The Messinian problem in the Pannonian Basin ... - geo.edu.ro

Sedimentary Geology 201 (2007) 111 – 140 

www.elsevier.com/locate/sed<strong>geo</strong> 

<strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> <strong>problem</strong> <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, 

Eastern Hungary — Insights from 

stratigraphic simulations 

Istvan Csato a, ⁎ , Christopher G. St C. Kendall b , Phil D. Moore c 

a Department of Geology, Coll<strong>in</strong> College, 2800 Spr<strong>in</strong>g Creek Pkwy, Plano TX 75074, United States 

b Department of Geology, University of South Carol<strong>in</strong>a, Columbia, SC 29208, United States 

c Research Comput<strong>in</strong>g Center, College of Arts and Sciences, University of South Carol<strong>in</strong>a, Columbia, SC 29208, United States 

Received 27 July 2006; received <strong>in</strong> revised form 23 April 2007; accepted 2 May 2007 

Abstract 

Earlier studies revealed a prom<strong>in</strong>ent unconformity <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> stratigraphic record of <strong>the</strong> lacustr<strong>in</strong>e <strong>Pannonian</strong> Bas<strong>in</strong>, but it 

was unclear what factors were responsible for <strong>the</strong> formation of this unconformity, and thus its orig<strong>in</strong> rema<strong>in</strong>ed controversial. <strong>The</strong> 

<strong>problem</strong> was fur<strong>the</strong>r complicated by <strong>the</strong> fact that stratal patterns <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> varied significantly along <strong>the</strong> paleo-marg<strong>in</strong>s of 

<strong>the</strong> lake. Our study <strong>in</strong>troduces quantitative stratigraphic simulations to analyze <strong>the</strong> role of subsidence, sediment supply, and lakelevel 

changes <strong>in</strong> <strong>the</strong> formation of <strong>the</strong> unconformity and <strong>the</strong> various architectural patterns that evolved <strong>in</strong> response to <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> 

events. <strong>The</strong> results suggest that a relative lake-level fall occurred <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>, accompanied and followed by tectonic <strong>in</strong>version 

<strong>in</strong> several parts of <strong>the</strong> bas<strong>in</strong>. S<strong>in</strong>ce <strong>the</strong> rate of tectonic subsidence and/or uplift varied <strong>in</strong> space and time, <strong>the</strong> size of <strong>the</strong> relative lakelevel 

fall varied significantly across <strong>the</strong> bas<strong>in</strong>, while various stratal architectural patterns formed <strong>in</strong> <strong>the</strong> same time <strong>in</strong>terval. <strong>The</strong> age 

of <strong>the</strong> unconformity was estimated, based on seismic correlations with paleomagnetic chronozones, to be between 5–6 Ma, which 

was ref<strong>in</strong>ed by stratigraphic simulations. Galeacysta etrusca cysts were found <strong>in</strong> <strong>the</strong> unconformity, which confirmed its late 

<strong>Mess<strong>in</strong>ian</strong> age. <strong>The</strong> surface is called <strong>the</strong> Intra-<strong>Mess<strong>in</strong>ian</strong> Unconformity (IMU) <strong>in</strong> this paper. Seismic <strong>in</strong>terpretations and simulations 

of stratal architecture led to <strong>the</strong> formulation of a bas<strong>in</strong> fill model and identification of four stratigraphic architectural patterns related 

to <strong>Mess<strong>in</strong>ian</strong> events <strong>in</strong>clud<strong>in</strong>g a major lake-level fall and coeval and subsequent uplift events <strong>in</strong> certa<strong>in</strong> parts of <strong>the</strong> bas<strong>in</strong>. 

© 2007 Elsevier B.V. All rights reserved. 

Keywords: <strong>Pannonian</strong> Bas<strong>in</strong>; <strong>Mess<strong>in</strong>ian</strong>; Stratigraphic model<strong>in</strong>g; Sal<strong>in</strong>ity crisis; Galeacysta etrusca 

1. Introduction: significance of <strong>the</strong> “<strong>Mess<strong>in</strong>ian</strong> 

<strong>problem</strong>” <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> 

<strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis, <strong>the</strong> desiccation of <strong>the</strong> 

Mediterranean Sea and its stratigraphic, tectonic and 

⁎ Correspond<strong>in</strong>g author. Tel.: +1 972 881 5712. 

E-mail address: icsato@ccccd.<strong>edu</strong> (I. Csato). 

climatic implications have attracted great <strong>in</strong>terest and 

extensive research. <strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> events <strong>in</strong> adjacent nonmar<strong>in</strong>e 

bas<strong>in</strong>s, such as <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> <strong>in</strong> Hungary are 

still not very well understood. Endemic fauna and scarcity 

of accurate age data make stratigraphic correlations <strong>in</strong> <strong>the</strong> 

late Miocene–Pliocene strata a great challenge. <strong>The</strong> goal of 

this paper is to generate an <strong>in</strong>sight <strong>in</strong>to <strong>the</strong> complex 

stratigraphic events that occurred <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> <strong>in</strong> 

<strong>Mess<strong>in</strong>ian</strong> time: called <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> <strong>problem</strong> <strong>in</strong> this paper. 

0037-0738/$ - see front matter © 2007 Elsevier B.V. All rights reserved. 

doi:10.1016/j.sed<strong>geo</strong>.2007.05.005

112 I. Csato et al. / Sedimentary Geology 201 (2007) 111–140 

Csato (1989, 1993) recognized a prom<strong>in</strong>ent unconformity 

formed <strong>in</strong> <strong>Mess<strong>in</strong>ian</strong> time with<strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> 

Bas<strong>in</strong>, and proposed a division of <strong>the</strong> postrift strata by this 

unconformity <strong>in</strong>to two major units. <strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> event 

that formed <strong>the</strong> unconformity and brought about <strong>the</strong> related 

paleo<strong>geo</strong>graphic changes <strong>in</strong> <strong>the</strong> bas<strong>in</strong> was <strong>in</strong>terpreted to 

be coeval with <strong>the</strong> sal<strong>in</strong>ity crisis <strong>in</strong> <strong>the</strong> Mediterranean. 

S<strong>in</strong>ce <strong>the</strong> lacustr<strong>in</strong>e <strong>Pannonian</strong> Bas<strong>in</strong> was assumed to be 

separated from <strong>the</strong> Mediterranean at this time, it rema<strong>in</strong>ed 

unclear whe<strong>the</strong>r <strong>the</strong> formation of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> unconformity 

could be expla<strong>in</strong>ed by a paleo<strong>geo</strong>graphic connection 

to <strong>the</strong> Mediterranean. Thus <strong>the</strong> “<strong>Mess<strong>in</strong>ian</strong> <strong>problem</strong>” <strong>in</strong> <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong> has a regional significance as to whe<strong>the</strong>r 

<strong>the</strong> major lake-level fall was l<strong>in</strong>ked to <strong>the</strong> desiccation of <strong>the</strong> 

Mediterranean. If it was, <strong>the</strong> question arises as to whe<strong>the</strong>r 

direct mar<strong>in</strong>e connections existed temporarily or o<strong>the</strong>r 

factors, such as changes <strong>in</strong> fluvial dra<strong>in</strong>age were 

responsible. It is also unclear what role tectonic reorganizations 

played <strong>in</strong> <strong>the</strong> formation of <strong>the</strong> <strong>Pannonian</strong> lake-level 

fall <strong>in</strong> <strong>Mess<strong>in</strong>ian</strong> time. 

In addition to formulation of regional tectono-sedimentary 

models, <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> <strong>problem</strong> <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> 

Bas<strong>in</strong> has economic significance as well. <strong>The</strong> major lakelevel 

fall generated substantial resedimentation and deposition 

of fall<strong>in</strong>g stage and lowstand systems tract sediments. 

<strong>The</strong>se facies have potential for form<strong>in</strong>g regional stratigraphic 

traps for hydrocarbons, provided o<strong>the</strong>r conditions, 

such as source rock and seal<strong>in</strong>g are favorable. This stratigraphic 

play must have developed not only <strong>in</strong> Hungary but 

also <strong>in</strong> neighbor<strong>in</strong>g countries where <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> is 

preserved, as <strong>the</strong> lake-level fall was a bas<strong>in</strong>-wide event and 

affected <strong>the</strong> paleo-marg<strong>in</strong>al areas all around <strong>the</strong> bas<strong>in</strong>. 

This paper focuses on <strong>the</strong> formation of stratigraphic 

architectural patterns and <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> unconformity. 

Subsurface data, <strong>in</strong>clud<strong>in</strong>g seismic and well log sections 

were <strong>the</strong> primary source of our analysis; sequence 

stratigraphic <strong>in</strong>terpretations followed by computer simulation 

of stratigraphic architectural patterns were used to 

model possible scenarios of <strong>the</strong> evolution of stratigraphy. 

<strong>The</strong> simulations tested whe<strong>the</strong>r <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> unconformity 

was produced by a “eustatic” lake-level change and/ 

or by o<strong>the</strong>r factors. It analyzed how subsidence and 

sediment supply may have contributed to <strong>the</strong> formation of 

<strong>the</strong> various stratal patterns. 

2. Geological overview 

2.1. Tectonic sett<strong>in</strong>g 

<strong>The</strong> <strong>Pannonian</strong> Bas<strong>in</strong> is a Neogene extensional bas<strong>in</strong> 

that lies between <strong>the</strong> Carpathian, Alp<strong>in</strong>e and D<strong>in</strong>aride 

thrust belts (Fig. 1) with<strong>in</strong> <strong>the</strong> mega-suture zone of <strong>the</strong> 

Fig. 1. Location of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> and Lake Pannon at <strong>Mess<strong>in</strong>ian</strong> time. Map of Lake Pannon is modified from Magyar et al. (1999).

I. Csato et al. / Sedimentary Geology 201 (2007) 111–140 

113 

African and European plates. <strong>The</strong> basement of <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong> consists of Paleogene and Paleozoic to 

Cretaceous crustal fragments that became imbricate 

nappes dur<strong>in</strong>g <strong>the</strong> Cretaceous Alp<strong>in</strong>e collision (Csontos 

et al., 1992; Tari et al., 1992). <strong>The</strong> large-scale 

allochthony of <strong>the</strong> Transdanubian Range was suggested 

by Horváth (1993). Tari (1996) and Mattick et al. (1996) 

believed that <strong>the</strong> nappe pile of <strong>the</strong> Eastern Alps 

cont<strong>in</strong>ued beneath <strong>the</strong> Danube Bas<strong>in</strong> towards <strong>the</strong> 

Transdanubian Range and <strong>the</strong> Western Carpathians. 

Nappes of Late Cretaceous <strong>in</strong> age have also been proven 

below <strong>the</strong> Great Hungarian Pla<strong>in</strong> (Grow et al., 1994). 

<strong>The</strong> <strong>Pannonian</strong> basement is composed of two ma<strong>in</strong> 

tectonic terra<strong>in</strong>s or micro-plates: <strong>the</strong> nor<strong>the</strong>rn Alp<strong>in</strong>e– 

Carpathian–<strong>Pannonian</strong> (ALCAPA) unit and <strong>the</strong> sou<strong>the</strong>rn 

<strong>Pannonian</strong> or Tisza–Dacia unit or Tisza Mega-unit (Haas 

and Péró, 2004) juxtaposed along <strong>the</strong> Mid-Hungarian 

shear zone (Fig. 2). <strong>The</strong> nor<strong>the</strong>rn unit orig<strong>in</strong>ated by a large 

lateral displacement caused by tectonic escape from <strong>the</strong> 

compressional zone of <strong>the</strong> Sou<strong>the</strong>rn Alps <strong>in</strong> <strong>the</strong> 

Paleogene–early Miocene (Ratschbacher et al., 1991). 

At <strong>the</strong> same time, <strong>the</strong> south <strong>Pannonian</strong> terra<strong>in</strong> experienced 

a different k<strong>in</strong>ematic history, <strong>in</strong>clud<strong>in</strong>g a nearly 90° 

clockwise rotation (Patrascu et al., 1994). It is subdivided 

<strong>in</strong>to NE–SW trend<strong>in</strong>g units based on dist<strong>in</strong>ct Mesozoic 

facies differences. At present, <strong>the</strong>se units are organized <strong>in</strong> 

a north-vergent folded belt, cropp<strong>in</strong>g out <strong>in</strong> <strong>the</strong> Apuseni 

Mounta<strong>in</strong>s <strong>in</strong> Romania and <strong>the</strong> Mecsek and Villány 

Mounta<strong>in</strong>s <strong>in</strong> Hungary. Csontos and Nagymarosy (1998) 

proposed a counterclockwise rotation of <strong>the</strong> ALCAPA 

and a clockwise motion of <strong>the</strong> Tisza–Dacia unit <strong>in</strong> late 

Oligocene–Miocene time. <strong>The</strong>y believed that <strong>the</strong> 

ALCAPA unit was thrust over <strong>the</strong> Tisza–Dacia unit 

along <strong>the</strong> Mid-Hungarian l<strong>in</strong>e. <strong>The</strong> pre-Tertiary structural 

units were studied <strong>in</strong> great detail by Haas et al. (2000). 

<strong>The</strong> formation of <strong>the</strong> Neogene <strong>Pannonian</strong> Bas<strong>in</strong> was 

studied by Royden et al. (1983a,b) and Royden and Báldi 

(1988) us<strong>in</strong>g <strong>the</strong>rmo-tectonic models. <strong>The</strong>ir results 

<strong>in</strong>dicate that <strong>in</strong>itial crustal th<strong>in</strong>n<strong>in</strong>g or rift<strong>in</strong>g occurred <strong>in</strong> 

<strong>the</strong> Middle Miocene and subsequent <strong>the</strong>rmal subsidence 

or <strong>the</strong> post-rift phase extended up to <strong>the</strong> present. Tari et al. 

(1992) and Horváth (1993) po<strong>in</strong>ted out that s<strong>in</strong>ce 

Neogene extension was superimposed on an earlier 

Alp<strong>in</strong>e compressional realm, <strong>the</strong> basement structures 

<strong>in</strong>fluenced <strong>the</strong> magnitude and <strong>geo</strong>metry of <strong>the</strong> subsequent 

cont<strong>in</strong>ental extension by reactivation of regional decollement 

levels. Apply<strong>in</strong>g Buck (1991)'s cont<strong>in</strong>ental extensional 

k<strong>in</strong>ematic model, it was proposed that <strong>the</strong> extension 

locally unroofed deep-ly<strong>in</strong>g rock masses, and eventually 

exposed metamorphic core complexes (Tari and Horváth, 

1995) <strong>in</strong> <strong>the</strong> Middle Miocene. <strong>The</strong> core complex 

extension was followed by wide-rift extension and f<strong>in</strong>ally 

Fig. 2. Structural units of <strong>the</strong> pre-Neogene basement <strong>in</strong> eastern Hungary (after Haas and Péró, 2004). Seismic Sections A, B, C and D are presented <strong>in</strong> 

Figs. 5−8.


by narrow-rift style extension <strong>in</strong> certa<strong>in</strong> deep sub-bas<strong>in</strong>s. 

Huismans et al. (2001) also <strong>in</strong>terpreted two ma<strong>in</strong> rift 

stages, one at 17.5–14 Ma and ano<strong>the</strong>r 11.5–8(?) Ma, 

separated by a compressional event that affected most of 

<strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. <strong>The</strong> observed unconformity at 

14 Ma (Horváth, 1995; Huismans et al., 2001)thatmarks 

<strong>the</strong> end of <strong>the</strong> first rift<strong>in</strong>g phase (mid-Badenian stage <strong>in</strong> 

Central Paratethys nomenclature) corresponds clearly 

with Hámor (1985)'s division between <strong>the</strong> Styre and 

Lei<strong>the</strong> orogenic cycles. It is believed that <strong>the</strong> earlier 

extension was driven by subduction roll-back along <strong>the</strong> 

Carpathian front <strong>in</strong> a back-arc sett<strong>in</strong>g (Horváth and 

Berckhemer, 1982; Royden, 1988) and <strong>the</strong> second, Upper 

Miocene (Sarmatian) extension was associated with 

as<strong>the</strong>nospheric upwell<strong>in</strong>g and rift push forces (Huismans 

et al., 2001). 

Initially, <strong>the</strong> Upper Miocene–Quaternary period of 

bas<strong>in</strong> evolution was thought to be tectonically quiet 

(Sclater et al., 1980). Vakarcs et al. (1994) observed 

signs of uplift based on seismic data at <strong>the</strong> bas<strong>in</strong> marg<strong>in</strong>s 

attributable to late stage compression of <strong>the</strong> bas<strong>in</strong>. 

Horváth (1995) published results from seismic <strong>in</strong>terpretations 

and paleo- and recent stress determ<strong>in</strong>ations 

that suggest at least two compressional events occurred 

<strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> <strong>in</strong> this time period. Accord<strong>in</strong>g to 

<strong>the</strong>se f<strong>in</strong>d<strong>in</strong>gs, <strong>the</strong> earlier event took place at about 10– 

11 Ma, and <strong>the</strong> later event was thought to have happened 

around 3 Ma. Csato (1995) us<strong>in</strong>g stratigraphic simulations 

suggested a <strong>Mess<strong>in</strong>ian</strong>–Pliocene <strong>in</strong>version. Horváth 

and Cloet<strong>in</strong>gh (1996) expla<strong>in</strong>ed <strong>the</strong> Quaternary 

differential movements (subsidence <strong>in</strong> <strong>the</strong> <strong>in</strong>ternal parts 

of <strong>the</strong> bas<strong>in</strong> and coeval uplift at <strong>the</strong> marg<strong>in</strong>s) as caused 

by an <strong>in</strong>crease <strong>in</strong> magnitude of horizontal compressional 

<strong>in</strong>traplate stresses. 

2.2. Sedimentary fill 

<strong>The</strong> <strong>Pannonian</strong> Bas<strong>in</strong> was filled by large deltaic 

systems that orig<strong>in</strong>ated from <strong>the</strong> ris<strong>in</strong>g Carpathians, Alps 

and D<strong>in</strong>arides. An understand<strong>in</strong>g of <strong>the</strong> late Miocene– 

Pliocene sedimentary history of <strong>the</strong> lacustr<strong>in</strong>e bas<strong>in</strong> fill 

developed from three major sources. <strong>The</strong> first was a 

seismic stratigraphic model <strong>in</strong>troduced by Mattick et al. 

(1988) and Pogácsás et al. (1988). This approach, toge<strong>the</strong>r 

Fig. 3. Location of data set. Coreholes with paleomagnetic <strong>in</strong>formation: T (Tiszapalkonya-I), D (Dévaványa-1), V (Vésztő-1); <strong>the</strong> l<strong>in</strong>es are <strong>the</strong> 

locations of seismic sections used <strong>in</strong> this study, seismic Sections A, B, C, D are presented <strong>in</strong> Figs. 5–8; Well logs are presented <strong>in</strong> Fig. 16: W-1 (Well- 

1), W-3 (Well-3); Basement features: J (Jászság Bas<strong>in</strong>), A (Algyő High), M (Makó Trough), B (Battonya High), BB (Békés Bas<strong>in</strong>), De (Derecske 

Trough); contour l<strong>in</strong>es represent <strong>the</strong> depths of <strong>the</strong> pre-Neogene basement <strong>in</strong> meters after Juhász (1998).


