Integrated Stratigraphy and Astronomical Tuning of Lower-Middle

ARTICLE IN PRESS

Quaternary International xxx (2009) 1–12

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Integrated stratigraphy and astronomical tuning of lower–middle Pleistocene Montalbano Jonico section (southern Italy)

N. Ciaranfi a,*, F. Lirer b, L. Lirer c, L.J. Lourens d, P. Maiorano a, M. Marino a, P. Petrosino c, M. Sprovieri b, S. Stefanelli a, M. Brilli e, A. Girone a, S. Joannin f, N. Pelosi b, M. Vallefuoco b a Dipartimento di Geologia e Geofisica, Universita` di Bari, Via E. Orabona 4, 70125 Bari, Italy b Istituto per l’Ambiente Marino Costiero (IAMC) Sede Napoli - CNR, Calata Porta di Massa, Interno Porto di Napoli, 80133, Napoli, Italy c Dipartimento di Scienze della Terra, Universita` degli Studi di Napoli Federico II, L.go San Marcellino 10, 80138 Napoli, Italy d Faculty of Geosciences, Department of Earth Sciences, Utrecht University, Utrecht, The Netherlands e Istituto di Geologia Ambientale e Geoingegneria (IGAG)dCNR, Via Bolognola 7, 00138 Rome, Italy f UMR 5125 PEPS, CNRS, France; Universite´ Lyon 1, Campus de La Doua, Baˆtiment Geóde, 69622 Villeurbanne Cedex, France article info abstract

Article history: Astronomical calibration of the lower–middle Pleistocene Montalbano Jonico section located in the Available online xxx Lucania Basin (Southern Italy) is presented. Previous papers widely discussed the integrated stratigraphy (calcareous nannofossils, sapropel stratigraphy, benthic and planktonic oxygen stable isotopes) and the paleoenvironmental features of this section and its potential suitability for the selection of the Middle Pleistocene Global Stratotype Section and Point (GSSP). In this study, new planktonic d18O data, additional biostratigraphical constraints and new tephrochronology on volcaniclastic layers occurring within the studied record are reported. The new chronostratigraphic framework provides a robust base for correlation of the oxygen isotope stratigraphy for the Montalbano Jonico section with the glacial and interglacial fluctuations of the Oceanic and Mediterranean d18O reference deep-sea records. Specifically, the lower part of the Montalbano Jonico section (Interval A) provides correlation of the planktonic and benthic d18O cycles to Marine Isotope Stage (MIS) 36 to MIS 23. Interval A includes a distinct peak of left-coiled neogloboquadrinids, the Globoratalia crassaformis influx, the First Occurrence of Gephyrocapsa omega, and the First Common Occurrence and Last Common Occurrence of Reticulofenestra asanoi. These stratigraphical constraints support the tuning of five sapropel layers included in this part of the section to insolation cycles i-112, i-104, i-102, i-90 and i-86. The upper part of the section (Interval B), which includes the temporary disappearance (td2) of G. omega and tephra layer V5, Ar/Ar age dated at 719.5 12.6 ka, is consistent with identification of MIS 22 to MIS 16 in the planktonic d18O pattern. The d18O time series of the whole section was reconstructed using the midpoints of individual sapropels and their correlative precession minima, visual comparison of the d18O pattern with the record available at the Mediterranean ODP Site 975, and, in the upper part of the section, the Ar/Ar age of tephra V5. The developed astronomical tuning revealed that the Montalbano Jonico section covers an interval from 1240 ka to 645 ka. A significant change in sedimentation rate occurs between Intervals A (0.53 m/ky) and Interval B (0.91 m/ky) at about 870 ka and is consistent with a sea-level drop from a bathyal to a circalittoral environment. Bioevents recognised in the Montalbano Jonico section have been dated according to the astronomical calibration, and age assignments of tephra V1–V4 and V6–V9 are also proposed. The Montalbano Jonico section fills the gap between the top of the Vrica section and the base of the Ionian informal Middle Pleistocene stage, and represents a Mediterranean reference section for the Mid-Pleistocene transition. Ó 2009 Elsevier Ltd and INQUA. All rights reserved.

1. Introduction

Astronomical dating of late Neogene sedimentary sequences from the Mediterranean has now been well established and forms the backbone of the Astronomical Tuned Neogene Time Scale * Corresponding author. (ATNTS2004; Lourens et al., 2004). The dating method is purely E-mail address: [email protected] (N. Ciaranﬁ). based on the calibration of sedimentary cycles such as sapropels,

Please cite this article in press as: Ciaranﬁ, N., et al., Integrated stratigraphy and astronomical tuning of lower–middle Pleistocene..., Quaternary International (2009), doi:10.1016/j.quaint.2009.10.027 ARTICLE IN PRESS

