GeolCarp_Vol55_No2_199

PALEOMAGNETIC RESULTS FROM THE MIOCENE IN NORTHREN AUSTRIA 199

GEOLOGICA CARPATHICA, 55, 2, BRATISLAVA, APRIL 2004

199206

Fig. 1. Geological framework of the study area with sampling loca-

tions. TBG Grund, KUF Kuffern, ML Mailberg, LA Laa/

Thaya, KHD Kleinhadersdorf, GD Gainfarn, DA Deutsch-

Altenburg, RB Rohrbach.

NEW PALEOMAGNETIC RESULTS FROM THE MIDDLE MIOCENE

(KARPATIAN AND BADENIAN) IN NORTHERN AUSTRIA

ROBERT SCHOLGER and KARL STINGL

Institute of Geophysics, Montanuniversität Leoben, Peter-Tunner-Str. 25, 8700 Leoben, Austria; scholger@unileoben.ac.at

(Manuscript received June 5, 2003; accepted in revised form December 16, 2003)

Abstract: We present new paleomagnetic results from the Middle Miocene in the Molasse Zone and the Vienna Basin

system (Northern Vienna Basin, Wiener Neustadt Basin, Hainburg Swell, Mattersburg Bucht). The magnetic measure-

ments were aimed at supporting stratigraphic age determinations where the polarity patterns of the primary magnetiza-

tions enabled a magnetostratigraphic zonation. Karpatian sediments in Laa/Thaya (brickyard) yielded a reverse polarity

zone in the lower part (3.20 m) and a normal polarity zone in the upper part (6.10 m) of the sequence, which are assigned

to Chrons C5Cr and C5Cn.2n. Three other sites in the Molasse Zone yielded single polarity results (two normal and one

reverse polarity) for Badenian sediments. Only normal polarity was found in four sites of Badenian age from the Vienna

Basin system. The new paleomagnetic results from Middle Miocene basin sediments (Karpatian and Badenian Stages)

located North and East of the pre-Neogene Eastern Alpine Basement in Northern Austria show a general trend towards

counterclockwise rotation of some 20 degrees with respect to the present North direction (according to 30° rotation with

respect to the stable European continent). The observed rotation values and paleo-inclinations are in accordance with

previous paleomagnetic results from Karpatian deposits in the Korneuburg Basin and other parts of the Alpine-Carpathian

Foredeep.

Key words: Miocene, Austria, Alpine-Carpathian Foredeep, Vienna Basin, magnetic stratigraphy.

Introduction

The Molasse Zone in Austria is part of the Alpine-Carpathian

Foredeep, whereas the Vienna Basin, Styrian Basin and

Lavant Valley Basin represent the north-western margin of the

Pannonian Basin System in Austria (Royden & Horváth

1988). The South Burgenland Swell separates the Styrian Ba-

sin from the Pannonian Basin. The separation between the in-

dividual basins is incomplete (Flügel 1988; Kröll et al. 1988),

thus enabling a partial link between the subbasins (Fig. 1).

The Paratethys, separated from the Mediterranean Tethys in

the Early Oligocene, deposited its marine sediments in several

stages of transgressions and regressions (Rögl 1996;

Steininger et al. 1984). These stages also included re-opening

and closure of seaways to the Mediterranean. Temporary con-

nections of the Paratethys with the Indopacific Ocean are best

documented in the molluscan faunas containing several

Indopacific faunal elements. Correlation of biozones between

different Paratethys parts (Central- and Eastern Paratethys)

and other faunal provinces are complicated by the tectonic

events. Global faunal changes could occur delayed in the

Paratethys and endemic evolution of the Paratethys inhabit-

ants would continue meanwhile. The stratigraphy of the sedi-

mentary basin filling of the Paratethys encompasses the Oli-

gocene, Miocene and the Pliocene (Rögl 1996).

The magnetic measurements aimed at improving strati-

graphic age determinations where the polarity patterns of the

primary magnetizations provided a magnetostratigraphic zo-

nation. Earlier studies gave evidence for the suitability of the

rocks for paleomagnetic investigations. For instance, Mau-

ritsch (1972, 1975) and Pohl & Soffel (1982) observed prima-

ry magnetization vectors, which gave evidence for large rota-

tions of the Tertiary volcanics in the Styrian Basin. During the

last years, sediments of Ottnangian to Sarmatian age were col-

lected from several basins of the Eastern Alps and analysed

paleomagnetically. Márton et al. (2000) found a tendency of

larger rotations in the older intramontane basins sediments in-

dicating essentially Middle Miocene rotation.

