NEW BIOSTRATIGRAPHIC AND LITHOLOGICAL DATA ON THE NEOGENE AND QUATERNARY OF THE LIVORNO AREA (TUSCANY, CENTRAL ITALY) - Riviste ...
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Rivista Italiana di Paleontologia e Stratigrafia
(Research in Paleontology and Stratigraphy)
vol. 126(3): 725-749. November 2020
NEW BIOSTRATIGRAPHIC AND LITHOLOGICAL DATA ON THE NEOGENE AND
QUATERNARY OF THE LIVORNO AREA (TUSCANY, CENTRAL ITALY)
RITA CATANZARITI & SIMONE DA PRATO
Istituto di Geoscienze e Georisorse (IGG) CNR Pisa, Via G. Moruzzi 1, 56126 Pisa. E-mail: catanzariti@igg.cnr.it, simone.daprato@igg.cnr.it
To cite this article: Catanzariti R. & Da Prato S. (2020) - New biostratigraphic and lithological data on the Neogene and Quaternary of the
Livorno area (Tuscany, Central Italy). Riv. It. Paleontol. Strat., 126(3): 725-749.
Keywords: Calcareous nannofossils; Foraminifers; Ostracods; Stratigraphy.
Abstract. Lithofacies analyses and datings using calcareous nannofossils, proved to be an excellent opportunity
to understand the palaeoenvironmental evolution of the area of the Tuscan coast, washed up by the Ligurian Sea.
A multidisciplinary approach, through lithological and micropaleontological data, collected from fifteen boreholes
and one outcrop, permitted the characterization of ten stratigraphic units in the subsurface of the Livorno area.
The correlations of these units depicted a stratigraphic architecture chronologically constrained. This study detected
early Pliocene (Zanclean) and early Pleistocene (Gelasian) marine deposits, referable to the outer neritic zone that
were dated to the calcareous nannofossil biozones MNN13, MNN14-15 and MNN18. In addition, early Pleistocene
(Calabrian) marine deposits, dated to the calcareous nannofossil biozones MNN19b, MNN19d, MNN19e, which may
be attributed to different bathymetric depths on the basis of benthic foraminifers and ostracods, highlighted sea level
changes. Finally, the areal distribution and the stratigraphic architecture of these units permitted the recognition and
the better constraining of the sedimentary dynamics impacted by major eustatic and tectonic changes.
Introduction surface stratigraphy. We took advantage of this situ-
ation taking into account new continuously-cored
The Livorno area is located in the Tuscan re- boreholes to investigate the Neogene-Quaternary
gion (Central Italy) on the Ligurian Sea coast (Fig. subsurface deposits, combining lithological and mi-
1). This is a highly urbanized area with all the con- cropaleontological analyses.
sequent issues, including soil pollution, saltwater The area was extensively studied in the
intrusion, groundwater contamination and soil seal- past by Barsotti et al. (1974); Ciampalini (2002);
ing. Tackling these problems requires knowledge Dall’Antonia et al. (2004); Ciampalini et al. (2006);
about the area’s geology and public administration Zanchetta et al. (2004, 2006); Bossio et al. (2008);
have promoted the development of scientific re- Ciampalini et al. (2013). These authors not only
search on the subsurface stratigraphy of the Livor- confirmed and enriched the stratigraphy tradition-
no area. In the last decades the development of in- ally proposed for this area, but also highlighted the
frastructure has provided boreholes and ephemeral complexity and the problems related to the sub-
outcrops as new elements for the study of the sub- surface Neogene-Quaternary successions. Howev-
er, by now there have not been detailed biostrati-
graphic studies able to provide useful chronological
constrains. In order to improve the understanding
Received: September 19, 2019; accepted: July 17, 2020 of the subsurface geology of this area, this paper
726 Catanzariti R. & Da Prato S.
aims to provide new biostratigraphic and palaeoen- Morphological and stratigraphical studies
vironmental data based on the study of calcareous have identified some orders of marine terraces lying
nannofossils, ostracods, benthic foraminifers and at different elevations (Fig. 2, Zanchetta et al. 2019),
mollusks, on late Miocene to Holocene marine and the genesis of which was linked to the interaction
continental successions. Stratigraphic correlations between glacio-eustatic oscillations and tectonic up-
and geological reconstructions were also performed lift, during middle and late Pleistocene. The high-
taking into account previous published and unpub- est of these terraces is named Terrazzo della Fat-
lished studies about the subsurface geology of the toria delle Pianacce (Barsotti et al. 1974; Lazzarotto
Livorno area (Barsotti et al. 1974; Dall’Antonia et al. et al. 1990) or Terrazzo I (Federici and Mazzanti
2004; Zanchetta et al. 2006, 2019; Bossio et al. 2008; 1995). This morphostratigraphical unit is placed at
Ciampalini et al. 2013), that are represented as a da- a maximum altitude of 120 m a.s.l., and is overlain
taset of logs and sediment cores organised in GIS to north by the Poggio ai Lecci formation (Barsotti
(Geographic Information System) by the Institute et al. 1974; Marroni et al. 1990) and to south by
of Goescience and Georesources of CNR (IGG- the Conglomerate of Villa Umbero I formation
DATABASE). (Barsotti et al. 1974). It was attributed to MIS 11
(Marcolini et al. 2003; Zanchetta et al. 2006). The
Terrazzo di Salviano (Malatesta 1942; Bossio et al.
Geological and stratigraphic setting 2008), also named Terrazzo di Villa Padula (Bos-
chian et al. 2006), is placed at an altitude of about
The Livorno area is located between the Tus- 40 m a.s.l., its age was related to MIS9c highstand
can coast and the Apennine chain. This area has been (Zanchetta et al. 2019).
affected by extensional tectonic processes linked to The lower of these morphostratigraphical
the eastward migration of the chain as consequence units (Fig. 2), is the Terrazzo di Livorno, also called
of the progressive opening of the Tyrrhenian Sea, Terrazzo II (Barsotti et al. 1974; Federici and Maz-
which has been occurring since Tortonian (Carmi- zanti 1995) that was correlated to MIS5e highstand
gnani et al. 2001). Extensional sedimentary basins (Hearty et al. 1986; Mauz 1999; Nisi et al. 2003;
were formed along normal NNW-SSE faults and Sarti et al. 2017; Zanchetta et al. 2019). On top of
were filled by late Miocene-Quaternary continen- these stratigraphic and morpho-stratigraphic units,
tal and marine sediments (Ghelardoni et al. 1968; the Pleistocene Ardenza Sands mainly occur (Bos-
Mariani & Prato 1988; Bossio et al. 1993; Pascucci chian et al. 2006).
