towards a new time scale for the upper miocene continental ... · egu stephan mueller special...

EGU Stephan Mueller Special Publication Series, 3, 79–94, 2002c© European Geosciences Union 2002

Towards a new time scale for the Upper Miocene continental seriesof the Pannonian basin (Central Paratethys)

M. Sacchi1 and F. Horvath2

1Istituto per l’Ambiente Marino Costiero (IAMC), Consiglio Nazionale delle Ricerche (CNR), Calata Porta di Massa, Portodi Napoli, 80100 – Napoli, Italy2Eotvos University, Department of Geophysics, Pazmany Peter setany 1/C – 1117 – Budapest, Hungary

Received: 2 May 2000 – Accepted: 29 May 2002

Abstract. In this study we assert that most of the “Pontian”stratigraphic succession of western Hungary is much olderthan Pontian stage (older than 7 Ma). In fact, these strataform a clearly distinct chronostratigraphic unit between thePontian strata (as they are defined in the type area of theBlack Sea basin) and the Pannonian strata (as they are de-fined in the type area of the Vienna basin). To denote such aproblematic chronostratigraphic interval we propose the in-troduction of a new stage (or substage) named Transdanubianbetween the Pannonian sensu stricto (s.s.) and Pontian s.s.stages of the Upper Miocene series of the Central ParatethysSystem (ca. 9.0–7.4 Ma in the chronology adopted in thisstudy).

The Transdanubian stage has been defined in terms ofbiostratigraphy, lithostratigraphy, magnetostratigraphy andallostratigraphy. The location of a suitable stratotype has alsobeen proposed. As a first approach, we tried to avoid the in-troduction of new terms in the already complex chronostrati-graphic nomenclature of the Pannonian basin. However, wearrived to the conclusion that the introduction of the Trans-danubian as a new stage (or substage) is a necessary break-through, to avoid further confusion and circular reasoning in-volving facies associations versus chronostratigraphic units.

Transdanubian strata represent a distinct anticipation ofthe Pontian facies within the intra-Carpathian area. The factthat these strata have been reported for decades as “Pontian”in the literature has been the source of much terminologicalconfusion and chronostratigraphic miscorrelation.

1 Introduction

During the Oligocene-Neogene the Pannonian basin was partof a vast epi-continental basin system that developed as aseries of brackish seaways, lakes and wetlands within theinteriors of central Eastern Europe and western Asia. Ma-

Correspondence to:M. Sacchi([email protected])

jor relics of this ancient aquatic realm, called Paratethys(Laskarev, 1924), are represented by the present-day BlackSea, the Caspian Sea and the Aral Sea (Fig. 1). It is generallyaccepted that open to restricted marine conditions prevailedin the Pannonian basin throughout the syn-rift phase (LowerMiocene to early Mid Miocene). However, since the earlypost-rift phase (late Mid Miocene) the basin became an iso-lated brackish-water lake that was progressively filled up bylarge prograding delta systems.

Establishing a reliable chronostratigraphic framework forthe Neogene non-marine sedimentary fill of the Pannonianbasin and understanding the variation in space and time offacies associations at basin scale have been long-debatedproblems. Paratethys stages were based mainly on mol-lusk assemblages. Correlation among marine episodes in theParatethys was obtained by marine planktonic microfossils,while correlation of regional stages of the Paratethys with thestandard marine stages still remains somewhat obscure, be-ing practically impossible in terms of biostratigraphy only(Magyar and Hably, 1994; Sacchi et al., 1997, 1999a, b).Nowadays consensus seems to be emerging around the needof a multidisciplinary approach to integrate the classic bios-tratigraphic analysis and geologic mapping on a lithostrati-graphic base (Sacchi, 2001).

According to the regional chronostratigraphy adopted forthe nonmarine strata of the intra-Carpathian area (Central Pa-ratethys) the Upper Miocene-Pliocene sequence of the Pan-nonian basin (Pannonian stage sensu (s.) Lorenthey, 1900,or “Pannonian sensu lato” (s.l.), is subdivided into Pannon-ian sensu Stevanovic, 1951, or “Pannonian sensu stricto”(s.s.) and Pontian (s. Andrussov, 1887) stages. An infor-mal twofold subdivision into “Lower Pannonian” and “UpperPannonian” is also used in Hungary, particularly in the prac-tice of seismic-stratigraphic interpretation. In this case theterm “Lower Pannonian” is often assumed to correspond tothe Pannonian stage s.s. and the term “Upper Pannonian” tothe Pontian stage, respectively. It is beyond the scope of thispaper to review the historical development of the Pannon-ian s.l. non-marine stratigraphy of the Central Paratethys.

80 M. Sacchi and F. Horvath: Towards a new time scale for the Upper Miocene continental series

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The reader is referred to the detailed reviews of Korpas-Hodi (1983), Papp et al. (1985), Steininger et al. (1990), Ste-vanovic et al. (1990), Rogl (1996, 1998), Sacchi et al. (1997,1999b), Magyar et al. (1999a, b), Muller et al. (1999), Sacchi(2001) (Fig. 2).

In the last few years several authors have pointed outthat the Late Miocene chronostratigraphy of the Paratethysis affected by terminological and conceptual inconsistencies

(Muller and Magyar, 1992; Magyar and Hably, 1994; Gya-log, 1996; Sacchi et al., 1997, 1999a, b; Horvath and Tari,1999). Particularly it has become clear that none of the stagenames currently used in the literature adequately representthe middle part of the Pannonian s. Lorenthey (1900) (ca.9.0–7.4 Ma, in the chronology adopted in this study). Thereason for the inadequacy of the official Paratethys stage sys-tem in offering a reliable chronostratigraphic picture of the

M. Sacchi and F. Horvath: Towards a new time scale for the Upper Miocene continental series 81

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Sacchi et al., 1997THIS STUDY

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Shift the boundary between Pannonian s. str. and Pontian s. Stevanoviæ (1951) up to the base of the Pontian as it is defined in its type section of the Eastern Paratethys.

Maintain the Pontian s. Stevanovi (1951) only for the Central Paratethys and use the term Pontian with two different meanings.

Introduce a new stage (Transdanubian) in order to fill the “chronostratigraphic gap” between the Pannonian s. str. and Pontian s. str. .

Delete the stage name "Pontian" from the Western-Central Paratethys stage system and reintroduce the use of the term “Pannonian” s. Lõrenthey (1900).

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Fig. 3. Correlation between the Late Neogene(a) Mediterranean and(b) Central Paratethys stages. Column(c) illustrates four possibleredrawings of the Late Miocene chrono-stratigraphic framework of the Pannonian basin (Central Paratethys) (from Sacchi et al., 1997,slightly modified) (see text for discussion).

Pannonian s.l. stage is multifold. Among the important fac-tors hindering time-stratigraphic correlation there are:

1) the general diachronous trends of the lithostratigraphicpatterns in the Paratethys continental realm (youngingfrom West to East);

2) documented radiations and migrations of endemic mol-lusk faunas from central to eastern Paratethys duringLate Miocene-Pliocene;

3) the remarkable facies dependence of faunas whichmakes it difficult to recognize the First and Last Oc-currence of index fossils (Sacchi, 2001).

