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Late villafranchian and early mid-pleistocene faunas in Italy
Palaeogeography, Palaeoclimatology, Palaeoecology Elsevier Publishing C o m p a n y , A m s t e r d a m - Printed in T h e N e t h e r l a n d s
LATE V I L L A F R A N C H I A N A N D E A R L Y M I D - P L E I S T O C E N E F A U N A S IN ITALY A. A Z Z A R O L I AND P. A M B R O S E T T I
Geological Institute, University of Florence, Florence (Italy) (Received J a n u a r y 5, 1970)
SUMMARY
Typical Upper Villafranchian assemblages survive with slight changes up to the end of the Lower Pleistocene. One of these, near Imola, can be correlated with a marine fauna attributed to the Upper Calabrian by GIGr~OUX (1916), and overlies the Plio-Pleistocene boundary by more than 1,000 m. Another faunal assemblage from Farneta, southern Tuscany, is perhaps the youngest assemblage with Villafranchian affinities in Italy. The beginning of the Cromerian is marked by a spectacular faunal revolution. In the surroundings of Rome the Cromerian can be correlated with the marine Sicilian. Other Cromerian faunas are recorded from Tuscany (San Gimignano and Farneta) and from Piedmont (Cortiglione Monferrato). LATE VILLAFRANCHIAN FAUNAS
In 1967 the senior author (AzzAROLI, 1970) restudied the stratigraphy of the Villafranchian of Europe and proposed a subdivision of this stage into four biozones, called respectively Lower Villafranchian, Middle Villafranchian, Upper Villafranchian a and Upper Villafranchian b. The Villafranchian ranges up to the end of the Lower Pleistocene and is followed at the beginning of the Middle Pleistocene by the Cromerian. Evidence was brought forward in this and in former papers (AZZAROL1, 1963) for a direct correlation of the Lower Villafranchian with the marine Upper Pliocene. The Middle Villafranchian was tentatively correlated with the lowermost marine Pleistocene (Red Crag) of east Anglia. No correlation was made in this paper between Upper Villafranchian continental faunas and marine faunas. By far the richest Upper Villafranchian site in Italy is the second lacustrine phase of the Upper Valdarno in Tuscany. It was formerly believed that its sediments reached to the very top of the Villafranchian (AzZAROH, 1965), but it now seems more likely that they extend only to the base of the Upper Villafranchian b. Other sites with faunal assemblages that still have a Villafranchian character, Palaeogeography, Palaeoclimatol., Palaeoecol., 8 (1970) 107-111
108
A. AZZAROLIAND P. AMBROSETTI
although somewhat younger than the highest beds of the second lacustrine phase of the Upper Valdarno have been recognized since. In 1968 AZZAROLI and BERZI (1970) restudied the stratigraphy and the'fauna of the hills south of Imola, a small town at the southern margin of the Po Plain, east-southeast of Bologna. This is the locality where G[GNOUX (1916) established his well-known correlation between the Villafranchian and the marine Calabrian. The result of this work may be summarized as follows. The local Pleistocene marine sequence (SELLI, 1962; CREMONINI et al., 1967) is made of more than 1,000 m of blue clays overlain by yellow littoral sands of much smaller, though highly variable thickness. The beginning of the Pleistocene is evidenced by the appearance of "cold" species such as Arctica islandica, Chlamys septemradiata, Panopaea norvegica etc. The blue clays have thus yielded faunas indicative of a cold climate, except in their intermediate part, where "cold" species are lacking. The yellow sands contain a rich marine fauna (TOLDO, 1905; GIGNOUX, 1916) of temperate climate, together with mammalian remains. Gignoux allocated the yellow sands to the Upper Calabrian, while Selli and Cremonini et al. located the blue clays in three different stages, namely Calabrian, Emilian and Sicilian, and referred the yellow sands to the Milazzian. Selli's datings are incompatible not only with Gignoux's, but also with those generally accepted in central Italy, as will be shown later. The mammalian fauna of the yellow sands is scanty and fragmentary, but is typical of the Upper Villafranchian and very probably belongs to the Upper Villafranchian b. Evidence for this dating is derived from the occurrence of Hippopotamus and of an elephant of the Elephas meridionalis stock, but more advanced than the type specimens of this species. Some molars of Equus stenonis (?) and several fragments of Dicerorhinus cf. etruscus, Leptobos (?) sp., Cervus (Eucladoceros) cf. dieranios rule out a post-Villafranchian age. It will be noted that this fauna occurs more than 1,000 m above the Plio-Pleistocene boundary, in a temperate environment