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New report of Ranina propinqua RistoRi, 1891 (Brachyura, Raninidae)
from central Italy
Federico Famiani, Angela Baldanza, Roberto Bizzarri, Antonio De Angeli, Alessandro Garassino,
and Giovanni Pasini
With 4 figures
Abstract: A new specimen of Ranina propinqua RistoRi, 1891 from the Early Pleistocene (Gela-
sian–Calabrian) of Orzalume-Cottano section (Orvieto, Umbria, central Italy) is reported. The study
of this complete specimen results in a detailed diagnosis for the species not reported in the original
description by RistoRi. Although the ecology and behaviour of Raninidae display a broad spectrum
of bathymetric and sedimentological ranges, the sedimentological and palaeoecological data for the
study specimens suggest that R. propinqua could be associated to relatively shallow, coastal marine
environments, at least during the last 2 Ma.
Key words: Crustacea, Decapoda, Raninidae, Early Pleistocene, Umbria, Italy.
1. Introduction
The occurrence of crustaceans in the fossil record
from Umbria (central Italy) was often considered very
poor, and limited to the reports by RistoRi during the
19th century. Recent discoveries, collections, and sub-
sequent publications (Pasini & GaRassino 2010; Bal-
danza et al. 2014) expanded our knowledge about the
presence of crustaceans in the Gelasian–Calabrian de-
posits across the Tuscany-Umbria regional boundary.
Herein, we provide an update on the sedimentologi-
cal and geological data on the fossiliferous localities
preserving remains and whole specimens of Ranina
propinqua RistoRi, 1891 from western Umbria (South
Valdichiana Basin). A well-preserved female speci-
men of R. propinqua has been recently found in the
Early Pleistocene sandy deposits, cropping out be-
tween the localities of Orzalume and Cottano, near
Orvieto (Umbria). This specimen allows re-examining
the original description of RistoRi, supplementing the
missing diagnosis for this species.
2. Geological overview of fossil sites
The studied area (Fig. 1) is situated at the Tuscany-
Umbria regional boundary (central Italy) and pertains
to the South Valdichiana extensional basin, enclosed
by the Meso-Cenozoic reliefs of Rapolano-Mt. Ceto-
na Ridge (westward) and of Narnese-Amerina Ridge
(eastward) (JacoBacci et al. 1970; Funiciello et al.
1981). The basin formed in the Late Miocene to Early
Pliocene, and was subsequently filled by proximal ma-
rine to coastal marine deposits of Piacenzian to Cala-
brian age. Most deposits, including all of those with
crustacean records, belong to the Early Pleistocene
“Chiani-Tevere” depositional cycle (Gelasian–Ca-
labrian: amBRosetti et al. 1987; GiRotti & mancini
2003; mancini et al. 2004; Baldanza et al. 2011, 2013,
2014; monaco et al. 2011). The main part of deposits
is linked to the evolution of a wave-dominated coast,
where spotted and roughly organized streams build
small fan deltas, except in the area between Città della
Pieve and Chiusi (Fig. 1) that was interpreted as a wide
©2015 E. Schweizerbart’sche Verlagsbuchhandlung, Stuttgart, Germany www.schweizerbart.de
DOI: 10.1127/njgpa/2015/0469 0077-7749/2015/0469 $ 2.50
N. Jb. Geol. Paläont. Abh. 275/3 (2015), 337–346 Article
Stuttgart, March 2015
E
eschweizerbart_xxx
338 F. Famiani et al.
deltaic system (VeRRi 1918; meRla 1944; amBRosetti
et al. 1977; BizzaRRi & Baldanza 2009; Baldanza et
al. 2011, 2013; monaco et al. 2011). Three sections
within the South Valdichiana Basin (Fig. 1) recently
return well-preserved specimens of Ranina, associat-
ed or not with other species of decapods, and are here
briefly described in their sedimentological features
and biostratigraphic constrains.
Fig. 1. Simplified geological scheme for the study area (modified after Baldanza et al. 2014). The location of the three fos-
siliferous localities described in the text is also reported.
