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The Messinian event in the Paratethys: Astronomical tuning of the Black Sea Pontian
Marine and Petroleum Geology 80 (2017) 321e332
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Marine and Petroleum Geology journal homepage: www.elsevier.com/locate/marpetgeo
Review article
The Messinian event in the Paratethys: Astronomical tuning of the Black Sea Pontian Yuliana V. Rostovtseva a, *, Alena I. Rybkina b a b
Geological Faculty, Lomonosov Moscow State University, Leninskie Gory, GSP-1 119991 Moscow, Russia Geophysical Centre of the Russian Academy of Sciences, Molodezhnaya St. 3, 119296 Moscow, Russia
a r t i c l e i n f o
a b s t r a c t
Article history: Received 9 September 2016 Received in revised form 27 November 2016 Accepted 5 December 2016 Available online 8 December 2016
This study presents new data on the orbitally calibrated Maeotian/Pontian and Pontian record of the Black Sea Basin (Paratethys) obtained by time-series analysis of magnetic susceptibility (MS) data from relatively deep-water Upper Miocene sediments exposed in the Zheleznyi Rog section (Taman Peninsula, Russia). In the studied interval, a ~145-m-long sedimentary sequence, spectral analysis revealed statistically significant signals with 6.1e8.2 m and 3.0e4.0 m wavelength. These signals correspond to the obliquity and precession cycles, respectively. This study correlates the main steps of Messinian Salinity Crisis (MSC) of the Mediterranean to the Black Sea Pontian record based on astronomical tuning of the study sequence and evaluation of integrated biostratigraphic, paleomagnetic and sedimentological data. Based on cyclostratigraphic results, Maeotian/Pontian beds with Actinocyclus octonarius accumulated from ~6.3 to 6.1 Ma. Most of the Novorossian sediments correspond to the first MSC step. The TG 22 (5.79 Ma) and TG 20 (5.75 Ma) glacial events occur in the uppermost Novorossian record and are marked by extraordinary high values of MS. The Portaferian, dated at the base as ~5.65 Ma and the top as ~5.45 Ma, corresponds to the second MSC step. The Novorossian/Portaferian transition is marked by the hiatus of approximately 150e160 kyr, which agrees well with the concept of the intra-Pontian unconformity in the Black Sea Basin and a sea-level drop in the Mediterranean from 5.6 to 5.46 Ma. The ages for the base and the top of the Bosphorian were estimated as ~5.45 Ma and ~5.27 Ma, respectively. The base of the Bosphorian corresponds to the third Lago Mare episode caused by the high sea-level connection between the Mediterranean and Eastern Paratethys. © 2016 Elsevier Ltd. All rights reserved.
Keywords: Messinian event Pontian Black sea Taman region Cyclostratigraphy Magnetic susceptibility
Contents 1. 2. 3.
4.
5.
Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 321 Materials and methods . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 322 Results . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 325 3.1. Magnetic susceptibility values . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 325 3.2. Spectral analysis . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 325 Discussion . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 327 4.1. Paleoenvironment and chronostratigraphic framework . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 327 4.2. Astronomical tuning . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 328 Conclusions . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 330 Acknowledgements . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 331 References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 331
* Corresponding author. E-mail addresses: [email protected] (Y.V. Rostovtseva), [email protected] (A.I. Rybkina). http://dx.doi.org/10.1016/j.marpetgeo.2016.12.005 0264-8172/© 2016 Elsevier Ltd. All rights reserved.
1. Introduction The Messinian Salinity Crisis (MSC) of the Mediterranean is the
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greatest event in the Miocene related to dramatic palaeoenvironmental changes and deposition of evaporites (Hsü et al., 1973). This unusual event, driven by tectonic reorganization and gradual climatic deterioration, influenced the sedimentary setting in the Paratethys, including the Black Sea region (Earthen Paratethys). Most researchers (e.g. Trubikhin, 1989; Nevesskaya et al., 2003; Clauzon et al., 2005; Snel et al., 2006; Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova et al., 2012; Popov et al., 2013) assume that the Black Sea Pontian partially or entirely corresponds to the MSC interval (Fig. 1). However, according to Pevzner et al. (2003), Semenenko et al. (2009) and Gozhyk et al. (2015), the Pontian should correlate with the pre-evaporite Messinian. The interpretation of individual MSC steps in the Miocene record of the Black Sea is also open to debate. Integrated multidisciplinary studies (Trubikhin (in Popov et al., 1996); Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova and Golovina, 2011; Radionova et al., 2012; Popov et al., 2013) showed that the change from normal to reversed polarity in the lower part of the Pontian relates to the Chron C3An/C3r boundary. The age of Chron C3An/C3r boundary has been estimated at 6.033 Ma (Hilgen et al., 2012). Given that date, the lowermost Pontian mainly corresponds to the Primary Lower Gypsum unit of the MSC. However, the age of the top of the Black Sea Pontian is controversial. Krijgsman et al. (2010) and Vasiliev et al. (2011) suggested a date of ~5.6 Ma for the upper boundary of the Black Sea Pontian. Other authors (Trubikhin (in Popov et al., 1996); Nevesskaya et al., 2003; Snel et al., 2006; Radionova et al., 2012; Popov et al., 2006, 2013; Rostovtseva and Rybkina, 2014) have proposed a date of 5.3e5.2 Ma for the top of the Black Sea Pontian. The top of the Azovian sediments (lower Kimmerian) is characterized by normal polarity related to the Chron C3n.4n (Thvera) (Trubikhin (in Popov et al., 1996); Radionova et al., 2012; Popov et al., 2006, 2013). The beginning of the normal-polarity Chron C3n.4n occurs at 5.235 Ma (Hilgen et al., 2012). Given these data, all the major steps of the Messinian event according to scenarios in discussion (Roveri et al., 2014: Primary Lower Gypsum 5.97e5.6 Ma, Resedimented Lower Gypsum 5.6e5.55 Ma, Upper Gypsum 5.55e5.33 Ma; Bache et al., 2015: peripheral evaporites 5.97e5.6 Ma, subaerial erosion 5.6e5.55 Ma, central evaporites 5.55e5.46 Ma) may be defined in the Pontian sedimentary succession of the Black Sea. According to
Gillet et al. (2007) and Suc et al. (2015), the intra-Pontian erosional surface (IPU) determined on the Western Black Sea margins is analogous to the Messinian Erosional Surface (MES) in the Mediterranean. Generally, in the Black Sea part of the Paratethys, the Pontian stage is subdivided in to the lower Pontian substage (Novorossian) and the upper Pontian substage (Portaferian and Bosphorian) (Ilyina et al., 1976; Nevesskaya et al., 1986; 2003; Popov et al., 2006, 2013) (Fig. 1). The Pontian sediments characteristically contain a brackish biota. The Portaferian sediments are marked by the appearance and distribution of Congeria subrhomboidea, which is absent in Bosphorian sediments. This paper presents the results of high-resolution cyclostratigraphic analysis of all the substages of the Pontian designated at the Zheleznyi Rog section (Taman Peninsula). This section comprises relatively deep-water (50e150 m) clay sediments and is located near the Arshintsevo section (Kerch Peninsula) with limestones defined in the Kerch-Taman region as the neo-stratotype Pontian (Andrusov, 1917, 1923; Nevesskaya et al., 2003) (Fig. 2). The Black Sea is known to be rich in Neogene petroleum systems. Hydrocarbon exploration there needs accurate chronostratigraphy. 2. Materials and methods The Zheleznyi Rog section is located on the Black Sea coast of Taman Peninsula (Fig. 2) (N4511006.100 E36 740 48.400 , Russia) and comprises well-exposed upper Sarmatian-Kimmerian sediments. Since its first description by Andrusov (1903), this geological section has been studied by paleomagnetic, palaeontological and lithological methods (Pevzner and Chikovani, 1978; Pevzner et al., 2003; Semenenko and Pevzner, 1979; Semenenko and Lulieva, 1982; Trubikhin, 1989; Chumakov et al., 1992; Chumakov, 2000; Popov and Zastrozhnov, 1998; Filippova, 2002; Rostovtseva, 2009; Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova and Golovina, 2011; Radionova et al., 2012; Chang et al., 2014). In the Zheleznyi Rog section, the total thickness of transitional Maeotian/ Pontian and Pontian sediments is approximately 145 m. Novorossian, Portaferian and Bosphorian sediments of the Pontian stage are defined in the Zheleznyi Rog section. The transitional Maeotian/Pontian beds (interval from 144.6 to
Fig. 1. Overview of the different time scales for the Mediterranean and Eastern Paratethys (Black Sea) in comparison with the international time scale.
