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Tephrochronological study in the Maccarese lagoon (near Rome, Italy): identification of Holocene tephra layers

Etude tephrochronologique dans la lagune de Maccarese (environs de Rome, Italie) : identification de niveaux de tephras holocènes
Gwénolé Jouannic, Pierre‑Yves Gillot, Jean‑Philippe Goiran, Jean-Claude Lefevre, Giuseppe Siani, Ferréol Salomon et Antonia Arnoldu‑Huyzendveld
p. 65-74

Résumés

English Français

Cette étude propose de retracer l’activité volcanique explosive du Sud de l’Italie enregistrée dans la région romaine depuis environ 8 000 ans. Cette étude est basée sur l'étude téphrochronologique d’un carottage (carotte LM2) réalisé en février 2010 dans la Lagune de Maccarese, près de l’aéroport Fiumicino de Rome. Rome est entourée de complexes volcaniques dont l’activité récente est régulièrement discutée. Les Monts Albans et Sabatini sont les deux principaux complexes volcaniques au Sud et au Nord de Rome. Les dernières traces d’activité de Sabatini sont datées à 251 ± 8 ka par 40Ar/39Ar. En revanche, les Monts Albans ont connu une activité plus tardive, et régulièrement discutée, jusqu’à 7,5 ka, d’après l'étude des plus jeunes dépôts tapissant le fond du lac de cratère le plus récent. Funiciello et al. (2003) décrivent cependant des coulées pyroclastiques et des dépôts de lahars séparés par un paléosol daté à 5,1 ± 0,1 ka 14C BP. Par ailleurs, des récits historiques relatent également des activités volcaniques pendant l’âge du Bronze. Cependant, jusqu’à maintenant, aucune étude n’a mis en évidence des dépôts volcaniques liés à cette activité récente. La recherche de téphras issus de l’activité volcanique campanienne, sicilienne et éolienne a donc été étendue à l'activité volcanique explosive récente de la région magmatique romaine. L'étude de la carotte LM2 a mis en évidence trois téphras. Leur analyse chimique, ainsi que des datations Radiocarbone, ont permis de les relier respectivement (1) à l'éruption d’Agnano-Monte-Spina (3,99 ± 0,03 ka 14C BP), (2) vraisemblablement à la dernière éruption des Monts Albans dont les dépôts ont été décrit par Funiciello et al. en 2003, et (3), pour la première fois dans le nord de l’Italie, à un niveau de téphra lié à l’activité volcanique des Champs Phlégréens et postérieur à l'éruption d'Agnano-Monte-Spina. L’augmentation de la population autour du complexe volcanique des Monts Albans et de Rome expose un nombre toujours plus grand de personnes à des risques volcaniques variés dans une région qui n’est pourtant pas assimilée au volcanisme au premier abord. La multiplication des sites d'étude permettra d'obtenir une chronologie précise de ces éruptions et d'estimer leurs conséquences environnementales.

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Texte intégral

We thank Christine Oberlin and the Radiocarbon dating Centre (University Claude Bernard, Lyon, France) who supported and funded this study. We also thank the Ecole Française de Rome (the “Tiber Delta” program) and the Soprintendenza Speciale per i Beni Archeologici di Roma (sede di Ostia) (Angelo Pellegrino and Cinizia Morelli) for allowing us to realize our coring campaign. This study was conducted through the ANR POLTEVERE (ref JCSHS3 002 01). We thank Emmanuelle Delque-Kolic (CEA, Saclay, France) for the radiocarbon dating by ARTEMIS, and Michel Fialin and Frederic Coufignal (Camparis, Université P. et M. Curie, Paris, France) for their help for analysis of volcanic fragments. We also thank reviewers for their detailed and constructive observations, which improved the manuscript.