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New report of Ranina propinqua RistoRi, 18 91 339
2.1. The Orzalume-Cottano section
About 10 km east from Orvieto, in the Orzalume-
Cottano area, a composite sedimentological and strati-
graphic section was described between 290 m and 390
m a.s.l. (Fig. 2; monaco et al. 2011). The section con-
sists of sandy gravel deposits at the base that grade
upwards to sands at the top. These deposits represent a
transgressive-regressive trend of a shallow coastal ma-
rine environment with small river supply (monaco et
al. 2011). The lowermost 35 m thick deposits directly
overlay Oligocene to Miocene sandstones (Macigno
s.l. auctorum) and have been interpreted as roughly
organized fan delta deposits (monaco et al. 2011). De-
posits of the intermediate section are represented by
fine to very fine sands and silty sands, locally weakly
cemented. These deposits were referred to a lower
shoreface environment, locally passing to the transi-
tion to offshore (monaco et al. 2011). The uppermost
section is characterized by massive to cross-laminated,
medium to coarse bioclastic sands. An upper shoreface
environment is inferred (monaco et al. 2011).
The new R. propinqua specimen collected from
this locality comes from deposits of the intermedi-
ate section; deposits considered herein are about 20
m thick, irregularly cemented sandy beds, with oli-
gotypic fossil horizons (Fig. 2). Irregularly cemented
beds occur in three main superimposed horizons: the
lowermost one, which contains the study specimen as
well as minor crab fragments (F. Famiani, pers. ob-
serv.), is characterized by Thalassinoides ichnofacies.
Locally, cementation is associated to the occurrence of
large Panopaea faujasi in life position. In the interme-
diate horizon, cementation occurs in association with
remains of trunks, pervasively drilled by Teredolites
and surrounded by a rich malacofauna (monaco et al.
2011). The uppermost cemented horizon is character-
ized by Cladocora caespitosa colonies in life position;
the largest one about 30 cm in diameter.
2.2. The San Lazzaro quarry section
The 27 m thick San Lazzaro quarry section (Fig. 1)
consists of fossiliferous and bioturbated fine sand,
silt and clay deposits (Fig. 2; Baldanza et al. 2014).
The deposits grade up from poorly sorted silty sand to
moderately sorted fine sand. Shell lags, bioturbation,
and cemented beds (arenite and/or siltite) are irregu-
larly interposed. In some cemented horizons Thalassi-
noides ichnofacies occurs. Fossil molluscs occur as
bioclastic lags, more or less concentrated or dispersed
within the sediment; well-preserved specimens are
often found in life position. Bivalves and gastropods
prevail, in addition to fragments of echinoids, rare
solitary corals, and benthic foraminifera. The decapod
crustacean assemblage, including one Ranina speci-
men, comes from the lowermost silty deposit (Fig. 2;
Baldanza et al. 2014). Decapods are present through-
out the section, documented by Thalassinoides ichno-
facies and by poorly preserved undeterminable crusta-
cean remains; among these, just one dactylus assigned
to Calappa cf. C. granulata (linnaeus, 1758) has been
previously reported by Baldanza et al. (2014: 268).
2.3. The Madonna degli Angeli site (Città della
Pieve)
The deposits are described beside a secondary road, in
the same area reported by RistoRi (1891) in his original
work of R. propinqua. The area is still accessible and
characterized by prevailing sandy deposits (Fig. 3A,
B), but unfortunately the lack of data do not allow to
identify the original RistoRi’s outcrop, either if or how
much the area was modified through the last hundred
years. At the moment we lack of a methodical investi-
gation on decapods’ occurrence, and the recent inspec-
tions of the site no longer provide decapods, although
the occurrence of undeterminable remains in washed
residues is common. Medium to coarse sand deposits
prevail, with subordinate silty sand, organized in up to
2 m thick tabular beds, gently dipping north-eastward
(Fig. 3A). Coarser deposits are usually normally grad-
ed, from coarse bioclastic and/or lithoclastic sand to
medium sand (Fig. 3D), or from medium to fine sand;
they also show an erosional base surface and a weak
horizontal to cross-lamination. Locally, symmet-
ric ripples are also visible. Finer deposits (fine sand
to silty sand) appear massive and bioturbated, with a
dominance of Thalassinoides ichnofacies (Fig. 3B, C).
Molluscs are frequent in shell horizons (mainly large
bivalves; Fig. 3B) as well as spotted in the sediment.
At least one coarse sand bed enriched in fragments of
echinoids occurs (Fig. 3E).
2.4. Stratigraphic constrains and palaeoenviron-
mental restoration
The integrate calcareous nannofossils and planktonic
foraminifera biostratigraphy allows us to place the
study sections in the Gelasian–Calabrian interval,
based upon the biostratigraphic scales by colalonGo
& saRtoni (1979), Rio et al. (1990), RaFFi (2002), and
iaccaRino & PRemoli silVa (2007). Decapods come
eschweizerbart_xxx
340 F. Famiani et al.
Fig. 2. Sedimentological and lithostratigraphic logs for the Orzalume-Cottano and the San Lazzaro quarry sections (re-
drawn and simplified after monaco et al. 2011 and Baldanza et al. 2014).
eschweizerbart_xxx
New report of Ranina propinqua RistoRi, 18 91 341
from Gelasian deposits (MNN 18-19a subzones, Glo-
borotalia inflata foraminiferal zone: Baldanza et al.