preceded by two cold periods separated by a first temperate episode. Another fauna of Upper Villafranchian age has recently been discovered in the yellow fluviatile sands near the medieval abbey of Farneta in the Chiana Valley, southern Tuscany (AzzAROLI, 1970). The most significant, and also the commonest element of the fauna is an elephant of the Elephas meridionalis stock, but decidedly more advanced than this species. Other faunal elements are Leptobos vallisarni, deer (two species), Equus stehlini (?), Homotherium (?) sp., a hyaena and a rhinoceros of the size of Dicerorhinus etruscus. Altogether, the fauna is similar, but not identical to the classical fauna of the second lacustrine phase of the Upper Valdarno. It is striking that Equus stenonis, Leptobos etruscus and Hippopotamus have not yet been detected in this fauna. An explanation of this and of the occurrence of the advanced elephant of the "meridionalis" stock may be that the Farneta Sands are slightly younger than the highest part of the Upper Villafranchian beds
Palaeogeography, Palaeoclimatol.,Palaeoecol., 8 (1970) 107-111
LOWER--MIDDLE PLEISTOCENE FAUNAS IN ITALY
]09
of the Upper Valdarno, and perhaps also a little younger than the yellow littoral sands of Imola, The uppermost Villafranchian faunas are clearly derived from the Middle Villafranchian and early Upper Villafranchian faunas. CROMERIAN FAUNAS
The beginning of the Cromerian marks the greatest revolution in the continental faunas of the whole Pleistocene Period. Most of the Villafranchian fauna was wiped out and replaced by a new fauna, which presumably immigrated from eastern Europe or from Asia. At present it is not known how many species survived the Lower Middle Pleistocene boundary, and Italian faunas are too poor to settle the matter. The faunal break is, however, spectacular, and was presumably due to a sharp climatic deterioration. The richest Cromerian assemblage in Italy comes from the surroundings of Rome (see Fig. l), where a definite correlation between a mammalian fauna and the marine Sicilian stage has been established (AMBROSETTL 1967: BONADONNA, 1968). Along the Tiber Valley a terrace can be followed over a distance of several kilometres; from 70 m above sea level near Nazzano (Ponte Altieri) it degrades to the present delta area and finishes heteropically into the sediments of the Ponte Galeria Formation. In the lower part of this formation many lenses of sandy clay are exposed which have yielded a rich microfauna with interesting species, such as Bofvina catanensis Cassidulina laevigata car#~ata, Hyalinaea balthica. The Ponte Galeria Formation is underlain by sandy clays heteropic of the grey Arctica islandica Sands of Via Farneto (Monte Mario), a classical Calabrian site: an erosion surface separates the two formations. The Ponte Galeria Formation can therefore be attributed only to the Sicilian, The continental faunas of the deltaic and fluviatile sediments of the Tiber Valley are of great interest. These faunas have been known for a century at least, but were incorrectly identified, so that their significance was realized only in recent years. The fauna of Ponte Galeria (Cava Arnolfi) includes Megaceros (Megaceroides) verticornis, Hippopotamus amphibius, Cervus acoronatus, Dama cf. dama, Elephas cf. trogontherii, Elephas cf. antiquus and Bos pr#nigenius. This is, in the light of our present knowledge of Pleistocene faunas, a Cromerian assemblage. It may be pointed out that the marine Sicilian microfaunas occur in the lower part of the Ponte Galeria Formation, while vertebrate remains are common in the middle and upper portions of the same formation. At present this is the only locality where Sicilian and Cromerian faunas can be directly correlated. On the Tiber Valley upstream of Rome the Cromerian sediments of the aforementioned terrace rest on the Villafranchian formation of the Sabina district, which is partly heteropic of the grey Arctica islandica (Calabrian) Sands of the Farnesina. Palaeogeograph.v, Palaeoclimatol., Palaeoecol., 8 (1970) 107-11 I
110
A. AZZAROLI AND P. AMBROSETTI V. Farneto
Villa dei Masslm~
V.
f
Damiano ~
Chigsa
Z7 V. SirnoniI
I
~
--
~
Ponte Altieri
~
I~
GrottediReglna/
Cava Arnolfi
..o~
Cava Rinaldl
E
1
.O
l
-
,
~',:,:,i
!i!~;~!
i--
Fig.1. Synopsis of the Plio-Pleistocene formations of the R o m e area. Heights in metres above sea level. 1 -- Pliocene, clays and sand banks; 2 -- Calabrian, sandy clays, sands and gravels; 3 = Sicilian and Cromerian, sandy clays, marls and gravels; 4 -- rubefied sands with volcanic products of the F l a m i n i a n - N o m e n t a n e a n (? Mindel-Riss) Interglacial; 5 = postN o m e n t a n e a n tuffites.