In this study we propose a new chronostratigraphic frame-work of the Upper Miocene continental record of the Pan-nonian basin, in the stratigraphic interval correspondingto the Tortonian-lowermost Messinian of the standard ma-rine time scale (ca. 9.0–7.0 Ma in the chronology adoptedin this study). The opportunity to introduce the conceptof Regional Stratotype Sections and Points (RSSPs) forlarge (intra)continental bioprovinces as regional standardsfor marine-continental correlations is also discussed.


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Fig. 4. Mediterranean and Paratethysstages for the last 15 Ma (after Rogl,1998 and Magyar et al. (1999a, b). Inthis study we adopt the Transdanubian(Sacchi, et al., 1999a, b) as an inter-mediate stage (or substage) betweenthe Pannonian s.str. (s. Stevanovic,1951) and the Pontian s.str. (Andrussov,1887). The Transdanubian substitutesthe lower part of Pontian s. Stevanovic(1951).

2 The need for a new time scale

Chronostratigraphic miscorrelation between the base of theeastern Paratethys Pontian (Pontian s.str.) and the base of theCentral Paratethys Pontian (Pontian s. Stevanovic, 1951) dueto diachronism of biofacies was first demonstrated in the Pan-nonian basin by Muller and Magyar (1992). This problemwas largely a consequence of the correlation suggested byStevanovic (1951) who proposed the “extension” of the Pon-tian stage of the eastern Paratethys to the central Paratethysrealm, based on the presumed coeval appearance of commonmollusc species on both sides of the Carpathians. However,the Pontian mollusc fauna of the Eastern Paratethys prac-tically consists of Pannonian Lake (Central Paratethys) im-migrants and their descendants, and hence is much youngerthan its intra-Carpathian counterpart (Muller et al., 1999).

The fact that the base of the Pontian s.str. stage is nearly2 Ma younger than the top of the Pannonian s.str actually rep-resents a major obstacle in the chronostratigraphic procedurewithin the Central Paratethys. This circumstance recalls theattention on the practice of adopting a stage defined in theEastern Paratethys (like the Pontian s.str.) for chronostrati-graphic subdivision in the Central Paratethys. The problem

is very complex indeed, as the term “Pontian” has deep rootsin the literature. It is widely used in the Mediterranean regionby both Paratethyan and Mediterranean stratigraphers, andcertainly, it would not be easy to convince workers to substi-tute it with a new stage name “labeled” for Central Paratethysuse only. On the other hand, the correlation of the EasternParatethys Pontian with time-equivalent strata of the CentralParatethys is still obscure.

One might consider that an easy (conceptual, not practi-cal) solution to the problem would be to “stretch” the upperboundary of the Pannonian s.str. stage (s. Stevanovic, 1951)up to the lower boundary of the Pontian s.str. stage (e.g.Rogl, 1996, 1998). This solution, unfortunately, would causeeven more confusion in the terminology. In fact, the “short”Pannonian s.str. stage (Stevanovic, 1951) at least had thebasic advantage of being correlative with the Lower Pannon-ian of the Hungarian literature (s. Lorenthey, 1900; Halavats,1903). This equivalence appears to be deeply rooted and sta-ble in the Central Paratethys stratigraphic terminology of thelast decades. With the eventual upward shifting of the topof the Pannonian s.str. stage this correlation would be lost,and much confusion would arise. Furthermore, the upper-most strata of a “stretched” Pannonian stage would include


sedimentary deposits that display typical “Pontian facies” re-semblance and have been referred to as Pontian for decades.

Whatever the solution may be, the key question remainshow to fill the “chronostratigraphic gap” between the Pan-nonian s.str. and Pontian s.str. stages (Fig. 3). In the fol-lowing pages possible options to “fill” this “gap“ within theUpper Miocene series of the Pannonian basin are presentedand discussed. Particularly we adopt the Transdanubian (ca.9.0–7.4 Ma in the chronology discussed in this study) asan intermediate stage (or substage) between the Pannonians.str. (s. Stevanovic, 1951) and the Pontian s.str. (Andrussov,1887) (Fig. 4).

3 The regional stratigraphic framework of SW Pannon-ian Basin

Several studies have been recently published on the sequencestratigraphy of the Upper Neogene fill of the Pannonian basin(Pogacsas et al., 1988; Elston et al., 1990; Csato, 1993;Ujszaszi and Vakarcs, 1993; Vakarcs et al., 1994, Vakarcs,1997). The results we present in this paper are based on therecent recognition and correlation of unconformity-boundedstratigraphic units within the non-marine Upper Miocenestrata of the western Pannonian basin (Sacchi et al, 1999a).Based on methods and procedures of sequence stratigra-phy (Vail, 1987; Galloway, 1989), five 3rd-order (with 106

year periodicities) sequences at regional scale in the UpperMiocene succession of the western Pannonian basin havebeen recognized (Fig. 5). The sequence stratigraphic pro-cedure was applied not as a rigid model or template, butrather to promote an integrated stratigraphic approach. Thisincludes full combination of biostratigraphy, magnetostratig-raphy, radiometric age determination, sequence (or genetic)stratigraphy and classic field study (Sacchi et al., 1999a).

A detailed lithostratigraphic and paleontologic descriptionalong with geophysical logs of Iharosbereny-I well were usedin this study. Available magnetostratigraphic data includedmagnetic polarity logs from a number of wells in the Hungar-ian part of the Pannonian basin (Lantos et al., 1992, Juhasz,1994; Lantos and Elston, 1995; Magyar et al, 1999b; Sac-chi et al., 1999a). Iharosbereny-I well log has been cor-related with the global magnetic polarity scale (Kande andKent, 1995, Berggren et al., 1995) and seismic reflectors inthe Southern Transdanubia. The obtained sequence strati-graphic framework was tied to a regional biostratigraphic andmagnetostratigraphic framework recently developed for theUpper Miocene succession of the Pannonian basin (Juhasz etal., 1999; Magyar et al., 1999a, b; Muller et al., 1999). Ra-diometric data on volcanic rocks interbedded within the Up-per Miocene continental strata of western Hungary were alsoused to constrain chronostratigraphic interpretation (Baloghet al., 1986; Balogh, 1995; Pecskay et al., 1995).

3.1 Magnetostratigraphy

Iharosbereny-1 is one among a series of continuously coredexploratory wells drilled in the Hungarian part of the Pan-nonian Basin that have been processed for detailed mag-netostratigraphic study (Juhaz et al., 1994, 1999; Magyaret al., 1999). The sedimentary succession cored at Iharos-bereny-1 displays no evidence for movement of connate orground water and the strata seem to have remained undis-turbed and unexposed since burial. Therefore, the studysamples most likely display original magnetization (Magyaret al., 1999b); minor secondary magnetization disappearedat 10–30 mT (Elston et al., 1990, 1994; Lantos and Elston,1995). Details of paleomagnetic studies have been publishedelsewhere (Elston et al., 1990, 1994; Kokay et al., 1991; Lan-tos et al., 1992; Lantos and Elston, 1995.

The magnetic polarity zones of Iharosbereny-1 well sec-tion have been correlated to the Global Polarity Time Scale(GPTS) of Cande and Kent, 1995 (Fig. 6). The magneticpolarity zones detected within the Iharosbereny-1 core sec-tion lie above the long normal polarity interval of ChronC5n (Juhaz et al., 1999; Magyar et al., 1999a). The firsttwo normal polarity intervals in the lower part of the sec-tion between ca. 1100 m and 1075 m and 990 m and 900may be namely correlated with chrons C4Ar.1n and C4An.Similarly, the major uppermost four normal polarity inter-vals at 180–240 m, 275–310 m, 380–410 m, 425–500 m canbe namely correlated to Chrons C3Bn, C3Br.2n, C3Br.1nand C4n.2n. Less obvious is the calibration of the large anddiscontinuous normal polarity zone developing at depth of525 m to 850 m. Juhaz et al. (1999) and Magyar et al. (1999)have proposed that the base of Chron C4n.1n can be locatedat a depth of ca. 730 m. in the Iharosbereny-1 section.

