GeolCarp_Vol59_No4_307

GEOLOGICA CARPATHICA, AUGUST 2008, 59, 4, 307—317

www.geologicacarpathica.sk

Introduction

Accumulation  and  preservation  of  sediment  on  shallow
ramps  are  controlled  by  eustatic  sea  level,  subsidence,  the
hydrodynamic regime of the system, and the ramp morphol-
ogy.  Consequently,  lateral  and  stratigraphic  facies  changes
are  a  common  feature,  and  sediment  accumulation  rate  is
highly  variable  through  time.  Sea-level  fluctuations  of  dif-
ferent amplitudes and frequencies play an important role for
shallow  ramp  systems  and  are  recorded  in  a  hierarchical
stacking of depositional sequences.

Depositional sequences are defined as stratigraphic units

comprising  a  succession  of  genetically  related  strata
(Mitchum  et  al.  1977)  and  based  on  seismic  stratigraphy,
Vail et al. (1977) introduced the term first-, second-, and third-
order sequences with durations of 200—300 Myr, 10—80 Myr,
and  1—10 Myr,  respectively.  Later,  when  sequence  analysis
was first applied to outcrops, the detection of small-scale se-
quences  enabled  a  higher  time  resolution.  Thus,  Vail  et  al.
(1991)  distinguished  six  orders  of  depositional  sequences,
lasting from tens of millions of years to a few ten-thousand
years, with third-order sequences spanning a time interval of
0.5—3 Myr (Haq et al. 1987). Such third-order sequences are
usually called sequences or depositional sequences. Howev-
er, there is still a controversial discussion on the origin and
duration  of  third-order  sequences.  While  first-  and  second-
order  sequences  are  seen  to  be  related  to  tectonic  and  tec-
tono-eustatic  changes  and  fourth-,  fifth-  and  sixth-order  se-
quences  are  explained  by  climatically  driven  sea-level
fluctuations in the Milankovitch frequency band, third-order

Correlation of Tethyan and Peri-Tethyan long-term and

high-frequency eustatic signals (Anisian, Middle Triassic)

ANNETTE E. GÖTZ

and ÁKOS TÖRÖK

Darmstadt University of Technology, Institute of Applied Geosciences, Schnittspahnstr. 9, D-64287 Darmstadt, Germany;

goetz@energycenter.tu-darmstadt.de

Department of Construction Materials and Engineering Geology, Budapest University of Technology and Economics, Sztoczek út. 2,

H-1521 Budapest, Hungary; torokakos@mail.bme.hu

(Manuscript received September 17, 2007; accepted in revised form February 1, 2008)

Abstract: During Anisian times, broad ramp systems developed on the northwestern Tethys shelf and in the adjacent
Peri-Tethyan realm. In both paleogeographical settings carbonate series display characteristic cyclic patterns, reflecting
long-term and high-frequency eustatic sea-level changes. Facies successions recognized within the small-scale sedi-
mentary cycles document a rapid transgressive phase followed by a prolonged highstand phase. The erosional base of
these deposits is interpreted as a sequence boundary. Transgressive deposits are characterized by bioclastic limestones
with reworked lithoclasts. Bioturbated mudstones represent the highstand deposits. Sedimentation of laminated mud-
stones is documented during the late highstand phase. Maximum flooding is recognized by thin condensed marly layers
at the top of bioclastic beds. Such meter-scale sedimentary cycles are the basic stratigraphic building blocks of the
Anisian series of Hungary and Germany, representing ramp deposits of the proximal Tethys shelf and the northern Peri-
Tethys Basin, respectively. Comparison of both depositional environments leads to a better understanding of cyclic
sedimentation of shallow-water carbonates and controlling factors. Eustatic signals of different scales are analysed and
used for correlation of sedimentary series between different paleogeographical settings.

Key words: Anisian, Germany, Hungary, Peri-Tethys Basin, NW Tethys shelf, sedimentary cycles, carbonate ramps.

sequences  are  discussed  as  resulting  from  a  combination  of
tectonic and glacio-eustatic changes (Vail et al. 1991). Addi-
tionally, changes in intraplate stress (Cloetingh 1988) as well
as  a  combination  of  plate  rifting  and  convergence  superim-
posed on second-order volume changes of mid-ocean ridges
(Miall 1990) are under discussion causing third-order cyclic-
ity. Finally, Strasser et al. (2000) suggested the formation of
third-order depositional sequences, at least within a passive-
margin  setting  such  as  the  northern  margin  of  the  Tethys
Ocean,  being  related  to  the  400,000  year  eccentricity  cycle
of the Earth’s orbit.