1 - Introduction

1Various works deal with tephrostratigraphy in north Italy, the dispersion of volcanic ashes during eruptions and the use of tephras as time-parallel chronological markers, and show the importance of tephra detection and characterization (Calanchi et al., 1996; Ramrath et al., 1999; Magny et al., 2006, 2007; Giaccio et al., 2009). Tephras investigations in cores have been primarily driven by a need for robust chronological markers to correlate environmental records. They also provide an estimate of eruptions frequency for volcanic centers when proximal informations have been removed by recent activity (Keller et al., 1978; McCoy, 1981; Paterne et al., 1988, 1990, 2008; Vezzoli, 1991; Calanchi et al., 1994, 1996, 1998; Narcisi & Vezzoli, 1999; Siani et al., 2004; Lowe et al., 2007).

2This paper presents a tephrostratigraphic study from a holocene sedimentary sequence cored in the Maccarese lagoon close to Fiumicino airport (Rome, Italy).

2 - Geological setting

3The Maccarese lagoon is located in the Tiber delta between two major volcanic massifs, Sabatini to the north and Alban Hills to the south (fig. 1), north from the present main active Italian volcanoes (i.e. Campanian volcanoes, the Aeolian Islands and Etna).

4The geomorphological features of this area are due to (1) post-orogenic extensional tectonics since the late Miocene, (2) volcanic activity of Alban hills and Sabatini Mountains, and (3) combined Tiber sedimentation and sediment reworking due to glacio-eustatic sea level changes during the Quaternary (Amorosi & Milli, 2001; Bellotti et al., 2007; Di Rita et al., 2010; Bellotti et al., 2011). Coastal lagoons have been developed in the delta on both sides of the Tiber, Ostia lagoons in the South and Maccarese lagoon in the North (Bellotti et al., 2007).

Fig. 1: Location of core LM2 and volcanic complexes around Rome.

Fig. 1: Location of core LM2 and volcanic complexes around Rome.
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3 - Materials and methods

3.1 - Coring

5The core LM2 was collected by Jean-Philippe Goiran and the Archéorient Laboratory team (University Lyon 2, France) in February 2010, in the southern part of the Maccarese lagoon (41°49’20,53” N, 12°17’34,94” E). Since February 2010, the Maccarese lagoon was artificially filled and Rome Fiumicino Airport's enlargement was built above the lagoon. The core is composed of clays and silts with two peat layers: from 4.46 m to 4.6 m depth and from 5.36 m to 5.95 m depth (fig. 2). The sedimentary record overlies the volcanic tuff from the Sabatini Mountains.

3.2 - Tephra identification

6Distal ash layers identification is often difficult to the naked eye. So, first, volume magnetic susceptibility measurements were performed (fig. 2) using a MS2-E1 surface scanning sensor from Bartington Instruments. This 1cm diameter-sensor is well adapted to measure the volume magnetic susceptibility on split cores with fine resolution. The sediments in the Maccarese lagoon mainly consist of clays and carbonates (fig. 2), which are essentially dia- and paramagnetic materials. Volcanic ashes are made of glass shards or pumice and phenocrists such as feldspars, pyroxenes, amphiboles and micas which are also dia- and paramagnetic minerals. Moreover, they generally contain ferromagnetic crystals such as magnetite. In distal deposits, magnetic dense particles, like titanomagnetite grains, may be absent, because they may sediment before the study site. Then, distal volcanic material mainly consists of glass shards that may contain titanomagnetites as small inclusions (Ananou et al., 2003). Thus, all layers or volcanic deposit containing these minerals commonly lead to an increase in the magnetic susceptibility values (Williamson et al., 1991; Bossuet et al., 1997; Walter-Simonnet et al., 2008). However, aphyric glasses (usually rhyolite) show low magnetic susceptibility values.

7Chemical analyzes (major elements) were carried out on tephras glass shards using a Cameca SX50 electron microprobe in Camparis Center from the University Pierre et Marie Curie Paris VI (France) (operating conditions: wavelength dispersive spectrometry, accelerating voltage of 15 keV, 10 nA beam current, 4 μm beam diameter). The chemical composition of glass shards is generally different than the chemical composition of bulk volcanic rock and reflects the conditions of formation of pyroclastites (fast ejection, fast cooling). Generally, eruptions have a special chemical composition that allows to distinguish them.