2014), in the San Lazzaro section, and from early Cal-
abrian deposits (MNN 19b-c subzones, G. inflata and
Globigerina cariacoensis foraminiferal zones: mo-
naco et al. 2011) in the Orzalume-Cottano site. The
exact provenance and age of the RistoRi’s specimen is,
however, more uncertain. As pointed out by Baldan-
za et al. (2014), sandy deposits in the Madonna degli
Angeli site, which are the most probable candidate for
the provenance of the holotype of R. propinqua, were
never investigated in detail in search for crabs, and no
additional specimens have been collected. Contrary
to the Pliocene age presumed by RistoRi, these sandy
Fig. 3. Deposits of the Madonna degli Angeli site, in the Città della Pieve area. A – General view of sandy sediments, show-
ing plane-parallel to slightly cross lamination. B – Massive fine sand/silt deposits, with occurrence of shell horizons (Sh)
and Thalassinoides bioturbation (Th). C – Detail of massive and locally cemented sand; Thalassinoides bioturbation (Th)
is still highlighted. D – Normally graded coarse to medium sand deposits. E – Detail of the horizon with echinoid spines
and fragments.
eschweizerbart_xxx
342 F. Famiani et al.
sediments are dated to the Gelasian–Calabrian inter-
val (MNN 18-19a subzones: BizzaRRi & Baldanza
20 09).
Based upon the sedimentological data and the ma-
lacological and micropalaeontological assemblages,
the three sections are referable to the same palaeoenvi-
ronmental context. A detailed description of the mala-
cofauna and the microfauna can be found in the previ-
ous works by BizzaRRi & Baldanza (20 09), monaco et
al. (2011), and Baldanza et al. (2014).
Throughout the study sections, at least within the
crab-bearing horizons, planktonic foraminifera are
absent or subordinate, and both the benthic foramini-
feral assemblages and the malacofauna attest for com-
parable palaeoenvironmental conditions of warm and
shallow water. Some sedimentological and palaeon-
tological features, such as the abundance of echinoid
plates and radioles, the occurrence of irregularly ce-
mented horizons mainly associated with Thalassinoi-
des ichnofacies, the presence of shell beds interpreted
as tempestites, and the common presence of warm-
water molluscs and foraminifera, are documented in
all of the study sections. The occurrence of bryozoans
(Cupuladriidae) has also been reported throughout the
Orzalume-Cottano and the S. Lazzaro sections (Rosso
et al. 2011; BizzaRRi et al. 2015).
Throughout the Orzalume-Cottano section, the
transition from a fan delta environment to a shoreface
environment is documented; the interval where the
Ranina specimen was found is identifiable with a 30-
40 m deep, storm-influenced lower shoreface/offshore
transition environment (monaco et al. 2011). In the S.
Lazzaro quarry section, the sedimentological features
suggest a fairly quiet depositional environment, occa-
sionally affected by waves, across the lower shoreface
and the transition to offshore. The occurrence of wood
and leaf fragments, resedimented during major storms,
or provided by river mouth supply, indicate proximity
to the coast. The occurrence of microborings on mol-
lusc shells (referable to Entobia, Gastrochaenolites,
Caulostrepsis and Meandropolydora; matteucci et
al. 2012), also indicate a nearshore environment. The
grain-size analyses and the datum of the malacofau-
na and the microfossil assemblages (Baldanza et al.
2014) lead to estimate an average depth between 18-20
and 45 m, with a reliable depth for crab interval of
about 30-40 m. These environments belong to a coast
fed by small and local river mouths, where sediments
are significantly redistributed across and alongshore
by waves (Baldanza et al. 2011, 2014; monaco et al.
2011). The sandy section of Madonna degli Angeli, as
well as the minor outcrops in the area quoted by Ris-
toRi (1891), are associated to the broad delta of Città
della Pieve (A3a facies association, Outer delta front
deposits – Sand bars: BizzaRRi & Baldanza 2009;
Baldanza et al. 2014). For this environment, shallower
depth, of about 10-20 m, is inferred (BizzaRRi & Bal-
danza 2009; Baldanza et al. 2014).
