FROM RIFT TO DRIFT AND WEST-MEDITERRANEAN-TYRRHENIAN TECTONIC
SETTING: A REVIEW
Carlo Savelli
Consiglio Nazionale delle Ricerche, Istituto di Scienze del Mare, via P. Gobetti, 101, 40129,
Bologna, Italy
E-mail address: carlo.savelli@bo.ismar.cnr.it
Pre-Oligocene, SE-directed flat subduction of European plate produced the submerged orogen of
the West-Mediterranean-Tyrrhenian region. WNW-directed steep subduction of African plate
accompanied the late Miocene-Recent oceanic opening of Tyrrhenian basin, eastern part of
submerged orogen. Post-orogenic rift-related extension and calc-alkaline volcanism initiated in
the Oligocene reached, in the Burdigalian, the stage of oceanic opening. In the Hercynian
lithosphere of southern Europe and the western part of submerged orogen formed, respectively,
the Sardinia-Provence and the north Algeria bathyal plains. During the Burdigalian, volcanism of
calc-alkaline type has been widespread in the margins of the two oceanic basins. The late
Miocene and late Pliocene drift episodes of the bathyal plains of Vavilov and Marsili occurred,
on the contrary, when volcanism has been absent or scarce in the Tyrrhenian Sea margins. The
contrast between abundance and lack of volcanism in the margins, at various times of rift-drift
transition, is interpreted to indicate diversity of tectonic setting. In the Oligo-Burdigalian,
drifting and calc-alkaline volcanism took place in the absence of subduction. The WNWdirected, steep subduction under the Tyrrhenian orogen commenced, probably, at 16/15 Ma (the
waning of Burdigalian spreading). The space-time study indicates that calc-alkaline volcanism
and extension are not linked only to subduction.
Subject terms: Geology Tectonics
Introduction
Extension tectonics and volcanism of Oligocene-Recent age of the West-MediterraneanTyrrhenian region are a consequence of the interactions between the European and African
plates. Figure 1 shows that SE-directed flat-slab (Alpine-type) subduction of European plate has
been replaced by WNW-directed steep-slab (Island-arc type) subduction of African plate. The
former subduction led to the Mediterranean submerged orogen of Alpine age (OAA) in the Late
Cretaceous-Eocene, and the latter produced basin opening and slab roll-back beneath the
Maghrebid-Apennine wedging. The OAA extending from Alpine Corsica to the Betic cordillera
(Fig. 2) was recognized as the westernmost branch of the western Alps related to the closure of
the Mesozoic Alpine Tethys2, 3, 4, 5, 6. The slab beneath the south Tyrrhenian bathyal plain 7 is
accompanied by release of 500 km deep seismic energy, high heat flow and positive gravity
anomal. Regional lithosphere models indicate crustal thinning of <10 km and a 30 km LID.
Various seafloor mineral deposits of hydrothermal origin are present, too8. Despite the young
age, the West-Mediterranean-Tyrrhenian region was subject of various tectonic interpretations
(see Supplementary Info S1).
Extension and magmatism commenced ca. 33/32 Ma (early Oligocene) in the OAA and the
Hercynian lithosphere extending from Provence to Corsica-Sardinia. The extension reached the
stage of consecutive emplacement of oceanic lithosphere in the Sardinia/Provence, north Algeria,
Vavilov and Marsili basins (Fig. 1) during the last 20 Ma (Burdigalian - Recent). Overall,
continental margin block rotation produced asymmetric basin opening (Fig.1)9. The SardiniaProvence and North Algeria basins are separated by the
Figure 1. Relief-shaded image of the west Mediterranean-Tyrrhenian area showing the Recent convergence fronts
of the Maghreb-Apennines and Alpine belts, the pre-Oligocene front of subduction of the European plate beneath
the extended orogen of Alpine age (OAA), and the oceanic basins of Sardinia-Provence (Sa-Pr b), Vavilov (V b),
Marsili (M b) and north Algeria. The white arrows show the counter-clockwise rotation of Corsica-Sardinia and
north Apennines, and the clockwise rotation of the Algeria margin and south Apennines. Legend: CTFZ = Catalan Tunisian fracture zone separating the west segment of European lithosphere and extended OAA from that to the east
(see text for discussion); CVZ = Catalan volcanic zone; GA = Gibraltar arc; RAF = Relict Alpine Front; TASZ =
Trans-Alboran fracture zone; WSG = west Sardinia graben. The Algerian Maghreb magmatic sites: Or R =
Oranois; Che = Cherchell; EA = East of Algiers; GK = Great Kabylia; LK = Little Kabylia; 41-P = 41° parallel
fracture zone. The figure was created using the Plotmap cartographic software 1.
