Cretaceous biostratigraphy and lithostratigraphy of the Glinzendorf Syncline based on well Gänserndorf UeT3 (Vienna Basin, Austria)

The 2200 m thick Cretaceous units of well Gänserndorf UeT3 have been biostratigraphically analyzed based on cuttings from 3210 m to 5140 m. The deposits from the Tirolic Glinzendorf Syncline (a part of the buried Northern Calcareous Alps) can be largely correlated with the Lower Gosau Subgroup of the Grünbach Syncline. An exception is the basal unit, which has no equivalent in the Grünbach Syncline. This lower unit is subdivided into a non-marine lower and a largely marine upper part. No age constraints are available for the lower part, whereas the upper part has a possible age range from middle Turonian to Coniacian. For this unit, which is documented for the first time from the Glinzendorf Syncline, we propose Glinzendorf Formation as new lithostratigraphic term. The Glinzendorf Fm. is overlain by the Grünbach Fm., which is intercalated by a thick unit of conglomerates. These are interpreted as equivalents of the Dreistetten Conglomerate Mb. The calcareous nannofossils of these units suggest a latest Santonian to early Campanian age. Non-marine conditions prevailed during deposition of the Grünbach Fm., but marine incursions are indicated for parts of the Dreistetten Conglomerate Mb. The top of the Grünbach Fm. is formed by an about 50-m-thick unit of coal, rich in Characeae oogonia, which, together with the Dreistetten conglomerates serve as marker layer for correlation with the outcrops in the Grünbach Syncline. The Grünbach Fm. is overlain by marls and silty shales of the Piesting Fm. for which a late Campanian and Maastrichtian age is documented. Marine conditions predominated during this interval. The topmost unit in well Gänserndorf UeT3 is overthrusted on the Maastrichtian Piesting Fm. and represents Campanian sandstones and conglomerates of the Grünbach Fm. This Gänserndorf Thrust is detected and biostratigraphically constrained for the first time.


Introduction
The Glinzendorf Syncline is an about 70 km long and up to 8 km wide, SW-NE trending structure in the Vienna Basin, which was briefly described by Wessely (1984;1992) and Hamilton et al. (1990).It is part of the Tirolic nappe system and reaches from Himberg in Austria in the SE to Jakubov, Gajary and Záhorská Ves in Slovakia in the NE (Wessely et al., 1993;Ralbovský and Ostrolucký, 1996) (Fig. 1).The structure is completely covered by Neogene deposits.
The Glinzendorf Syncline is part of a series of surface and subsurface outcrops of the Cretaceous to Paleogene Gosau Group, which range from the Gießhübl and Grünbach-Neue Welt outcrops along the southwestern margin of the Vienna Basin to the Brezová and Myjava region in Slovakia in the Western Carpathians (Plöchinger et al., 1961;Schlagintweit and Wagreich, 1992;Wagreich and Marschalko, 1995;Hofer et al., 2013) (Fig. 1).These occurrences are linked by subsurface outcrops, such as the Gießhübl and Glinzendorf synclines and the Prottes and Studienka Gosau (Wessely, 1992;1993;2006;Hofer et al., 2013 and literature therein).According to Wessely et al. (1993), the Glinzendorf Syncline might continue into the Grünbach Syncline in the SE, but this was doubted by Hofer et al. (2013).

Limitations
Using cuttings for calcareous nannoplankton biostratigraphy has several limitations.Down-core contamination frequently occurs and only in obvious cases (e.g., Miocene taxa in Cretaceous samples), this contamination can be reliably identified and excluded.In addition, reworking of stratigraphically older nannofossils from underlaying strata during deposition of younger strata is a process, which causes dilution of the autochthonous signal at varying amplitudes.Therefore, in the following we indicate the potential biostratigraphic range for each sample.Overlaps of these ranges are used to derive a most likely biostratigraphic zonation of the well but we emphasize that this method necessarily implies considerable uncertainties especially in detecting exact boundaries.