The Cromerian deposits of Ponte Galeria and of the Tiber Valley are capped by deposits containing the products of the first volcanic activity of Latium. Immediately after the first occurrence of these products the sequence is interrupted by an erosional surface. In the local Pleistocene chronology this erosional surface represents the Flaminian cold period ( = Mindel?), while the erosional surface between the Calabrian and the Cromerian represents the Cassian ( = Giinz?) cold period. Palaeogeography, Palaeoclirnatol., Palaeoecol., 8 (1970) 107-111
LOWER-MIDDLE PLEISTOCENE FAUNASIN ITALY
II[
Apart from the Ponte Galeria fauna, C r o m e r i a n faunas are scanty in Italy. Two faunas were recently discovered in Tuscany. The first comes from a small lacustrine basin with lignites at M o n t e Oliveto near San G i m i g n a n o , Siena province. The most characteristic faunal element is Megaceros verticornis (an savini?), a c c o m p a n i e d by Equus caballus (large), ox, elephant (Elephas antiquus?) etc. The second f a u n a comes from the ferruginous gravels at the top of the Upper Villafranchian sands of F a r n e t a (see p.108); characteristic species are Megaceros ( Megaceroides) verticornis (a frontal with antlers) and Elephas antiquus (?) (limb bones). In n o r t h e r n Italy the best C r o m e r i a n fossil is a fine antler of Cervus pliotarandoides (probably a s y n o n y m of Megaceros verticornis) from Cortiglione Monferrato, P i e d m o n t (DE ALESSANDRI, 1903). The fossil is said to come from gravels with white calcareous concretions; similar gravels overlie disconformably the lacustrine f o r m a t i o n of the Lower Villafranchian at Villafranca d'Asti. Post-Villafranchian species of elephants (Elephas antiquus, Elephas trogontherii) have been recorded by ZUFFARD1 (1913) from several localities near Villafranca d'Asti. There can be little d o u b t that they come from c o n t i n e n t a l deposits overlying the fluvio-lacustrine Lower Villafranchian formation. Their age, however, is not exactly known. REFEREN('ES
AMBROSETTI, P., 1967. Cromerian fauna of the Rome area. Quaternaria, 9:267 284. AZZAROLI, A., 1963. Rinoceronti pliocenici del Valdarno Inferiore. Palaeontographia ltaliea, 57: 11 20. AZZAROLI, A., 1965. The two Villafranchian horses of the Upper Valdarno. Palaeontographia Italica, 59:1 12. AZZaROLI, A., 1970. Villafranchian correlations based on large mammals. Giorn. Geol., 35(2), in press. AZZAROLI,A. and BERZl, A., 1970. On an Upper Villafranchian fauna at lmola, northern Italy, and its correlation with the marine sequence of the Po Plain. Palaeontographia Itallca, in press. BONADONNA,F. P., 1968, Studi sul Pleistocene del Lazio, 5. La biostratigrafia di Monte Mario e la "'Fauna MalacoIogica Mariana'" di Cerulli lrelli. Mere. Soc. Geol. ltal., 7(2): 261-322. CREMONINI, G., ELMI, C. and MONESI, A., 1967. La serie del Santerno (lmola). Comm. Mediterranean Neogene, Intern. Congr., 4th Session, Bolo,~na, 1967 Guidebook to the E,x'earsions, pp.98 102. DE ALESSANDRI,G., 1903. Sopra alcuni avanzi di Cervidi pliocenici del Piemonte. Atti Acead. Sci. Torino, 38: 573-586. GtGNOUX, M., 1916. L'6tage Calabrien (Plioc6ne superieur marin) sur le versant nord-est de l'Apennin entre le Monte Gargano et Plaisance. Bull. Soc. Gkol. France, 3(4): 324 348. SELtl, R., 1962. Le Quaternaire marin du versant Adriatique et lonien de la peninsule italienne. Quaternaria, 4:391-413. TOLDO, G., 1905. Note preliminari sulle condizioni geologiche dei contrafforti appenninici compresi fra il Sillaro e il Lamone. Boll. Soc. Geol. Ital., 24:343 386. ZUr-VARDLP., 1913. El&anti fossili del Piemonte. Palaeontagraphia ltafica, 19:121 178.
