Messinian Sea Level Fall in the Dacic Basin (Eastern Paratethys Palaeogeographical Implications From...

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Messinian sea level fall in the Dacic Basin (Eastern Paratethys):

palaeogeographical implications from seismic sequencestratigraphy

Karen A. Leever,1,3 Liviu Matenco,1,3 Traian Rabagia,1,3 Sierd Cloetingh,1,3 Wout Krijgsman2,3 and

Marius Stoica2,3

1Faculty of Earth and Life Sciences, VU University Amsterdam, De Boelelaan 1085, 1081 HV Amsterdam, The Netherlands; 2Department of

Earth Sciences, Utrecht University, Budapestlaan 17, 3584 CD Utrecht, The Netherlands; 3ISES (Netherlands Research Centre for Integrated

Solid Earth Science)

Introduction

Patterns of basin infill are a functionof changes in accommodation space(rates of eustatic sea level change and

subsidence) and sediment supply (e.g.Galloway, 1989; Schlager, 1993). Bothare ultimately controlled by the inter-action of tectonics and climate. A

dramatic example of this interactionoccurred in the Mediterranean Seaduring the Messinian Salinity Crisis(MSC, 5.96 to 5.33 Ma; Krijgsman

et al., 1999 and references therein;Fig. 1): its disconnection from theAtlantic Ocean led to a sea level fall

of more than 1000 m (Clauzon, 1978;Savoye and Piper, 1991). This causedextensive erosion of the basin marginsand deposition of thick evaporites in

its centre, and influenced the tectonicevolution of the neighbouring orogens

and basin margins (e.g. Gorini et al.,2005; Willett et al., 2006; Govers

et al., 2009). The MSC low-standabruptly ended with the Zancleanflooding of the Mediterranean basinthrough the Strait of Gibraltar (Blanc,

2002; Loget and Van Den Driessche,2006).

During the Messinian, the Mediter-ranean Sea was flanked to the north

by Paratethys, a generally shallowepicontinental sea that had formed asa remnant of the closing Tethys Oceansince the Oligocene (Fig. 2a). In the

course of its evolution, Paratethysfragmented in various semi-isolatedsubdomains that gradually lost salin-ity, resulting in the development ofbrackish to fresh-water environments,

their faunas recording periodic isola-tion from or connection with the mainCentral or Eastern Paratethys realm.The characteristic endemic faunas led

to the definition of separate Neogenebiostratigraphies for each basin (e.g.Ro gl, 1996) and resulted in largeuncertainties in the correlations oflocal stages, especially between the

Central and Eastern Paratethys(Fig. 1).

The observation of Messinian faunaof Paratethyan affinity in Mediterra-

nean deposits (Lago Mare facies;Ruggieri, 1967) incited the scientificinterest in the physical connectionbetween the two realms during the

MSC and the signature of the MSC inthe Paratethys. Base level falls inParatethys have been repeatedly

attributed to the MSC, in the Panno-

nian Basin (Csato et al., 2007), the

Black Sea (Hsu and Giovanoli, 1979;Gillet et al., 2007) and its westernappendix, the Dacic Basin (e.g. Clau-zon et al., 2005; Stoica et al., 2007).

Previous studies addressing the

expression of the MediterraneanMSC in the Dacic Basin either pro-posed a direct connection to the Medi-terranean (Clauzon et al., 2005) or

influence on base level through theBlack Sea (Gillet et al., 2007). Thewestern Dacic Basin was thought tobe desiccated except for a remnant

lake on the northern margin (Clauzonet al., 2005; Gillet et al., 2007). Inthis paper, we use seismic sequence

stratigraphy supported by bio- andmagnetostratigraphic data, giving dif-ferent constraints on the palaeo-

geographical evolution of the westernDacic Basin during the major sea level

changes of the Messinian SalinityCrisis.