Lithology
The Cretaceous deposits of the Glinzendorf Syncline rest uncomfortably on Jurassic units (Wessely, 1992;2006 and own data OMV).The upper Jurassic Ruhpolding Fm. forms the basement of the Cretaceous strata in Gänserndorf UeT3 (OMV data).The Cretaceous of the Glinzendorf Syncline comprises an about 2000 m thick package, which can be separated from top to base into seven units based on lithologies and wire log patterns (Fig. 2).Note that all thicknesses are based only on drilling depth in Gänserndorf UeT3 and do not represent true thicknesses.
Unit 1 (3210-3550 m) is a 340-m-thick succession.Silty shales, sandstones and rare conglomerates predominate the lower part.Foraminifers (Goupillaudina sp.) have been recorded in this lower part from cuttings at 3510 m, 3520 m, 3540 m and 3550 m (Fig. 3).Marls and silty shales with two subordinate coal layers occur in the upper part of unit 1. Characeae oogonia appear at 3370 m.SP and RES logs show high frequency and high amplitude serrations forming two coarsening upwards sequences.
Unit 2 (3550-3970 m) is a 420 m thick succession of marls and shales with rare intercalations of sandstones.Its base is formed by a thin sandstone bed containing foraminifers (Goupillaudina sp.) (3930 m), another thin sandstone intercalation with Goupillaudina occurs at 3700 m.SP-and RES-logs are characterized by low amplitude shale line patterns interrupted by few peaks correlated with sandstone layers.Only the upper part displays some low amplitude serrations.
Unit 3 (3970-4020 m) forms a 50 m thick bed of coal and coaly limestones with numerous Characeae oogonia.This unit serves as marker horizon for OMV-cross-correlation with other wells in the Glinzendorf Syncline and is indicated by a shale-line wire log pattern.
Unit 4 (4020-4250 m) is an about 230 m thick sequence of conglomerates, which are rich in exotic volcanogenic components, such as quartz porphyry in a reddish matrix (see also Wessely, 1992;2006).In wire logs, this unit is marked by very high, moderately serrated RES-values accompanied by very low, shale-line SP-values.
of the conglomerates and identified a southern source in the Juvavicum.An undifferentiated Senonian age (= Coniacian to Campanian and possibly also Maastrichtian) was proposed by Mišík (1994) for Ga-125. Hofer et al. (2013) performed geochemical analyses on some samples from the wells Glinzendorf T3 and Markgrafneusiedl T1, to distinguish marine and limnic successions and Stern and Wagreich (2013) provided data on heavy mineral distribution from samples from wells Markgrafneusiedl T1 and Glinzendorf T1.Hofer et al. (2013) and Stern and Wagreich (2013) assumed a Santonian to Campanian or even Maastrichtian age for the analyzed deposits, based on unpublished sources.Pavlishina et al. (2004) indicated an early to middle Campanian age based on palynology from well Markgrafneusiedl T1.A Coniacian to Santonian age was stated by Wessely (1992) for the northernmost Austrian part of the Glinzendorf Syncline for grey marls of well Heidenberg 1 based on unpublished OMV reports.For the main part of Glinzendorf Syncline, Wessely (1992;2006) proposed a Santonian to Maastrichtian age based on unpublished spores and pollen data.In addition, Wessely (1992) mentioned unpublished globotruncanid foraminifers and calcareous nannoplankton, which might support this correlation.For the upper units in Gänserndorf UeT3, Wessely (1992;2006) mentioned Maastrichtian globotruncanid foraminifers, but did not provide identifications or illustrations.Interestingly, Mišík (1994) emphasized the absence of Globotruncanidae and Orbitoididae from the coeval deposits of the well Gajary 125 well in Slovakia.Similarly, we have not been able to detect Globotruncanidae in our samples from Gänserndorf UeT3.
Concluding, for none of the wells drilling the Glinzendorf Syncline, a reliably and comprehensible biostratigraphy has been published so far.