Hierarchical stacked cyclic patterns are well documented

in the Anisian (Middle Triassic) carbonate series studied in
Germany and Hungary (Fig. 1) and enable a detailed analy-
sis of eustatic signals used for long-distance correlation.

Sedimentary cycles were first described from the Anisian

Muschelkalk series of NW Germany by Fiege (1938). Later,
Schüller  (1967)  and  Schulz  (1972)  published  sections  from
Lower  Saxony  and  N  Hesse  and  interpreted  small-scale  fa-
cies  successions  as  shallowing-upward  cycles.  A  first  se-
quence-stratigraphic interpretation of meter-scale cycles rec-
ognized  in  Lower  Muschelkalk  sections  from  Central
Germany  was  published  by  Götz  (1996).  Middle  Triassic
third-order depositional sequences (sensu Vail et al. 1991) of
the  eastern  part  of  the  Germanic  Basin,  and  corresponding
sedimentary deposits of the Alpine realm, were addressed in
the works of Szulc (1999, 2000).

In S Hungary, Middle Triassic ramp deposits of the Mecsek

Mountains show characteristic facies successions, related to
large-scale sea-level changes at the scale of third-order cy-

309

CORRELATION OF TETHYAN AND PERI-TETHYAN EUSTATIC SIGNALS (ANISIAN, MIDDLE TRIASSIC)

clicity  (Török  1998,  2000).  A  correlation  of  these  Tethyan
sequences  with  those  described  from  the  Peri-Tethys  Basin
was  first  published  by  Török  (2000).  New  biostratigraphic
data  (Götz  et  al.  2003;  Ruckwied  et  al.,  in  prep.)  enable  a
more  precise  correlation  of  Anisian  sequences  of  these  two
different  paleogeographical  settings.  The  composition  and
preservation  of  small-scale  sequences  within  this  ramp  sys-
tem is addressed by the present study for the first time.

A detailed description of the sedimentary facies and pa-

lynofacies of the sections in Central Germany and S Hunga-
ry is found in Török (1993, 1998), Götz (1996), Götz &
Feist-Burkhardt (1999) and Götz et al. (2003).

Geological setting

During Anisian times, Central Europe was subdivided into

two major depositional areas: The northwestern Tethys shelf
and  the  semi-enclosed  Peri-Tethys  Basin  (Germanic  Basin)
that was connected with the Tethys Ocean via gate ways in
the South (Fig. 2). Broad ramp systems developed along the
Tethys  shelf  and  in  the  adjacent  Peri-Tethys  Basin.  Today
outcrops in the Northern Calcareous Alps (Rüffer 1995), the
Western  Carpathians  (Michalík  et  al.  1992),  the  Dolomites

(Zühlke  2000)  and  southern  Hungary  (Török  1998)  docu-
ment the evolution of such ramps in the northwestern Tethy-
an  shelf  area  (Dercourt  et  al.  2000).  Muschelkalk  sections
described from the Netherlands (Pöppelreiter 2002), Central
Germany (Götz & Feist-Burkhardt 1999; Rameil et al. 2000)
and  Poland  (Szulc  2000;  Kedzierski  2002)  display  the  Ani-
sian  ramp  morphology  along  a  NW-SE  cross-section  in  the
Germanic realm.

In Central Germany and S Hungary (Mecsek Mts), the Ani-

sian  ramp  deposits  are  mud-dominated  (Götz  1996;  Török
1998). The major lithofacies type is bioturbated mudstone, the
so-called “Wellenkalk”. Bioclastic marker beds and fossil-rich
units are used for lithostratigraphic subdivision (Fig. 1). Bios-
tratigraphy  is  based  on  conodonts  (Kozur  1974;  Götz  1995;
Kovács  &  Rálisch-Felgenhauer  2005;  Ruckwied  et  al.,  in
prep.),  palynomorphs  (Mädler  1964;  Barabás-Stuhl  1993;
Götz et al. 2003; Ruckwied et al., in prep.) and crinoids (Hag-
dorn & Głuchowski 1993; Hagdorn et al. 1997).