2 N. Ciaranfi et al. / Quaternary International xxx (2009) 1–12 carbonate cycles, diatomite layers, combined with several (Cita and Castradori, 1995; Ciaranfi et al., 1997; Ciaranfi and D’Ales- geochemical and petrophysical climate sensitive proxies, to the sandro, 2005; Cita et al., 2006, 2008), although the absence of a clear computed time series of the quasi-periodic variations of Earth’s paleomagnetic signal in the succession prevents the recognition of orbit and axis (Hilgen, 1991a,b; Hilgen et al., 1995, 2000a,b, 2003; the Brunhes/Matuyama boundary, the primary criterion for the Hilgen and Krijgsman, 1999; Krijgsman et al., 1999; Langereis et al., definition of GSSP.This paper presents the astronomical calibration of 1997; Lourens et al., 1996a,b, 1998, 2001; Sierro et al., 2001, 2003; the composite Montalbano Jonico section based on the previously Lourens, 2004; Abels et al., 2005). This time scale provides precise developed benthic and planktonic stable oxygen isotope stratig- and accurate numerical ages, not only for the sedimentary cycles, raphy, together with new planktonic d18O data, additional biostrati- but also for calcareous plankton events and magnetic polarity graphical constraints and new tephrostratigraphic study of the reversals recorded in the tuned sections. Accordingly, all the middle volcaniclastic layers occurring in the studied record. to late Neogene stages are by now defined in tuned land-based marine sections in the Mediterranean region. The Pleistocene part 2. Study section of the ATNTS2004 is based on a few ODP Sites (964, 969 and 967) and piston cores (RC9-181, MD84641, KC01B, KC01), with the The lower–middle Pleistocene Montalbano Jonico composite exception of the Lower Pleistocene interval in which data from the section crops out in the Lucania Basin (Balduzzi et al.,1982), a minor land-based marine sequences of Vrica and Singa (Calabria, Italy) basin of Bradano Trough (Casnedi, 1988) between the Apennines were also included. The Vrica section includes the GSSP of the Chain to the west and the Apulia foreland eastward (Fig. 1A). It Pliocene–Pleistocene boundary (Aguirre and Pasini, 1985). At belongs to the argille subapennine unit (Azzaroli, 1968) and is present, the Calabrian Stage and the Lower/Middle and Middle/ about 450 m thick consisting of coarsening upwards deposits from Upper Pleistocene boundaries should be regarded as informal (Cita muddy clays to muddy sands and including nine volcaniclastic and Castradori, 1995; Cita et al., 2006, 2008). layers (V1–V9) (Fig. 2). Locally, some terraced marine deposits and The Montalbano Jonico composite section, cropping out in sandy-conglomerate bodies of continental origin lie horizontally on Southern Italy, due to its continuity and exposure condition, together the muddy succession (Ciaranfi et al., 2001). The whole section has with the available detailed integrated stratigraphy, has been been reconstructed in the field by means of selected stratigraphic proposed as the reference succession for the upper portion of Cala- sections including volcaniclastic layers, diagnostic macrobenthic brian Stage (Cita et al., 2008). The section can fill the gap between the assemblages and biostratigraphic data (Ciaranfi et al., 2001; top of Vrica section (according to Lourens et al., 1998 the top of Vrica D’Alessandro et al., 2003; Stefanelli, 2003; Maiorano et al., 2004). A section is directlyabove insolation cycles i-116) and the base of Ionian stratigraphical gap divides the Montalbano Jonico section into two informal Middle Pleistocene stage. Further, the section has been parts: the lower part, termed ‘‘Interval A’’ 168 m thick and the considered suitable for the selection of the Middle Pleistocene GSSP upper part, termed ‘‘Interval B’’ 280 m thick.

Fig. 1. Location map of Montalbano Jonico section (A) and of Ocean Drilling Program sites cited in the present paper (B).

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Fig. 2. Lithological sequence of Montalbano Jonico section with indication of a few volcaniclastic layers.

The main results concerning stratigraphical data and paleo- 3. Methods environmental reconstruction are shown in Fig. 3. Several deep- ening–shallowing cycles forming a regressive succession and the 3.1. Stable Isotopes middle Pleistocene infill of Lucania Basin have been recognised based on micro- and macro-invertebrate benthic assemblages, Oxygen and carbon stable isotope analyses throughout the which mainly indicate changes in paleo-bathymetry from bathyal Montalbano Jonico composite section were partially presented in to circalittoral environments (D’Alessandro et al., 2003; Stefanelli, previous papers (Brilli et al., 2000; Ciaranfi et al., 2001; Stefanelli, 2003; Ciaranfi and D’Alessandro, 2005; Girone, 2005). Specifically, 2003; Maiorano et al., 2004; Stefanelli et al., 2005; Joannin et al., benthic paleocommunities from Interval A are clearly indicative of 2008). In detail, benthic and planktonic d18O and d13C values were upper slope environments, with a maximum depth of about 500 m, measured on benthic foraminiferal species Cassidulina carinata and while paleocommunities of Interval B indicate outer- to inner shelf on planktonic foraminifer Globigerina bulloides. settings (D’Alessandro et al., 2003; Stefanelli, 2003). The whole Isotopes of planktonic foraminifera (202 samples) from Interval section represents the regressive part of a third-order cycle that A and benthic foraminifera (402 samples) from Intervals A and B of includes higher fourth- (Intervals A and B) and fifth-order cyclicity the Montalbano section were measured at ‘‘Centro di Studio per il as a consequence of tectonic processes with superimposed Milan- Quaternario e l’Evoluzione Ambientale’’ CNR Laboratory (Rome). kovitch scale climate cyclicity (Ciaranfi et al., 1997, 2001). About 40 specimens of G. bulloides and C. carinata were handpicked The section spans the interval across the small Gephyrocapsa from fraction >125 mm with a mean sampling resolution of 0.83 and Pseudoemiliania lacunosa zones (Marino, 1996; Maiorano et al., and of 1.2 m, respectively, and were measured on a Finnigan Mat 2004). Quantitative biostratigraphic data reveal the following bio- 252 mass spectrometer with KIEL II carbonate preparation device events: the First Common Occurrence (FCO) of Reticulofenestra (see Brilli et al., 2000 for details). asanoi, the First Occurrence (FO) of Gephyrocapsa omega, the Last Stable isotopes from Interval B of Montalbano section were Common Occurrence (LCO) of Reticulofenestra asanoi, the beginning measured at the Istituto Ambiente Marino Costiero (IAMC-CNR), and the end of the second temporary disappearance (‘‘td 2’’ in isotope geochemistry laboratory in Naples. There, w20 specimens Maiorano and Marino, 2004)ofG. omega. An influx of Globorotalia of G. bulloides, were handpicked from a total of 140 samples with crassaformis has been also recognised in the lower part of Interval A a mean 1.5 m sampling resolution. Samples were measured by (Joannin, 2007). Sapropel layers are observed in the Interval A, automated continuous flow carbonate preparation GasBenchII based on benthic foraminiferal analyses and on preliminary device (Spo¨tl and Vennemann, 2003) and a ThermoElectron Delta planktonic d18O data (Stefanelli, 2003, 2004; Stefanelli et al., 2005). Plus XP mass spectrometer at the IAMC-CNR (Naples) isotope The afore-mentioned bioevents are recognised on a wide scale and geochemistry laboratory. Acidification of samples was performed at have been precisely dated by Lourens et al. (2004) and Raffi et al. 50 C. An internal standard (Carrara Marble with d18O ¼2.43& vs. (2006). Their correlation (Fig. 4) with the astronomically calibrated VPDB and d13C ¼ 2.43& vs VPDB) was run every 6 samples and the sapropel stratigraphy available in Mediterranean area (Fig. 1B) (de NBS19 international standard was measured every 30 samples. Kaenel et al., 1999; Raffi, 2002; Maiorano and Marino, 2004) Standard deviations of carbon and oxygen isotope measures were provides a powerful tool for the astronomical tuning of the lith- estimated at 0.1& and 0.08&, respectively. All isotope data are ostratigraphic record of Montalbano composite section. A paleo- reported in per mil (&) relative to the VPDB standard. magnetic study was also carried out in several intervals of the section in order to precisely locate the position of the Brunhes– 3.2. Tephrostratigraphic analysis Matuyama reversal. Unfortunately the results indicate that the section has been re-magnetised during the Brunhes Chron (Sag- The thickness of the volcaniclastic layers is ca 2 cm, except for notti et al., 2009). V5, which is some 20 cm thick. All samples were strongly altered