Material and methods
To clarify the stratigraphy of the Gänserndorf UeT3 well (48°18'18.4764''N, 16°43'41.4038''E, drilled 1985-1987), OMV provided cutting samples from 3210 m to 5140 m for biostratigraphic analysis.Each of the 97 analyzed samples was treated for few seconds in an ultrasonic bath.Afterwards smear slides were made drying few drops of suspension on the object glass and fixed using Canada balsam.All smear slides were investigated with a Leica microscope with 1000 magnification.UCzones were applied for Cretaceous samples as defined by Burnett (1998).In total thirty-three samples were barren of calcareous nannofossils.Ranges of calcareous nannoplankton species follow https://www.mikrotax.org/Nannotax3/index.html and references therein.In addition, wire log data (SP, RES) have been provided by OMV.Data on the lithology was derived in 2020 from thin section analysis of cuttings by A.V. with a resolution of 10 m, including information of the occurrence of Characeae oogonia and larger foraminifers (Fig. 2).The list of nannofossil taxa detected in the investigates samples in provided in Table 1 (note that downfall is not listed).
as allochthonous intercalation and is overlain by conglomerates and silty shales.In wire logs, the lower unit is characterized by a funnel shaped to cylindrical SP-log with low amplitudes and a RES-log with serrated, positive excursions indicating coarse, conglomeratic units.
Unit 7 (4830-5140 m) consists of a 310-m-thick succession of marls with two intercalations of coal in its basal half.Wire logs are characterized by a cylindrical, low amplitude SP-log and a shale-line RES-log.
Unit 5 (4250-4550 m) is an about 300 m thick fining upwards unit starting with basal conglomerates and sandstones passing into silty shales and shales with rare intercalations of coal.In wire logs, the succession is characterized by a funnel shaped to cylindrical SPlog with moderately high amplitudes and a RES-log of generally low variation interrupted by a marked positive excursion indicating basal conglomerates.Rare orbitoid foraminifers occur at 4300 m.
Unit 6 (4550-4830 m) consist of a 280-m-thick succession of grey to greenish grey and violet-brownish silty shales with conglomerates in its basal parts.Anhydrite is drilled between 4630 m and 4670 m.This anhydrite is interpreted strata and the rich and diverse Miocene assemblages dilute the comparatively scarce autochthonous material.Without information from seismics, it would be difficult to decide whether the Cretaceous taxa are autochthonous or reworked.All samples below m are clearly of pre-Neogene age and lack the high amount of downfall.Rare occurrences of Miocene taxa in samples 3910 m, 4590 m, 4710 m and 4890 m are obviously results of downhole contaminations.
The nannoplankton assemblages of the Gänserndorf UeT3 well allow a separation eight zones: Zone 1 (3210-3370 m) is covered by nine samples.All samples contain moderately to well preserved autochthonous assemblages, which however are