2005) on rocks belonging to the Tuscan and Ligurian
units. In the hills surrounding the study area, Mes-
Material and methods
sinian lower-middle Pliocene and lower Pleistocene
marine deposits and in minor amount middle-late Fifteen boreholes, whose maximum depths range between
Pleistocene continental deposits outcrop (Figs. 1-2). circa -40 m and -10 m, and one outcrop, were sampled and investiga-
The Messinian is mainly represented by conglom- ted (location and details are reported in Fig. 1 and Tab. 1). Detailed
stratigraphic analyses were performed through macroscopic descrip-
erates, clays and gypsum (Era Morta River Clays tion of sediment colour (according to the Munsell Soil Color Charts),
and Gypsum formation, Cerri & Sandrelli 1994), texture, sedimentary structures, macrofossils, plant remains and orga-
covered by the Pliocene Blue Clay Formation. This nic matter. Calcareous nannofossils were used as biostratigraphic tool
late formation is covered by a Pleistocene marine to date marine sediments. Ostracod and benthic foraminiferal faunas
were investigated as palaeoenvironmental indicators, and ostracods
succession, that from the base to the top comprises also allowed the dating of the Messinian continental deposits. In fi-
Santernian-Emilian open sandy silts pertaining to gure 3 it is represented an integrated biostratigraphic scheme where
the Morrona Formation (Boschian et al. 2006), fol- we reported the calcareous nannofossil zones and events of Rio et
lowed by fine to medium-grained sands referable to al. (1990), and the foraminifer zones and events of Iaccarino et al.
(2007), furthermore the ostracod events (from Carbonnel 1978 and
the Emilian Nugola Vecchia Sands (Lazzarotto et Grossi et al. 2011) useful for both dating and correlation are also
al. 1990; Dall’Antonia et al. 2004). Above this lat- shown. In the scheme we propose the stage Calabrian and its sub-
ter lies, through an unconformity, a further marine stages Santernian, Emilian and Sicilian (see Rio 1982), mainly used
to date Italian sediments and useful for correlation with stratigraphic
succession of gravels and sandy silts of Sicilian age units outcropping on the Tuscan coast. The Santernian corresponds
referable to the Fabbriche Sands formation (Barto- to the lower part of the Calabrian (same GSSP as the Calabrian) and
letti et al. 1986; Dall’Antonia et al. 2004). comprises zones MNN19a (upper part), MNN19b and MNN19c;
Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 727
Fig. 1 - Location map of the study
area and schematic geologi-
cal setting. Red points indi-
cate the location of the inve-
stigated boreholes (see Tab.
1 for geographic coordina-
tes). Green squares indicate
the borehole logs included
in the IGG-DATABASE.
The green lines visualize the
cross sections represented in
Fig. 23.
Tab. 1 - Geographic coordinates and
depths of the studied bo-
reholes.
the Emilian corresponds to the middle part of the Calabrian, embra- mainly on microfossils but occasionally other groups (mollusks) were
cing zone MNN19d; the Sicilian corresponds to the upper part of observed in the hand samples. The list of ostracods and foramini-
the Calabrian, spanning zones MNN19e to MNN19f (lower part). fers considered in this paper can be found in Appendix. The relative
For the study of calcareous nannofossils and microfossils abundance of microfossils was evaluated on 50 g of residue. For
were chosen lithologies suitable to contain these fossil groups, so ostracods the classes of abundance are: R (Rare, < 2), F (Few, 3-5),
resulting in a different number of samples prepared. C (Common, 6-10), A (Abundant, >10); for foraminifers they are:
The study of ostracods, benthic foraminifers and occasio- R (Rare, < 10), F (Few, 10-50), C (Common, 50-100), A (Abundant,
nally of planktonic foraminifers, was performed on 146 samples of >100). Palaeocological information on taxa and assemblages and the
approximately 150 g, which were disaggregated in warm water, wa- palaeoenvironmental scheme are derived from literature (e.g. Allen
shed through a 74 μm sieve and finally dried in an oven at 100°C. 1970; Bonaduce et al. 1975; Wright et al. 1978; Athersuch et al. 1989;
The residue was analysed through an optical microscope. Ninety- Sgarrella & Moncharmont Zei 1993; Yassini & Jones 1995; Meisch
four samples that were studied in previous papers (Bossio et al. 2008; 2000; Smith & Horne 2002; Gliozzi & Grossi 2008; Frezza et al. 2009;
Ciampalini et al. 2013) were reanalysed. Investigations were focused Faugno et al. 2015; Adegoke et al. 2017) and summarized in figure 4.
728 Catanzariti R. & Da Prato S.
Fig. 2 - Composite stratigraphy of
the Livorno area, with litho-
stratigraphic and morpho-
stratigraphic units, and cor-
relation with marine isotope
stages (modified from Zan-
chetta et al. 2019).
On the whole, 131 core samples and 2 outcrop samples were ous nannofossil content, only 90 resulted useful to
selected for the analyses of the calcareous nannofossils. The samples
allow a reliable dating of the sediments because sev-
were prepared as smeared-slide using standard procedures (Bown &
Young 1998). Observations were performed using a polarising light eral samples were affected by heavily reworking with
microscope at 1250X magnification. Data were collected in semi- no autochthonous species observed, or resulted to
quantitative form, the relative frequencies of index species were defi- be barren. In the fruitful samples were detected as-
ned counting them in term of specimens in a prefixed area of the slide
(200 fields of view, roughly corresponding to 4 mm2). The abundance
semblages referable to the early Pliocene-late Pleis-
data are reported as letters, R (Rare, < 1 per mm2), F (Few, 1-5 per tocene MNN biozones of Rio et al. (1990) (Fig. 3).
mm2), C (Common, > 5 per mm2), A (Abundant, > 10 per mm2). The The early Pliocene MNN13 Zone was recog-
selected taxa considered in the nannofossil assemblages are referenced nised on the occurrence of assemblages containing
in Young et al. (2017), and we listed theme in Appendix. In this paper
for biostratigraphic purpose we used the scheme proposed by Rio et Amaurolithus delicatus, Helicosphaera sellii, Calcidiscus
al. (1990), therefore we adopted the biometric subdivision proposed macintyrei, Discoaster brouweri, Discoaster pentaradiatus,
by the authors for the genus Gephyrocapsa, so “small Gephyrocapsa” is re- Discoaster surculus and Sphenolithus abies. The early
ferred as specimens smaller than 4.0 mm in size, “medium Gephyrocap-
Pliocene combined MNN14-15 Zone was recog-
sa” is referred as specimens 4.0 − 5.5 mm in size, “large Gephyrocapsa”
is referred as specimens larger than 5.5 mm in size. nised on the presence of C. macintyrei, Discoaster
asymmetricus, D. brouweri, D. pentaradiatus, Discoaster ta-
malis, H. sellii, Pseudoemiliania lacunosa, Reticulofenestra
Results and data pseudoumbilicus and “small Gephyrocapsa”.