3. Material
One adult female raninid crab (MSNM i28012 – lcxp: 27
mm) three-dimensionally preserved inside a coarse sub-
nodular sandy concretion, from the Early Pleistocene (Gela-
sian–Calabrian) of Orzalume-Cottano section (Orvieto,
Umbria, central Italy). The studied specimen, assigned to R.
propinqua RistoRi (Raninidae de Haan, 1839), is housed in
the palaeontological collection of the Museo di Storia Natu-
rale di Milano (MSNM).
Abbreviations: lcxp: carapace length; MPUR: Museo Pa-
leontologico Università “La Sapienza”, Roma; MSNM:
Museo di Storia Naturale, Milano; MUSNAF: Museo di
Storia Naturale dell’Accademia dei Fisiocritici, Siena.
4. Systematic palaeontology
Infraorder Brachyura latReille, 1802
Section Podotremata Guinot, 1977
Subsection Raninoidia de Haan, 1839
Superfamily Raninoidea de Haan, 1839
Family Raninidae de Haan, 1839
Subfamily Ranininae de Haan, 1839
Genus Ranina lamaRck, 1801
Type species: Cancer raninus linnaeus, 1758; subsequent
designation by latReille (1810).
Fossil species included: See kaRasawa et al. (2014).
Ranina propinqua RistoRi, 1891
Fig. 4 A-D
*1891 Ranina propinqua RistoRi, pp. 11-14, pl. 3, figs. 4-7
(illustrated as mirrored).
1898 Ranina propinqua. – Lőrenthey, p. 137.
1910 Ranina propinqua. – FaBiani, p. 93.
1929 Ranina propinqua. – GlaessneR, p. 363.
2006 Ranina propinqua. – De anGeli & GaR assino, p. 38.
2006 Ranina propinqua. – mann i, p. 108, fig. 38.
2009 Ranina propinqua. – de anGeli et al., pp. 120-121.
2010 Ranina propinqua. – scHweitzeR et al., p. 74.
2010 Ranina propinqua. – Pasini & GaRassino, p. 116.
2011 Ranina propinqua. – de anGeli & BescHin, p. 13.
eschweizerbart_xxx
New report of Ranina propinqua RistoRi, 18 91 343
Fig. 4. A – Ranina propinqua RistoRi, 1891, MPUR i.543, holotype, dorsal view. B – R. propinqua, MUSNAF 7075, dorsal
view. C – R. propinqua, MSNM i28012, dorsal view, part. D – R. propinqua, MSNM i28012, dorsal view of counter-part.
Scale bar equals 10 mm.
eschweizerbart_xxx
344 F. Famiani et al.
2014 Ranina propinqua. – Pasini, GaRassino & de an-
Geli in Baldanza et al., p. 274, 276, Fig. 6A-E.
2014 Ranina propinqua. – GaRassino, Pasini, de anGeli
& hyžný, p. 122, Fig. 1F.
Diagnosis: Based upon the specimens of R. propinqua
known to date (holotype MPUR i.543, and two additional
specimens, MUSNAF 7075 and MSNM i28012), a diagno-
sis is provided: Carapace large, wide, broadened anteriorly
with wide teeth; dorsal surface with big spiny tubercles
uniformly arranged; pointed rostrum with parallel margins
converging distally, forming a single apex; rostrum slightly
ridged medially; anterolateral margin armed immediately
behind extraorbital tooth with two wide teeth, the first bi-
fid and the second one trifid; posterolateral margin smooth,
rimmed; orbitofrontal margin wide, with three teeth in-
dented by two fissures; orbits directed anteriorly, relatively
wide; chelipeds strong, isochelous, homodontous; propodus
large, flattened; upper margin armed with two spiny strong
median and distal teeth; lower margin armed with a row
of small spines; dactylus curved, flattened; upper margin
armed with a row of spiny teeth; serrate occlusal margin;
index short with triangular teeth on occlusal margin.
Discussion: RistoRi (1891) described R. propinqua based on
a sole well-preserved female specimen from the “Pliocene”
of Città della Pieve (Perugia, Umbria) (Fig. 4A). The author
did not provide a detailed diagnosis, limiting the description
to some observations related to the carapace ornamentation
and to the general shape and ornamentation of the chelae
(RistoRi 1891: 12-13). This and its presumed geological age,
justified the description of the new fossil species, which
was assigned to the Pliocene yellow sands in general terms
(RistoRi 1891: 11). The area reported by RistoRi in his origi-
nal work is still accessible and characterized by prevailing
sandy deposits. According to BizzaRRi & Baldanza (2009)
the type deposits of Città della Pieve are now referred to the
Gelasian–Calabrian interval (Early Pleistocene). Recently
Pasini, GaRassino & de anGeli in Baldanza et al. (2014)
studied the holotype and one additional specimen from the
San Lazzaro Section (Fabro Scalo, Terni, Umbria) (Fig. 4B),
updating the morphological description of R. propinqua
now assigned to the Early Pleistocene, based upon updated
sedimentological and stratigraphical data (Baldanza et al.