Cyclic stacking patterns and eustatic evolution

The Anisian deposits of the Peri-Tethys Basin document

the evolution of a NW-SE striking homoclinal ramp system

Fig. 2. Paleogeography of the Middle Triassic, modified after Szulc (2000) and Haas (2001), based on data by Ziegler (1982) and Mostler (1993).

310

GÖTZ and TÖRÖK

with  a  characteristic  lateral  facies  distribution  of  lagoonal
marls  and  inner  ramp  peritidal  dolomites,  bioclastic  mid-
ramp  grain-/packstones  and  outer  ramp  mudstones  (Lukas
1991;  Götz  1996;  Pöppelreiter  2002).  The  stratigraphic  se-
ries is build up of bioturbated mudstones and bioclastic beds,
showing  characteristic  deepening-shallowing  trends.  The
basal mudstones of the Anisian (Lower Wellenkalk, Wellen-
kalk 1 Member) overlay the Upper Buntsandstein (Röt) silt-
stones  and  become  marlstones  up  section.  A  some  meters
thick marly interval in the middle part of the Lower Wellen-
kalk  is  overlain  by  bioturbated  mudstones  and  platy  mud-
stones  with  bioclastic  grainstones  (Oolithbank  Member)  on
top. The succeeding bioturbated mudstone package (Middle
Wellenkalk,  Wellenkalk 2  Member)  is  overlain  by  brachio-
pod  grain-/packstones  (Terebratelbank  Member).  A  third
platy  mudstone  series  (Upper  Wellenkalk,  Wellenkalk 3
Member)  with  bioclastic  peloid-grainstones  (Schaumkalk-
bank Member) terminates the Lower Muschelkalk carbonate
series.  The  biostratigraphic  framework  of  the  carbonate  se-
ries  studied  is  based  on  conodonts  (Götz  1995;  Narkiewicz
1999), indicating a Bithynian to early Illyrian age. Thus, the
correlation of the Anisian Tethyan and Peri-Tethyan series is
very  precise  and  enables  a  high  time  resolution.  The  strati-
graphic  stacking  of  these  sediments  displays  the  long-term
eustatic  history  of  the  Peri-Tethyan  realm  with  two  major
flooding phases (Fig. 3). The first transgressive phase during
the  Bithynian  is  recognized  in  the  Lower  Wellenkalk
(Wellenkalk 1 Member) mudstones with maximum flooding
in the uppermost part of this member, documented by a mar-
ly  interval  with  numerous  hardgrounds.  Bioclastic  grain-
stones of the Oolithbank Member represent the highstand de-
posits.  The  next  transgressive  pulse  occurred  within  the
Pelsonian  (Wellenkalk 2  Member)  and  culminated  with  the
deposition  of  thick  brachiopod  shell  beds  (Terebratelbank
Member)  representing  the  most  pronounced  Anisian  flood-
ing phase recognized over the whole Peri-Tethys Basin (Szulc
1999).  Mudstones  of  the  Upper  Wellenkalk  (Wellenkalk 3
Member)  are  interpreted  as  early  highstand  deposits.  Pro-
grading shoal deposits of the uppermost Lower Muschelkalk
(Schaumkalkbank Member) are a characteristic sedimentary
feature of the late highstand phase.

Characteristic meter-scale facies successions build small-

scale  sequences.  These  are  the  basic  stratigraphic  blocks  of
the  third-order  depositional  sequences  (Götz  &  Feist-
Burkhardt 1999), and represent simple sequences sensu Vail
et  al.  (1991)  and  small-scale  sequences  after  Strasser  et  al.
(1999), respectively. Götz (1996) interpreted these cycles as
high-frequency  cycles  that  display  orbital  induced  high-fre-
quency sea-level changes during Anisian times (Götz 2002,
2004).  Stacked  small-scale  sequences  form  characteristic
sets  of  3  to  4  sequences  (Rameil  et  al.  2000;  Kedzierski
2002) that are characteristic features of the third-order depo-
sitional sequences described by Aigner & Bachmann (1992)
and Szulc (1999).