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112.8 m) consist mostly of diatomaceous clays with Actinocyclus octonarius (Fig. 3). The Novorossian sediments (interval from 112.8 to 44.4 m) consist of clays, with the lower part of the section containing sporadic diatomite layers (diatomite marker beds SP, Ch, and N according to Radionova and Golovina, 2011). The first remains of Paradacna abichi related to Pontian malacofauna assemblage occur in sediments approximately 5e6 m above the top of the diatomite SP. The magnetic reversal event corresponding to the Chron C3An/C3r boundary occurs near the base of the diatomite Ch (Trubikhin, 1989; Radionova and Golovina, 2011; Radionova et al., 2012). The thin detrital limestone layer that occurs at the top of the transitional Maeotian/Pontian beds records local erosion and may mark the base of the Pontian (layer L. 39, Fig. 3). The noncalcareous clays are dominant at the top of the Novorossian. The Novorossian sediments are approximately 68 m thick. The Portaferian sediments are only 6 m thick (interval from 44.4 to 38.4 m). These sediments contain Congeria subrhomboidea and are lithologically varied. These beds include detrital shell limestone, clay breccia, a paleosol horizon, and sandy clay (Fig. 4). The Bosphorian sediments (interval from 38.4 to 0 m), devoid of
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Congeria subrhomboidea, consist of calcareous clays (clays containing 10e50% CaCO3), that are marked by cycles of light-grey and grey clays. The thickness of the Bosphorian section is up to 38 m. In terms of magnetostratigraphy most of the Pontian are characterized by reversed polarity with an episode of normal polarity near the base (Trubikhin, 1989; Pevzner et al., 2003; Vasiliev et al., 2011). The Kimmerian sediments that directly overlie the Pontian sedimentary succession at Zheleznyi Rog have normal polarity. The Upper Miocene sediments were investigated by cyclostratigraphic methods using the magnetic-susceptibility rocks and statistical techniques. Cyclostratigraphic methods are explained in many publications, including the well-known monograph of Weedon (2003). Magnetic susceptibility was measured with a “KM-7” magnetic susceptibility metre with a sensitivity of 106SI units (GF Instruments, Brno, Czech Republic). In total, 2145 measurements of the magnetic susceptibility of Maeotian/Pontian and Pontian rocks were obtained with an average vertical spacing of 7 cm. For the statistics, the PAST programme (Hammer et al., 2001) was used for spectral analysis (Lomb-Scargle periodograms), including REDFIT
Fig. 2. The Zheleznyi Rog (ZR) section. (A) Location of the study sediments and Arshintsevo section (AR). (B) Panoramic view of the Pontian sediments.
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Fig. 3. Lithological column of the investigated section and the results of the magnetic susceptibility (MS) measurements. (A) The interval between 0 and 44.4 m. (B) The interval between 44.4 and 112.8 m. (C) The interval between 112.8 and 144.6 m. The diatomite marker beds are presented (A, SP, Ch, N according to Radionova and Golovina, 2011). Paleomagnetic polarity patterns were obtained by Trubikhin (in Popov et al., 1996), Vasiliev et al. (2011) and Radionova et al. (2012). Paleontological data were obtained by Filippova (2002), Radionova and Golovina (2011), Radionova et al. (2012).
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Fig. 4. Portaferian sediments and the base of the Bosphorian in the Zheleznyi Rog (ZR) section. (A) Panoramic view of the top of Novorossian, Portaferian and the base of Bosphorian sediments. (B) Portaferian sediments. (C) Identified layers in Portaferian sediments.
(Schulz and Mudelsee, 2002) and wavelet analysis. Additionally, the frequency values of the Lomb-Scargle and REDFIT periodograms were used as targets for a Gaussian bandpass filter with the AnalySeries programme (Paillard et al., 1996). The Gaussian bandpassfilter data were compared with long-term insolation changes at the end Miocene (Laskar et al., 2004). The rock magnetic properties of the Upper Miocene samples of the Zheleznyi Rog section indicate greigite (a magnetofossil and early diagenetic mineral) as the main iron sulphide carrying the primary magnetization (Vasiliev et al., 2011; Chang et al., 2014). 3. Results 3.1. Magnetic susceptibility values The magnetic susceptibility (MS) of the transition Maeotian/ Pontian and Pontian rocks ranges widely with values from 0.016 to 0.937 103 SI units (Fig. 3). The rocks at the Maeotian/Pontian transition exhibit MS values ranging from 0.04 to 0.16 103 SI units. Novorossian rocks exhibit MS values ranging from 0.016 to 0.937 103 SI units. Extraordinarly high values of MS (from 0.52 to 0.937 103 SI) occur in clays of the upper part of the
Novorossian at the intervals 65.8e62.0 m and 59.2e51.6 m. Portaferian rocks exhibit MS values ranging from 0.03 to 0.19 103 SI units. The Bosphorian clays exhibit MS values from 0.05 to 0.32 103 SI units with higher values (up to 0.42 103 SI) at the top of these sediments. 3.2. Spectral analysis Spectral analysis of the MS data from Portaferian sediments clearly illustrates the lack of signal that passes the 95% and 99% confidence intervals (Fig. 5). The strongest peak visible in LombScargle and REDFIT periodograms (at 9.4 m) does not reach the 95% confidence interval. Also, the Portaferian succession (characterized by thickness up to 6 m) is too thin to clearly support the presence of a 9.4 m cycle. The wavelet reveals shorter period cycles, which differ from the periodicity at 9.4 m. Based on spectralanalysis results and lithological data, we infer that the Portaferian, which includes re-sedimented deposits, displays a poor record of astronomical cyclicity. Spectral analysis of the MS-data of lower Pontian (Novorossian) sediments suggests strong periodicity. The Lomb-Scargle periodogram reveals only one significant signal with periodicity at 59.7 m
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Fig. 5. REDFIT spectral analysis (left) and Wavelet analysis (right) of the magnetic susceptibility (MS) data from 38.4 to 44.4 m (A, B) and from 44.4 to 112.8 m (C, D).
which passes the 99% confidence interval. The REDFIT analysis supports peaks at 59.7, 3.1, 2.7 and 2.3 m that pass the 99% confidence intervals (Fig. 5C). Significantly, the REDFIT periodogram with frequency values transformed into depth-domain also displays the signal at 6.1 m (Fig. 6). This peak is supported by wavelet analysis that clearly illustrates the presence of a cycle between 5.6 and 7.4 m (Fig. 5D). To help identify Milankovitch cyclicity, we used the ratios between the observed periodicities. The predicted ratio of the long eccentricity period (400-kyr eccentricity cycle) to obliquity peak is 9.7:1. The predicted ratios of the obliquity period (41-kyr obliquity cycle) to the 24, 22 and 19 kyr precession peaks are 1.7:1, 1.9:1 and 2.2:1, respectively. The ratio of the signal at 59.7 to the peak at 6.1 m is 9.7:1. The ratios of the signal at 6.1 m to peaks at 3.1, 2.7 and 2.3 m are 1.9:1, 2.2:1 and 2.6:1, respectively. Based on these ratios, we suggest that the precession (signals at 3.1, 2.7 and 2.3 m), obliquity (signal at 6.1 m) and 400-kyr eccentricity (signal at 59.7 m) cycles
are expressed in the MS-data of Novorossian sediments. Eccentricity, obliquity and precession cycles have been defined in the Miocene and Pliocene sedimentary record of the Mediterranean (Lirer et al., 2009; Gunderson et al., 2012) and of the Eastern Paratethys (Popescu et al., 2006, 2010). Taking into account the changes in sedimentation rate, the peak at 6.1 m may be analogous to the signals at 7.1e7.8 m and 8.0e8.2 m that were detected in the MS-record of Maeotian/Pontian beds with Actinocyclus octonarius, and the Bosphorian sediments of the Zheleznyi Rog section, respectively (Fig. 6). In addition, precession cycles (signals at 3.0e3.2 and 4.0 m) were identified in the MS-data of Maeotian/Pontianbeds with Actinocyclus octonarius as well as the Bosphorian and Novorossian sediments (Fig. 6). The wavelet analysis of the Pontian sediments (0e112.8 m) and the whole succession (0e144.6 m) showed signals at 5.6e8.1 m and at 2.4e4.8 m (Fig. 7). The Gaussian filter centred at 6.1, 8.0 (midpoint of 7.8e8.2 m) m, 3.1 (mid-point of 3.0e3.2 m), and 4.0 m
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Fig. 6. Lomb-Scargle (left) and REDFIT (right) periodograms displaying periodicities in the intervals 144.6e112.8 m, (A, B); 112.8e44.4 m, (C, D); 38.4e0 m, (E, F) (modified from Rostovtseva and Rybkina (2014)).
revealed the presence of the 21 and 39 cycles in the whole succession (0e144.6 m) (Fig. 7). 4. Discussion 4.1. Paleoenvironment and chronostratigraphic framework The beginning of the Pontian was marked by a transgression (Popov et al., 2004). At that time, deep-water environments in which clays accumulated existed in the Black Sea (Popov et al., 2004). Based on the dominant brackish mollusk fauna, the salinity of the water was low, but it was not less than 5e8‰ (Popov et al., 2006). According to Radionova and Golovina (2011), the pulsing marine-water invasion and short-term connection with Eastern Mediterranean facilitated the appearance of coccoliths and marine diatoms during the Maeotian/Pontian transition and during the start of the Pontian. The end of the Novorossian was marked by a regression. In the Portaferian, the Eastern Paratethys was restricted, which caused the separation the Caspian Basin from the Euxinian Basin (Black Sea) in the northern part (Nevesskaya et al., 1986, 2003;
Popov et al., 2004, 2006). According to Krijgsman et al. (2010), the Portaferian represents a regressive event in the Dacic Basin during which the early Pontian ostracod fauna indicative of basinal conditions was replaced by littoral, fluvial and lacustrine species. The Bosphorian substage introduced by Andrusov (1923) in the Kerch-Taman region (Black Sea) corresponds to the transgressive event in the Paratethys. In the Dacic Basin, the beginning of the Bosphorian corresponds to a second bloom of ostracod fauna (Krijgsman et al., 2010) and to a lithological change to more basinal sequences (Jipa, 1997) in the East Carpathian Pontian sections. Biostratigraphic and paleomagnetic dating by Krijgsman et al. (2010) placed the Maeotian/Pontian boundary at 6.04 ± 0.01 Ma, and the Novorossian/Portaferian boundary at 5.8 ± 0.1 Ma. In the Dacic Basin, the Portaferian/Bosphorian boundary is dated at 5.5 ± 0.1 Ma. Snel et al. (2006) estimated the Maeotian/Pontian boundary date at 6.15 ± 0.11 Ma. The age of the Pontian/Kimmerian transition is 5.3 ± 0.1 Ma. The bases of the Portaferian and Bosphorian are dated at 6.0 and 5.6 Ma, respectively. The length of the Pontian stage is approximately 0.85 Myr. In the Pontian, the Eastern Paratethys (Euxinian-Caspian Basin) biogeographically belongs to the Dacic Basin (Popov et al., 2004).
