Appendix A. Supplementary data

Appendix A. Supplementary data

related to the article:

Luberti, G. M., Marra, F., & Florindo, F. (2017). A review of the stratigraphy of Rome (Italy) according to geochronologically and paleomagnetically constrained aggradational successions, glacio-eustatic forcing and volcano-tectonic processes. Quaternary International 438(B), 40-67. doi: 10.1016/j.quaint.2017.01.044.

A review of the stratigraphy of Rome (Italy) according to geochronologically and paleomagnetically constrained aggradational successions, glacio-eustatic forcing and volcano-tectonic processes Gian Marco Luberti (*), Fabrizio Marra (**), Fabio Florindo (**)

(*) I.S.P.R.A. - Istituto Superiore per la Protezione e la Ricerca Ambientale, Via V. Brancati, 48 - 00144 Roma, Italy. (**) I.N.G.V. - Istituto Nazionale di Geofisica e Vulcanologia, Via di Vigna Murata, 605 – 00143 Roma, Italy. Corresponding Author: Fabrizio Marra, tel. +39 06 5186 0420, fax: +39 06 5186 0507, e-mail: [email protected]

Supplementary information In this supplementary text we provide a discussion describing the scientific evidence and/or the ethical reason supporting the revision of the stratigraphic units introduced by the official geological maps realized for the CARG Project and for the Municipality of Rome (Funiciello et al., 2008; Funiciello and Giordano 2008a, 2008b, 2008c) and that we have reported in grey (proposed for rejection) and in italics (proposed for chronostratigraphic relocation) in Table 3 of the main text (and also included here). Moreover, several stratigraphic units not reported in the official maps are also included and described. Each unit is discussed in stratigraphic descending order in the following sections; a proposal for rejection or relocation is provided at the end of each section. 1. Tavolato Formation (TAL) In contrast to the attribution of an age younger than 5 ka by Funiciello and Giordano (2008a; 2008b), these deposits have been shown to be part of the sin-eruptive and immediately post-eruptive depositional processes occurred 69±1 through 36±1 ka in consequence of the activity of the Albano Maar. In particular, the uppermost deposit of the Ciampino plain cropping out at the Ciampino Bowling (see Fig. 13 in the main text) is characterized by the occurrence of a primary pumice fall deposit at its base, which is geochemically and geochronologically correlated with that occurring at the base of the last eruptive cycle (Albano Unit 7, 36±1 ka; Freda et al., 2006; Giaccio et al., 2009). The occurrence of lahar phenomena in historical ages was also ruled out based on the archaeological evidence of a lake level close to the present day elevation at the times of the construction of the Roman emissary tunnel, as implicit in its constructive technique (D'Ambrosio et al., 2010), 70 m lower than the lowest point along the crater rim facing the Ciampino Plain. A fact preventing any possible overspill of the Albano Lake in Roman times. D'Ambrosio et al. (2010) also remarked the wrong reference of Tito Livio's report about the occurrence of the lake overflow made in Funiciello et al. (2002; 2003). Indeed, the Latin author describes the phenomenon as "an unusual increase of the lake level" which induced the Roman engineers to realize the lake emissary, as opposed to the version by Dionigi di Alicarnasso, describing a less reliable catastrophic overflow of the lake waters. Finally, the occurrence of historical reworked deposits within the Ciampino and the Tor Vergata areas has been related to the emplacement of large colluvial and alluvial deposits filling the paleo-incisions since the Bronze age, a feature common to all the post-galcial alluvial

successions, as evidenced in the Grottaperfetta stream valley (Cinti et al., 2008) and in the main Tiber valley (Marra et al., 2013). Proposal: The Tavolato Formation should be removed and the corresponding deposit attributed to the activity of Albano Maar spanning 69-36 ka.