Depending on the position within the ramp system, sedi-

mentary cycles show a spatially different development of fa-
cies successions. Deposits of the proximal ramp in the west-
ern part of the Peri-Tethys Basin show asymmetrical
sequences (Götz 1994, 1996; Rameil et al. 2000; Götz &

Wertel  2002).  Bioclastic  beds  with  reworked  hardground
pebbles  represent  the  transgressive  phase.  Since  pebbles
were  reworked  during  transgression,  the  hardground  may
correspond to the sequence boundary. Bioturbated and lami-
nated  mudstones  are  interpreted  as  highstand  deposits
(Fig. 4). Maximum flooding is recognized by thin condensed
marly layers at the top of bioclastic beds. Lowstand deposits
are not recorded so that the transgressive surfaces at the base
of bioclastic beds directly overlie the sequence boundaries or
even  erode  it  away  (Götz  1996;  Rameil  et  al.  2000).  Re-
worked lithoclasts at the base of bioclastic beds derive from
mudstones  or  hardgrounds  below  these  beds;  they  may  be
completely reworked or are partially eroded. These erosional
(ravinement)  surfaces  are  developed  within  the  entire  basin
and are used for basin-wide high-resolution correlation (Pöp-
pelreiter 2002; Götz 2004; Fig. 5).

Deposits of the distal ramp are represented by nodular and

platy mudstones and crinoidal wackestones/packstones,
showing symmetrical cycle patterns (Kedzierski 2002;

Fig. 3. Third-order depositional sequences of the Anisian in Central
Germany and Southern Hungary. Abbreviations: sb – sequence
boundary, TSd – transgressive deposits, mfz – maximum flood-
ing zone, eHSd – early highstand deposits, lHSd – late highstand
deposits. M.M. – Middle Muschelkalk.

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GÖTZ and TÖRÖK

Fig. 5).  Highly  proximal  sedimentary  series  are  character-
ized  by  small-scale  sequences  built  of  dolomitic  mudstones
and  red  marlstones  of  the  lagoonal  and  inner  ramp  setting.
These sediments represent highstand deposits. Due to perma-
nent reworking, transgressive deposits are recorded by a peb-
ble lag (Pöppelreiter 2002; Fig. 5).

Cyclic patterns change in space and time. The superimpo-

sition  of  high-frequency  and  long-term  sea-level  changes  is
stratigraphically  documented  by  different  thicknesses  and
changing  shallowing-up  patterns.  Within  the  long-term
transgression aggradational sedimentary successions and in-
creasing  thickness  of  cycles  are  observed.  Phases  of  maxi-
mum  flooding  are  characterized  by  starvation,  documented
in  basin-wide  deposition  of  condensed,  organic-rich  marls
and amalgamated brachiopod and crinoid shell beds with nu-
merous firmgrounds and hardgrounds. In the Peri-Tethys Ba-
sin the upper part of the Lower Wellenkalk and the Terebra-
tel Beds represent these phases (Fig. 3). Long-term highstand
deposits  show  shallowing-up  facies  successions  and  increas-
ing thickness of cycles. In addition, dolomitic mudstones are
characteristic features of the highstand phase (Götz 2002). In
the Peri-Tethys Basin the Oolith Beds and Schaumkalk Beds
represent  these  periods.  Both  units  are  shallowing-up  sedi-
ment  bodies,  reflecting  phases  of  regression  during  the  late
highstand.  In  these  stratigraphical  units  emersion  surfaces
were described from the southeastern part of the basin, repre-
senting sequence boundaries (Szulc 1999, 2000).