115 

with sedimentological analysis of deltaic and turbiditic 

systems (Bérczi and Philips, 1985; Bérczi, 1988), 

generated a new understand<strong>in</strong>g of <strong>the</strong> depositional 

mechanisms and facies systems of <strong>the</strong> bas<strong>in</strong> fill. <strong>The</strong> 

<strong>in</strong>itial seismic stratigraphic concept was ref<strong>in</strong>ed and 

developed <strong>in</strong>to a more sophisticated sequence stratigraphic 

model by Pogácsás et al. (1992, 1993), Újszászi and 

Vakarcs (1993), Vakarcs et al. (1994) and Vakarcs (1997). 

<strong>The</strong> second source was well log correlations across <strong>the</strong> 

entire <strong>Pannonian</strong> Bas<strong>in</strong> conducted by Gajdos (1989) tied 

to modern delta depositional models. He recognized that 

<strong>the</strong> eastern <strong>Pannonian</strong> Bas<strong>in</strong> was filled from two ma<strong>in</strong> 

sedimentary sources, one <strong>in</strong> <strong>the</strong> nor<strong>the</strong>ast, and a younger 

one advanc<strong>in</strong>g from <strong>the</strong> northwest. He also identified 

o<strong>the</strong>r large delta systems to <strong>the</strong> south. F<strong>in</strong>ally, Pogácsás et 

al. (1992, 1993, 1994) correlated radiometric and 

paleomagnetic ages across <strong>the</strong> bas<strong>in</strong> establish<strong>in</strong>g a new 

chronostratigraphy and advanc<strong>in</strong>g understand<strong>in</strong>g of <strong>the</strong> 

non-mar<strong>in</strong>e bas<strong>in</strong> fill history. 

Most of <strong>the</strong> papers <strong>in</strong> <strong>the</strong> late 1980s and early 1990s 

correlated third-order lake-level changes to <strong>the</strong> Haq et al. 

(1987) eustatic curve, argu<strong>in</strong>g that <strong>the</strong> lake-level changes 

<strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> dur<strong>in</strong>g <strong>the</strong> Late Miocene and 

Pliocene were <strong>in</strong> phase with global sea-level. Mattick 

et al. (1994) proposed that <strong>the</strong> sequences <strong>the</strong>y identified 

were produced by delta lobe switch<strong>in</strong>g <strong>in</strong> a bas<strong>in</strong> that 

Fig. 4. Correlation of paleomagnetic chronozones from Tiszapalkonya-I, Dévaványa-1 and Vésztő-1 coreholes (after Elston et al., 1994) to <strong>the</strong> global 

scale (Berggren et al., 1995). <strong>The</strong> Intra-<strong>Mess<strong>in</strong>ian</strong> Unconformity (IMU) formed approximately <strong>in</strong> C3r–C3An zones.

Fig. 5. Seismic Section A (see Fig. 3 for location). <strong>The</strong> IMU clearly divides <strong>the</strong> sedimentary fill <strong>in</strong>to two major units. <strong>The</strong> bas<strong>in</strong> edges underwent tectonic <strong>in</strong>version and uplift from late <strong>Mess<strong>in</strong>ian</strong> 

onward. Mi: Middle Miocene synrift unit. Kiskunság- and Hajdúság-type Architecture: categories of stratal patterns of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> coasts; see Section 4.5 and Fig. 9 for details. 

116 I. Csato et al. / Sedimentary Geology 201 (2007) 111–140


Fig. 6. Seismic Section B (see Fig. 3 for location). A late (probably Quaternary) uplift occurred at <strong>the</strong> Algyő High. A: Algyő High, M: Makó Trough, B: Battonya High, BB: Békés Bas<strong>in</strong>, De: Derecske 

Trough. Hajdúság-type Architecture: a category of stratal pattern of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> coasts; see Section 4.5 and Fig. 9 for details. 

117

Fig. 7. Seismic Section C (see Fig. 3 for location). <strong>The</strong> northwestern edge of <strong>the</strong> bas<strong>in</strong> underwent uplift from <strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> to <strong>the</strong> Quaternary. J: Jászság Bas<strong>in</strong>, BB: Békés Bas<strong>in</strong>, B: Battonya High; 

Mi: Middle Miocene synrift unit. Battonya-type Architecture: a category of stratal pattern of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> coasts; see Section 4.5 and Fig. 9 for details. 



119 

Fig. 8. Seismic Section D (see Fig. 3 for location). This section connects <strong>the</strong> Jászság- and <strong>the</strong> Hajdúság-type architectural patterns (see Section 4.5 and 

Fig. 9 for details): <strong>The</strong> IMU is a type I unconformity <strong>in</strong> <strong>the</strong> Hajdúság-type architecture where a large lowstand systems tract formed above it; and it is a 

type II unconformity with a shelf marg<strong>in</strong>-type systems tract <strong>in</strong> <strong>the</strong> Jászság-type architecture. Mi: Middle Miocene synrift unit. bs: bas<strong>in</strong> floor fan-slope 

fan; pw: lowstand prograd<strong>in</strong>g wedge; LST: Lowstand Systems Tract; TST: Transgressive Systems Tract; HST: Highstand Systems Tract; SMST: 

Shelf Marg<strong>in</strong> Systems Tract. 

progressively became shallower with time. Juhász et al. 

(1997, 1999) carried out a detailed cycle analysis us<strong>in</strong>g 

well data and concluded that <strong>the</strong> <strong>Pannonian</strong> sequences 

were not controlled by eustatic changes. Instead, <strong>the</strong>y 

suggested that <strong>the</strong> rhythm of <strong>the</strong> water level changes <strong>in</strong> <strong>the</strong> 

<strong>Pannonian</strong> Lake was opposite to that of <strong>the</strong> eustatic 

changes of <strong>the</strong> world oceans. <strong>The</strong>y believed that <strong>the</strong> highfrequency 

cyclicity <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> was driven by 

climatic changes coupled with changes <strong>in</strong> sediment 

supply. Cloet<strong>in</strong>gh (1988) proposed that changes <strong>in</strong> 

<strong>in</strong>traplate stresses could also expla<strong>in</strong> relative sea-level 

changes. Sacchi et al. (1999) based on detailed <strong>in</strong>tegrated 

stratigraphic studies <strong>in</strong> <strong>the</strong> western <strong>Pannonian</strong> Bas<strong>in</strong> saw 

no evidence that <strong>the</strong> unconformities <strong>in</strong> <strong>the</strong> bas<strong>in</strong> fill were 

l<strong>in</strong>ked to eustatic changes. 

A significant unconformity formed <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>, 

termed Intra-<strong>Mess<strong>in</strong>ian</strong> Unconformity (IMU) <strong>in</strong> this 

paper. Paleo<strong>geo</strong>graphical isolation of <strong>the</strong> Mediterranean 

took place <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> and <strong>the</strong> Mediterranean bas<strong>in</strong> 

became desiccated. This event, known as <strong>the</strong> Mediterranean 

sal<strong>in</strong>ity crisis (Hsü et al., 1977; Cita, 1982; Cita, 

1991), co<strong>in</strong>cided with <strong>the</strong> formation of widespread 

erosional surfaces around <strong>the</strong> marg<strong>in</strong>s of <strong>the</strong> Mediterranean 

(Cita and Ryan, 1978). Us<strong>in</strong>g astronomically 

calibrated stratigraphic data Krijgsman et al. (1999) 

dated <strong>the</strong> onset of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis to 5.96± 

0.02 Ma. Separated by <strong>the</strong> ris<strong>in</strong>g Carpathian–D<strong>in</strong>aride 

mounta<strong>in</strong> belt, <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> was already a lake 

at this time. <strong>The</strong> question arises as to whe<strong>the</strong>r <strong>the</strong> IMU, 

formed <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> close to <strong>the</strong> Miocene–


Pliocene boundary, was caused by <strong>the</strong> sal<strong>in</strong>ity crisis or 

whe<strong>the</strong>r <strong>the</strong> tim<strong>in</strong>g was a co<strong>in</strong>cidence and o<strong>the</strong>r factors 

were responsible for this feature. 

3. Data and methods: seismic <strong>in</strong>terpretations and 

stratigraphic simulations 

<strong>The</strong> stratigraphic architecture of a bas<strong>in</strong> evolves as a 

dynamic response to <strong>the</strong> comb<strong>in</strong>ed effect of subsidence/ 

uplift, sea/lake-level changes and sediment supply (e.g. 

Helland-Hansen and Gjelberg, 1994). In many cases, it 

is difficult to decipher <strong>the</strong> relative roles of <strong>the</strong>se three 

ma<strong>in</strong> factors from observations of <strong>the</strong> stratigraphic 

record. Passive cont<strong>in</strong>ental marg<strong>in</strong>s, where <strong>the</strong> concept 

of seismic stratigraphy was orig<strong>in</strong>ally formulated (Vail 

et al., 1977), have relatively slow and steady subsidence 

rates and sediment supply, thus <strong>the</strong> stratigraphic 

sequences may be <strong>the</strong> products of eustatic sea-level 

variations. However, rapidly subsid<strong>in</strong>g sub-bas<strong>in</strong>s, 

ris<strong>in</strong>g marg<strong>in</strong>s and differential subsidence patterns are 

common to various tectonic zones of active extensional 

sett<strong>in</strong>gs. <strong>The</strong> sediment supply can vary greatly, both <strong>in</strong> 

time and space, respond<strong>in</strong>g to local uplift<strong>in</strong>g zones that 

may act as po<strong>in</strong>t sources of sediments (e.g. Gawthorpe et 

al., 1994; Thamó-Bozsó et al., 2002). Thus <strong>the</strong> evolv<strong>in</strong>g 

sequences and stratigraphic patterns may reflect lake/ 

sea-level changes, changes <strong>in</strong> sediment supply, tectonic 

signals or some comb<strong>in</strong>ation of all. An unconformity 

might become a conformable surface along a bas<strong>in</strong> 

marg<strong>in</strong> where local subsidence/uplift rates are appropriate, 

i.e. different systems tracts may be synchronous. 

Similarly, stratigraphic patterns identical to those 

expected of transgressive and subsequent highstand 

systems tracts may be produced by changes <strong>in</strong> sediment 

supply rates without relative sea/lake changes (e.g. 

Csato and Kendall, 2002). <strong>The</strong>refore, <strong>the</strong> understand<strong>in</strong>g 

of <strong>the</strong> stratigraphy of active bas<strong>in</strong>s requires both 

observations and quantitative analysis. This paper 

records <strong>the</strong> use of computer simulations of depositional 

sequences and architectural patterns observed on 

seismic data to model <strong>the</strong> role of subsidence, sediment 

supply and lake-level changes <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. 

Computer models of sediment accumulation <strong>in</strong> bas<strong>in</strong>s 

have been classified <strong>in</strong>to <strong>geo</strong>metrical and process-based 

models (Den Bezemer et al., 2000). Geometrical models 

<strong>in</strong>volve matches between <strong>the</strong> observed stratigraphy and 

<strong>the</strong> computer output by vary<strong>in</strong>g <strong>the</strong> <strong>in</strong>put parameters that 

control tectonics and deposition. <strong>The</strong> SEDPAK stratigraphic 

simulation program (Kendall et al., 1991, 1993; 

Whittle, 1993; Moore, 1997; Lev<strong>in</strong>, 1999) provides<strong>the</strong> 

<strong>geo</strong>metrical models used for our quantitative analysis. 

<strong>The</strong> program creates accommodation by vary<strong>in</strong>g subsidence 

and sea-level. <strong>The</strong> total subsidence has two 

components: tectonic subsidence def<strong>in</strong>ed by <strong>the</strong> user; 

and flexural isostatic compensation due to sediment load. 

<strong>The</strong> sediments are compacted accord<strong>in</strong>g to compaction 

data of Baldw<strong>in</strong> and Butler (1985). <strong>The</strong> program 

simulates both clastic and carbonate sediment accumulation. 

<strong>The</strong> clastic sediments are modeled by deposition of 

mud and sand prisms <strong>in</strong> <strong>the</strong> accommodation space at rates 

def<strong>in</strong>ed by <strong>the</strong> user. Two-dimensional sections may be 

modeled with sediment supply at both ends of <strong>the</strong> 

modeled section, thus SEDPAK has <strong>the</strong> capability to 

simulate stratigraphic architectures formed from multiple 

sediment sources. When <strong>the</strong> simulation output establishes 

a satisfactory match to <strong>the</strong> observed section, it is assumed 

that <strong>the</strong> <strong>in</strong>put parameters, <strong>in</strong>clud<strong>in</strong>g subsidence, sea/lakelevel 

changes and sediment supply are correct. This way, 

a reconstruction of <strong>the</strong> stratigraphic history may be obta<strong>in</strong>ed 

and <strong>the</strong> observed stratigraphic patterns may be 

<strong>in</strong>terpreted. 

Our study focused on eastern Hungary where <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong> fill reaches its greatest depths (3–6km). 

Regional seismic sections constructed from hydrocarbon 

exploration profiles constituted <strong>the</strong> basic data set for 

<strong>in</strong>terpretations (Fig. 3). Geological time calibration was 

based on paleomagnetic <strong>in</strong>formation obta<strong>in</strong>ed from three 

core holes, namely <strong>the</strong> Tiszapalkonya-I, Dévaványa-1 and 

Vésztő-1 (Figs. 3 and 4). Magnetic polarity zones 

correlated to <strong>the</strong> global polarity scale gave numerical 

ages of <strong>the</strong> sediments (Lantos et al., 1992; Elston et al., 

1994). <strong>The</strong> depths of <strong>the</strong> polarity zones were converted to 

two-way travel time and annotated onto seismic sections 

located close to <strong>the</strong> cored holes. <strong>The</strong>n <strong>the</strong> ages were 

correlated along seismic sections across <strong>the</strong> bas<strong>in</strong>. This 

method of establish<strong>in</strong>g a chronostratigraphic framework 

of sediments <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> was first used by 

Pogácsás et al. (1992, 1993, 1994). A fourth cored hole, 

Kaskanthyú-2 lay outside our study area, but its 

microplankton zones were correlated to <strong>the</strong> magnetic 

polarity zones (Sütő-Szentai, 2000) and so could be used 

to calibrate <strong>the</strong> time framework of <strong>the</strong> simulation. 

4. Seismic <strong>in</strong>terpretations 

Three regional seismic sections that cross <strong>the</strong> <strong>Pannonian</strong> 

Bas<strong>in</strong> <strong>in</strong> eastern Hungary are shown <strong>in</strong> Figs. 5−7. 

Our study focused primarily on <strong>the</strong> bas<strong>in</strong> scale stratigraphic 

evolution seen on <strong>the</strong>se l<strong>in</strong>es with particular 

<strong>in</strong>terest <strong>in</strong> <strong>Mess<strong>in</strong>ian</strong> events. <strong>The</strong> pre-Neogene basement, 

<strong>the</strong> synrift–postrift boundary and <strong>the</strong> Intra-<strong>Mess<strong>in</strong>ian</strong> 

Unconformity (IMU) are marked on <strong>the</strong> sections. <strong>The</strong> age 

of IMU was clearly correlated between chronozones C3n 

and C3Ar, <strong>the</strong>refore its age is between 4.18 and 6.98 Ma,


121 

very likely between 5.23 and 6.56 Ma (Fig. 4). <strong>The</strong> 

exist<strong>in</strong>g paleomagnetic data do not allow more accurate 

age determ<strong>in</strong>ation, but based on our simulation results 

(see Section 5.1) and especially d<strong>in</strong>oflagellate <strong>in</strong>formation, 

we suggest a possible age range between 5 and 6 Ma 

(5.5±0.5 Ma), likely to be close to 5.3–5.5 Ma (see 

discussion <strong>in</strong> Section 7). 

4.1. Section A 

<strong>The</strong> IMU <strong>in</strong> eastern Hungary is clearly identified on 

seismic profiles. Section A is an example (Fig. 5), oriented 

NE–SW mostly along <strong>the</strong> Szolnok Unit of Haas and Péró 

(2004) (Fig. 2). <strong>The</strong> nor<strong>the</strong>astern part of this unit is 

represented by <strong>the</strong> Cretaceous–Paleogene “flysch” successions 

and its southwestern part is composed of 

Jurassic–Lower Cretaceous sedimentary and volcanic 

rocks. <strong>The</strong> flysch unit is divided <strong>in</strong>to two segments <strong>in</strong> 

Section A by a deep half-graben. <strong>The</strong> synrift succession 

accumulated mostly <strong>in</strong> <strong>the</strong> Langhian–Serravallian (middle 

Miocene) time <strong>in</strong>terval (Karpatian–Badenian regional 

stages, Hámor, 1997). <strong>The</strong> two major pre-Neogene units 

have an abrupt tectonic contact and each of <strong>the</strong>m 

underwent rift<strong>in</strong>g by form<strong>in</strong>g half-graben and occasionally 

full-graben structures. <strong>The</strong> synrift phase ended <strong>in</strong> <strong>the</strong> 

late Serravallian (Sarmatian regional stage) when, as 

Horváth (1995) po<strong>in</strong>ted out, a compressional tectonic 

event coupled with a eustatic sea-level fall produced a 

marked unconformity surface throughout <strong>the</strong> <strong>Pannonian</strong> 

Bas<strong>in</strong>. <strong>The</strong> identification of <strong>the</strong> pre-Neogene basement 

and <strong>the</strong> top synrift surface on <strong>the</strong> seismic section was 

based on reflection characteristics and well <strong>in</strong>formation 

available on <strong>the</strong> l<strong>in</strong>e of section. 

<strong>The</strong> postrift sedimentary fill is composed of two 

sequences separated by <strong>the</strong> IMU. This two-fold division is 

evident everywhere <strong>in</strong> eastern Hungary. S<strong>in</strong>ce <strong>the</strong> age of 

IMU is estimated ∼ 5.5 Ma <strong>in</strong> our detailed correlation, we 

named <strong>the</strong> two sequences Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong> 

and Late <strong>Mess<strong>in</strong>ian</strong>–Pliocene systems, respectively. 

Marked deltaic progradation and aggradation filled a 

large part of <strong>the</strong> bas<strong>in</strong> <strong>in</strong> <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong> 

time. This unit represents a second-order (Vail et al., 1991) 

highstand systems tract. Third-order sequences (Pa1–Pa4 

sequences) were identified and correlated with<strong>in</strong> <strong>the</strong> pre- 

IMU second-order sequence by Vakarcs (1997).<strong>The</strong>se 

higher-order sequences were <strong>in</strong>terpreted to be driven by 

eustatic changes (Vakarcs et al., 1994), or eustatic and 

tectonic changes (Vakarcs, 1997) or <strong>the</strong>y may have 

evolved as sedimentary responses solely to tectonic 

activity (Juhász et al., 2006) or climatic variations (Juhász 

et al., 1997). Sacchi et al. (1999) also identified four thirdorder 

sequences (Pan-1–Pan-4) <strong>in</strong> this time <strong>in</strong>terval. 