major transcurrent structure known as the “north Balearic fracture zone” or the “Paul Fallot
transform fault”) which dates back to the plate interactions of Hercynian age10. This structure
extending from the Catalan volcanic zone to the magmatic island of La Galite (Tunisian
offshore) - hereafter called “Catalan-Tunisian fracture zone” - separates the western portion of
the Mediterranean OAA and European lithosphere from that to the east. In particular, the fracture
zone divides the Sardinia-Provence oceanic basin (European lithosphere) from the north
Algerian basin (the western portion of the OAA), and this from the OAA portion that will see the
Tyrrhenian opening. Another major lineation zone is found along the 41° parallel. It separates the
north and south Tyrrhenian where thinned continental and oceanic lithosphere are rimmed by the
the north and south Apennines which rotated counter-clockwise and clockwise, respectively11.
In the Earth Sciences, a generally accepted idea is that magmatism of calc-alkaline type
results from partial melting of sources which underwent metasomatic modification via chemical
recycling of subducted (mainly upper) crustal material. Though, the temporal interval between
subduction and igneous manifestations is matter of debate. The pervasive presence of calcalkaline volcanism above the zones of Recent plate convergence is probably at the origin of the
tenet that melt uprising and metasomatism overlapped in time with subduction and
metamorphism also in the geological past. On the other hand, the geological record suggests that
calc-alkaline volcanism occurred, too, in rift setting far from subduction, which implicates that
metasomatism and metamorphism took most likely place earlier than the eruptive activity. The
temporal gap between the metasomatism linked to the tectonic mode of plate convergence and
volcanism of calc-alkaline type can be highly variable. The episodes of oceanic basin opening
and their space-time relationships with volcanism are re-examined to contribute to the debate pro
or against the concomitance of subduction and calc-alkaline volcanism.
Because igneous petrology of magmatism is out of the scope, the datasets S4 and S6 are
shown in the Supplementary material. Among the literature geochronology data of the West
Mediterranean-Tyrrhenian region there can be some incorrectness because of the diverse quality
of analysed material, and diversity of laboratories and analytical methods. However, dubious
(few) ages can be tentatively pointed out by means of plausible temporal correlation among the
re-examined large data set.
Volcanoclastic rocks showing calc-alkaline nature are widespread among the
allochthounous sediments of the Apennines (Fig. 2; Supplementary Info S3 and Datasets S5, S6).
If they have been produced from lost emission centres which were originally sited in the
Tyrrhenian OAA, their space-time distribution can also be meaningful for the reconstruction of
the link between calc-alkaline volcanism and tectonic setting. For the first time, allochthonous
and “in-situ” volcanics have been jointly considered.
Figure 2. Distribution of “in situ” magmatics of the west Mediterranean, and allochthonous volcanoclastics of the
Apennines. (A); Oligocene-Aquitanian (between ca. 33/32 and ca. 20 Ma): intrusives (red circle), volcanics (red
triangle) and allochthonous volcanoclastics (elongated red triangle without rim shows presumed position; green
numbers in italics; see Suppl. dataset S4). Site 13: buried andesite volcano of the early Oligocene. White arrows: 1 =
pre-Oligocene (> 33 Ma), SE-directed subduction beneath the orogen of Alpine Age (OAA); 2 = Post-Burdigalian
(< 16 Ma), WNW-directed subduction of African lithosphere; this reconstruction considers that subduction was
absent in the Oligocene - Burdigalian time. (B); Burdigalian (ca. 20 - 16 Ma): intrusives (black circle), volcanics
(black triangle) and allochthonous volcanoclastics (elongated gray triangle); Langhian-Tortonian (between ca. 16
and 7.5 Ma): intrusives (yellow circle), volcanics (black rimmed yellow triangle) and allochthonous volcanoclastics
(elongated yellow triangle). In the Burdigalian, calc-alkaline magmatism of andesitic and silicic type was
accompanied by eruption of tholeiitic lavas and rifting reached the stage of oceanic spreading in the SardiniaProvence basin to the east of the Catalan-Tunisian fracture zone (CTFZ; European plate), and north Algerian basin
to the west. The scheme shows the inferred position of the WNW subduction hinge zone at ca. 6.3 (Vavilov
opening) and 1.67 Ma (Marsili opening), the Apennine outcrops of the allochthonous volcanoclastic rocks, and the
hypothetical sites of “lost” volcanic edifices and adjacent sedimentary lows which, according to the geodynamic
interpretation (see Guerrera et alii, 1998, and Cibin et alii, 2001 in the Suppl. info), were originally sited in the
Tyrrhenian OAA (offshore Sardinia-Corsica). Dotted line: the lithosphere-asthenosphere section of Fig. 7/A.
Figure 3. Shaded relief image of the Tyrrhenian seafloor; depths are colour-coded, illumination from the NW after
multibeam bathymetric survey16 below 200 m waterdepth.The Tyrrhenian bathyal plains of Vavilov (V) and Marsili
(M) reach depth of 3600 m (proper blue).