The number of small-scale sequences described from the

Lower  Muschelkalk  (Bithynian-early  Illyrian)  series  of  the
Peri-Tethys  Basin  is  relatively  constant  (E  Netherlands:  16
(Pöppelreiter 2002); Hesse, W Thuringia and Lower Franco-
ny:  20  (Kramm  1994;  Götz  1994;  Götz  &  Feist-Burkhardt
1999; Götz & Wertel 2002); E Thuringia and Brandenburg:
21 (Rameil et al. 2000; Kedzierski 2002); and S Poland: 23
(Kedzierski  2002)).  Small-scale  sequences  described  from
carbonate  series  of  the  proximal  ramp  (E  Netherlands)  are
commonly  incomplete  successions  or  not  recorded  at  all.
Distal sections (Poland) show the most complete sedimenta-
ry series with the highest number of cycles. Considering that
the Lower Muschelkalk was deposited within 2 to 3 million
years  (Harland  et  al.  1990;  Gradstein  et  al.  1995;  Menning
1995;  Hardenbol  et  al.  1998;  Ogg  2004;  Menning  et  al.
2005), the small-scale cycles may represent the short orbital
eccentricity cycle of 100,000 years. Stacked small-scale se-
quences  forming  sets  of  3  to  4  sequences  (Rameil  et  al.
2000) may be interpreted as reflecting the eustatic signal re-
lated to the 400,000 year eccentricity cycle.

The Mid-Triassic ramp system of S Hungary displays a

characteristic  lateral  facies  distribution  of  coastal  sabkhas,
inner  ramp  peritidal  dolomites,  shoal  deposits  and  lagoonal
marls,  storm  to  fair-weather  influenced  mid-ramp  carbon-
ates, proximal to distal shell beds and low-energy outer ramp
deposits (Török 1998). The stratigraphic stacking of these fa-
cies units records long-term sea-level changes at a third-or-
der scale (Török 2000).

The earliest sediments of the ramp system are greenish-red

siltstones (Patacs Siltstone, Fig. 1) with pseudomorphs of an-
hydrite after gypsum, desiccation cracks, bird’s eye structures
and ripple marks indicating a peritidal setting. Phyllopods re-

flect  a  hypersaline  environment,  while  lingulid  brachiopods
are indicators of restricted marine influence. Sporomorphs in-
dicate an early Anisian age for the Patacs Siltstone (Barabás-
Stuhl 1993; Barabás & Barabás-Stuhl 2005). The succeeding
anhydrite and gypsum layers (Magyarürög Anhydrite) are arid
tidal flat, that is sabkha deposits (Török 1998) that are over-
lain  by  dolomitized  peritidal  carbonates  (Hetvehely  Dolo-
mite). The next unit of the deepening-upward succession con-
sists  of  bituminous  limestones  (Viganvár  Limestone)  with
bivalve  coquinas  (Szente  1997)  interpreted  as  storm  influ-
enced, temporarily anaerobic to dysaerobic mid-ramp deposits
(Török  1998).  The  overlying  dolomitized  calcarenites  (ooid
packstones)  of  the  Rókahegy  Dolomite  represent  small  car-
bonate sand bars of an inner ramp setting.

Anisian mid- and outer ramp deposits are characterized by

flaser-bedded  limestones  and  marlstones  (Lapis  Limestone)
with numerous coquinas (tempestites) and hummocky cross-
laminated calcisiltite beds, indicating permanent storm activ-
ity.  In  the  Mecsek  Mountains  the  deepest  facies  are  repre-
sented by brachiopod beds (Zuhánya Limestone), displaying
outer  ramp  deposits  (Török  1993).  Open  marine  conditions
are  indicated  by  the  presence  of  ammonites  and  conodonts
(Kovács & Rálisch-Felgenhauer 2005) as well as maximum
abundance  of  marine  acritarchs  (Götz  et  al.  2003).  A
Bithynian-Pelsonian age for these beds is based on crinoids
(Hagdorn et al. 1997) and palynomorphs (Götz et al. 2003).
The  Lapis  Limestone  corresponds  to  the  lower  and  middle
part of the German Lower Muschelkalk (lower Jena Forma-
tion; Török 2000); the lower Zuhánya Limestone represents
a  stratigraphical  equivalent  of  the  German  Terebratelbank
Member (Götz et al. 2003; Fig. 3).

In the upper Anisian (Illyrian) significant spatial differences

occur in the grade of dolomitization and facies development.
In the western Mecsek Mountains, carbonates are extensively
dolomitized (Csukma Dolomite). These beds formed in the su-
pratidal to peritidal zone of the inner ramp. In the central part
of the Mecsek Mountains limestones with intercalated beds of
ooid-crinoid packstones/grainstones prevail (Kozár Lime-
stone). These sediments are considered to be reworked crinoi-
dal bioherms and ooid shoals and may mark a lowering of the
wave base due to relative sea-level fall (Török 1998).