The early Pleistocene MNN18 Zone was
Biostratigraphy detected on the presence of rare D. brouweri in as-
Among the samples analysed for the calcare- semblage with forms of “small Gephyrocapsa”, C.
Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 729
Fig. 3 - Integrated biostratigraphic scheme adopted to date the units occurring in the subsurface of the Livorno area. Biozones are plotted ver-
sus the chronostratigraphic scale and Geomagnetic Polarity Time Scale (GPTS, Lourens et al. 2004). The ages of the Marine Isotope
Stages (MIS) are from LR04 18O dataset (Lisieki & Raymo 2005), MIS2=0,029-0,014 Ma, MIS3=0,057-0,029 Ma, MIS4=0,071-0,057,
MIS5=0,130-0,071 Ma, MIS6=0,191-0,130 Ma. Calcareous nannofossil biochronology after Raffi et al. (2016). Foraminifer events after
Iaccarino et al. (2007), ostracod events after Ruggieri (1973, 1980), Ciampo (1998), Guernet (2005), Dall’Antonia et al. (2004), Faranda
& Gliozzi (2008).
macintyrei, H. carteri, H. sellii and P. lacunosa. The early Stratigraphy, dating and palaeoenvironmental
Pleistocene MNN19b Zone was recognised on as- considerations
semblages where C. macintyrei occurs with “medium The boreholes investigated provided a wide
Gephyrocapsa”. The early Pleistocene MNN19d Zone range of lithologies and faunal associations that
was well characterized by the concomitant presence were grouped into different stratigraphic units
of “large Gephyrocapsa”, “medium Gephyrocapsa” (Fig. 5) some of which can be correlated with
and “small Gephyrocapsa”. The early Pleistocene the outcropping formations of the nearby area
MNN19e Zone was recognised on the common to (all data are summarized in Tab. 2). The units are
abundant occurrence of “small Gephyrocapsa”. Fi- described below from bottom to top with all the
nally, assemblages containing rare Emiliania huxleyi stratigraphic, biostratigraphic and palaeoenviron-
with scarce to rare “small Gephyrocapsa” and “me- mental considerations derived both from data
dium Gephyrocapsa”, were attributed to MNN21a- collected for this work and comparisons of data
MNN21b zones. found in literature.
730 Catanzariti R. & Da Prato S.
Fig. 4 - Simplified sketch showing the mainly depositional facies and palaeoenvironments (modified from Allen 1970 and Adegoke et al. 2017).
The bathymetric zonation is modified from Wright et al. (1978). Ostracod and benthic foraminifer schematic assemblages and bathy-
metric distribution of selected taxa found out in this work are also shown (see text and table 2 for more explanations).
Unit 1 - This unit includes two lithofacies (1a leri in the lower part of the unit (up to 16 m) allows
and 1b). Lithofacies 1a comprises mainly brown silty the recognition of the ostracod late Messinian Loxo-
sands and beige-grey silty clays, sometime with mil- concha muelleri biozone of Grossi et al. (2011). The
limetric gypsum crystals. Sporadic intercalations of appearance (from 15.80 m) of the paratethyan taxa
deposits made of heterometric gravels and sands L. djafarovi, E. praebaquana, Ammnicythere sp. (Gliozzi
locally cemented, constitute the 1b. Unit 1 (already 1999) permits the attribution of the upper part of
described in Bossio et al. 2008), was recovered only the unit to the Loxocorniculina djafarovi biozone of
in the south-eastern part of the Livorno area (Magri- Carbonnel (1978); the first occurrence of L. dja-
gnano-S22 borehole, Fig.6), where its maximum farovi can be also related to the astronomical age of
thickness is of about 10 m. The ostracod associations 5.40 Ma (Grossi et al. 2011). This unit represents
are quite rich and diversified, and are characterized the upper part of the post-evaporitic interval in It-
by the common occurrence of the mesohaline spe- aly (Cosentino et al. 2007; Grossi et al. 2011) and
cies Loxocorniculina djafarovi, Euxinocythere praebaquana, can be correlated with the Era Morta River Clays
Ammnicythere accicularia, Tyrrhenocythere pontica and the and Gypsum formation, which outcrops in the sur-
euryhaline species Loxoconcha muelleri, Cyprideis sp. rounding area (Mazzanti 2016).
Benthonic foraminifers are represented primarily by
Ammonia tepida and Ammonia spp. Chara oogonia and Unit 2 - This unit is mainly characterized by
mollusks are also present. These associations indi- massive grey clays and grey silty sand levels with
cate continental environment with oligo-mesohaline common mollusks. It was documented in the Ban-
water (endoreic basin of “Lago-Mare”), as reported ditella, Ardenza-S1 and Salviano-S9 boreholes and
in Gliozzi & Grossi (2008). in the Scasso outcrop (Figs. 7-10). Its maximum
The occurrence of Cyprideis sp. and L. muel- thickness is of about 25 m.
Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 731
Fig. 5 - a) Schematic stratigraphic log of the units (from 1 to 10) occurring in the subsurface of the Livorno area, reconstructed from the
investigated boreholes and outcrop. The thickness of each unit represents its maximum extension. b) Legend of symbols used in
figure 6 to 21.
732 Catanzariti R. & Da Prato S.
Samples from this unit yield well diversified 15). Its maximum thickness is of about 40 m.
and well preserved abundant fossils. The calcareous nannofossils are common in
The calcareous nannofossils are common in all samples showing good to moderate preservation.
all samples and show good to moderate preserva- On the whole, the assemblages contain Calcidiscus
tion. The main represented taxa are C. macintyrei, D. leptoporus, C. macintyrei, Coccolithus pelagicus, specimens
asymmetricus, D. pentaradiatus, D. tamalis, D. variabilis, of Gephyrocapsa muellerae, G. sinuosa, G. ericsonii and
“small Gephyrocapsa”, H. carteri, H. sellii, Pontosphaera G. oceanica that were grouped as “small Gephyro-
spp., R. pseudoumbilicus, and S. abies. In the unit the capsa” , “medium Gephyrocapsa” and “large Gephyro-
Zanclean zones MNN13 (occurrence of H. sellii capsa”, H. carteri, H. sellii, Pseudoemiliana lacunosa and
with A. delicatus, Fig. 7) and MNN14-15 (occurrence small specimens of Reticulofenestra (between 3.0 and
of D. asymmetricus with P. lacunosa, Fig. 8), and the 5.0 μm). Rare and scattered specimens of Ponto-
Gelasian Zone MNN18 (occurrence of D. brouweri sphaera, Rhabdosphaera, Umbilicosphaera and very rare
and “small Gephyrocapsa”, see Figs. 9 and 10) were specimens belonging to the calcareous dinoflagel-
documented. late Thoracosphaera also occur. Reworking is present
Samples taken from the clayey lithofacies of with Cretaceous (Watznaueria, Micula, Aspidolithus),
the Ardenza-S1 borehole (Fig. 8) contain rich mi- and Paleogene (Toweius, Dictyococcites, Discoaster, Sphe-
crofossiliferous assemblages that are represented by nolithus) taxa. Unit 3 can be attributed to the Santer-
the foraminifers Lenticulina cultrata, Lenticulina spp., nian MNN 19b Zone on the occurrence of “me-
Melonis pompilioides, Uvigerina rutila, Planulina arimi- dium Gephyrocapsa” along with C. macintyrei (Figs. 6
niensis and Sigmoilopsis coelata, and by the ostracods and 14), and to the Emilian MNN19d Zone on the
Bythocipris obtusata, Krithe spp., Parakrithe and Hery- occurrence of “large Gephyrocapsa” (Figs. 11-13 and
howella asperrima. These microfossiliferous assem- 15).