The Dacic Basin within theParatethys realm

The Dacic Basin (Fig. 2) developed inthe foreland of the South Carpathiansafter the Carpathian collision(c. 11 Ma, Matenco and Bertotti,

2000; Stoica et al., 2007). Part ofEastern Paratethys, it was separated

ABS T R ACT

The signature of the Mediterranean Messinian Salinity Crisis(MSC) in the Paratethys has received wide attention because ofthe inferred changes in connectivity and base level. In this

article, we present sequence stratigraphic interpretations on aseismic transect across the western part of the semi-isolatedLate MiocenePliocene Dacic Basin (Eastern Paratethys, Roma-nia), chronologically constrained by biostratigraphic field

observations and well data. They reveal significant sea levelchanges during the middle Pontian that are coeval with theMSC. These changes were most likely transmitted to the

western Dacic Basin from the downstream Black Sea andcontrolled by the sill height of the interconnecting gateway.During the middle Pontian lowstand of the western Dacian

Basin, sedimentation continued in a remnant300 m deep lakewith a positive water balance. Our observations show that theevolution of semi-isolated sedimentary basins is stronglydependent on the communication with other depositional

realms through its control on base level and sediment supply.

Terra Nova, 22, 1217, 2010

Correspondence: Karen A. Leever, Univer-

sity of Oslo, Department of Geosciences,

P.O. Box 1047, Blindern N-0316 Oslo,

Norway. Tel.: +47 228 55779; Fax: +47

228 54215; e-mail: [email protected]

12

2009 Blackwell Publishing Ltd

doi: 10.1111/j.1365-3121.2009.00910.x


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from the Central Paratethys (Panno-nian and Transylvanian basins) by the

uplifting Carpathian mountain chainduring the Middle early Late Mio-cene (e.g. Sanders et al., 1999). It hasbeen argued that the present connec-

tion between the two realms, theDanube river crossing the South Car-pathians at the Iron Gates (Fig. 2b),was established during the MSC

(Clauzon et al., 2005). The Miocene

connection between the brackish Dacicbasin and the much larger Black Sea is

proven by the common Eastern Parat-ethys fauna (e.g. Popov et al., 2006and references therein). The basinswere linked by a narrow corridor north

of Dobrogea herewith defined as the

Scythian gateway (Fig. 2a). There,the sedimentation is interrupted by aLower Middle Pontian unconformity

(Saulea et al., 1969).Integrated magneto-biostratigraphic

dating of long and continuous sedi-mentary successions in the east and

south Carpathian foredeep recentlyestablished a detailed chronology forthe Mio-Pliocene Dacic Basin, resol-ving uncertainties in the absolute ages

of local stages (Fig. 1; Vasiliev et al.,2004, 2005). This new time scaleshows that the acme of the MSC

corresponds to the middle Pontian(Portaferrian) substage. The Plioceneflooding of the Mediterranean at5.33 Ma roughly coincides with theMiddleUpper Pontian (Portaferrian

Bosphorian) boundary, rather thanwith the previously assumed Pontian

Dacian boundary (Ro gl, 1996) or theuppermost part of the Bosphorian

(Clauzon et al., 2005).A sequence stratigraphic study of

the uppermost MiocenePliocene sed-

iments of the Dacic basin is favouredby the period of relative tectonicquiescence which characterized thistime interval. Recent detailed struc-

tural and tectonic studies (e.g. Mat-enco et al., 2003, 2007; Tarapoancaet al., 2003 and references therein)have demonstrated that the periodbetween 11 Ma and the onset of the

Quaternary is characterized only byconstant and reduced subsidence, gen-erally related to the pull exerted by theVrancea slab in the SE Carpathians

corner.

Upper Miocene to Recent

sedimentary architectureA series of 2D industry seismic reflec-

tion profiles (largely unpublished ex-cept Matresu, 2004; Rabagia andMatenco, 1999) were combined intoa > 200 km cross section across the

central-western part of the DacicBasin, correlating sedimentologicaland biostratigraphical features de-scribed in wells and outcrops nearthe basin margins (Leever, 2007;

Stoica et al., 2007 and references

therein) with the subsurface geometryof the Upper MiocenePliocene sedi-

ments. The interpretation was corrob-orated by additional seismic lines andwell data (see also supplement andLeever, 2007).