Small-scale sequences are well documented within inner

and  shallow  mid-ramp  deposits.  During  transgression,  bio-
clastic limestones were deposited. A thin clay horizon on top
of these bioclastic beds marks the phase of maximum flood-
ing.  Sequence  boundaries  are  recognized  by  the  erosional
base of transgressive deposits, showing reworked lithoclasts.
As  in  siliciclastic  systems,  these  surfaces  may  display  ra-
vinement  surfaces.  Calcareous  marls  characterize  the  early
highstand  phase,  whereas  late  highstand  deposits  are  repre-
sented  by  calcareous  marls  with  intercalating  platy  lime-
stones (Fig. 4).

The characteristic feature of high-frequency cycles within

outer ramp deposits (Zuhánya Limestone) is a succession of
limestone beds and calcareous marls. A thick limestone unit
at the base of the cycle represents the transgressive phase,
whereas the following nodular limestone-marl alternation is
interpreted as highstand deposits (Fig. 6). Bioturbated mud-
stones occur during the early highstand phase, whereas late

313

CORRELATION OF TETHYAN AND PERI-TETHYAN EUSTATIC SIGNALS (ANISIAN, MIDDLE TRIASSIC)

highstand deposits are characterized by massive limestone
beds with thin marly layers.

The described sedimentary features clearly express a cy-

clic sedimentation related to relative sea-level changes. The
long-term eustatic signals are also recognized by characteris-
tic  palynofacies  patterns  and  stable  isotope  signatures.  In
both  settings,  the  semi-closed  Peri-Tethys  Basin  and  the
open Tethys shelf, two striking plankton peaks occur in the
Bithynian  and  Pelsonian,  respectively.  Within  these  strati-
graphic  intervals  the

C values reach two local maxima

(Fig. 7) and are interpreted as displaying the most open ma-
rine conditions during major transgression phases, which, in
terms of sequence stratigraphy, represent maximum flood-
ing. The coinciding trends in

C values and relative abun-

dance  and  diversity  of  acritarchs  support  this  interpretation
(cf. discussion in Feist-Burkhardt et al. 2008). Furthermore,
similar trends are recognized in Anisian series of Poland and
Switzerland  (Szulc  2000;  Götz  et  al.  2005;  Feist-Burkhardt
et al. 2008). Therefore, organic facies proves to be a power-
ful  correlation  tool  in  sequence  stratigraphic  interpretation
and correlation of different paleogeographical settings.

Fig. 6. High-frequency cycle within the Zuhánya Limestone Forma-
tion  of  Southern  Hungary  (Mecsek  Mountains),  representing  the
small-scale  facies  succession  of  outer  ramp  deposits.  Abbrevia-
tions:  sb  –  sequence  boundary,  TSd  –  transgressive  deposits,
mfz – maximum flooding zone, eHSd – early highstand deposits,
lHSd – late highstand deposits.

Fig. 7. Relative abundance of marine plankton and

C-signatures within the Anisian of Southern Hungary (reference sections Bükkösd, Orfü,

Kozár) and Central Germany (reference section Ringgau) and sequence stratigraphic interpretation. Abbreviations: sb – sequence boundary, TSd
– transgressive deposits, mfz – maximum flooding zone, eHSd – early highstand deposits, lHSd – late highstand deposits, Fm – formation.

314

GÖTZ and TÖRÖK

Short-term fluctuations in sea level are well documented

in small-scale sequences. The cyclic pattern is depending on
the particular ramp position, namely inner, mid or outer
ramp setting. High-frequency cycles are traceable along the
ramp systems studied using distinct erosional and flooding
surfaces (Fig. 5). Similar small-scale successions recorded in
carbonate series of both an open proximal shelf and an epeir-
ic setting enable a high-resolution correlation.