2. Sandy-cobble lithofacies (MNNa) This is the uppermost unit of the Tavolato Formation that Funiciello and Giordano (2008a) refer as a historical lahar deposit, firstly identified by Giordano et al. (2002) on petrographic and sedimentologic basis. However, no radiometric constraint for such unit is available, and there is no reason to think that this deposit is not the sin-eruptive lahar deposit of the Albano unit 6 (Peperino Albano), as reported by Giaccio et al. (2007; 2009). On the other hand, the occurrence of lahar deposits triggered by overspill of the Albano Lake in Roman Epoch has been excluded based on the series of historical, archaeological, hydraulical, and hydrogeological evidence mentioned in the previous section and described in detail in D'Ambrosio et al. (2010). Proposal: The Sandy-cobble lithofacies unit should be removed.

3. Albalonga Unit (UAL), Villa Doria Unit (SDV), Peperino di Albano (MNN), Cantone Unit (STL), Corona del Lago Unit (KRL), Coste dei Laghi Unit (DSN), Montagnaccio Unit (TGO) These units are the products of the Albano Maar eruptive activity (Funiciello and Giordano, 2008a). However, in the 1:50,000 Rome's map (Funiciello et al., 2008) and in its legend these units are not present. For most of these units Funiciello and Giordano (2008a) report the age determinations by Freda et al. (2006), so the units are related to the seven eruptive units already introduced and described by these authors, whose chronostratigraphy was refined by Giaccio et al. (2009), who correlated the proximal seven units with four distal units. Proposal: These units should be removed and, based on the seven units identified by Freda et al. (2006), replaced by the Albano 1-7 units reported by Giaccio et al. (2009). Moreover, the stratigraphic position of Peperino di Albano reported by Funiciello and Giordano (2008a) is incorrect, since this is the sixth eruptive unit and not the fifth one.

4. Pavona Unit (PVN), Quarto Laghetto Unit (KLG) The deposits cropping out on the rim of the crater originally called Giuturna by Fornaseri et al. (1963) have been recently correlated through 40Ar/39Ar ages and petrographic/geochemical data to the Albano Unit 1 and Unit 3 of 69±1 ka (Marra et al., 2016a). Proposal: These units should be removed and the deposits attributed to the Albano First Eruptive Cycle (Freda et al, 2006).

5. Saccopastore Unit (SKP) The Saccopastore deposits were attributed to the "Tyrrhenian stage" (MIS 5.5) based on the classification of the sedimentary deposits as a fluvial terrace of the last interglacial stage, made at the time of the discovery (Blanc, 1939). In contrast, Marra et al. (2015) have shown that the fluviallacustrine deposits of Saccopastore correlate with the aggradational succession deposited within the

Tiber and Aniene river valleys (Karner & Marra, 1998) in response to post-glacial sea-level rise during GT III, at the onset of MIS 7. Thus they are attributed to the Vitinia Formation. Marra et al. (2015) also recognized an aggradational sequence, named Epi-Tyrrhenian Formation, being equivalent to the marine deposits firstly recognized in the coastal area by Hearty and Dai Pra (1986) and included in the Eutyrrhenian Formation by Conato et al. (1980), which was correlated to MIS 5.5 thorough the age of a tephra layer occurring in its upper portion in Cava Rinaldi and dated 129±2 ka. These continental deposits are present along the coast in terraces at an elevation of about 35-40 m a.s.l., whereas they seem not to be present in the urban area, being probably eroded during the Last Glacial Maximum (Marra et al., 2015; 2016b). Proposal: This unit should be removed, and their deposits included into the Vitinia Formation.

6. Riserva della Macchia Unit (RDM) Funiciello and Giordano (2008a; 2008b) describe this unit as fluvial-lacustrine deposits outcropping close to the coast, in the sector south to the Tiber delta. However, no age is provided by radiometric constraint and no stratigraphic relationships are reported, and no reference is given to support their existence as a separate unit. Elevation of the deposits ranging 15-25 m a.s.l. accounts for their correlation with the terrace correlated to MIS 5.3 (and possibly with that of MIS 5.1, at least in part) by Marra et al. (2016b), and should be considered as part of the Epi-Tyrrhenian Formation. Proposal: This unit should be removed, and its deposits included into the Epi-Tyrrhenian Formation.

