
0.01
9 0.
40
6
0.
36
3 0.
39
1
0.
05
1 0.
05
1
0.
05
0 0.11
2
0.
42
6 0.
09
6
0.
41
3
0.
29
5
wa
te
r d
epth
num
be
r 41\
2
3
20
20 20 20
8
8
8 8
20
20
6
6
co
rre
la
ti
o
n
0.
63
0
1
–
0
.295
0.
52
1 –0
.3
1
0
–0
.3
3
4
0.
27
4 –0
.4
2
4
0.53
4
0.
43
7 –0
.1
1
9
0.
20
1
–0
.0
8
8
si
gn
if
ic
an
ce
0.
00
0 –
0.
08
1
0.
00
4 0.
07
0
0.
17
3 0.
22
2 0.
11
1 0.05
6
0.
03
1 0.
31
3
0.
31
7
0.
41
8
inbe
nthi
c fo
ra
m
in
ife
ra
num
be
r
41 51\
2
4
24
24 24
10 10 10 10
19 19
8
8
co
rre
la
ti
o
n
–
0
.212
–
0
.542
1
–
0
.388
0.
68
0
0.
37
6 –0
.4
0
2
0.
48
9 –0
.4
9
4
–
0
.055
0.
40
1
–0
.8
7
5
0.
00
5
si
g
n
if
ic
a
n
ce
0.
09
2
0.00
0 –
0.
03
1
0.
00
0
0.
14
2 0.
12
5 0.
07
6 0.07
3
0.
41
2
0.
04
4
0.
00
2 0.
49
6
o
x
y
phyl
ic
fo
ra
m
ini
fe
ra
num
be
r 41
51
51\
2
4
24
24
10 10 10 10
19
19
8 8
co
rre
la
ti
o
n
0.
03
6 –0
.1
0
2
–0
.2
2
7
1
–
0
.472
–
0
.603
0.
87
8
–
0
.888
0.82
1
0.
42
4
–
0
.461
–
0
.014
–
0
.522
si
g
n
if
ic
a
n
ce
0.
41
2
0.23
8
0.
05
5
–
0.
01
0
0.
03
3
0.
00
0
0.
00
0
0.00
2
0.
03
5
0.
02
3 0.
48
6
0.
09
2
a
bunda
nc
e be
nthi
c
fo
ra
m
in
ife
ra
num
be
r
41 51
51
51\
2
4
24
10
10
10
10
19
19 8
8
co
rre
la
ti
o
n
–
0
.139
–
0
.375
0.
30
0
0.
26
6
1
0.
53
6 –0
.4
8
9
0.
54
9 –0
.5
2
7
–0
.3
5
7
0.
22
2
–0
.4
3
9
0.
29
6
si
g
n
if
ic
a
n
ce
0.
19
4
0.00
3
0.
01
6
0.
03
0 –
0.
05
5
0.
07
6
0.
05
0 0.05
9
0.
06
7 0.
18
0
0.
13
8
0.
23
8
di
ve
rs
it
y
b
enthi
c
fo
ra
m
in
ife
ra
num
be
r 41
51
51
51 51\
2
4
10
10
10 10
19 19
8
8
co
rre
la
ti
o
n
–0
.1
9
2
0.17
9
–0
.1
4
3
–0
.0
3
9
–0
.3
2
6
1
–
0
.631
0.
54
4
–0
.6
2
0
–0
.2
3
1
0.
07
8
0.
29
5
0.
49
0
si
g
n
if
ic
a
n
ce
0.
20
2
0.20
1
0.
25
3 0.
42
8 0.
06
0
–
0.
01
9
0.
04
2
0.02
1 0.
29
1
0.
42
7
0.
35
2
0.
25
5
d
iv
ers
it
y p
lan
k
to
n
ic
fo
ra
m
in
ife
ra
num
be
r
21
24
24 24
24
26\
1
1
11
11
11
8
8
4
4
co
rre
la
ti
o
n
–0
.1
0
4
–0
.2
6
1
0.
13
4
0.
25
0 0.
16
9
–
0
.402
1
–
0
.820
0.85
1 0.
22
1
–0
.6
7
6
0.
43
2
–0
.8
1
4
si
g
n
if
ic
a
n
ce
0.
32
7
0.10
9 0.
26
6
0.
12
0 0.
21
4
0.
02
1 –
0.
00
1
0.00
0 0.
29
9
0.
03
3 0.
28
4
0.
09
3
a
bunda
nc
e pla
n
k
to
n
ic
fo
ra
m
in
ife
ra
num
be
r
21
24
24 24 24
26 26\
1
1
11
11
8
8 4
4
co
rre
la
ti
o
n
–0
.3
0
4
–0
.0
2
1
0.
10
0
–0
.0
5
7
0.
01
1
0.
57
9
–
0
.494
1
–0
.9
5
3
–0
.5
1
5
0.
38
8
0.
03
3
0.
40
1
si
g
n
if
ic
a
n
ce
0.
09
0
0.46
1 0.
32
2
0.
39
7 0.
48
0
0.
00
1
0.
00
5 –
0.00
0 0.
09
6
0.
17
1
0.
48
4
0.
29
9
w
a
rm
wat
er p
lan
k
ton
ic
fo
ra
m
in
ife
ra
num
be
r
21
24
24 24 24
26
26 26\
1
1
11
8
8
4
4
co
rre
la
ti
o
n
0.
29
5
–0
.0
8
2
0.
02
7
0.
07
0 0.
11
2
–
0
.720
0.
56
1
–
0
.956
1
0.
46
7 –0
.5
1
7
0.
21
4
–0
.5
7
2
si
g
n
if
ic
a
n
ce
0.
09
7
0.35
2 0.
45
1
0.
37
2 0.
30
1
0.
00
0
0.
00
1
0.
00
0 –
0.
12
2
0.
09
5 0.
39
3
0.
21
4
co
ld
er
w
a
te
r p
lan
k
ton
ic
fo
ra
m
in
ife
ra
num
be
r
21
24
24 24 24
26
26
26 26\
1
1
8
8
4
4
co
rre
la
ti
o
n
–0
.1
4
0
0.14
7
–0
.5
3
8
0.
25
4
–0
.2
9
2
0.
06
1
0.
22
9
–0
.2
3
4
0.06
3
1
0.
28
3 0.
06
5
0.
16
3
si
g
n
if
ic
a
n
ce
0.
22
3
0.18
9
0.
00
0 0.
06
2
0.
03
8
0.
38
7 0.
13
6 0.
13
0
0.38
3
–
0.
00
1 0.
36
3
0.
19
0
ic
hnofa
br
ic
t
y
pe
1
num
be
r 32
38
38 38
38
25 25 25
25
24
9\
1
23
12
3 31
31
co
rre
la
ti
o
n
0.
25
9
0.06
0 –0
.0
6
6
–0
.1
2
3
–0
.0
9
8
–0
.4
0
8
–0
.1
3
8
–0
.1
8
2
0.22
8
–
0
.151
1
–
0
.181
0.
50
5
si
g
n
if
ic
a
n
ce
0.
07
6
0.36
0 0.
34
7
0.
23
2 0.
27
8
0.
02
1 0.
25
6 0.
19
1 0.13
6
0.
00
9 –
0.
16
5
0.
00
2
ic
hnofa
br
ic
t
y
pe
6
num
be
r
32
38
38 38 38
25 25 25 25
24
9 24
9\
1
23
31
31
co
rre
la
ti
o
n
0.
40
8 0.34
1
–0
.6
5
3
0.
32
0
–0
.5
3
8
0.
26
6
0.
08
1 –0
.1
0
4
–0
.0
2
5
0.
15
4
–0
.0
6
9
1
0.
44
0
si
g
n
if
ic
a
n
ce
0.
09
4
0.12
7
0.
00
8 0.
14
3
0.
02
9
0.
16
9 0.
38
8 0.
35
6 0.46
4
0.
10
5
0.
28
9
–
0.
00
7
Co
cc
ol
ith
u
s pe
lagicu
s
num
be
r 12
13
13 13
13
15 15 15 15
68
68
70\
3
3
31
co
rre
la
ti
o
n
0.
70
5
0.48
3
–0
.5
6
2
0.
09
7
–0
.7
3
2
0.
33
4
–0
.5
9
2
0.
10
9
–0
.2
1
5
0.
10
7 0.
03
8
0.
47
3
1
si
gn
if
ic
an
ce
0.
00
5
0.04
7
0.
02
3 0.
37
6
0.
00
2 0.
11
2
0.
01
0 0.
35
0 0.22
1
0.
19
2 0.
37
9
0.
00
0 –
re
wo
rk
ed
n
a
n
n
o
p
lan
k
ton
num
be
r
12
13
13 13
13 15
15 15 15
68 68
70 70\
3
3
Table 2:
Continued
from
the
previous
pages.