3.3 - Chronology

8The chronological framework of the sedimentary sequence is based on six radiocarbon dates of wood fragments, plants macrofossils and peat samples (tab. 1). Two radiocarbon dating methods were used: Accelerator Mass Spectrometer (AMS) at the CEA (ARTEMIS, Saclay, France) and Liquid Scintillation Counting (LSC) at the Center for Radiocarbon Dating of the University Claude Bernard (Lyon, France). Core LM2 recorded sedimentation processes from ca. 9,136-9,427 cal. yr BP (at 20.5 m depth). The youngest age (2,353-2,694 cal. yr BP) was obtained at 3.6 m depth.

9The six radiocarbon ages were converted to calendar years using the program OxCal and the Calib software (Stuiver & van der Plicht, 1998), and the calibration curve IntCal09 (Reimer et al., 2009). Two different sedimentation rates are observed in the age-depth diagram (fig. 3). Between the base of the core and 7 m depth, the sedimentation rate is ca. 0.85 cm/year, but it decreases to 0.08 cm/year above 7 m depth. This change in sedimentation rate is consistent with chronological data from different other studies conducted in the Tiber delta (Lambeck et al., 2004; Bellotti et al., 2007; Di Rita et al., 2010; Bellotti et al., 2011; Giraudi et al., 2011).

Fig. 2: Simplified stratigraphic log of the core LM2 with samples position for radiocarbon dating and magnetic susceptibility record.

Fig. 2: Simplified stratigraphic log of the core LM2 with samples position for radiocarbon dating and magnetic susceptibility record.
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3.4 - Tephra characterization

10Samples were selected on and around peaks of magnetic susceptibility as well as between peaks. But, magnetic susceptibility were difficult to use along the upper 2 meters of the core. Then, in order to obtain a complete sampling, this part of the core was cut every 5 cm and the 20 samples were analyzed.

11Samples have been attacked with 10% solution of acetic acid in order to remove carbonates, then with 35 % solution of hydrogen peroxide in order to remove organic matter. Finally, the samples were sieved at 40 microns. The > 40 µm fraction was observed with a binocular lens and a light microscope (fig. 4).

Tab. 1: Radiocarbon dates from the core LM2.

Tab. 1: Radiocarbon dates from the core LM2.
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Fig. 3: Ages versus depth in core LM2

Fig. 3: Ages versus depth in core LM2
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Fig. 4: Glass shards from LM2-451, LM2-544 and LM2-640 tephras (optical microscopy).

Fig. 4: Glass shards from LM2-451, LM2-544 and LM2-640 tephras (optical microscopy).
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Tab. 2: Major oxides concentrations of volcanic glass shards from tephras layers observed in core LM2 (electron microprobe analyses).

Tab. 2: Major oxides concentrations of volcanic glass shards from tephras layers observed in core LM2 (electron microprobe analyses).
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4 - Results and discussion

4.1 - Magnetic susceptibility

12The magnetic susceptibility of this sediment is often low because clays and carbonates which compose the core are dia- and paramagnetic minerals. However, the magnetic susceptibility data show several peaks (fig. 2) due to the occurrence of ferromagnetic minerals in the sediment. The two tephra layers observed at naked eye, LM2-451 and LM2-544 (at 4.51 m depth and 5.44 m depth respectively) do not correspond to high magnetic susceptibility values. There are two possible reasons: 1) heavy ferromagnetic minerals sedimented before the Maccarese lagoon, and 2) hightly differentiated magmas are usually impoverished in ferromagnetic minerals.

13Only one sample (tephra layer LM2-640 at 6.40 m depth) corresponds to a high magnetic susceptibility value indicating the presence of ferromagnetic minerals in the sediment. Other peaks with high magnetic susceptibility values can be attributed to detrital material deposits due to continental erosion. The upper 4 meters of the core are marked by rapid and significant changes in magnetic susceptibility record. These variations may correspond to Bronze Age human occupations in the Roman region. Indeed, deforestation was very extended during this period and induced soil erosion and an increased supply of detrital sediments in the lagoon. This hypothesis was recently confirmed by Balsam et al. (2011).