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Fig. 7. Magnetic susceptibility (MS): a: original data; a Gaussian filter was applied centring at b: 8.0 (for intervals 144.6e112.8 m and 44.4e0 m) and 6.1 (for interval 112.8e44.4 m) m; c: 4.0 (for intervals 144.6e112.8 m and 44.4e0 m) and 3.1 (for interval 112.8e44.4 m) m; the Wavelet analysis: d (for the entire record, from 144.6 to 0 m).
4.2. Astronomical tuning Based on integrated paleomagnetic, palaeontological and lithological data, many authors place a paleomagnetic reversal in the lower part of the Pontian at 6.033 Ma (Trubikhin (in Popov et al., 1996); Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova and Golovina, 2011; Radionova et al., 2012; Popov et al., 2013). Our spectral analysis suggests that the repetitive signals 6.1e8.2 m and 3.1e4.0 m probably record astronomical cyclicity. In our study, a Gaussian filter centred at 6.1e8.0 m (6.1 m for the Novorossian, 8.0 m for the Maeotian/Pontian transition and the upper Pontian) reveals the presence of 14 cycles in the interval from the paleomagnetic reversal in the lower part of the Pontian to the base of the Kimmerian in the Zheleznyi Rog section, (i.e. from 96 to 0 m) (Fig. 8). On the basis of the ratios between the observed periodicities, we infer that the peak at 6.1e8.2 m corresponds to the obliquity cycle (41,000 yr). Given this, the 96-m interval is estimated to have a duration of ~0.57 Myr. The Novorossian/Portaferian boundary is dated at ~5.65 (5.7) Ma. According to Krijgsman et al. (2010), the age of the base of the Portaferian in the Eastern Paratethys is 5.8 ± 0.1 (5.7e5.9) Ma. In the upper part of the Novorossian (from 65.8 to 59.2 m), the bases of intervals with extraordinarily high values of MS (up to 0.834 and 0.937 103 SI units) correlate to the glacial peaks TG 22 (5.79 Ma) and TG 20 (5.75 Ma), respectively (Shackleton et al., 1995; Hodell et al., 2001). These results are consistent with
palaeontological and lithological features. As shown by Radionova et al. (2012), the upper part of the Novorossian in the Zheleznyi Rog section (from 79 m and upward the section) is marked by the complete disappearance of calcareous nanoplankton and marine diatom species. Radionova and Golovina (2011) suggested that increased regression and disconnection with marine basins occurred at the end of the Novorossian. Based on cyclostratigraphic results, the disappearance of coccoliths and marine diatoms occurred at ~5.88 Ma. The extraordinarly high values of MS can be explained by restricted-basin circulation and increased productivity of diagenetic sulphide minerals during glacial events. Peaks TG 20e22 are both marked by a significant drop in global sea level (on the order of 50 m) (Shackleton et al., 1995; Hodell et al., 2001). The stratigraphic level of 5.97 Ma, which relates to the MSC onset and glacial peak TG32 and correlates with the base of the “stagnation horizon” (from 93.6 to 86.8 m). This “stagnation horizon” is represented by clays containing manganese-bearing minerals. It was first described by Andrusov (1903) in the Zheleznyi Rog section. Thus, most Novorossian sediments (from 93.6 m and upward the section) in the relatively deep-water Zheleznyi Rog section can be considered analogous to the MSC onset and the first evaporitic stage (i.e. Roveri et al., 2014: Primary Lower Gypsum 5.97e5.6 Ma; Bache et al., 2015: peripheral evaporites 5.97e5.6 Ma) in the Mediterranean. The base of thin detrital limestone layer (layer L.39, Fig. 3) that is located at the top of transitional Maeotian/Pontian sediments is dated at ~6.1 Ma.
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Fig. 8. Original magnetic susceptibility (MS) data (logarithmically transformed and detrended) filtered according to the high-frequency signal revealed by the periodograms in Fig. 6. Gaussian filtering was applied, centring at 8.0 m (for intervals 144.6e112.8 m and 44.4e0 m) and 6.1 m (for interval 112.8e44.4 m). The sporadic diatomite layers are presented (A, SP, Ch, N; diatomites SP, Ch and N according to Radionova and Golovina, 2011). Paleomagnetic polarity patterns were obtained by Trubikhin (in Popov et al., 1996), Vasiliev et al. (2011) and Radionova et al. (2012). Paleontological data were obtained by Radionova and Golovina (2011) and Radionova et al. (2012). The numbers in the circles are the set of cycles. MSC ¼ the Messinian Salinity Crisis. MS ¼ magnetic susceptibility.
The Maeotian/Pontian beds with Actinocyclus octonarius (interval from 144.6 to 114.6 m) accumulated from ~6.3 to 6.1 Ma. This age determination agrees well with our previous studies
(Rostovtseva and Rybkina, 2014; Rybkina and Rostovtseva, 2014). Our results show a poor astronomical record in the thin Portaferian sequence, which includes a detrital shell limestone and clay
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breccias. As shown by Krijgsman et al. (2010) the base of the Portaferian corresponds to a fall in Paratethyan water level. The Gaussian filter centred at 6.1e8 m reveals low obliquity in this part of the Zheleznyi Rog section. The Bosphorian sediments (0e38.4 m) display the presence of 4e5 cycles (4.8 cycles, for signal at 8 m) related to the obliquity period. This gives a duration of ~205 kyr for this sedimentary succession. According to Trubikhin (1989) and Vasiliev et al. (2011), the base of the Kimmerian with normal polarity in the Zheleznyi Rog section correlates to the Thvera (C3n.4n). Given the age of 5.235 Ma for C3r/C3n (Hilgen et al., 2012), the base of the Bosphorian in the Zheleznyi Rog section can be dated as ~5.45 (5.5) Ma. Given these determination, the Black Sea Bosphorian correlates to the Upper Gypsum and the Lago Mare biofacies characterized by Paratethyan fossil assemblages. Based on biostratigraphic and paleomagnetic results, the base of the Bosphorian in the Dacic Basin is variously dated at 5.5 ± 0.1 (5.4e5.6) Ma (Krijgsman et al., 2010), 5.6 Ma (Snel et al., 2006), or 5.45 Ma (Popescu et al., 2006; Bache et al., 2012). The Bosphorian beds were defined by Andrusov (1923) in the Kerch-Taman region (Black Sea) including the Zheleznyi Rog section. Subsequently, numerous researchers have confirmed the Bosphorian in the Zheleznyi Rog section (Kolesnikov, 1940; Trubikhin, 1989; Popov et al., 1996; Pevzner et al., 2003; Radionova et al., 2012). In the Zheleznyi Rog section, the Bosphorian beds lie with apparent conformity on the Portaferian sediments, and they probably reflect a change from regressive lowstand conditions to transgressive conditions. According to Krijgsman et al. (2010), global warming and more humid conditions after TG12 at 5.5 Ma (Hodell et al., 2001; Hilgen et al., 2007) led to the positive hydrological change (overflow) in the Paratethys, which further caused a widespread transgression in the late Pontian. As proposed by Bache et al. (2012), the re-flooding of the Mediterranean Basin by Atlantic waters occurred at 5.46 Ma and the marine connection with the Dacic Basin occurred at 5.45 Ma. In addition to detecting obliquity cycles, spectral analysis suggests strongly expressed precession periodicity (signal at 4 m) in the Bosphorian sedimentary succession. The Upper Gypsum and the Lago Mare Unit at Eraclea Minoa (Mediterranean) also display related precession-driven climate oscillations (Hilgen et al., 2007; Bache et al., 2012). The level at 5.33 Ma, which corresponds to the Miocene/Pliocene boundary in the Mediterranean, appears to correlate with Layer 64 of the Pontian in the Zheleznyi Rog section (Fig. 8). Based on integrated biostratigraphic, paleomagnetic and cyclostratigraphic results, we estimate the dates for the base and the top of Portaferian in the Zheleznyi Rog section to be ~5.65 Ma and ~5.45 Ma, respectively. Taking into account the 6 m thickness of sediments and the presence of re-sedimented deposits in the record of Portaferian as well as obtained astronomical cycles in metres, we propose a ~150e160 ky hiatus between the lower and upper Pontian. This is consistent with the concept of intra-Pontian unconformity (Gillet et al., 2007; Suc et al., 2015) and suggests that the Novorossian/Portaferian transition was related to a phase of high-amplitude Mediterranean sea-level drop and the onset of the Messinian Erosional Surface (MES) in the Black Sea (Tari et al., 2015, 2016; Krezsek et al., 2016). During the Messinian, a major sea-level drop in the Mediterranean occurred from 5.6 to 5.46 Ma (Clauzon et al., 1996; Bache et al., 2012). The TG14 (5.58 Ma) and TG12 (5.54 Ma) glacial events took place in this stage of the MSC. If the inferred hiatus was absent in intra-Pontian sedimentary record in the Zheleznyi Rog section, the top of the Miocene here could be dated at ~5.46 (5.5) Ma based on the presence of the 14 obliquity cycles in the uppermost 96 m of the Pontian. However, this would be inconsistent with (1) the presence of a 38-m-thick