blages are indicative of the outer neritic zone; in A generic Calabrian age for Unit 3 is sup-
particular the co-occurrence of Bythocypris spp. and ported by the occurrence of the ostracods Palmocon-
Krithe spp. indicates water deeper than 250 m (Fig. 4, cha subrugosa, Cytheropteron ruggierii and by the “cold
Sciuto et al. 2003; Sciuto & Rosso 2015) and seems guest” Cytheropteron testudo.
to be confined to the MNN14-MNN15 Zone. The lower part of the unit, referable to
Deposits with the same lithologies, refer- Zone MNN19b (Magrignano-S22 and Picchian-
able to MNN18 Zone, were recognised in outcrop ti-S1 boreholes (Figs. 6, 14), contains Aurila spp.,
(Scasso, Fig. 10) and in the Salviano S9 borehole Macrocypris adriatica, Urocythereis sp., Xestoleberis com-
(Fig.9). In outcrop (Scasso, Fig. 10), in this unit were munis, that point out the inner neritic zone (Fig. 4).
also identified planktonic foraminifers mostly rep- The abundance variations of some taxa (e.g. Krithe
resented by Globorotalia aemiliana, Globigerina bulloides, compressa, see Picchianti-S1 borehole, Fig. 14) also
Globigerinoides sacculifer, Orbulina universa, L. cultrata, testify bathymetric oscillations. Lithologies and pa-
Siphonina reticulata, S. coelata, and ostracods manly leobathymetries seem to indicate lower shoreface or
represented by Argilloecia sp., Henryhowella asperrima, proximal offshore. In the part of the unit referable
Krithe compressa, Krithe spp., Parakrithe spp. The ben- to Zone MNN19d, we recognised a main microfos-
thic foraminifers and ostracods indicate that depo- siliferous association, characterised by the common
sition took place at the boundary between the inner occurrence of the foraminifers Valvulineria bradyana,
and outer neritic zone (Fig. 4). Kassidulina neocarinata and Bulimina marginata, and
This unit can be correlated with the Blue the ostracods K. compressa and Cyrtheropteron spp.
Clays Formation that outcrops extensively in the (e.g. C. ruggieri, C. vespertilio). In Viale Carducci bore-
surrounding area. hole (Fig. 13), Unit 3 is characterised by the occur-
rence of deep-water marine species that decrease
Unit 3 - This unit is characterized by sandy numerically from the bottom to the top, while
clays, blue grey sandy silts, with layers of gravels shallow-water marine species such as Palmoconcha
and sands in its lower part. turbida and Leptocythere multipunctata show an oppo-
It was documented in the Magrignano-S22, site trend. This reflects a bathymetric decrease in a
Via Roma, Via Garibaldi-S2, Viale Carducci, Picchi- depositional environment, which was interpreted as
anti-S1 and Via Filzi-S1 boreholes (Figs. 6 and 11- proximal offshore, also testified by the monotonousNeogene and Quaternary of the Livorno area (Tuscany, Central Italy)
Tab. 2 - Summary of all data collected for the units recognised in the Livorno area. The reported foraminifers and ostracods are useful to identify the different environments, calcareous nannofossils allow
for recognising the biozones proposed by Rio et al. (1990) for the Western Mediterranean. The biochronology of the calcareous nannofossil events is that proposed by Raffi et al. (2016). The ages
of Marine Isotope Stages (MIS) are those proposed by Lisiecki & Raymo (2005).
733734 Catanzariti R. & Da Prato S.
Fig. 6 - Stratigraphic log of the Magrignano-S22 borehole with the range chart of selected calcareous nannofossils and microfossils (modified
from Bossio et al. 2008). For symbols see legend in Fig. 3.
fine lithologies. thereis jonesi). In particular, two main biofacies can be
Lithologies, age and microfaunal content link distinguished. In the first one benthic foraminifers
this unit with the Morrona Formation, consequent- occur with abundant A. beccarii, Quinqueloculina semi-
ly it is also etheropic with the Nugola Vecchia Sands nula, and common Ammonia parkinsoniana, E. crispum,
(Boschian et al. 2006, and references therein). Lobatula lobatula and N. boueanum, while ostracods
mainly consist of P. turbida, Pontocyhere turbida and
Unit 4 - This unit is composed of sands and Aurila convexa. These microfauna are characteristic
sandy gravels overlain by a succession of silty-sandy of the proximal inner neritic zone, and the mostly
to clay sediments. sandy lithology in which they occur, is indicative of
It was documented in the Via Pompilia-S3, upper-lower shoreface (Fig. 4, Tab. 2). In the second
Porto Mediceo-S3, Calata Magnale-S7 and Torre biofacies, shallow-water taxa (e.g. Aurila, Ammonia,
Marzocco-S1 boreholes (Figs. 16-19). Its maximum Elphidium, Lobatula) are numerically less represented
thickness is of about 30 m. and in association with frequent specimens of C.
The most represented calcareous nannofos- neocarinata, V. bradyana, Bosquetina carinella and P. jone-
sil specimens are “small Gephyrocapsa”, the amount sii. This assemblage indicates the distal inner neritic
of which varies from common to abundant. This zone, and the lithological characters are indicative
calcareous nannofossils data ascribe the unit to the of proximal offshore (Fig. 4, Tab. 2). The presence
Sicilian MNN19e Zone. of A. cymbaeformis, A. lancaeformis, A. punctata, A.
Fragments of echinoids, and marine mol- punticruciata and Hyalinea baltica allows the attribu-
lusks are frequent. The microfaunal assemblages tion of the unit to the early Pleistocene (Fig. 3).
are characterized by abundant well diversified fora- Age and lithologies allow the correlation of
minifers (e.g. Ammonia beccarii, A. tepida, Elphidium this unit with the Fabbriche Sands formation (Bar-
crispum, Hyalinea baltica, Nonion boueanum) and com- toletti et al. 1986; Boschian et al. 2006 and refer-
mon ostracods (Aurila cymbaeformis, A. lancaeformis, ences therein).