3.2 Sequence stratigraphy

The Upper Miocene stratigraphic sequences of the SW Pan-nonian basin have been designated from bottom to top,as Sarmatian-1 (SAR-1) and Pannonian-1 (PAN-1) throughPannonian-4 (PAN-4). The stacking pattern of stratigraphicsequences gives a general picture of the evolutionary stagesof the prograding delta systems in the SW Pannonian basin.Maximum thickness of the whole sequence stack is in theorder of 3 km. The major unconformity at the base of thepost-rift sequence of the western Pannonian basin in South-ern Transdanubia is often associated with a significant strati-graphic gap whose amplitude increases from WSW (Dravabasin) to ENE (Somogy). This may cause amalgamation ofmore sequence boundaries (Fig. 5).

Calibration of seismic profiles with borehole data showsthat maximum flooding surface mfs-2 marks the peak of amajor flooding event associated with large scale transgres-sion of Congeria czjzeki lacustrine beds (Szak Fm.) ontothe Pannonian basin margins. Mfs-2 correlates with the baseof magnetic polarity zone C4An and hence can be dated at9.03 Ma. It represents a quasi-isochronous surface at basin


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PLIOCENEMIOCENE

Pia

cen

zian

Ro

ma

nia

nS

SE

LA

TE

TE

CT

ON

ICIN

VE

RS

ION

AN

D U

PL

IFT

EA

RLY

TE

CT

ON

ICIN

VE

RS

ION

PO

ST-

RIF

T

SU

BS

IDE

NC

E

Da

cian

Za

ncle

an

Po

ntia

n

Pa

nn

on

ian

Sa

rma

tian

Serravallian

Me

ssinia

n

Torto

nia

n

Tra

ns-

da

nu

bia

n

TH

IS S

TU

DY

Sar-1

Sar-1

+ P

an-1

Congeria

czjzeki b

eds

Congeria

rhom

boid

ea b

eds

PA

N-3 P

AN

-4

SO

UT

HE

RN

TR

AN

SD

AN

UB

IA(W

ES

TE

RN

HU

NG

AR

Y)

0

50

km

Bu

da

pe

st

WE

ST

ER

NH

UN

GA

RY

PL

IO-P

LE

IST

OC

EN

EU

PL

IFT

Ib-I

Two-way travel time (s)

1.0

1.5

2.0

2.5

12345678910

1112

13

ST

AN

DA

RD

ST

AG

ES

Tim

e(M

a)

EPOCH

CE

NT

RA

LP

AR

AT

ET

HY

SS

TA

GE

S

NN

W

0 2

0 K

m

Fig.5.

Tectonicand

sequencestratigraphic

framew

orkof

Pannonian

s.l.strata

basedon

theinterpretation

ofca.

1700km

ofseism

icsections

acrossw

esternH

ungary(from

Sacchi,

2001,m

odified).


0

100

200

300

400

500

600

700

800

900

1000

1100

1200

1300

1377

C3r

C3An

C3Ar

C4n

C4r

C4Ar

C5n

C4An

C3Br

C3Bn

10

6

7

8

9

Depth(m)

6.935

7.091

7.1707.135

7.4327.3757.341

7.5627.650

8.072

8.699

9.025

9.2309.308

9.740

6.567

6.2696.137

5.894

CHRONS

T I M

E (M

a)

TIME (Ma)

PO

LA

RIT

Y

CK

95

IHAROSB R NY-1E É

9.6429.580

8.2578.225

8.6518.635

Fig. 6. Correlation of Iharosbereny-1well polarity zones with the Global Po-larity Time Scales (GPTS) of Candeand Kent (1995) (CK95) (after Juhaszet al., 1994, 1999; Magyar et al., 1999b;Sacchi, 2001).

scale and correlates with the top of Pannonian s.str. stage(Lower Pannonian s. Lorenthey, 1900) (Figs. 5–8).

Sequence boundary Pan-2 correlates with the base of zoneC4r (ca. 8.7 Ma). It is associated with a significant dropof base level of erosion within the Pannonian basin, whichwas accompanied by extensive subaerial exposure of the lakemargins. This is documented in the so-called marginal faciesof Transdanubia (Sacchi, 2001).

Maximum flooding mfs-3 is within the lower part of zoneC3Br (ca. 7.4 Ma). It represents the final stage of a secondimportant flooding event within the basin, which is again

characterized by the development of open lake strata. Sub-surface data show maximum flooding surface mfs-3 may becorrelated to offshore lacustrine marl with Congeria rhom-boidea. This surface represents another useful quasi time-line at basin scale that may be regarded as a good proxy inwestern Hungary for the base of Pontian as it is defined inthe stratotype area of the Black Sea basin. Consequently, thestratigraphic unit bounded by maximum flooding surfacesmfs-2 and mfs-3 can be correlated with the lower part Pon-tian s. Stevanovic (1951). This unit can be seen as an “antic-ipation“ of the Pontian s.str. facies in Hungary. According to


Somogy

Dráva basinMecsek

Bakony

Iharosberény-I

Lake Balaton

0 50 km

Pre-Sarmatiansyn-rift strata

and pre-rift basement

Iharosberény-I SECTION NA-41 / So-1NTw

o-w

ay

tra

vel t

ime

(s)

STw

o-w

ay tra

vel tim

e (s)

0.43 s

0.75 s

0.62 s

PAN-2

PAN-3

Pan-3 3rd-order sequence boundary

Magnetostratigraphic calibration (Ma)

3rd-order maximum flooding surfacemfs-2

9.03

PAN-2 3rd-order stratigraphic sequence

0

0.5

1.0

1.5

2.0

0

0.5

1.0

1.5

2.00 5 km

mfs-3 (7.43 Ma)

mfs-2 (9.03 Ma)Pan-2 SB (ca 8.70 Ma)

Somogy

Dráva basinMecsek

Bakony

Iharosberény-I

Lake Balaton

0 50 km

Pre-Sarmatiansyn-rift strata

and pre-rift basement

Iharosberény-I SECTION NA-41 / So-1NTw

o-w

ay

tra

ve

l tim

e (

s)S

Tw

o-w

ay tra

vel tim

e (s)

0.43 s

0.75 s

0.62 s

PAN-2

PAN-3

Pan-3 3rd-order sequence boundary

Magnetostratigraphic calibration (Ma)

3rd-order maximum flooding surfacemfs-2

9.03

PAN-2 3rd-order stratigraphic sequence

0

0.5

1.0

1.5

2.0

0

0.5

1.0

1.5

2.00 5 km

mfs-3 (7.43 Ma)

mfs-2 (9.03 Ma)Pan-2 SB (ca 8.70 Ma)

Fig. 7. Magnetostratigraphic cali-bration of Pannonian s.l. strata atIharosbereny-I well site with the GPTSof Cande and Kent, 1995 (CK 95) (af-ter Magyar et al., 1999b; Sacchi et al.,1999a; Sacchi 2001). Maximum flood-ing surfaces mfs-2 (9.03 Ma) and mfs-3 (7.43 Ma) represent two quasi time-lines at basin scale.

this interpretation it is concluded that Pontian s.str. (youngerthan 7 Ma) strata are practically missing in outcrop in central-western Hungary.