7. Tenuta di Campo Selva Unit (TSV) Funiciello and Giordano (2008b) report that this unit is known through a quarry site description given by Arnoldus-Huyzendveld et al. (1991), but not list it in the references. According to Funiciello and Giordano (2008b) this unit comprehends beach, lagoon, aeolic and fluvial facies deposits. Although no radiometric constraint is provided, nor its stratigraphic relationships with other units are described, this unit is correlated with MIS 7. In contrast, based on elevation at 26 m a.s.l., of the terraced surface mapped in Tenuta di Campo Selva where the outcrop reported by Funiciello and Giordano (2008b) is located, Marra et al. (2016b) identified it as the coastal terrace of the MIS 5.3 sub-stage, equivalent to that ascribed to the Riserva della Macchia unit. Proposal: The deposits cropping out in Tenuta di Campo Selva should be considered a sub-unit of the Epi-Tyrrhenian Formation, like those of the Riserva della Macchia unit. Based on its more constrained elevation and thus more reliable correlation with the terrace at around 26 m a.s.l., we have introduced a sub-unit named Tenuta di Campo Selva in Table 3 to designate the deposits of the intermediate Tyrrhenian terrace of MIS 5.3.

8. Vitinia Formation Unit (VTN), Via Nomentana Unit (NMT) The Vitinia Formation Unit is positioned by Funiciello and Giordano (2008a; 2008b; 2008c) and by Funiciello et al. (2008) stratigraphically below the Tufo Giallo di Sacrofano (TGS), which they improperly renamed (see ahead) as Via Nomentana Unit, and whose age is 285±2 ka (Karner et al., 2001). In contrast, several 40Ar/39Ar age determinations strictly constrain deposition of the Vitinia Formation in the time span 269±4 - 208±2 ka, providing correlation with MIS 8.2 through 7.1

(Marra et al., 2016c; Villa et al., 2016). Therefore, this unit is more recent than the TGS and should be placed above it. Moreover, the age determination in Karner et al. (2001) was provided on a sample of TGS collected in Via Nomentana, therefore the re-naming of this volcanic unit is totally unjustified. Proposal: The Vitinia Formation must be placed above the TGS and the Via Nomentana unit name should be removed.

9. Via Mascagni succession (VM) (not reported by Funiciello et al., 2008; Funiciello and Giordano 2008a; 2008b; 2008c) The sedimentary deposits underlying the TGS at the Sedia del Diavolo and Via Mascagni sections (Palombo et al., 2004) represent a sub-sequence deposited during sea-level oscillation of MIS 8.5 (Marra, 2004) named Via Mascagni succession (Marra et al., 2014a). In contrast, Funiciello and Giordano (2008a; 2008b; 2008c) and Funiciello et al. (2008) include these deposits in the younger Vitinia Formation. Proposal: The sedimentary deposits underlying the TGS should be introduced under the name of Via Mascagni succession and placed in the correct chronostratigraphic position between TGS and Aurelia Formation.