Palaeogeo,~raphy, Palaeocfimatol., Palaeoeeol., 8 (1970) 107 1I1
LATE V I L L A F R A N C H I A N A N D E A R L Y M I D - P L E I S T O C E N E F A U N A S IN ITALY A. A Z Z A R O L I AND P. A M B R O S E T T I
Geological Institute, University of Florence, Florence (Italy) (Received J a n u a r y 5, 1970)
SUMMARY
Typical Upper Villafranchian assemblages survive with slight changes up to the end of the Lower Pleistocene. One of these, near Imola, can be correlated with a marine fauna attributed to the Upper Calabrian by GIGr~OUX (1916), and overlies the Plio-Pleistocene boundary by more than 1,000 m. Another faunal assemblage from Farneta, southern Tuscany, is perhaps the youngest assemblage with Villafranchian affinities in Italy. The beginning of the Cromerian is marked by a spectacular faunal revolution. In the surroundings of Rome the Cromerian can be correlated with the marine Sicilian. Other Cromerian faunas are recorded from Tuscany (San Gimignano and Farneta) and from Piedmont (Cortiglione Monferrato). LATE VILLAFRANCHIAN FAUNAS
In 1967 the senior author (AzzAROLI, 1970) restudied the stratigraphy of the Villafranchian of Europe and proposed a subdivision of this stage into four biozones, called respectively Lower Villafranchian, Middle Villafranchian, Upper Villafranchian a and Upper Villafranchian b. The Villafranchian ranges up to the end of the Lower Pleistocene and is followed at the beginning of the Middle Pleistocene by the Cromerian. Evidence was brought forward in this and in former papers (AZZAROL1, 1963) for a direct correlation of the Lower Villafranchian with the marine Upper Pliocene. The Middle Villafranchian was tentatively correlated with the lowermost marine Pleistocene (Red Crag) of east Anglia. No correlation was made in this paper between Upper Villafranchian continental faunas and marine faunas. By far the richest Upper Villafranchian site in Italy is the second lacustrine phase of the Upper Valdarno in Tuscany. It was formerly believed that its sediments reached to the very top of the Villafranchian (AzZAROH, 1965), but it now seems more likely that they extend only to the base of the Upper Villafranchian b. Other sites with faunal assemblages that still have a Villafranchian character, Palaeogeography, Palaeoclimatol., Palaeoecol., 8 (1970) 107-111
108
A. AZZAROLIAND P. AMBROSETTI
although somewhat younger than the highest beds of the second lacustrine phase of the Upper Valdarno have been recognized since. In 1968 AZZAROLI and BERZI (1970) restudied the stratigraphy and the'fauna of the hills south of Imola, a small town at the southern margin of the Po Plain, east-southeast of Bologna. This is the locality where G[GNOUX (1916) established his well-known correlation between the Villafranchian and the marine Calabrian. The result of this work may be summarized as follows. The local Pleistocene marine sequence (SELLI, 1962; CREMONINI et al., 1967) is made of more than 1,000 m of blue clays overlain by yellow littoral sands of much smaller, though highly variable thickness. The beginning of the Pleistocene is evidenced by the appearance of "cold" species such as Arctica islandica, Chlamys septemradiata, Panopaea norvegica etc. The blue clays have thus yielded faunas indicative of a cold climate, except in their intermediate part, where "cold" species are lacking. The yellow sands contain a rich marine fauna (TOLDO, 1905; GIGNOUX, 1916) of temperate climate, together with mammalian remains. Gignoux allocated the yellow sands to the Upper Calabrian, while Selli and Cremonini et al. located the blue clays in three different stages, namely Calabrian, Emilian and Sicilian, and referred the yellow sands to the Milazzian. Selli's datings are incompatible not only with Gignoux's, but also with those generally accepted in central Italy, as will be shown later. The mammalian fauna of the yellow sands is scanty and fragmentary, but is typical of the Upper Villafranchian and very probably belongs to the Upper Villafranchian b. Evidence for this dating is derived from the occurrence of Hippopotamus and of an elephant of the Elephas meridionalis stock, but more advanced than the type specimens of this species. Some molars of Equus stenonis (?) and several fragments of Dicerorhinus cf. etruscus, Leptobos (?) sp., Cervus (Eucladoceros) cf. dieranios rule out a post-Villafranchian age. It will be noted that this fauna occurs more than 1,000 m above the Plio-Pleistocene boundary, in a temperate environment preceded by two cold periods separated by a first temperate episode. Another fauna of Upper