Sequence boundary Pan-4 (ca. 5.0 Ma) is likely to be as-sociated with a stratigraphic gap (Juhasz et al., 1999) andsignificant tectonic overprint as suggested by the generaltectono-stratigraphic patterns within the Neogene basin fill.The higher rank unit bounded by Pan-1 SB and Pan-4 SB ap-proximately correlates with the Tortonian-Messinian strata ofthe standard time scale. The major unconformity developingat Pan-4 SB subdivides the post-rift strata of western Pannon-

ian basin into two main tectono-stratigraphic units namelyLate Miocene and Pliocene in age (Fig. 5).

4 Definition of Transdanubian stage (or substage)

Based on the integrated stratigraphy of the Upper Miocenesuccession of SW Pannonian basin discussed in this study,we propose the introduction of the Transdanubian stage in theregional chronostratigraphic scale of the Central Paratethys(Fig. 9). The Transdanubian is intended to substitute the


IHAROSB R NY-1 WELLE É

Lith

olo

gy

De

pth

(m

)

Ma

gn

etic

po

larity

Ch

ron

s

Ag

e (

Ma

)

Chrono-stratigraphy

ParatethysStandard

PLIO-PLEIST.

6.94

7.17

7.43

7.65

8.07

8.70

9.03

9.23

9.31

100

200

300

400

500

600

700

800

900

1000

1100

1200

1300

1400

PA

NN

ON

IAN

(s

.str.)

TR

AN

SD

AN

UB

IAN

PO

NT

IAN

(s

.str.)

P A

N

N

O

N

I A

N

(

s. l.

)

BADENIAN

S e d i m e n t a r y

Clastics

Carbonates

textures and structures

low high

Clay

Sand Grav.

Silt

VF F

MS WS PS GS RS

M CVC 4 64

Depositionalsystem/element

Depositional settingand

base level changes

ALLUVIALPLAIN

DELTAPLAIN

PERIODICALLYFLOODED

DELTA PLAIN

SHOREFACE

NEARSHORE

OFFSHORE

OFFSHORE

LAKE SHOREFACE

BEACH BAR

BAY

BAY

INLET REEF

DELTA FRONT

SWAMP

C3A

C4n

C4r

C4Ar

C4An

C3B

OFFSHORE

NEARSHORE

fp b/s sl of 76 mV 4 0 OHM 175Sta

ckin

g p

atte

rn

Sys

tem

s tr

act

Sp

on

tan

eo

us

po

ten

tial

Re

sist

ivity

S e

q u

e n

c e

P

A N

- 2

Sys

tem

s tr

act

bo

un

din

g s

urf

ace

mfs - 2

Pan - 2

mfs - 3

LST

TST

HST

LST

TST

HST

3rd

-ord

er

seq

ue

nce

S e

q u

e n

c e

P

A N

- 3

Lowstand systems tract (LST) Trangressive systems tract (TST) Highstand systems tract (HST)

Pan - 2 3rd-order sequence boundary mfs - 2 Maximum flooding surface fs Minor flooding surface

Stratigraphic gap

T O

R

T

O

N

I A

N

L A

T

E

M

I O

C

E

N

E

ME

SS

INIA

N

CK

95

fp = flood plain b/s = bay/shoreface ol = open lacustrinesl = shallow lacustrine

SB

fs

fs

TOP OF LST

TOP OF LST

SB

Fig. 8. Interpretation of the Pannonian s.l. (Upper Miocene) succession cored at Iharosbereny-1 well site, western Pannonian basin, Hungary.Chronostratigraphic subdivision of Pannonian s.l. strata is after Sacchi et al. (1999a, b). Magnetic polarity zones have been calibrated to theGPTS of Cande and Kent (1995) (CK95).

lower part of the “Pontian” s. Stevanovic (1951) which re-vealed to be significantly older than Pontian age s.str.

In terms of the informal chronostratigraphy often used inHungary, the Transdanubian may be introduced as the thirdmiddle subdivision of the Pannonian s.l. stage (s. Lorenthey,1900). It is worth noting that the concept of an intermedi-

ate stage between “Lower Pannonian” (Pannonian s.str.) and“Upper Pannonian” (Pontian s.str.) is not new. In fact sincethe earliest stratigraphic studies on Pannonian strata, Hornes(1901) had defined a “Middle Pontian” interval (MittlereCongerienschichten) and Halavats (1903) “Middle Pannon-ian” strata (Congeria ungulacaprae and Congeria balatonica


RT

L A T E M I O C E N EMID

MIOCENE

P A N N O N I A N S. L.

EARLY LATEMID

MESSINIAN ZANCL.TORTONIANSERRA-VALLIAN

DacianPontian s.str.Pannonian s.str.

SA

RM

AT

IAN

PLIOCENE Epoch

Age

Polarity

56789101112 TIME (Ma)

Regional

CH

RO

NO

-S

TR

AT

IGR

AP

HY

SE

QU

EN

CE

S

TR

AT

IGR

AP

HY

MA

GN

ET

O-

ST

RA

TI-

GR

AP

HY

Local

Cen

tral P

aratethys

2nd-o

rder

(T-R

)cycles

3rd-o

rder

sequen

ces

Cande &

Kent

(1995)

Chron

C5r

C5A

n

C5A

r

C5n

C4A

r

C4A

n

C4r

C4n

C3B

rC

3B

nC

3A

r

C3A

n

C3r

C3n

(Hungarian)

Pa

n-3

Pa

n-1

Sa

r-1

PAN-4PAN-3PAN-2PAN-1SAR-1

Seq

uen

ceboundary

Maxim

umflo

oding

surface

Sequence

mfs -4

mfs -2

mfs -3

??

?

???

?

Berggren

et al. (199

5)

Astaracian

Vallesian

Turolian

Zones

Stages

K

rijgsman et al. (19

96)

T

HIS

ST

UD

Y

T

HIS

ST

UD

Y

BIO

ST

RA

TIG

RA

PH

Y

INT

EG

RA

TE

D S

TR

AT

IGR

AP

HY

OF

TH

E P

AN

NO

NIA

N S

.L. S

EQ

UE

NC

E O

F S

W H

UN

GA

RY

deep water

Dino-

flagellatessublittoral

littoral

Mollusc zones

Mam

mal

Magyar et al. (1999a, b)

Sacch

i (2001

)

Sacchi (2

001)

Lym

nocardiumdecorum

L. serb

icum

L. praeponticum

Mecsekia ultim

a S. b. pannonicus

Pontiadinium

pecsvaradensis

Spiniferitesbentorii oblungus

Spiniferitesparadoxus

Spiniferitesvalidus

Lym

nocardiumponticu

m L

ymnocardium

soproniense

Lym

nocardiumschedelianum

Lym

nocardiumconjungens

C. praerhom

boidea

Congeria

rhomboidea

Galeacystaetrusca

P. vodopici

P. vutskitsi

P. dainellii

P. carbonifera

Prosodacnomya

"Paludina beds" (freshw

ater)

Sarm

atian fauna(restricted m

arine)

Congeria czjzeki

rnithop

sisC

. o

Congeria

hoernesi

Congeria

banatica

Congeria

digitifera

MN

7-8

MN

9

MN

10

MN

11

MN

12

MN

13

Transdanubian

Pa

n-2

Pa

n-4

?