Biostratigraphy
In total, 104 species-level taxa of calcareous nannoplankton have been detected in the samples.Of these, only 50 taxa are autochthonous.Of the remaining taxa, one might be reworked from Jurassic strata (Triscutum?sp.).The ubiquitous Watznaueria barnesiae might also be partly reworked from older strata in many samples (Figs 4,5).All other species represent downfall comprising Paleogene and Neogene taxa.These Paleogene taxa have been reworked into Neogene deposits and are part of the downfall from the Neogene because no Paleogene strata rest on the Cretaceous of the Glinzendorf Syncline.Therefore, the assemblages of the samples down to 3690 m are extremely distorted by downfall from Neogene  Deflandre and Fert, 1954) Bramlette and Martini, 1964   Zone 3 (3570-3750 m) is covered by ten samples of which only two are barren (3650 m, 3690 m).The calcareous nannoplankton assemblages comprise rare, moderately preserved specimens, suggesting restricted marine conditions.A Maastrichtian age is indicated by the presence of Russellia bukryi (UC17-UC20) in samples 3570 m and 3750 m (Fig. 4) and by the occurrence of Micula murus (UC20) in sample 3610 m (Burnett, 1998;Lees and Bown, 2005) (Fig. 5).
Zone 4 (3770-3950 m) is covered by 10 samples with rare and moderately preserved calcareous nannoplankton.A biostratigraphically important species is Eiffelithus eximinus, which has its last occurrence in the Calcareous Nanoplankton Zone UC15 (Burnett, 1998) and occurs in samples 3770 m, 3850 m, 3890 m, 3930 m and 3950 m.In addition, the occurrence of Zeugrhabdotus blowii (LOD UC16), which does not pass the Campanian/Maastrichtian boundary, points to a Campanian age of the samples up to 3770 m (Burnett, 1998;Lees, 2007) (Fig. 5).The lower boundary is set by the occurrence of Arkhangelskiella cymbiformis (UC13-UC20) and Reinhardites levis (UC14d-UC18), resulting in a late Campanian age for this wellinterval (Burnett, 1998).Marine conditions seem to have prevailed, although quality and quantity of the assemblages suggest that conditions were not ideal for calcareous nannoplankton.
Zone 5 (3970-4210) is covered by 13 samples, of which three were barren of nannofossils.Most of the other samples contained extremely rare and moderately to well preserved calcareous nannoplankton.Plant debris is frequent in all samples.The nannoplankton assemblages of this sequence gave a rather wide stratigraphic range.Micula staurophora and Micula swastica (Fig. 4) have a Coniacian to Maastrichtian range (samples 3990 m, 4090 m, 4130 m) (Burnett, 1998;Lees and Bown, 2005), which can be slightly narrowed down to the Santonian to Maastrichtian, based on the occurrence of Lucianorhabdus cayeuxii in sample 4190 m (Burnett, 1998).Only the presence of Uniplanarius sissinghii in sample 4070 m (Fig. 4), narrows the range even further down to Campanian to lower Maastrichtian (UC15-UC19) (Burnett, 1998) (Fig. 5).Therefore, we suppose a Campanian age as most likely solution.The low diversity and scarceness of nannofossils might be related to a very shallow, coastal marine depositional environment, which was unsuitable for calcareous nannoplankton.Overall, however, marine conditions seem to have been established during most of the deposition of this zone.
Zone 6 (4230-4550 m) is characterized by its poor nannoplankton content.Eleven out of 17 samples from this zone were barren of nannofossils and two yielded only rare Watznaueria barnesiae, which might have been reworked even from Jurassic strata.The potentially autochthonous assemblages of this interval from samples 4310 m, 4370 m and 4550 m are very poor and nannofossils are extremely rare.The presence of Uniplanarius sissinghii in sample 4310 m suggests a Campanian age (Burnett, 1998).The maximum age is set strongly diluted by Neogene downfall.Arkhangelskiella cymbiformis and Micula staurophora are frequent in these samples (Figs 4,5).Three samples (3250 m, 3290 m, 3370 m) contain Broinsonia parca parca (Fig. 4), which is indicative for the Calcareous nanoplankton Zones UC14-15d (Burnett, 1998) and suggests a Campanian age (Fig. 5).This age assignment is supported by the occurrence of Eiffelithus eximinus in sample 3330, which has its last occurrence in the Calcareous Nanoplankton Zone UC15e (Burnett, 1998).The constant occurrence of autochthonous nannoplankton points to prevailing marine conditions.
Zone 2 (3390-3550 m) is covered by eight samples, of which six are barren of nannofossils.Only samples 3410 m and 3430 m yield poor assemblages with the Campanian to Maastrichtian Arkhangelskiella cymbiformis and Micula staurophora (Burnett, 1998;Lees and Bown, 2005).The lack of autochthonous calcareous nannoplankton suggests prevailing non-marine conditions.Turonian and Coniacian.Coastal marine conditions, which were not ideal for calcareous nannoplankton seem to have prevailed, interrupted by repeated non-marine phases, reflected by barren samples.
Zone 8 (5030-5140 m) is covered only by three samples, which contain extremely rare and poorly preserved nannofossils.Watznaueria barnesiae in samples 5130 m and 5140 m has an enormous stratigraphic range from the Bathonian to the Maastrichtian (Mattioli and Erba, 1999;Lees and Bown, 2005) and might be reworked.The Jurassic ?Triscutum is recorded from sample 5030 m.Therefore, the scarce nannofossils of this unit seem to be entirely reworked and the depositional setting was probably non-marine.
to the latest Santonian to Campanian by the occurrence of Arkhangelskiella cymbiformis in sample 4550 m (Burnett, 1998) (Fig. 5).Overall, non-marine conditions seem to have prevailed.
Zone 7 (4570-4890 m) is covered by 16 samples of which six were barren of nannofossils.The assemblages of this interval contain rare, moderately preserved calcareous nannofossils.The occurrence of Eiffellithus eximius (UC8-UC16) in sample 4890 m and of Calculites obscurus (UC8-UC20) in sample 4810 m indicate middle Turonian as maximum age (Burnett, 1998).The occurrence of Micula adumbrata in sample 4570 m allows a correlation with the Coniacian zones UC9-UC10 (Burnett, 1998) (Fig. 5).Based on these data, we correlate this interval with the middle conditions, reflected by orbitoid sandstones, pass into middle to outer neritic water depths (Summesberger et al., 2002).The uppermost unit of the Grünbach Syncline is represented by turbiditic shales and sandstones of the Zweiersdorf Formation, which is of Danian to Thanetian age (Hradecká et al., 1999;Summesberger et al., 2002).Wessely (2006) correlated the Cretaceous of the Glinzendorf Syncline with the formations of the Grünbach Syncline starting with the Santonian Maiersdorf Formation, followed by the Campanian Grünbach Fm., and the Maastrichtian Piesting Fm.Based on this scheme, the Cretaceous succession of Gänserndorf UeT3 would be completely correlated with the Grünbach Fm.We agree only partly with the schematic and conceptual correlation of Wessely (2006), because it does not resolve the appearance of Campanian strata (unit 1) on top of Maastrichtian ones (unit 2) and it does not explain the occurrence of Turonian/Coniacian strata in the basal fill of the syncline (units 6 and 7).Therefore, we propose the following lithostratigraphic subdivision and correlation (Fig. 2).
The Turonian to Coniacian age of the lower part of the Cretaceous fill of the Glinzendorf Syncline excludes a correlation with the Santonian to Campanian Grünbach Fm.This unit has not been described so far from the Glinzendorf Syncline and no formation name is available for it.Therefore, we propose Glinzendorf Formation as new name.
Type area: Subsurface Glinzendorf Syncline, in the area of Glinzendorf and Gänserndorf.The transition into the southern and northern parts of the Glinzendorf Syncline will have to be evaluated based on biostratigraphic data from additional wells.
Lithology: Shales with intercalations of coals and marls in its basal part and silty shales and conglomerates with an allochthonous intercalation of anhydrite in the upper part (see descriptions of units 6 and 7 in the results chapter).
Fossils: Only calcareous nannofossils have been detected so far.
Depositional environment: the coal bearing lower part (unit 7) seems to have formed under limnic conditions.Terrestrial conditions are reflected by repeated reddish and brownish coloring of the shales.Conglomerates at the base of the more marine influenced upper part may point to alluvial fans, which are soon replaced by coastal marine settings.Marine calcareous nannofossils Based on these data, Unit 1 is of Campanian age and Unit 2 is subdivided into a late Campanian and a Maastrichtian interval (Fig. 5).Units 3 and 4 are of late Campanian age and Unit 5 is correlated with the early Campanian but may span to the latest Santonian.Unit 6 contains middle Turonian and Coniacian parts.No biostratigraphic data are available for Unit 7.