Bosphorian succession in the Zheleznyi Rog section with the base dated in the Dacic Basin as ~5.6e5.5 Ma (Snel et al., 2006; Krijgsman et al., 2010); (2) the transgressive sequence of the uppermost Zheleznyi Rog Pontian (i.e. Bosphorian) considering that the period from 5.6 to 5.46 Ma is a major sea-level drop in the Mediterranean (Clauzon et al., 1996; Bache et al., 2012); and (3) the presence of the thin Portaferian sedimentary succession with resedimented deposits and erosional surfaces. If the 14 cycles in the uppermost 96 m of the Pontian correlates to precession changes, the top of the Miocene in the Zheleznyi Rog section dates at ~5.69 Ma. In that case, the Pontian/Kimmerian boundary would be marked by hiatus of at least ~460 kyr that disagrees with palaeontological and lithological data including the presence of Bosphorian beds in the Zheleznyi Rog section. Thus, we infer that the Novorossian/Portaferian transition in the Zheleznyi Rog section corresponds to the development of the Messinian Erosional Surface (MES). In the Taman sections, the Azovian/Kamyshburunian boundary is marked by replacement of clay sediments by red oolitic iron ores. This transition was described by Krijgsman et al. (2010) as the “red sequence” in the Zheleznyi Rog section. The Azovian beds, with sedimentary features similar to upper Pontian sediments, are characterized by an erosional base that lacks significant truncation of Miocene deposits. The lower part of the Azovian sediments is characterized by reversed polarity (Radionova et al., 2012). The top of the Azovian is characterized by a regressive succession and normal polarity related to the Thvera. In the Black Sea Basin, the Miocene/Pliocene boundary commonly is placed at the Bosphorian/ Azovian boundary (Nevesskaya et al., 2003; Radionova et al., 2012). Our results allowed calculation of average sedimentation rates. For the Maeotian/Pontian transition the sedimentation rate was estimated at 16.3 cm/kyr. For the Novorossian, the sedimentation rate was estimated at 13.5 cm/kyr, and for the Bosphorian it was estimated at 19.5 cm/kyr. These rates are consistent with the mean rate of deposition in the Black Sea (Denisov, 1998). The recent sedimentation rate in the Black Sea varies from 15 to 760 cm/kyr for deep-water and shelf environments (Denisov, 1998). During the Pleistocene and Holocene, the mean sedimentation rate in the Black Sea deep basin has been 10e50 cm/kyr (Degens et al., 1978). According to Popescu et al. (2010: Fig. 6), the sedimentation rate in the Black Sea (Site 380) is 13 cm/kyr for the latest Messinian and the earliest Zanclean (5.46e5.1 Ma). The presence of a 41-kyr periodicity in the studied sedimentary record may be explained by obliquity-driven changes in highlatitude insolation (more tilt implying more sunlight of higher latitudes). An insolation gradient may be recorded in the Miocene sediments of the Taman region, which accumulated between low and high latitudes in the Northern Hemisphere (~45 N) (Rybkina et al., 2015). In this study, the cyclostratigraphic estimates obtained by Gaussian filtering at 6.1e8.0 m (obliquity cyclicity) agrees with the results of the bandpass filtering centred at 3.1e4.0 m (precession cyclicity). 5. Conclusions Astronomical tuning of the Maeotian/Pontian transition and the Pontian sedimentary record at the Zheleznyi Rog (Taman region, Black Sea Basin) confirms that the Pontian began at ~6.1 Ma. The Maeotian/Pontianbeds with Actinocyclus octonarius (interval from 144.6 to 112.8 m) were deposited from ~6.3 to 6.1 Ma. The Novorossian sediments extending from the base “stagnation horizon” (93.6 m) to the Novorossian/Portaferian boundary correspond to the first MCS step (5.97e5.6 Ma). The TG 22 (5.79 Ma) and TG 20 (5.75 Ma) glacial events are reflected in the uppermost Novorossian
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record with extraordinarily high values of MS (levels 65.8 and 59.2 m). In the Novorossian, the final phase of marine invasion occurred no later than ~5.88 Ma. The estimated ages of base and the top of Portaferian in the Zheleznyi Rog section are ~5.65 Ma and ~5.45 Ma, respectively. The Portaferian corresponds to the second MSC step, which is marked by development of the Messinian Erosional Surface (MES). The Novorossian/Portaferian boundary is marked by a hiatus of ~150e160 kyr that agrees well with the presence of re-sedimented deposits and erosional boundaries in Portaferian sedimentary sequence and the concept of intra-Pontian unconformity (Gillet et al., 2007; Suc et al., 2015). The Bosphorian section that corresponds to the transgressive phase in Black Sea Basin is analogous to the re-flooding of the Mediterranean (Bache et al., 2012) and the third Lago Mare episode (Popescu et al., 2015), both of which were caused by a high sea-level connection between the Mediterranean and Eastern Paratethys. The top of the Bosphorian dates at ~5.27 Ma. On the basis of astronomical cyclicity data, the Pontian sedimentary record in the Zheleznyi Rog section dates at ~0.67 Myr. However, the length of the Pontian stage is at least ~830 kyr (from 6.1 to 5.27 Ma), taking into account integrated biostratigraphic, paleomagnetic and sedimentological data. In the MS-data of this study, the peaks at 6.1e8.2 m and at 3.0e4.0 m related to the obliquity and precession cycles, respectively. During the Pontian, and at the end of the Maeotian, the average sedimentation rate varied from 13.5 to 19.5 cm/kyr. Acknowledgements We are grateful to Valery M. Trubikhin, Irina A. Goncharova, Natalia Yu. Filippova, Larisa A. Golovina and Sergey V. Popov, and thank them for their fruitful discussions. References Andrusov, N., 1903. Geological researches at the Taman Peninsula. Mater. Geol. Russ. 21, 257e383. Andrusov, N., 1917. In: Karpinsky, A.P. (Ed.), Pontian stage. Geology of Russia, Petrograd 4 (2), 1e41. Andrusov, N., 1923. Apsheronian stage. Proc. Geol. Comm. 110, 294. Bache, F., Popescu, S.-P., Rabineau, M., Gorini, C., Suc, J.-P., Clauzon, G., Olivet, J.-L., Rubino, J.-L., Melinte-Dobrinescu, M.C., Estrada, F., Londeix, L., Armijo, R., Meyer, B., Jolivet, L., Jouannic, G., Leroux, E., Aslanian, D., Dos Reis, A.T., Mocochain, L., Dumurd zanov, N., Zagorchev, I., Vesna Lesi c, V., Tomi c, D.M., Namık Cþagatay, M.N., Brun, J.-P., Sokoutis, D., Csato, I., Ucarkus, G., Ҫakır, Z., 2012. A two step process for the reflooding of the Mediterranean after the Messinian Salinity Crisis. Basin Res. 24, 125e153. Bache, F., Gargani, J., Suc, J.-P., Gorini, C., Rabineau, M., Popescu, S.-P., Leroux, E., Do Couto, D., Jouannic, G., Rubino, J.-L., Olivet, J.-L., Clauzon, G., Dos Reis, A.T., Aslanian, D., 2015. Messinian evaporite deposition during sea level rise in the Gulf of Lions (Western Mediterranean). Mar. Pet. Geol. 66, 262e277. Chang, L., Vasiliev, I., van Baak, C., Krijgsman, W., Dekkers, M.J., Roberts, A.P., Fitz, Gerald J.D., van Hoesel, A., Winklhofer, M., 2014. Identification and environmental interpretation of diagenetic and biogenic greigite in sediments: a lesson from the Messinian Black Sea. Geochem. Geophys. Geosyst. 15, 3612e3627. Chumakov, I.S., Byzova, S.L., Ganzey, S.S., 1992. Geochronology and Correlation of Late Cenozoic Paratethys. Nauka, Moscow, pp. 1e96. Chumakov, I.S., 2000. On the Problem of Lower Pontian (Novorossian Substage) EuxinianeCaspian, vol. 3. Moscow University Geology Bulletin, pp. 17e23. Clauzon, G., Suc, J.-P., Gauter, F., Berger, A., Loutre, M.-F., 1996. Alternate interpretation of the Messinian Salinity Crisis: controversy resolved? Geology 24 (4), 363e366. Clauzon, G., Suc, J.-P., Popescu, S.M., Marunteanu, M., Rubino, J.-L., Marinescu, F., Jipa, D., Melinte, M.C., 2005. Influence of the Mediterranean sea level changes over the Dacic Basin (Eastern Paratethys) in late Neogene. The Mediterranean Lago Mare deciphered. Basin Res. 17, 437e462. Degens, E.T., Stoffers, P., Golubic, S., Dickman, M.D., 1978. Varve chronology: estimated rates of sedimentation in the Black Sea deep basin. US Government Printing Office, pp. 499e508. Denisov, V.I., 1998. Regularities of Formationsuspended Materialin the BlackSea. Abstract of PhD dissertation. Rostov State University, Rostov-on-Don Press, p. 25.