?

?

Fig.9.

Biostratigraphic

definitionofthe

Transdanubian

stage,or

substage(Late

Miocene

oftheC

entralParatethys

)and

correlationw

ithm

agnetostratigraphicand

sequencestratigraphic

units(after

Sacchi,2001).


LakeBalaton

Balatonhighland

Tihanypeninsula

Fig. 10. Alternating shallow lacustrine and terrestrial strata cropping out at Tihany-Fehérpart, Lake Balaton. The section is currently regarded as Pontian faciostratotype in Hungary (Müller and Szónoky, 1990). Our study showed, however, that these strata are much older than the Pontian stage. We suggest this section may be selected as stratotype Transdanubian (ca. 9.0 to 7.4 Ma ).

Fig. 10. Alternating shallow lacustrine and terrestrial strata cropping out at Tihany- Feherpart, Lake Balaton. The section is currentlyregarded as Pontian faciostratotype in Hungary (Muller and Szonoky, 1990). Our study showed, however, that these strata are much olderthan the Pontian stage. We suggest this section may be selected as Transdanubian stratotype (ca. 9.0 to 7.4 Ma).

beds). Both these stratigraphic units substantially coincidewith the Transdanubian stage defined and discussed in thisstudy.

The Transdanubian time interval is actually not repre-sented in any proposed stratotype of the Miocene Series ofthe Central Paratethys.

Name– The name “Transdanubian” is proposed after thename of the inner Carpathian region west of the Danube river,to denote the stratigraphic interval in study. It is the regionof Hungary where the best outcrops of these rocks can befound.

Rank of the Chronostratigraphic Unit– The Transdanu-bian has a duration of ca. 1.6 Ma. It could be ascribed to therank of stage or substage, depending on the reorganization ofthe general chronostratigraphic framework.

Location of the stratotype– A suitable stratotype for theTransdanubian stage is represented by the Tihany-Feherpartsection which is presently used as faciostratotype for local(Hungarian) reference to the Pontian facies of the Black Sea(Muller and Szonoky, 1990). This section is exposed at the

northern shore of Lake Balaton, western Hungary (Fig. 10).

Selection of a boundary stratotype– The lower bound-ary of Transdanubian stratotype section is not exposed atTihany-Feherpart, but has been cored in the near subsur-face (55.4 m beneath the topographic surface at Lake Bala-ton shore, Tihany-62 well). This stratigraphic level crops outin the northern Transdanubia (Bakony, Vertes, Gerecse Mts.)and more research work should be to be done to select an ap-propriate Transdanubian boundary stratotype in this area. Apossible candidate in scope may be preliminarily selected inthe clay pit sections exposed at Tatabanya area at the bound-ary between the open lacustrine strata (Szak Fm.) and thebase of the overlying silty layers of Somlo Fm (top of theCongeria czjzeki bearing beds).

Biostratigraphic definition– In terms of molluscan bio-zonation (Magyar et al, 1999b) the Transdanubian stage cor-responds to the littoral Congeria balatonica-Lymnocardium(decorum–serbicum) zone and the Congeria ungulacaprae-Prosodacnomya (carbonifera–dainelli) zone (see MiddlePannonian of Halavats, 1903). Its lower part correlates


3.0

1.5

00

1.5

3.0

Lake Balaton

WE

ST

ER

N P

AN

NO

NIA

N B

AS

IN

Iha

ros

be

rén

y-I

K

ap

os

vá

r

Him

es

há

za

S

ze

ks

zá

rd

Bá

tas

zé

k

BA

KO

NY

ME

CS

EK

SO

MO

GY

PA

NN

ON

IAN

S.S

.

TR

AN

SD

AN

UB

IAN

Tih

an

yP

áp

a

NN

WS

SE

02

0 k

m

Depth (km)

Depth (km)

8.7

7

.4

9.0

Pan-2

mfs-2

mfs-2

mfs-3

mfs-3

PA

NN

ON

IAN

BA

SIN

FIL

LP

OS

T-R

IFT

IGNEOUS

IGNEOUS

SY

N-R

IFT

PA

NN

ON

IAN

S.L

.(L

AT

E M

IOC

EN

E)

PA

NN

ON

IAN

S.S

.

TR

AN

SD

AN

UB

IAN

(this

stu

dy)

PO

NT

IAN

S.S

.

PR

E-P

AN

NO

NIA

N(M

IDD

LE

MIO

CE

NE

)P

RE

-MID

DL

EM

IOC

EN

E

PR

E-R

IFT

BA

SE

ME

NT

P

an

-33rd

-ord

er s

eq

ue

nce b

oun

da

ry

3rd

-ord

er m

axim

um

floo

din

g s

urfa

ce

mfs

-2

Mag

ne

tostra

tigra

ph

ic c

alib

ratio

n (M

a)

9.0

Pa

n-1

+S

ar-1

mfs-3

PO

NT

IAN

S.S

. P

an-3

mfs

-2C

onge

ria czjze

ki bed

s

Congeria

rhom

boid

ea b

eds

0

50

km

Bu

da

pe

st

WE

ST

ER

NH

UN

GA

RY

Fig.11.S

ketch-sectionacross

thew

esternP

annonianbasin,based

onregionalseism

icprofiles.

The

stratigraphicunitbetw

eenm

aximum

floodingsurfaces

mfs-2

andm

fs-3(ca.9.0-7.4

Ma)

representsthe

Transdanubian

stagediscussed

inthis

study.


L A T E M I O C E N EMID-

MIOCENE

P A N N O N I A N S. L.

EARLYLATE MID

MESSINIAN ZANCL. TORTONIAN SERRA-VALLIAN

Dacian Pontian s.str. Pannonian s.str.

SA

RM

AT

IAN

PLIOCENEEpoch

Age

Polarity

5 6 7 8 9 10 11 12TIME (Ma)

Regional

CH

RO

NO

-S

TR

AT

IGR

AP

HY

MA

GN

ET

O-

S

TR

AT

I-

GR

AP

HY

L

oca

l

2nd

-ord

er(T

-R)

cycl

es

3rd

-ord

erse

que

nces

Can

de &

Ken

t

(1

99

5)

Chron

C5

r

C5

An

C5

Ar

C5

n

C4

Ar

C4

An

C4

r

C4

n

C3

Br

C3

Bn

C3

Ar

C3

An

C3

r

C3

n

(Hu

ngar

ian

)

Pa

n-2

Pa

n-3

Pa

n-1

PAN-4 PAN-3 PAN-2 PAN-1 SAR-1

Seq

uenc

ebo

unda

ry

Max

imum

flood

ing

surf

ace

Sequence

mfs

-4

mfs

-2

mfs

-3

??

?

? ?

?

VIE

NN

A B

AS

INP

AN

NO

NIA

N B

AS

INB

LA

CK

SE

A B

AS

IN

VIE

NN

A B

AS

INP

AN

NO

NIA

N B

AS

INB

LA

CK

SE

A B

AS

IN

NW

SE

PA

NN

ON

IAN

TR

AN

SD

AN

UB

IAN

PO

NT

IAN

t 2 t 2

t 1 t 1

Ber

ggr

en e

t al

.