A. punctata and A. punticruciata gathered as Aurila
spp., Bosquetina dentata, Cytheridea neapolitana, K. com- Unit 5 - This unit comprises well rounded
pressa, Loxoconcha ovulata, Muellerina problematica, Neo- polygenic gravels with a grey sandy or silty matrix,
cytherideis fasciata, P. subrugosa, P. turbida and Pterygocy- passing upward and laterally into grey sands or greyNeogene and Quaternary of the Livorno area (Tuscany, Central Italy) 735
Fig. 7 - Stratigraphic log of the Bandi-
tella borehole with the range
chart of selected calcareous
nannofossils. For symbols
see legend in figure 5.
silty clays. In the upper portion of the unit there are This unit was documented in the Magri-
dark organic clays locally passing to a peat layer. gnano-S22, Ardenza-S1, Salviano-S9, Via Roma,
This unit was recorded in the Picchianti-S1 Picchianti-S1, Via Filzi-S1 and Torre Marzocco-S1
and Via Filzi-S1 boreholes, where its maximum boreholes (Figs. 6, 8, 9, 11, 14, 15 and 19).
thickness is of about 10 m (Figs. 14-15). Its maximum thickness is of about 4 m.
In this unit it is present a microfauna repre- On the whole, the unit is represented by li-
sented by ostracods (Candona neglecta, Ilyocypris gibba thologies unsuitable for micropaleontological anal-
and Cyprideis torosa), and a macrofauna represented yses (Dall’Antonia et al. 2004); however, we were
by mollusks (Galba truncatula, Anisus spirorbis, Gyrau- able to prepare few samples from not cemented li-
lus crista, Valvata cristata and Bithynia). thologies that contain a fauna rich in ostracods, rep-
Fauna and lithological characters, found in resented by Aurila spp., Loxoconcha elliptica, N. fascia-
the sandy sediments of this unit (Picchianti-S 1 ta, N. subspiralis, P. subrugosa, Po. turbida, Semicytherura
borehole, Fig. 14), allow us to infer an estuarine incongruens and S. rarecostata, and foraminifers, which
system that moves towards a continental environ- are mostly represented by A. beccarii, E. crispum and
ment. In the Via Filzi borehole (Fig. 15), this unit is L. lobatula. In the calcarenitic layers present in in the
represented by sandy gravel sediments, with a fin- subsurface of the harbour area (Torre Marzocco-S1,
ing-upward sequence, that are interpreted as fluvial Fig. 19), marine mollusks (e.g. Vermetus and Lithodo-
deposits passing to freshwater lake deposits (Fig. 4). mus holes) were also found. These assemblages are
On the basis of lithological and micro-mac- typical of littoral environment (Fig. 4).
rofaunistical similarities, this unit may correspond The occurrence of P. turbida and S. incongru-
to the middle-late Pleistocene Corea formation of ens allows the attribution of the unit to a generic
Zanchetta et al. (2006), dated to MIS6 and its transi- Quaternary. However, thanks to the presence of
tion to MIS5 (Fig. 22). the characteristic calcarenitic layers, this unit may be
linked to the “Panchina I” (corresponding to the
Unit 6 - It consists of calcarenitic layers, grey “Calcareniti di Castiglioncello” of Mazzanti 2016),
and orange sands, and locally clayey silts levels. that was attributed to the middle-late Pleistocene736 Catanzariti R. & Da Prato S.
Fig. 8 - Stratigraphic log of the Ardenza-S1 borehole with the range chart of selected calcareous nannofossils and microfossils (benthic fora-
minifers and ostracods). For symbols see legend in figure 5.
Fig. 9 - Stratigraphic log of the Salviano-S9 borehole with the range chart of selected calcareous nannofossils and microfossils (benthic fora-
minifers and ostracods). For symbols see legend in figure 5.
MIS5e (Fig. 22; Zanchetta et al. 2004; Zanchetta et ed to the fluvial activity of the late Pleistocene in
al. 2006 and references therein). the surrounding area (e.g. Ardenza and Cignolo
For what regards the calcarenitic layer that streams), which are related to the MIS5d (Fig. 22),
occurs in the Magrignano-S22 borehole (Fig. 6), its because of their stratigraphic position on top of
altitude above sea level, which now results to be at the “Panchina I” (Ciampalini et al. 2006; Bossio et
about 20 m, and its stratigraphic position, led some al. 2008).
authors to correlate these deposits with the Villa
Padula Calcarenite formation (dated to MIS 7 or Unit 8 - This unit includes well rounded sands
MIS9c hightstand by Bossio et al. 2008). and reddish silts and silty sands, with millimetric
nodules of Fe-Mn. Silts and sands are barren of
Unit 7 - This unit comprises alternating layers fossils and locally appear pedogenized. It was doc-
of silts, sands and gravels. It was documented in umented in the Via Garibaldi-S2, Picchianti-S1 and
the Banditella, Ardenza-S1, Salviano-S9, Via Roma Via Filzi-S1 boreholes (Figs. 12, 14 and 15) and in
and Via Pompilia-S3 boreholes (Figs. 7-9, 11 and the Scasso outcrop (Fig. 10). Its maximum thick-
16). Its maximum thickness is of about 3 m. ness is of about 5 m.
It is barren of fossils. This unit may corre- Lithologies are barren of fossils and inter-
spond to the late Pleistocene Rio Maggiore Con- preted as eolian and fluvial deposits.
glomerates and to all those fluvial deposits relat- Stratigraphic and lithological considerations,Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 737
Fig. 10 - Stratigraphic log of the Scasso outcrop with the range chart of selected calcareous nannofossils and microfossils (foraminifers and
ostracods). For symbols see legend in figure 5.
Fig. 11 - Stratigraphic log of the Via Roma borehole with the range chart of selected calcareous nannofossils and microfossils (benthic fora-
minifers and ostracods) taxa. For symbols see legend in figure 5.
mostly based on the characteristic presence of mil- Unit 9 - This unit includes sandy silts and
limetric nodule of Fe-Mn, for intense pedogenesis, silty-clayey sands. It was documented in the Calata
allow the correlation of the unit with the Ardenza Magnale-S7, Darsena-SA and Paduletta boreholes
Sands (Ciampalini et al. 2006; Bossio et al. 2008) (Figs. 18, 20 and 21). Its maximum thickness is of
and the Donoratico Sands (see Boschian et al. about 22 m.