The Anisian carbonate series of the Northern Calcareous

Alps  (Fig. 8)  represent  the  Tethyan  shelf  area  composed
mainly  of  pure  calcareous  homoclinal  ramp  deposits  of  the
Steinalm  Formation  and  strongly  bioturbated  shelf  deposits
of  the  Virgloria  Formation,  the  latter  consisting  of  carbon-
ates with a low clastic content. In late Anisian (Pelsonian/Il-
lyrian)  times,  the  clastic  input  gradually  diminished  and  fi-
nally  disappeared,  resulting  in  the  predominance  of  the
Steinalm Formation with respect to the Virgloria Formation
(Rüffer 1995; Rüffer & Bechstädt 1998). The Steinalm For-
mation  comprises  mud-dominated  inner  to  outer  ramp  de-
posits. In this environment, characterized by unstable muddy
substrate,  reef-building  organisms  were  completely  absent.
Neither  reef-builders  nor  high-energy  shoals  were  present
during  Anisian  times.  Tempestites  were  intercalated  with

typically mud-supported carbonates, especially during the fi-
nal (Illyrian) stage of the homoclinal ramp.

During Pelsonian times, a major transgression gave rise to

open marine pelagic conditions.

The resulting deposits (Hallstatt Formation) occur

throughout the Alpine shelf, mainly in the southern and east-
ernmost parts of the depositional area of the Northern Cal-
careous Alps (Mandl 1984, 1996; Rüffer 1995).

Within the Anisian series, transgressive surfaces character-

ized by crinoidal wackestones are the most prominent signa-
tures. After a decrease in particles, the late transgressive and
early highstand deposits comprise crinoids, fecal pellets, and
brachiopods. Mid-ramp microbial packstones and inner ramp
stromatolites  are  characteristic  of  the  late  highstand  phase.
Due to the low depositional relief, third-order sea-level fluc-
tuations caused extensive lateral shifts in facies, but did not
change  the  mechanism  of  sediment  production,  reworking
and  transportation.  The  lack  of  erosional  surfaces  and  su-
pratidal facies in most areas of the Northern Calcareous Alps
hinders  the  detection  of  sequence  boundaries  and  lowstand
deposits, respectively. However, based on conodont data the
depositional  sequences  A3  and  A4  detected  in  the  western
Northern Calcareous Alps (Rüffer & Zühlke 1995) are corre-

Fig. 8. Correlation of Anisian third-order depositional sequences of the Peri-Tethys Basin and Tethys shelf. Abbreviations: NCA – North-
ern Calcareous Alps, CSA – Central Southern Alps (Dolomites), L.M. – Lower Muschelkalk, Fm – Formation, C. Fm – Contrin For-
mation, sb – sequence boundary, TSd – transgressive deposits, mfz – maximum flooding zone, HSd – highstand deposits. Compiled
after Rüffer (1995), Zühlke (2000), Götz et al. (2003, 2005), Feist-Burkhardt et al. (2008) and this study.

315

CORRELATION OF TETHYAN AND PERI-TETHYAN EUSTATIC SIGNALS (ANISIAN, MIDDLE TRIASSIC)

latable with the two third-order depositional sequences of the
Lower Muschelkalk of the Peri-Tethyan realm.

In the Western Carpathians, the Anisian Geldek Member

of the Vysoká Formation documents the evolution of a mud-
dominated homoclinal ramp system with most open marine
conditions during the Pelsonian (Michalík 1992). Conodonts
serve as age-diagnostic index fossils and will enable a pre-
cise correlation for sequence stratigraphic interpretation, not
available for this depositional series yet.

In the Southern Alps, marked facies variations in time and

space,  as  well  as  differential  subsidence/uplift  characterize
the Anisian basin development in this part of the NW Tethyan
shelf area (Zühlke 2000). As a result of these variations, the
basin fill includes a large number of lithostratigraphic units.
In the eastern Southern Alps and parts of the central South-
ern  Alps,  carbonate-evaporite  ramps  of  the  Lower  Sarl  and
Lusnizza Formations (Fig. 8) conformably overlie the Early
Triassic Werfen Formation. Further to the W, the Lower Sarl
Formation  was  erosionally  truncated  or  did  not  develop  at
all.  The  western  and  southern  Dolomites  (central  Southern
Alps,  CSA)  were  the  site  of  several  large  structural  highs
with a long-term depositional gap, which lasted until the ear-
ly  Pelsonian  or  the  early  Illyrian.  In  the  eastern  and  central
Southern Alps, carbonate ramps of the Lower Sarl and Olang
Formations  persisted  until  the  late  Bithynian  and  earliest
Pelsonian,  respectively.  Around  the  Bithynian/Pelsonian
boundary, the basin architecture in the central Southern Alps
changed completely. Partitioning of the basin into structural
highs/lows  became  distinct  and  the  depocentres  moved  to
the  W.  In  the  late  Pelsonian,  homoclinal  and  distally  steep-
ened  carbonate  ramps  of  the  Upper  Sarl  Formation  devel-
oped. Coeval structural lows feature dysaerobic to oxic basi-
nal deposition with interbedded turbidites (Dont Formation)
shed from adjacent structural highs.