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Fig. 3. Quantitative distribution of selected calcareous nannofossils (Maiorano et al., 2004) and paleo-depth curves according to distribution of benthic foraminifera and macrobenthic fauna. mainly within the glassy matrix, generally presenting a clayey Centro Interdipartimentale di Servizio per Analisi Geomineralogiche consistence, due to partial to complete devitrification. In order to (CISAG) at the University of Naples Federico II. Instrument calibration eliminate the clayey fraction, samples were repeatedly washed in was based on international mineral and glass standards. Individual deionised water keeping the water-sample mixture for at least 24 h analyses of glass shards with total oxide sums lower than 95% were on an oscillating platform. During each washing step the suspended excluded. The results represent the average value of at least 5 point fraction was removed. The final mixture was washed in an ultra- analyses for each sample, recalculated to 100% water free. sonic tank for at least four cycles of 6 h each, and then rewashed in 40Ar/39Ar dating was performed on sample V5; sanidine grains a diluted acetic acid solution. The residual solid material was oven- in the size range 0.1–0.3 mm were handpicked from the loose dried for 24 h at 80 C and finally sieved at 14 intervals. The single sample after pre-treatment. Radiometric dating was carried out at grain size classes were carefully investigated under a binocular the Department of Geology and Geophysics of the University of microscope. This observation made it possible to identify samples Wisconsin in Madison. Irradiation, analysis and general interpretive containing glass fragments and crystal grains. The primary tephra principles are described in detail by Smith et al. (2008). layers were distinguished from the epiclastic ones since the former showed a homogeneous grain-size distribution and contained 4. Results and discussion a high percentage of jagged glass fragments, the latter mainly contained foraminiferal shells, rare limestone lithic fragments and 4.1. Chemical and mineralogical composition of volcaniclastic layers sub-rounded crystal grains. Due to the intense argillification of the layers, loose grains extracted from the samples were investigated in A detailed description of the lithological composition of the preference to thin sections. loose grains extracted from the samples, referred to the 24 fraction, Major-element analysis on glass fragments was performed on and the semi-quantitative evaluation of mineral content are a SEM JEOL JSM 5310 (15 kV, ZAF Correction Routine) with EDS at reported in Table 1. Acicular glass shards of V2 layer, glass

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Fig. 4. Biostratigraphic correlation between Montalbano Jonico composite section and ODP sites 964 and 967. Calcareous nannofossil events are from Maiorano et al. (2004) and this study at Montalbano Jonico section, and from Maiorano and Marino (2004) at Sites 964 and 967. Globorotalia crassaformis influx at Montalbano Jonico section is from Joannin (2007). Sapropel stratigraphy is according to Emeis et al. (2000) at Site 964, and to Kroon et al. (1998) at Site 967. Corrected composite depth (ccd) at Site 964 is from Lourens (2004). fragments, sanidine crystals and minor clinopyroxene and biotite the phonolite field, the V5 and V7 in the trachyte field. Chemical grains of V5 layer are shown in Fig. 5A and B, respectively. composition of crystal grains was determined also on V1 and V6. Among the tephra layers identified throughout the successions, Among all the aforementioned investigated layers, V5 is the only glass composition could be obtained only on V2, V5 and V7 layers. one composed of sub-angular glass fragments with rare lava lithic The chemical analysis of the glass fragments is reported in Table 2. clasts and shows a sharp basal contact with the underlying The chemical compositions were classified according to Total Alkali– deposits. These features suggested the primary emplacement from Silica diagram (TAS; Le Bas et al.,1986)(Fig. 6). The V2 sample plots in a pyroclastic column. The fine dimension of glass shards and the

Table 1 Main features of investigated pyroclastic layers, with semi-quantitative evaluation of crystal grains percentage (vol%). X ¼ 25%, XX ¼ 50%, XXX ¼ 75%.