10. Madonna degli Angeli Formation (FKB), Tuscolo Member Lava Units (FKBi1a), Castiglione Member (FKB2), Lava Units (FKBa), Pyroclastic Units (FKBb) The Madonna degli Angeli succession was firstly introduced by Giordano et al. (2006), as a suite of heterogeneous volcanic deposits emplaced above the Pozzolanelle pyroclastic-flow deposits during the post-calderic phase of the Villa Senni eruption cycle. Marra et al. (2009) and Gaeta et al. (2016) established ages ranging 365-351 ka for the products of this volcanic phase and an overall duration of 15±4 ka for the whole Villa Senni eruption cycle. However, Funiciello and Giordano (2008b) included in the Madonna degli Angeli Formation and mapped (Funiciello and Giordano 2008a; Funiciello et al., 2008) as part of this succession several more recent products, which do not belong to the post-calderic phase of the Villa Senni eruption cycle, but are part of the successive Faete Phase (308±4 - 241±5 ka; Gaeta et al., 2016). The latter is separated by a ca. 45 ka long dormancy with respect to the end of the previous cycle and should be distinguished and mapped separately. In particular, the Lava Units FKBa include the Capo di Bove Lava, dated at 277±2 ka by Karner et al. (2001). The Tuscolo member Lava Units FKBi1a include the Saponara and Osa lava flows, dated 277±2 ka (Karner et al., 2001) and at 297±4 ka (Marra et al, 2003), respectively. More in general, a wide range of scoria cones and lava flows all dated in the time span 308 - 241 ka corresponding to the Faete Phase of activity (Marra et al., 2003; Gaeta et al., 2016) are included by Funiciello et al. (2008) in the Madonna degli Angeli Formation. Proposal: The correct name of Madonna degli Angeli succession (Giordano et al., 2006; Gaeta et al., 2016) should be adopted and referred only to the products of the post-calderic activity of the Villa Senni eruption cycle, ranging 365-351 ka.

11. Castelporziano Unit (CLZ)

This unit is mapped by Funiciello et al. (2008) at the top of the terrace between Castelporziano and Pomezia, and placed in lower stratigraphic position with respect to the nearby deposits of the Aurelia Formation (AEL). However, based on reconstruction of the terraced surfaces correlated with MIS 9, MIS 7 and MIS 5 in this area by Marra et al. (2016b), the deposits cropping out in Castelporziano are interpreted as the inner dune at the rear of the MIS 9 coastal terrace and should be included (even as a sub-unit) in the Aurelia Formation. Proposal: The Castelporziano Unit should be removed and the corresponding deposits included in the Aurelia Formation.

12. Pebbly-sandy lithofacies (VSNa) According to Funiciello and Giordano (2008a; 2008b) this unit is emplaced with lahar mechanism above the Pozzolanelle (PL) pyroclastic-flow deposit, based on the lack of a paleosoil separating the two units. However, in our opinion this deposit should be interpreted as deriving by the reworking of the PL deposit during the regressive phase of MIS 10 and should be considered the MIS 10/9 equivalent of the "Conglomerato Giallo", which originated from the Pozzolane Rosse during MIS 12/11. It should be therefore considered a sedimentary unit part of the Aurelia Formation. Proposal: This unit should be removed, and the deposits included as sub-unit into the Aurelia Formation.

13. Valle Marciana Unit (MAK), Prata Porci Unit (PRK), Pantano Secco Unit (PSK) Valle Marciana has been recently dated at 102±2 ka, whereas ages of Prata Porci and Pantano Secco centers are assessed at 365±1 and 364±1 ka, respectively (Marra et al. 2016a). In contrast to this geochronologic evidence, Valle Marciana Unit (MAK) is positioned by Funiciello and Giordano (2008a; 2008b) and by Funiciello et al. (2008) stratigraphically below the Ariccia Unit, which is dated at 201-204 ka (Marra et al., 2003). Moreover, Funiciello and Giordano (2008b) consider the volcanic centers of Prata Porci (PRK) and Pantano Secco (PSK) as part of the "Via dei Laghi" Synthem, and attribute to them ages younger than 200 ka (Upper Pleistocene p.p.). Proposal: All these units should be repositioned according to their radiometric ages, which also provide their stratigraphic order, with the latter two units belonging to the Villa Senni Eruptive cycle.

14. Nuova California Unit (NCF) This sedimentary unit has no radiometric constraint and no precise literature references. Funiciello and Giordano (2008b) describe this unit as composed of beach, lagoon, and fluvial deposits, outcropping in the Pomezia and Ardea area. In addition, Funiciello et al. (2008) do not include this unit in the legend, as well as in the map. Based on elevation ranging 36-41 m a.s.l. the deposit are to be ascribed to Epi-Tyrrhenian Formation (Marra et al., 2016b). Proposal: This unit should be removed.