In the shallow part of the basin, two

seismic sequences, separated by amajor unconformity (SB2), were dis-tinguished in the post-orogenic sedi-

ments of the Dacic Basin (Fig. 3 andFig. S1). These sequences are Meotian

Lower Pontian (SSQ1) and MiddlePontian Dacian (SSQ2) in age and

are characterized by well-developedclinoforms, arranged into progradingbodies progressively filling the basinaccommodation space. Based on the

depositional shelf edge trajectory (sen-su Galloway, 1989), the sequenceswere subdivided into mainly progra-

dational (LST1, LST2) and prograda-tional-aggradational units (HST1).These geometric units were inter-preted in terms of composite strati-graphic base level fluctuations,

describing changes in accommodationat the shoreline (e.g. Catuneanu,2006): the progradational units weredeposited during periods of falling

and low base level (LST1, LST2), theprogradational-aggradational oneduring rising and high base level

(HST1).In front of HST1, a forced regres-

sive prism is recognized (indicated by

P on the inset in Fig. 3), the deposi-

tion of which is associated with ero-sion of HST1 and onto which LST2 isonlapping. This onlap may be as aresult of a change in source areaarising from the base level fall which

defined the sequence boundary be-tween SSQ1 and SSQ2 (SB2). SB2was an erosional surface during thedeposition of the forced regressive

prism and a sediment bypass surfacewith probably some erosion duringdeposition of LST2. The base level fallassociated with SB2 is roughly esti-

mated at 100 m, based on the eleva-tion difference between the inferredshorelines above and below the se-quence boundary (at >190 km and154 km respectively for HST1 and

LST2; Fig. 3 and Fig. S1), taking intoaccount the differential compactionacross the Getic fault (Fig. 3). A moreaccurate estimate would require depth

conversion and restoration of thesection, along with better constraintson the nature of the topsets of HST1

4

5

6

7

8

sl

- +

?

Piac.

M

essinian

Zanclean

Tortonian

MSC

Time(Ma)

Steiningere

ta

l.,

1988

Sacc

hie

ta

l.,

1999

Csa

toe

ta

l.,

2007

Continental

sed

imentation

SSQ1

LST2

HST1

TST2

SSQ2

Intra-Messinian

unconformity

Vas

ilieve

ta

l.,

2004

,2005

Stoicae

ta

l.,

unpu

blis

he

dda

ta

R

+

D

P

Pn

R

D

P

M

CentralParatethys

Eastern Paratethys /Dacic Basin

SB2

HST2

Fig. 1 Correlation chart for the Centraland Eastern Paratethys (Pannonian

Dacic Basin), showing differences in

the absolute age of the Pontian stage

and relative sea level change in the Dacic

Basin. Pn, Pannonian; M, Meotian; P,Pontian; D, Dacian; R, Romanian. Da-

cian and Romanian substages in the

Pannonian basin cannot be separated at

present at the precision required by this

figure because of the mostly continental

sedimentation and are therefore com-

bined (R+D) in the Central Paratethys

timescale. Note that the Pontian stage is

furthermore separated in Odessian

(Lower), Portaferian (Middle) and Bos-

phorian (Upper). Mediterranean MSC

lowstand sensu Krijgsman et al. (1999)

(5.65.33 Ma) is highlighted.

Terra Nova, Vol 22, No. 1, 1217 K. A. Leever et al. Messinian sea level fall in the Dacic Basin

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2009 Blackwell Publishing Ltd 13


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to determine properly the position ofthe shoreline at that time.

LST2 is restricted to the centre ofthe basin (see Fig. 2b for the evolutionof the lake extent during this time)and characterized by a very flat shelf

edge trajectory, toplap terminationsand clinoform heights of ca 300 ms.