200 SCHOLGER and STINGL

Scholger (1998) studied Miocene (Karpatian) sections in

the Korneuburg Basin. In the Teiritzberg waste disposal site,

a section of 4 meters thickness across a fossil rich layer was

excavated for paleomagnetic sampling. In the Obergänsern-

dorf sandpit, two parallel profiles of 6 meters thickness across

fossil rich layers and an overlapping section towards the

hanging wall were sampled. The overall mean magnetization

for the Teiritzberg and Obergänserndorf sites showed normal

polarity with evidence for a counterclockwise rotation of the

Korneuburg Basin of approximately 20 degrees with respect

to the present magnetic North direction and a paleolatitude of

34 degrees at the time of deposition (Scholger 1998).

Similar results were obtained in the Early Miocene Lignite

mining district of Voitsberg (Styrian Basin), with evidence

for a 20° counterclockwise rotation of the basin with respect

to present North direction (Mauritsch & Scholger 1998). A

detailed magnetostratigraphic section of the coal bearing se-

quence was studied with the task of an age determination for

the sediments (Steininger et al. 1998). The rich mammal fau-

na from the upper part of the hanging wall sequence, indica-

tive of Neogene mammal Zone MN4, allowed a biostrati-

graphic correlation of the normally magnetized part of the

section with Chron C5Dn and the lower, reversely magne-

tized part of the section with Chron C5Dr of the geomagnetic

polarity time scale (GPTS). Thermal treatment with tempera-

tures of 700 °C lead to a corresponding paleomagnetic result

for tuffites, which overlie the coal bearing sequence.

Methods

Sampling in the Molasse Zone included the section in the

locality Grund (TBG), which was excavated and studied in

detail (Æoriæ et al. 2004). Complementary results of Karpa-

tianBadenian age could be obtained from the former sandpit

Silberberg located 700 m south of Kuffern (KUF), the quarry

on the south-eastern slope of the Buchberg at Mailberg (ML)

and the brickyard in the eastern part of Laa/Thaya (LA) in the

Eastern Molasse Zone (Fig. 1, Table 1). The data for the Vi-

enna Basin comprise published results from sites in the Kor-

neuburg Basin (Teiritzberg and Obergänserndorf), a new site

in a gravel pit located 500 m south of Kleinhadersdorf (KHD)

in the Northern Vienna Sub-Basin, as well as one new site

from an excavation south-west of Gainfarn (GD) in the Wien-

Site

WGS84E WGS84N

Tectonic unit

Strat Lithology

Facies

Azimuth Dip

TBG Grund

16.059

48.639

Eastern Molasse Zone

clay, silt

marine

KUF Kuffern

15.653

48.317

Eastern Molasse Zone

clay, sand

shallow sea

149

Mailberg

16.157

48.671

Eastern Molasse Zone

lime marl

shallow sea, reef

150

LA2 Laa/Thaya

16.411

48.717

Eastern Molasse Zone

clay, silt

deep sea

LA3 Laa/Thaya/Profile

16.411

48.718

Eastern Molasse Zone

clay, silt

deep sea

KHD Kleinhadersdorf

16.594

48.661

Northern Vienna Basin

silt

delta

Gainfarn

16.176

47.950

Wiener Neustadt Basin

silt/clay

shallow sea

359

Deutsch-Altenburg 1

16.884

48.129

Hainburg Swell

limestone

shallow sea

206

Rohrbach

16.435

47.719

Mattersburg Bucht

clay

shallow sea

124

Table 1: Basic geographical and geological data of the paleomagnetic sampling localities in Northern Austria. TBG Grund, KUF

Kuffern, ML Mailberg, LA Laa/Thaya, KHD Kleinhadersdorf, GD Gainfarn, DA Deutsch-Altenburg, RB Rohrbach.

er Neustadt Sub-Basin. The easternmost part of the study area

was covered by sampling sites from the Hainburg Swell in the

Pfaffenberg quarry near Deutsch-Altenburg (DA), and from

the brickyard at Rohrbach (RB) located in the Mattersburg

Bucht (Fig. 1, Table 1). Importantly, all investigated sites have

been studied by means of other, independent stratigraphic

methods at the same time (Æoriæ et al. 2004).