15. Tufi Stratificati Varicolori di La Storta (LTT)

Funiciello and Giordano (2008a; 2008b; 2008c) and Funiciello et al. (2008) place this unit between the Tufo Rosso a Scorie Nere (449±2 ka) (RNR) and the Pozzolane Nere (407±3 ka) (PNR) pyroclastic-flow deposits. A suite of undistinguished pyroclastic fall deposits was originally reported as the "Tufi Stratificati Varicolori di La Storta" by Mattias and Ventriglia (1970). Marra et al. (2014b) distinguished and dated several units: the 447±7 ka Fall E and the 444±7 ka Fall F, erupted in the final stages of the Tufo Rosso a Scorie Nere Eruptive cycle; the 416±6 - 410±2 ka Vico α fallouts from the Vico Volcanic District (Cioni et al., 1987), and the Sant'Abbondio Ashfall Succession (SA), whose early deposits were dated at 387±4 ka, while the latest one have a poorly constrained age of 375±40 ka. Proposal: This unit should be removed and the corresponding deposits should be designated by the names introduced by Marra et al. (2014b).

16. Fosso del Torrino Formation (FTR) Funiciello and Giordano (2008a; 2008b; 2008c) and Funiciello et al. (2008) place this unit between the Pozzolane Rosse (456±4 ka) (RED) and the Tufo Rosso a Scorie Nere (449±2 ka) (RNR) pyroclastic-flow deposits. However, deposition of this unit cannot be distinguished from that of the San Paolo Formation, which occurred during glacial termination V, mainly in the time span 437 410 ka (Marra et al., 2016c). Indeed, there is no evidence that the Fosso del Torrino Unit emplaced before 449 ka, and even in this case it should be included within the San Paolo Formation. Proposal: The stratigraphic position of this unit is incorrect and its name is not justified; it should be named as San Paolo Formation and repositioned above the Tufo Rosso a Scorie Nere Unit (RNR).

17. Tufi Stratificati Varicolori di Sacrofano (SKF), Prima Porta Unit (PPT) According to Funiciello and Giordano (2008a; 2008b), the Tufi Stratificati Varicolori di Sacrofano Unit mainly consists of fallout deposits, including two or occasionally three pumice levels already known as “Granturchi” (Fornaseri et al., 1963), that Karner et al. (2001) had geochronologically constrained and re-named as Tufi Terrosi con Pomici Bianche. However, this unit was firstly introduced by Mattias and Ventriglia (1970) to designate a large suite of heterogeneous, undistinguished Monti Sabatini volcanic deposits comprised between the Tufo Giallo della Via Tiberina (546±3 ka) and the Tufo Rosso a Scorie Nere (449±2 ka). A detailed chronostratigraphy of the deposits emplaced in this time span was provided in Karner et al. (2001) who recognized two previously undetected large pyroclastic-flow forming eruptive cycles (Tufo Giallo di Prima Porta, TGPP, 514±6 ka; Grottarossa Pyroclastic Sequence, GRPS, 508±9 ka), and a suite of ash- and pumice-fall deposits (Tufi Terrosi con Pomici Bianche, TTPB, 487±4 ka). A detailed stratigraphy of the TTPB was provided in Sottili et al. (2004), who recognized three main pumice-and-scoria fallout units (Fall A, Fall B, Fall C), as well as a later unit (Fall D) representing the basal Plinian fallout of the TRSN eruption cycle. Ages of Fall A and Fall B were re-assessed at 496±3 - 491±14 ka by Marra et al. (2014b). Proposal: This unit is outdated and should be removed and replaced by the geochronologically constrained deposits erupted in the corresponding time-span: TGPP, GRPS, TTPB. Moreover, the re-nomination of the TGPP as Prima Porta Unit is not justified. 18. Valle Giulia Formation (VGU)