474
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
Factor
loadings
1 2 3 4 5
colder water planktonic foraminifera
0.847
0.160
0.373
0.218 –0.604
diversity planktonic foraminifera
0.814
0.394
0.282 –0.285 –0.345
abundance planktonic foraminifera
–0.726 –0.199 –0.638 –0.307 0.565
magnetic susceptibility
–0.724 –0.184 –0.527
0.176
calcium carbonate
–0.689
–0.443 –0.389
reworked nannoplankton
0.598
0.211
0.266
δ
18
O Globigerinoides trilobus
–0.363 –0.361 –0.108 0.231
∆δ
18
O
0.363 0.927 0.316
0.159
ichnofabric type 1
–0.780
0.184
0.373 0.145
δ
13
C Hoeglundina elegans
0.256 0.609 0.290 –0.130 0.140
inbenthic
foraminifera
0.365 0.277 0.883 0.359 0.251
abundance benthic foraminifera
0.475
0.389
0.740
0.499 0.328
Coccolithus pelagicus
0.166
0.648
0.261
0.144
δ
18
O Hoeglundina elegans
0.498
0.227
0.632
ichnofabric type 6
0.230
0.496
organic carbon
–0.255 –0.233
0.725 0.255
warm water planktonic foraminifera
0.324
0.289
0.475
δ
13
C Globigerinoides trilobus
0.140
0.366 0.555
diversity benthic foraminifera
–0.214 –0.275 –0.556 –0.149 –0.196
oxyphylic foraminifera
–0.443 –0.424 –0.550
Explained variance
initial eigenvalue
Sum of squared
factor loadings
Factor
Total
% of
variance
Cumulative
%
Total
% of
variance
Cumulative
%
% of
variance
after
rotation
4.7
2.1
2.9
1.3
1.1
23.4
10.7
14.4
6.3
5.6
23.4
34.1
48.5
54.7
60.3
34.9
3.2
24.1
3.3
4.7
1
2
3
4
5
6
7
8
9
10
11
12
13
14
15
16
17
18
19
20
6.12
2.89
2.40
1.57
1.16
0.99
0.86
0.75
0.55
0.49
0.40
0.35
0.29
0.28
0.24
0.19
0.16
0.13
0.07
0.03
30.6
14.5
12.0
7.8
5.8
5.2
4.3
3.7
2.8
2.5
2.0
1.8
1.4
1.4
1.2
0.9
0.8
0.7
0.3
0.1
30.6
45.1
57.1
64.9
70.7
75.9
80.3
84.1
86.8
89.3
91.3
93.1
94.5
95.9
97.1
98.0
98.9
99.5
99.9
100.0
Factor
loadings
1 2 3 4 5
colder water planktonic foraminifera
0.806
–0.142 0.228 –0.483
diversity planktonic foraminifiera
–0.803
0.302
–0.239
abundance planktonic foraminifera
0.793
–0.222 –0.129
magnetic susceptibility
–0.662
0.119 –0.167 0.102
calcium carbonate
0.657
reworked nannoplankton
–0.405 –0.167
0.132 0.211 –0.115
δ
18
O Globigerinoides trilobus
1.007
0.314
∆δ
18
O
0.112 –0.871 0.288
0.214
ichnofabric type 1
0.588
0.245
δ
13
C Hoeglundina elegans
–0.135 0.196 0.786 0.165
inbenthic foraminifera
–0.162 –0.124
0.675
abundance benthic foraminifera
0.113
0.662
Coccolithus pelagicus
0.558
δ
18
O Hoeglundina elegans
0.389
0.528 0.471 0.208
ichnofabric type 6
–0.230
–0.147 0.772
organic carbon
0.250
0.481
warm water planktonic foraminifera
–0.350 –0.121 –0.342 –0.283 0.596
δ
13
C Globigerinoides trilobus
0.231 0.523
diversity benthic foraminifera
–0.116 –0.240
oxyphylic
foraminifera
–0.221 –0.185 –0.246 0.228
Table 3b
Table 3c
compared to calcite tests (Grossmann 1984). Uvi-
gerina grilli does not show dependency of
δ
18
O
from depth in the section (Table 2) but weak
variations (SD= 0.23) around the mean of 1.62.
The obvious periods in U. grilli
δ
18
O do not cor-
relate with magnetic susceptibility (Table 2).
Carbon isotopes
Stable carbon isotopes in G. trilobus demon-
strate a weak but significant increase from the
bottom to the top of the sequence (Fig. 3c). In the
deeper part, the increase starts with 2.48 at 102 m
and ends with 2.66 at 40 m. Variability is not
large (residuals: 0.21) and the periodicity is close
to having a significant negative correlation with
magnetic susceptibility (Table 2). Carbon iso-
topes of G. trilobus do not show any relation to
depth in the upper part, but values vary more
(SD = 0.29) around the mean of 2.63 compared to
the deeper part (Fig. 3c). The positive correlation
of
δ
13
C oscillations with periods in magnetic sus-
ceptibility is significant in this part of the section
(Table 2).
δ
13
C-values of G. bulloides exhibit
similar variability (SD = 0.24) around a mean val-
ue of 0.91, which is much lower than that of G.
trilobus (Fig. 3c). The correlation in
δ
13
C be-
tween both planktonic species is significant, the
result of parallel fluctuations (Fig. 3c). The large
differences between the
δ
13
C of G. trilobus and
G. bulloides may result from their different habi-
tats (Chiessi et al. 2007).
Carbon isotopes of H. elegans are distin-
guished by a significant increase in the deeper
part of the section (Table 2) starting with 1.81 at
102 m and reaching 2.37 at 40 m. Variations are
weak (residuals: 0.17) and correlate negatively
with magnetic susceptibility (Fig. 3d; Table 2).
The few measurements in the upper part of the
section do not define a trend, but hint at strong
variability (SD = 0.28) around a mean value of
2.68. Although there are only a few measure-
ments in the upper part, the negative correlation
with magnetic susceptibility is significant (Ta-
ble 2). This tendency is confirmed by the in-
benthic U. grilli for which there are more
measurements. The linear relations in
δ
13
C be-
tween H. elegans and U. grilli shows a signifi-
cant slope of the regression line (b = 0.892) and
the 95% confidence limit includes the coefficient
of 1 for identical relations. A constant difference
of —1.92 between H. elegans and U. grilli is
shown by the intercept of the regression line. As
mentioned above, it has been found that pore wa-
ter gradients of
δ
13
C decrease with sediment
depth due to decomposition of sedimentary or-
ganic matter and by the amount of carbon used as
a food supply (Rohling & Cooke 1999). As indi-
cated for H. elegans, constancy of carbon isotope
Table 3a
475
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
Table 3a—c: a – Factor extraction based on maximum likelihood
method and oblimin rotation with Kaiser normalization. b – Factor
pattern matrix after oblimin rotation showing important factor load-
ings. c – Factor structure matrix after oblimin rotation showing
important factor loadings.
Factor
1 2 3 4 5 6
1
1 0.352
0.541
0.053
–0.203
–0.067
2
0.352 1
0.188
–0.285 0.077
–0.099
3
0.541 0.188 1
0.235 0.086
–0.398
4
0.053 –0.285 0.235 1
0.147 –0.274
5
–0.203 0.077 0.086 0.147 1
–0.131
6
–0.067 –0.099 –0.398 –0.274 –0.131 1
ratios for U. grilli in the upper part of the section is con-
firmed by large variations (SD of 0.31) around 0.562
(Fig. 3d). The negative correlation between
δ
13
C and mag-
netic susceptibility in the upper part of the section as found
with few measurements by H. elegans is also manifested by
U. grilli (Table 2).
Oxygen isotope differences
Stratification of water masses can be estimated by the differ-
ence in
δ
18
O (
∆δ
18
O; Báldi 2006) between G. trilobus and the
benthic U. grilli (Fig. 3e). The lacking measurements of U.
grilli in the deeper core can be replaced by the transformation
δ
18
O
grilli
=
δ
18
O
elegans
— 0.582, n = 6.
Because differences between
δ
18
O at the warmer sea sur-
face and the colder bottom are negative, absolute values
were used (Fig. 3e). The weak but significant decrease ( b =
—0.006) in the lower part of the section indicates tendency
toward poorly stratified water, starting with differences of
2.96 at 102 m declining to 2.59 at 40 m. Variations around
the linear regression are weak (residuals: 0.219). These vari-
ations do not correspond to periods in magnetic susceptibili-
ty (Table 2). The opposite tendency in
∆δ
18
O can be seen in
the upper part of the section. There, the variability increase is
more than double (b = 0.017) that of the lower part of the sec-
tion ending with
∆δ
18
O = 3.35 at 8 m. This indicates intensi-
fication of water stratification in the younger sediments
(Fig. 3e). Variability around the regression line is similar to
that in the lower part of the section (residuals: 0.209). Also,
in the upper part of the section,
∆δ
18
O oscillations do not
correspond to variations of magnetic susceptibility (Table 2).
Ichnofossils
The cores, having been cut vertically, were examined for
ichnofossils at 25 cm intervals (376 samples). Twelve ichno-
species were identified (Pervesler et al. 2008). The ichnotaxa
Phycosiphon, Nereites and Thalassinoides provide informa-
tion about environmental conditions on the paleo-sea bot-
tom. Phycosiphon predominates throughout the entire
sequence, accompanied by major occurrences of Nereites
(Pervesler et al. 2008). Both taxa represent pioneers that bur-
row in sediments with high amounts of particulate food and
Table 3d: Correlation matrix between factors.
oxygenated pore water. After an increased import of particu-
late organic matter, the deposit feeders producing Phycosi-
phon and Nereites are the first settlers (Wetzel & Uchmann
2001). They live entirely within the sediment and require ox-
ygen rich pore waters as they horizontally rework the sedi-
ment. Nereites becomes less abundant when food content is
reduced or when bottom conditions are more stable favour-
ing ichnotaxa with burrows opening to the sea floor, such as
Thalassinoides, Chondrites, Trichichnus and Zoophycos
(Pervesler et al. 2008).
The average proportions of two ichnofabric types de-
scribed in Pervesler et al. (2008) provide more information
about the paleoenvironment. In the first ichnofabric type
(Type 6 in Pervesler et al. 2008), Nereites, depending on
well-oxygenated sediments, crosses Phycosiphon living at
the same level. In the second ichnofabrics type (Type 1 in
Pervesler et al. 2008), Thalassinoides, which characterizes
stable bottom conditions at a higher level, crosses both Phy-
cosiphon and Nereites burrows (Pervesler et al. 2008). The
ichnofabric type with abundant Nereites does not show sig-
nificant trends (Table 1) but demonstrates variations corre-
sponding to those of magnetic susceptibility (Table 1;
Fig. 4a). In the deeper part of the section (bottom to 68 m),
the Thalassinoides ichnofabric is completely lacking. It ap-
pears and reaches a maximum between 60 m and 55 m, then
decreases to 40 m (Fig. 4b). Periodic less frequent appear-
ances in the upper part of the section correlate negatively
with magnetic susceptibility (Table 2; Fig. 4b).
Benthic foraminifera
Benthic foraminfera were investigated in 74 samples taken
throughout the section at 1.2 m spacing. 102 taxa could be
distinguished (Báldi & Hohenegger 2008). The life style and
distribution of benthic foraminifera allows further inferences
about the paleoenvironment of the sea floor (e.g. Jorissen
1999; Murray 2006).
Inbenthic foraminifera
All species, which lead an inbenthic life today or extinct
species for which an inbenthic life is inferred on the basis of
morphological relations to living representatives, are
summed and counted as a percentage of the total fauna (Bál-
di & Hohenegger 2008). Proportions of inbenthic foramin-
ifera increase upward (Fig. 4c; Table 1). This increase is
insignificant in the deeper part from 102 m to 40 m (Table 2)
varying with a SD of 7.1 around the mean of 30.3 %. The
significant increase in the upper part of the section (Table 3)
starts with 35.5 % at 40 m reaching 44.2 % at the top. While
negative correlations with magnetic susceptibility are insig-
nificant in the deeper part of the section, they approach sig-
nificance in the upper part (Table 2).