Section A shows that a major relative lake-level fall 

occurred <strong>in</strong> <strong>Mess<strong>in</strong>ian</strong> time and produced <strong>the</strong> IMU. This 

relative lake-level fall apparently affected <strong>the</strong> entire 

bas<strong>in</strong> and a major reorganization of sedimentation 

followed. <strong>The</strong> highly progradational–aggradational 

deltaic advancement stopped and thick fall<strong>in</strong>g stage 

and lowstand systems tracts (Catuneanu, 2002, 2006) 

formed at <strong>the</strong> paleo-marg<strong>in</strong>s (see paleo-marg<strong>in</strong>s marked 

Kiskunság-type and Hajdúság-type Architecture <strong>in</strong> 

Fig. 5, and for more detailed explanation see Section 

4.5 and Fig. 9). <strong>The</strong> entire Late-<strong>Mess<strong>in</strong>ian</strong>–Pliocene 

bas<strong>in</strong> fill is a major retrogradational system. Vakarcs 

(1997) identified three more third-order sequences and 

Sacchi et al. (1999) one more sequence above <strong>the</strong> IMU. 

<strong>The</strong> seismic section shows that <strong>the</strong> bas<strong>in</strong> marg<strong>in</strong>s are 

tilted today <strong>in</strong> response to tectonic <strong>in</strong>version. <strong>The</strong> 

<strong>in</strong>version may have begun <strong>in</strong> <strong>Mess<strong>in</strong>ian</strong> time when 

subsidence rates slowed and <strong>the</strong>n evolved to uplift <strong>in</strong> <strong>the</strong> 

Pliocene. This <strong>in</strong>version corresponds to Horváth 

(1995)'s late stage compressional event. Some compressional 

tectonic features appear above <strong>the</strong> flysch 

ridge <strong>in</strong> <strong>the</strong> middle of <strong>the</strong> section suggest<strong>in</strong>g that this 

part of <strong>the</strong> bas<strong>in</strong> was also impacted by compression that 

occurred mostly <strong>in</strong> post-<strong>Mess<strong>in</strong>ian</strong> time. 

4.2. Section B 

Section B (Fig. 6) is almost parallel to Section A, but 

it crosses more basement features. From SW to NE, it 

beg<strong>in</strong>s on <strong>the</strong> Algyő High and passes across <strong>the</strong> Makó 

Trough, Battonya High and Békés Bas<strong>in</strong>. To <strong>the</strong> NE, it 

reaches <strong>the</strong> Derecske Trough and <strong>the</strong>n <strong>the</strong> basement 

rises fur<strong>the</strong>r to <strong>the</strong> nor<strong>the</strong>ast. <strong>The</strong> basement rocks 

<strong>in</strong>clude crystall<strong>in</strong>e metamorphic rocks of Paleozoic/ 

Precambrian age, Mesozoic sedimentary rocks of <strong>the</strong> 

Villány Unit and metamorphic and Triassic sedimentary 

rocks of <strong>the</strong> Békés Unit (Haas and Péró, 2004). <strong>The</strong> 

IMU clearly represents a bas<strong>in</strong>-wide erosional event that 

stopped <strong>the</strong> advancement of <strong>the</strong> Tortonian–Lower 

<strong>Mess<strong>in</strong>ian</strong> delta system from <strong>the</strong> nor<strong>the</strong>ast, which had 

built a 2000–3000 m thick second-order highstand 

systems tract (see paleo-marg<strong>in</strong> marked Hajdúság-type 

Architecture <strong>in</strong> Fig. 6, and for more detailed explanation 

see Section 4.5 and Fig. 9). This section shows that a 

sou<strong>the</strong>rn delta system may be located fur<strong>the</strong>r south of 

<strong>the</strong> section although <strong>the</strong> rates of sediment supply to this 

system were not as great as from <strong>the</strong> nor<strong>the</strong>rn source. 

<strong>The</strong> Late <strong>Mess<strong>in</strong>ian</strong>–Pliocene–Quaternary bas<strong>in</strong> fill is a 

second-order retrogradational cycle that <strong>in</strong>cludes thick 

lowstand sediments <strong>in</strong> <strong>the</strong> bas<strong>in</strong> center and sharp onlap 

configurations onto <strong>the</strong> IMU surface. This section also 

provides evidence of tectonic <strong>in</strong>version, primarily at <strong>the</strong>


Fig. 9. A. Map of Lake Pannon at <strong>Mess<strong>in</strong>ian</strong> time. Four types of architectural patterns have been def<strong>in</strong>ed <strong>in</strong> this study for <strong>the</strong> stratigraphy of <strong>the</strong> 

<strong>Mess<strong>in</strong>ian</strong> coasts that are named by us<strong>in</strong>g <strong>geo</strong>graphical names. B. <strong>The</strong> four coastal architectural patterns at <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> lake. Hajdúság-type: large 

aggradational-progradational delta <strong>in</strong> <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong>; a shallow progradational unit below IMU; IMU is a type I unconformity with a 

large lowstand systems tract (LST). Jászság-type: large progradational delta <strong>in</strong> <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong>; IMU is a type II unconformity with a 

shelf marg<strong>in</strong> systems tract (SMST). Kiskunság-type: large aggradational–progradational delta <strong>in</strong> <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong>; IMU is a type I 

unconformity with a large lowstand systems tract. 

nor<strong>the</strong>astern marg<strong>in</strong> and most likely also at <strong>the</strong> Algyő 

High. Apparent syn-depositional compressional features 

<strong>in</strong> <strong>the</strong> Derecske Trough show evidence of local activity 

<strong>in</strong> Tortonian time. 

4.3. Section C 

Section C (Fig. 7) is perpendicular to Sections A and 

B. It reaches <strong>the</strong> Bükk Unit and crosses <strong>the</strong> Mid- 

Hungarian L<strong>in</strong>e, <strong>in</strong>tersects <strong>the</strong> Szolnok and Villány units 

and crosses <strong>the</strong> Békés Unit to <strong>the</strong> SE. A large delta 

system that prograded from <strong>the</strong> northwest is represented 

<strong>in</strong> <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong> section, while at that 

time, <strong>the</strong>re was m<strong>in</strong>imal sediment supply from <strong>the</strong> 

sou<strong>the</strong>ast. <strong>The</strong> IMU onlaps <strong>the</strong> pre-Neogene basement 

of <strong>the</strong> Battonya High, which means that this basement 

structure was emergent <strong>in</strong> <strong>the</strong> Tortonian, <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> 

and <strong>in</strong> <strong>the</strong> lower part of <strong>the</strong> Pliocene (see paleo-marg<strong>in</strong>s 

marked Kiskunság-type and Battonya-type Architecture 

<strong>in</strong> Fig. 7, and for more detailed explanation see Section 

4.5 and Fig. 9). Most of <strong>the</strong> post-IMU lowstand deposits 

were derived from <strong>the</strong> northwest and formed large 

lowstand progradational wedges. <strong>The</strong> Battonya High 

became submergent later <strong>in</strong> <strong>the</strong> Pliocene and shallow 

water deltas started to advance bas<strong>in</strong>ward on <strong>the</strong> top of 

this high. <strong>The</strong> strong tilt<strong>in</strong>g and tectonic <strong>in</strong>version of <strong>the</strong>


123 

Fig. 10. A. A sea/lake-level chart applied <strong>in</strong> our simulations. B. Input subsidence histories at locations A and B, Section A (Fig. 11). C. Input shale 

supply histories at <strong>the</strong> two ends of Section A (Fig. 11). 

northwest <strong>in</strong> Section C may have started <strong>in</strong> Late 

<strong>Mess<strong>in</strong>ian</strong> and apparently cont<strong>in</strong>ued to <strong>the</strong> Quaternary. 

<strong>The</strong> considerable uplift and tilt<strong>in</strong>g <strong>in</strong> <strong>the</strong> northwest was 

probably responsible for <strong>the</strong> predom<strong>in</strong>antly northwestern 

orig<strong>in</strong> of <strong>the</strong> post-IMU deposits <strong>in</strong> this section. 

4.4. Section D 

A detailed sequence stratigraphic <strong>in</strong>terpretation was 

made on a shorter composite seismic profile (Section D 

<strong>in</strong> Fig. 8). This l<strong>in</strong>e has a key position <strong>in</strong> that it provides 

<strong>geo</strong>metrical, facies and time relationships at <strong>the</strong> nor<strong>the</strong>rn 

end of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> lake where it connects different 

stratal architectures on both sides of <strong>the</strong> lake. 

<strong>The</strong> Neogene bas<strong>in</strong> is underla<strong>in</strong> by Upper Cretaceous–Paleogene 

flysch and Lower Cretaceous formations 

(Fülöp et al., 1987) and <strong>the</strong> synrift mar<strong>in</strong>e 

sediments are Middle Miocene <strong>in</strong> age (Hámor, 1983, 

1985). <strong>The</strong> dom<strong>in</strong>ant nor<strong>the</strong>astern and northwestern 

delta systems of <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong>


Fig. 11. Simulation outputs of Section A at 12 Ma (end of synrift phase), 5.5 Ma (prior to <strong>the</strong> IMU lake-level fall) and <strong>the</strong> present. 

accumulated a great thickness of sediment (2–2.5 km) 

<strong>in</strong>dicat<strong>in</strong>g an abundant sediment supply from <strong>the</strong> 

uplift<strong>in</strong>g Carpathian mounta<strong>in</strong> cha<strong>in</strong> and also rapid 

subsidence that created accommodation for <strong>the</strong> deltaic 

sediments to accumulate. Simple distance and time 

calculations give a relatively fast rate of advancement of 

<strong>the</strong> deltas (50–70 km/Ma), which is <strong>in</strong> agreement with 

<strong>the</strong>ir strongly progradational character (Tortonian– 

Lower <strong>Mess<strong>in</strong>ian</strong> delta advanc<strong>in</strong>g from <strong>the</strong> NW of <strong>the</strong> 

section of Fig. 8). 

<strong>The</strong> IMU is a prom<strong>in</strong>ent surface, especially at <strong>the</strong> 

nor<strong>the</strong>astern marg<strong>in</strong> of <strong>the</strong> lake where large fall<strong>in</strong>g stage 

and lowstand systems tracts (Catuneanu, 2002, 2006) 

formed and onlapped <strong>the</strong> slope of <strong>the</strong> IMU, thus 

suggest<strong>in</strong>g a considerable relative fall of lake-level (see 

<strong>the</strong> sharp surface of <strong>the</strong> Intra-<strong>Mess<strong>in</strong>ian</strong> Unconformity 

at <strong>the</strong> NE side of <strong>the</strong> section of Fig. 8) <strong>The</strong>se fall<strong>in</strong>g 

stage/lowstand systems tracts may constitute a major 

potential hydrocarbon exploration play that <strong>in</strong>cludes 

bas<strong>in</strong> floor fans, slope fans and lowstand prograd<strong>in</strong>g 

wedge sediments (bs, pw symbols <strong>in</strong> Fig. 8). <strong>The</strong> 

northwestern delta system was more progradational and 

less aggradational before <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> event (see <strong>the</strong> 

mostly progradational character of <strong>the</strong> Tortonian–Lower 

<strong>Mess<strong>in</strong>ian</strong> delta at <strong>the</strong> NW). <strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> relative 

lake-level fall did not give rise to significant accumulation 

of lowstand sediments, <strong>in</strong>stead mostly shelf 

marg<strong>in</strong> systems tract formed (SMST <strong>in</strong> Fig. 8) on <strong>the</strong>


125 

Fig. 12. A. Input subsidence histories at locations A, B, C, and D of Section D (Fig. 13). B. Input shale supply histories at <strong>the</strong> two ends of Section D 

(Fig. 13). 

northwest marg<strong>in</strong> of <strong>the</strong> lake, which suggests that <strong>the</strong> 

relative lake-level fall was not as severe <strong>in</strong> <strong>the</strong> northwest 

as <strong>in</strong> <strong>the</strong> nor<strong>the</strong>ast. 

On <strong>the</strong> nor<strong>the</strong>ast side, a shallow progradational unit 

formed directly below <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> unconformity. This 

unit <strong>in</strong>dicates a highstand systems tract that built on a 

surface marked by a downlapp<strong>in</strong>g configuration. <strong>The</strong> 

downlap surface may be a correlative surface of an 

unconformity formed by a lake-level fall or it may 

<strong>in</strong>dicate a transgressive episode as well. This <strong>problem</strong> is 

addressed <strong>in</strong> <strong>the</strong> next section of <strong>the</strong> paper. 

<strong>The</strong> pre-<strong>Mess<strong>in</strong>ian</strong> deltaic advancement was <strong>in</strong>terrupted 

by <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> event on both sides of <strong>the</strong> lake, 

but <strong>the</strong> result<strong>in</strong>g architectural patterns are different. <strong>The</strong> 

<strong>Mess<strong>in</strong>ian</strong> unconformity <strong>in</strong> <strong>the</strong> northwest resembles a 

type II unconformity (Posamentier and Vail, 1988; Vail et 

al., 1991) with little resedimentation (shelf marg<strong>in</strong> 

systems tract, SMST <strong>in</strong> Fig. 8), while <strong>the</strong> same <strong>Mess<strong>in</strong>ian</strong> 

event produced widespread fall<strong>in</strong>g stage/lowstand deposits 

(type I unconformity sensu Posamentier and Vail, 

1988; Vail et al., 1991) on <strong>the</strong> nor<strong>the</strong>astern side (bs, pw 

symbols <strong>in</strong> Fig. 8). <strong>The</strong> post-<strong>Mess<strong>in</strong>ian</strong> architecture is also 

different on opposite sides of <strong>the</strong> lake. Little sediment 

accumulation occurred <strong>in</strong> <strong>the</strong> nor<strong>the</strong>ast follow<strong>in</strong>g <strong>the</strong> 

<strong>Mess<strong>in</strong>ian</strong> event, evidenced by <strong>the</strong> fact that <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> 

unconformity lies at shallow depth <strong>in</strong> that area (∼ 0.2 s 

TWT), whereas it is at ∼ 1.2–1.5 s TWT depth on <strong>the</strong> 

northwestern side. Most of <strong>the</strong> Late <strong>Mess<strong>in</strong>ian</strong>–Pliocene 

section onlaps aga<strong>in</strong>st <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> unconformity on <strong>the</strong> 

nor<strong>the</strong>astern side of <strong>the</strong> lake form<strong>in</strong>g a major secondorder 

lowstand systems tract (bs, pw symbols <strong>in</strong> Fig. 8). 

<strong>The</strong> same Late <strong>Mess<strong>in</strong>ian</strong>–Pliocene unit partly onlaps <strong>the</strong> 

<strong>Mess<strong>in</strong>ian</strong> unconformity <strong>in</strong> <strong>the</strong> northwest, but most of it is 

deposited on top of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> surface. <strong>The</strong>refore, <strong>the</strong> 

Late <strong>Mess<strong>in</strong>ian</strong>–Pliocene forms a complete sequence (<strong>in</strong> a 

shallow water sett<strong>in</strong>g) represented by a lowstand systems 

tract to a highstand systems tract (SMST, LST, TST, HST 

symbols at <strong>the</strong> NW side of <strong>the</strong> section <strong>in</strong> Fig. 8) on<strong>the</strong> 

northwestern side of <strong>the</strong> lacustr<strong>in</strong>e bas<strong>in</strong>. In contrast, it 

rema<strong>in</strong>s a lowstand and partially transgressive systems 

tract to <strong>the</strong> nor<strong>the</strong>ast (bs, pw, TST symbols at <strong>the</strong> NE side 

of <strong>the</strong> section <strong>in</strong> Fig. 8). 

In Fig. 8, <strong>the</strong> top of <strong>the</strong> lowstand prograd<strong>in</strong>g wedge, 

i.e. top of <strong>the</strong> lowstand systems tracts and <strong>the</strong> top of <strong>the</strong> 

transgressive systems tracts are <strong>in</strong>dicated by dashed 

l<strong>in</strong>es at <strong>the</strong> NW and NE sides of <strong>the</strong> bas<strong>in</strong>. <strong>The</strong> seismic


section clearly shows that <strong>the</strong> top surfaces of ei<strong>the</strong>r of 

<strong>the</strong>se systems tracts lie at different stratigraphic 

horizons, <strong>the</strong>y cannot be connected from <strong>the</strong> NW to 

<strong>the</strong> NE marg<strong>in</strong> of <strong>the</strong> bas<strong>in</strong>. In o<strong>the</strong>r words, apparently, 

<strong>the</strong> lowstand systems tract at <strong>the</strong> NE marg<strong>in</strong> (bs, pw 

symbols <strong>in</strong> Fig. 8) is correlative to <strong>the</strong> shelf marg<strong>in</strong> 

systems tract at <strong>the</strong> NW marg<strong>in</strong> (SMST <strong>in</strong> Fig. 8); <strong>the</strong> 

transgressive systems tract <strong>in</strong> <strong>the</strong> NW (see <strong>the</strong> dashed 

l<strong>in</strong>e of <strong>the</strong> top of <strong>the</strong> transgressive systems tract and <strong>the</strong> 

TST symbol <strong>in</strong> Fig. 8) is correlative partly with <strong>the</strong> 

lowstand systems tract <strong>in</strong> <strong>the</strong> NE; and <strong>the</strong> transgressive 

systems tract <strong>in</strong> <strong>the</strong> NE (TST) is partly correlative to <strong>the</strong> 

highstand systems tract at <strong>the</strong> NW marg<strong>in</strong> (HST symbol 

<strong>in</strong> Fig. 8). Section D provides an example of how 

different systems tracts (such as lowstand vs. highstand 

or shelf marg<strong>in</strong> systems tract and transgressive vs. 

highstand systems tract) have been formed coevally and 

are correlative along <strong>the</strong> paleo-marg<strong>in</strong> of Lake Pannon 

due to spatially variable subsidence/uplift rates. <strong>The</strong> 

two different types of paleo-marg<strong>in</strong>s are marked 

Jászság-type and Hajdúság-type Architecture <strong>in</strong> Fig. 8 

(see next section and Fig. 9 for summary of architecture 

types). 