Standard paleomagnetic sample cubes and cylinders for un-

consolidated rocks were used. Alternatively, oriented cores of

2.5 cm diameter were collected using a portable coring appara-

tus with a non-magnetic hollow drill bit, where drilling was

possible. Specimens were subjected to detailed stepwise de-

magnetization procedure (alternating field and/or thermal treat-

ment). During thermal demagnetization, the bulk susceptibility

of the specimens was routinely measured to observe possible

mineral transformations. Paleomagnetic data analyses included

principal component analysis based on visual inspection of or-

thogonal projections. Stepwise saturation, measurements of the

coercivity, demagnetization of the saturation magnetization

and Curie-point determinations helped to identify the magnetic

minerals in the sediments. Additional measurements of the

anisotropy of the magnetic susceptibility were intended to de-

scribe the sediment texture in terms of paleocurrent directions

and foliation planes. All measurements were carried out in the

Paleomagnetic Laboratory Gams of the University of Leoben.

Natural remanent magnetization (NRM) was measured on a

three-axis cryogenic dc-squid magnetometer with in-line de-

gausser (2G Enterprises). Geofyzika KLY-2 instruments were

used for measuring low-field magnetic susceptibility and its

anisotropy.

Results

Laboratory measurements

In the localities Grund and Kuffern, anisotropy of low-field

magnetic susceptibility gave reliable evidence for a primary

sedimentary origin of the magnetic fabric. Most of the speci-

mens did not show a statistically significant anisotropy at all,

and the remaining samples yielded susceptibility ellipsoids

which indicated depositional fabrics: the maximum suscepti-

bility axes (k1) were aligned in the horizontal plane, while the

minimum susceptibility axes (k3) formed clusters around the

PALEOMAGNETIC RESULTS FROM THE MIOCENE IN NORTHREN AUSTRIA 201

Table 2: Paleomagnetic results from the EarlyMiddle Miocene in Northern Austria. AF/TH number of samples treated with alter-

nating field or thermal demagnetization. Dec b.c., Inc b.c. declination and inclination of the mean characteristic remanent magnetiza-

tion vector before bedding correction. K concentration parameter. conf

confidence angle. Dec a.c., Inc a.c. direction after

bedding correction. n number of results for mean direction. N/R number of normal and reverse polarity results. k mean low-field

susceptibility (10

SI units). L magnetic lineation (k1/k2). F magnetic foliation (k2/k3). Mol area mean direction for the sites

from the Molasse Zone. V.B. area mean direction for the sites from the Vienna Basin and subbasins.

Fig. 2. Demagnetization behaviour and mineral magnetic characterization of samples from the Molasse Zone in Grund (TBG) and

Kuffern (KUF). Zijderveld diagrams showing NRM in the horizontal (filled symbols) and vertical plane (open symbols) during demagne-

tization. Change of NRM during demagnetization, IRM acquisition and backfield, and Curie-point determination.

pole to the bedding plane. Magnetic lineation (L = k1/k2) was

typically below 1.01, and the average magnetic foliation (F =

k2/k3) was 1.016 in Grund and 1.013 in Kuffern (Table 2).

The results suggest the presence of a weak or moderate pale-

ocurrent (NNWSSE) during the time of deposition. During

demagnetization, well defined demagnetization paths with up

to three components of NRM and a good separation of the un-

blocking coercivity spectra could be obtained. Typically, the

NRM decayed rapidly at low demagnetizing field strengths

and the samples were fully demagnetized at 100 mT alternat-

ing-field strengths (Fig. 2). Isothermal remanence acquisition

curves and backfield experiments indicated the dominance of

a low-coercivity magnetic carrier mineral with a remanence

coercivity below 50 mT. In some samples, a second magnetic

phase with higher coercivity was observed (Fig. 2 KUF

2.01). Only 25 % of the samples from the locality Grund

yielded good results. A well grouped normal polarity compo-

nent, which decayed towards the origin between 10 and

AF/TH Dec b.c. Inc b.c.

conf Dec a.c. Inc a.c.

conf

N/R

TBG

46/0

330

13/0

1.001

1.016

KUF

12/6

345

350

12/0

1.008

1.013

3/3

146

138

145

138

0/4

LA2

27/0

345

15/0

1.011

1.072

LA3

47/0

353

13/9

130

KHD

13/0

343

6/0

1.000

9/0

335

338

6/0

1.009

1.010

6/5

351

331

7/0

6/0

325

334

6/0

104

1.000

Mol

338.6

51.0

90.4

9.2

339.2

53.9

86.1

9.4

V.B.

336.7

48.8

27.9 20.6

336.6

57.3

139.1

9.0

202 SCHOLGER and STINGL

Fig. 3. Demagnetization behaviour and mineral magnetic characterization of samples from the Molasse Zone in Mailberg (ML). Stereo-

graphic projection and Zijderveld diagrams showing NRM in the horizontal (filled symbols) and vertical plane (open symbols) during de-

magnetization. Change of NRM during demagnetization, IRM acquisition and backfield, and Curie-point determination.