Results
Episodes of oceanic opening
Burdigalian (ca. 20 – 16 Ma)
Post-collision, continental extension and calc-alkaline volcanism initiated in the
Oligocene reached the stage of oceanic opening in the Burdigalian (ca. 20 – 16 Ma). Figure 3
shows that this seafloor spreading episode occurred in the European lithosphere (SardiniaProvence basin) and the western part of submerged orogen (north Algeria basin). The SardiniaProvence and north Algeria basins are found respectively east and west of the Catalan-Tunisian
fracture zone (Figs. 1 and 3). As both the two deep basins are not penetrable by deep drilling the
timing of their oceanic opening can be studied only in the margins.
Formation of Sardinia-Provence basin and counter-clockwise rotation of the Hercynian
magma-rich margin of Corsica-Sardinia have been determined from paleomagnetic and
geochronological data about the widespread volcanism of western Sardinia12, 13. A temporal
overlap of the Sardinian-Provence and north Algeria openings has been considered by various
authors5, 10. A 17.8 Ma dating of monazite (deformed leucogranite of Edough granitoid Massif of
Little Kabylia; site 12,) may reflect the age of thrusting connected with opening of the north
Algeria basin14. Emplacement of granitoids, and andesite and dacite bodies along the Algerian
coast (16-15 Ma) may go with the end of oceanic spreading of the corresponding offshore15.
Figure 4. Multibeam seafloor morphology of the Vavilov bathyal plain from bathymetric survey16; illumination
from the NW. Main morphological elements are: the large volcanoes Vavilov (V) and Magnaghi (M), the Gortani
(G) and D’Ancona (Da) ridges, the De Marchi (De) and Flavio Gioia (F) tilted blocks and the Selli Line (SL) fault.
Refer to text for discussion of salient features of the DSDP and ODP drillsites; the site of ODP 654 drilling is placed
65 km (35 nm) to the WNW of site 653.
Late Miocene (ca. 7.5 – 6.3 Ma)
A recent morpho-bathymetric multibeam survey16 (Fig. 3) and available information of
basement lithology17 provide important evidence for the better understanding of the complex
Tyrrhenian opening. The morpho-structural features of the Vavilov bathyal plain (VB; 34003600 m bsl; Fig. 5) are multifaceted. In its northern part, two seamounts represent inherited
stretched relics of OAA. The western De Marchi (De) and the Flavio Gioia (F) seamount to the
east show N-S trend and elevation of 1200 m above the plain. The NE-SW Selli line (SL) is an
important morphological feature separating the Tyrrhenian bathyal area from the passive margin
offshore Sardinia. The former area is located within the stretched OAA and the latter belongs to
the Hercynian lithosphere of the rotated Corsica-Sardinia block. The SL is the sea-floor
expression of low-angle, east-dipping detachment faulting of continental crust which soles in the
upper mantle beneath the Vavilov basin6. The N-S oriented, 40 km long Gortani ridge (G) with
elevation of ca. 300/400 m is positioned between the De Marchi and Flavio Gioia. In G, beneath
80 m thick sediments of late Pliocene – Quaternary age, the ODP site 655 drilled basalts of
MORB (Mid Ocean Ridge Basalt) type. To the east of (G) and north of Vavilov seamount (V),
ODP site 651 is floored with mantle peridotite. In the sourthern part of the Vavilov plain
between the big volcanoes Magnaghi (M) and (V), the arcuate D’Ancona (Da) ridge initiates
between the SL and De Marchi with elevation of 200-400 m and sediment cover up to 250 m.
This bathyal structure reflects the complex architecture of oceanic opening within the stretched
relics of OAA. Seismic reflection and magnetic anomaly data indicates that isolated, deep-seated
blocks of probable continental crust occur in the up to 800 m high part of the D’Ancona ridge
flanking Vavilov seamount.
In the eastern rim of Vavilov bathyal plain, at waterdepth of 3507 m the DSDP site 373
drilled 190 meter of lava flow and breccia of MORB-like composition below 280 m of early
Pliocene-Quaternary sediments (Fig. 4). Six whole rock K/Ar determinations point to 7.5 to 6.3
+/- 0.8 Ma (late Tortonian – early Messinian) for the site 373 basalt sequence18, 19. The
Tyrrhenian sea evaporitic sediments are linked to the global event called the “Messinian” salinity
crisis which initiated 5.96 Ma ago20, after the start of the Messinian at ca. 7.25 Ma, and ended at
5.33 Ma21 (start of the Pliocene). Thus, the Vavilov opening is older than the evaporitic event.
The absence of evaporites in the bathyal plain ought to reflect a shallow waterdepth which
impeded inflow of Atlantic water in sufficient amount to form such deposits at the time of the
salinity crisis.