4.5. Identification of stratal architectural patterns 

Four stratal architectural patterns formed on <strong>the</strong> paleo- 

<strong>Mess<strong>in</strong>ian</strong> lake marg<strong>in</strong>s have been identified <strong>in</strong> this study 

and named us<strong>in</strong>g local <strong>geo</strong>graphical names (see Fig. 3 for 

<strong>geo</strong>graphical regions). (1) Hajdúság-type architecture, 

identified at <strong>the</strong> nor<strong>the</strong>astern end of Section A (Fig. 5)and 

<strong>the</strong> nor<strong>the</strong>astern end of Section D (Fig. 7), is a highly 

progradational–aggradational delta system <strong>in</strong> <strong>the</strong> Tortonian–Lower 

<strong>Mess<strong>in</strong>ian</strong>. Prior to <strong>the</strong> IMU, a shallow progradational 

unit developed on <strong>the</strong> topset of <strong>the</strong> Tortonian 

delta. A large, thick lowstand systems tract formed over 

<strong>the</strong> IMU surface. (2) Jászság-type architecture, identified 

at <strong>the</strong> northwestern end of Section D (Fig. 7), <strong>in</strong>cludes a 

primarily progradational delta system before <strong>the</strong> IMU and 

a shelf marg<strong>in</strong>-type systems tract follow<strong>in</strong>g <strong>the</strong> IMU. (3) 

Kiskunság-type pattern, identified at <strong>the</strong> southwestern end 

of Section A (Fig. 5), is similar to <strong>the</strong> Hajdúság 

architecture except that no shallow progradational unit 

formed prior to <strong>the</strong> IMU. (4) Battonya-type pattern, 

identified at <strong>the</strong> sou<strong>the</strong>astern end of Section C (Fig. 6), has 

a p<strong>in</strong>chout configuration <strong>in</strong>dicat<strong>in</strong>g that no delta system 

developed <strong>in</strong> <strong>the</strong> sou<strong>the</strong>astern corner of <strong>the</strong> study area <strong>in</strong> 

Tortonian–<strong>Mess<strong>in</strong>ian</strong> times. A summary of <strong>the</strong>se stratal 

stack<strong>in</strong>g patterns is shown <strong>in</strong> Fig. 9. <strong>The</strong> simulation 

experiment <strong>in</strong> <strong>the</strong> next section quantitatively analyzes <strong>the</strong> 

relative role of subsidence/uplift, lake-level changes and 

sediment supply <strong>in</strong> <strong>the</strong> formation of <strong>the</strong>se four types of 

architectural patterns associated with <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> 

events. 

5. Sequence stratigraphic simulations 

5.1. Simulation parameters 

5.1.1. Paleobathymetry 

<strong>The</strong> simulation started between 20 and 17 Ma with 

rift<strong>in</strong>g, formation of half-grabens and grabens. This time 

<strong>in</strong>terval corresponds to <strong>the</strong> onset of rift<strong>in</strong>g <strong>in</strong> most subbas<strong>in</strong>s 

<strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> system (Horváth, 1995; 

Hámor, 1997). <strong>The</strong> paleobathymetry prior to 12 Ma was 

compared to and calibrated with Báldi et al. (2002)'s data. 

Although <strong>the</strong>ir study area was <strong>in</strong> southwest Hungary, <strong>the</strong> 

paleo-water depth <strong>in</strong>formation for <strong>the</strong> mid-Miocene 

section could be extrapolated to <strong>the</strong> study area. Tectonic 

<strong>in</strong>version was applied <strong>in</strong> <strong>the</strong> program at 12 Ma <strong>in</strong> 

accordance with Horváth (1995)'s Sarmatian <strong>in</strong>version 

that affected most of <strong>the</strong> bas<strong>in</strong> and toge<strong>the</strong>r with a sea-level 

fall brought about shallow water conditions and sub-aerial 

emergence of former structural highs. Rapid subsidence 

started after 12 Ma and deep (around 1000 m) conditions 

developed shortly after this event. <strong>The</strong> bas<strong>in</strong> gradually 

became shallower after 5.5 Ma until it filled completely. 

5.1.2. Subsidence 

Four stages to <strong>the</strong> subsidence history can be 

dist<strong>in</strong>guished. In <strong>the</strong> first stage (up to 12 Ma), <strong>the</strong> 

subsidence was spatially variable and relatively fast 

locally, produc<strong>in</strong>g <strong>the</strong> rifts. Subsidence was <strong>in</strong>terrupted 

by a short uplift event at 12 Ma, which ended <strong>the</strong> rift 

phase. After this event, <strong>the</strong> subsidence pattern became 

spatially more uniform and very fast (0.54–0.39 m/Ka) 

across <strong>the</strong> bas<strong>in</strong>. This fast subsidence was term<strong>in</strong>ated by 

tectonic <strong>in</strong>version start<strong>in</strong>g at 5.5 Ma. <strong>The</strong> <strong>in</strong>version was 

not uniform; it was prom<strong>in</strong>ent <strong>in</strong> <strong>the</strong> Kiskunság area 

(southwest end of Section A) and <strong>in</strong> <strong>the</strong> Hajdúság area 

(nor<strong>the</strong>astern end of Sections A and D), but no uplift 

occurred <strong>in</strong> <strong>the</strong> Jászság Bas<strong>in</strong> (northwestern side of 

Section D). <strong>The</strong> subsidence pattern after this <strong>in</strong>version 

was not uniform but varied greatly. Renewed subsidence 

was applied <strong>in</strong> <strong>the</strong> Hajdúság area <strong>in</strong> Section D from 

3.2 Ma, no subsidence occurred <strong>in</strong> <strong>the</strong> Kiskunság area 

and cont<strong>in</strong>uous subsidence was used <strong>in</strong> <strong>the</strong> simulation <strong>in</strong> 

<strong>the</strong> central bas<strong>in</strong> and <strong>in</strong> <strong>the</strong> Jászság. 

5.1.3. Sea-level 

No sea/lake-level curve has been constructed specifically 

for <strong>the</strong> late Miocene–Pliocene <strong>Pannonian</strong> Bas<strong>in</strong>. 

Global charts, such as <strong>the</strong> Haq et al. (1987) curve and 

stable isotope curves measured at ocean drill<strong>in</strong>g


127 

Fig. 13. Simulation outputs of Section D at 12 Ma (end of synrift phase), 5.8 Ma (prior to <strong>the</strong> IMU lake-level fall), 4 Ma and <strong>the</strong> present. SMST: shelf 

marg<strong>in</strong> systems tract; LST: lowstand systems tract.


Fig. 14. A. Model of sedimentary fill for <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong>, eastern Hungary. Two ma<strong>in</strong> sediment supply systems developed that are named <strong>in</strong> 

this study by us<strong>in</strong>g <strong>geo</strong>graphical names: Hajdúság system (H) transported sediments from <strong>the</strong> nor<strong>the</strong>ast and Jászság–Kiskunság system (Já, K) from <strong>the</strong> 

northwest–west. A third system may have existed <strong>in</strong> <strong>the</strong> south. B. Model of sedimentary fill <strong>in</strong> <strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong>–Pliocene. <strong>The</strong> sizes of <strong>the</strong> arrows <strong>in</strong>dicate 

<strong>the</strong> relative abundance of sediment supply from different directions: <strong>the</strong> largest <strong>in</strong>flux was <strong>the</strong> Jászság system and <strong>the</strong> least amount of sediment was 

transported by <strong>the</strong> Hajdúság system after <strong>the</strong> IMU event. <strong>The</strong> edges of <strong>the</strong> bas<strong>in</strong> to <strong>the</strong> nor<strong>the</strong>ast, northwest and west, except for <strong>the</strong> Jászság Bas<strong>in</strong>, were 

uplifted by tectonic <strong>in</strong>version. J: Jászság Bas<strong>in</strong>, BB: Békés Bas<strong>in</strong>, B: Battonya High, M: Makó Trough.


129 

program sites were utilized to f<strong>in</strong>d a match with 

observed unconformities (Vakarcs et al., 1994; Vakarcs, 

1997). <strong>The</strong> sea-level curve used <strong>in</strong> our simulations was 

constructed to <strong>in</strong>clude published sea/lake-level changes, 

and modified where appropriate to f<strong>in</strong>d a match with <strong>the</strong> 

observed stratigraphy. <strong>The</strong> sizes of <strong>the</strong> sea/lake-level 

falls and rises were calibrated from clear matches 

between <strong>the</strong> simulated stratigraphy and <strong>the</strong> sections. 

<strong>The</strong> sea-level history prior to 12 Ma <strong>in</strong> our model 

followed <strong>the</strong> stable oxygen isotope curve of Vakarcs et 

al. (1998) that had an overall lower<strong>in</strong>g trend with falls at 

around 17, 15, 14 and 13 Ma. <strong>The</strong> <strong>Pannonian</strong> Bas<strong>in</strong> was 

connected to <strong>the</strong> sea dur<strong>in</strong>g this period, thus <strong>the</strong> eustatic 

variations must have impacted its base-level and it is 

considered reasonable to use a global curve. <strong>The</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong> became a shallow water sett<strong>in</strong>g at 

12 Ma due to uplift and fur<strong>the</strong>r sea-level lower<strong>in</strong>g. 

Climatic cool<strong>in</strong>g was detected by Jiménez-Moreno et al. 

(2005) from palynological analysis <strong>in</strong> Hungary for <strong>the</strong> 

late Badenian–Sarmatian period (from 14 Ma), which is 

<strong>in</strong> agreement with a eustatic sea-level fall evidenced by 

worldwide <strong>in</strong>crease <strong>in</strong> δ 18 O values. Follow<strong>in</strong>g this 

event, <strong>the</strong> bas<strong>in</strong> was isolated from <strong>the</strong> world oceans, thus 

<strong>the</strong> lake-level history did not necessarily follow global 

charts. <strong>The</strong> ages of Vakarcs (1997)'s unconformities 

were applied <strong>in</strong> our simulation, <strong>in</strong>clud<strong>in</strong>g 10.8 and 

9.15 Ma lake-level falls. <strong>The</strong> next lake-level fall, which 

occurred <strong>in</strong> our model at 5.5 Ma produced <strong>the</strong> great 

<strong>Mess<strong>in</strong>ian</strong> unconformity. After <strong>the</strong> IMU event, Vakarcs 

(1997)'s ages were used aga<strong>in</strong>, specifically lake-level 

falls at 4.4, 4.0 and 3.2 Ma. 

5.1.4. Sediment supply 

<strong>The</strong> simulation program <strong>in</strong> general deposits alternat<strong>in</strong>g 

mud and sand layers, and <strong>the</strong> depositional angles 

and depositional distance can be def<strong>in</strong>ed by <strong>the</strong> user. 

<strong>The</strong> amount of sediment is represented <strong>in</strong> <strong>the</strong> program 

by <strong>the</strong> area of sediments deposited <strong>in</strong> <strong>the</strong> section. In this 

study, a relatively low rate of sediment supply 

characterized <strong>the</strong> rift phase of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, 

but <strong>the</strong>n supply <strong>in</strong>creased substantially to form <strong>the</strong> 

prograd<strong>in</strong>g–aggrad<strong>in</strong>g deltas after 12 Ma that gradually 

filled <strong>the</strong> bas<strong>in</strong>. <strong>The</strong> deltaic deposition <strong>in</strong>to a deep bas<strong>in</strong> 

ceased around 5.5 Ma and <strong>the</strong> sediment supply was cut. 

<strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> sea-level fall triggered erosion and 

resedimentation that fur<strong>the</strong>r <strong>in</strong>creased <strong>the</strong> sediment 

supply, eventually fill<strong>in</strong>g <strong>the</strong> shallow bas<strong>in</strong>. 

5.2. Simulation on Section A 

Section A is located <strong>in</strong> <strong>the</strong> Tisza Unit (Figs. 2 and 3)of 

<strong>the</strong> pre-Neogene basement. Flysch forms a ridge <strong>in</strong> <strong>the</strong> 

center of <strong>the</strong> section that is bounded by deep half-grabens. 

<strong>The</strong> basement rises both to <strong>the</strong> nor<strong>the</strong>ast and southwest, 

thus <strong>the</strong> section transects three ma<strong>in</strong> structural doma<strong>in</strong>s 

with<strong>in</strong> <strong>the</strong> Tisza Unit. Fig. 10 summarizes <strong>the</strong> simulation 

<strong>in</strong>put parameters, <strong>in</strong>clud<strong>in</strong>g <strong>the</strong> sea-level curve, subsidence 

rates at selected locations and sediment supply rates 

from both sides of <strong>the</strong> section. Fig. 11 shows <strong>the</strong> 

simulation output at 12 Ma (end of syn-rift phase), 

5.5 Ma (prior to IMU) and at <strong>the</strong> present. 

<strong>The</strong> subsidence curves reveal that <strong>the</strong> three structural 

doma<strong>in</strong>s had different subsidence histories. <strong>The</strong> central 

flysch ridge experienced relatively cont<strong>in</strong>uous and slow 

subsidence throughout its history, while <strong>the</strong> Kiskunság and 

Hajdúság doma<strong>in</strong>s were strongly <strong>in</strong>verted after 5.5 and 

particularly 3.2 Ma (see Locations A and B <strong>in</strong> Fig. 10B). 

<strong>The</strong> rates of sediment supply <strong>in</strong>creased enormously 

between 12 and 5.5 Ma, while deposition was able to 

keep pace with <strong>the</strong> rapid subsidence rates and produce 

progradational delta systems <strong>in</strong> a deep bas<strong>in</strong> sett<strong>in</strong>g. Both 

<strong>the</strong> rates of sedimentation and subsidence were lowered 

and <strong>the</strong> lake-level dropped at 5.5 Ma when <strong>the</strong> IMU 

formed. Note that a shallow progradational unit formed on 

<strong>the</strong> topset of <strong>the</strong> Tortonian delta before <strong>the</strong> IMU event. Our 

simulation solution was that follow<strong>in</strong>g a short lake-level 

fall that produced a modest lowstand systems tract, <strong>the</strong> 

lake-level was stabilized at highstand, but <strong>the</strong> sediment 

supply was cut and <strong>the</strong>n gradually <strong>in</strong>creased aga<strong>in</strong> while 

<strong>the</strong> lake-level was stable. This change <strong>in</strong> sediment supply 

caused a retreat of <strong>the</strong> delta and produced subsequently a 

progradational unit on <strong>the</strong> topset of <strong>the</strong> former delta. 

5.3. Simulation on Section D 

Section D l<strong>in</strong>ks <strong>the</strong> Jászság Bas<strong>in</strong> and <strong>the</strong> Hajdúság 

area, which are separated by <strong>the</strong> same flysch ridge unit 

shown <strong>in</strong> Section A. <strong>The</strong> <strong>in</strong>put values are summarized <strong>in</strong> 

Fig. 12 and <strong>the</strong> simulation output is presented <strong>in</strong> Fig. 13 

for 12, 5.8, 4 Ma and <strong>the</strong> present. 

<strong>The</strong> northwest sub-bas<strong>in</strong> (Jászság Bas<strong>in</strong>) subsided 

cont<strong>in</strong>uously until late <strong>Mess<strong>in</strong>ian</strong> time when <strong>the</strong> 

subsidence slowed and rema<strong>in</strong>ed constant (Location A 

<strong>in</strong> Fig. 12A). <strong>The</strong> subsidence accelerated from about 

10 Ma and <strong>the</strong> basement reached a depth of 3000 m by 

<strong>the</strong> present. <strong>The</strong> central flysch ridge <strong>in</strong> <strong>the</strong> section shows 

a similar pattern with slower subsidence rates at <strong>the</strong> 

beg<strong>in</strong>n<strong>in</strong>g (Location B <strong>in</strong> Fig. 12A). <strong>The</strong> trough east of 

<strong>the</strong> central ridge (Location C <strong>in</strong> Fig. 12A) underwent 

faster subsidence dur<strong>in</strong>g <strong>the</strong> synrift stage than <strong>in</strong> o<strong>the</strong>r 

parts of <strong>the</strong> section and <strong>the</strong> subsidence rate became even 

faster <strong>in</strong> <strong>the</strong> postrift time until <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> event. 

However, <strong>the</strong> subsidence slowed down considerably <strong>in</strong> 

<strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> and <strong>the</strong> resumed subsidence after 5.5 Ma


Fig. 15. A. Correlation of <strong>the</strong> third-order sequences of Vakarcs (1997), Sacchi and Müller (2004) and <strong>the</strong> two-fold division about <strong>the</strong> IMU of this 

study. B. Representative sections <strong>in</strong> southwestern Hungary (Sacchi et al., 1999; Sacchi and Müller, 2004) and eastern Hungary (this study) show<strong>in</strong>g 

<strong>the</strong> significance of <strong>the</strong> IMU surface <strong>in</strong> <strong>the</strong> late Miocene–Pliocene sedimentary fill of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> (<strong>the</strong> <strong>in</strong>terpreted sections are presented at 

different scales). 

never reached <strong>the</strong> former level characteristic of <strong>the</strong> bas<strong>in</strong> 

prior to <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>. At <strong>the</strong> nor<strong>the</strong>astern end of <strong>the</strong> 

section (Hajdúság realm), subsidence stopped completely, 

uplift took place and subsidence did not resume 

until about 2.6 Ma (Location D <strong>in</strong> Fig. 12A). <strong>The</strong> 

<strong>in</strong>version affected all sub-bas<strong>in</strong>s along <strong>the</strong> section 

<strong>in</strong>dicated by <strong>the</strong> slow<strong>in</strong>g down of subsidence rates 

everywhere, though only <strong>the</strong> nor<strong>the</strong>astern part of <strong>the</strong> 

section shows evidence of uplift <strong>in</strong> our simulation. 

5.4. Simulation of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> event 

To produce <strong>the</strong> observed <strong>Mess<strong>in</strong>ian</strong> unconformity <strong>in</strong> 

<strong>the</strong> simulations, a specific lake-level fall was applied.


131 

However, <strong>the</strong> lake-level fall alone was <strong>in</strong>sufficient to 

produce <strong>the</strong> architectural patterns observed on <strong>the</strong> 

seismic section. Add<strong>in</strong>g differential subsidence between 

segments of <strong>the</strong> simulated sections enabled <strong>the</strong> achievement 

of a match between <strong>the</strong> observations and <strong>the</strong> 

simulation output. In <strong>the</strong> case of Section D, without 

differential subsidence and <strong>in</strong>version <strong>in</strong> <strong>the</strong> Hajdúság 

segment, <strong>the</strong> simulation was not able to produce <strong>the</strong> 

shelf marg<strong>in</strong> systems tract <strong>in</strong> <strong>the</strong> northwest (Jászság) or 

<strong>the</strong> coeval, large lowstand systems tract <strong>in</strong> <strong>the</strong> nor<strong>the</strong>ast 

(Hajdúság). On <strong>the</strong> o<strong>the</strong>r hand, differential subsidence 

alone, without lake-level fall, could not produce <strong>the</strong> 

bas<strong>in</strong>-wide unconformity representative of this time. As 

a result, <strong>the</strong> stratigraphic simulation of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> 

unconformity and <strong>the</strong> related stratal architecture <strong>in</strong> <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong> were found to be <strong>the</strong> comb<strong>in</strong>ed 

product of a lake-level fall and tectonic <strong>in</strong>version. 