Sample Thickness Lithology and texture Type of juvenile clasts (24) Presence Type of crystal grain of the layer of crystal grains (24) V1 <2 cm Silty-sized pale grey layer No juvenile clast was preserved after pre-treatment. XXX Plagioclase, clinopyroxene, with clayey matrix Crystal grains are embedded by a thin glass border orthopyroxene V2 <2 cm Silty-sized grey layer Thin glass shards mainly y-shaped XXX Feldspar, green clinopyroxene, with clayey matrix. brown clinopyroxene, biotite V5 20 cm Silty-sand sized whitish layer Tubular vesicles whitish pumice fragments. XX Feldspar, green clinopyroxene, with clayey matrix Glass shards with tubular and ovoidal vesicles brown clinopyroxene, biotite V6 <2 cm Silty-sized grey layer No juvenile clast was preserved after pre-treatment XXX Feldspar, green clinopyroxene, with clayey matrix sphene

V7b <1 cm Silty-sized pale grey layer Rare badly preserved pumice fragments X Feldspar, green clinopyroxene with clayey matrix with tubular vesicles

V7t <1 cm Silty-sized pale grey layer Mostly analcimised pumice fragments XX Feldspar, green clinopyroxene with clayey matrix with tubular vesicles

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16 V2 15 V5 V7 14 phonolite 13 O 2 12 tephri-phonolite trachyte O+K

2 11 foidite Na 10 phono-tephrite 9 latite

8 tephrite 7 40 45 50 55 60 65 70

SiO2

Fig. 6. Total Alkali–Silica (TAS) plot for investigated tephra layers.

explosive volcanic event, a direct emplacement by a pyroclastic cloud can be excluded.

4.2. Tephrochronology

Many volcanic sources were active in southern Italy during the Pleistocene (Fig. 7A and B). By comparing the obtained results with existing geochemical, chronological and tephrostratigraphical data

8° 14° 16° 18° A N

44° 44° Mt. Amiata Adriatic Sea Cimini

Vico Sabatini 42° Ernici 42° Alban Hills Fig. 5. Microphotographs of glass shards selected from sample V2 (A) and of total Roccamonfina content of sample V5 (B). Campi Flegrei Vulture Procida I. Somma- Ischia I. Vesuvio bubble walls preserved shape make it possible to hypothesise the 40° provenance from a co-ignimbrite cloud, even if a pyroclastic fall Tyrrhenian Sea emplacement mechanism cannot be excluded. The other layers due to the reduced thickness, the low percentage of glass fragments, the Ustica I. ITA Aeolian I. Ionian Sea prevalence of foraminifera shells, and the scarce occurrence of LY 38° quartz and muscovite grains, can be interpreted as remobilised Etna volcanoclastic layers. For those layers, although sourced from an Tyrrhenian sea Pantelleria I. 0 100 km 12° 14° 16° 18° Table 2 SEM-EDS glass composition, recalculated to 100% water free, of all the investigated tephra samples. n ¼ number of averaged analyses. FeOtot ¼ Total Fe as FeO. B Ma Sample V2 V5 V7 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 pr. Mt. Amiata n 19 11 5 Vulsini Vico SiO2 58.69 0.81 63.79 0.76 63.71 0.24 Sabatini Alban Hills TiO2 0.19 0.04 0.45 0.08 0.29 0.07 Roccamonfina Al2O3 19.48 0.43 17.85 0.53 18.41 0.17 Campi Flegrei FeOtot 4.07 0.16 2.78 0.13 1.54 0.09 No volcanic Ischia Island activity Somma-Vesuvio MnO 0.05 0.01 0.13 0.01 0.00 0.10 Vulture Extint Aeolian I. MgO 0.36 0.16 0.45 0.23 0.36 0.07 volcano Ustica CaO 1.96 0.06 1.38 0.06 1.71 0.09 Active Etna volcano Pantelleria Na2O 7.22 0.64 6.02 0.45 5.61 0.21 K2O 7.82 0.80 7.00 0.62 8.07 0.16 Cl 0.16 0.08 0.15 0.09 0.30 0.10 P O 0.15 0.13 n.d. 2 5 Fig. 7. (A) Location of main Italian volcanic centres active in the last 1 Ma. (B) Chro- Total 100.00 100.00 100.00 nogram of activity at main volcanic centres active in the last 1 Ma (from Russo Ermolli Real sum 95.96 96.44 65.36 et al., 2010).

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(Keller et al.,1978; Capaldi et al.,1979; Caggianelli et al.,1992; Karner et al., 1999; Munno et al., 2001; Pinti et al., 2001, 2007; Brauer et al., 2007) and taking into account the chronological constraints derived from the stratigraphic position of the investigated tephra layers, an attempt was made to correlate the tephra layers found at Mon- talbano with the products of already described pyroclastic deposits or, at least, to point out a possible source for the tephra layers. In the following a summary of the steps followed for tentative attribution is reported. V1. The modal content of this layer (aluminium augite clinopyroxene, Fe-enstatite orthopyroxene, bytownite plagioclase and opaques) makes it possible to hypothesise an ‘‘orogenic’’ signature for the volcanic source. The orogenic volcanic source closest to the Montalbano Jonico area is represented by the Aeolian arc, where volcanism in the westernmost sector started 1.3 Ma (Gillot, 1987), 400 500 600 700 800 900 1000 but no tentative correlation of this layer with aeolian products can be made, due both to the poor resolution of oldest aeolian activity Age (ka) available in literature and to the lack of chemical composition of V1 Fig. 8. 40Ar/39Ar determinations for sample V5. glass fragments. V2. The phonolitic composition of this tephra layer has no counterpart in the terrestrial records of alkaline volcanoes known older deposit. As far as the source of this tephra layer is concerned, at present. The start of phonolitic activity both at Sabatini and a definite hypothesis cannot be made. A generic Campanian source Vulsini volcanic complexes is dated at ca 0.6 ka (Vezzoli et al., 1987; was hypothesised for this layer by Capaldi et al. (1979) simply based Cioni et al., 1993). A younger age is reported for the first phases of on chemical composition, but the age here determined falls outside activity at Roccamonfina volcano (ca 0.55 ka; Rouchon et al., 2008). of the range of activity of Campanian sources known at present. V5. Twenty 40Ar/39Ar age determinations on single sanidine V7. This is a trachytic layer, with Na- rich sanidine. Glass frag- crystals extracted from sample V5 (Table 3, Fig. 8) yielded an ments are generally deeply devitrified, so only limited microprobe isochron age of 719.5 12.6 ka (2s error). This primary layer is composition data could be obtained. trachytic and the composition determined here resembles that As to the possible source of the uppermost tephra layers, Vulture obtained by Capaldi et al. (1979) for the main tephra interbedded in volcano is worth a further separate discussion, since it represents the the Montalbano section, although the age of ca 1.1 reported therein volcanic source closest to Montalbano Ionico. This volcano is located does not fit the stratigraphic reconstruction here. Stratigraphical 40 km west of the Montalbano area, in the Melfi neighbourhood and constraints, however, together with the lower mean error associated was active during the emplacement of the Montalbano marine with the modern 40Ar/39Ar technique, precludes correlation with the succession. Volcanic activity at Vulture started ca 750 ka (Buettner