2014: 268). Following the description by Baldanza et al.
(2014: 271, fig. 5) the review of the holotype and the ad-
ditional specimen has pointed out that the first anterolateral
tooth in R. propinqua is bifid, whereas the second one is
trifid, as attested by the study of the new specimen from Or-
vieto (Fig. 4C, D), characters not reported by RistoRi (1891)
in his description.
4. Final remarks
According to the recently collected data (Baldanza et
al. 2014; this paper), the fossil record of Ranina pro-
pinqua in Umbria, as well as the more general docu-
mentation of crustaceans (Pasini & GaRassino 2010),
is more widespread than previously known. The bio-
stratigraphic constrains suggest that these findings
are younger than previously hypothesized, and all at-
tributable to Early Pleistocene rather than Pliocene.
This reduces the stratigraphic gap between the fossil
species and the extant and fossil R. ranina. Regard-
ing the palaeoenvironmental aspects, extant Ranina
is usually reported from sandy sediments in which
they burrow (skinneR & Hill 1987), although raninids
are also associated to muddy, soft substrates and even
gravelly bottoms (luque et al. 2012; luque in press).
The new data regarding R. propinqua described here,
and RistoRi’s holotype itself, come from shallow ma-
rine nearshore deposits (fine to coarse sand), and this
reflects the life style of the genus. Nevertheless, these
considerations are largely derived from the only living
species, and all bathymetric considerations are specu-
lative. Extant R. ranina commonly lives from 10 to
100 m depth, and some specimens have been reported
from 200 m depth in Hawaiian waters (FieldinG &
haLey 1976: 131). Based upon the sedimentological
features and the facies analysis, the specimens of R.
propinqua are associated to relatively shallow water
settings (10 to 40 m). Thus, the use of R. propinqua as
an indicator of moderate to high energy nearshore ma-
rine environmental conditions seems reliable. Similar
data are provided for Cenozoic Raninidae from the
area of Vicenza. In this case, R. pellattieroi de anGeli
& BescHin, 2011, R. bouilleana A. milne edwaRds,
1872, R. speciosa (münsteR, 1840), and R. ornata de
anGeli & BescHin, 2011 are related to warm, shallow
water lagoon deposits (de anGeli & BescHin 2011).
Thus, the use of this approach, based on facies analy-
sis, should be considered for other studies, in order to
better define the palaeoenvironmental and palaeoeco-
logical implications of the occurrences of Ranina.
Acknowledgements
We wish to thank danièle Guinot (Museum national
d’Histoire naturelle, Paris) for useful suggestions about the
extant Ranina ranina and its relative references; rodney M.
Feldmann (Kent State University, Ohio), and Barry W.M.
Van Bakel (Oertijdmuseum De Groene Poort, Boxtel) for
useful suggestions about the characters of the representa-
tives of the subfamily Ranininae; JaVieR luque (University
of Alberta, Canada), and torrey nyBorg (Loma Linda Uni-
versity, California, USA), for careful review and criticism.
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Manuscript received: September 10th, 2014.
Revised version accepted by the Stuttgart editor: Novem-
ber 11th, 2014.
Addresses of the authors:
FedeRico Famiani, School of Science and Technology, Ge-
ology Division, Università di Camerino, Via Gentile III da
Varano, 62032, Camerino, Italy;
e-mail: federico.famiani@unicam.it
RoBeRto BizzaRRi, anGela Baldanza, Department of Phys-
ics and Geology, Università di Perugia, Piazza Università 1,
06123 Perugia, Italy;
e-mail: roberto.bizzarri@libero.it;
angela.baldanza@unipg.it
antonio de anGeli, Associazione Amici del Museo Zan-
nato, Piazza Marconi 15, 36075 Montecchio Maggiore (Vi-
cenza), Italy;
e-mail: antonio.deangeli@alice.it
alessandRo GaRassino, Natural History Museum, Palaeon-
tology Department, Corso Venezia 55, 20121 Milano, Italy;
e-mail: alegarassino@gmail.com
GioVan ni Pasini, Via Alessandro Volta 16, 22070 Appiano
Gentile (Como), Italy;
e-mail: juanaldopasini@tiscali.it
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