In the central Southern Alps, late Pelsonian carbonate ramps

of the Upper Sarl Formation are bounded by an erosional un-
conformity or a disconformity. In the Illyrian characteristic fa-
cies  transitions  between  distally  steepened  carbonate  ramps
(Contrin Formation) and narrow marine inlets (Moena Forma-
tion)  or  regional  basins  (Ambata  Formation)  are  recognized.
The  two  third-order  depositional  sequences  An3  and  An4  of
Bithynian-early Illyrian age described from the central South-
ern  Alps  (Rüffer  &  Zühlke  1995)  correspond  to  the  Lower
Muschelkalk sequences of the Peri-Tethys Basin.

Conclusions

The Anisian depositional series from Southern Hungary

and Central Germany represent shallow marine carbonates of
two different paleogeographical settings: the proximal shelf
of the Tethys Ocean and its northern Peri-Tethyan realm.
Both settings are mud-dominated with reworked material
due to periodical storm activity. Storms were more severe in
the open shelf position than in the semi-closed setting, which
is documented in the different development and quantity of
tempestites.

Sea-level changes are clearly recorded. Characteristic fa-

cies successions as well as palynofacies and stable isotope

signatures document third-order cyclicity, and small-scale
sequences can be interpreted as having formed through high-
frequency sea-level changes in tune with orbital cycles. The
detected cyclic patterns are very similar in both settings and
therefore enable a high-resolution long-distance correlation
of large-scale sequences.

The sedimentary organic matter and isotopic signals of the

Anisian  successions  of  the  gate  ways  connecting  the  semi-
closed Germanic Basin and the open Tethys shelf were stud-
ied  (Götz  et  al.  2005;  Feist-Burkhardt  et  al.  2007)  and  they
match the signals from the S Hungarian depositional series.
The most open marine facies occurs in the Pelsonian, reflect-
ing a major flooding phase in the NW Tethyan shelf domain
(major  flooding  surface  237.05 Ma  of  Haq  et  al.  1987)  and
its  northern  peripheral  basin.  Two  third-order  depositional
sequences are detected in the two different paleogeographi-
cal settings studied (Fig. 8) and are traceable along the entire
NW Tethyan realm (Rüffer & Zühlke 1995; Hardenbol et al.
1998;  Szulc  2000;  Götz  et  al.  2003).  The  detected  eustatic
signals  were  also  described  from  the  Northern  Calcareous
Alps (Rüffer 1995) and the Southern Alps (Zühlke 2000) and
are  therefore  interpreted  as  over-regional  signatures  of  the
northern  Tethys  margins  and  adjacent  basins.  However,  re-
gional tectonically events cannot be excluded for the Middle
Triassic  and  the  interpretation  of  solely  climatically  driven
fluctuation of sea level resulting in characteristic cyclic pat-
terns  within  the  sedimentary  record  during  the  Anisian  still
has to be done carefully. In many cases there are also tecton-
ic  changes  controlling  accommodation,  and/or  sea-floor
spreading  influencing  long-term  sea-level  changes.  There-
fore, further studies on sedimentary cycle patterns of differ-
ent scales and in different settings are needed.

Acknowledgments:  This  study  was  supported  by  the  Deu-
tsche  Forschungsgemeinschaft  DFG  (Project  GO  761/1-1)
and  the  Hungarian  Science  Foundation  (Project  OTKA
T  037652).  We  acknowledge  the  very  thorough  and  con-
structive  reviews  of  János  Haas  (Budapest),  Jozef  Michalík
(Bratislava) and André Strasser (Fribourg) which greatly im-
proved the manuscript.

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