Table 3 Complete 40Ar/39Ar incremental heating results for sample V5.

Sample ID Laser Power 40Ar/39Ar 37Ar /39Ar 36Ar/39Ar Fa 40Ar* 39Ar K/Ca Apparent ageb

File no. (%) 1s 1s 1s 1s (%) mol 1016 2s ka Single crystal fusions Sanidine J ¼ 0.0002616 0.17% (1s)c m ¼ 1.0051 0.02% (1s)d BE4834 # 35.0 1.6944 0.0025 0.0462 0.0007 0.0005 0.0001 1.5486 0.0343 91.39 11.87 9.312 730.7 32.4 BE4836 # 35.0 2.2866 0.0077 0.0398 0.0010 0.0023 0.0002 1.5999 0.0672 69.97 4.61 10.808 754.9 63.4 BE4837 # 35.0 1.7915 0.0050 0.0567 0.0009 0.0008 0.0002 1.5656 0.0506 87.39 8.25 7.589 738.7 47.7 BE4839 # 35.0 2.2327 0.0074 0.0318 0.0007 0.0023 0.0002 1.5590 0.0581 69.83 5.31 13.512 735.6 54.8 BE4840 # 35.0 1.6465 0.0080 0.0529 0.0014 0.0004 0.0002 1.5382 0.0651 93.42 4.04 8.124 725.8 61.4 BE4842 # 35.0 1.5600 0.0047 0.0298 0.0007 0.0002 0.0001 1.5155 0.0345 97.14 8.89 14.407 715.1 32.5 BE4843 # 35.0 1.5793 0.0059 0.0200 0.0010 0.0004 0.0002 1.4560 0.0643 92.19 4.35 21.456 687.0 60.7 BE4845 # 35.0 1.7352 0.0099 0.0647 0.0023 0.0004 0.0004 1.6103 0.1078 92.80 2.58 6.647 759.8 101.7 BE4846 # 35.0 1.8158 0.0064 0.0315 0.0009 0.0010 0.0002 1.5362 0.0541 84.60 6.39 13.639 724.8 51.1 BE4848 # 35.0 1.6462 0.0056 0.0298 0.0014 0.0003 0.0002 1.5561 0.0447 94.53 6.13 14.417 734.3 42.2 BE4849 # 35.0 1.7518 0.0071 0.0425 0.0009 0.0010 0.0002 1.4551 0.0577 83.06 4.21 10.109 686.6 54.4 BE4851 # 35.0 1.7964 0.0064 0.0353 0.0010 0.0011 0.0002 1.4627 0.0528 81.42 5.83 12.183 690.2 49.8 BE4852 # 35.0 3.0660 0.0089 0.0332 0.0014 0.0054 0.0002 1.4709 0.0707 47.98 4.16 12.959 694.1 66.7 BE4854 # 35.0 3.8789 0.0148 0.0285 0.0013 0.0081 0.0005 1.4732 0.1592 37.98 2.95 15.089 695.1 150.2 BE4855 # 35.0 3.6536 0.0163 0.0247 0.0018 0.0077 0.0004 1.3932 0.1189 38.13 2.66 17.409 657.4 112.2 BE4857 # 35.0 1.6215 0.0062 0.0355 0.0018 0.0006 0.0004 1.4538 0.1053 89.65 3.13 12.105 686.0 99.4 BE4858 # 35.0 1.8263 0.0078 0.0275 0.0016 0.0009 0.0002 1.5525 0.0634 85.01 4.07 15.610 732.5 59.8 BE4860 # 35.0 1.6561 0.0067 0.0551 0.0015 0.0006 0.0003 1.4934 0.0850 90.17 3.88 7.799 704.7 80.2 BE4861 # 35.0 1.6590 0.0066 0.0411 0.0014 0.0006 0.0002 1.4825 0.0707 89.36 3.68 10.474 699.5 66.7 BE4863 # 35.0 1.6385 0.0089 0.0490 0.0015 0.0002 0.0003 1.5912 0.0825 97.11 3.00 8.769 750.8 77.9 Weighted mean from 20 of 20 steps MSWD: 0.62 Weighted mean age: 719.5 12.6 Inverse isochron from 20 of 40Ar/36Ar 2s: 289.3 18.5 MSWD: 0.63 Isochron age: 722.5 15.1 20 steps

# indicates increments that have been included in weighted mean and isochron calculations. a F is the ratio of radiogenic 40Ar to K-derived 39Ar. b 10 37 39 All ages calculated using the decay constants of Steiger and Ja¨ger (l40K ¼ 5.543 10 /yr) and corrected for Ar and Ar decay, half lives of 35.2 days and 269 years, respectively. c J-value calculated relative to 28.02 Ma for the Fish Canyon sanidine. d m: mass discrimination per atomic mass unit.