Villafranchian age has recently been discovered in the yellow fluviatile sands near the medieval abbey of Farneta in the Chiana Valley, southern Tuscany (AzzAROLI, 1970). The most significant, and also the commonest element of the fauna is an elephant of the Elephas meridionalis stock, but decidedly more advanced than this species. Other faunal elements are Leptobos vallisarni, deer (two species), Equus stehlini (?), Homotherium (?) sp., a hyaena and a rhinoceros of the size of Dicerorhinus etruscus. Altogether, the fauna is similar, but not identical to the classical fauna of the second lacustrine phase of the Upper Valdarno. It is striking that Equus stenonis, Leptobos etruscus and Hippopotamus have not yet been detected in this fauna. An explanation of this and of the occurrence of the advanced elephant of the "meridionalis" stock may be that the Farneta Sands are slightly younger than the highest part of the Upper Villafranchian beds
Palaeogeography, Palaeoclimatol.,Palaeoecol., 8 (1970) 107-111
LOWER--MIDDLE PLEISTOCENE FAUNAS IN ITALY
]09
of the Upper Valdarno, and perhaps also a little younger than the yellow littoral sands of Imola, The uppermost Villafranchian faunas are clearly derived from the Middle Villafranchian and early Upper Villafranchian faunas. CROMERIAN FAUNAS
The beginning of the Cromerian marks the greatest revolution in the continental faunas of the whole Pleistocene Period. Most of the Villafranchian fauna was wiped out and replaced by a new fauna, which presumably immigrated from eastern Europe or from Asia. At present it is not known how many species survived the Lower Middle Pleistocene boundary, and Italian faunas are too poor to settle the matter. The faunal break is, however, spectacular, and was presumably due to a sharp climatic deterioration. The richest Cromerian assemblage in Italy comes from the surroundings of Rome (see Fig. l), where a definite correlation between a mammalian fauna and the marine Sicilian stage has been established (AMBROSETTL 1967: BONADONNA, 1968). Along the Tiber Valley a terrace can be followed over a distance of several kilometres; from 70 m above sea level near Nazzano (Ponte Altieri) it degrades to the present delta area and finishes heteropically into the sediments of the Ponte Galeria Formation. In the lower part of this formation many lenses of sandy clay are exposed which have yielded a rich microfauna with interesting species, such as Bofvina catanensis Cassidulina laevigata car#~ata, Hyalinaea balthica. The Ponte Galeria Formation is underlain by sandy clays heteropic of the grey Arctica islandica Sands of Via Farneto (Monte Mario), a classical Calabrian site: an erosion surface separates the two formations. The Ponte Galeria Formation can therefore be attributed only to the Sicilian, The continental faunas of the deltaic and fluviatile sediments of the Tiber Valley are of great interest. These faunas have been known for a century at least, but were incorrectly identified, so that their significance was realized only in recent years. The fauna of Ponte Galeria (Cava Arnolfi) includes Megaceros (Megaceroides) verticornis, Hippopotamus amphibius, Cervus acoronatus, Dama cf. dama, Elephas cf. trogontherii, Elephas cf. antiquus and Bos pr#nigenius. This is, in the light of our present knowledge of Pleistocene faunas, a Cromerian assemblage. It may be pointed out that the marine Sicilian microfaunas occur in the lower part of the Ponte Galeria Formation, while vertebrate remains are common in the middle and upper portions of the same formation. At present this is the only locality where Sicilian and Cromerian faunas can be directly correlated. On the Tiber Valley upstream of Rome the Cromerian sediments of the aforementioned terrace rest on the Villafranchian formation of the Sabina district, which is partly heteropic of the grey Arctica islandica (Calabrian) Sands of the Farnesina. Palaeogeograph.v, Palaeoclimatol., Palaeoecol., 8 (1970) 107-11 I
110
A. AZZAROLI AND P. AMBROSETTI V. Farneto
Villa dei Masslm~
V.
f
Damiano ~
Chigsa
Z7 V. SirnoniI
I
~
--
~
Ponte Altieri
~
I~
GrottediReglna/
Cava Arnolfi
..o~
Cava Rinaldl
E
1
.O
l
-
,
~',:,:,i
!i!~;~!
i--
Fig.1. Synopsis of the Plio-Pleistocene formations of the R o m e area. Heights in metres above sea level. 1 -- Pliocene, clays and sand banks; 2 -- Calabrian, sandy clays, sands and gravels; 3 = Sicilian and Cromerian, sandy clays, marls and gravels; 4 -- rubefied sands with volcanic products of the F l a m i n i a n - N o m e n t a n e a n (? Mindel-Riss) Interglacial; 5 = postN o m e n t a n e a n tuffites.