Oxyphylic foraminifera
Species belonging to this group (Báldi & Hohenegger
2008) need well-aerated bottom water reflecting an
epibenthic or shallow inbenthic mode of life (e.g. Corliss
476
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
Fig. 4. a – Percentages of ichnofabric type 6 with Phycosiphon and Nereites. b – Percentages of ichnofabric type 1 with Thalassinoides
crossing Phycosiphon and Nereites. c – Percentages of inbenthic foraminifera. d – Percentages of oxyphylic foraminifera. e – Abun-
dance of benthic foraminifera. f – Diversity of benthic foraminifera. Grey and white bands indicate periods obtained by moving averages
of magnetic susceptibility.
1991; Jorissen 1999). Percentages of oxyphylic foraminifera
decrease from the bottom to the top of the section (Fig. 4d;
Table 1). In the deeper part of the section, the significant de-
crease (Table 2) starts with 29.3 % at 102 m declining to
17.7 % at 40 m. Variations are weak (residuals: 5.2) correlat-
ing positively with magnetic susceptibility (Table 2). In the
upper part of the section, percentages vary intensively
(SD = 9.2) around a mean of 22.0 %. These variations are
positively correlated with magnetic susceptibility (Table 2).
Abundance
The benthic foraminiferal abundances were standardized
for 200 g dry sediment (Báldi & Hohenegger 2008). High
abundance often reflects the dominance of a few species
adapted to a specific habitat or dwelling in extreme habitats
due to their opportunistic life; they can reproduce there un-
impeded by interspecific competitors (e.g. Valiela 1995).
The exponential growth in populations with unimpeded re-
production makes a logarithmic scale necessary to allow
comparisons using linear statistical methods.
Abundance increases from the bottom to the top or the
cored section, with a negative correlation to magnetic sus-
ceptibility (Fig. 4e; Table 1). The increase is insignificant in
the deeper part (40 m to 102 m; Table 2), where abundance
oscillates weakly (SD=6.64
×10
3
) around a geometric mean
of 7.34
×10
3
individuals 200 g
—1
. These variations are nega-
tively correlated with magnetic susceptibility (Table 2). In
477
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
the upper part of the section, strong variations
(SD = 1.70
×10
4
) around a geometric mean of 1.35
×10
4
indi-
viduals 200 g
—1
are negatively correlated with magnetic sus-
ceptibility (Table 2). The significant increase in abundance
from the bottom to the top of the sequence appears to be a
stepwise function with mean values differing significantly
between the lower and upper part of the section.
Diversity
In contrast to the high abundance that is often correlated
with the dominance of a few species, diversity is characterized
by numerous species possessing similar specimen abundanc-
es. Therefore, diversity is an indicator of habitat quality for the
organism group (a discussion of the different factors causing
diversity see Valiela 1995). From the various diversity mea-
sures, the Measure of Evenness (J’), derived from the Shan-
non Information Measure H’, was selected (Krebs 1989).
Diversity decreases significantly from the bottom to the
top of the cored sequence (Fig. 4f; Table 1) exhibiting a pos-
itive correlation with magnetic susceptibility. The decrease
is also significant in the deeper part of the section starting
with J’ = 0.678 at 102 m reaching J’ = 0.584 at 40 m with
weak variations (residuals: 0.096). Except the deepest sam-
ple, variations around a mean of J’ = 0.660 are weak from
100 m to 53 m (SD = 0.048) suddenly intensifying (SD of
0.063) between 53 m and 38 m with a significantly lower
mean of J’ = 0.571 (Fig. 4f). Diversity variability is again
more intensive in the upper part of the section (8 m to 40 m),
with no significant relation to depth (Table 2). Again, the
mean is lower (J’ = 0.564) compared to the two lower inter-
vals. Variations correlating with magnetic susceptibility (Ta-
ble 2) have the highest amplitudes (SD = 0.098). Therefore,
the significant decrease in diversity is not linear but is best
explained by a stepwise function (Fig. 4f).
Planktonic foraminifera
This group of microorganisms can be used to evaluate
conditions in the upper 500 meters of the pelagic realm.
Planktonic foraminifera respond to many different environ-
mental factors, but are mainly affected by temperature and
nutrients (e.g. Hilbrecht 1996; Arnold & Parker 1999). Wa-
ter depth is an important factor influencing the life cycles de-
pendent on the depth of the thermocline, pycnocline, or the
chlorophyll maximum (Arnold & Parker 1999).
Planktonic foraminifera were investigated from 36 samples
taken at approximately 2.4 m intervals along the cored section
(Rupp & Hohenegger 2008). They were grouped at the gener-
ic level or put into morphological groups such as 4-chambered
or 5-chambered globigernids. Beside the taxonomic investiga-
tion and their relationship to environmental factors, some indi-
ces and proportions characterizing the environment and/or
environmental factors were measured.
Cold and cold-temperate water indicators
According to Hilbrecht (1996) and Li et al. (1999), higher
abundances of “four- and five chambered globigerinids” as
well as Turborotalita signalize cold water, while Globotur-
borotalita and Globorotalia prefer cool-temperate water.
The high percentages of cold water planktonic foramin-
ifera do not show a significant trend along the section (Ta-
ble 1) oscillating with a standard deviation of 15.9 around a
mean of 70.7 % (Fig. 5a). Variability is more intensive
(SD = 20.3) in the upper core compared to the deeper part
(SD = 13.9). In both parts of the stratigraphic sequence, the
variations have a significant negative correlation with mag-
netic susceptibility (Table 2).
Warm and warm-temperate water indicators
Orbulinids, Globigerinoides and Globoquadrina are re-
garded as warm water indicators, while Globigerinella pre-
fers warm-temperate environments (Bicchi et al. 2003; Rupp
& Hohenegger 2008).
In percentage abundance, this group behaves oppositely to
the group indicating cold water masses (Fig. 5b). This is evident
in the high negative correlation between the two groups (Ta-
ble 1). Relations of warm water indicators to depth in the sec-
tion are insignificant for the entire sequence (Tables 1, 2). From
102 m to 40 m, percentages vary little (SD = 11.4) around a
mean of 22.7 %. Variations become greater (SD = 14.7) in the
upper part of the section around a lower mean of 15.9 %. In
contrast to the cooler water indicators, the percentages of warm
water planktonic foraminifera correspond positively to periods
of increased magnetic susceptibility (Table 2).
Abundance
The planktonic foraminiferal abundances were standard-
ized for 1 g dry sediment (Rupp & Hohenegger 2008). Be-
cause of the exponential growth in populations, logarithms
of numbers were used for further linear statistical analyses.
Abundance declines from the bottom to the top of the se-
quence (Table 1) but these relations are insignificant in both
the deeper and upper part of the section (Table 2). While
mean abundance is high between 52 m and 102 m (geomet-
ric mean: 493.0 individuals g
—1
with a SD of 267.1), abun-
dance is low from 52 m to 8 m (geometric mean: 189.7
individuals g
—1
with a significantly higher SD of 310.3
caused by a maximum of 1100 individuals g
—1
at 30 m;
Fig. 5c). The decline in abundance can be explained by a
stepwise function with different means (Fig. 5c). Negative
correlations with magnetic susceptibility are significant for
both the lower and the upper parts of the section (Table 2).
Diversity
Diversity of the planktonic foraminifera was calculated us-
ing the Simpson Index 1-D (D = Dominance; Rupp & Ho-
henegger 2008). Similarly to benthic foraminifera, the
diversity of planktonic foraminifera is the opposite of abun-
dance, as shown by the high negative correlation between
both indices (Table 1). These correlations are not as high as
for benthic foraminifera because diversity is constant through-
out the entire sequence (regression coefficient b = 7E-05; Ta-
ble 1) while abundance decreases. Evaluation of the increase
478
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
in plankton diversity is hampered by an extreme outlier at
26 m (1-D = 0.25; Fig. 5d). Deleting the outlier from the analy-
sis improves measure of the increase (b = 0.0006), but it still
remains insignificant. Diversity increases significantly
(b = 0.0017) in the deeper part of the section starting with
0.699 at 102 m and reaching 0.804 at 40 m (Fig. 5d) with re-
siduals of 0.077. Neglecting the outlier at 26 m, diversity var-
ies with standard deviations of 0.055 around a mean of 0.764.
Correlation with magnetic susceptibility is significant
throughout the whole section (Table 1).
Calcareous nannoplankton
Samples for the investigation of calcareous nannoplankton
were taken at approximately 1 m spacing down to 100 m (94
samples). Seven additional samples were taken in ~ 20 cm
intervals between 100 m and 102 m (Ćorić & Hohenegger
2008). Percentages of dominant species were used for char-
acterizing assemblages and their dependence on environ-
mental factors. Two groups with strong relations to
environmental factors were analyzed, supporting the results
obtained from planktonic foraminifera.
Coccolithus pelagicus
Coccolithus pelagicus is as an important paleoecologic in-
dicator. It is abundant in cold water (Okada & McInyre
1979; Winter et al. 1994). High proportions of this species
also indicate higher nutrient levels and eutrophic conditions
(Ćorić & Hohenegger 2008).
Fig. 5. a – Percentages of cold and cold temperate planktonic foraminifera. b – Percentages of warm and warm temperate planktonic for-
aminifera. c – Abundance of planktonic foraminifera. d – Diversity of planktonic foraminifera. e – Percentages of the nannoplankton
Cocolithus pelagicus. f – Percentages of reworked nannoplankton. Grey and white bands indicate periods obtained by moving averages of
magnetic susceptibility.
479
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
The proportion of C. pelagicus increases from the bottom
to the top of the section (Table 1; Fig. 5e). In the deeper part
of the section (40 m to 102 m) the increase is insignificant
(Table 2), where proportions vary (SD = 3.14) around an av-
erage of 4.71 %. Between 8 m and 40 m, percentages are
more variable (SD = 3.82) around a higher mean of 7.43 %
(Fig. 5e). The significant increase of C. pelagicus along the
sequence is thus not linear, but follows a stepwise function
(Fig. 5e). Correlations with magnetic susceptibility are nega-
tive and significant in the deeper part of the section, but in-
significant in the upper part (Table 2).
Reworked nannoplankton
Late Cretaceous, Paleogene and Early Miocene taxa indi-
cate reworking of older sediments due to tectonic movement
or increased erosion (Ćorić & Hohenegger 2008).