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Fig. 9. Stratigraphic correlation of Montalbano Jonico composite section (benthic and planktonic oxygen stable isotope stratigraphy) with LR04 benthic stack (Lisiecki and Raymo, 2005), Pacific (Mix et al., 1995a,b; Shackleton et al., 1995) and Atlantic (Bickert et al., 1997) d18O benthic records, Mediterranean d18O planktonic record of ODP-Site 975 (Lourens, 2004), and d18O planktonic stack (Lourens, 2004; Lourens et al., 2004). Astronomical ages of Ocean calcareous nannofossil events are from Lourens et al. (2004), Raffi et al. (2006), and this study. Mediterranean calcareous nannofossil events at ODP sites 964 and 967 are from Maiorano and Marino (2004), recalibrated in this study (see Table 3), and Lourens et al. (1998), Lourens (2004) and Raffi et al. (2006). Summer insolation 65 N (La041:1) is from Laskar et al. (2004). Sapropel stratigraphy is from Lourens et al. (2004) and Lourens (2004). V1–V9: tephra layers in Montalbano Jonico section. Ages of polarity boundaries are from Lourens (2004). Thick grey dotted line is the position of tephra V5 plotted versus Ar/ Ar age from this work. et al., 2006). In the first stages of activity, widespread trachypho- Mediterranean ODP-Site 975 and KC0IB cores (Lourens, 2004), two nolitic ignimbritic deposits were emplaced together with minor selected d18O datasets from (ii) Pacific Ocean (Shackleton et al., pyroclastic fall products (e.g. Masseria Boccaglie pyroclastic fall; 1995; Mix et al., 1995a,b) and (iii) Atlantic Ocean (Bickert et al., <720 ka). The preliminary data on the Montalbano succession does 1997), and (iv) the stacked benthic d18O record of Lisiecki and not support an origin from the Vulture volcano of V5 pyroclastic Raymo (2005). Based on the high-resolution integrated strati- layer, because of its alkali-trachytic chemical composition. Its age is graphic framework available for the Montalbano Jonico section, compatible with that of 714þ/18 ka determined by Buettner et al. glacial and interglacial intervals reported for the reference ocean (2006) on Masseria Boccaglie pyroclastic fall products, but the records were correlated respectively with glacial and interglacial composition precludes correlation, as Masseria Boccaglie tephra stages in the Montalbano section, from MIS 36 to MIS 16. More ranges in composition from tephritic phonolitic to tephritic (Bona- details on stratigraphic interpretation of oxygen isotope curves donna et al., 1998). from Montalbano Jonico record are discussed below. 18 The d Obenthos record shows evident differences between 4.3. Integrated stratigraphy Montalbano Jonico section Intervals A and B both in mean values and in duration of the oscillating peaks. In particular, benthic oxygen Benthic and planktonic d18O records from Montabano Jonico isotope values during the glacial phases of Interval A (from MIS 36 to section are shown in Fig. 9 along with results from: (i) the MIS 23), are lighter (ranging between 2.7& and 2.8&) than those

Summer insolation 65°N ODP-Site 969D ODP-Site 967 Montalbano Jonico Interval A 550 400450500 Lithology 80 % N. sp. (sin) % N. sp. (sin) 70 i-102 i-102 020406080100 020406080100 core section core section lithology sapropel core section lithology sapropel i-104 60 i-104 Insolation cycles influx 38 G.crassaformis influx 967 sapropel 1150 i-106 969D-3H sapropel 25 G. crassaformis 6 5 influx 20 27 50 G. crassaformis i-110 20 27 5 21 7 39 28 i-112 i-112 21 28 26 40 i-112 1200 6 i-114 40 30 6 27

i-116 969D-3H 967A-4H Age (ka) 967C-4H 22 7 20 1250 i-118 1 41 050100 i-120 7 28 % N. sp. (sin) cc 10 i-122 22 29 29 42 1300 2 m 0 3 12 0 δ18O G. bulloides

Fig. 10. Sapropel correlation between the astronomically tuned ODP sites 969D and 967 (Lourens et al., 1998) and Montalbano Jonico section Interval A. The percentage of left- coiling neogloboquadrinids (N. sp. [sin.]) is related to the total of left and right-coiling neogloboquadrinids. Dotted line shows the correlation between the sapropel corresponding to insolation cycle 112 in sites 969D, 967 and Montalbano section Interval A.

N. Ciaranfi et al. / Quaternary International xxx (2009) 1–12 9 reported form Interval B (from MIS 22 to MIS 16) (3.0–3.2&). This the short- and mid-term resolution, with the deeper isotope record pattern is reflected in both oxygen isotope changes measured from thus suggesting an uninterrupted coupling of surface water dynamics the Atlantic and Pacific benthic records (Fig. 9) and the change in in the Mediterranean basin during the studied interval. This allowed paleodepth from bathyal to circalittoral environments occurring correlation of glacial and interglacial cyclicity, using oxygen isotope between Intervals A and B (Ciaranfi et al., 2001; D’Alessandro et al., values from the surface waters, to the reference ocean datasets, 2003; Stefanelli, 2003, 2004) in response to the global sea level drop clearly identifying MIS 36–23. The FO of G. omega and the LCO of R. recorded from MIS 23 to MIS 22 (e.g., Prell, 1982; Ruddiman et al., asanoi (Interval A, Fig. 9), which are distinct and highly reliable bio- 1989). The progressive shallowing can be ascribed to climate effects, events (Raffi et al., 2006), together with the occurrence of two sap- although evidence of superimposed tectonic instability has been ropel layers at the top of Interval A, represent important constraints also recognised based on taphonomic signatures (D’Alessandro for the identification of MIS 25 and i-cycle 90, and MIS 23 and i-cycle et al., 2003) and on facies analyses (Ciaranfi et al., 1996) revealing 86, respectively (Maiorano et al., 2004; Stefanelli et al., 2005)(Fig. 9), the presence of ‘‘turbidites and graded laminites’’ sequences, higher following Pierre et al. (1999) and Lourens et al. (2004). However, it is sedimentation rate and increased terrigenous supply. noteworthy that few data indicate that the FO of G. omega occurs at MIS 27 or in the topmost Jaramillo in the Sicily Channel (Di Stefano, 4.3.1. Interval A 1998; Di Stefano, personal communication). The tuning of the three 18 The d OG. bulloides record from the interval A of the Montalbano sapropel layers occurring in the lower part of the Interval A, to Jonico section shows comparable patterns, in terms of variability at insolation cycles i-102, i-104, i-112 according to Lourens et al. (2004)