Funiciello and Giordano (2008a; 2008b; 2008c) and Funiciello et al. (2008) place the Valle Giulia Formation below the Palatino Unit (PTI), dated 530±2 ka (Marra et al., 2009). However, deposition of the deposits of the Valle Giulia Formation occurred during glacial termination VI at the onset of MIS 13, between 530±2 and 487±4 ka (Karner and Marra, 1998). Indeed, this aggradational succession is mainly emplaced above the Tufo del Palatino pyroclastic-flow deposit (TP: 530±2 ka, Marra et al., 2009), which in northern Rome rests directly above the basal gravel layer of the Valle Giulia Formation (e.g.: km 8 of Via Flaminia, see Fig. 10 in the main text). Proposal: This unit should be stratigraphically located in a protracted time span, encompassing TP and TTPB (see Figure 6 in the main text).

19. Ashfall Succession (AF) (not reported by Funiciello et al., 2008; Funiciello and Giordano 2008a; 2008b) Marra et al. (2009) identified a suite of ash- and scoria-fall deposits in the locality of Cave, 20 km east of Rome, and at km 10 of Via Tiburtina, comprised between the Tufo di Acque Albule (427±2 ka) and the Pozzolane Rosse (456±4 ka) pyroclastic-flow deposits. The basal and an upper fallout deposit of this succession were dated at 517±1 and 500±3 ka, respectively. Proposal: This unit should be included in the stratigraphic succession of Rome.

20. Casale del Cavaliere Unit (KKA) The Casale del Cavaliere Unit (De Rita et al., 2002) was previously identified by Karner et al. (2001) who named it Tufo di Bagni Albule, and described its chronostratigraphic and petrographic feature in the type-section at km 17.3 of Via Tiburtina, nearby the Bagni di Tivoli (Acque Albule) locality. A comment by Karner et al. (2006) remarked on the inopportune re-naming of this volcanic unit. Marra et al. (2009) dated this unit 427±2 ka, including it in the Tufo del Palatino eruption cycle (530±2 - 427±2 ka), and revising its stratigraphic position with respect to the Tufo Giallo di Prima Porta (TGPP, 514±6), previously placed below the Tufo di Bagni Albule in the correlative cross-sections by Karner et al. (2001). These authors also revised the name into Tufo di Acque Albule, according to the correct spelling of the locality. However, Funiciello and Giordano (2008a; 2008b; 2008c) and Funiciello et al. (2008) still locate this unit above the Prima Porta Unit (Tufo Giallo di Prima Porta, 514±6 ka), in evident stratigraphically inconsistent position. Proposal: The Casale del Cavaliere Unit should be renamed as Tufo di Acque Albule, and should be repositioned between Tufo del Palatino and Tufo Giallo di Prima Porta.

21. Tor de’ Cenci Unit (TDC) The formal name of this unit, Tufo Pisolitico di Trigoria (TPT), was introduced by Karner et al. (2001) based on the type-locality in which Palladino et al. (2001) described the litostratigraphic features of this stratified, pyroclastic-flow and surge-flow deposit. Karner et al. (2001) dated it at 561±2 ka, remarking the incorrectness of the previously adopted name (Tor de' Cenci: Marra & Rosa, 1995). Proposal: The unit should be renamed as TPT.

22. Fosso di Malafede succession (FM), Vitinia gravels (not reported by Funiciello et al., 2008; Funiciello and Giordano 2008a; 2008b) Marra and Florindo (2014) identified a minor aggradational succession, erosively above the upper portion of the Santa Cecilia Formation cropping out at the Fosso di Malafede, and correlated it with the sea-level oscillation during sub-stages 15.2/15.1, through the geochronologic constraints provided by age of an intercalated tephra dated 591±6 ka (Marra et al., 2009), and by that of the overlying Tufo Pisolitico di Trigoria (561±2 ka). Moreover, an early aggradational phase corresponding to the deposits recovered in the INGV borehole was also recognized by Marra and Florindo (2014), as evidenced by the occurrence of a pyroclastic-flow deposit dated 649±4 ka (Karner et al., 2001; Florindo et al., 2007) above a 6 m thick gravel layer whose deposition largely preceded the canonical GT VII at 621 ka (Lisiecki & Raymo, 2005). This sub-sequence has been named "Vitinia gravels" in Marra et al. (2014a), however, based on stratigraphic and paleogeographic reconstruction in Marra and Florindo (2014), those cropping out in Vitinia (Conato et al., 1980) are more likely the gravels of the main aggradational phase of the Santa Cecilia Formation, occurring at the onset of MIS 15.5 around 620 ka, whereas the only so far recognized deposit of the early aggradational phase should be considered that recovered in the INGV borehole. Proposal: The sedimentary deposits belonging to the Fosso di Malafede succession should be introduced in the stratigraphic succession as a distinct unit, above the Santa Cecilia Formation.