The proportion of reworked nannofossils increases signifi-
cantly from the bottom to the top of the section, and is posi-
tively correlated with magnetic susceptibility (Table 1). This
is in contrast to C. pelagicus, which is negatively correlated
with magnetic susceptibility. Similar to the latter, an increase
is insignificant in both parts of the sequence (Table 2). Per-
centages vary slightly (SD = 1.18) around 1.2 % in the deeper
part of the section, becoming more variable (SD = 5.62)
around a higher mean of 5.05 % in the upper part (Fig. 5f).
Again, the increase over the entire section is not linear but can
be explained with a stepwise function (Fig. 5f).
Environmental factors
To explain the factors that influenced the environmental
variables explained above, we used the statistical methods
summarized as ‘Latent Structure Models’ (Krzanowski &
Marriott 1995), often termed ‘Factor Analysis’ (Davis 2002).
We used the ‘Maximum Likelihood Factor Analysis’, first
developed by Lawley (1940), because it avoids many prob-
lems arising by other factor analytical methods (for details
see Krzanowski & Marriott 1995; Davis 2002). After finding
the optimum solution of independent factors explaining the
frequency distribution of variables, these artificial mathe-
matical factors can be interpreted as natural environmental
factors. However, the independence of natural factors in en-
vironmental science as postulated by orthogonal factors,
even though rotated, is unsustainable. For example, produc-
tivity of phytoplankton depends on non-stratified water
masses, temperature and other parameters. Therefore, an ob-
lique factor rotation optimizes the correlation between vari-
ables and factors that is expressed in the ‘structure matrix’. It
also optimizes the correlation between factor loadings and
the correlation matrix of variables expressed in the ‘pattern
matrix’. By this process, factors are no longer independent
but inter-correlated to different degrees. The ‘direct oblimin
method’ (Jennrich & Sampson 1966) with Kaiser normaliza-
tion was used here to get oblique (correlated) factors.
Previous calculations of factor analyses based on principal
component extraction demonstrated that the variable ‘water
depth’ is a single factor. Therefore, this variable was excluded
from the analysis. Before starting factor analysis, all percent-
age data were linearized by the arcsine-root transformation
(Parker & Arnold 1999) and abundance data transformed to
logarithms.
Five factors explaining 70 % of total variance were ex-
tracted and rotated for optimizing relations between vari-
ables and factors as well as optimizing correlations between
factors (Table 3a). Factor loadings of variables are shown in
the pattern and structure matrix (Table 3b,c). Factor scores
for variables were calculated using the regression method.
In the following, five significant factors (eigenvalue > 1)
are explained by their loadings and are interpreted in terms
of ecology.
Factor 1
The main factor, initially explaining 30.6 % of total vari-
ance, and increasing to 34.9 % after oblique rotation
(Table 3a), is most positively loaded by the variables ‘cold
water planktonic foraminifera’, ‘abundance of planktonic for-
aminifera’ and ‘calcium carbonate content’, with additional
positive loading by ‘organic carbon content’ and ‘differences
in
δ
18
O between planktonic and benthic foraminifera’. High
negative loadings are from ‘diversity of planktonic foramin-
ifera’, ‘magnetic susceptibility’, ‘reworked nannoplankton’
and ‘warm water planktonic foraminifera’, with lesser nega-
tive loadings by ‘ichnofabric type 6 with Nereites’ and ‘oxy-
phylic benthic foraminifera’ (Table 3b,c).
This factor represents the mean temperature of the sea
without differentiation between surface and bottom waters.
This interpretation is supported by the dependence of the
above variables on temperature. Beside direct temperature
indicators such as warm and cold water foraminifera, the
higher amount of calcium carbonate partly results from
abundant planktonic foraminifera preferring nutrient-rich
cold water combined with organic carbon originating from
marine photosynthetic organisms. The negative loading by
magnetic susceptibility confirms the correlation between ter-
rigenous input through intensified weathering and erosion at
times of maxima in eccentricity and obliquity, which led to
higher insolation and increased seasonal differences. The
higher input of terrigenous material during warm periods
also explains the negative loading of reworked nannofossils
for this cold-water factor. Factor scores, indirectly scaling
paleo-temperature of the seawater during deposition, can
now be used to demonstrate temperature changes in the time
interval during which the sediments were deposited (Fig. 6).
Periods of colder water were from 101 m to 92 m, from 73 m
to 50 m and from 35 m to 23 m, while in the other intervals
warm water dominated (Fig. 6).
Factor 2
This factor, initially explaining 14.5 % of total variance, be-
comes less important (3.2 %) after oblique rotation (Table 3a).
Two opponents with extreme loadings characterize this factor.
δ
18
O of the planktonic foraminifer G. trilobus positively loads
this factor, while ‘differences in
δ
18
O between planktonic and
480
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
benthic foraminifera’ shows high negative loadings
(Table 3b,c). ‘Ichnofabric 1 with Thalassinoides’ has a high
positive factor loading, while lower but significant positive
loadings by ‘
δ
18
O of the benthic H. elegans’ and ‘diversity of
planktonic foraminifera’ additionally characterize this factor.
The extreme loading by positive
δ
18
O in both the plank-
tonic and benthic foraminifers and the high negative loading
in the
∆δ
18
O values allows the interpretation of this factor as
a signal for stratified water masses. Positive scores indicate
non-stratified, mixed water, while negative scores are typical
of stratified water masses (Fig. 6).
The relation between Factors 1 and 2 demonstrate the advan-
tage of oblique rotated factors. Both are positively correlated
(Table 3d) confirming the correspondence between stratifica-
tion and warm surface water. Differences between both factors
show that water mixing occurred during warm water periods
(Fig. 6). The intensive variation of this factor between 10 m and
40 m is partly caused by more intense environmental changes,
but the incomplete stratigraphic record resulting from loss of
sediments through tectonics must also be considered (Hoheneg-
ger et al. 2008; Ćorić & Hohenegger 2008).
Fig. 6. Comparing factor scores obtained by maximum likelihood factor analysis with the single scale of nonmetric multidimensional scaling
(MDS) and insolation curves between —14.379 and —14.142 Myr. Colors of the units indicate ‘warm’ (orange) and ‘cold’ (blue) temperatures.
Factor 3
The importance of the third factor, with an initial variance
proportion of 12 % increasing to 24.1 % after oblique rotation
approximates the Factor 1 (Table 3a). Factor 3 is high posi-
tively loaded by a series of variables starting with ‘
δ
13
C of H.
elegans’ and followed in decreasing order by ‘inbenthic fora-
minifera’, ‘abundance of benthic foraminifera’, ‘percentages
of C. pelagicus’ and ‘
δ
18
O of H. elegans’ (Table 3b,c). Lower
positive loadings are by ‘differences in
δ
18
O between plank-
tonic and benthic foraminifera’ and ‘ichnofabric 1 with
Thalassinoides’. ‘Warm water planktonic foraminifera’, ‘oxy-
phylic benthic foraminifera’ and ‘diversity of benthic foramin-
ifera’ load this factor negatively (Table 3b,c).
According to the positive and negative loadings, this fac-
tor seems to scale dysoxic bottom conditions. The main ar-
gument is based on the richness of inbenthic foraminifera
coupled with their abundance, while diversity of benthic for-
aminifera is low. The indication of oxygen-depleted bottom
sediments is supported by the negative loading of oxyphylic
benthic foraminifera and the positive loadings by the trace
481
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
fossil Thalassinoides that prefers stable bottom conditions
with burrows opening to the sea floor. Therefore, factors
scores can be used as a scale measuring the intensity of oxy-
gen depletion.
Again, this factor indicating the degree of oxygen deple-
tion is highly positively correlated with Factor 1, which
characterizes cold water, and less, but still significantly posi-
tively correlated with Factor 2 indicating the degree of strati-
fication of the water (Table 3d). Using factor scores, oxygen
depletion increases from the bottom to the top of the section,
partially mimicking oscillations found in the temperature
Factor 1 (Fig. 6).
Factor 4
Representing 7.8 % of the initial variance, the importance
of this factor decreases to 3.3 % after rotation (Table 3a).
The main variable loading this factor is ‘ichnofabric type 6
with Nereites’ followed in decreasing importance by ‘organ-
ic carbon content’, ‘
δ
18
O of H. elegans’, ‘
δ
18
O of G. trilo-
bus’, ‘
δ
13
C of G. trilobus’, ‘oxyphylic benthic foraminifera’,
‘cold water planktonic foraminifera’ and ‘reworked nanno-
plankton’ (Table 3b,c). This factor is weakly negatively
loaded by ‘warm water planktonic foraminifera’, ‘diversity’
and ‘abundance of planktonic foraminifera’ (Table 3b,c).
This factor clearly indicates the input of particulate terrig-
enous organic material (POM) that is relatively rich in oxy-
gen (type III kerogen) during periods of colder water. These
produce the ideal environment for the opportunistic ichno-
fossil Nereites. Therefore, factor scores as a scale character-
ize the input of oxygen-rich particulate organic matter from
land (Fig. 6).
Factor 5
The importance of this factor with a proportion of 5.8 % of
the initial variance does not significantly decrease after ob-
lique rotation (4.7 %). Two variables, ‘warm-water plank-
tonic foraminifera’ and ‘
δ
13
C of G. trilobus’, load this factor
positively, accompanied by ‘differences in
δ
18
O between
planktonic and benthic foraminifera’ and ‘
δ
18
O of H. ele-
gans’ (Table 3b,c). ‘Cold-water planktonic foraminifera’, ac-
companied with ‘abundance of planktonic foraminifera’ and
‘reworked nannoplankton’, cause negative loadings.
This factor reflects surface productivity, indicated by the
high
δ
13
C of the shallow dwelling G. trilobus, a species that
prefers warm water coupled with a high degree of stratifica-
tion (Table 3b,c). These dependencies of Factor 5 explain
the significant negative correlation to the temperature Fac-
tor 1 characterizing cold-water masses (Table 3d). Using fac-
tor scores as scales, variations of the temperature factor are
weakly negatively mirrored by the productivity Factor 5
(Fig. 6).
Paleoenvironmental interpretation
Relating the numerical factors obtained by latent structure
analysis to the main environmental parameters influencing
the distribution of organisms in the sea enables reconstruc-
tion of the environment in the Paratethys of the southern
Vienna Basin and its changes during the late Early Badenian
between —14.379 and —14.142 Myr. This precise dating (Ho-
henegger et al. 2008) allows evaluation of the variation of in-
solation, e.g. intensity of the sunlight that depends on orbital
cycles during this time. Using Laskar et al. (2004), we calcu-
lated the insolation for summer months at 65° N for the time
interval represented by the Baden-Sooss section to determine
whether they can explain the changes in environmental con-
ditions in the Badenian Sea on the southwestern border of
the Vienna Basin. Although the environment changed con-
tinuously, the sequence could be partitioned into stratigraph-
ic units deposited under similar conditions. These units are
discussed in detail below (Fig. 6).