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Review article
The Messinian event in the Paratethys: Astronomical tuning of the Black Sea Pontian Yuliana V. Rostovtseva a, *, Alena I. Rybkina b a b
Geological Faculty, Lomonosov Moscow State University, Leninskie Gory, GSP-1 119991 Moscow, Russia Geophysical Centre of the Russian Academy of Sciences, Molodezhnaya St. 3, 119296 Moscow, Russia
a r t i c l e i n f o
a b s t r a c t
Article history: Received 9 September 2016 Received in revised form 27 November 2016 Accepted 5 December 2016 Available online 8 December 2016
This study presents new data on the orbitally calibrated Maeotian/Pontian and Pontian record of the Black Sea Basin (Paratethys) obtained by time-series analysis of magnetic susceptibility (MS) data from relatively deep-water Upper Miocene sediments exposed in the Zheleznyi Rog section (Taman Peninsula, Russia). In the studied interval, a ~145-m-long sedimentary sequence, spectral analysis revealed statistically significant signals with 6.1e8.2 m and 3.0e4.0 m wavelength. These signals correspond to the obliquity and precession cycles, respectively. This study correlates the main steps of Messinian Salinity Crisis (MSC) of the Mediterranean to the Black Sea Pontian record based on astronomical tuning of the study sequence and evaluation of integrated biostratigraphic, paleomagnetic and sedimentological data. Based on cyclostratigraphic results, Maeotian/Pontian beds with Actinocyclus octonarius accumulated from ~6.3 to 6.1 Ma. Most of the Novorossian sediments correspond to the first MSC step. The TG 22 (5.79 Ma) and TG 20 (5.75 Ma) glacial events occur in the uppermost Novorossian record and are marked by extraordinary high values of MS. The Portaferian, dated at the base as ~5.65 Ma and the top as ~5.45 Ma, corresponds to the second MSC step. The Novorossian/Portaferian transition is marked by the hiatus of approximately 150e160 kyr, which agrees well with the concept of the intra-Pontian unconformity in the Black Sea Basin and a sea-level drop in the Mediterranean from 5.6 to 5.46 Ma. The ages for the base and the top of the Bosphorian were estimated as ~5.45 Ma and ~5.27 Ma, respectively. The base of the Bosphorian corresponds to the third Lago Mare episode caused by the high sea-level connection between the Mediterranean and Eastern Paratethys. © 2016 Elsevier Ltd. All rights reserved.
Keywords: Messinian event Pontian Black sea Taman region Cyclostratigraphy Magnetic susceptibility
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4.
5.
Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 321 Materials and methods . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 322 Results . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 325 3.1. Magnetic susceptibility values . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 325 3.2. Spectral analysis . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 325 Discussion . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 327 4.1. Paleoenvironment and chronostratigraphic framework . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 327 4.2. Astronomical tuning . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 328 Conclusions . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 330 Acknowledgements . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 331 References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 331
* Corresponding author. E-mail addresses: [email protected] (Y.V. Rostovtseva), [email protected] (A.I. Rybkina). http://dx.doi.org/10.1016/j.marpetgeo.2016.12.005 0264-8172/© 2016 Elsevier Ltd. All rights reserved.
1. Introduction The Messinian Salinity Crisis (MSC) of the Mediterranean is the
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greatest event in the Miocene related to dramatic palaeoenvironmental changes and deposition of evaporites (Hsü et al., 1973). This unusual event, driven by tectonic reorganization and gradual climatic deterioration, influenced the sedimentary setting in the Paratethys, including the Black Sea region (Earthen Paratethys). Most researchers (e.g. Trubikhin, 1989; Nevesskaya et al., 2003; Clauzon et al., 2005; Snel et al., 2006; Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova et al., 2012; Popov et al., 2013) assume that the Black Sea Pontian partially or entirely corresponds to the MSC interval (Fig. 1). However, according to Pevzner et al. (2003), Semenenko et al. (2009) and Gozhyk et al. (2015), the Pontian should correlate with the pre-evaporite Messinian. The interpretation of individual MSC steps in the Miocene record of the Black Sea is also open to debate. Integrated multidisciplinary studies (Trubikhin (in Popov et al., 1996); Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova and Golovina, 2011; Radionova et al., 2012; Popov et al., 2013) showed that the change from normal to reversed polarity in the lower part of the Pontian relates to the Chron C3An/C3r boundary. The age of Chron C3An/C3r boundary has been estimated at 6.033 Ma (Hilgen et al., 2012). Given that date, the lowermost Pontian mainly corresponds to the Primary Lower Gypsum unit of the MSC. However, the age of the top of the Black Sea Pontian is controversial. Krijgsman et al. (2010) and Vasiliev et al. (2011) suggested a date of ~5.6 Ma for the upper boundary of the Black Sea Pontian. Other authors (Trubikhin (in Popov et al., 1996); Nevesskaya et al., 2003; Snel et al., 2006; Radionova et al., 2012; Popov et al., 2006, 2013; Rostovtseva and Rybkina, 2014) have proposed a date of 5.3e5.2 Ma for the top of the Black Sea Pontian. The top of the Azovian sediments (lower Kimmerian) is characterized by normal polarity related to the Chron C3n.4n (Thvera) (Trubikhin (in Popov et al., 1996); Radionova et al., 2012; Popov et al., 2006, 2013). The beginning of the normal-polarity Chron C3n.4n occurs at 5.235 Ma (Hilgen et al., 2012). Given these data, all the major steps of the Messinian event according to scenarios in discussion (Roveri et al., 2014: Primary Lower Gypsum 5.97e5.6 Ma, Resedimented Lower Gypsum 5.6e5.55 Ma, Upper Gypsum 5.55e5.33 Ma; Bache et al., 2015: peripheral evaporites 5.97e5.6 Ma, subaerial erosion 5.6e5.55 Ma, central evaporites 5.55e5.46 Ma) may be defined in the Pontian sedimentary succession of the Black Sea. According to
Gillet et al. (2007) and Suc et al. (2015), the intra-Pontian erosional surface (IPU) determined on the Western Black Sea margins is analogous to the Messinian Erosional Surface (MES) in the Mediterranean. Generally, in the Black Sea part of the Paratethys, the Pontian stage is subdivided in to the lower Pontian substage (Novorossian) and the upper Pontian substage (Portaferian and Bosphorian) (Ilyina et al., 1976; Nevesskaya et al., 1986; 2003; Popov et al., 2006, 2013) (Fig. 1). The Pontian sediments characteristically contain a brackish biota. The Portaferian sediments are marked by the appearance and distribution of Congeria subrhomboidea, which is absent in Bosphorian sediments. This paper presents the results of high-resolution cyclostratigraphic analysis of all the substages of the Pontian designated at the Zheleznyi Rog section (Taman Peninsula). This section comprises relatively deep-water (50e150 m) clay sediments and is located near the Arshintsevo section (Kerch Peninsula) with limestones defined in the Kerch-Taman region as the neo-stratotype Pontian (Andrusov, 1917, 1923; Nevesskaya et al., 2003) (Fig. 2). The Black Sea is known to be rich in Neogene petroleum systems. Hydrocarbon exploration there needs accurate chronostratigraphy. 2. Materials and methods The Zheleznyi Rog section is located on the Black Sea coast of Taman Peninsula (Fig. 2) (N4511006.100 E36 740 48.400 , Russia) and comprises well-exposed upper Sarmatian-Kimmerian sediments. Since its first description by Andrusov (1903), this geological section has been studied by paleomagnetic, palaeontological and lithological methods (Pevzner and Chikovani, 1978; Pevzner et al., 2003; Semenenko and Pevzner, 1979; Semenenko and Lulieva, 1982; Trubikhin, 1989; Chumakov et al., 1992; Chumakov, 2000; Popov and Zastrozhnov, 1998; Filippova, 2002; Rostovtseva, 2009; Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova and Golovina, 2011; Radionova et al., 2012; Chang et al., 2014). In the Zheleznyi Rog section, the total thickness of transitional Maeotian/ Pontian and Pontian sediments is approximately 145 m. Novorossian, Portaferian and Bosphorian sediments of the Pontian stage are defined in the Zheleznyi Rog section. The transitional Maeotian/Pontian beds (interval from 144.6 to
Fig. 1. Overview of the different time scales for the Mediterranean and Eastern Paratethys (Black Sea) in comparison with the international time scale.