4.2 - Glass shards chemistry

4.2.1 - Tephra LM2-451

14This 1.5 cm thick tephra is dated to 3,977 - 4,158 cal. yr BP using peat sampled from 4.45 to 4.50 m depth (tab. 1). Major elements analyses (tab. 2) show it has got a trachytic composition which is characteristic of the alkaline series from the Campanian products (fig. 5 & 6). During this time interval, three main Campanian eruptions occurred: the Avellino eruption from the Somma-Vesuvius complex (ca. 3.8 cal. ka BP, Sulpizio et al., 2008, 2010a,b; 3.9 cal. ka BP, Sevink et al., 2011), the Averno eruption at 4,249 ± 95 cal. years BP (Isaia et al., 2004, 2009; Smith et al., 2011) and the volcanic activity of Astroni. The first activity of Astroni started at 4 249 ± 95 cal. years BP (Isaia et al., 2004, 2009; Smith et al., 2011). The eruption of Lupura Fossa, which followed the last of the seven phases of the Astroni eruption, is dated at 4,085 ± 100 cal. years BP (Di Vito et al., 1999) in the Phlegraean Fields (tab. 3). Even if there may be a possible synchronism with Avellino eruption, this eruption doesn't correspond to LM2-451 tephra. Its trachy-phonolitic composition is different from the one of Avellino (tab. 4). In return, it is characteristic of phlegrean products. So, this tephra layer may correspond to the Astroni eruption whose age and chemistry are consistent (tab. 4). It is the first time that this tephra layer originated from Phlegrean Fields is described in north Italy.

4.2.2 - Tephra LM2-544

15This tephra was observed at 544 cm in the second peat layer and dated by AMS 14C dates at 4,416 - 4,523 cal. years BP (tab. 1). Its major elements chemistry shows a phonolitic composition indicating a phlegrean (Campanian) origin (fig. 7). During this period, two phlegrean phonolitic eruptions occurred. The eruption of Astroni started at 4,249 ± 95 cal. years BP (Isaia et al., 2004, 2009; Smith et al., 2011) and the Agnano Monte Spina eruption dated to 4,555 ± 75 cal. years BP (de Vita et al., 1999; Di Vito et al., 1999). The chemical compositions of Astroni and Agnano Monte Spina eruptions are similar. Our LM2-544 tephra layer may correspond to the tephra layer attributed to Agnano Monte Spina described in Lake Accesa by Magny et al. (2006, 2007), north of Maccarese Lagoon.

4.2.3 - Tephra LM2-640

16There is no datable material around this level. Then, we have estimated the age of this tephra by linear interpolation and obtained an age of ~5,965 cal. years BP (tab. 1, fig. 3).

17Glass shards are rare but their chemical composition shows very low silica (47-52 %), high FeO (7-9%) and high K2O (5-9%) contents (fig. 6 & 8). This chemical chacracteristics can be attributed to Alban Hills volcanic products. The last activity of the Alban Hills was dated to 5,100 ± 100 14C years BP (5,850 ± 130 cal. years BP) (Funiciello et al., 2003). The estimated age of LM2-544 tephra and the age of the last activity of Alban Hills are consistent. Thus, we can attribute LM2-544 tephra to the last known volcanic activity of Alban Hills.

Fig. 5: Geochemical composition of glass shards from the LM2-451 tephra layer and from Avellino

Fig. 5: Geochemical composition of glass shards from the LM2-451 tephra layer and from Avellino
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(Calanchi et al., 1996; Calanchi et al., 1998; Wulf et al., 2004; Magny et al., 2007; Calanchi & Dinelli, 2008; Sulpizio et al., 2008; Turney et al., 2008), Agnano Monte Spina (De Vita et al., 1999; Wulf et al., 2004; Magny et al., 2006; Piochi et al., 2008; Zanchetta et al., 2011) and Astroni (Siani et al., 2004; Smith et al., 2011) tephras plotted in the total alkali versus silica diagram (TAS, Le Bas et al., 1986).