Unit 1 (101 m to 102 m; —14.379 Myr to —14.377 Myr)
The environment during deposition of the deepest part of
the section can be reconstructed as fully marine with water
depth around 300 m. In spite of warm temperatures and well-
stratified water masses, oxygen depletion of the sediment
was not extreme. The input of terrigenous particulate organic
material rich in oxygen as well as the export productivity
from the surface waters remained at a medium level (Fig. 6).
The trace fossil Trichichnus indicating firm bottom reacted
to the decreased input of oxygen, and high proportions of in-
benthic foraminifera are explained through the dysaerobic
conditions. Surface waters were characterized by abundant
warm-water planktonic foraminifera (Globigerinella, Globo-
quadrina) and the calcareous nannoplankton assemblage
with warm-water indicators Reticulofenestra and Spheno-
lithus.
Unit 2 (92 m to 101 m; —14.377 Myr to —14.359 Myr)
The temperature decreased during this interval, reaching a
minimum around 97 m, afterwards returning to mean tem-
peratures at 93 m. This parallels the insolation curve as well
as the signal for stratified water masses (Fig. 6). Both fac-
tors, cold and non-stratified water do not lead to major
changes in oxygenation. On the contrary, moderate dysoxia
at the beginning of this interval decreased continuously until
its end. This decline can be explained by the rise in oxygen-
rich particulate organic material. Increasing bottom instabili-
ty is mirrored in the proportion of the Nereites dominated
ichnofabric type 6. Additionally, the number of inbenthic
foraminifera decrease continuously while oxyphylic taxa be-
come important. Among planktonic foraminifera, the “five-
chambered globigerinds” and Turborotalita indicate cold
non-stratified water masses as does the nannoplankton spe-
cies Coccolithus pelagicus.
Unit 3 (89 m to 92 m; —14.359 Myr to —14.353 Myr)
This is a short transitional interval. Temperatures re-
mained at a medium level. Stratification and surface produc-
tivity increased together with a decline in terrigenous
oxygen-rich organic material. Ichnofabric type 3 with Scoli-
482
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
cia replaced Trichichnus of the previous period suggesting a
higher sedimentation rate (Pervesler et al. 2008) in this unit.
A few laminated layers are visible (Wagreich et al. 2008).
Higher sedimentation rates are also indicated by the magnet-
ic susceptibility (Fig. 2a). Percentages of inbenthic foramin-
ifera decreased, while oxyphylic forms increased slightly.
Globorotalia dominated the planktonic foraminifera, with
lower proportions of the warm-water Globigerinoides.
Unit 4 (80 m to 89 m; —14.353 Myr to —14.344 Myr)
This unit is characterized by abundant mm thick lamina-
tions, especially between 82 m and 85 m (Wagreich et al.
2008) and high magnetic susceptibility (Fig. 2a). The tem-
perature was warm and conditions became the most olig-
otrophic of the entire section. During the times of maximum
lamination, the waters were well oxygenated and the input of
terrigenous oxygen-rich particulate organic matter reached a
minimum (Fig. 6). The lamination, partly destroyed by the
opportunistic Phycosiphon, can be explained by the higher
sedimentation rates impeding bioturbation (Pervesler et al.
2008).
Dating of the sequence indicates a mean sedimentation
rate of 470 mm/kyr for the deeper, tectonically unaffected
part (Hohenegger et al. 2008). Distances of ~1 mm between
the dark lamellae in the main laminated part at 84.5 m cor-
respond to an annual sedimentation rate of 1000 mm/kyr,
roughly doubling the ‘normal’ sedimentation rate, and is
reflected in the peak in magnetic susceptibility (Fig. 2a).
Stretching the insolation curve to correct for the higher sed-
imentation rate, shows a maximum corresponding to the
peak in temperature (Fig. 6). Oxyphylic benthic foramin-
ifera are abundant and the proportion of inbenthics is low
(Fig. 4c,d). The planktonic foraminifer Globorotalia domi-
nates throughout the unit, indicating waters deeper than
240 m. This genus is accompanied in the lower and upper
part of the unit by Globigerinoides and in the strongly lam-
inated central part of the unit by the warm-water indicators
Globigerinella and Globoquadrina (Rupp & Hohenegger
2008). Globigerinoides and Globigerinita are abundant in
the transition to the succeeding unit 5. Reticulofenestra
minuta dominates the calcareous nannoplankton, some-
times accompanied by Sphenolithus. Beside these warm-
water indicators, Umbilicosphaera jafarii, characteristic for
warm and slightly hypersaline water, makes its first appear-
ance (Ćorić & Hohenegger 2008).
Unit 5 (73 m to 80 m; —14.344 Myr to —14.323 Myr)
This interval marks a transition from warm to cooler water
conditions (Fig. 6). Declining temperature is coupled with an
increase in eutrophication (Fig. 6). The input of oxygen-rich
particulate organic material is high, thus the ichnofabric type
with Nereites needing oxygen rich sediments dominates. At
the end of this interval, bottom conditions become more oxy-
gen depleted as indicated by Zoophycus and Scolicia (Per-
vesler et al. 2008). The increase in eutrophication is also
documented in the decline of oxyphylic and the increase of
inbenthic foraminifera (Fig. 4c,d). The planktonic foramini-
fer Globorotalia dominates the whole unit, where Globiger-
inoides has its maximum in the deeper part and is abundant
up to the end of the interval (Rupp & Hohenegger 2008).
Coccolithus pelagicus indicating non-stratified cooler water
becomes more common than in the previous unit, while the
warm water species R. minuta decreases. The abundant U.
jafarii as an additional warm-water species hint to the less
cooling during this interval (Ćorić & Hohenegger 2008).
Unit 6 (62 m to 73 m; —14.323 Myr to —14.301 Myr)
Together with the subsequent unit, this interval is character-
ized by low but constant terrestrial sediment input as indicated
by magnetic susceptibility (Fig. 2a). Temperature continues
the decline that started in the previous period, while eutrophi-
cation perpetuates at a medium level (Fig. 6). Water mass
changes from well- to non-stratified water and the input of
oxygen-rich particulate organic material remains high, while
shallow water productivity weakens during this interval. Dur-
ing high oxygen-rich input of particulate organic material, the
ichnofabric type with Nereites dominates. Decrease of this in-
put in the uppermost part leads to dysoxic bottom conditions
and the first Thalassinoides ichnofossil appears (Fig. 4b). The
proportion of inbenthic foraminifera is high in the deeper part
and decreases towards the upper part, whereas oxyphylic taxa
are of low to medium abundance (Fig. 4d). Globorotalia
reaches its highest proportions in this unit, and along with
“four-chambered globigerinids” dominates the planktonic
foraminifera. The nannoplankton U. jafarii reaches its highest
proportion in this unit. Reticulfenestrids are of medium abun-
dance, while the proportion of C. pelagicus is high, but not ex-
treme, confirming the cooler conditions during this interval
(Ćorić & Hohenegger 2008).
Unit 7 (49 m to 62 m; —14.301 Myr to —14.275 Myr)
Temperature cools to a local minimum at 58 m, afterwards
rising slightly to a medium level at 50 m. This tendency is also
pictured in a distinct lack of stratification of the water mass.
Oxygen depletion reaches a maximum at 52 m that is the high-
est for the deeper, tectonically unaffected part of the section
(Fig. 6). This maximum coincides with a peak in shallow-water
productivity, whereas the input of particulate organic material
gets a minimum. Ichnofabric type 1 with Thalassinoides, which
prefers dysoxic bottom conditions shows its highest proportions
during this period (Pervesler et al. 2008). Inbenthic foraminifera
increase to a maximum at 53 m, where a minimum in oxy-
phylic species is observed (Fig. 4d). The slightly increasing in-
put of oxygen-rich particulate organic material at the end of this
unit, which is also marked by an increment of coarse-grained
sediments (Wagreich et al. 2008), leads to higher abundance of
the benthic foraminifer Trifarina angulosa, which prefers well-
aerated, turbulent bottom water (Báldi & Hohenegger 2008).
Colder water planktonic foraminifera dominate in the lower part
of the interval, but their abundance decrease, when warm-water
planktonic foraminifera like Globigerinella and Globoquadrina
become abundant (Fig. 5a,b; Rupp & Hohenegger 2008). Dom-
inance of the nannoplankton R. minuta, abundant C. pelagicus
together with the complete lack of Sphenolithus indicate medi-
483
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
um water temperature and lower salinity (Ćorić & Hohenegger
2008). The latter is additionally documented by the benthic for-
aminifer Trifarina angulosa (Báldi & Hohenegger 2008).
Unit 8 (38 m to 49 m; —14.275 Myr to —14.258 Myr)
The temperature increased during this interval. This ten-
dency is correlated with a trend toward oligotrophic condi-
tions. Although temperatures were high, the increased
stratification of the water mass is interrupted at 43 m. This is
also reflected in a lower input of particulate organic material.
The sea bed sediments were oxygen depleted at the begin-
ning of the interval, characterized by ichnofabric type 1 with
Thalassinoides, but later became oxygenized as a result of
increased terrigenous input indicated by a maximum of mag-
netic susceptibility (Fig. 2a). Nereites becomes the dominant
ichnofossil in the younger interval. After the strong increase
of inbenthic foraminifera in the previous interval, a slight de-
cline in their abundance between 42 m and 49 m is followed
by a large increase at the end (Fig. 4c). The benthic foramin-
ifer T. angulosa is abundant in the lower part (Báldi & Ho-
henegger 2008) but decreases towards the end. The
proportion of the warm water planktonic foraminiferal gen-
era Globigerinoides, Globigerinella and Globigerinita in-
creases (Rupp & Hohenegger 2008). Dominance of the
nannoplankton R. minuta together with fewer sphenolithids
indicates the warm water and euryhaline conditions in the
upper part of the unit (Ćorić & Hohenegger 2008).
Unit 9 (35 m to 38 m; —14.258 Myr to —14.237 Myr)
The first major tectonic disturbances can be seen in the
lower part of this unit, between 35 m and 37 m (Wagreich et
al. 2008). They are indicated by a strong decrease in magnet-
ic susceptibility at the beginning of the period separating it
from the previous interval. Environmental conditions
changed rapidly. The temperature increased to a maximum at
37 m and suddenly changes back to colder at the end of the
interval. Oxygen depletion shows the opposite trend and the
input of particulate organic material follows the same trend.