Fig. 11. Age–depth proﬁle of Montalbano Jonico composite section. The black diamonds represent the tie-points while the white ones are the position of the tephra layers. The age reported with the star is the Ar/Ar data for tephra V5 from this work.

10 N. Ciaranﬁ et al. / Quaternary International xxx (2009) 1–12

Table 4

Montalbano Jonico section Calcareous plankton event Interval meter ATNTS2004 Age (ka) MIS end td 2 G. omega Montalbano Jonico Interval B 155.45 771.04 18/19 beginning td 2 G. omega Montalbano Jonico Interval B 82.65 826.86 20 LCO R. asanoi Montalbano Jonico Interval A 162.55 907.53 23 Re-entrance medium ¼ FO G. omega Montalbano Jonico Interval A 138.15 952.56 25 FCO R. asanoi Montalbano Jonico Interval A 70.95 1087.29 32 inﬂux G. crassaformis Montalbano Jonico Interval A 51.8-59.6 1145.26-1121.72 34

Tephra layers Interval meter ATNTS2004 Age (ka) V1 Montalbano Jonico Interval A 115.1 1001.77 27 V2 Montalbano Jonico Interval B 20.3 889.79 22 V3 Montalbano Jonico Interval B 105.8 805.42 20 V4 Montalbano Jonico Interval B 134.2 792.64 19 V5 Montalbano Jonico Interval B 227.7 719.5+-0.12* 17/18 V6 Montalbano Jonico Interval B 239.7 693.52 17 V7 Montalbano Jonico Interval B 242.7 687.20 17 V8 Montalbano Jonico Interval B 258.7 653.50 16 V9 Montalbano Jonico Interval B 262.7 645.10 16

* Ar/Ar age

18 (Fig. 9), is supported by the FCO of R. asanoi occurring just above i- noisier background in the d Oplankton record from Montalbano cycle 102 (Maiorano and Marino, 2004) (Fig. 4), the Globorotalia Jonico Interval B, the above-mentioned stratigraphic constraints crassaformis influx (Joannin et al., 2008)astronomicallydatedat and the direct comparison between d18O from Montalbano Jonico 1.135 Ma (ODP-Site 967 Lourens et al.,1998) and by the correlation of Interval B and the oxygen signal from ODP-Site 975 (oxygen isotope the left-coiling neogloboquadrinids pattern recorded in Interval A, chronology of Pierre et al., 1999 modified by Lourens, 2004) offers with the ODP-Site 969D and 967 (Lourens et al., 1998)(Fig. 10). This a reasonable constraint to the age-model of the studied record correlation shows a distinct peak of neogloboquadrinids left-coiled through MIS 22–16. just below the insolation cycle i-112 (sapropels 21 and 28 in ODP-sites 969D and 967, Lourens et al., 1998). 5. Age model and implication for biochronology and 4.3.2. Interval B tephrochronology Isotope data for planktonic foraminifera from Interval B show a higher complexity with a noisier signal associated with abrupt and Following Lourens et al. (1996b) and Lourens (2004), a 3 ky time 18 large d OG. bulloides variations. This behaviour is interpreted as directly lag was used between the midpoints of each individual sapropel reflecting the influence of a shallow shelf setting. The deposition of (corresponding to insolation cycles i-112, i-104, i-102, i-90 and Interval B in a shallow shelf environment is indicated by oxygen i-86) and their correlative precession minima to reconstruct the isotope values recorded for planktonic foraminifera, with abrupt benthic and planktonic d18O time series of Interval A. In addi- lightening of values, possibly related to effects of salinity. However, tion, G. bulloides d18O record of Montalbano Jonico Interval B this local control does not definitively mask a response of the isotope has been tuned to the same record from Mediterranean ODP- record to global events such as cooling, as indicated by correlation Site 975 (Lourens, 2004) by visual correlation combined with with the signal reported form the Mediterranean ODP-Site 975. Ar/Ar age for the tephra layer V5 (uppermost part of Mon- The Ar/Ar age for the tephra layer V5 (719.5 12.6 ka) supports talbano Interval B), dated at 719.5 12.6 ka (Fig. 9). This 18 the identification of MIS 17 in the d Obenthos record. In addition, the correlation is also supported by the glacial-interglacial oscilla- temporary disappearance of G. omega (td2), located according to tions observed in C. carinata d18O record of Montalbano Jonico additional data from Maiorano and Marino (2004), provides a clear compared with open ocean benthic stacks (Fig. 9). identification of MIS 19 (Fig. 9). The temporary disappearance was A cubic spline is needed to describe the age–depth relationship also documented in the Eastern Mediterranean Sea and in the for Montalbano Jonico section (Fig. 11). This figure reflects the ocean area (Castradori, 1992; Maiorano and Marino, 2004), major change in sedimentation rate between Intervals A and B although a slightly variable extent of this interval is known within indicating an average sedimentation rate of 0.53 m/ky and 0.91 m/ the Mediterranean (Maiorano and Marino, 2004). Despite the ky, respectively (Fig. 11).