Overlying all of the previous depositsand extending to the edges of the

section is a unit (TST2) characterizedby small clinoforms near the basinmargins (part h in Fig. 3 and Fig. S1)and seismic transparency in the centre

(Fig. 3, inset). This seismically trans-parent part of TST2 is considered a

condensed interval of distal bottom-sets associated with the clinoforms

near the basin margins, in agreementwith the distal facies observed in welllogs (Fig. S2). According to the defi-nition of the genetic unit in Catu-

neanu (2006), the maximum flooding

surface separating TST and HSTshould be expected somewhere in themiddle of the transparent unit. The

reflection we picked for reasons ofmappability is a lithological transitionrather than a systems tract boundary.HST2 represents the regressive stage

of complete basin fill during theDacian-Quaternary consisting ofsandstones and lignites deposited in alimnic environment (Popescu et al.,

2006). These could be considered aseparate unit, but the transitionfrom HST2 is not resolved in our

seismic data being so close to thesurface.

Control on the Mio-Pliocenesequences: palaeogeographicalsetting

The observed base level changes maybe as a result of local or regionalcontrol. We will argue for the latterand discuss the independent con-

straints derived from the geometry ofthe sediments (determined by theinterplay of sealake level change,tectonics and supply) and from age

correlations.The key criterion to indicate control

of (relative) sea level rather than

sediment supply on sedimentary archi-tecture (sensu Galloway, 1989) is sub-aerial exposure of marine sediments atthe sequence boundary (Schlager,1993). In the Dacic Basin, surrounded

on all sides by elevated topography,the supply was generally high through-out the entire Mio-Pliocene interval.This is best expressed by the architec-

ture of sequence SSQ1, lacking a cleartransgressive systems tract because

rates of rise post-dating LST1 neveroutpaced sedimentation rates (e.g.Catuneanu, 2006): HST1 on the

northern basin margin is both aggrad-ing and prograding into the basin. Themain evidence for subaerial exposureof the shelf is the truncation of HST1,

which favours an accommodationcontrol on depositional geometries.The sediments of both HST1 andTST2HST2 reach the basin margin

at the northern end of the section

(a)

(b)

Fig. 2 Location maps. (a) Messinian palaeogeography of the Mediterranean andParatethys just before the Messinian Salinity Crisis (modified from Popov et al.,

2006) showing the Dacic Basin (DB) in relation to the Carpathians and other

Paratethys sub-basins. (b) Location of interpreted seismic lines and wells in the

western part of the Dacic Basin. Dashed lines within the remnant lake indicate

the decreasing deep basin area due to the progressive infilling of the basin during the

Middle Pontian lowstand (LST2). Extent of eastern lake from Clauzon et al. (2005).

Messinian sea level fall in the Dacic Basin K. A. Leever et al. Terra Nova, Vol 22, No. 1, 1217

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(Fig. 3), overstepping the footwallblock of the Getic Fault: the accom-

modation space for these units isunrelated to fault motions. Therefore,the observed sedimentary architectureis most likely controlled by absolute

changes in the water level.

These changes may either reflectvariations in the local water budgetof the isolated basin, or regional (i.e.

also affecting the surrounding Parate-thys basins) changes in sea level. Thewater level changes in lakes and semi-isolated basins are in contrast to

those in the open sea a function ofthe hydrological balance in the drain-age area and supply and accommoda-tion are therefore intimately linked: a

dry climate would lead to a lower lakelevel and at the same time reducedsedimentation rates (e.g. Garcia-

Castellanos, 2006). Within the limita-tions of the 2D data, a decrease insedimentation rates is not evidentconsidering the relatively short timeavailable for the deposition of LST2

(Figs 1 and 3). Also, the overall lowsalinity in the Dacic Basin (e.g.Marinescu et al., 1981) points at apositive water balance, suggesting

regional, rather than local, controlon the base level.