Stratification of the water column was initially high but de-
creased suddenly with sinking temperatures (Fig. 6). Shal-
low water productivity continued to decrease. Magnetic
susceptibility is high, indicating intensified input of terrige-
nous material. Laminations also suggest an increased sedi-
mentation rate. Thus, bottom conditions are similar to the
middle part of unit 4 between 82 m and 85 m. The opportu-
nistic ichnofossil Phycosiphon dominates (ichnofabric
type 4; Pervesler et al. 2008) and Nereites becomes abundant
at the end of this interval. The proportion of inbenthic fora-
minifera is low at the beginning and increases rapidly until
the end of the interval. Trifarina angulosa declines until the
end of this period, reaching ‘normal’ proportions there (Bál-
di & Hohenegger 2008). After a maximum of colder water
planktonic foraminfera at the beginning of the interval,
warm-water genera like Globigerinoides, Globigerinella and
Globigerinita become abundant but are replaced at the end
by colder water “five-chambered globigerinids” (Rupp &
Hohenegger 2008). Environmental changes are also mirrored
in calcareous nannoplankton. The colder water indicator C.
pelagicus marks the beginning and the end of the interval ac-
companied by > 5 % reworked nannoplankton, the warm-
water indicators R. minuta and S. heteromorphus are
abundant during the middle part of the unit. The normally
rare S. heteromorphus reaches its highest abundance ( > 3 %)
in the entire sequence (Ćorić & Hohenegger 2008).
Unit 10 (27 m to 35 m; —14.237 Myr to —14.210 Myr)
An approximately 50 cm thick conglomerate layer is de-
veloped between 27.2 m and 27.7 m and significant tectonic
faults are visible between 29 m and 30 m and at 35 m
(Wagreich et al. 2008: Appendix 1B,C). Magnetic suscepti-
bility is lower than in the previous period, but there is in-
tense variability correlated with high terrestrial input at the
beginning and end of the interval. The temperature declined
sharply with a minimum at the end, and the waters became
more dysoxic (Fig. 6). The water column varied between
non-stratified and weakly stratified and the input of terrige-
nous particulate organic material as well as surface produc-
tivity reached a local minimum at 30 m (Fig. 6). The
laminations from the previous period continue, but disappear
in the middle of the unit to return and increase again towards
the end (Wagreich et al. 2008). Ichnofabric type 4, with the
pioneer Phycosiphon crossing the lamellae, is frequent at the
bottom and at the top of the unit, whereas the weakly-stabi-
lized bioturbated bottom sediment of the lower part of the
unit show ichnofabric type 6 with Nereites. This was later re-
placed by ichnofabric type 1 dominated by Thalassinoides
characterizing firm bottom conditions. Proportions of in-
benthic foraminifera increase reaching maximum percentag-
es at the end of the period, while oxyphylic species are rare.
Oxygen depletion during the later part of this interval is also
manifested in the deep infaunal species Bolivina elongata. It
reaches an abundance maximum of 30 % at 27 m (Báldi &
Hohenegger 2008: fig. 3a). Colder water “five-chambered
globigerinids”, Globorotalia and “four-chambered globiger-
inids” constitute > 90 % of planktonic foraminifera (Rupp &
Hohenegger 2008: figs. 2, 4). The abundance of the colder
water nannoplankton species C. pelagicus is highest in this
unit, where peak occurrences coincide with non-stratified
water masses (Fig. 5e). Abundant reticulofenestrids indicate
more stratified water in the middle part and at the end of the
period (Ćorić & Hohenegger 2008).
Unit 11 (21 m to 27 m; —14.210 Myr to —14.192 Myr)
The upper two meters of this unit are strongly affected by
tectonics (Wagreich et al. 2008: Appendix 1B). The magnet-
ic susceptibility is highly variable, suggesting varying terrig-
enous input. The temperature increased from a minimum at
the beginning of the interval to a more moderate level at the
end. Oxygen depletion decreased after an initial maximum
(Fig. 6). The initially non-stratified water mass tends to-
wards weak stratification with a sharp return to non-stratified
conditions at 22 m. Input of particulate organic material in-
creased while that from shallow productivity remained mod-
erate; both decline sharply at 22 m (Fig. 6). Ichnofabric
484
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
types also change from laminations overprinted by Phycosi-
phon (ichnofabric type 4 in Pervesler et al. 2008) to pure
Nereites-dominated sediments (ichnofabric type 5_2 in Per-
vesler et al. 2008), then to dysoxic bottom conditions as
characterized by Thalassinoides (ichnofabric type 1). The
proportion of inbenthic foraminifera remains high, between
40 and 50 %, whereas oxyphylic taxa show low percentages
(Fig. 4c,d). The deep infaunal species Bolivina elongata
reaches its second maximum of 30 % at 22.5 m, then de-
creases upwards (Báldi & Hohenegger 2008). Colder water
planktonic foraminifera, especially the “five-chambered glo-
bigerinids”, Globigerinita and Globoturborotalita, which
dominated the previous unit decrease slightly. The warm-
water indicator Globigerinoides reappears in extremely low
proportions at the end of the interval. The incomplete record
of planktonic foraminifera resulting from the large sample
spacing cannot resolve the break in the other environmental
variables at 22 m. The better record of calcareous nanno-
plankton clearly demonstrates this change with C. pelagicus,
attaining maximum abundance (16 %) at 22 m and by the
highest proportion (20 %) of reworked nannofossils (Ćorić
& Hohenegger 2008).
Unit 12 (16 m to 21 m; —14.192 Myr to —14.171 Myr)
Magnetic susceptibility is the lowest within the upper part
of the section between 8 m and 40 m, but variability is high
indicating major changes in terrigenous input. The tempera-
ture increases slightly from medium to high, then decreases
rapidly at 17 m. This is also documented by the change from
highly stratified to weakly stratified waters at 19 m (Fig. 6).
Oxygen depletion becomes intense at 17 m. Input of terrige-
nous particulate organic material is high and shallow produc-
tivity tended to a maximum. The opportunistic ichnofossils
Phycosiphon and Nereites dominate during this period after
initial presence of Thalassinoides (Pervesler et al. 2008). In-
benthic foraminifera are dominated by Bolivina viennensis
but are slightly less abundant than in the preceding unit. Pro-
portions of oxyphylic species increase rapidly, but this may
be caused through reworking and transport from shallower
regions (Fig. 4d). The decrease in colder water planktonic
foraminifera continues, with a minimum of 40 % at 16 m,
while warm water foraminifera, especially Globigerinoides,
increase to a maximum of 40 % at the same depth
(Fig. 5a,b). The lower temperature of the water at 17 m depth
is mirrored by the increase of the nannoplankton species C.
pelagicus. Reworked nannoplankton indicate input from the
land (Ćorić & Hohenegger 2008).
Unit 13 (? 8 m; 10 m to 16 m; —14.171 Myr to —14.149 Myr)
After a strong increase at the beginning of the unit, mag-
netic susceptibility attained the third maximum peak along
the section at 14 m (Fig. 2a) followed by a decrease to 8 m
(Fig. 2a). Temperatures remained constantly high, similar to
the input of terrigenous particulate organic material. In con-
trast to the usual opposite behaviour between temperature
and oxygen depletion, the latter remains high during this in-
terval. Water masses were well stratified. Shallow water pro-
ductivity was extremely high at the bottom of the unit but
decreased rapidly upwards. The well-oxygenized sea floor
was favourable for ichnofabric type 6 with Nereites.
Thalassinoides, Scolicia and Trichichnus characterized oxy-
gen depleted bottom conditions at the end of the interval
(Pervesler et al. 2008). Percentages of inbenthic foraminifera
are always high, around 40 %, but increase considerably
from 10 m to 8 m (Fig. 4c). Oxyphylic benthic foraminifera
parallel the trend in inbenthics, but this could be caused by
transport from shallower regions (Báldi & Hohenegger
2008). This is also supported by the extremely high propor-
tion of reworked nannoplankton. During this interval, the
cold water planktonic foraminifera suddenly decrease at
14 m replaced by warm water planktonic genera. This
change is also marked by the dominance of the warm water
nannoplankton species U. jafarii at 14 m replacing the high
proportions of the colder water indicator C. pelagicus else-
where (Ćorić & Hohenegger 2008).
Conclusion
The stratigraphic sequence cored at Baden-Sooss allows re-
construction of the paleoenvironment and changes during the
late Early Badenian, just prior to the time the stratotype sedi-
ments of the Badenian were deposited. The position of the lo-
cality on the southwestern border of the small Vienna Basin
close to the Alpine landmass complicates the paleoceano-
graphic interpretation, which is traditionally based on proxies
and variables typical of the open ocean. For instance, stable
oxygen isotopes cannot be used as paleotemperature indica-
tors in the Badenian Sea of the Vienna Basin because of the
varying salinities caused by the freshwater input from nearby
landmasses and because the restricted Vienna Basin had only
narrow connections to the larger water body of the Pannonian
Sea (Kováč et al. 2004; Strauss et al. 2006). The shape and
depth of the basin, together with the opening and closing of
connections to the Pannonian Sea/Paratethys, influenced
both the shallow and deep water circulation (Colling 2001).
Stratification of the water mass has to be interpreted carefully.
The few measurements of Ca/Mg-ratios of the aragonitic fora-
minifer Hoeglundina elegans indicate bottom water tempera-
tures around 16.5 °C at water depths estimated to be between
—250 m and —300 m for the older part of the section, declining
to 14 °C in the upper part, which was deposited in water
depths between —200 m and —250 m. Although differences in
the uptake of Mg between species and even within a single
specimen (Toyofuku & Kitazato 2006) hamper precise estima-
tions, the slight temperature differences between surface
planktonic and benthic foraminifera in stratified water are sig-
nificant.
Stratification became somewhat better developed during
deposition of the upper strata. The middle of the thermocline
would be expected to be much deeper than the sea bottom at
this locality. The thermocline was probably fully developed
only in the center of the basin.
Evidence from the base of the section at 102 m
(—14.379 Myr) indicates high water temperatures and strati-
fied water masses. Both parameters decrease to a minimum
485
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
at 97 m (—14.368 Myr), then increase constantly upward.