Discussion
The Cretaceous units of the Glinzendorf Syncline represent eastern equivalents of contemporaneous deposits of Tirolic units of the Northern calcareous Alps such as the Grünbach Syncline and formed under largely similar depositional environments (Wessely, 2006;Hofer et al., 2013).Therefore, Wessely (2006) applied the lithostratigraphic scheme of the Grünbach Syncline, established by Summesberger et al. (2000;2002) and Wagreich and Summesberger (2001), also for the Glinzendorf Syncline.
In the Grünbach Syncline, sedimentation commenced during the Santonian with the conglomerates of the Kreuzgraben Formation and the few-meter-thick, fully marine Maiersdorf Formation, comprising limestones rich in brachiopods and rudists along with sandstones.These are overlain by the Grünbach Formation, an about 150 thick succession of shales, sandstones and coals, which is famous for its reptile fauna (Bunzel, 1871) and for its diverse flora (Plöchinger et al., 1961;Herman and Kvaček, 2007;Summesberger et al., 2000;2002;Hofer et al., 2011).The thick Dreistetten Conglomerate Member is intercalated within the Grünbach Fm. (Grundtner, 2011).The conglomerates are overlain by an about 60-m-thick unit of coal-bearing limestones, marls and sandstones with marine mollusc faunas alternating with limestones bearing Characeae oogonia (Schlagintweit and Wagreich, 1992).A latest Santonian to early Campanian age was proposed by Summesberger et al. (2000;2002) for the Grünbach Fm. based on ammonites and inoceramid bivalves, nannofossils and 87 Sr/ 86 Sr data from the underlying Maiersdorf Fm. and the overlying Piesting Fm.The Grünbach Fm. formed under lacustrine and brackish conditions with rare marine incursions.Coastal swamps characterized the environment with alluvial fans at the basin margins (Summesberger et al., 2002;Hofer et al., 2011).The Dreistetten Conglomerate Member is interpreted as fan to fan delta complex within the Grünbach Fm. (Grundtner, 2011).
The Piesting Fm. overlies the Grünbach Fm. and represents a several hundred-meter-thick unit of grey marls, silt and sandstones with intercalations of orbitoid sandstones, which occur especially in the basal part (Schlagintweit and Wagreich, 1992;Summesberger et al., 2000;2002;Wagreich and Summesberger, 2001).Based on its inoceramid and ammonite faunas, the Piesting Fm. is correlated with the late Campanian to Maastrichtian, which is supported by the calcareous nannoplankton assemblages (Summesberger et al., 2002).The Piesting Fm. formed under marine conditions.Inner neritic foraminifers, and passes quickly into marls and shales.This development is identical to the succession described from the Grünbach Syncline, where sandstones and orbitoid sandstones and conglomerates formed during the initial transgressive phase, passing upsection into more open marine "Inoceramus-marls" (Schlagintweit and Wagreich, 1992;Summesberger et al., 2002).The lower part of the Piesting Fm. in the Glinzendorf Syncline is of Campanian age, which is in line with data from the Grünbach Syncline.A shallowing occurred around the Campanian/Maastrichtian boundary indicated again by sandstone intercalations bearing the shallow water foraminifer Goupillaudina sp..The top part of the Piesting Fm. in Gänserndorf UeT3 can be correlated with the Maastrichtian, which again is in line with data from the Grünbach Syncline.Maastrichtian globotruncanid foraminifers from Gänserndorf UeT3 derived from this unit (Wessely, 1992;2006).This interval reflects the maximum of marine influx within the Cretaceous successions of the Glinzendorf Syncline (Fig. 2).
The presence of Danian to Thanetian deposits of the Zweiersdorf Fm. can be excluded for Gänserndorf UeT3 and is, to our knowledge, not documented so far from the Glinzendorf Syncline.