2006), and its attribution to the late Pleistocene. The ostracofauna analysed in the Darsena-SA
Ciampalini & Sammartino (2007), on the presence borehole, consists of Candona neglecta and Ilyocypris
of Mousterian tools (Middle Paleolithic), linked gibba with very rare benthic foraminifera specimens
the Ardenza Sands to the late Pleistocene MIS4 to reworked. This micropaleontological assemblage
MIS3 isotopic stages (Fig. 22), which embrace great indicates a freshwater or oligohaline continental pa-
part of the Wurm glacial stage. Due to this correla- laeoenvironment (Fig. 4, Tab. 2). The macrofauna
tion we could infer a similar age for Unit 8. are mostly represented by fresh water mollusks (e.g.738 Catanzariti R. & Da Prato S.
Fig. 12 - Stratigraphic log of the Via Garibaldi-S2 borehole with the range chart of selected calcareous nannofossils and microfossils (benthic
foraminifers and ostracods) taxa. For symbols see legend in figure 5.
Fig. 13 - Stratigraphic log of the Viale Carducci borehole with the range chart of selected calcareous nannofossils and microfossils (benthic
foraminifers and ostracods) taxa. For symbols see legend in figure 5.
Ancylus, Bithynia and Pisidium) and land snails mol- very well with those of other continental depos-
lusks (e.g. Carychium, Punctum and Vallonia). its reported in literature (Federici 1993; Antonioli
The litholocical and faunal features, match et al. 2000; Dall’Antonia et al. 2004). StratigraphicNeogene and Quaternary of the Livorno area (Tuscany, Central Italy) 739
Fig. 14 - Stratigraphic log of the Picchianti-S1 borehole with the range chart of selected calcareous nannofossils and microfossils (ostracods)
taxa (modified from Ciampalini et al. 2013). For symbols see legend in figure 5.
Fig. 15 - Stratigraphic log of the Via Filzi-S1 borehole with the range chart of selected calcareous nannofossils taxa. For symbols see legend
in figure 5.
considerations and correlation with near boreholes Unit 10 - This unit consists of fine to coarse
suggest a late Pleistocene age, probably linked with sands, alternating silts and sands, locally with met-
MIS2 (Dall’Antonia et al. 2004). ric levels of Posidonia oceanica. It was detected in the740 Catanzariti R. & Da Prato S.
Fig. 16 - Stratigraphic log of the Via Pompilia-S3 borehole with the range chart of selected calcareous nannofossils and microfossils (benthic
foraminifers and ostracods) taxa. For symbols see legend in figure 5.
Fig. 17 - Stratigraphic log of the Porto Mediceo-S3 borehole with the range chart of selected calcareous nannofossils and microfossils (benthic
foraminifers and ostracods) taxa. For symbols see legend in figure 5.
Porto Mediceo-S3, Calata Magnale-S7, Torre Mar- MNN21a-MNN21b zones.
zocco-S1, Darsena-SA, and Paduletta boreholes The ostracodfauna are mostly represented
(Figs. 17-21). Its maximum thickness is of about 15 by Aurila spp., Loxoconcha spp., Xestoleberis spp. The
m. main represented foraminifers are A. beccarii, N.
Few samples, containing scarce calcareous boueanum, E. crispum, Quinqueloculina spp., Haynesina
nannofossils represented by E. huxleyi with “small depressula and Triloculina sp. Marine molluska (e.g.
Gephyrocapsa” and “medium Gephyrocapsa”, permit Chlamys, Venus, Nucula and Tellina) also occur. These
us to refer the unit to an interval of time corre- fossil assemblages characterise the proximal inner
sponding to the middle-late Pleistocene-Holocene neritic zone (Fig. 4).Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 741
Fig. 18 - Stratigraphic log of the Calata Magnale-S7 borehole with the range chart of selected calcareous nannofossils and microfossils (benthic
foraminifers and ostracods) taxa. For symbols see legend in figure 5.
Fig. 19 - Stratigraphic log of the Torre Marzocco-S1 borehole with the range chart of selected calcareous nannofossils and microfossils
(benthic foraminifers and ostracods) taxa. For symbols see legend in figure 5.
The palaeoenvironment, the lithologies and al. 2004), which brought the sea to the present-
the richness of Posidonia oceanica remains, allow us day level, starting from the end of the last glacial
to relate the Unit 10 to the Holocene sediments maximum (transition from MIS2 to MIS1, Fig.
of the Versilian transgression (Dall’Antonia et 22).742 Catanzariti R. & Da Prato S.
Fig. 20 - Stratigraphic log of the Darsena-SA borehole with the range chart of selected calcareous nannofossils and microfossils (benthic
foraminifers and ostracods) taxa. For symbols see legend in figure 5.
Discussion and conclusion The transition to the overlying Pliocene sedi-
ments was not documented, but only supposed to
The different units were characterised through have occurred in the area between Magrignano-S22
lithofacies analysis, taking into account lithology, and Salviano-S9 boreholes, on the basis of the re-
micropalentological and macropaleontological con- constructed cross-sections (Section 1, Fig. 23).
tent. In addition, where it was possible, they were Marine deposits confined into Unit 2, and re-
biostratigraphically constrained. Furthermore, on ferable to the early Pliocene MNN13 and MNN14-
the basis of their lithologies and faunal and floral 15 zones and the early Pleistocene MNN18 Zone,
contents they were correlated to lithostratigraphic occur from South to North in an inner belt with
units described in literature and outcropping in the semicircular pattern (Sections 1-3, Fig. 23). These
surrounding area. So, we can tell a reliable palaeoen- deposits are characterised by microfaunal assem-
vironmental story of this area spanning the late blages that testify palaeoenvironments referable
Messinian to Holocene time interval (Tab. 2). For to the inner and outer neritic zones. The accepted
the subsurface stratigraphic study of the Livorno stratigraphic model for the Tuscan area, argues that
area, a data set of continuous logs of cores derived during the Gelasian and early Calabrian time inter-
from the IGG-DATABASE was also used (location val (corresponding to zones MNN18-MNN19a)
in Fig. 1). On the basis of these data, we performed there was no marine sedimentation (Bossio et al.
four schematic geological cross-sections, which de- 1986; 1993). On the contrary, our data extend the
pict the stratigraphic architecture (Fig. 23). presence of the Pliocene marine cycle to the early
The continental deposits of Unit 1, were Pleistocene (Gelasian MNN18), and allow us to ex-
found exclusively in the south-eastern area of clude that the Livorno area took part in the general
Livorno (Section 1, Fig 23). Micropaleontological epirogenic uplift that interested the rest of Tuscany,
content and lithologies show that an endoreic ba- during the late Pliocene-early Pleistocene time span.
sin, with oligo-mesohaline waters, developed during In addition, unpublished calcareous nannofossil
the late Messinian, as it occurred in other areas of data, collected from boreholes drilled in the Tus-
the Mediterranean (Caruso et al. 2020 and reference cany coastal area (offshore and inland), referable to
therein). zones MNN16a, MNN16b-MNN17 and MNN18Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 743
Fig. 21 - Stratigraphic log of the
Paduletta borehole with the
range chart of selected cal-
careous nannofossils taxa.