100 mT, could be isolated in 13 samples, mainly from profiles

F and H (Roetzel & Pervesler 2004). 12 samples from Kuffern

yielded demagnetization paths towards the origin between 3

and 50 mT. These components are regarded as the primary

characteristic remanence direction vectors.

The samples from Mailberg differed substantially from the

results described above. Magnetic susceptibility and NRM in-

tensity were typically very low. The samples could not be de-

magnetized in alternating fields up to 110 mT. The shape of

the IRM (isothermal remanent magnetization) acquisition

curves, remanence coercivity values of 400 mT and Curie-

points in the range of 620 °C indicate a hematite-like phase as

the dominant magnetic carrier (Fig. 3). Thermal demagnetisa-

tions yielded scattered demagnetization paths along great cir-

cles. Interestingly, the remanence vectors, which reside in the

hematite-like phase, represent a very well grouped reverse po-

larity component. Due to the weak susceptibility values,

anisotropy of magnetic susceptibility was insignificant for all

samples from Mailberg.

In the two neighbouring sites of the magnetostratigraphic

section in Laa/Thaya, we observed different magnetic carrier

minerals. Samples from the site LA2 can be described similar

to the samples from the site Grund, with a low coercivity mag-

netic carrier mineral (Fig. 4 LA2.01) and demagnetization

paths towards the origin. Contrastingly, the results of samples

from LA3 indicated an interchange of high and low coercivity

magnetic carriers in different stratigraphic levels. Curie-point

determinations were affected by changes in the magnetic min-

eralogy of the samples during heating at temperatures above

400 °C, which is usually attributed to a higher concentration

of pyrite (Fig. 4). Unfortunately, only 50 % of the studied

samples yielded demagnetization paths, that could be used for

the calculation of mean directions. Both polarities were

present, and the normal and reverse directions were aligned

antipodal. However, it has to be mentioned, that the reverse

polarity was always residing in the high coercivity phase, and

the mean characteristic direction for the reverse polarity group

had to be calculated by means of great circle intersection anal-

yses (Fig. 4).

Although there was variability as to the relative contribu-

tions of the respective remanence components, mostly the

same magnetic mineral associations were present in the sedi-

ments from the Vienna Basin system. Samples from Kleinha-

dersdorf in the Northern Vienna Sub-Basin and Gainfarn in

the Wiener Neustadt Sub-Basin are characterized by a rela-

tively uniform demagnetization behaviour and magnetic min-

eralogy. NRM was typically fully demagnetized at 50 mT al-

ternating field strengths. The majority of the demagnetization

paths showed simple two-component systems. A viscose

component could be removed with alternating fields of 1 to

10 mT. A second, low coercivity magnetic phase carried a

well grouped normal polarity component. During IRM acqui-

sition, magnetic saturation could be reached at low to interme-

diate fields, and Curie-points were observed at temperatures

below 600 °C (Fig. 5).

Results from Deutsch-Altenburg at the Hainburg Swell and

from the brickyard Rohrbach located in the Mattersburg

Bucht indicated a higher contribution of a high coercivity

phase, probably goethite. Some samples could not be fully de-

magnetized towards the origin by means of alternating field

204 SCHOLGER and STINGL

demagnetization, but showed demagnetization paths towards

an irremovable second vector component. In accordance with

this observation, the respective IRM acquisition curves

showed influence from a higher coercivity phase (Fig. 6).

However, isolated difference vectors in such samples yielded

significant grouping together with the results from samples

that were fully demagnetized. Curie-point determinations

were again affected by changes in the magnetic mineralogy of

the samples due to a higher concentration of pyrite (Fig. 6).

Characteristic remanence directions

The directions of the primary components, which were used

for the magnetostratigraphic zonation and calculation of

paleomagnetic mean directions, are presented in a stereo-

graphic projection in Fig. 7, and in Table 2. Characteristic re-

manent magnetization directions (ChRM) for single samples

were determined by principal component analyses of the mag-

netization components observed during thermal or alternat-

ing-field demagnetization. The quality of the demagnetization

data varied strongly in accordance with the different rock

types. 91 results from a total of 183 processed samples were

suitable for further analyses. The majority yielded consistent

demagnetization paths towards the origin, which indicated a

low coercivity carrier mineral, most probably magnetite, as

the primary carrier of the remanence. The second, smaller

group represents results from well defined difference vectors,

where demagnetization paths did not show decay towards the

origin.