Arguments for regional control on

the base level are additionally pro-vided by age correlations with eventsin other Paratethys basins and theMediterranean (Figs. 1 and 2). The

Gilbert fan delta described atthe Danube outlet of the Iron Gatesas a Pliocene transgression followingthe Messinian desiccation of the Dacic

Basin (Fig. 3; Clauzon et al., 2005)could be correlated in our seismic lineswith either the upper part of TST2 orwith HST2, which, according to our

well data (Fig. S1), together comprisesthe time interval of Upper PontianDacian (i.e. Pliocene; Vasiliev et al.,2005; Fig. 1). The SB2 unconformitycan be traced to the northern basin

margin, where Stoica et al. (2007)determined its age between Meotianand Upper Pontian times. The MiddlePontian base level drop in the Dacic

basin (LST2) is coeval with the largesea level drop reaching the deep partsof the Black Sea (Gillet et al., 2007),and with the low-stand of the Medi-terranean during the MSC (Fig. 1).

We propose the following model forthe Pontian base-level evolution of theDacic Basin. Once the sea level ofFi

g.

3

Sequencestratigraphicinter

pretationofaseismicsectionextendingfromthewesterntothenorthernmarginofthewesternDacicBasin(locationinFig.2b).Surfacedatain

thewesternmostareafromClauzo

net

al.

(2005).SeismicdataandmoredetaileddescriptioninSupplement(Fig.S1).Notetheveryflatshelfedgetrajectoryo

fLST2,restrictedto

thecentreofthesection,whileTS

T2extendstotheedgeofthesection,to

thebasinmargins.Inset:Seismicdetail

ofSB2.


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the Black Sea had dropped below theScythian gateway, it no longer exerted

any control on the base level in theDacic Basin (e.g. Garcia-Castellanos,2006; Fig. 4). The Dacic lake levelremained largely constant in the mid-

dle Pontian because of a positivewater balance, modified only by ero-sional lowering of the outlet to theBlack Sea. This explains the extended

period of constant to slowly fallingbase level during the deposition ofLST2, corresponding to a maximumwater depth of300 m derived from

the height of the clinoforms. Some-what speculatively, sediment supplywas probably strongly influenced bythe connection with the upstream

Pannonian Basin through the IronGates. The intra-Messinian unconfor-mity of the Pannonian Basin (Csato

et al., 2007) correlates with LST2(Fig. 1), which suggests that the cor-responding Pannonian water level fallmay have been in response to the baselevel lowering in the Dacic Basin (see

also Tari et al., 1992; Leever et al.,submitted). The re-establishment ofthe connection between basins wasprobably driven by the sea-level rise in

the larger Black Sea realm over theheight of the Scythian gateway.

Conclusions

Seismic sequence stratigraphic inter-pretation is shown to be an importantadditional tool in constraining palaeo-geographical evolution. Our study

confirmed that the effects of the Mes-sinian Salinity Crisis extended intoParatethys at least as far as into thewestern part of the Dacic basin, where

a major sea level fall was observed inthe Middle Pontian. The response ofthe Dacic basin to downstream sealevel changes was controlled by the sill

level of the gateway to the Black Sea.Once disconnected, the base level in

the Dacic basin was determined by itslocal hydrological balance. Connec-tivity with both the downstream BlackSea and the upstream Pannonian

basin is identified as the key factorinfluencing the Pontian sedimentaryarchitecture in the Dacic Basin respec-tively controlling base level and sedi-

ment supply.

Acknowledgements

The authors are indebted to RomanianNational Agency for Mineral Resources,

Petrom SA and Sterling Resources (UK)

LTD for providing and allowing publi-

cation of the seismic and well data. Thework is part of KALs PhD thesis, funded

by and carried out in the framework of

ISES. Critical comments by J.P. Suc, M.

Rabineau and three anonymous reviewershelped to improve the manuscript.

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Received 9 April 2009; revised version

accepted 1 October 2009

Supporting Information

Additional Supporting Information

may be found in the online versionof this article:

Figure S1 Seismic sequence strati-graphy.

Figure S2 Seismic facies and welllog.

Please note: Wiley-Blackwell arenot responsible for the content orfunctionality of any supporting mate-

rials supplied by the authors. Any

queries (other than missing material)should be directed to the correspond-ing author for the article.


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