For symbols see legend in
figure 5.
(IGG-Database), allow us to recognise a continuous the Messinian Unit 1 (section 1, Fig. 23), probably
marine sedimentation during the Pliocene to early due to a tectonic lowering. During MNN19d, the
Pleistocene time interval. sea reached the outer zones of the area (sections 2
Data collected so far do not record sediments and 3, Fig. 23) expressing depths that characterised
referable to the uppermost Gelasian-lowermost Ca- a distal inner neritic zone. Furthermore, in the up-
labrian MNN19a Zone, confirming emersion dur- per part of the Viale Carducci borehole (Fig. 13), we
ing this time interval as reported in literature for the can observe the regressive trend of the marine cycle
western side of the Northern Apennines (e.g. Bos- dating to MNN19d Zone, testified by the transition
sio et al. 1998) and our study did not even record the from distal to proximal neritic zone. As a whole,
lower Calabrian MNN19c Zone, probably because Unit 3 seems to reach a greater depth from E-SE to
this zone represents a very narrow interval of time W-NW (Fig. 23).
(Fig. 3). Instead, we recognised marine sediments Sediments referable to the Calabrian (Sicil-
in Unit 3, which were dated to the Calabrian (San- ian) MN19e Zone, which constitute Unit 4, were
ternian p.p. to Emilian) MNN19b and MNN19d detected exclusively around the Livorno harbour
zones. Microfauna found in sediments related to zone and in the corresponding inner part (Fig. 23).
zones MNN19b show a transgressive trend. In fact, The microfauna observed allows the recognition of
during Zone MNN19b, the sea level reached the in- evident bathymetric variations and consequently of
ner parts of the Livorno area overlying deposits of the transgressive phase that marks the beginning744 Catanzariti R. & Da Prato S.
neritic. In addition, overall, the thickness of the
deeper bathymetric levels, represented by offshore
proximal deposits, and referable to the distal inner
neritic zone, have different thicknesses in different
boreholes. For example, in the Calata Magnale-S7
borehole (Fig. 18), these deposits have a thickness
of more than 20 m, while in the Via Pompilia-S3
borehole (Fig. 16) they are reduced to a few me-
ters. This could be explained with the presence of
a particularly articulate Pleistocene sedimentary ba-
sin, whose origin should be investigated, but that
could be related to tectonic dynamics. Sediments at-
tributed to the Sicilian are very rare in Tuscany and
limited to small outcrops and very few boreholes
(Bartoletti et al. 1986; Dall’Antonia et al. 2004).
So, our paper confirms the presence of these sedi-
ments in the Livorno subsurface and shows an area
of distribution wider than that reported in literature
(Boschian et al. 2006). In addition, the micropaleon-
tological analyses allowed us to identify sedimentary
environments deeper than those known for the Si-
cilian succession (Bartoletti et al. 1986; Boschian et
al. 2006).
Our data do not record the late Calabrian
(Sicilian)-Chibanian MNN19f-MNN20 zones. Ac-
tually, there are not marine sediments related to this
interval of time that is only testified by the patchy
occurrence of the coastal deposits of Villa Battaglia
Conglomerates or Villa Umberto I Conglomerates
(Boschian et al. 2006; Zanchetta et al. 2006; Zanchet-
ta et al. 2019). The unrecorded Sicilian-Chibanian
sediments lead us to suppose that the coastal plain
could have been exposed to erosion by tectonic up-
lift, since the warmer conditions characterising at
least the MNN20 Zone (MIS11 and MIS13, Fig. 22)
would require sea-level high stand.
The first marine sediments overlaying the Si-
Fig. 22 - Livorno area subsurface units, plotted against the calcareous cilian sediments are transgressive deposits referable
nannofossil biostratigraphy and the δ18O stack of Lisiecki & to Unit 6 (Fig. 23), which are datable to the late Pleis-
Raymo (2005), with sea-level and temperatures estimates for tocene MIS5e. The subsequent sediments of units 7
the Pleistocene. In grey the undocumented interval of time.
to 9, testify transitional and continental conditions
during the late Pleistocene MIS5d, MIS4 and MIS3,
of the second Calabrian marine transgressive-re- linked to glacio-eustatic control.
gressive cycle, cited in the literature (Dall’Antonia Holocene lagoonal and marine sediments of
et al. 2004). Actually, in the Via Pompilia-S3, Porto Unit 10 are found in the northern and western part
Mediceo-S3, Marzocco-S1 boreholes (Figs. 16, 17 of the study area (section 2, Fig. 23). This unit, in
and 19), from the bottom to the top of the strati- the Darsena-SA borehole (Fig. 20), shows a com-
graphic successions, it is possible to distinguish en- plete depositional sequence with a progressive pas-
vironments that move from proximal inner neritic sage from transitional to marine environment that
to distal inner neritic and return to proximal inner testifies the Versilian transgression (Federici 1993),Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 745
Fig. 23 - Straight-line stratigraphic
cross sections showing stra-
tigraphic correlations among
selected boreholes and
outcrops. The different units
can be visualized. Location
of boreholes (red points and
numbers) and sections are
reported in Fig. 1.
occurred during MIS2 to MIS1 transition. Magrignano-S22 borehole (Fig. 6) because of the
For what concerns the marine terraces (Fig. presence of the early Calabrian (Santernian) MN-
2), their different altitude above sea level and dif- N19b Zone in the underlying sediments.
ferent age indicate a general uplift of the area from The highest terrace order, named Terrazzo
the Quaternary (Zanchetta et al. 2019). The Livor- della Fattoria Pianacce, which was related to the
no Terrace is placed at an altitude of about 20 m middle Pleistocene MIS11 (Zanchetta et al. 2006),
a.s.l. and related to the Eutyrrhenian transgression is constituted by a tilted surface ranging from about
(MIS5e, Federici & Mazzanti 1995; Hearty et al. 120 m to 20 m a.s.l. (Zanchetta et al. 2019).
1986; Mauz 1999; Nisi et al. 2003).
The second order of marine terraces (Villa Acknowledgments: We are very grateful to Alessandro
Ciampalini for helpful suggestions on determination of mollusks and
Padula and Salviano Terraces) is placed at an alti- for critical reading of the paper. We thank Alessandro Ellero (Istituto
tude of about 40 m a.s.l. and was related to middle di Geoscienze e Georisorse-CNR) for constructive advises. We are
Pleistocene MIS7- 9(?) (Zanchetta et al. 2019). grateful to Ilaria Lotti and Enrico Pribaz (Autorità di Sistema Portuale
The Salviano Terrace, which was doubtfully del Mar Tirreno Settentrionale) for kindly making available some
cores and respective stratigraphic logs. We are also thankful to two
attributed to the middle Pleistocene by Bossio et anonymous reviewers for the constructive suggestions that greatly
al. (2008), in our paper is better constrained in the improved the paper.746 Catanzariti R. & Da Prato S.