Accord<strong>in</strong>g to our simulation, <strong>the</strong> relative lake-level fall 

was around 200 m <strong>in</strong> <strong>the</strong> Hajdúság and Kiskunság 

systems and less than 100 m <strong>in</strong> <strong>the</strong> Jászság. <strong>The</strong> virtually 

cont<strong>in</strong>uous subsidence <strong>in</strong> <strong>the</strong> Jászság did not allow <strong>the</strong> 

formation of a significantly large lowstand systems 

tract. S<strong>in</strong>ce <strong>the</strong> <strong>in</strong>version <strong>in</strong> <strong>the</strong> Hajdúság system lasted 

about 3 million years and more <strong>in</strong> <strong>the</strong> Kiskunság, it 

facilitated <strong>the</strong> deposition of a considerable amount of 

resedimented material onto <strong>the</strong> bas<strong>in</strong> slopes <strong>in</strong> <strong>the</strong> form 

of large lowstand systems tracts <strong>in</strong> those areas. 

<strong>The</strong> simulation of a tectonic <strong>in</strong>version between about 

5.5–2.6 Ma or longer seems to be <strong>in</strong> agreement with 

Horváth and Cloet<strong>in</strong>gh (1996) who proposed <strong>in</strong>traplate 

stress changes <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. Sacchi et al. (1999) 

also correlated a relative lake-level fall at <strong>the</strong> Miocene– 

Pliocene boundary <strong>in</strong> western Hungary, and <strong>the</strong>ir 

explanation was that a regional tilt<strong>in</strong>g of <strong>the</strong> western 

<strong>Pannonian</strong> Bas<strong>in</strong> fill occurred at that time, mark<strong>in</strong>g a 

regional tectonic change. Fodor et al. (1999) reconstructed 

<strong>the</strong> Cenozoic stress field evolution <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> 

system and proposed that a compressional stress field had 

propagated through <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> from <strong>the</strong> latest 

Miocene onwards, which also seems to be <strong>in</strong> agreement 

with our simulation results. Bada et al. (2001)'s f<strong>in</strong>ite 

element models analyzed <strong>the</strong> possible causes of compression 

<strong>in</strong> extensional bas<strong>in</strong>s and po<strong>in</strong>ted out that topography-<strong>in</strong>duced 

gravitational forces from <strong>the</strong> surround<strong>in</strong>g 

mounta<strong>in</strong> belt may have contributed to <strong>the</strong> development of 

compressional deformation <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. 

Tomljenović and Csontos (2001) expla<strong>in</strong>ed <strong>the</strong> <strong>in</strong>versions 

by a northward and counterclockwise motion of <strong>the</strong> 

Adriatic plate that <strong>in</strong>duced transpressive deformation <strong>in</strong> 

<strong>the</strong> <strong>in</strong>terior of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. 

<strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> event <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> shows 

that variations <strong>in</strong> tectonic subsidence/uplift along a 

bas<strong>in</strong>'s marg<strong>in</strong> may overpr<strong>in</strong>t <strong>the</strong> effect of water-level 

changes and can lead to simultaneous formation of 

various architectural patterns. O<strong>the</strong>r authors also 

reported similar observations <strong>in</strong> o<strong>the</strong>r bas<strong>in</strong>s, for 

example, Gawthorpe et al. (1994) observed coeval 

type I and type II unconformities <strong>in</strong> half-grabens. 

6. Results of seismic <strong>in</strong>terpretations and 

stratigraphic simulations: stratigraphic model 

6.1. Model of bas<strong>in</strong> fill 

Lake Pannon had formed a large bay <strong>in</strong> <strong>the</strong> territory 

of Hungary by <strong>Mess<strong>in</strong>ian</strong> time (Fig. 14) as it gradually 

filled with sediment. Two large deltaic systems formed 

<strong>in</strong> <strong>the</strong> Tortonian, one advanc<strong>in</strong>g from <strong>the</strong> nor<strong>the</strong>ast and 

ano<strong>the</strong>r from <strong>the</strong> northwest and west. We use <strong>the</strong> same 

<strong>geo</strong>graphical names <strong>in</strong> this study to designate <strong>the</strong>se 

sediment sources as have been used to name architectural 

patterns. <strong>The</strong> nor<strong>the</strong>astern system is called 

Hajdúság and <strong>the</strong> architectural pattern formed <strong>in</strong> this 

system is <strong>the</strong> Hajdúság-type architecture. <strong>The</strong> northwest-western 

delta system is called Jászság–Kiskunság 

system <strong>in</strong> this paper. <strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> event generated a 

major reorganization of sediment supply patterns: <strong>the</strong> 

Hajdúság source became significantly r<strong>edu</strong>ced and <strong>the</strong> 

bulk of <strong>the</strong> sediments were transported by <strong>the</strong> Jászság 

and partly Kiskunság sources (Fig. 14B) to <strong>the</strong> lake. <strong>The</strong> 

Jászság and Kiskunság supply systems appear dist<strong>in</strong>ct 

follow<strong>in</strong>g <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> event. 

From <strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> onward, <strong>the</strong> bas<strong>in</strong> marg<strong>in</strong>s 

were exposed to tectonic <strong>in</strong>version <strong>in</strong> <strong>the</strong> Hajdúság area, 

<strong>the</strong> north of <strong>the</strong> Jászság and <strong>in</strong> <strong>the</strong> Kiskunság. <strong>The</strong> uplift 

most likely cont<strong>in</strong>ued to <strong>the</strong> Quaternary north of <strong>the</strong> 

Jászság and at <strong>the</strong> Kiskunság area. <strong>The</strong> Jászság Bas<strong>in</strong> 

and o<strong>the</strong>r deep portions of <strong>the</strong> lake subsided cont<strong>in</strong>uously, 

thus a ra<strong>the</strong>r vary<strong>in</strong>g subsidence/uplift pattern 

developed <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> follow<strong>in</strong>g <strong>the</strong> 

<strong>Mess<strong>in</strong>ian</strong>. Not only <strong>the</strong> pre-Neogene basement units 

but also portions of <strong>the</strong>se units experienced substantially 

different subsidence histories. Some grabens, such as 

<strong>the</strong> Makó Trough, Békés Bas<strong>in</strong> or Jászság Bas<strong>in</strong> 

subsided to depths of several km, while ridges between 

<strong>the</strong>se grabens subsided relatively slowly follow<strong>in</strong>g <strong>the</strong> 

Sarmatian compression of Horváth (1995). More data 

cover<strong>in</strong>g <strong>the</strong> region surround<strong>in</strong>g <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> 

would be necessary to identify <strong>the</strong> <strong>geo</strong>graphical areas of 

<strong>in</strong>version more accurately. 

Fig. 9 summarizes <strong>the</strong> vary<strong>in</strong>g architectural patterns 

along <strong>the</strong> marg<strong>in</strong> of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> lake. <strong>The</strong> Hajdúságtype 

architecture was produced by rapid subsidence 

dur<strong>in</strong>g <strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong>, a large lake-

Fig. 16. Seismic section and well logs (see Fig. 3 for location) show <strong>the</strong> locations of samples where Galeacysta etrusca was discovered (Sütő-Szentai, 2006) at <strong>the</strong> IMU surface. Ge: Galeacysta etrusca 

occurrences with depth <strong>in</strong> m. Mi: Middle Miocene synrift unit. 



133 

Fig. 17. Correlation of <strong>the</strong> IMU of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> with occurrences of Galeacysta etrusca <strong>in</strong> <strong>the</strong> Apenn<strong>in</strong>e, Umbro-Marche (Bert<strong>in</strong>i, 2006) and 

Dacic Bas<strong>in</strong>s (Clauzon et al., 2005). S<strong>in</strong>ce Galeacysta etrusca was found <strong>in</strong> <strong>the</strong> IMU and not above <strong>the</strong> IMU <strong>in</strong> this study (Fig. 16) (Sütő-Szentai, 

2006), its age is likely late <strong>Mess<strong>in</strong>ian</strong>, however ages of stratigraphic horizons are uncerta<strong>in</strong> <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> because of lack of accurate age 

data. 

level fall <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> and coeval cessation of bas<strong>in</strong> 

subsidence and subsequent renewed but slow subsidence 

<strong>in</strong> <strong>the</strong> late Pliocene. Prior to <strong>the</strong> IMU event, a 

shallow progradational unit formed on <strong>the</strong> topset of <strong>the</strong> 

Tortonian delta system, which was produced by a 

sudden decrease and subsequent <strong>in</strong>crease <strong>in</strong> sediment 

supply accord<strong>in</strong>g to our model<strong>in</strong>g results. <strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> 

lake-level fall coupled with <strong>the</strong> tectonic <strong>in</strong>version 

made <strong>the</strong> IMU a type I unconformity <strong>in</strong> this architecture 

where a considerable mass of lowstand systems tract 

sediment was accumulated. 

<strong>The</strong> Jászság-type architecture has two ma<strong>in</strong> components, 

a predom<strong>in</strong>antly progradational delta system <strong>in</strong> 

<strong>the</strong> Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong> and a shelf marg<strong>in</strong> 

systems tract complex above <strong>the</strong> IMU, thus <strong>the</strong> IMU is a 

type II unconformity <strong>in</strong> this architecture. A high rate of 

sediment supply was responsible for <strong>the</strong> primarily 

progradational character of <strong>the</strong> Tortonian pattern. 

Cont<strong>in</strong>uous subsidence without a major <strong>in</strong>terruption <strong>in</strong> 

<strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> caused accumulation of shelf marg<strong>in</strong> 

systems tracts <strong>in</strong>stead of a lowstand systems tract 

follow<strong>in</strong>g <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> lake-level fall. 

<strong>The</strong> IMU has <strong>the</strong> character of a type I unconformity 

aga<strong>in</strong> <strong>in</strong> <strong>the</strong> Kiskunság-type architecture because of 

large-scale uplift <strong>in</strong> this region that accentuated <strong>the</strong> 

impact of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> lake-level fall. Large lowstand 

systems tract deposits accumulated on <strong>the</strong> IMU surface, 

onlapp<strong>in</strong>g its slope. No shallow progradational unit 

formed below <strong>the</strong> IMU <strong>in</strong> this pattern, which is unique 

to <strong>the</strong> Hajdúság-type architecture. 

<strong>The</strong> Battonya-type architecture lacks any major delta 

system <strong>geo</strong>metry as this island must have been far from 

sediment sources and it was not large enough to become 

a major sediment source. <strong>The</strong> IMU p<strong>in</strong>ches out onto <strong>the</strong> 

basement high. <strong>The</strong> island subsided <strong>in</strong> <strong>the</strong> late Pliocene 

and may have been uplifted <strong>in</strong> <strong>the</strong> Quaternary. 

6.2. Stratigraphic stages 

Two detailed regional correlations of <strong>the</strong> Late 

Miocene–Pliocene strata have been constructed from 

seismic data, one by Vakarcs (1997) <strong>in</strong> eastern, 

northwestern and southwestern Hungary and ano<strong>the</strong>r 

by Sacchi et al. (1999) and Sacchi and Müller (2004) <strong>in</strong> 

western and southwestern Hungary. <strong>The</strong> two sets of 

sequences identified by <strong>the</strong>se authors are presented and 

matched to each o<strong>the</strong>r <strong>in</strong> Fig. 15. <strong>The</strong> IMU surface was 

clearly recognized by <strong>the</strong>se authors and was named Pa-4 

<strong>in</strong> Vakarcs (1997) and Pan-4 <strong>in</strong> Sacchi and Müller 

(2004); however <strong>the</strong> estimated age of <strong>the</strong> same physical 

surface shows a discrepancy between <strong>the</strong>se studies. This 

difference <strong>in</strong> age estimation, although it appears 

substantial, is understandable consider<strong>in</strong>g <strong>the</strong> <strong>in</strong>accuracy 

of seismic correlation of paleomagnetic ages (Juhász 

et al., 2006). Both studies identified four sequences 

with<strong>in</strong> our Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong> unit. <strong>The</strong> age 

differences may arise, <strong>in</strong> addition to <strong>the</strong> <strong>in</strong>accuracy of 

<strong>the</strong> possible age determ<strong>in</strong>ation method, from <strong>the</strong> fact 

that a third- or higher order maximum flood<strong>in</strong>g surface 

or unconformity <strong>in</strong> western Hungary may become a 

conformable surface <strong>in</strong> eastern Hungary and vice versa 

because of <strong>the</strong> different subsidence and sediment supply 

histories (Csato and Kendall, 2002), thus correlation of 

<strong>the</strong>se surfaces across <strong>the</strong> country may be difficult to 

carry out. 

Our proposal <strong>in</strong> this study is to use <strong>the</strong> IMU surface 

as a basis for a bas<strong>in</strong>-wide subdivision of <strong>the</strong> succession 

<strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. <strong>The</strong> rationale beh<strong>in</strong>d this


proposal is that <strong>the</strong> IMU is recognizable and correlatable 

everywhere where it formed and it represents <strong>the</strong> s<strong>in</strong>gle 

most dramatic event <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> that 

completely changed <strong>the</strong> character of <strong>the</strong> sedimentation. 

<strong>The</strong> conditions changed abruptly from a deep-water, 

rapidly subsid<strong>in</strong>g bas<strong>in</strong> with <strong>in</strong>tense deltaic deposition 

to a shallow<strong>in</strong>g, retrogradational system with extensive 

resedimentation follow<strong>in</strong>g IMU erosion. For nam<strong>in</strong>g <strong>the</strong> 

two stages separated by IMU, we prefer to us<strong>in</strong>g <strong>the</strong> 

global stage names (Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong> and 

Late <strong>Mess<strong>in</strong>ian</strong>–Pliocene) because <strong>the</strong>se names allow 

<strong>the</strong>se events to be placed <strong>in</strong> a regional context more 

easily. However it is understood that <strong>the</strong> available dat<strong>in</strong>g 

methods cannot provide an accurate age determ<strong>in</strong>ation 

for <strong>the</strong> IMU, thus us<strong>in</strong>g local stage names is reasonable. 

In this case, our preference is to use Lőren<strong>the</strong>y's twofold 

stage names, <strong>Pannonian</strong> and Levantian. This 

possibility was considered by Sacchi et al. (1997) and 

it was <strong>the</strong>ir possible solution #4 to reconcile <strong>the</strong> 

<strong>problem</strong>s of local stage names <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. 

<strong>The</strong> three-stage nomenclature proposed by Sacchi et al. 

(1997, 1999) and Sacchi and Müller (2004) <strong>in</strong>clud<strong>in</strong>g 

<strong>Pannonian</strong>, Transdanubian and Pontian stages for <strong>the</strong> 

pre-IMU strata is reasonable, but <strong>the</strong> bas<strong>in</strong>-wide 

correlation of <strong>the</strong> bound<strong>in</strong>g surfaces of <strong>the</strong>se stages 

has not yet been achieved. 

<strong>The</strong> IMU event has significant exploration implications. 

Van Balen et al. (1999) modeled bas<strong>in</strong> scale fluid 

flow <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> and found that overpressure 

built up between 6.3 and 5.5 Ma, a period match<strong>in</strong>g <strong>the</strong> 

<strong>Mess<strong>in</strong>ian</strong> event. This result may be expla<strong>in</strong>ed by <strong>the</strong> rapid 

and large sediment <strong>in</strong>flux and resedimentation enter<strong>in</strong>g <strong>the</strong> 

bas<strong>in</strong> from <strong>the</strong> northwest and west (Late <strong>Mess<strong>in</strong>ian</strong>– 

Pliocene sequence of this study) follow<strong>in</strong>g <strong>the</strong> IMU event 

(Fig. 14). <strong>The</strong> rapid accumulation of a large mass of 

sediments generated overpressure. Most of <strong>the</strong> hydrocarbon 

accumulations <strong>in</strong> <strong>the</strong> central parts of <strong>the</strong> bas<strong>in</strong> 

accumulated <strong>in</strong> turbiditic sandstones that were deposited 

above <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> unconformity (Csato, 1989, 1992). 

7. Galeacysta etrusca and <strong>the</strong> dilemma of 

paleo<strong>geo</strong>graphic connections 

Sütő-Szentai (1994, 2000, 2002), Magyar et al. 

(1999) and Geary et al. (2000) published d<strong>in</strong>oflagellate 

zonations of <strong>the</strong> late Miocene–Pliocene <strong>Pannonian</strong> 

Bas<strong>in</strong> fill. <strong>The</strong> ages of <strong>the</strong>se zones were determ<strong>in</strong>ed 

from available paleomagnetic data, <strong>the</strong>refore <strong>the</strong>ir 

accuracy is uncerta<strong>in</strong> (see Section 6.2). Never<strong>the</strong>less, 

<strong>the</strong>y can be used for age considerations along with 

ostracod zones <strong>in</strong> <strong>the</strong> non-mar<strong>in</strong>e <strong>Pannonian</strong> Bas<strong>in</strong> (e.g. 

Magyar et al., 2001; Szuromi-Korecz et al., 2004). One 

of <strong>the</strong> authors of this study collected core samples from 

exploratory wells <strong>in</strong> <strong>the</strong> eastern <strong>Pannonian</strong> Bas<strong>in</strong> and 

d<strong>in</strong>oflagellate assemblages were identified by Sütő- 

Szentai (2006) <strong>in</strong> those samples. <strong>The</strong> result was <strong>the</strong> 

discovery of G. etrusca <strong>in</strong> cores taken from <strong>the</strong> IMU 

zone as demonstrated <strong>in</strong> Fig. 16. It is important to note 

Fig. 18. A tentative correlation for <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> between <strong>the</strong> Mediterranean, Eastern Paratethys and <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. TG5-21 are <strong>in</strong>terglacial 

events (with high sea-level) of Shackleton et al. (1995) from oxygen isotopes.


135 

that s<strong>in</strong>ce only a few core samples, each a few m long, 

were drilled <strong>in</strong> <strong>the</strong>se hydrocarbon exploration wells, no 

cont<strong>in</strong>uous sampl<strong>in</strong>g was possible. Thus, <strong>the</strong> depths of 

<strong>the</strong> top and bottom of biostratigraphic zones (def<strong>in</strong>ed by 

<strong>the</strong> appearance and disappearance of <strong>the</strong> G. etrusca) 

could not always be determ<strong>in</strong>ed accurately. However, it 

is certa<strong>in</strong> that <strong>the</strong> core samples <strong>in</strong> Well-1 and-3 of 

Fig. 16 were taken from <strong>the</strong> IMU unconformity (<strong>in</strong> case 

of Well-3, a core was obta<strong>in</strong>ed from immediately below 

<strong>the</strong> IMU and ano<strong>the</strong>r precisely at <strong>the</strong> IMU), <strong>the</strong>refore <strong>the</strong> 

IMU is <strong>in</strong> <strong>the</strong> etrusca zone (no core samples were drilled 

around <strong>the</strong> IMU zone <strong>in</strong> <strong>the</strong> o<strong>the</strong>r wells shown <strong>in</strong> 

Fig. 16). G. etrusca existed before <strong>the</strong> IMU as <strong>the</strong> lower 

core sample of Well-3 and palynologic data <strong>in</strong> o<strong>the</strong>r 

wells (Sütő-Szentai, 2006) prove. However, no G. 

etrusca has been reported from cores taken above <strong>the</strong> 

IMU <strong>in</strong> <strong>the</strong> area where <strong>the</strong> IMU can be identified (Sütő- 

Szentai, 2006), which suggests that <strong>the</strong> G. etrusca 

disappeared after <strong>the</strong> IMU events, by <strong>the</strong> early Pliocene. 