Fig. 6: K2O versus SiO2 binary diagram (modified after Peccerillo & Taylor, 1976) for volcanic glass shards from tephra layers of LM2 core and the Alban hills, Eolian Islands, Etna, Somma-Vesuve and Phlegrean Fields (Siani et al., 2004). Series: A/ tholeiitic, B1/ low K calc-alkaline, B2/ high K calc-alkaline, C/ shoshonitic series, D/ alkaline series.

Fig. 6: K2O versus SiO2 binary diagram (modified after Peccerillo & Taylor, 1976) for volcanic glass shards from tephra layers of LM2 core and the Alban hills, Eolian Islands, Etna, Somma-Vesuve and Phlegrean Fields (Siani et al., 2004). Series: A/ tholeiitic, B1/ low K calc-alkaline, B2/ high K calc-alkaline, C/ shoshonitic series, D/ alkaline series.
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Fig. 7: K2O versus SiO2 binary diagram for chemical analyses of glass shards from the tephra layer LM2-544 and from Avellino, Astroni, Agnano-Monte-Spina eruptions (for authors, see figure 5).

Fig. 7: K2O versus SiO2 binary diagram for chemical analyses of glass shards from the tephra layer LM2-544 and from Avellino, Astroni, Agnano-Monte-Spina eruptions (for authors, see figure 5).
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Fig. 8: FeO versus total alkali and K2O versus SiO2 binary diagrams for chemical analyses of glass shards from the tephra layer LM2-640 and from Campanian province (for authors, see figure 5), Etna (Corsaro et al., 2004, 2005, 2007; Viccaro et al., 2007; Ferlito et al., 2008; Branca et al., 2009) and Alban Hills (Gaeta, 1998; Freda,2006; Gaeta et al., 2006) eruptions.

Fig. 8: FeO versus total alkali and K2O versus SiO2 binary diagrams for chemical analyses of glass shards from the tephra layer LM2-640 and from Campanian province (for authors, see figure 5), Etna (Corsaro et al., 2004, 2005, 2007; Viccaro et al., 2007; Ferlito et al., 2008; Branca et al., 2009) and Alban Hills (Gaeta, 1998; Freda,2006; Gaeta et al., 2006) eruptions.
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Tab. 3: Campi Flegrei volcanic eruptions during Bronze age. (a) Santacroce et al. (1987), (b) Rolandi et al. (1998), (c) de Vita et al. (1999), (d) Di Vito et al. (1999), (e) Andronico & Cioni (2002), (f) Funiciello et al. (2003), (g) Isaia et al. (2004), (h) Isaia et al. (2009), (i) Sacchi et al. (2009) and (j) Sevink et al. (2011).

Tab. 3: Campi Flegrei volcanic eruptions during Bronze age. (a) Santacroce et al. (1987), (b) Rolandi et al. (1998), (c) de Vita et al. (1999), (d) Di Vito et al. (1999), (e) Andronico & Cioni (2002), (f) Funiciello et al. (2003), (g) Isaia et al. (2004), (h) Isaia et al. (2009), (i) Sacchi et al. (2009) and (j) Sevink et al. (2011).
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Tab. 4: Comparative table of average chemical compositions of glass hards from LM2-451 tephra and tephras from the litterature. (a) Di Vita et al. (1999), (b) Siani et al. (2004), (c) Wulf et al. (2004), (d) Magny et al. (2006), (e) Piocchi et al. (2008), (f) Sulpizio et al. (2008), (g) Smith et al. (2011) and (h) Zanchetta et al. (2011).