Gänserndorf Thrust
The occurrence of coarse siliciclastic Campanian strata of the Grünbach Formation on top of the pelitic Maastrichtian Piesting Fm. has not been described so far from Gosau deposits.It can be explained by a thrust, which transported lateral equivalents of unit 5 over Maastrichtian units or by an overturned and eroded a relation with the Campanian conglomerates of the Glinzendorf syncline.
The top of the Grünbach Fm. in the Glinzendorf Syncline is formed by coal and coaly limestones with Characeae oogonia of late Campanian age (unit 3).Limnic conditions prevailed during the formation of this part of the Grünbach Fm., which is corroborated by the geochemical data of Hofer et al. (2013).The coal bearing unit 3 of Gänserndorf UeT3 is identical in facies and thickness to the succession described by Gruber et al. (1992) and Schlagintweit and Wagreich (1992) from the Campanian successions of the Miesenbach outcrops, which are situated north of the Grünbach Syncline.
Unit 1 (3210-3570 m) is also of late Campanian age.Like unit 5, it is subdivided into a limnic basal part and a more marine influenced upper part and bears rare layers with Characeae oogonia and coal.Therefore, we interpret unit 1 also as Grünbach Fm. and as originally lateral equivalent of unit 5.In seismics, the boundary between unit 2 (Piesting Fm.) and unit 1 (Grünbach Fm.) is indicated by a slightly more prominent reflector and an unconformity.The shallow water foraminifer genus Goupillaudina has been recorded from basal parts of unit 1.This is in line with Plöchinger et al. (1961) and Oberhauser (1963), who recorded this genus from the Grünbach syncline, where these authors described it as typical for the coal bearing series of the Grünbach Fm.The Piesting Fm. in the Glinzendorf Syncline commences with sandstones, bearing shallow water

Figure 2 :
Figure 2: Wire logs (SP, RES) and lithologies of well Gänserndorf UeT3.Calcareous nannofossil assemblages define eight zones; grey intervals indicate barren samples.The 20-m-interval separating the zones represent uncertainty due to sampling distance.Chronostratigraphy and lithostratigraphy based on the age of the nannoplankton subunits and prevailing lithologies.Marine and non-marine phases are based on the presence or absence of marine calcareous nannofossils and the occurrence of Characeae and foraminifers.

Figure 5 :
Figure 5: Occurrences of biostratigraphically important calcareous nannoplankton species in well Gänserndorf UeT3 and age interpretation.

Figure 6 :
Figure 6: Seismic survey showing Cretaceous units of the Glinzendorf Syncline and lithostratigraphic subdivision based on well Gänserndorf UeT3.See red line in Figure 1 for position of the section.Note that seismic depth is given in True Vertical Depth, which is not fully identical with drilling depth.

Table 1 :
Cretaceous calcareous nannofossil taxa detected in the investigated cuttings-samples.