<strong>The</strong>refore, it appears that <strong>the</strong> IMU unconformity 

matches <strong>the</strong> top of <strong>the</strong> etrusca zone. 

G. etrusca has been found <strong>in</strong> <strong>the</strong> Mediterranean 

(Bert<strong>in</strong>i et al., 1995; Bert<strong>in</strong>i, 2006)<strong>in</strong>strata5.33–5.35 Ma 

<strong>in</strong> age, as well as <strong>in</strong> <strong>the</strong> Dacic Bas<strong>in</strong> (Clauzon et al., 2005), 

where its appearance was dated at 5.33 to 5.52 Ma, all <strong>in</strong> 

<strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> (Fig. 17). If <strong>the</strong> disappearance of G. 

etrusca may be correlated across <strong>the</strong> Paratethys and 

Mediterranean, <strong>the</strong> age of <strong>the</strong> IMU <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> 

may also correlate with <strong>the</strong> 5.33–5.52 Ma ages, but <strong>the</strong> 5– 

6 Ma age range used <strong>in</strong> this study is most likely correct. 

Por and Dimentman (1985) believed from mollusk 

records that a Paratethyan fresh water <strong>in</strong>fluence reached 

<strong>the</strong> Central Mediterranean <strong>in</strong> <strong>the</strong> latest <strong>Mess<strong>in</strong>ian</strong>. <strong>The</strong> 

presence of G. etrusca <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> and 

surround<strong>in</strong>g areas may also suggest a paleo<strong>geo</strong>graphic 

connection between <strong>the</strong> Mediterranean, Central and 

Eastern Paratethys <strong>in</strong> late <strong>Mess<strong>in</strong>ian</strong> time (Sprovieri 

et al., 2003; Clauzon et al., 2005; Bert<strong>in</strong>i, 2006). 

However, it is not necessarily a proof for direct mar<strong>in</strong>e 

connections (Benson and Rakic-El Bied, 1991; Rouchy 

et al., 2001); it may ra<strong>the</strong>r <strong>in</strong>dicate freshen<strong>in</strong>g of water <strong>in</strong> 

<strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. Ostracod faunas also show a 

strong Paratethyan <strong>in</strong>fluence <strong>in</strong> Italy <strong>in</strong> <strong>the</strong> latest 

<strong>Mess<strong>in</strong>ian</strong> (Gliozzi, 1999); <strong>the</strong> discovery of Cyprideis 

<strong>in</strong> <strong>the</strong> Mediterranean suggested a Paratethyan water 

connection (Benson, 1973; Ryan, 1973). Paratethyan 

leptocy<strong>the</strong>rids, such as Cyprideis pannonica (Méhes) 

and Loxoconcha kochi (Méhes) were found <strong>in</strong> <strong>Mess<strong>in</strong>ian</strong> 

formations <strong>in</strong> Spa<strong>in</strong> and Italy (Gliozzi et al., 2005), 

and <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> (Szuromi-Korecz, 1992). 

In <strong>the</strong> Eastern Paratethys, Clauzon et al. (1996) 

provided evidence for water exchanges between <strong>the</strong> 

Dacic Bas<strong>in</strong> and <strong>the</strong> Mediterranean <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>. 

<strong>The</strong> mar<strong>in</strong>e connection was facilitated by <strong>the</strong> open<strong>in</strong>g of 

<strong>the</strong> Marmara Sea <strong>in</strong> west Anatolia (Çağatay et al., 2006; 

Flecker and Ellam, 2006). This region moved westward 

and its western part underwent extension due to rollback 

effects of <strong>the</strong> Hellenic convergent zone (Mart et al., 

2004). However, Vasiliev et al. (2004) did not f<strong>in</strong>d a 

good correlation <strong>in</strong> <strong>the</strong> paleo-environments between <strong>the</strong> 

South Carpathian foredeep and <strong>the</strong> Mediterranean. A 

tentative <strong>Mess<strong>in</strong>ian</strong> correlation between <strong>the</strong> <strong>Pannonian</strong> 

Bas<strong>in</strong>, <strong>the</strong> Dacic Bas<strong>in</strong> and <strong>the</strong> Mediterranean is 

proposed <strong>in</strong> Fig. 18. 

<strong>The</strong> Intra-<strong>Mess<strong>in</strong>ian</strong> Unconformity <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> 

Bas<strong>in</strong> may have formed <strong>in</strong> association with <strong>the</strong> tectonic 

reorganization that produced extensive erosional surfaces 

<strong>in</strong> <strong>the</strong> Mediterranean <strong>in</strong> <strong>Mess<strong>in</strong>ian</strong> time (e.g. Lofi 

et al., 2005) and led to <strong>the</strong> sal<strong>in</strong>ity crisis itself. <strong>The</strong> 

sal<strong>in</strong>ity crisis most likely did not form as a consequence 

of a eustatic sea-level fall but as a result of paleo<strong>geo</strong>graphic 

isolation from <strong>the</strong> Atlantic <strong>in</strong> response to plate 

tectonic motions (Vidal et al., 2002; Roveri et al., 2001; 

Warny and Wrenn, 2002; Roveri et al., 2003; Warny 

et al., 2003; Krijgsman et al., 2004; Clauzon et al., 2005; 

Jolivet et al., 2006). In fact, eustatic rises occurred 

several times dur<strong>in</strong>g <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> and nei<strong>the</strong>r <strong>the</strong> onset 

nor <strong>the</strong> end of <strong>the</strong> sal<strong>in</strong>ity crisis corresponds <strong>in</strong> time with 

global sea-level changes (Vidal et al., 2002). <strong>The</strong>refore, 

<strong>the</strong> IMU <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, if l<strong>in</strong>ked to tectonism 

<strong>in</strong> <strong>the</strong> Mediterranean, was not a eustatically controlled 

event ei<strong>the</strong>r. <strong>The</strong> drastic lower<strong>in</strong>g of sea-level <strong>in</strong> <strong>the</strong> 

Mediterranean most likely drove down <strong>the</strong> <strong>Pannonian</strong> 

lake-level through hydrological connections. A similar 

stratigraphic horizon to <strong>the</strong> <strong>Pannonian</strong> IMU was also 

discovered <strong>in</strong> <strong>the</strong> Black Sea. Gillet et al. (2003) proved 

that this horizon was connected to erosional surfaces 

toward <strong>the</strong> marg<strong>in</strong>al slopes of <strong>the</strong> Black Sea, formed 

dur<strong>in</strong>g <strong>the</strong> sal<strong>in</strong>ity crisis. It is plausible that desiccation 

of <strong>the</strong> Mediterranean <strong>in</strong>duced sea/lake-level falls <strong>in</strong> 

surround<strong>in</strong>g bas<strong>in</strong>s such as <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, Dacic 

Bas<strong>in</strong> and Black Sea and, on some occasions, sea-level 

rises also led to some water exchanges between <strong>the</strong>se 

areas (Clauzon et al., 2005). Although <strong>the</strong> late 

<strong>Mess<strong>in</strong>ian</strong> lake-level drawdown fundamentally shaped 

<strong>the</strong> sedimentary history of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, <strong>the</strong> size 

of <strong>the</strong> lake-level fall and <strong>the</strong> scale of erosion was much 

less than <strong>in</strong> <strong>the</strong> Mediterranean (Cita and Ryan, 1978). 

<strong>The</strong> <strong>Pannonian</strong> Bas<strong>in</strong> did not desiccate and no evaporites 

precipitated. Jolivet et al. (2006)'s reconstructions 

show that renewed north–south compression started <strong>in</strong> 

<strong>the</strong> Mediterranean <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>, eventually lead<strong>in</strong>g 

to <strong>the</strong> closure of <strong>the</strong> Straight of Gibraltar. <strong>The</strong> <strong>Pannonian</strong> 

<strong>in</strong>versions of this time (discussed <strong>in</strong> this paper) may


have been part of this major tectonic <strong>in</strong>teraction between 

Africa and Europe. 

8. Summary and conclusions 

This paper demonstrates that quantitative simulations 

of stratigraphic architectural patterns based on 

sequence stratigraphic <strong>in</strong>terpretations are a powerful 

tool for determ<strong>in</strong><strong>in</strong>g changes <strong>in</strong> base-level, sediment 

supply and subsidence/uplift rates, and <strong>the</strong>ir relative 

<strong>in</strong>fluences on stratal architecture. Model<strong>in</strong>g is especially 

useful <strong>in</strong> active extensional sett<strong>in</strong>gs where <strong>the</strong>se 

parameters vary not only <strong>in</strong> time but also <strong>in</strong> space for 

specific periods. 

A prom<strong>in</strong>ent unconformity was recognized on 

seismic sections, which is a regional, strongly developed 

erosional surface. It formed <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>, and <strong>in</strong> this 

study is called <strong>the</strong> Intra-<strong>Mess<strong>in</strong>ian</strong> Unconformity 

(IMU). <strong>The</strong> events that produced IMU caused <strong>the</strong> s<strong>in</strong>gle 

most profound change <strong>in</strong> <strong>the</strong> Late Miocene–Quaternary 

history of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. Rapid subsidence and 

thick deltaic depositions changed abruptly to retrogradational 

sediment accumulation. <strong>The</strong>refore, <strong>the</strong> IMU 

is proposed to def<strong>in</strong>e stratigraphic stages of <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong>. Tortonian–Lower <strong>Mess<strong>in</strong>ian</strong> or <strong>Pannonian</strong> 

and Late <strong>Mess<strong>in</strong>ian</strong>–Pliocene or Levantian units 

or stages are used <strong>in</strong> this work. 

Our experience has shown that <strong>the</strong> ages of <strong>the</strong> Late 

Miocene–Pliocene stratigraphic surfaces <strong>in</strong> eastern 

Hungary cannot be determ<strong>in</strong>ed with an accuracy of 

0.01 or even 0.1 Ma <strong>in</strong> spite of earlier efforts (Juhász 

et al., 2006); <strong>the</strong> resolution is much lower because of a 

lack of sufficient age data. Our estimation of <strong>the</strong> age of 

IMU is that it falls around a range of 5–6 Ma based on 

our seismic correlations with paleomagnetic polarity 

zones from core holes. This estimation was tuned by 

stratigraphic simulations and also seems to be supported 

by a match with <strong>the</strong> top part of <strong>the</strong> G. etrusca zone. A 

more accurate age determ<strong>in</strong>ation will require a new deep 

core hole penetrat<strong>in</strong>g <strong>the</strong> IMU and an astronomically 

calibrated chronological analysis. Never<strong>the</strong>less, <strong>the</strong> 

IMU is <strong>Mess<strong>in</strong>ian</strong> <strong>in</strong> age and most likely formed <strong>in</strong> 

association with <strong>the</strong> tectonic and paleo<strong>geo</strong>graphic 

events that took place <strong>in</strong> <strong>the</strong> sal<strong>in</strong>ity crisis. 

Lake Pannon formed a northward narrow<strong>in</strong>g bay <strong>in</strong> 

<strong>the</strong> territory of eastern Hungary <strong>in</strong> <strong>the</strong> Tortonian–Lower 

<strong>Mess<strong>in</strong>ian</strong> and was filled by two major delta systems: 

one sourced from <strong>the</strong> nor<strong>the</strong>ast (called Hajdúság system 

<strong>in</strong> this paper) and ano<strong>the</strong>r from <strong>the</strong> northwest–west 

(called Jászság–Kiskunság sources). A major lake-level 

fall occurred <strong>in</strong> <strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> that produced <strong>the</strong> 

IMU surface, and tectonic <strong>in</strong>version started at about <strong>the</strong> 

same time. <strong>The</strong>se two ma<strong>in</strong> factors toge<strong>the</strong>r profoundly 

altered <strong>the</strong> bas<strong>in</strong> fill processes. <strong>The</strong> Hajdúság delta 

system became less significant and <strong>the</strong> major sediment 

<strong>in</strong>flux shifted fur<strong>the</strong>r northwestward to <strong>the</strong> areas of <strong>the</strong> 

Jászság and Kiskunság. 

Four types of stratal architecture of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> lake 

marg<strong>in</strong> were identified on seismic data and were modeled 

<strong>in</strong> stratigraphic simulations. <strong>The</strong> Hajdúság architecture 

was generated by rapid subsidence <strong>in</strong> <strong>the</strong> Tortonian, 

dim<strong>in</strong>ish<strong>in</strong>g subsidence and uplift <strong>in</strong> <strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> 

and Pliocene and renewed, slow subsidence <strong>in</strong> <strong>the</strong> late 

Pliocene. An abrupt decrease and subsequent <strong>in</strong>crease <strong>in</strong> 

sediment supply was also determ<strong>in</strong>ed by <strong>the</strong> simulations 

prior to <strong>the</strong> IMU event. <strong>The</strong> IMU is a type I unconformity 

and is associated with large quantities of lowstand 

systems tract sediments <strong>in</strong> this architecture. Rapid 

Tortonian and slightly slower late Miocene–Pliocene 

subsidence, and a large sediment supply, formed <strong>the</strong> 

Jászság architecture. <strong>The</strong> IMU is a type II unconformity 

with shelf marg<strong>in</strong> systems tracts <strong>in</strong> <strong>the</strong> Jászság. In <strong>the</strong> 

Kiskunság architecture, tectonic uplift played a major role 

and magnified <strong>the</strong> impact of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> lake-level fall. 

<strong>The</strong> IMU is a type I unconformity. No delta systems 

developed at <strong>the</strong> Battonya area <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> time, 

ra<strong>the</strong>r, <strong>the</strong> Battonya High was an island and <strong>the</strong> IMU 

surface onlapped onto <strong>the</strong> flank of <strong>the</strong> high. 

Acknowledgements 

Keyu Liu generously helped with <strong>the</strong> Sedpak 

outputs. We are grateful for <strong>the</strong> contributions of <strong>the</strong> 

reviewers and <strong>the</strong> thorough and very helpful edit<strong>in</strong>g of 

Christopher Field<strong>in</strong>g. 

References 

Bada, G., Horváth, F., Cloet<strong>in</strong>gh, S., Coblentz, D.D., 2001. Role of 

topography-<strong>in</strong>duced gravitational stresses <strong>in</strong> bas<strong>in</strong> <strong>in</strong>version: <strong>the</strong> 

case study of <strong>the</strong> <strong>Pannonian</strong> bas<strong>in</strong>. Tectonics 20, 343–363. 

Báldi, K., Benkovics, L., Sztanó, O., 2002. Badenian (Middle 

Miocene) bas<strong>in</strong> development <strong>in</strong> SW Hungary: subsidence history 

based on quantitative paleobathymetry of foram<strong>in</strong>ifera. International 

Journal of Earth Sciences 91, 491–504. 

Baldw<strong>in</strong>, B., Butler, C.O., 1985. Compaction curves. American 

Association of Petroleum Geologists Bullet<strong>in</strong> 69, 622–626. 

Benson, R.H., 1973. Psychrospheric and cont<strong>in</strong>ental Ostracoda from 

ancient sediments <strong>in</strong> <strong>the</strong> floor of <strong>the</strong> Mediterranean. Initial Reports 

of <strong>the</strong> Deep Sea Drill<strong>in</strong>g Project 13, Part 2. Texas A&M University, 

Ocean Drill<strong>in</strong>g Program, College Station, TX, pp. 2002–2008. 

Benson, R.H., Rakic-El Bied, K., 1991. Biodynamics, sal<strong>in</strong>e giants and 

late Miocene catastrophism. Carbonates and Evaporites 6, 127–168. 

Bérczi, I., 1988. Prelim<strong>in</strong>ary sedimentological <strong>in</strong>vestigations of a 

Neogene depression. In: Royden, L.H., Horváth, F. (Eds.), <strong>The</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong>: A Study <strong>in</strong> Bas<strong>in</strong> Evolution. American 

Association of Petroleum Geologists Memoir, vol. 45. American


137 

Association of Petroleum Geologists, Tulsa, Oklahoma, USA, 

pp. 107–116. 

Bérczi, I., Philips, R.L., 1985. Processes and depositional environments 

with<strong>in</strong> Neogene deltaic-lacustr<strong>in</strong>e sediments, <strong>Pannonian</strong> Bas<strong>in</strong>, 

sou<strong>the</strong>ast Hungary. Eötvös L. Geophysical Institute, Geophysical 

Transactions Special Edition, vol. 31. Eötvös Lóránd Geophysical 

Institute, Budapest, Hungary, pp. 55–74. 

Berggren, W.A., Kent, D.V., Swisher III, C.C., Aubry, M.-P., 1995. A 

revised Cenozoic <strong>geo</strong>chronology and chronostratigraphy. In: 

Berggren, W.A., Kent, D.V., Audry, M.-P., Hardenbol, J. (Eds.), 

Geochronology, Time Scales and Global Stratigraphic Correlation. 

SEPM (Society for Sedimentary Geology) Special Publication, 

vol. 54. Society for Sedimentary Geology, Tulsa, Oklahoma, USA, 

pp. 129–212. 

Bert<strong>in</strong>i, A., 2006. <strong>The</strong> Nor<strong>the</strong>rn Apenn<strong>in</strong>es palynological record as a 

contribute for <strong>the</strong> reconstruction of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> palaeoenvironments. 

Sedimentary Geology 188–189, 235–258. 

Bert<strong>in</strong>i, A., Corrad<strong>in</strong>i, D., Suc, J.-P., 1995. On Galeacysta etrusca and 

<strong>the</strong> connections between <strong>the</strong> Mediterranean and <strong>the</strong> Paratethys. 

Abstracts, Xth R.C.M.N.S. Congress, Bucharest, Romania, p. 141. 

Buck, W.R., 1991. Modes of cont<strong>in</strong>ental lithospheric extension. 

Journal of Geophysical Research 96, 163–168. 

Çağatay, M.N., Görür, N., Flecker, R., Sakınç, M., Tünoğlu, C., Ellam, 

R., Krijgsman, W., V<strong>in</strong>cent, S., Dikbaş, A., 2006. Paratethyan– 

Mediterranean connectivity <strong>in</strong> <strong>the</strong> Sea of Marmara region (NW 

Turkey) dur<strong>in</strong>g <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>. Sedimentary Geology 188–189, 

171–187. 

Catuneanu, O., 2002. Sequence stratigraphy of clastic systems: concepts, 

merits, and pitfalls. Journal of African Earth Sciences 35, 1–43. 

Catuneanu, O., 2006. Pr<strong>in</strong>ciples of Sequence Stratigraphy. Elsevier, 

Amsterdam. 

Cita, M.B., 1982. <strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis <strong>in</strong> <strong>the</strong> Mediterranean: a 

review. In: Berckhemer, H., Hsü, K.J. (Eds.), Alp<strong>in</strong>e-Mediterranean 

Geodynamics. Geodynamic Series, vol. 7. American Geophisical 

Union, Wash<strong>in</strong>gton, DC, pp. 113–140. 