(

1995

)

SE

QU

EN

CE

S

TR

AT

IGR

AP

HY

C

entr

al

Par

atet

hy

s

T

HIS

ST

UD

Y

TH

IS S

TU

DY

?Trans-

danubian

7.4

3

9.0

3

PR

E-P

AN

NO

NIA

N B

AS

EM

EN

T

R T

Pa

n-4

?

Sa

r-1

?

Str

ato

typ

e P

an

no

nia

n s

.str.

(Vö

sen

do

rf )

Pro

pose

dst

rato

type

“Tra

nsda

nubi

an"

(Tih

any-

Feh

érpa

rt)

Str

ato

typ

eP

on

tian

s.s

tr.

(Od

ess

a)

7

.43

9.0

3

500

km

Fig

.12.

Chr

onos

trat

igra

phic

fram

ewor

kof

the

uppe

rM

ioce

nest

rato

type

sect

ions

ofth

eP

arat

ethy

sst

age

syst

em(f

rom

Sac

chi,

2001

,mod

ified

).


to the sublittoral Congeria praerhomboidea zone and theSpiniferites validus microplankton zone, though it may out-reach their rather uncertain upper boundaries. The lowerboundary of the Transdanubian correlates with the base ofChron C4An and displays an age of 9.03 Ma, while the up-per boundary is within the lower part of zone C3Br (7.43 Ma)(Fig. 9).

Allostratigraphic definition– From the perspective of al-lostratigraphy (Salvador, 1994) the Transdanubian stage maybe defined as a genetic stratigraphic unit (s. Galloway,1989) bounded by two consecutive third-order maximumflooding surfaces, namely, mfs-2 and mfs-3 of this study(Fig. 11). Transdanubian strata correspond to a regressive-transgressive cycle that can be regarded as an “anticipation”of the Pontian facies of the Black Sea in Hungary.

Recognition of Transdanubian boundaries in the outcropand subsurface– As they correspond to maximum floodingsurfaces, both boundaries of the Transdanubian stage are eas-ily recognized in the outcrop (sharp facies contrast betweenthe underlying open lacustrine beds and the overlying regres-sive fluviatile-terrestrial strata) as well as in deep seismics(high-amplitude and high-lateral continuity of reflectors atthe top of transgressive systems tract typically overlain bydownlapping strata of the highstand systems tract deposits).

Completeness of the boundary stratotype section– Re-gional stratigraphic correlation indicates that the criticalinterval for defining the base of the Transdanubian stageis remarkably complete in the whole northern Transdanu-bian area. Sequence stratigraphy predicts that condensationand/or minor non-depositional hiatus may occur at maximumflooding surfaces. However if hiatuses occur, their durationis likely to be below the resolution provided by biostratigra-phy.

Magnetostratigraphic definition– Based on correlationwith calibrated magnetostratigraphy of Iharosbereny-I well,the lower boundary of the Transdanubian stage can be placedat the base of chron C4An of the global magnetic polar-ity scale (Cande and Kent, 1992, 1995; Berggren, 1995)(Figs. 7–9).

Geochronology– According to the revised calibration ofglobal magnetic polarity scale of Cande and Kent (1995), thelower boundary of the Transdanubian stage displays a mag-netostratigraphic age of 9.025 Ma (Figs. 7–9).

Potential correlation with Eastern Paratethys stages–Based on its integrated stratigraphic definition the Trans-danubian stage as a first approach, might be tentatively cor-related with the Maeotian stage of the Eastern Paratethys(Pevzner, 1987).

5 Discussion

If the Late Miocene chronostratigraphy of the Mediter-ranean can be regarded as one of the best known time in-tervals of the stratigraphic column, on the other end theLate Miocene chronostratigraphy of Central-Eastern Europe(Central Paratethys) appears to be, some decades after its in-

troduction, still far from satisfactory. Apart from the obviousdifficulties in correlating non-marine stages of the Paratethysand standard marine stages, the Paratethys Stage System isclearly affected by severe internal inconsistency. Particularly,the boundaries and the internal subdivision of the broad timeinterval between the Sarmatian (Mid-Late Serravallian) andthe Pleistocene have not been unambiguously defined at in-terregional scale.

In the last decades, the use of different names or even dif-ferent meanings for the same names has proliferated to suchan extent that, possibly, the only unequivocal chronostrati-graphic term one could use to indicate rocks of that time in-terval is “Pannonian” (s. l.) as it was originally introducedby Roth (1879) more than a century ago.

One “mission” of stratigraphy is trying to find the largestinternational consensus around the definition and conve-nience in the practical use of Stages. In fact, modern trendsin chronostratigraphy include the concept of Global Stra-totype Section and Points (GSSPs). Of course one can-not approach the chronostratigraphic study of the Paratethysbioprovince (although it is a huge bioprovince) in terms of“global” stages. Nevertheless, we believe it might be worth-while to agree upon regionally valid, useful, and accepteddefinition of stages. The wider the region where a certainstage can be successfully tested and used, the higher is itsintrinsic value. Therefore, an international cooperation andeffort would be required in order to work out “Regional(i.e. Paratethyan) Stratotype Section and Points” (RSSPs)(Fig. 12). This would probably be a necessary step towardsthe process of abandoning excessive fragmentation and pro-liferation of local chronostratigraphic subdivisions within thecontinental realm of Paratethys.

6 Conclusions

We propose the introduction of the Transdanubian as an in-termediate stage (or substage) between the Pannonian s.str.and Pontian s.str stages of the Upper Miocene series of theCentral Paratethys System (ca. 9.0–7.4 Ma in the chronologyadopted in this study) (Figs. 2, 4 and 9).

The reason for introducing a new stage in the already com-plex chronostratigraphic framework of the Paratethys stagesystem is twofold. The Transdanubian stage is a rock unitlikely to be recognizable at regional scale and it may sig-nificantly enhance stratigraphic correlation in the CentralParatethys. On the other hand, we consider its introduction asa necessary breakthrough, to avoid further confusion and cir-cular reasoning involving facies associations versus chronos-tratigraphic units.

Transdanubian strata correspond to a regressive-transgres-sive cycle that can be regarded as an “anticipation” of thePontian facies of the Black Sea in Hungary (Fig. 12). Theintroduction of the Transdanubian stage may help to unravelthe long-lasted debate on Late Neogene chronostratigraphyof the central Paratethys. A major impact of the new strati-graphic correlation we present in this study is the significant


revision of Late Miocene paleogeographic reconstruction ofthe Mediterranean area and timing of geodynamic processesin the Pannonian basin.

Acknowledgements.This research has benefited from joint workand fruitful discussion at various stages with Imre Magyar andPal Muller who are kindly acknowledged here. We thank Jean-Pierre Berger, Davide Castradori, Maria Bianca Cita, AndrasNagymarosy, Andras Galacz, Fred Rogl, Fritz Steininger, GunterSchweigert and Dionz Vass, for their suggestions and comments.Sincere thanks are also due to two anonymous referees who sig-nificantly improved the early version of manuscript and to PatriciaSclafani who revised the English text.

This work was supported by the Italian-Hungarian CooperationAgreement (CNR-MTA) for the period 1998-2000.

References

Andrussov, N.: Geogische Untersuchungen in der westlichen Halfteder Halbinsel Kertsch, Bull. D. Societe d. natur. D. l. Nouv.Russie, 2, 69–147, 1887.