Table 5 Astronomical ages (Ma) of calcareous nannofossil events at the Mediterranean ODP sites 964 and 967 according to ATNTS of Lourens et al. (2004) (this study). 1From Maiorano and Marino (2004); 2corrected composite depth (ccd) of Site 964 from Lourens (2004); 3from Lourens et al. (1998), Lourens (2004) and Rafﬁ et al. (2006).

Calcareous nannofossil event ODP Site 964 ODP Site 967

Depth Depth Age (Ma) MIS Depth Age (Ma) MIS (rmcd)1 (ccd)2 this study (rmcd)1 this study LO G. omega 24.07 23.14 0.556 15/14 22.26 0.572 15 End td 2 G. omega 29.88 28.77 0.774 19 27.46 0.768 19/18 Beginning td 2 G. omega 30.63 29.51 0.805 20 28.95 0.818 21/20 End td 1 G. omega 31.99 30.85 0.863 21 30.24 0.860 21 Beginning td 1 G. omega 32.36 31.21 0.878 22 31.2 0.892 22 LCO R. asanoi 32.93 31.77 0.901 23 31.431/31.473 0.899/0.9013 23 Re-entrance medium ¼ FO G. omega 34.31 33.13 0.957 25 33.191/33.253 0.955/0.9573 25 FCO R. asanoi 37.36 36.11 1.087 32 36.39 1.088 32 LO large Gephyrocapsa – – – – /41.223 /1.2573 38

N. Ciaranﬁ et al. / Quaternary International xxx (2009) 1–12 11

The astronomical tuning of the studied record indicates that the References Montalbano Jonico section covers an interval from 1240 ka to 645 ka. The gap between intervals A and B spans a time interval of Abels, H.A., Hilgen, F.J., Krijgsman, W., Kruk, R.W., Raffi, I., Turco, E., Zachariasse, W.J., w 2005. Long-period orbital control on middle Miocene global cooling: Integrated 19.52 ky corresponding to an interval about 9.63 m thick. stratigraphy and astronomical tuning of the Blue Clay Formation on Malta. Astronomical tuning of the Montalbano Jonico record provides Paleoceanography 20 (4), PA4012. doi:10.1029/2004PA001129. the ages of bioevents recognised in the section (Table 4). The age Aguirre, E., Pasini, G., 1985. The Pliocene–Pleistocene boundary. Episodes 8, 11–120. Azzaroli, A., 1968. Studi illustrativi della Carta Geologica d’Italia: formazioni geo- assignments are comparable with data available for Mediterranean logichedLe Argille subappennine. Servizio Geologico d’Italia 1, 153–185. record (Table 5) in accordance with the calibration to the ATNTS of Balduzzi, A., Casnedi, R., Crescenti, U., Mostrardini, F., Tonna, M., 1982. Il Plio- Lourens et al. (2004) and the corrected composite depth (ccd, Pleistocene del sottosuolo del bacino lucano (Avanfossa appenninica). Geo- Lourens, 2004) for Site 964. logica Romana 21, 89–111. Bickert, T., Curry, W.B., Wefer, G., 1997. Late Pliocene to Holocene (2.6–0 Ma) Interpolated ages of the tephra layers V1–V4, V6–V9 occurring in western equatorial Atlantic deep-water circulation: inferences from benthic the Montalbano Jonico section are proposed (Table 4)basedon stable isotope. In: Shackleton, N.J., Curry, W.B., Richter, C., Bralower, T.J. (Eds.), astronomical tuning of the oxygen isotope records. These ages did not Proceedings of the Ocean Drilling Program. Scientific Results 154, College Station (TX), pp. 239–253. correlate with the interpolated ages proposed for several tephra layers Bonadonna, F.P., Brocchini, D., Laurenzi, M.A., Principe, C., Ferrara, G., 1998. Strati- by Lourens (2004) from Ionian Sea KC01B core. At present, the authors graphical and chronological correlations between Monte Vulture volcanics and would not want to speculate on possible tephra-correlation due to the sedimentary deposits of the Venosa Basin. Quaternary International 47/48, 87–96. Brauer, A., Wulf, S., Mangili, C., Moscariello, A., 2007. Tephrochronological dating of poor tephrachronology database available for this time interval. varved interglacial lake deposits from Pia`nico-Se`llere (Southern Alps, Italy) to around 400 ka. Journal of Quaternary Science 22, 85–96. 6. Concluding remarks Brilli, M., Lerche, I., Ciaranfi, N., Turi, B., 2000. Evidences of precession and obliquity orbital forcing in oxygen-18 isotope composition of Montalbano Jonico Section (Basilicata, southern Italy). Applied Radiation and Isotopes 52, 957–964. The new stratigraphical and chronological data acquired for the Buettner, S., Principe, C., Villa, I.M., Brocchini, D., 2006. 39Ar/40Ar geochronology of Montalbano Jonico section allow the proposal of an astronomical Mt. Vulture. In: Principe, C. (Ed.), La Geologia del Monte Vulture, pp. 73–86. Caggianelli, A., Dellino, P., Sabato, L., 1992. Depositi lacustri infrapleistocenici con tuning of the record. The integrated stratigraphic framework intercalazioni vulcanoclastiche (Bacino di Sant’Arcangelo, Basilicata). Il Qua- (biostratigraphy, sapropel stratigraphy, radiometric dating of tephra ternario 5 (1), 123–132. V5) provides correlation of benthic and planktonic d18Odatato Capaldi, G., Civetta, L., Lirer, L., Munno, R., 1979. Caratteri petrografici ed eta` K/Ar a continuous MIS 36–MIS 17 record. 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