Cita, M.B., 1991. Development of a scientific controversy. In: Mueller, 

D.V., McKenzie, J.A., Weissert, H. (Eds.), Controversies <strong>in</strong> Modern 

Geology; Evolution of Geological <strong>The</strong>ories <strong>in</strong> Sedimentology, Earth 

History and Tectonics. Academic Press, London, UK, pp. 13–23. 

Cita, M.B., Ryan, W.B.F., 1978. <strong>Mess<strong>in</strong>ian</strong> erosional surfaces <strong>in</strong> <strong>the</strong> 

Mediterranean. Mar<strong>in</strong>e Geology 27, 3–4. 

Clauzon, G., Suc-J.-P., Gautier, F., Berger, F., Loutre, A., 1996. 

Alternate <strong>in</strong>terpretation of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis: controversy 

resolved? Geology 24, 363–366. 

Clauzon,G.,Suc,J.-P.,Popescu,S.-M.,Marunteanu,M.,Rub<strong>in</strong>o,J.-L., 

Mar<strong>in</strong>escu, F., Mel<strong>in</strong>tes, M.C., 2005. Influence of Mediterranean sealevel 

changes on <strong>the</strong> Dacic Bas<strong>in</strong> (Eastern Paratethys) dur<strong>in</strong>g <strong>the</strong> late 

Neogene: <strong>the</strong> Mediterranean Lago Mare facies deciphered. Bas<strong>in</strong> 

Research 17, 437–462. 

Cloet<strong>in</strong>gh, S., 1988. Intraplate stresses: a new element <strong>in</strong> bas<strong>in</strong> 

analysis. In: Kle<strong>in</strong>spehn, K.L., Paola, C. (Eds.), New Perspectives 

<strong>in</strong> Bas<strong>in</strong> Analysis. Spr<strong>in</strong>ger, New York, NY, pp. 205–230. 

Csato, I., 1989. <strong>Pannonian</strong> sedimentological facies relations of <strong>the</strong> 

hydrocarbon accumulations with<strong>in</strong> <strong>the</strong> central part of <strong>the</strong> <strong>Pannonian</strong> 

bas<strong>in</strong>. Abstracts, 10th IAS Regional Meet<strong>in</strong>g on Sedimentology. 

Hungarian Geological Society, Budapest, Hungary, pp. 60–62. 

Csato, I., 1992. <strong>The</strong> <strong>Mess<strong>in</strong>ian</strong> water-level change and <strong>the</strong> connected 

stratigraphic traps <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> bas<strong>in</strong>, Hungary. Technical 

Programme and Abstracts of Papers, European Association of 

Petroleum Geoscientists and Eng<strong>in</strong>eers, 4th Conference and Technical 

Exhibition. European Association of Petroleum Geoscientists and 

Eng<strong>in</strong>eers, Houten, Ne<strong>the</strong>rlands, p. 110. 

Csato, I., 1993. Neogene sequences <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> bas<strong>in</strong>, Hungary. 

Tectonophysics 226, 377–400. 

Csato, I., 1995. Sequence stratigraphic <strong>in</strong>terpretations and model<strong>in</strong>g <strong>in</strong> 

lacustr<strong>in</strong>e rift bas<strong>in</strong>s: <strong>the</strong> Sou<strong>the</strong>rn Dead Sea bas<strong>in</strong>, Israel and 

<strong>Pannonian</strong> Bas<strong>in</strong>, Hungary. PhD Dissertation, Columbia, SC. 

Csato, I., Kendall, C.G.StC., 2002. Model<strong>in</strong>g of stratigraphic 

architectural patterns <strong>in</strong> extensional sett<strong>in</strong>gs — towards a 

conceptual model. Computers & Geosciences 28, 351–356. 

Csontos, L., Nagymarosy, A., 1998. <strong>The</strong> Mid-Hungarian l<strong>in</strong>e: a zone 

of repeated tectonic <strong>in</strong>versions. Tectonophysics 297, 51–71. 

Csontos, L., Nagymarosy, A., Horváth, F., Kovác, M., 1992. Tertiary 

evolution of <strong>the</strong> Intra-Carpathian area: a model. Tectonophysics 

208, 221–241. 

Den Bezemer, T., Kooi, H., Kranenborg, J., Cloet<strong>in</strong>gh, S., 2000. 

Model<strong>in</strong>g gra<strong>in</strong>-size distributions. A comparison of two models 

and <strong>the</strong>ir numerical solution. Tectonophysics 320, 347–373. 

Elston, D.P., Lantos, M., Hámor, T., 1994. High resolution polarity 

records and <strong>the</strong> stratigraphic and magnetostratigraphic correlation 

of Late Miocene and Pliocene (<strong>Pannonian</strong> s. l.) deposits of 

Hungary. In: Teleki, P.G., Mattick, R.E., Kókay, J. (Eds.), Bas<strong>in</strong> 

Analysis <strong>in</strong> Petroleum Exploration. A Case Study from <strong>the</strong> Békés 

Bas<strong>in</strong>, Hungary. Kluwer Academic Publisher, Dordrecht, Ne<strong>the</strong>rlands, 

pp. 111–142. 

Flecker, R., Ellam, R.M., 2006. Identify<strong>in</strong>g Late Miocene episodes of 

connection and isolation <strong>in</strong> <strong>the</strong> Mediterranean–Paratethyan realm 

us<strong>in</strong>g Sr isotopes. Sedimentary Geology 188–189, 189–203. 

Fodor, L., Csontos, L., Bada, G., Györfi, I., Benkovics, L., 1999. 

Tertiary tectonic evolution of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> system and 

neighbour<strong>in</strong>g orogens: a new syn<strong>the</strong>sis of paleostress data. In: 

Durand, B., Jolivet, L., Horváth, F., Séranne, M. (Eds.), <strong>The</strong> 

Mediterranean Bas<strong>in</strong>s: Tertiary Extension with<strong>in</strong> <strong>the</strong> Alp<strong>in</strong>e 

Orogen. Geol. Soc. Spec. Pub., vol. 156. <strong>The</strong> Geological Society, 

London, United K<strong>in</strong>gdom, pp. 295–334. 

Fülöp, J., Berzsányszky, K., Haas, J., 1987. <strong>The</strong> new map of <strong>the</strong> 

basement of Hungary. Acta Geologica Hungarica 30, 3–20. 

Gajdos, I., 1989. Adatok az alföldi pannoniai s.l. fejlődéstörténetéhez 

es ennek gyakorlati vonatkozásai a szénhidrogén-kutatásban. 

Földtani Kutatás 32, 8–21 (<strong>in</strong> Hungarian with English summary). 

Gawthorpe, R.L., Fraser, A.J., Collier, A.J., 1994. Sequence stratigraphy 

<strong>in</strong> active extensional bas<strong>in</strong>s: implications for <strong>the</strong> <strong>in</strong>terpretation of 

ancient bas<strong>in</strong>-fills. Mar<strong>in</strong>e and Petroleum Geology 11, 642–658. 

Geary, D.H., Magyar, I., Müller, P., 2000. Ancient Lake Pannon and its 

endemic molluscan fauna (Central Europe; Mio-Pliocene). In: 

Rossiter, A., Kawanabe, H. (Eds.), Advances <strong>in</strong> Ecological 

Research, vol. 31. Academic Press, London, UK, pp. 463–482. 

Gillet, H., Lericolais, G., Rehault, J.P., D<strong>in</strong>u, C., 2003. La stratigraphie 

oligo-miocène et la surface d'érosion mess<strong>in</strong>ienne en mer Noire, 

stratigraphie sismique haute resolution. Comptes Rendus Geoscience 

335, 907–916 (<strong>in</strong> French with English abstract and abridged 

English version). 

Gliozzi, E., 1999. A late <strong>Mess<strong>in</strong>ian</strong> brackish water ostracod fauna of 

Paratethyan aspect from Le Vicenne Bas<strong>in</strong> (Abruzzi, central 

Apenn<strong>in</strong>es, Italy). Palaeo<strong>geo</strong>graphy, Palaeoclimatology, Palaeoecology 

151, 191–208. 

Gliozzi, E., Rodriguez-Lazaro, J., Nachite, D., Mart<strong>in</strong>-Rubio, M., 

Bekkali, R., 2005. An overview of Neogene brackish leptocy<strong>the</strong>rids 

from Italy and Spa<strong>in</strong>: biochronological and palaeo<strong>geo</strong>graphical 

implications. Palaeo<strong>geo</strong>graphy, Palaeoclimatology, Palaeoecology 

225, 283–301. 

Grow, J.A., Mattick, R.E., Bérczi-Makk, A., Péró, C.S., Hajdú, D., 

Pogácsás, G.Y., Várnai, P., Varga, E., 1994. Structure of <strong>the</strong> Békés 

bas<strong>in</strong> <strong>in</strong>ferred from seismic reflection, well and gravity data. In:


Teleki, P.G., Mattick, R.E., Kókai, J. (Eds.), Bas<strong>in</strong> Analysis <strong>in</strong> 

Petroleum Exploration. Kluwer Academic Publishers, Dordrecht, 

Ne<strong>the</strong>rlands, pp. 1–38. 

Haas, J., Péró, C.S., 2004. Mesozoic evolution of <strong>the</strong> Tisza Mega-unit. 

International Journal of Earth Sciences 93, 297–313. 

Haas, J., Mioè, P., Pamiè, J., Tomljenović, B., Árkai, P., Bérczi-Makk, A., 

Koroknai, B., Kovács, S., Felgenhauer, E.R., 2000. Complex 

structural pattern of <strong>the</strong> Alp<strong>in</strong>e–D<strong>in</strong>aridic–<strong>Pannonian</strong> triple junction. 

International Journal of Earth Sciences 89, 377–389. 

Hámor, G., 1983. <strong>The</strong> Quantitative Methods of Paleo<strong>geo</strong>graphic 

Reconstructions. Hungarian Geological Institute Special Paper. 

Hungarian Geological Institute, Budapest, Hungary. 

Hámor, G., 1985. Geology of <strong>the</strong> Nógrád–Cserhát area. Geologica 

Hungarica, vol. 22. Akadémiai Kiadó, Budapest, Hungary. 

Hámor, G., 1997. A magyarországi miocén fejlődéstörténete és 

ősföldrajza. Fülöp József Emlékkönyv. Akadémiai Kiadó, Budapest, 

pp. 231–250 (<strong>in</strong> Hungarian). 

Haq, B.U., Hardendol, J., Vail, P.R., 1987. Chronology of fluctuat<strong>in</strong>g 

sea levels s<strong>in</strong>ce <strong>the</strong> Triassic (250 Myr ago to present). Science 235, 

1156–1167. 

Helland-Hansen, W., Gjelberg, J.G., 1994. Conceptual basis and 

variability <strong>in</strong> sequence stratigraphy: a different perspective. 

Sedimentary Geology 92, 31–52. 

Horváth, F., 1993. Towards a mechanical model for <strong>the</strong> formation of 

<strong>the</strong> <strong>Pannonian</strong> bas<strong>in</strong>. Tectonophysics 226, 333–357. 

Horváth, F., 1995. Phases of compression dur<strong>in</strong>g <strong>the</strong> evolution of <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong> and its bear<strong>in</strong>g on hydrocarbon exploration. 

Mar<strong>in</strong>e and Petroleum Geology 12, 837–844. 

Horváth, F., Berckhemer, H., 1982. Mediterranean backarc bas<strong>in</strong>s. In: 

Berckhemer, H., Hsü, K.J. (Eds.), Alp<strong>in</strong>e-Mediterranean Geodynamics. 

. Geodynamic Series, vol. 7. American Geophisical Union, 

Wash<strong>in</strong>gton, DC, pp. 141–173. 

Horváth, F., Cloet<strong>in</strong>gh, S., 1996. Stress-<strong>in</strong>duced late-stage subsidence 

anomalies <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. Tectonophysics 266, 287–300. 

Huismans, R.S., Podladchikov, Y.Y., Cloet<strong>in</strong>gh, S., 2001. Dynamic 

model<strong>in</strong>g of <strong>the</strong> transition from passive to active rift<strong>in</strong>g, 

application to <strong>the</strong> <strong>Pannonian</strong> bas<strong>in</strong>. Tectonics 20, 1021–1039. 

Hsü, K.J., Montadert, L., Bernoulli, D., Cita, M.B., Erickson, A., 

Garrison, R.E., Kidd, R.B., Melieres, F., Müller, C., Wright, R., 

1977. History of <strong>the</strong> Mediterranean sal<strong>in</strong>ity crisis. Nature 267, 

399–403. 

Jiménez-Moreno, G., Rodríguez-Tovar, F.J., Pardo-Igúzquiza, E., 

Fauquette, S., Suc, J.-P., Müller, P., 2005. High-resolution 

palynological analysis <strong>in</strong> late early-middle Miocene core from 

<strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, Hungary: climatic changes, astronomical 

forc<strong>in</strong>g and eustatic fluctuations <strong>in</strong> <strong>the</strong> Central Paratethys. 

Palaeo<strong>geo</strong>graphy, Palaeoclimatology, Palaeoecology 216, 73–97. 

Jolivet, L., Augier, R., Rob<strong>in</strong>, C., Suc, J.-P., Rouchy, J.M., 2006. 

Lithospheric-scale <strong>geo</strong>dynamic context of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity 

crisis. Sedimentary Geology 188–189, 9–33. 

Juhász, G., 1998. A magyarországi neogén mélymedencék 

pannónia képződménye<strong>in</strong>ek litosztratigráfiája. In: Bérczi, I., 

Jámbor, Á. (Eds.), Occasional Papers of <strong>the</strong> Geological Institute 

of Hungary, vol. 194. Hungarian Geological Institute, Budapest, 

Hungary, pp. 469–483. 

Juhász, E., Kovács, L.Ó., Müller, P., Tóth-Makk, Á., Philips, L., 

Lantos, M., 1997. Climatically driven sedimentary cycles <strong>in</strong> <strong>the</strong> 

late Miocene sediments of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, Hungary. 

Tectonophysics 282, 257–276. 

Juhász, E., Philips, L., Müller, P., Ricketts, B., Tóth-Makk, Á., Lantos, 

M., Lovács, L.Ó., 1999. Late Neogene sedimentary facies and 

sequences <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, Hungary. In: Durand, B., Jolivet, L., 

Horváth, F., Séranne, M. (Eds.), <strong>The</strong> Mediterranean Bas<strong>in</strong>s: Tertiary 

Extension with<strong>in</strong> <strong>the</strong> Alp<strong>in</strong>e Orogen. . Geol. Soc. Spec. Pub., vol. 156. 

<strong>The</strong> Geological Society, London, United K<strong>in</strong>gdom, pp. 335–356. 

Juhász, G., Pogácsás, G., Magyar, I., Vakarcs, G., 2006. Integráltsztratigráfiai 

és fejlődéstörténeti vizsgálatok az Alföld pannóniai s.l. 

rétegsorában. Földtani Közlöny 136, 51–86 (<strong>in</strong> Hungarian with 

English Abstract). 

Kendall, C.G.StC., Strobel, J., Cannon, R.L., Bezdek, J., Biswas, G., 

1991. <strong>The</strong> simulation of <strong>the</strong> sedimentary fill of bas<strong>in</strong>s. Journal of 

Geophysical Research 96, 6911–6929. 

Kendall, C.G.StC., Whittle, G.L., Ehrlich, R., Moore, P.D., Cannon, R.L., 

Hellmann, D.R., 1993. Computer sedimentary simulation models 

sequence stratigraphy. Oil & Gas Journal 91, 46–51. 

Krijgsman, W., Hilgen, F.J., Raffi, I., Sierrom, F.J., Wilson, D.S., 1999. 

Chronology, causes and progression of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity 

crisis. Nature 400, 652–655. 

Krijgsman, W., Gaboardi, S., Hilgen, F.J., Iaccar<strong>in</strong>o, S., de Kaenel, E., 

van der Laan, E., 2004. Revised astrochronology for <strong>the</strong> A<strong>in</strong> el 

Beida section (Atlantic Morocco); no glacio-eustatic control for <strong>the</strong> 

onset of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis. Stratigraphy 1, 87–101. 

Lantos, M., Hámor, T., Pogácsás, G., 1992. Magneto- and seismostratigraphic 

correlations of <strong>Pannonian</strong> s.l. (late Miocene and 

Pliocene) deposits <strong>in</strong> Hungary. Paleontologia y Evolucion 24–25, 

35–46. 

Lev<strong>in</strong>, P.A., 1999. Sequence stratigraphic simulation; a tool for 

model<strong>in</strong>g <strong>the</strong> stratal architecture with<strong>in</strong> sedimentary depositional 

systems. PhD Dissertation, University of South Carol<strong>in</strong>a, Columbia, 

SC. 

Lofi, J., Gor<strong>in</strong>i, C., Berné, S., Clauzon, G., Tadeu Dos Reis, A., 

Ryan, W.B.F., Steckler, M.S., 2005. Erosional processes and paleoenvironmental 

changes <strong>in</strong> <strong>the</strong> Western Gulf of Lions (SW France) 

dur<strong>in</strong>g <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis. Mar<strong>in</strong>e Geology 217, 1–30. 

Magyar, I., Geary, D.H., Müller, P., 1999. Paleo<strong>geo</strong>graphic evolution 

of <strong>the</strong> Late Miocene Lake Pannon <strong>in</strong> central Europe. Palaeo<strong>geo</strong>graphy, 

Palaeoclimatology, Palaeoecology 147, 151–167. 

Magyar, I., Juhász, G., Szuromi-Korecz, A., Sütő-Szentai, M., 2001. A 

pannóniai Tótkomlósi Mészmárga Tagozat kifejlődése és kora a 

Battonya-pusztaföldvári-hátság környezetében. Földtani Közlöny 

133, 521–540 (<strong>in</strong> Hungarian with English abstract). 

Mart, Y., Ryan, W.B.F., Lun<strong>in</strong>a, O.V., 2004. Review of <strong>the</strong> tectonics of 

<strong>the</strong> Levant Rift system: <strong>the</strong> structural significance of oblique 

cont<strong>in</strong>ental breakup. Tectonophysics 395, 209–232. 

Mattick, R.E., Philips, R.L., Rumpler, J., 1988. Seismic stratigraphy and 

depositional framework of sedimentary rocks <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> bas<strong>in</strong> 

<strong>in</strong> sou<strong>the</strong>astern Hungary. In: Royden, L.H., Horváth, F. (Eds.), <strong>The</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong>, a Study <strong>in</strong> Bas<strong>in</strong> Evolution. American Association 

of Petroleum Geologists, Memoir, vol. 45. American Association of 

Petroleum Geologists, Tulsa, Oklahoma, USA, pp. 117–145. 

Mattick, R.E., Rumpler, J., Újfalusy, A., Szanyi, B., Nagy, I., 1994. 

Sequence stratigraphy of <strong>the</strong> Békés bas<strong>in</strong>. In: Teleki, P.G., Mattick, 

R.E., Kókai, J. (Eds.), Bas<strong>in</strong> Analysis <strong>in</strong> Petroleum Exploration. 