Balogh, K.: K/Ar study of the Tihany Volcano, Balaton Highland,Hungary, Report on the work supported by the European Com-munity in the frame of program “IBS”, Institute of Nuclear Re-search, Hungarian Academy of Sciences, Debrecen, pp12, 1995.

Balogh, K., Arva-Sos, E., Pecskay, Z., and Ravasz-Baranyai, L.:K/Ar dating of Post-Sarmatian alkali basaltic rocks in Hungary,Acta Miner. Petrogr., 28, 75–93, 1986.

Berggren, W. A., Hilgen, F. J., Langereis, C. G., Kent, D. V., Obra-dovich, J. D., Raffi, I., Raymo, M. E., and Shackleton, N. J.:Late Neogene chronology: New perspectives in high-resolutionstratigraphy, GSA Bullettin, 107, 11, 1272–1287, 1995.

Cande, S. C. and Kent, D. V.: Revised calibration of the geomag-netic polarity time scale for the Late Cretaceous and Cenozoic,Jour. of Geoph. Res., 100, B4, 6093–6095, 1995.

Csato, I.: Neogene sequences in the Pannonian Basin, Hungary,Tectonophysics, 226, 377–400. 1993.

Eltson, D. P., Lantos, M., and Hamor, T.:, Magnetostratigraphic andseismic stratigraphic correlations of Pannonian (s. l.) deposits inthe Great Hungarian Plain. Annu. Rep. Hung. Geol. Surv., 1988(I), 110–134, 1990.

Eltson, D. P., Lantos, M., and Hamor, T.: High-resolution polarityrecords and the stratigraphic and magnetostratigraphic correla-tion of the Late Miocene and Pliocene (Pannonian s. l.) depositsof Hungary, in: Teleki, P. G., Mattick, R. E., Kokai, J. (Eds.):Basin Analysis in Petroleum Exploration. A case study from theBekes basin, Hungary, Kluwer Academic Publishers, Dordrecht,111–142, 1994.

Fejfar, O.: Tableau stratigraphique de l’Eocene superieure au Pleis-tocene, Symp. de Gunzburg (unpublished), 1988.

Galloway, W. E.: Genetic stratigraphic sequences in basin analy-sis I: architecture and genesis of flooding surface-bounded depo-sitional units, AAPG Bullettin, 73, 125–142, 1989.

Gyalog, L. (Ed.): A foldtani terkepek jelkulcsaes a retegtaniegysegek rovid lerasa (Key of geological maps and short descrip-tion of the lithostratigraphical units) – MAFI alk. kiadv. (Hung.Geol. Surv.), Budapest, 1–171, 1996.

Halavats, J.: Die Fauna der pontischen Schichten der Umge-bung des Balatonsees, in: Resultate der wissenschaftlichen Er-forschung des Balatonsees, 1/1, Palaontologischer Anhang 4/2,Holzel, Wien, 1–80, 1903.

Horvath, F. and Tari, G.: IBS Pannonian Basin project: a review ofthe main results and their bearings on hydrocarbon exploration,in: Durand, B. Jolivet, L., Horvath, F., and Seranne, M. (Eds.):The Mediterranean Basins: Tertiary Extension within the AlpineOrogen, Geological Society, London, Special Publications, 156,195–213, 1999.

Hornes, R.,: Congeria Oppenheimi und Hilberi, zwei neue Formender Rhomboidea-Gruppe aus den oberen pontischen Schichtenvon Konigsgnad (Kiralykegye), Sitzungsberichte d. kais. Akad.d. Wiss., math.-naturw. Klasse, Bd. CX. Abth. I., 206–236, 1901.

JamborA.: Review of the geology of the s.l. Pannonian formationsof Hungary, Acta Geol. Hung., 32 (3–4), 269–324, 1989.

Juhasz, E., Kovacs, L.O., Muller, P., Toth-Makk, A., Phillips, L.,Lantos, M.: Climatically driven sedimentary cycles in the LateMiocene sediments of the Pannonian basin, Hungary, Tectono-physics, 282, 257–276, 1997.

Juhasz, E., Budai, T., Farkas-Bulla, J., Hamor, T., Lan-tos, M., Muller, P., Toth-Makk, A.: A Pannon-medenceNeogen uledekeinek veszletes sedimentologiai facies-elemzesees ertekelese. Jelentes az IBS project kekreteben vegzettmunkakrol, ELTE Geofiz. Tsz., konzvtar, Budapest, 1994.

Juhasz, E., Phillips, L., Muller, P., Ricketts, B., Toth-Makk, A.,Lantos, M., Kovacs, L.O.: Late Neogene sedimentary facies andsequences in the Pannonian Basin, Hungary, in: Durand, B. Jo-livet, L., Horvath, F., and Seranne, M. (Eds.): The MediterraneanBasins: Tertiary Extension within the Alpine Orogen, GeologicalSociety, London, Special Publications, 156, 335–356, 1999.

Kokay, J., Hamor, T., Lantos, M., and Muller, P.: The paleomag-netic and geological study of borehole section Berhida 3, AnnualReport of the Hungarian Geological Institute, 1989, 45–63, 1991.

Korpas-Hodi, M. (Ed.): Dunantuli Kozephegyseg – Paleoecologyand biostratigraphy of the pannonian mollusca fauna in the north-ern foreland of the Transdanubian Central Range, Ann. Inst.Geol. Publ. Hung., 66, 163pp, 1983.

Krijgsman, W., Garces, M., Langereis, C. G., Daams, R., van derMeulen, A. J., Agustı, J., and Cabrera, L.: A new chronology forthe middle to late Miocene continental record in Spain, Earth andPlanetary Science Letters, 142, 367–380, 1996.

Lantos, M. and Elston, D. P.: Low to high-amplitude oscilla-tions and secular variation in a 1.2 km Late Miocene inclinationrecord, Physics of the Earth and Planetary Interiors, 90, 37–53,1995.

Lantos, M., Hamor, T. and Pogacsas, G.: Magneto- and seismo-stratigraphic correlations of Pannonian s.l. (late Miocene andPliocene) deposits in Hungary, Paleontologia i Evolucio, 24–25,35–46, 1992.

Laskarev, V.: Sur les equivalents du Sarmatien superieur en Serbie,Recueil de travaux offert a M. Jovan Cvijic, Beograd, 1924.

Lorenthey, I.: Foraminifera der pannonischen Stufe Ungarns, NeuesJb. f. Min. Geol. und Palaont., 2, 99–107, 1900.

Magyar, I. and Hably, L.: Stratigraphic position of late Neogenepaleobotanical sites in Hungary: Miocene or Pliocene? Acta Pa-leobot. Polonica, 34 (2), 195–203, 1994.

Magyar, I., Geary, D. H., and Muller, P.: Paleogeographic evolutionof the Late Miocene Lake Pannon in Central Europe, Palaeo-geogr. Palaeoclimatol. Paleoecol., 147, 151–167, 1999a.

Magyar, I., Geary, D. H., Suto-Szentai, M., Lantos, M., andMuller, P.: Integrated biostratigraphic, magnetostratigraphic andchronostratigraphic correlations of the Late Miocene Lake Pan-non deposits, Acta Geol. Hung., 42/1, 5–31, 1999b.


Mancini, E. A. and Tew, B. H.: Recognition of maximum floodingevents in mixed siliciclastic-carbonate systems: Key to globalchronostratigraphic correlation, Geology, 25, 351–354, 1997.