The cooler period between 92 m and 100 m corresponds to
the insolation minimum between —14.376 and —14.360 Myr
(Laskar et al. 2004). Although temperatures were low, the
slightly disaerobic conditions at 102 m intensify, then be-
come more oxic again. Percentages of oxyphylic benthic
foraminifera, colder water planktonic foraminifera and the
cold water nannoplankton species Coccolithus pelagicus all
increase upward. Producers of the ichnofossils Phycosiphon
and Nereites sought particulate organic material rich in oxy-
gen as food, and reworked the sediment.
Between 73 m and 92 m (—14.357 Myr to —14.344 Myr) the
evidence suggests high temperatures. Magnetic susceptibility
is high, and the sediment input double the normal sedimenta-
tion rate, i.e. from around 400 mm/kyr to ca. 1000 mm/kyr.
The insolation curve shows two prominent peaks between
—14.360 and —14.300 Myr that could have been responsible
for strong seasonal changes causing higher weathering rates
and sediment input, while the weak trough between insolation
peaks had little influence on the main environmental trend.
The higher sedimentation rate is indicated not only by the
maxima in magnetic susceptibility, but also by the increased
input of reworked nannoplankton and by abundant, partly un-
disturbed 1 mm sediment laminations. Due to the well-strati-
fied water, the deeper waters were oxygen depleted, and the
proportion of inbenthic foraminifera becomes the lowest of
the entire section, but increases at the end of this interval.
Oxyphylic benthic foraminifera are abundant along with
warm water planktonic foraminifera (Globigerinoides) and
calcareous nannoplankton (reticulofenestrids, sphenolithids).
Bottom sediments were more prone to bioturbation at the be-
ginning and at the end of this unit. Conditions were optimal
for the pioneers Phycosiphon and Nereites. Phycosiphon was
able to reoccupy the laminated central part of this unit. Other
ichnofossils were excluded due to the high sedimentation rate.
Sedimentation rates were low and steady during deposi-
tion of the strata between 49 m and 73 m (—14.344 Myr to
—14.301 Myr), as indicated by the slight variability of mag-
netic susceptibility. Low temperatures induced oxygen deple-
tion. A temperature increase started at 52 m (—14.280 Myr)
and continued into the following periods. This ‘cool’ period
is divided into two parts, paralleling the insolation curve.
Stratification of the water masses decreased accompanied by
a peak in accumulation of particulate organic material. The
minima of both variables can be found in the middle of the
overlying unit around 56 m. Due to the stable bottom condi-
tions with low oxygen, the ichnofossil Thalassinoides,
which produced burrows with openings, appeared in the
lower part of this unit and became abundant in the upper
part. Proportions of inbenthic foraminifera are high. Colder
water planktonic foraminifera such as “five-chambered glo-
bigerinids” and Globorotalia, and the nannoplankton species
C. pelagicus dominate during this interval. Higher sedimen-
tation rates and low salinity at the end of this period are indi-
cated by absence of Sphenolithus and by presence of the
inbenthic foraminifer Trifarina angulosa.
The overlying ‘warm period’ between 38 m and 49 m
(—14.301 Myr to —14.275 Myr) is the last tectonically unaf-
fected section in the core. It contains the second maximum of
terrestrial sedimentary input as documented by magnetic sus-
ceptibility. This is suddenly interrupted by tectonic deforma-
tion between 36 m and 38 m. Temperatures were highest
during this period, but oxygen depletion was lower than in the
previous interval, remaining at moderate level. Water mass
stratification was interrupted around 43 m (—14.264 Myr) by
mixing. Oxygenation of the bottom waters is reflected in the
higher proportion of oxyphylic benthic foraminifera. The ich-
nofossil Nereites is abundant, while in the water column
warm-water planktonic foraminifera and nannoplankton are
abundant.
The upper part of the section is tectonically disturbed lead-
ing to a 43 % loss of the stratigraphic record (Hohenegger et
al. 2008). Comparison with the insolation curve becomes
more difficult. A major rapid cooling can be reconstructed be-
tween 35 m and 38 m (—14.258 Myr to —14.237 Myr), then
slowing to reach a minimum temperature around 26 m
(—14.211 Myr). Oxygen depletion shows the opposite trend
reaching a maximum at the same depth. Both environmental
factors tend to an average level at 21 m (—14.192 Myr). Strati-
fication of the water varied strongly during this interval and
the proportion of inbenthic foraminifera is high. The abun-
dance of all benthic foraminifera becomes the highest of the
entire sequence. Due to changing bottom conditions, Nereites
dominates the ichnofauna alternating with Thalassinoides.
Planktonic foraminifera are almost exclusively colder water
forms, while the nannoplankton C. pelagicus is abundant.
The youngest strata from 8 m to 21 m (—14.192 Myr to
—14.142 Myr) are characterized by the third maximum of
magnetic susceptibility corresponding to an insolation maxi-
mum. Extreme amounts of reworked nannoplankton docu-
ment higher sediment input. Temperature is relatively high
and oxygen depletion, normally opposite to temperature, re-
mains at an elevated level. The proportion of inbenthic fora-
minifera is also higher compared to the earlier warm-water
periods. The proportion of pelagic cold-water indicators like
C. pelagicus remains higher than in other warm-water peri-
ods, whereby alternations with the warm-water, higher salin-
ity indicator Umbilicosphaera jafarii suggest apparently
rapid environmental changes, but this may be a reflection of
the discontinuous sedimentary record.
The tectonic deformation of this part of the section pro-
duces artificially rapid changes by interrupting otherwise
continuous sedimentation. Stronger oscillations of magnetic
susceptibility in the upper part of the section compared to the
lower part, together with the increased input of sediment in-
dicated by the reworked nannoplankton and shallow water
benthic foraminifera as well as by the coarse-grained materi-
al (sands and conglomerates), documents the greater tectonic
activity during deposition of the younger strata.
General trends during deposition of the sequence are de-
clining temperatures and increasing oxygen depletion. The
only effect of the slight shallowing from —260 m to —240 m
water depth was on the decreasing abundance of a few deep
dwelling planktonic foraminifera (e.g. Globorotalia).
The precise dating of the core between —14.379 and
—14.142 Myr allows correlation of the environmental chang-
es with the global paleoclimate (e.g. Zachos et al. 2001;
Shevenell et al. 2004; Holbourn et al. 2007) taking into ac-
486
HOHENEGGER, ANDERSEN, BÁLDI, ĆORIĆ, PERVESLER, RUPP and WAGREICH
count the position of the Badenian Sea as a marginal basin
separated from the main Paratethys through sills. Therefore,
periods with higher temperatures in the deeper part of the se-
quence led to strong differences between the mixed surface
layer and the upper thermocline during summer, while these
differences became weaker in winter. During ‘cooler’ peri-
ods, temperature differences between surface and bottom
waters were not so strong in summer and extremely weak in
winter, and vertical transport of nutrients was not hindered
by density differences. This is indicated by the higher plank-
ton productivity during cold periods, leading to peaks in or-
ganic carbon and calcium carbonate content.
The cooling tendency between ~ —14.7 and —13.9 Myr
(Phase 2 in Holbourn et al. 2007 after the Middle Miocene
‘Monterey’ carbon isotope excursion), when these sediments
were deposited, was mainly controlled by global climatic
factors. Low orbital eccentricity and obliquity led to en-
hanced organic burial, as can be shown by the higher
δ
13
C
ratios of Hoeglundina elegans and Globigerinoides trilobus
(Fig. 3c,d). Enhanced organic burial favoured atmospheric
CO
2
drawdown and global cooling. When insolation varia-
tions were minimal, as during the time of deposition of the
upper core, the ocean-climate system became more suscepti-
ble to CO
2
changes (Berger & Loutre 2003). Strong oscilla-
tions in the upper part of the section can be explained by the
fluvial input due to ‘cooler’ weather, i.e. stronger physical
erosion in the hinterland, together with tectonic movements
that brought coarser material into the basin.
The paleoenvironment of the Baden-Sooss core was con-
trolled primarily by varying insolation intensities depending
on orbital cycles. Seasonal changes strongly influenced tem-
perature and stratification of the water mass in the marginal
sea of the Vienna Basin. The general trend to lower tempera-
tures and increased oxygen depletion of the deeper waters
follows global climate changes, intensified or weakened by
local paleogeographic conditions.
Acknowledgments: The study was supported by the Projects
P13743-BIO, P13740-GEO and P16793-B06 of the Austrian
Science Fund (FWF). We thank Maksuda Khatun, Fred Rögl,
Anna Selge and Karl Stingl, coworkers in these projects, for
their help and discussion. Further thanks are due to Maria
Fencl, Wilfried Körner, Robert Scholger, Alfred Uchman and
Inge Wimmer-Frey for cooperation in various respects. Spe-
cial thanks are due to Willam W. Hay, who critically com-
mented the manuscript and improved the English text.
References
Abdul Aziz H., Di Stefano A., Foresi L.M., Hilgen F.J., Iaccarino
S.M., Kuiper K.F., Lirer F., Salvatorini G. & Turco E. 2008: In-
tegrated statigraphy and
40
Ar/
39
Ar chronology of early Middle
Miocene sediments from DSDP Leg 42A, Site 372 (Western
Mediterranean). Palaeogeogr. Palaeoclimatol. Palaeoecol. 257,
123—138.
Arnold A.J. & Parker W.C. 1999: Biogeography of planktonic Fora-
minifera. In: Sen Gupta B.K. (Ed.): Modern Foraminifera. Klu-
wer Academic Publishers, Dordrecht, 103—122.
Báldi K. 2006: Paleoceanography and climate of the Badenian
(Middle Miocene, 16.4—13.0 Ma) in the Central Paratethys
based on foraminifera and stable isotope (
δ
18
O and
δ
13
C) evi-
dence. Int. J. Earth Sci. (Geol. Rdsch.) 95, 119—142.
Báldi K. & Hohenegger J. 2008: Paleoecology of benthic foramin-
ifera of Baden-Sooss section (Badenian, Middle Miocene, Vien-
na Basin, Austria). Geol. Carpathica 59, 5, 411—424.
Bemis B.E., Spero H., Bijma J. & Lea D.W. 1998: Reevaluation of
the oxygen isotopic composition of planktonic foraminifera:
experimental results and revised paleotemperature equations.
Paleoceanography 13, 150—160.
Berger A. & Loutre M.-F. 2003: Climate 400,000 years ago, a key
to the future. In: Droxler A.W., Poore R.Z. & Burckle L.H.
(Eds.): Earths climate and orbital eccentricity: The marine iso-
tope stage 11 question. Geophys. Monogr. Ser. 137, Amer.