Kluwer Academic Publishers, Dordrecht, Ne<strong>the</strong>rlands, pp. 39–65. 

Mattick, R.E., Teleki, P.G., Philips, L., Clayton, J.L., David, G., 

Pogácsás, G., Bardócz, B., Simon, E., 1996. Structure, stratigraphy, 

and petroleum <strong>geo</strong>logy of <strong>the</strong> Little Hungarian Pla<strong>in</strong> Bas<strong>in</strong>, 

Northwestern Hungary. American Association of Petroleum 

Geologists Bullet<strong>in</strong> 80, 1780–1800. 

Moore, P.D., 1997. Sedimentary simulations; design and application of 

SEDPAK. PhD Dissertation, University of South Carol<strong>in</strong>a, 

Columbia, SC. 

Patrascu, St., Panaiotu, C., Seclaman, M., Panaiotu, C.E., 1994. 

Tim<strong>in</strong>g of rotational motion of Apuseni Mts. (Romania):


139 

paleomagnetic data from Tertiary magmatic rocks. Tectonophysics 

233, 163–176. 

Pogácsás, G., Lakatos, L., Újszászi, K., Vakarcs, G., Várkonyi, L., 

Várnai, P., Révész, I., 1988. Seismic facies, electro facies and 

Neogene sequence chronology of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. Acta 

Geologica Hungarica 31, 175–207. 

Pogácsás, G., Szabó, A., Szalay, J., 1992. Chronostratigraphic 

relations of <strong>the</strong> progradational delta sequence of <strong>the</strong> Great 

Hungarian Pla<strong>in</strong>. Acta Geologica Hungarica 35, 311–327. 

Pogácsás, G., Müller, P., Magyar, I., 1993. <strong>The</strong> role of seismic 

stratigraphy <strong>in</strong> understand<strong>in</strong>g biological evolution <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> 

Lake. Geologia Croatica 46, 63–69. 

Pogácsás, G., Mattick, R.E., Elston, D.P., Hámor, T., Jámbor, Á., 

Lakatos, L., Lantos, M., Simon, E., Vakarcs, G., Várkonyi, L., 

Várnai, P., 1994. Correlation of seismo- and magnetostratigraphy 

<strong>in</strong> sou<strong>the</strong>astern Hungary. In: Teleki, P.G., Mattick, R.E., Kókai, J. 

(Eds.), Bas<strong>in</strong> Analysis <strong>in</strong> Petroleum Exploration. Kluwer Academic 

Publishers, Dordrecht, Ne<strong>the</strong>rlands, pp. 143–160. 

Por, F.D., Dimentman, C., 1985. Cont<strong>in</strong>uity of <strong>Mess<strong>in</strong>ian</strong> biota <strong>in</strong> <strong>the</strong> 

Mediterranean bas<strong>in</strong>. In: Stanley, D.J., Wezel, F.-C. (Eds.), 

Geological Evolution of <strong>the</strong> Mediterranean Bas<strong>in</strong>. Spr<strong>in</strong>ger– 

Verlag, New York, pp. 545–557. 

Posamentier, H.W., Vail, P.R., 1988. Eustatic controls on clastic 

deposition II — sequence and systems tract models. In: Wilgus, 

C.K., Hast<strong>in</strong>gs, B.S., Kendall, C.G.St.C., Posamentier, H.W., 

Ross, C.A., Van Wagoner, J.C. (Eds.), Sea Level Changes — An 

Integrated Approach. SEPM (Society for Sedimentary Geology) 

Special Publication, vol. 42. Society for Sedimentary Geology, Tulsa, 

Oklahoma, USA, pp. 125–154. 

Ratschbacher, L., Frisch, W., L<strong>in</strong>zer, H.G., Merle, D., 1991. Lateral 

extension <strong>in</strong> <strong>the</strong> Eastern Alps, part 2; structural analysis. Tectonics 

10, 257–271. 

Rouchy, J.M., Orszag-Sperber, F., Blanc-Valleron, M.-M., Pierre, C., 

Riviere, M., Combourieu-Nebout, N., Panayides, I., 2001. Paleoenvironmental 

changes at <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong>–Pliocene boundary <strong>in</strong> <strong>the</strong> 

eastern Mediterranean (sou<strong>the</strong>rn Cyprus bas<strong>in</strong>s): significance of <strong>the</strong> 

<strong>Mess<strong>in</strong>ian</strong> Lago-Mare. Sedimentary Geology 145, 93–117. 

Roveri, M., Bassetti, M.A., Ricci Lucchi, F., 2001. <strong>The</strong> Mediterranean 

<strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis: an Apenn<strong>in</strong>e foredeep perspective. 

Sedimentary Geology 140, 201–214. 

Roveri, M., Manzi, V., Ricci Lucchi, F., Rogledi, S., 2003. Sedimentary 

evolution of <strong>the</strong> Vena del Gesso bas<strong>in</strong> (Nor<strong>the</strong>rn Apenn<strong>in</strong>es, Italy): 

implications for <strong>the</strong> onset of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis. 

Geological Society of America Bullet<strong>in</strong> 115, 387–405. 

Royden, L.H., 1988. Late Cenozoic tectonics of <strong>the</strong> <strong>Pannonian</strong> bas<strong>in</strong> 

system. In: Royden, L.H., Horváth, F. (Eds.), <strong>The</strong> <strong>Pannonian</strong> 

Bas<strong>in</strong>, a Study <strong>in</strong> Bas<strong>in</strong> Evolution. American Association of 

Petroleum Geologists, Memoir, vol. 45. American Association of 

Petroleum Geologists, Tulsa, Oklahoma, USA, pp. 27–48. 

Royden, L.H., Báldi, T., 1988. Late Cenozoic tectonics of <strong>the</strong> 

<strong>Pannonian</strong> bas<strong>in</strong> system. In: Royden, L.H., Horváth, F. (Eds.), 

<strong>The</strong> <strong>Pannonian</strong> Bas<strong>in</strong>, a Study <strong>in</strong> Bas<strong>in</strong> Evolution. American 

Association of Petroleum Geologists, Memoir, vol. 45. American 

Association of Petroleum Geologists, Tulsa, Oklahoma, 

USA, pp. 1–16. 

Royden, L.H., Horváth, F., Rumpler, J., 1983a. Evolution of <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong> system, 1. Tectonics 2, 63–90. 

Royden, L.H., Horváth, F., Nagymarosy, A., Stegena, L., 1983b. 

Evolution of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong> system, 2. Subsidence and 

<strong>the</strong>rmal history. Tectonics 2, 91–137. 

Ryan, W.B.F., 1973. <strong>The</strong> Pliocene record <strong>in</strong> deep-sea Mediterranean 

sediments. Initial Reports of <strong>the</strong> Deep Sea Drill<strong>in</strong>g Project 13, Part 

2. Texas A&M University, Ocean Drill<strong>in</strong>g Program, College 

Station, TX, pp. 1341–1343. 

Sacchi, M., Müller, P., 2004. Orbital cyclicity and astronomical 

calibration of <strong>the</strong> upper Miocene cont<strong>in</strong>ental succession cored at 

<strong>the</strong> Iharosberény-I well site, Western <strong>Pannonian</strong> Bas<strong>in</strong>, Hungary. 

In: D'Argenio, B., Fischer, A.G., Premoli Silva, I., Weissert, H., 

Ferreri, V. (Eds.), Cyclostratigraphy: Approaches and Case 

Histories. SEPM (Society of Sedimentary Geology) Special 

Publication, vol. 81. Society for Sedimentary Geology, Tulsa, 


Sacchi, M., Horváth, F., Magyar, I., Müller, P., 1997. Problems and 

progress <strong>in</strong> establish<strong>in</strong>g a Late Neogene chronostratigraphy for <strong>the</strong> 

Central Paratethys. Neogene Newsletter 37–46. 

Sacchi, M., Horváth, F., Magyari, O., 1999. Role of unconformitybounded 

units <strong>in</strong> <strong>the</strong> stratigraphy of <strong>the</strong> cont<strong>in</strong>ental record: a case 

study from <strong>the</strong> Late Miocene of <strong>the</strong> western <strong>Pannonian</strong> Bas<strong>in</strong>, 

Hungary. In: Durand, B., Jolivet, L., Horváth, F., Séranne, M. 

(Eds.), <strong>The</strong> Mediterranean Bas<strong>in</strong>s: Tertiary Extension with<strong>in</strong> <strong>the</strong> 

Alp<strong>in</strong>e Orogen. Geol. Soc. Spec. Pub., vol. 156. <strong>The</strong> Geological 

Society, London, United K<strong>in</strong>gdom, pp. 357–390. 

Sclater, J.G., Royden, L.H., Horváth, F., Burchfiel, B.C., Sempken, S., 

Stegena, L., 1980. <strong>The</strong> formation of <strong>the</strong> <strong>in</strong>tra-Carpathian bas<strong>in</strong>s as 

determ<strong>in</strong>ed from subsidence data. Earth and Planetary Science 

Letters 51, 139–162. 

Shackleton, N.J., Hall, M.A., Pate, D., 1995. Pliocene stable isotope 

stratigraphy of Site 846. In: Pisias, N.G., Mayer, L.A., Janecek, T.R., 

Palmer-Julson, A., van Andel, T.H. (Eds.), Proceed<strong>in</strong>gs of <strong>the</strong> 

Ocean Drill<strong>in</strong>g Program, Scientific Results, vol. 138. Texas 

A&M University, Ocean Drill<strong>in</strong>g Program, College Station, TX, 

pp. 337–355. 

Sprovieri, M., Sacchi, M., Rohl<strong>in</strong>g, E.J., 2003. Climatically <strong>in</strong>fluenced 

<strong>in</strong>teractions between <strong>the</strong> Mediterranean and <strong>the</strong> Paratethys dur<strong>in</strong>g 

<strong>the</strong> Tortonian. Paleoceanography 18, 1034–1044. 

Sütő-Szentai, M., 1994. Microplankton associations of organic 

skeleton <strong>in</strong> <strong>the</strong> surround<strong>in</strong>g of Villány Mts. Földtani Közlöny 

124, 451–479 (<strong>in</strong> Hungarian with English abstract). 

Sütő-Szentai, M., 2000. Organic walled microplankton zonation of <strong>the</strong> 

<strong>Pannonian</strong> s.l. <strong>in</strong> <strong>the</strong> surround<strong>in</strong>gs of Kaskantyú, Paks and 

Tengelic (Hungary). Annual Report of <strong>the</strong> Geological Institute of 

Hungary 1994–1995/II. Hungarian Geological Institute, Budapest, 

Hungary, pp. 153–175. 

Sütő-Szentai, M., 2002. Analysis of microplanktons of organic 

skeleton from borehole Nagykozár-2 (S-Hungary). Folia Comloensis 

11, 93–110. 

Sütő-Szentai, M., 2006. Jelentés a Középalföld tervezési terület 

őslénytani (D<strong>in</strong>oflagellata, Ostracoda) vizsgálatáról. Unpublished 

report, Új őslénytani adatok: A középalföldi fúrások szervesvázú 

mikroplankton vizsgálatának értékelése, Sütő Zoltánné, 7300 

Komló, Május 1 u 7 (<strong>in</strong> Hungarian). 

Szuromi-Korecz, A., 1992. A Délkelet-Dunántúl pannónian s.l. 

képződménye<strong>in</strong>ek rétegtani értékelése ostracoda faunájuk alapján. 

Őslénytani Viták Discussiones Palaeontologicae 38, 5–20 (<strong>in</strong> 

Hungarian with English abstract). 

Szuromi-Korecz, A., Sütő-Szentai, M., Magyar, I., 2004. Biostratigraphic 

revision of <strong>the</strong> Hód-I well: Hungary's deepest borehole 

failed to reach <strong>the</strong> base of <strong>the</strong> upper Miocene <strong>Pannonian</strong> stage. 

Geologica Carpathica 55, 475–485. 

Tari, G., 1996. Neoalp<strong>in</strong>e tectonics of <strong>the</strong> Danube bas<strong>in</strong> (NW 

<strong>Pannonian</strong> bas<strong>in</strong>, Hungary). In: Ziegler, P.A., Horváth, F. (Eds.), 

Structure and Prospects of Alp<strong>in</strong>e Bas<strong>in</strong>s and Forelands. Peri- 

Tethys Memoir, vol. 2. Editions du Muséum National d'Histoire 

Naturelle, Paris, France, pp. 439–454.


Tari, G., Horváth, F., 1995. Middle Miocene extensional collapse <strong>in</strong> 

<strong>the</strong> Alp<strong>in</strong>e-<strong>Pannonian</strong> transition zone. In: Horváth, F., Tari, G., 

Bokor, C.S. (Eds.), Extensional Collapse of <strong>the</strong> Alp<strong>in</strong>e Orogene 

and Hydrocarbon Prospects <strong>in</strong> <strong>the</strong> Basement and Basement Fill 

of <strong>the</strong> Western <strong>Pannonian</strong> Bas<strong>in</strong>. AAPG International Conference 

and Exhibition, Nice, France, Guidebook to Fieldtrip, 

vol. 6. American Association of Petroleum Geologists, Tulsa, 


Tari, G., Horváth, F., Rumpler, J., 1992. Styles of extension <strong>in</strong> <strong>the</strong> 

<strong>Pannonian</strong> Bas<strong>in</strong>. Tectonophysics 208, 203–219. 

Thamó-Bozsó, E., Kercsmár, Z.S., Nádor, A., 2002. Tectonic control 

on changes <strong>in</strong> sediment supply: Quaternary alluvial systems, Körös 

sub-bas<strong>in</strong>, SE Hungary. In: Jones, S.J., Frostick, L.E. (Eds.), 

Sediment Flux to Bas<strong>in</strong>s: Causes, Controls and Consequences. 

Geol. Soc. Spec. Pub., vol. 191, pp. 37–53. 

Tomljenović, B., Csontos, L., 2001. Neogene–Quaternary structures <strong>in</strong> 

<strong>the</strong> border zone between Alps, D<strong>in</strong>arides and <strong>Pannonian</strong> Bas<strong>in</strong> 

(Hrvatsko zagorje and Karlovac Bas<strong>in</strong>s, Croatia). International 

Journal of Earth Sciences 90, 560–578. 

Újszászi, K., Vakarcs, G., 1993. Sequence stratigraphic analysis <strong>in</strong> <strong>the</strong> 

South Transdanubian region, Hungary. Geophysical Transactions 

38, 69–87. 

Vail, P.R., Mitchum, R.M., Thomson III, S., 1977. Seismic 

stratigraphy and global changes of sea level. In: Payton, C.W. 

(Ed.), Seismic Stratigraphy Applications to Hydrocarbon Exploration. 

American Association of Petroleum Geologists Memoir, 

vol. 26. American Association of Petroleum Geologists, Tulsa, 


Vail, P.R., Audemard, F., Boweman, S.A., Eisner, P.N., Perez-Criz, C., 

1991. <strong>The</strong> stratigraphic signatures of tectonics, eustacy and 

sedimentology — an overview. In: E<strong>in</strong>sele, G., Ricken, W., 

Seilachter, T. (Eds.), Cycles and Events <strong>in</strong> Stratigraphy. Spr<strong>in</strong>ger– 

Verlag, Berl<strong>in</strong>, Germany, pp. 617–659. 

Vakarcs, G., 1997. Sequence stratigraphy of <strong>the</strong> Cenozoic <strong>Pannonian</strong> 

Bas<strong>in</strong>, Hungary. PhD. <strong>The</strong>sis, Rice University, Houston, TX. 

Vakarcs, G., Vail, P.R., Tari, G., Pogácsás, G., Mattick, R.E., Szabó, A., 

1994. Third-order Miocene–Pliocene depositional sequences <strong>in</strong> <strong>the</strong> 

prograd<strong>in</strong>g delta complex of <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. Tectonophysics 

240, 81–106. 

Vakarcs, G., Hardenbol, J., Abreu, V.S., Vail, P.R., Várnai, P., Tari, G., 

1998. Oligocene–middle Miocene depositional sequences of <strong>the</strong> 

central paratethys and <strong>the</strong>ir correlation with regional stages. In: de 

Graciansky, P.-C., Hardenbol, J., Jacqu<strong>in</strong>, T., Vail, P.R. (Eds.), 

Mesozoic and Cenozoic Sequence Stratigraphy of European 

Bas<strong>in</strong>s. SEPM (Society for Sedimentary Geology) Special 

Publication, vol. 60. Society for Sedimentary Geology, Tulsa, 


Van Balen, R.T., Lenkey, L., Horváth, F., Cloet<strong>in</strong>gh, S.A.P.L., 1999. 

Two-dimensional model<strong>in</strong>g of stratigraphy and compaction-driven 

fluid flow <strong>in</strong> <strong>the</strong> <strong>Pannonian</strong> Bas<strong>in</strong>. In: Durand, B., Jolivet, L., 

Horváth, F., Séranne, M. (Eds.), <strong>The</strong> Mediterranean Bas<strong>in</strong>s: 

Tertiary Extension with<strong>in</strong> <strong>the</strong> Alp<strong>in</strong>e Orogen. Geol. Soc. Spec. 

Pub., vol. 156. <strong>The</strong> Geological Society, London, United K<strong>in</strong>gdom, 

pp. 391–414. 

Vasiliev, I., Krijgsman, W., Stoica, M., Langereis, C.G., 2004. Mio- 

Pliocene magnetostratigraphy <strong>in</strong> <strong>the</strong> sou<strong>the</strong>rn Carpathian foredeep 

and Mediterranean–Paratethys correlations. Terra Nova 17, 376–384. 

Vidal, L., Bickert, T., Wefer, G., Röhl, U., 2002. Late Miocene stable 

isotope stratigraphy of SE Atlantic ODP Site 1085: relation to 

<strong>Mess<strong>in</strong>ian</strong> events. Mar<strong>in</strong>e Geology 180, 71–85. 

Warny, S.A., Wrenn, J.H., 2002. Upper Neogene d<strong>in</strong>oflagellate cyst 

ecostratigraphy of <strong>the</strong> Atlantic coast of Morocco. Micropaleontology 

48, 257–272. 

Warny, S.A., Bart, P.J., Suc, J.-P., 2003. Tim<strong>in</strong>g and progression of 

climatic, tectonic and glacioeustatic <strong>in</strong>fluences on <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> 

sal<strong>in</strong>ity crisis. Palaeo<strong>geo</strong>graphy, Palaeoclimatology, Palaeoecology 

202, 59–66. 

Whittle, G.L., 1993. Us<strong>in</strong>g computer model<strong>in</strong>g to <strong>in</strong>vestigate <strong>the</strong> 

controls on platform and marg<strong>in</strong> sedimentary <strong>geo</strong>metries. PhD 

Dissertation, University of South Carol<strong>in</strong>a, Columbia, SC.

The Messinian problem in the Pannonian Basin ... - geo.edu.ro

You also want an ePaper? Increase the reach of your titles

Delete template?

Save as template?