APPENDIX A Loxoconcha elliptica Brady, 1868
Taxonomic Appendix Loxoconcha muelleri (Mehes, 1908)
Loxoconcha ovulata (Costa, 1853)
CALCAREOUS NANNOFOSSILS Loxocorniculina djafarovi (Schneider, 1956)
Amaurolithus delicatus Gartner and Bukry, 1975 Macrocypris adriatica (Breman, 1975)
Calcidiscus macintyrei (Bukry and Bramlette, 1969) Loeblich and Tap- Muellerina problematica (Seguenza, 1884)
pan, 1978 Neocytherideis fasciata (Brady & Robertson, 1874)
Calcidiscus leptoporus (Murray & Blackman 1898) Loeblich & Tappan, Neocytherideis subspiralis (Brady, Crosskey & Robertson, 1874)
1978 Palmoconcha subrugosa (Ruggieri, 1977)
Discoaster asymmetricus Gartner, 1969 Palmoconcha turbida (Müller, 1894)
Discoaster brouweri Tan, 1927, emend. Bramlette and Riedel, 1954 Parakrithe cf. P. cristallina (Reuss, 1850)
Discoaster pentaradiatus Tan, 1927 Parakrithe cf. P. dimorpha Bonaduce, Ciampo & Masoli, 1976
Discoaster surculus Martini and Bramlette, 1963 Parakrithe rotundata Aiello, Barra, abate & Bonaduce 1993
Discoaster tamalis Kamptner, 1967 Pontocythere turbida (Müller, 1894)
Discoaster variabilis Martini and Bramlette, 1963 Pterygocythereis jonesi (Baird, 1850)
Emiliania huxleyi (Lohmann 1902) Hay & Mohler, in Hay et al. 1967 Sagmatocythere versicolor (Müller, 1894)
Gephyrocapsa Kamptner, 1943 Semicytherura incongruens (Müller, 1894)
Helicosphaera carteri (Wallich 1877) Kamptner, 1954 Semicytherura rarecostata Bonaduce, Ciampo & Masoli, 1976
Helicosphaera sellii (Bukry and Bramlette, 1969) Jafar and Martini, Tyrrenocythere pontica (Livental, 1961)
1975 Urocythereis gr. U. margaritifera (Müller, 1894)
Pontosphaera Lohmann, 1902 Xestoleberis communis Müller, 1894
Pseudoemiliania lacunosa Kamptner, 1963 ex Gartner, 1969
Rhabdosphaera Haeckel, 1894 FORAMINEFERS
Reticulofenestra Hay, Mohler & Wade, 1966 Ammonia beccarii (Linnaeus, 1758)
Reticulofenestra pseudoumbilicus (Gartner, 1967) Gartner, 1969 Ammonia parkinsoniana (d’Orbigny, 1839)
Sphenolithus abies Deflandre in Deflandre and Fert, 1954 Ammonia tepida (Cushman, 1926)
Umbilicosphaera sibogae (Weber - van Bosse 1901) Gaarder, 1970 Bolivina aenariensis Costa, 1856
Bolivina catanensis Seguenza, 1862
CALCAREOUS DINOFLAGELLATE Brizalina alata (Seguenza, 1862)
Thoracosphaera Kamptner, 1927 Bulimina cf. B. minima Tedeschi & Zanmatti, 1957
Bulimina marginata d’Orbigny, 1826
OSTRACODS Cassidulina neocarinata Thalmann, 1950
Amnicythere accicularia (Olteanu) Cibicidoides cf. C. kullembergi (Parker, 1958)
Argilloecia cf. A. robusta Bonaduce, Ciampo & Masoli, 1976 Cibicidoides pseudoungeriana (Cushman, 1922)
Aurila convexa (Baird, 1850) Dorothia gibbosa (d’Orbigny, 1826)
Aurila cymbaeformis (Seguenza, 1883) Elphidium crispum (Linnaeus, 1758)
Aurila lanceaeformis Uliczny, 1969 Eponides repandus (Fichtel & Moll, 1798)
Aurila punctata (Muenster, 1830) Fursenkoina complanata (Egger, 1893)
Aurila punticruciata Ruggieri, 1975 Globigerina bulloides d’Orbigny, 1826
Bosquetina carinella (Reuss, 1850) Globigerinoides sacculifer (Brady, 1877)
Bythocypris obtusata producta (Seguenza, 1880) Globobulimina affinis (d’Orbigny, 1839)
Callistocythere pallida (Mueller, 1894) Globorotalia bononiensis Dondi, 1963
Candona neglecta Sars, 1887 Globorotalia aemiliana Colalongo & Sartoni, 1967
Carinocythereis bairdi Uliczny, 1969 Gyroidina soldanii d’Orbigny, 1826
Cyprideis torosa (Jones, 1850) Haynesina depressula (Walker & Jacob, 1798)
Cytherella russoi Sissingh, 1972 Heterolepa cf. H. dertonensis (Ruscelli, 1954)
Cytheretta subradiosa (Roemer, 1838) Hyalinea baltica (Schroeter, 1783)
Cytheridea neapolitana Kollmann, 1960 Lenticulina cultrata Montfort, 1808)
Cytheropteron cf. C. alatum Sars, 1866 Lobatula lobatula (Walker & Jacob, 1798)
Cytheropteron ruggierii Pucci, 1956 Melonis pompilioides (Fichtel & Moll, 1798)
Cytheropteron testudo Sars, 1869 Nonion boueanum (d’Orbigny, 1846)
Cytheropteron vespertilio (Reuss, 1850) Orbulina universa d’Orbigny, 1839
Euxinocythere praebaquana (Livental, 1956) Planulina ariminensis d’Orbigny, 1826
Henryhowella asperrima (Reuss, 1850) Pullenia bulloides (d’Orbigny, 1846)
Ilyocypris gibba (Ramdohr, 1808) Quinqueloculina seminula (Linnaeus, 1758)
Krithe compressa (Seguenza, 1880) Sigmoilopsis coelata Costa, 1855
Leptocythere bacescoi (Rome, 1942) Sigmoilopsis schlumbergeri (Silvestri, 1904)
Leptocythere castanea (Sars, 1866) Siphonina reticulata (Cžjžek, 1848)
Leptocythere multipunctata (Seguenza, 1883) Textularia sagittula Defrance, 1824
Leptocythere ramosa (Rome, 1942) Uvigerina rutila Cushman and Todd, 1941
Loxoconcha rhomboidea (Fischer, 1855) Valvulineria bradyana (Fornasini, 1900)Neogene and Quaternary of the Livorno area (Tuscany, Central Italy) 747
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