The Cromerian deposits of Ponte Galeria and of the Tiber Valley are capped by deposits containing the products of the first volcanic activity of Latium. Immediately after the first occurrence of these products the sequence is interrupted by an erosional surface. In the local Pleistocene chronology this erosional surface represents the Flaminian cold period ( = Mindel?), while the erosional surface between the Calabrian and the Cromerian represents the Cassian ( = Giinz?) cold period. Palaeogeography, Palaeoclirnatol., Palaeoecol., 8 (1970) 107-111
LOWER-MIDDLE PLEISTOCENE FAUNASIN ITALY
II[
Apart from the Ponte Galeria fauna, C r o m e r i a n faunas are scanty in Italy. Two faunas were recently discovered in Tuscany. The first comes from a small lacustrine basin with lignites at M o n t e Oliveto near San G i m i g n a n o , Siena province. The most characteristic faunal element is Megaceros verticornis (an savini?), a c c o m p a n i e d by Equus caballus (large), ox, elephant (Elephas antiquus?) etc. The second f a u n a comes from the ferruginous gravels at the top of the Upper Villafranchian sands of F a r n e t a (see p.108); characteristic species are Megaceros ( Megaceroides) verticornis (a frontal with antlers) and Elephas antiquus (?) (limb bones). In n o r t h e r n Italy the best C r o m e r i a n fossil is a fine antler of Cervus pliotarandoides (probably a s y n o n y m of Megaceros verticornis) from Cortiglione Monferrato, P i e d m o n t (DE ALESSANDRI, 1903). The fossil is said to come from gravels with white calcareous concretions; similar gravels overlie disconformably the lacustrine f o r m a t i o n of the Lower Villafranchian at Villafranca d'Asti. Post-Villafranchian species of elephants (Elephas antiquus, Elephas trogontherii) have been recorded by ZUFFARD1 (1913) from several localities near Villafranca d'Asti. There can be little d o u b t that they come from c o n t i n e n t a l deposits overlying the fluvio-lacustrine Lower Villafranchian formation. Their age, however, is not exactly known. REFEREN('ES
AMBROSETTI, P., 1967. Cromerian fauna of the Rome area. Quaternaria, 9:267 284. AZZAROLI, A., 1963. Rinoceronti pliocenici del Valdarno Inferiore. Palaeontographia ltaliea, 57: 11 20. AZZAROLI, A., 1965. The two Villafranchian horses of the Upper Valdarno. Palaeontographia Italica, 59:1 12. AZZaROLI, A., 1970. Villafranchian correlations based on large mammals. Giorn. Geol., 35(2), in press. AZZAROLI,A. and BERZl, A., 1970. On an Upper Villafranchian fauna at lmola, northern Italy, and its correlation with the marine sequence of the Po Plain. Palaeontographia Itallca, in press. BONADONNA,F. P., 1968, Studi sul Pleistocene del Lazio, 5. La biostratigrafia di Monte Mario e la "'Fauna MalacoIogica Mariana'" di Cerulli lrelli. Mere. Soc. Geol. ltal., 7(2): 261-322. CREMONINI, G., ELMI, C. and MONESI, A., 1967. La serie del Santerno (lmola). Comm. Mediterranean Neogene, Intern. Congr., 4th Session, Bolo,~na, 1967 Guidebook to the E,x'earsions, pp.98 102. DE ALESSANDRI,G., 1903. Sopra alcuni avanzi di Cervidi pliocenici del Piemonte. Atti Acead. Sci. Torino, 38: 573-586. GtGNOUX, M., 1916. L'6tage Calabrien (Plioc6ne superieur marin) sur le versant nord-est de l'Apennin entre le Monte Gargano et Plaisance. Bull. Soc. Gkol. France, 3(4): 324 348. SELtl, R., 1962. Le Quaternaire marin du versant Adriatique et lonien de la peninsule italienne. Quaternaria, 4:391-413. TOLDO, G., 1905. Note preliminari sulle condizioni geologiche dei contrafforti appenninici compresi fra il Sillaro e il Lamone. Boll. Soc. Geol. Ital., 24:343 386. ZUr-VARDLP., 1913. El&anti fossili del Piemonte. Palaeontagraphia ltafica, 19:121 178.
Palaeogeo,~raphy, Palaeocfimatol., Palaeoeeol., 8 (1970) 107 1I1