23. Fosso della Crescenza Formation (FCZ) Funiciello and Giordano (2008a; 2008b) describe this unit as consisting of fluvial and palustrine, mainly fining-upward deposits, already known in literature as Maremmano Auctt.. However, as already remarked by Marra and Rosa (1995), the "Maremmano" comprehends different sedimentary successions, including the Paleotiber 2b and Valle Giulia Formations. According to geologic sections provided by Funiciello and Giordano (2008a; 2008c) and Funiciello et al. (2008), in the urban area the deposits attributed to the FCZ Unit mostly match with the Santa Cecilia (SC), the Ponte Galeria 1 (PG 1), and the Ponte Galeria 2 (PG 2) Formations, as described in Marra and Florindo (2014). Moreover, Karner and Marra (1998) have correlated fluviallacustrine succession with gravel at the base cropping out in Via Flaminia Nuova at the confluence of the Acquatraversa and Crescenza valleys to the San Paolo Formation, based on the age of 462±7 ka of a reworked tephra layer occurring at the top of the gravel. In contrast, a fining-upward succession occurring around 70 m a.s.l. in the Crescenza Valley (Blanc et al., 1953), correlates the analogous continental sediments of the Monte Ciocci Formation described, at the same elevation, in the Gianicolo - Monteverde ridge by Marra (1993). Proposal: This unit should be removed and the correct attribution of the deposits, ranging from the Monte Ciocci to San Paolo Formations, should be re-evaluated in each geologic section.

24. Sandy Litho-facies (PGL3c) Funiciello and Giordano (2008a; 2008b) have preferred to adopt a subdivision for the Ponte Galeria Formation (PGL) based on the lithofacies description, rather than refer to the litho-stratigraphic units introduced by Conato et al. (1980) and used by successive authors (e.g.: Milli, 1997; Milli et al., 2008; Marra et al., 1998). In Table 3 we have reported the correlation among these standard

units and those re-named in the CARG maps. However, the Sandy Litho-facies (PGL3c) that Funiciello and Giordano (2008a) have reported as the uppermost unit of the PGL is in reality the basal portion of the Santa Cecilia Formation. Actually, this sand horizon includes the tephra layer dated 607±6 ka by Karner and Renne (1998) and used as one geochronologic constraint to institute the SC Formation and correlate it with MIS 15 by Karner and Marra (1998). Proposal: This unit name should be removed and the deposits ascribed to the Santa Cecilia Formation.

25. Clayey-sand Lithofacies (PGLb), Conglomerate Lithofacies (PGLa) Funiciello and Giordano (2008a; 2008b) include these two lithofacies into the Ponte Galeria Formation, although they explicitly report the occurrence of the deposits at 60-50 m a.s.l. in the Monte Mario and Gianicolo areas, where they were identified as the formally introduced earliest aggradational succession of the Paleotiber, the Monte Ciocci unit (Marra, 1993). Proposal: These unit names should be removed and the deposits ascribed to the Monte Ciocci Formation.