Tab. 4: Comparative table of average chemical compositions of glass hards from LM2-451 tephra and tephras from the litterature. (a) Di Vita et al. (1999), (b) Siani et al. (2004), (c) Wulf et al. (2004), (d) Magny et al. (2006), (e) Piocchi et al. (2008), (f) Sulpizio et al. (2008), (g) Smith et al. (2011) and (h) Zanchetta et al. (2011).
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4.2.4 - Historic volcanic activity of the Alban Hills

18Many historians of Ancient Rome (Julius Obsequens, Hostillius Tullius, Cicero, Livy, Pliny the Elder), quoted by Heiken et al. (2005), related disastrous events all around the Alban Hills during the six centuries before Jesus Christ. They often described "a shower of stones on Rome" or "stones thrown from the crater" on more or less accurate dates (De Benedetti et al. (2008). No tephrostratigraphic study have shown presence of tephras from very late roman volcanic activity. Considering our chronological data, tephras related to Alban Hills activity during the Bronze Age would be recovered in the first two meters of our core. But, such tephra layer hasn't been found. The lack of glass shards may be explained by the type of eruptive activity, i.e. there is no expulsion of volcanic glass during phreatic eruptions. During phreatic eruptions rocks are broken by water vapor under pressure but there is no mission of magma at the surface. In this case the plume is only composed by water vapor.

5 - Conclusion

19The core performed into the Maccarese lagoon is of great tephrochronological interest. Ages obtained in this study complete works on the Tiber delta formation and the sea level evolution in this area (Lambeck et al., 2004; Bellotti et al., 2007, 2011; Goiran et al., 2009, 2010; De Rita et al., 2010; Bellotti et al., 2011; Giraudi et al., 2011). Our study has highlighted several eruptive episodes that historically affected the Roman region, and, for the first time in this part of Italy, shows a record of post-Agnano-Monte-Spina volcanic activity of Phlegrean Fields. The observed tephra layers are important chronological markers in the sedimentary record in the Tiber delta.

20The volcanic activity of Alban Hills during the Bronze Age is not recorded in this core. Doubts about the veracity of the chronicles remain unsolved although they come from multiple sources. Nevertheless, our study shows the need of such studies in other areas around the Alban Hills.

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Table des illustrations

Titre Fig. 1: Location of core LM2 and volcanic complexes around Rome.
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Titre Fig. 2: Simplified stratigraphic log of the core LM2 with samples position for radiocarbon dating and magnetic susceptibility record.
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Titre Tab. 1: Radiocarbon dates from the core LM2.
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Titre Fig. 3: Ages versus depth in core LM2
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Titre Fig. 4: Glass shards from LM2-451, LM2-544 and LM2-640 tephras (optical microscopy).
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Titre Tab. 2: Major oxides concentrations of volcanic glass shards from tephras layers observed in core LM2 (electron microprobe analyses).
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Titre Fig. 5: Geochemical composition of glass shards from the LM2-451 tephra layer and from Avellino
Crédits (Calanchi et al., 1996; Calanchi et al., 1998; Wulf et al., 2004; Magny et al., 2007; Calanchi & Dinelli, 2008; Sulpizio et al., 2008; Turney et al., 2008), Agnano Monte Spina (De Vita et al., 1999; Wulf et al., 2004; Magny et al., 2006; Piochi et al., 2008; Zanchetta et al., 2011) and Astroni (Siani et al., 2004; Smith et al., 2011) tephras plotted in the total alkali versus silica diagram (TAS, Le Bas et al., 1986).
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Titre Fig. 6: K2O versus SiO2 binary diagram (modified after Peccerillo & Taylor, 1976) for volcanic glass shards from tephra layers of LM2 core and the Alban hills, Eolian Islands, Etna, Somma-Vesuve and Phlegrean Fields (Siani et al., 2004). Series: A/ tholeiitic, B1/ low K calc-alkaline, B2/ high K calc-alkaline, C/ shoshonitic series, D/ alkaline series.
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Titre Fig. 7: K2O versus SiO2 binary diagram for chemical analyses of glass shards from the tephra layer LM2-544 and from Avellino, Astroni, Agnano-Monte-Spina eruptions (for authors, see figure 5).
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Titre Fig. 8: FeO versus total alkali and K2O versus SiO2 binary diagrams for chemical analyses of glass shards from the tephra layer LM2-640 and from Campanian province (for authors, see figure 5), Etna (Corsaro et al., 2004, 2005, 2007; Viccaro et al., 2007; Ferlito et al., 2008; Branca et al., 2009) and Alban Hills (Gaeta, 1998; Freda,2006; Gaeta et al., 2006) eruptions.
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Titre Tab. 3: Campi Flegrei volcanic eruptions during Bronze age. (a) Santacroce et al. (1987), (b) Rolandi et al. (1998), (c) de Vita et al. (1999), (d) Di Vito et al. (1999), (e) Andronico & Cioni (2002), (f) Funiciello et al. (2003), (g) Isaia et al. (2004), (h) Isaia et al. (2009), (i) Sacchi et al. (2009) and (j) Sevink et al. (2011).
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Titre Tab. 4: Comparative table of average chemical compositions of glass hards from LM2-451 tephra and tephras from the litterature. (a) Di Vita et al. (1999), (b) Siani et al. (2004), (c) Wulf et al. (2004), (d) Magny et al. (2006), (e) Piocchi et al. (2008), (f) Sulpizio et al. (2008), (g) Smith et al. (2011) and (h) Zanchetta et al. (2011).
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Fichier image/png, 20k
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Gwénolé Jouannic, Pierre‑Yves Gillot, Jean‑Philippe Goiran, Jean-Claude Lefevre, Giuseppe Siani, Ferréol Salomon et Antonia Arnoldu‑Huyzendveld, « Tephrochronological study in the Maccarese lagoon (near Rome, Italy): identification of Holocene tephra layers », Quaternaire, vol. 24/1 | 2013, 65-74.