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112.8 m) consist mostly of diatomaceous clays with Actinocyclus octonarius (Fig. 3). The Novorossian sediments (interval from 112.8 to 44.4 m) consist of clays, with the lower part of the section containing sporadic diatomite layers (diatomite marker beds SP, Ch, and N according to Radionova and Golovina, 2011). The first remains of Paradacna abichi related to Pontian malacofauna assemblage occur in sediments approximately 5e6 m above the top of the diatomite SP. The magnetic reversal event corresponding to the Chron C3An/C3r boundary occurs near the base of the diatomite Ch (Trubikhin, 1989; Radionova and Golovina, 2011; Radionova et al., 2012). The thin detrital limestone layer that occurs at the top of the transitional Maeotian/Pontian beds records local erosion and may mark the base of the Pontian (layer L. 39, Fig. 3). The noncalcareous clays are dominant at the top of the Novorossian. The Novorossian sediments are approximately 68 m thick. The Portaferian sediments are only 6 m thick (interval from 44.4 to 38.4 m). These sediments contain Congeria subrhomboidea and are lithologically varied. These beds include detrital shell limestone, clay breccia, a paleosol horizon, and sandy clay (Fig. 4). The Bosphorian sediments (interval from 38.4 to 0 m), devoid of
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Congeria subrhomboidea, consist of calcareous clays (clays containing 10e50% CaCO3), that are marked by cycles of light-grey and grey clays. The thickness of the Bosphorian section is up to 38 m. In terms of magnetostratigraphy most of the Pontian are characterized by reversed polarity with an episode of normal polarity near the base (Trubikhin, 1989; Pevzner et al., 2003; Vasiliev et al., 2011). The Kimmerian sediments that directly overlie the Pontian sedimentary succession at Zheleznyi Rog have normal polarity. The Upper Miocene sediments were investigated by cyclostratigraphic methods using the magnetic-susceptibility rocks and statistical techniques. Cyclostratigraphic methods are explained in many publications, including the well-known monograph of Weedon (2003). Magnetic susceptibility was measured with a “KM-7” magnetic susceptibility metre with a sensitivity of 106SI units (GF Instruments, Brno, Czech Republic). In total, 2145 measurements of the magnetic susceptibility of Maeotian/Pontian and Pontian rocks were obtained with an average vertical spacing of 7 cm. For the statistics, the PAST programme (Hammer et al., 2001) was used for spectral analysis (Lomb-Scargle periodograms), including REDFIT
Fig. 2. The Zheleznyi Rog (ZR) section. (A) Location of the study sediments and Arshintsevo section (AR). (B) Panoramic view of the Pontian sediments.
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Fig. 3. Lithological column of the investigated section and the results of the magnetic susceptibility (MS) measurements. (A) The interval between 0 and 44.4 m. (B) The interval between 44.4 and 112.8 m. (C) The interval between 112.8 and 144.6 m. The diatomite marker beds are presented (A, SP, Ch, N according to Radionova and Golovina, 2011). Paleomagnetic polarity patterns were obtained by Trubikhin (in Popov et al., 1996), Vasiliev et al. (2011) and Radionova et al. (2012). Paleontological data were obtained by Filippova (2002), Radionova and Golovina (2011), Radionova et al. (2012).
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Fig. 4. Portaferian sediments and the base of the Bosphorian in the Zheleznyi Rog (ZR) section. (A) Panoramic view of the top of Novorossian, Portaferian and the base of Bosphorian sediments. (B) Portaferian sediments. (C) Identified layers in Portaferian sediments.
(Schulz and Mudelsee, 2002) and wavelet analysis. Additionally, the frequency values of the Lomb-Scargle and REDFIT periodograms were used as targets for a Gaussian bandpass filter with the AnalySeries programme (Paillard et al., 1996). The Gaussian bandpassfilter data were compared with long-term insolation changes at the end Miocene (Laskar et al., 2004). The rock magnetic properties of the Upper Miocene samples of the Zheleznyi Rog section indicate greigite (a magnetofossil and early diagenetic mineral) as the main iron sulphide carrying the primary magnetization (Vasiliev et al., 2011; Chang et al., 2014). 3. Results 3.1. Magnetic susceptibility values The magnetic susceptibility (MS) of the transition Maeotian/ Pontian and Pontian rocks ranges widely with values from 0.016 to 0.937 103 SI units (Fig. 3). The rocks at the Maeotian/Pontian transition exhibit MS values ranging from 0.04 to 0.16 103 SI units. Novorossian rocks exhibit MS values ranging from 0.016 to 0.937 103 SI units. Extraordinarly high values of MS (from 0.52 to 0.937 103 SI) occur in clays of the upper part of the
Novorossian at the intervals 65.8e62.0 m and 59.2e51.6 m. Portaferian rocks exhibit MS values ranging from 0.03 to 0.19 103 SI units. The Bosphorian clays exhibit MS values from 0.05 to 0.32 103 SI units with higher values (up to 0.42 103 SI) at the top of these sediments. 3.2. Spectral analysis Spectral analysis of the MS data from Portaferian sediments clearly illustrates the lack of signal that passes the 95% and 99% confidence intervals (Fig. 5). The strongest peak visible in LombScargle and REDFIT periodograms (at 9.4 m) does not reach the 95% confidence interval. Also, the Portaferian succession (characterized by thickness up to 6 m) is too thin to clearly support the presence of a 9.4 m cycle. The wavelet reveals shorter period cycles, which differ from the periodicity at 9.4 m. Based on spectralanalysis results and lithological data, we infer that the Portaferian, which includes re-sedimented deposits, displays a poor record of astronomical cyclicity. Spectral analysis of the MS-data of lower Pontian (Novorossian) sediments suggests strong periodicity. The Lomb-Scargle periodogram reveals only one significant signal with periodicity at 59.7 m
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Fig. 5. REDFIT spectral analysis (left) and Wavelet analysis (right) of the magnetic susceptibility (MS) data from 38.4 to 44.4 m (A, B) and from 44.4 to 112.8 m (C, D).
which passes the 99% confidence interval. The REDFIT analysis supports peaks at 59.7, 3.1, 2.7 and 2.3 m that pass the 99% confidence intervals (Fig. 5C). Significantly, the REDFIT periodogram with frequency values transformed into depth-domain also displays the signal at 6.1 m (Fig. 6). This peak is supported by wavelet analysis that clearly illustrates the presence of a cycle between 5.6 and 7.4 m (Fig. 5D). To help identify Milankovitch cyclicity, we used the ratios between the observed periodicities. The predicted ratio of the long eccentricity period (400-kyr eccentricity cycle) to obliquity peak is 9.7:1. The predicted ratios of the obliquity period (41-kyr obliquity cycle) to the 24, 22 and 19 kyr precession peaks are 1.7:1, 1.9:1 and 2.2:1, respectively. The ratio of the signal at 59.7 to the peak at 6.1 m is 9.7:1. The ratios of the signal at 6.1 m to peaks at 3.1, 2.7 and 2.3 m are 1.9:1, 2.2:1 and 2.6:1, respectively. Based on these ratios, we suggest that the precession (signals at 3.1, 2.7 and 2.3 m), obliquity (signal at 6.1 m) and 400-kyr eccentricity (signal at 59.7 m) cycles
are expressed in the MS-data of Novorossian sediments. Eccentricity, obliquity and precession cycles have been defined in the Miocene and Pliocene sedimentary record of the Mediterranean (Lirer et al., 2009; Gunderson et al., 2012) and of the Eastern Paratethys (Popescu et al., 2006, 2010). Taking into account the changes in sedimentation rate, the peak at 6.1 m may be analogous to the signals at 7.1e7.8 m and 8.0e8.2 m that were detected in the MS-record of Maeotian/Pontian beds with Actinocyclus octonarius, and the Bosphorian sediments of the Zheleznyi Rog section, respectively (Fig. 6). In addition, precession cycles (signals at 3.0e3.2 and 4.0 m) were identified in the MS-data of Maeotian/Pontianbeds with Actinocyclus octonarius as well as the Bosphorian and Novorossian sediments (Fig. 6). The wavelet analysis of the Pontian sediments (0e112.8 m) and the whole succession (0e144.6 m) showed signals at 5.6e8.1 m and at 2.4e4.8 m (Fig. 7). The Gaussian filter centred at 6.1, 8.0 (midpoint of 7.8e8.2 m) m, 3.1 (mid-point of 3.0e3.2 m), and 4.0 m
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Fig. 6. Lomb-Scargle (left) and REDFIT (right) periodograms displaying periodicities in the intervals 144.6e112.8 m, (A, B); 112.8e44.4 m, (C, D); 38.4e0 m, (E, F) (modified from Rostovtseva and Rybkina (2014)).
revealed the presence of the 21 and 39 cycles in the whole succession (0e144.6 m) (Fig. 7). 4. Discussion 4.1. Paleoenvironment and chronostratigraphic framework The beginning of the Pontian was marked by a transgression (Popov et al., 2004). At that time, deep-water environments in which clays accumulated existed in the Black Sea (Popov et al., 2004). Based on the dominant brackish mollusk fauna, the salinity of the water was low, but it was not less than 5e8‰ (Popov et al., 2006). According to Radionova and Golovina (2011), the pulsing marine-water invasion and short-term connection with Eastern Mediterranean facilitated the appearance of coccoliths and marine diatoms during the Maeotian/Pontian transition and during the start of the Pontian. The end of the Novorossian was marked by a regression. In the Portaferian, the Eastern Paratethys was restricted, which caused the separation the Caspian Basin from the Euxinian Basin (Black Sea) in the northern part (Nevesskaya et al., 1986, 2003;
Popov et al., 2004, 2006). According to Krijgsman et al. (2010), the Portaferian represents a regressive event in the Dacic Basin during which the early Pontian ostracod fauna indicative of basinal conditions was replaced by littoral, fluvial and lacustrine species. The Bosphorian substage introduced by Andrusov (1923) in the Kerch-Taman region (Black Sea) corresponds to the transgressive event in the Paratethys. In the Dacic Basin, the beginning of the Bosphorian corresponds to a second bloom of ostracod fauna (Krijgsman et al., 2010) and to a lithological change to more basinal sequences (Jipa, 1997) in the East Carpathian Pontian sections. Biostratigraphic and paleomagnetic dating by Krijgsman et al. (2010) placed the Maeotian/Pontian boundary at 6.04 ± 0.01 Ma, and the Novorossian/Portaferian boundary at 5.8 ± 0.1 Ma. In the Dacic Basin, the Portaferian/Bosphorian boundary is dated at 5.5 ± 0.1 Ma. Snel et al. (2006) estimated the Maeotian/Pontian boundary date at 6.15 ± 0.11 Ma. The age of the Pontian/Kimmerian transition is 5.3 ± 0.1 Ma. The bases of the Portaferian and Bosphorian are dated at 6.0 and 5.6 Ma, respectively. The length of the Pontian stage is approximately 0.85 Myr. In the Pontian, the Eastern Paratethys (Euxinian-Caspian Basin) biogeographically belongs to the Dacic Basin (Popov et al., 2004).