26. Monte delle Piche Formation (MDP) Funiciello and Giordano (2008a; 2008b) describe the "Monte delle Piche" series introduced by Conato et al. (1980) as a more than one hundred meter thick clayey marine succession in stratigraphic continuity with the underlying Monte Mario Formation. They therefore consider this unit older than the Monte Ciocci Unit that Marra (1993), instead, considered the basal conglomerate of a transgressive cycle leading to the deposition of the marine deposits of Monte delle Piche. According to Funiciello and Giordano (2008a; 2008b) the uncomformity reported by Marra (1993) between the Monte Mario and Monte delle Piche Formations is not supported by stratigraphic or paleontological data. However, the discontinuity between the two successions is clearly attested by biostratigraphic data in Carboni (1980) who describes a sterile sand horizon at -20 m a.s.l., testifying a drastic sea-level drop, and a second sandy horizon at -64 m a.s.l., evidencing another bathimetric upwelling. The lowest discontinuity has been better evidenced in a dedicated borehole (“MG2”; Marra & Florindo, 2014) which found a 8 m thick sand level with abundant benthic species between -45 and -58 m a.s.l.. The two sandy horizons mark as many transgressive cycles correlated with the ingressive deposits of Monte delle Piche (Marra, 1993) and of the PG1 succession (Marra & Florindo, 2014). These horizons are traced back toward the inland in a SW-NE cross-section integrating borehole data reported in Marra (1993) with new borehole data by Marra and Florindo (2014), allowing at correlating them with the basal gravel horizons of the PG 1 and of the Monte Ciocci Formations, respectively. Proposal: The Monte delle Piche Unit should be considered a sub-unit of the Monte Ciocci Formation and collocated above the Monte Ciocci Unit, with which it constitutes the Monte Ciocci Formation.

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Table 3 - Chrono-litho-stratigraphic succession of Rome as defined in the present work, based on 40 Ar/39Ar ages of volcanic products and correlation of aggradational successions with sea-level rise during glacial terminations. First column provides correlation with marine isotopic stage (MIS; first row) and Glacial Termination (T, second row). Numbering of isotopic stages after Bassinot et al. (1994). Second column provides ages for the isotopic intervals reported in first column (first row), and ages for glacial terminations (second row), after astrochronocalibration by Lisiecki and Raymo (2005), with the exception of the last glacial termination (T-I) for which is reported the age of Melt-water pulse 1A after Stanford et al. (2006). 40Ar/39Ar ages of the eruptive cycles and eruptive units after Gaeta et al. (2016) and Marra et al. (2016c) and references therein, are also provided in this column. The third column provides names of the Formations and of the successions (see also Fig. 2a in the main text) corresponding to the aggradational successions. The fourth and fifth columns provide names of the volcanic units and their 40Ar/39Ar ages. The sixth column reports nomenclature and stratigraphic units introduced by the official 1:50,000/1:10,000 geologic maps (Funiciello and Giordano 2008a; Funiciello et al., 2008; Funiciello and Giordano 2008c), in italic if the units were placed in an incorrect position in the stratigraphic column (here are moved into the correct, geochronologically constrained position); in grey text the units that should be removed, because of the not justified introduction of a different name with respect to the previous literature name (either when the stratigraphic position and the age constraints of the unit previously introduced have not changed, as well as when the unit is placed in different stratigraphic position but in reality corresponds to another, already introduced one). For newly introduced units, placed in a wrong chronostratigraphic position, that do not corresponds to any other previously introduced unit, the name proposed by Funiciello et alii (2008) is adopted, but re-placed in the chrono-lithostratigraphic scheme correctly, according to geochronologic/morphostratigraphic constraints. In square brackets: units without any chronostratigraphic constraint. See text and supplementary online material for details. The Plio-Pleistocene marine successions are reported in the last rows according to chronology proposed by Cosentino et al. (2009). All 40Ar/39Ar ages are calibrated for the Fish Canyon Tuff sanidine standard at 28.02 Ma and the Alder Creek sanidine at 1.194 Ma (Renne et al., 1998); errors are reported at 2σ uncertainty. Ages in italic for Eruption Units are assessed on weighted mean of more samples or according to criteria reported in Marra et al., 2014a.