The sites in the Molasse Zone were characterized by mostly

flat lying sedimentary bedding planes, disabling the applica-

tion of a paleomagnetic fold test to prove the relative age of

the remanence acquisition. However, the occurrence of nor-

mal and antipodal reverse directions (in Mailberg, as well as

within the magnetostratigraphic section in Laa/Thaya) gives

evidence for a primary nature of the magnetization vectors.

For instance, marls of Badenian age from the locality Mail-

berg in the Eastern Molasse Zone yielded a reverse compo-

nent (Dec = 145°, Inc = 47°), that is antipodal within the sta-

tistical confidence limits to the normal vector direction

observed in Grund (Dec = 330; Inc = 48).

In contrast, only normal polarity results were obtained from

the sites in the Vienna Basin system, but the pre-tectonic ori-

gin of the magnetization directions could be proved by a sig-

nificant area-scale fold test (Table 2). The concentration pa-

rameter of the area-mean direction for 4 studied sites in the

Vienna Basin system before and after bedding correction im-

proves from K = 27.9 to K = 139.1. The mean directions for

the Middle Miocene in the Molasse Zone (Dec = 339.2; Inc =

53.9) and the Vienna Basin system (Dec = 336.6; Inc = 57.3)

in Northern Austria are indistinguishable from each other

within statistical limits (Table 2).

Fig. 6. Demagnetization behaviour and mineral magnetic characterization of samples from the Vienna Basin system in Deutsch-Altenburg

(DA) and Rohrbach (RB). Zijderveld diagrams showing NRM in the horizontal (filled symbols) and vertical plane (open symbols) and ste-

reographic projection during demagnetization. Change of NRM during demagnetization, IRM acquisition and backfield, and Curie-point de-

termination.

PALEOMAGNETIC RESULTS FROM THE MIOCENE IN NORTHREN AUSTRIA 205

Fig. 7. Stereographic projection of the characteristic remanence magnetization directions after bedding correction. Equal area projection

with full symbols for lower hemisphere and open symbols for upper hemisphere. Mean values for normal and reverse polarity are shown

with

confidence intervals. The demagnetization planes shown for the Site Mailberg (ML) are not included in the mean value. See also

Table 2.

Conclusion

In the localities Grund and Kuffern well grouped normal

polarity components could be isolated, which are regarded as

the primary characteristic remanence direction vectors. Only

normal polarity was observed in both sites. The results from

Mailberg yielded a very well grouped reverse polarity compo-

nent in samples from a 20 cm marl layer, while no paleomag-

netic results could be obtained from the diamagnetic Leitha

limestone in the hanging wall and footwall of this layer. In the

profile in Laa/Thaya (brickyard), both polarities were present,

and the normal and reverse directions were aligned antipodal.

The lower part of the sequence (3.20 m) was characterized by

reverse polarity, the upper part (6.10 m) yielded only normal

polarity results. Compared with the stratigraphic time scale of

Berggren et al. (1995), the reverse is assigned to Chron C5Cr

and the normal to Chron C5Cn.2n (16.32716.488 Ma). The

normal chron also comprises the upper part of the Karpatian

as measured in the Korneuburg Formation (Æoriæ et al. 2004).

Only normal polarity is found in the sediments of Badenian

age from Kleinhadersdorf in the Northern Vienna Basin,

Gainfarn in the Wiener Neustadt Basin, Deutsch-Altenburg at

the Hainburg Swell and Rohrbach in the Mattersburg Bucht.

The new results from Middle Miocene basin sediments

(Karpatian and Badenian Stages) located North and East of

the Eastern Alpine Basement in Northern Austria show a gen-

eral trend for synsedimentary counterclockwise rotations of

some 20 degrees with respect to the present North direction

(according to 30° rotation with respect to the stable European

continent). The observed rotation values and paleo-inclina-

tions are in accordance with previous paleomagnetic results

from Karpatian deposits in Teiritzberg (Dec = 340°,

206 SCHOLGER and STINGL

Inc = 49°) and Obergänserndorf (Dec = 336°; Inc = 56°) in

the Korneuburg Basin (Scholger 1998). This pattern of rota-

tions is in accordance with paleomagnetic results from other

parts of the Alpine-Carpathian Foredeep (e.g. Márton et al.

2001).

Acknowledgements: This study is part of FWF Project

P13738 (Austrian Research Fund). For Zijderveld analyses

we used the PALDIR software of the Paleomagnetic laborato-

ry Fort Hoofdijk at the University of Utrecht (NL).

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