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Fig. 7. Magnetic susceptibility (MS): a: original data; a Gaussian filter was applied centring at b: 8.0 (for intervals 144.6e112.8 m and 44.4e0 m) and 6.1 (for interval 112.8e44.4 m) m; c: 4.0 (for intervals 144.6e112.8 m and 44.4e0 m) and 3.1 (for interval 112.8e44.4 m) m; the Wavelet analysis: d (for the entire record, from 144.6 to 0 m).
4.2. Astronomical tuning Based on integrated paleomagnetic, palaeontological and lithological data, many authors place a paleomagnetic reversal in the lower part of the Pontian at 6.033 Ma (Trubikhin (in Popov et al., 1996); Krijgsman et al., 2010; Vasiliev et al., 2011; Radionova and Golovina, 2011; Radionova et al., 2012; Popov et al., 2013). Our spectral analysis suggests that the repetitive signals 6.1e8.2 m and 3.1e4.0 m probably record astronomical cyclicity. In our study, a Gaussian filter centred at 6.1e8.0 m (6.1 m for the Novorossian, 8.0 m for the Maeotian/Pontian transition and the upper Pontian) reveals the presence of 14 cycles in the interval from the paleomagnetic reversal in the lower part of the Pontian to the base of the Kimmerian in the Zheleznyi Rog section, (i.e. from 96 to 0 m) (Fig. 8). On the basis of the ratios between the observed periodicities, we infer that the peak at 6.1e8.2 m corresponds to the obliquity cycle (41,000 yr). Given this, the 96-m interval is estimated to have a duration of ~0.57 Myr. The Novorossian/Portaferian boundary is dated at ~5.65 (5.7) Ma. According to Krijgsman et al. (2010), the age of the base of the Portaferian in the Eastern Paratethys is 5.8 ± 0.1 (5.7e5.9) Ma. In the upper part of the Novorossian (from 65.8 to 59.2 m), the bases of intervals with extraordinarily high values of MS (up to 0.834 and 0.937 103 SI units) correlate to the glacial peaks TG 22 (5.79 Ma) and TG 20 (5.75 Ma), respectively (Shackleton et al., 1995; Hodell et al., 2001). These results are consistent with
palaeontological and lithological features. As shown by Radionova et al. (2012), the upper part of the Novorossian in the Zheleznyi Rog section (from 79 m and upward the section) is marked by the complete disappearance of calcareous nanoplankton and marine diatom species. Radionova and Golovina (2011) suggested that increased regression and disconnection with marine basins occurred at the end of the Novorossian. Based on cyclostratigraphic results, the disappearance of coccoliths and marine diatoms occurred at ~5.88 Ma. The extraordinarly high values of MS can be explained by restricted-basin circulation and increased productivity of diagenetic sulphide minerals during glacial events. Peaks TG 20e22 are both marked by a significant drop in global sea level (on the order of 50 m) (Shackleton et al., 1995; Hodell et al., 2001). The stratigraphic level of 5.97 Ma, which relates to the MSC onset and glacial peak TG32 and correlates with the base of the “stagnation horizon” (from 93.6 to 86.8 m). This “stagnation horizon” is represented by clays containing manganese-bearing minerals. It was first described by Andrusov (1903) in the Zheleznyi Rog section. Thus, most Novorossian sediments (from 93.6 m and upward the section) in the relatively deep-water Zheleznyi Rog section can be considered analogous to the MSC onset and the first evaporitic stage (i.e. Roveri et al., 2014: Primary Lower Gypsum 5.97e5.6 Ma; Bache et al., 2015: peripheral evaporites 5.97e5.6 Ma) in the Mediterranean. The base of thin detrital limestone layer (layer L.39, Fig. 3) that is located at the top of transitional Maeotian/Pontian sediments is dated at ~6.1 Ma.
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Fig. 8. Original magnetic susceptibility (MS) data (logarithmically transformed and detrended) filtered according to the high-frequency signal revealed by the periodograms in Fig. 6. Gaussian filtering was applied, centring at 8.0 m (for intervals 144.6e112.8 m and 44.4e0 m) and 6.1 m (for interval 112.8e44.4 m). The sporadic diatomite layers are presented (A, SP, Ch, N; diatomites SP, Ch and N according to Radionova and Golovina, 2011). Paleomagnetic polarity patterns were obtained by Trubikhin (in Popov et al., 1996), Vasiliev et al. (2011) and Radionova et al. (2012). Paleontological data were obtained by Radionova and Golovina (2011) and Radionova et al. (2012). The numbers in the circles are the set of cycles. MSC ¼ the Messinian Salinity Crisis. MS ¼ magnetic susceptibility.
The Maeotian/Pontian beds with Actinocyclus octonarius (interval from 144.6 to 114.6 m) accumulated from ~6.3 to 6.1 Ma. This age determination agrees well with our previous studies
(Rostovtseva and Rybkina, 2014; Rybkina and Rostovtseva, 2014). Our results show a poor astronomical record in the thin Portaferian sequence, which includes a detrital shell limestone and clay
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breccias. As shown by Krijgsman et al. (2010) the base of the Portaferian corresponds to a fall in Paratethyan water level. The Gaussian filter centred at 6.1e8 m reveals low obliquity in this part of the Zheleznyi Rog section. The Bosphorian sediments (0e38.4 m) display the presence of 4e5 cycles (4.8 cycles, for signal at 8 m) related to the obliquity period. This gives a duration of ~205 kyr for this sedimentary succession. According to Trubikhin (1989) and Vasiliev et al. (2011), the base of the Kimmerian with normal polarity in the Zheleznyi Rog section correlates to the Thvera (C3n.4n). Given the age of 5.235 Ma for C3r/C3n (Hilgen et al., 2012), the base of the Bosphorian in the Zheleznyi Rog section can be dated as ~5.45 (5.5) Ma. Given these determination, the Black Sea Bosphorian correlates to the Upper Gypsum and the Lago Mare biofacies characterized by Paratethyan fossil assemblages. Based on biostratigraphic and paleomagnetic results, the base of the Bosphorian in the Dacic Basin is variously dated at 5.5 ± 0.1 (5.4e5.6) Ma (Krijgsman et al., 2010), 5.6 Ma (Snel et al., 2006), or 5.45 Ma (Popescu et al., 2006; Bache et al., 2012). The Bosphorian beds were defined by Andrusov (1923) in the Kerch-Taman region (Black Sea) including the Zheleznyi Rog section. Subsequently, numerous researchers have confirmed the Bosphorian in the Zheleznyi Rog section (Kolesnikov, 1940; Trubikhin, 1989; Popov et al., 1996; Pevzner et al., 2003; Radionova et al., 2012). In the Zheleznyi Rog section, the Bosphorian beds lie with apparent conformity on the Portaferian sediments, and they probably reflect a change from regressive lowstand conditions to transgressive conditions. According to Krijgsman et al. (2010), global warming and more humid conditions after TG12 at 5.5 Ma (Hodell et al., 2001; Hilgen et al., 2007) led to the positive hydrological change (overflow) in the Paratethys, which further caused a widespread transgression in the late Pontian. As proposed by Bache et al. (2012), the re-flooding of the Mediterranean Basin by Atlantic waters occurred at 5.46 Ma and the marine connection with the Dacic Basin occurred at 5.45 Ma. In addition to detecting obliquity cycles, spectral analysis suggests strongly expressed precession periodicity (signal at 4 m) in the Bosphorian sedimentary succession. The Upper Gypsum and the Lago Mare Unit at Eraclea Minoa (Mediterranean) also display related precession-driven climate oscillations (Hilgen et al., 2007; Bache et al., 2012). The level at 5.33 Ma, which corresponds to the Miocene/Pliocene boundary in the Mediterranean, appears to correlate with Layer 64 of the Pontian in the Zheleznyi Rog section (Fig. 8). Based on integrated biostratigraphic, paleomagnetic and cyclostratigraphic results, we estimate the dates for the base and the top of Portaferian in the Zheleznyi Rog section to be ~5.65 Ma and ~5.45 Ma, respectively. Taking into account the 6 m thickness of sediments and the presence of re-sedimented deposits in the record of Portaferian as well as obtained astronomical cycles in metres, we propose a ~150e160 ky hiatus between the lower and upper Pontian. This is consistent with the concept of intra-Pontian unconformity (Gillet et al., 2007; Suc et al., 2015) and suggests that the Novorossian/Portaferian transition was related to a phase of high-amplitude Mediterranean sea-level drop and the onset of the Messinian Erosional Surface (MES) in the Black Sea (Tari et al., 2015, 2016; Krezsek et al., 2016). During the Messinian, a major sea-level drop in the Mediterranean occurred from 5.6 to 5.46 Ma (Clauzon et al., 1996; Bache et al., 2012). The TG14 (5.58 Ma) and TG12 (5.54 Ma) glacial events took place in this stage of the MSC. If the inferred hiatus was absent in intra-Pontian sedimentary record in the Zheleznyi Rog section, the top of the Miocene here could be dated at ~5.46 (5.5) Ma based on the presence of the 14 obliquity cycles in the uppermost 96 m of the Pontian. However, this would be inconsistent with (1) the presence of a 38-m-thick