Geophys. Union, Washington, DC, 17—26.
Bicchi E., Ferrero E. & Gonera M. 2003: Paleoclimatic interpreta-
tion based on Middle Miocene planktonic Foraminifera: the
Silesio Basin (Paratethys) and Monteferrano (Tethys) records.
Palaeogeogr. Palaeoclimatol. Palaeoecol. 196, 265—303.
Chiessi C.M., Ulrich S., Mulitza S., Pätzold J. & Wefer G. 2007:
Signature of the Brazil-Malvinas Confluence (Argentine Ba-
sin) in the isotopic composition of planktonic foraminifera
from surface sediments. Mar. Micropaleontology 64, 52—66.
Cicha I., Papp A., Seneš J. & Steininger F.F. 1975: Badenian. In:
Steininger F.F. & Nevesskaya L.A. (Eds.): Stratotypes of Medi-
terranean Neogene stages. 2. VEDA, Bratislava, 43—49.
Colling A. (Ed.) 2001: Ocean circulation. The open University. But-
terworth & Heinemann, Milton Keynes, UK, 1—286.
Corliss B.H. 1991: Morphology and habitat preferences of benthic
foraminifera from the northwest Atlantic Ocean. Mar. Micro-
paleontology 17, 195—236.
Ćorić S. & Hohenegger J. 2008: Quantitative analyses of calcareous
nannoplankton assemblages from the Baden-Sooss section
(Middle Miocene of Vienna Basin, Austria). Geol. Carpathica
59, 5, 447—460.
Davis J.C. 2002: Statistics and data analysis in geology. John Wiley
& Sons, New York, XVI + 639 pp.
Espitaliè J., LaPorte J.L., Madec M., Marquis F., Leplat P., Paulet
J. & Boutefeu A. 1977: Méthode rapide de characterisation des
roches mères de leur potential pétrolier et de leur degree
d’evolution. Rev. Inst. Francaise Pétrole 32, 23—42.
Grossmann E.L. 1984: Stable isotope fractionation in live benthic
foraminifera from the Southern California borderland. Palaeo-
geogr. Palaeoclimatol. Palaeoecol. 47, 301—327.
Hammer O. & Harper D. 2005: Paleontological data analysis.
Blackwell Publishing, Malden, MA, 1—351.
Hilbrecht H. 1996: Extant planktonic foraminifera and the physical
environment in the Atlantic and Indian Oceans. Mitt. Geol. Inst.
Eidg. Techn. Hochsch. Univ. Zürich, Neue Folge 300, 1—93.
Hohenegger J. 2005: Estimation of environmental paleogradient
values based on presence/absence data: a case study using
benthic foraminifera for paleodepth estimation. Palaeogeogr.
Palaeoclimatol. Palaeoecol. 217, 115—130.
Hohenegger J., Ćorić S., Khatun M., Pervesler P., Rögl F., Rupp C.,
Selge A., Uchman A. & Wagreich M. 2008: Cyclostratigraphic
dating in the Lower Badenian (Middle Miocene) of the Vienna
Basin (Austria) – the Baden-Sooss core. Int. J. Earth Sci.
DOI 10.1007/s00531-007-0287-7.
Holbourn A., Kuhnt W., Schulz M., Flores J.-A. & Andersen N.
2007: Orbitally-paced climate evolution during the middle Mi-
ocene “Monterey” carbon-isotope excursion. Earth Planet. Sci.
Lett. 261, 534—550.
Jennrich R.I. & Sampson P.F. 1966: Rotation for simple loadings.
Psychometrika 32, 363—379.
Jorissen F.J. 1999: Benthic foraminiferal microhabitats below the sedi-
ment-water interface. In: Sen Gupta B.K. (Ed.): Modern foramin-
487
MULTIVARIATE ANALYSIS OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)
ifera. Kluwer Academic Publishers, Dordrecht, 161—179.
Khatun M. 2007: Sedimentary petrology of Miocene (Badenian)
sediments – comparison of the Southern Vienna Basin (Aus-
tria) and the Bengal Basin (Bangladesh). Unpubl. PhD Thesis,
University of Vienna, 1—108.
Kováč M., Baráth I., Harzhauser M., Hlavatý I. & Hudáčková N.
2004: Miocene depositional systems and sequence stratigraphy
of the Vienna Basin. Cour. Forsch.-Inst. Senckenberg 246,
187—212.
Krebs C.J. 1998: Ecological methodology. Harper & Row Publish-
ers, New York, NY, XII + 654pp.
Kroon D. & Darling K. 1995: Size and upwelling control of the sta-
ble isotope composition of Neogloboquadrina dutertrei
(d’Orbigny), Globigerinoides ruber (d’Orbigny) and Globiger-
ina bulloides d’Orbigny: examples from the Panama Basin and
Arabian Sea. J. Foram. Res. 25, 39—52.
Kruskal J.B. 1964: Nonmetric multidimensional scaling: a numeri-
cal method. Psychometrika 29, 115—131.
Krzanowski W.J. & Marriott F.H.C. 1995: Multivariate analysis.
Part 2. Classification, covariance structures and repeated mea-
surements. Arnold, London, VIII + 280pp.
Laskar J., Robulet P., Joutel F., Gastineau M., Correia A.C.M. &
Levrard B. 2004: A long-term numerical solution for the inso-
lation quantities of the Earth. Astronomy & Astrophysics 428,
261—285.
Lawley D.N. 1940: The estimation of factor loadings by the method
of maximum likelihood. Proc. Roy. Soc. Edinburgh, Ser. A60,
64—82.
Li Q., James N.P., Bone Y. & McGowran B. 1999: Palaeoceano-
graphic significance of recent foraminiferal biofacies on the
southern shelf of Western Australia: a preliminary study.
Palaeogeogr. Palaeoclimatol. Palaeoecol. 147, 101—120.
Murray J.W. 2006: Ecology and applications of benthic foramin-
ifera. Cambridge University Press, Cambridge, XI + 426pp.
Okada H. & McInyre A. 1979: Seasonal distribution of the modern
Coccolithophores in the western North Atlantic Ocean. Mar.
Biology 54, 319—328.
Papp A. & Steininger F. 1978: Holostratotypus des Badenien. Holos-
tratotypus: Baden-Sooss (südlich von Wien), Niederösterreich,
Österreich. Badener Tegel—Keferstein, 1828 (Unterbaden; M4b;
Obere Lagenidenzone). In: Papp A., Cicha I., Seneš J. & Stein-
inger F. (Eds.): Chronostratigraphie und Neostratotypen: Mi-
ozän der Zentralen Paratethys. Bd. VI. M
4
Badenien (Moravien,
Wielicien, Kosovien). VEDA SAV, Bratislava, 138—145.
Parker W.C. & Arnold A.J. 1999: Quantitative methods of data anal-
ysis in foraminiferal ecology. In: Sen Gupta B.K. (Ed.): Modern
Foraminifera. Kluwer Academic Publishers, Dordrecht, 71—89.
Pervesler P., Uchman A. & Hohenegger J. 2008: New methods for
ichnofabric analysis and correlation with orbital cycles exem-
plified by the Baden-Sooss section (Middle Miocene, Vienna
Basin). Geol. Carpathica 59, 5, 395—409.
Rohling E.J. & Cooke S. 1999: Stable oxygen and carbon isotopes
in foraminiferal carbonate shells. In: Sen Gupta B.K. (Ed.):
Modern foraminifera. Kluwer Academic Publishers, Dor-
drecht, 239—258.
Rupp C. & Hohenegger J. 2008: Paleoecology of planktonic forami-
nifera from the Baden-Sooss section (Middle Miocene, Bade-
nian, Vienna Basin, Austria). Geol. Carpathica 59, 5, 425—445.
Selge A. 2005: Cyclostratigraphy by means of mineral magnetic pa-
rameters in the middle Badenian (Middle Miocene) core Sooß /
Baden (Vienna Basin, Austria). Unpubl. Diploma Thesis, Uni-
versity of Leoben, 1—84.
Sharp Z. 2007: Principles of stable isotope geochemistry. Pearson
Prentice Hall, Upper Saddle River, NJ, XII + 344pp.
Shepard R.N. 1962: The analysis of proximities: multidimensional
scaling with an unknown distance function. I and II. Psy-
chometrika 27, 125—139, 219—246.
Shevenell A.E., Kennett J.P. & Lea D.W. 2004: Middle Miocene
Southern Ocean cooling and Antarctic cryosphere expansion.
Science 305, 1766—1770.
Spero H.J. & Lea D.W. 1996: Experimental determination of stable
isotope variability in Globigerina bulloides: implications for
paleoceanograohic reconstructions. Mar. Micropaleontology
28, 231—246.
Strauss P., Harzhauser M., Hinsch R. & Wagreich M. 2006: Se-
quence stratigraphy in a classic pull-apart basin (Neogene,
Vienna Basin). A 3D seismic based integrated approach. Geol.
Carpathica 57, 185—197.
Toyofuku T. & Kitatzato H. 2006: Mg/Ca micro-distribution in for-
aminiferal tests – implication of laboratory culture experi-
ments. Anuário do Instituto de Geocincias 29—1, 469—470.
Valiela I. 1995: Marine ecological processes (2
nd
edition). Springer
Verlag, New York, XIV + 686pp.
Van der Zwaan G.J., Jorissen F.J. & de Stitger H.C. 1990: The
depth dependency of planktonic/benthic foraminiferal ratios:
Constraints and applications. Mar. Geol. 95, 1—16.
Wagreich M., Pervesler P., Khatun M., Wimmer-Frey I. & Scholger
R. 2008: Probing the underground at the Badenian type locali-
ty: geology and sedimentology of the Baden-Sooss section
(Middle Miocene, Vienna Basin, Austria). Geol. Carpathica
59, 5, 375—394.
Wetzel A. & Uchman A. 2001: Sequential colonization of muddy
turbidites: examples from Eocene Beloveža Formation, Car-
pathian, Poland. Palaeogeogr. Palaeoclimatol. Palaeoecol.
168, 171—186.
Winter A., Jordan R. & Roth P. 1994: Biogeography of living coc-
colithophores in ocean waters. In: Winter A. & Siesser W.
(Eds.): Coccolithophores. Cambridge University Press, Cam-
bridge, 13—37.
Zachos J., Pagani M., Sloan L., Thomas E. & Billups K. 2001:
Trends, rhythms, and aberrations in global climate 65 Ma to
Present. Science 292, 696—693.