Référence électronique

Gwénolé Jouannic, Pierre‑Yves Gillot, Jean‑Philippe Goiran, Jean-Claude Lefevre, Giuseppe Siani, Ferréol Salomon et Antonia Arnoldu‑Huyzendveld, « Tephrochronological study in the Maccarese lagoon (near Rome, Italy): identification of Holocene tephra layers », Quaternaire [En ligne], vol. 24/1 | 2013, mis en ligne le 01 mars 2016, consulté le 21 janvier 2025. URL : http://journals.openedition.org/quaternaire/6494 ; DOI : https://doi.org/10.4000/quaternaire.6494

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Auteurs

Gwénolé Jouannic

Laboratoire Chrono-Environnement, UMR 6249 CNRS/UFC, 16, route de Gray, F-25030 BESANÇON cedex. Email : gwenole.jouannic@univ‑fcomte.fr

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Pierre‑Yves Gillot

Université Paris-Sud, Laboratoire des Interactions et Dynamique des Environnements de Surface (IDES), UMR CNRS 8148, Bâtiment 504, F-91405 ORSAY cedex. Email : pierre-yves.gillot@u-psud.fr;

Jean‑Philippe Goiran

 CNRS - UMR 5133 - Maison de l’Orient et de la Méditerranée, 7 rue Raulin, 69007 LYON. Email : jean‑philippe.goiran@mom.fr;

Jean-Claude Lefevre

Centre de Datation par le Radiocarbone, UMR 5138 CNRS/UCB/ Maison de l’Orient et de la Méditerranée, 40 Bd Niels Bohr, F-69622 VILLEURBANNE cedex. Email : jean-claude.lefevre@univ-lyon1.fr;

Giuseppe Siani

Université Paris-Sud, Laboratoire des Interactions et Dynamique des Environnements de Surface (IDES), UMR CNRS 8148, Bâtiment 504, F-91405 ORSAY cedex. Email : giuseppe.siani@u-psud.fr;

Ferréol Salomon

Université de Lyon - UMR 5600, 5 avenue Pierre Mendes-France, F-69676 BRON cedex. Email : ferreol.salomon@univ-lyon2.fr;

Articles du même auteur

Antonia Arnoldu‑Huyzendveld

 Digiter S.r.l., Via della Fortezza, 58, I-0004 ROCCA DI PAPA (RM). Email : digiter@libero.it

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