Muller, P. and Magyar, I.: Stratigraphic significance of the UpperMiocene lacustrine cardiid Prosodacnomya (Kotcse section, Pan-nonian basin, Hungary), Foldtani Kozlony, Budapest, 112/1, 1–38, 1992.

Muller, P. and Szonoky, M.: Faciostratotype Tihany-Feherpart(Hungary), (“Balatonica Beds” by Lorenthey, 1905), in: Ste-vanovic, P., Nevesskaya, L., Marinescu, F., Sokac, A., andJambor, A. (Eds.): Chronostratigrapie und Neostratotypen,Neogen der westlichen (“Zentrale”) Paratethys, Pontien, Jazuand Sanu, Zagreb-Beograd, 427–436, 1990.

Muller, P., Geary, D. H., and Magyar, I.: The endemic molluscsof the Late Miocene Lake Pannon: their origin, evolution andfamily-level taxonomy, Lethaia., 32, 47–60, 1999.

Papp, A., Jambor, A., and Steininger, F. F. (Eds.): Chronostrati-graphie und Neostratotypen, Miozan der Zentralen Paratethys 7,Pannoniaen. Akademiai Kiado, Budapest, 636pp, 1985.

Pecskay, Z., Lexa, J., Szakacs, A., Balogh, K., Seghedi, I., Konecny,V., Kovacs, M., Marton, E., Kaliciak, M., Szeky-Fux, V., Poka,T., Gyarmati, P., Edelstein, O., Rosu, E., and Zec, B.: Spaceand time distribution of Neogene-Quaternary volcanism rocks inthe Carpatho-Pannonian Region, in: Downes, H. and Vaselli,O. (Eds.): Neogene and related magmatism in the Carpatho-Pannonian Region, Acta Vulcanol., 7, 15–28, 1995.

Pevzner, M. A.: The Pontian of the Eastern Paratethys: its durationand position in the magnetochronological scale, Ann. Inst. Geol.Publ. Hung., 70, 169–171, 1987.

Pogacsas, Gy., Lakatos, L.,Ujszaszi, K., Vakarcs, G., Varkonyi, L.,Varnai, P., and Revesz, I.: Seismic facies, electro facies and Neo-gene sequence chronology of the Pannonian basin, Acta Geol.Hung., 31 (3-4), 175–207, 1988.

Roth, L.: Geologische Skizze des Kroisbach-Ruster Bergzuges unddes sudlichen Teiles des Leita-Gebirges, Foldtani Kozlony, Bu-dapest, 9, 139–150, 1879.

Rogl, F.: Stratigraphic correlation of the Paratethys Oligocene andMiocene. Mitt. Ges. Geol. Bergbaustud.Osterr., Wien, 41, 65–73, 1996.

Rogl, F.: Paleogeographic considerations for Mediterranean andParatethys seaways (Oligocene and Miocene), Ann. Naturhist.Mus. Wien, 99 A, 279–310, 1998.

Rogl, F. and Steininger, F. F.: Vom Zerfall de Tethys zu Mediterranund Paratethys. Die neogene Palaogeographie und Palinspastikdes zirkum-mediterranen Raumes, Ann. Naturhist. Mus. Wien,85 A, 135–163, 1983.

Rogl, F., Bernor, R. L., Dermitzakis, M. D., Muller, C., andStancheva, M.: On the Pontian correlation in the Aegean (AeginaIsland), Newsletter Stratigr., 24 (3), 137–158, 1991.

Sacchi, M.: Late Miocene evolution of the western Pannonianbasin, Hungary, Ph.D. thesis, Eotvos Lorand University, Bu-dapest, Hungary, 193pp, 2001.

Sacchi, M., Horvath, F., and Magyari, O. : Role of unconformity-bounded units in the stratigraphy of the continental record: a case

study from the Late Miocene of the western Pannonian basin,Hungary, in: D. B. Jolivet, L., Horvath, F., and Seranne, M.:The Mediterranean Basins: Tertiary Extension within the AlpineOrogen, Geological Society, London, Special Publications, 156,357–390, 1999a.

Sacchi, M., Horvath, F., Magyar, I., and Muller, P.: Problems andprogress in establishing a Late Neogene Chronostratigraphy forthe Central Paratethys, Neogene Newsletter, Padova, 4, 37–46,1997.

Sacchi, M., Horvath, F., Magyar, I., and Muller, P.: Problemsand progress in establishing a Late Neogene Chronostratigra-phy for the Central Paratethys. Comments and Replies, NeogeneNewsletter, 6, 25–59, 1999b.

Salvador, A. (Ed.): International Stratigraphic Guide. InternationalSubcommission on Stratigraphic classification of InternationalCommission on Stratigraphy, The Geological Society of Amer-ica, 215pp, 1994.

Steininger, F. F., Muller, C., and Rogl, F.: Correlation of Cen-tral Paratethys, Eastern Paratethys and Mediterranean stages, in:Royden, L. H. and Horvath, F. (Eds.): The Pannonian Basin: astudy in basin evolution, AAPG Mem., 45, 79–87, 1988.

Steininger, F. F., Bernor, R. L., Fahlbusch, V., and Mein, P.: Eu-ropean Neogene marine/continental chronologic relations, in:Lindsay, E. H., Fahlbusch, V., and Mein, P. (Eds.): EuropeanNeogene Mammal Chronology, Plenum Press, New York, 15–46, 1990.

Stevanovic, P. M.: Pontische Stufe im engeren Sinne – Obere Con-gerienschichten Serbiens und der angrenzenden Gebiete. Ser-bische Akademie der Wissenschaften, Sonderausgabe, Mathe-matisch-Naturwissenschaftliche Klasse, 2, Beograd, 187, 1–351,1951.

Stevanovic, P. M., Nevesskaya, L. A., Marinescu, F., Sokac, A.,and Jambor,A. (Eds.): Chronostratigraphie und Neostratotypen,Neogen der westlichen (“Zentrale”) Paratethys 8, Pontien, Jazuand Sanu, Zagreb-Beograd, 952pp, 1990.

Ujszaszi, K. and Vakarcs, G.: Sequence stratigraphic analysis inthe South Transdanubian region, Hungary, Geophysical Transac-tions, 38, 2–3, 69–87, 1993.

Vail, P. R.: Seismic stratigraphy interpretation procedure, AAPGStudies in Geology, 27, 1, 1–10, 1987.

Vakarcs, G.: Sequence stratigraphy of the Cenozoic Pannonianbasin, Hungary, PhD thesis, Rice University, Houston, Texas,514pp, 1997.

Vakarcs, G., Vail, P. R., Tari, G., Pogacsas, Gy., Mattick, R. E.,and Szabo, A.: Third-order Miocene-Pliocene depositional se-quences in the prograding delta complex of the Pannonian Basin,Tectonophysics, 240, 81–106, 1994.

Vass, D., Kovac, M., and Lexa, J.: Molasse basins and volcanic ac-tivity in west Carpathian Neogene. Its evolution and geodynamiccharacter, Geol. Carpathica, 39, 539–561, 1988.

Vass, D., Repcok, I., Balogh, K., and Halmai, J.: Revised radiomet-ric time-scale for central Paratethyan Neogene, Ann. Inst. Geol.Publ. Hung. LXX, 423–434, 1987.

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