Bosphorian succession in the Zheleznyi Rog section with the base dated in the Dacic Basin as ~5.6e5.5 Ma (Snel et al., 2006; Krijgsman et al., 2010); (2) the transgressive sequence of the uppermost Zheleznyi Rog Pontian (i.e. Bosphorian) considering that the period from 5.6 to 5.46 Ma is a major sea-level drop in the Mediterranean (Clauzon et al., 1996; Bache et al., 2012); and (3) the presence of the thin Portaferian sedimentary succession with resedimented deposits and erosional surfaces. If the 14 cycles in the uppermost 96 m of the Pontian correlates to precession changes, the top of the Miocene in the Zheleznyi Rog section dates at ~5.69 Ma. In that case, the Pontian/Kimmerian boundary would be marked by hiatus of at least ~460 kyr that disagrees with palaeontological and lithological data including the presence of Bosphorian beds in the Zheleznyi Rog section. Thus, we infer that the Novorossian/Portaferian transition in the Zheleznyi Rog section corresponds to the development of the Messinian Erosional Surface (MES). In the Taman sections, the Azovian/Kamyshburunian boundary is marked by replacement of clay sediments by red oolitic iron ores. This transition was described by Krijgsman et al. (2010) as the “red sequence” in the Zheleznyi Rog section. The Azovian beds, with sedimentary features similar to upper Pontian sediments, are characterized by an erosional base that lacks significant truncation of Miocene deposits. The lower part of the Azovian sediments is characterized by reversed polarity (Radionova et al., 2012). The top of the Azovian is characterized by a regressive succession and normal polarity related to the Thvera. In the Black Sea Basin, the Miocene/Pliocene boundary commonly is placed at the Bosphorian/ Azovian boundary (Nevesskaya et al., 2003; Radionova et al., 2012). Our results allowed calculation of average sedimentation rates. For the Maeotian/Pontian transition the sedimentation rate was estimated at 16.3 cm/kyr. For the Novorossian, the sedimentation rate was estimated at 13.5 cm/kyr, and for the Bosphorian it was estimated at 19.5 cm/kyr. These rates are consistent with the mean rate of deposition in the Black Sea (Denisov, 1998). The recent sedimentation rate in the Black Sea varies from 15 to 760 cm/kyr for deep-water and shelf environments (Denisov, 1998). During the Pleistocene and Holocene, the mean sedimentation rate in the Black Sea deep basin has been 10e50 cm/kyr (Degens et al., 1978). According to Popescu et al. (2010: Fig. 6), the sedimentation rate in the Black Sea (Site 380) is 13 cm/kyr for the latest Messinian and the earliest Zanclean (5.46e5.1 Ma). The presence of a 41-kyr periodicity in the studied sedimentary record may be explained by obliquity-driven changes in highlatitude insolation (more tilt implying more sunlight of higher latitudes). An insolation gradient may be recorded in the Miocene sediments of the Taman region, which accumulated between low and high latitudes in the Northern Hemisphere (~45 N) (Rybkina et al., 2015). In this study, the cyclostratigraphic estimates obtained by Gaussian filtering at 6.1e8.0 m (obliquity cyclicity) agrees with the results of the bandpass filtering centred at 3.1e4.0 m (precession cyclicity). 5. Conclusions Astronomical tuning of the Maeotian/Pontian transition and the Pontian sedimentary record at the Zheleznyi Rog (Taman region, Black Sea Basin) confirms that the Pontian began at ~6.1 Ma. The Maeotian/Pontianbeds with Actinocyclus octonarius (interval from 144.6 to 112.8 m) were deposited from ~6.3 to 6.1 Ma. The Novorossian sediments extending from the base “stagnation horizon” (93.6 m) to the Novorossian/Portaferian boundary correspond to the first MCS step (5.97e5.6 Ma). The TG 22 (5.79 Ma) and TG 20 (5.75 Ma) glacial events are reflected in the uppermost Novorossian
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record with extraordinarily high values of MS (levels 65.8 and 59.2 m). In the Novorossian, the final phase of marine invasion occurred no later than ~5.88 Ma. The estimated ages of base and the top of Portaferian in the Zheleznyi Rog section are ~5.65 Ma and ~5.45 Ma, respectively. The Portaferian corresponds to the second MSC step, which is marked by development of the Messinian Erosional Surface (MES). The Novorossian/Portaferian boundary is marked by a hiatus of ~150e160 kyr that agrees well with the presence of re-sedimented deposits and erosional boundaries in Portaferian sedimentary sequence and the concept of intra-Pontian unconformity (Gillet et al., 2007; Suc et al., 2015). The Bosphorian section that corresponds to the transgressive phase in Black Sea Basin is analogous to the re-flooding of the Mediterranean (Bache et al., 2012) and the third Lago Mare episode (Popescu et al., 2015), both of which were caused by a high sea-level connection between the Mediterranean and Eastern Paratethys. The top of the Bosphorian dates at ~5.27 Ma. On the basis of astronomical cyclicity data, the Pontian sedimentary record in the Zheleznyi Rog section dates at ~0.67 Myr. However, the length of the Pontian stage is at least ~830 kyr (from 6.1 to 5.27 Ma), taking into account integrated biostratigraphic, paleomagnetic and sedimentological data. In the MS-data of this study, the peaks at 6.1e8.2 m and at 3.0e4.0 m related to the obliquity and precession cycles, respectively. During the Pontian, and at the end of the Maeotian, the average sedimentation rate varied from 13.5 to 19.5 cm/kyr. Acknowledgements We are grateful to Valery M. Trubikhin, Irina A. Goncharova, Natalia Yu. Filippova, Larisa A. Golovina and Sergey V. Popov, and thank them for their fruitful discussions. References Andrusov, N., 1903. Geological researches at the Taman Peninsula. Mater. Geol. Russ. 21, 257e383. Andrusov, N., 1917. In: Karpinsky, A.P. (Ed.), Pontian stage. Geology of Russia, Petrograd 4 (2), 1e41. Andrusov, N., 1923. Apsheronian stage. Proc. Geol. Comm. 110, 294. Bache, F., Popescu, S.-P., Rabineau, M., Gorini, C., Suc, J.-P., Clauzon, G., Olivet, J.-L., Rubino, J.-L., Melinte-Dobrinescu, M.C., Estrada, F., Londeix, L., Armijo, R., Meyer, B., Jolivet, L., Jouannic, G., Leroux, E., Aslanian, D., Dos Reis, A.T., Mocochain, L., Dumurd zanov, N., Zagorchev, I., Vesna Lesi c, V., Tomi c, D.M., Namık Cþagatay, M.N., Brun, J.-P., Sokoutis, D., Csato, I., Ucarkus, G., Ҫakır, Z., 2012. A two step process for the reflooding of the Mediterranean after the Messinian Salinity Crisis. Basin Res. 24, 125e153. Bache, F., Gargani, J., Suc, J.-P., Gorini, C., Rabineau, M., Popescu, S.-P., Leroux, E., Do Couto, D., Jouannic, G., Rubino, J.-L., Olivet, J.-L., Clauzon, G., Dos Reis, A.T., Aslanian, D., 2015. Messinian evaporite deposition during sea level rise in the Gulf of Lions (Western Mediterranean). Mar. Pet. Geol. 66, 262e277. Chang, L., Vasiliev, I., van Baak, C., Krijgsman, W., Dekkers, M.J., Roberts, A.P., Fitz, Gerald J.D., van Hoesel, A., Winklhofer, M., 2014. Identification and environmental interpretation of diagenetic and biogenic greigite in sediments: a lesson from the Messinian Black Sea. Geochem. Geophys. Geosyst. 15, 3612e3627. Chumakov, I.S., Byzova, S.L., Ganzey, S.S., 1992. Geochronology and Correlation of Late Cenozoic Paratethys. Nauka, Moscow, pp. 1e96. Chumakov, I.S., 2000. On the Problem of Lower Pontian (Novorossian Substage) EuxinianeCaspian, vol. 3. Moscow University Geology Bulletin, pp. 17e23. Clauzon, G., Suc, J.-P., Gauter, F., Berger, A., Loutre, M.-F., 1996. Alternate interpretation of the Messinian Salinity Crisis: controversy resolved? Geology 24 (4), 363e366. Clauzon, G., Suc, J.-P., Popescu, S.M., Marunteanu, M., Rubino, J.-L., Marinescu, F., Jipa, D., Melinte, M.C., 2005. Influence of the Mediterranean sea level changes over the Dacic Basin (Eastern Paratethys) in late Neogene. The Mediterranean Lago Mare deciphered. Basin Res. 17, 437e462. Degens, E.T., Stoffers, P., Golubic, S., Dickman, M.D., 1978. Varve chronology: estimated rates of sedimentation in the Black Sea deep basin. US Government Printing Office, pp. 499e508. Denisov, V.I., 1998. Regularities of Formationsuspended Materialin the BlackSea. Abstract of PhD dissertation. Rostov State University, Rostov-on-Don Press, p. 25.
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