In the southern part of the Vavilov plain (below the 40° parallel; Fig. 4), the W-E
trending lithosphere stretching was probably stronger than in the northern part. In fact, in the
plain eastern margin, along the 13°E longitude the presence of oceanic crust at site DSDP 373
(MORB-like basalt) and continental crust in the Flavio Gioia seamount suggests diverse intensity
of lithosphere stretching. The interactions among faulting and magmatism showed clearly
diverse characteristics in the south and north part of the Tyrrhenian basin. The strong extensional
deformation of the south Tyrrhenian (e.g. simple shear Wernicke model) was a result of eastdipping low-angle detachment faulting 6, 17. Hyperextension affected both the OAA, where
Vavilov oceanic lithosphere is emplaced, and the adjacent submerged continental margin of
Hercynian Sardinia. In the Vavilov plain are found mantle peridotites (ODP site 651) and
MORB-type basalts (DSDP site 373; eastern rim). In the Sardinia margin volcanism is absent.
North of the 41° parallel lineation zone, 8 - 6 Ma old granitoid plutonism extends from the
submerged Vercelli seamount and Etruschi ridge to the islands of Montecristo and Elba11 (Figs.
5, 6). High-angle faulting accompanied moderate extension of this continental lithosphere22.
Strong igneous activity and moderate extensional tectonics (e.g. pure shear Wernicke model)
contrast with the hyperextension and weak volcanism of the south Tyrrhenian “mature “ rift.
Overall, low-angle detachment faulting linked to mantle peridotite exposure and non-axial
magma-poor volcanism of the Vavilov plain, in the late Miocene, ought to provide useful
constraints for the oceanic opening of the large continental margins23. Moving from north to
south, the emplacement of granitoids and MORB-type basalts probably reflects increasing
strength of lithosphere extension (Fig.6). The stretching of Tyrrhenian upper plate lithosphere
seems to mirror the diverse nature of the lower plate which subducted beneath the Apennines:
the less subductable continental lithosphere of Adria passes to the cold, more subductable
oceanic lithosphere of the Ionian seafloor22.
Late Pliocene (ca. 1.87 – 1.67 Ma)
Between 1.87 and 1.67 Ma about the Olduvai chron, MORB-type basalts were emplaced
in the western rim of Marsili plain (ODP site 650)17. The Tyrrhenian oceanic opening has been
discontinuous. The intensity of extension and volcanism varied in the course of time. The late
Tortonian-early Messinian and late Pliocene episodes of the Vavilov and Marsili plains have
been characterized by hyperextension and low-standing localized volcanism linked to roundshape magnetic anomaly. The Pliocene and Quaternary episodes (see Supplementary Info S2), on
the contrary, show minor extension and strong high-standing volcanism, and elongated magnetic
patterns. Overall, oceanic opening has been characterized by accretion of alternating horizontal
and vertical type accompanied by eruption of deep-seated and high-standing volcanics,
respectively.
Peri-basinal magmas coeval with oceanic opening between 20 and 16 Ma
European plate
Volcanics showing composition from basalt and andesite to ryolite, and K/Ar datings
between ca. 19.8 and 15.8 Ma occur in the graben of western Sardinia, in southern Corsica and
Mallorca island. Literature geochemistry and age data of these rocks are listed in Supplementary
Table S4.
Mediterranean orogen of Alpine age
Dikes crop out in Malaga-Marbella (site 14, Betic region) in the form of W-E trending
westwards translated bodies24. The rootless dike swarm composition, tholeiitic and transitional to
calc-alkaline, ranges from low-K basaltic andesite to medium-K andesite (samples AM24 to
FG22; Supplementary Dataset S4). The Malaga basaltic dikes yielded 40Ar/39Ar ages of 17.4,
17.7, 19.8, 17.4, 30.2 and 33.6 Ma 24, 25. Granite dike from the Malaga area (site 14; sample
MI22), granite clast from ODP Hole 977 (site 15, sample 7646), diorite clast from Carboneras
(site 10) and dacite from Mar Menor (site 17; sample MM2703) yielded 40Ar/39Ar ages of 18.5,
17.6, 18.9 and 18.5 Ma, respectively24, 25, 26. Intrusive rocks from the Sierra Cabrera (site 16)
yielded Rb/Sr dates of 20.4 and 18.8 Ma27. The K/Ar and Ar/Ar age spectrum between 19.8 and
17.4 Ma of Alboran-Betic magmatics appears to be analytically consistent since it has been
obtained from samples of highly diverse potassium content such as tholeiite groundmass and Kfeldspar separates of granite and dacite. More radiometric age determinations could clarify if
tholeiitic volcanism older than 19 Ma occurred in the Malaga area.
Figure 2/B shows that intrusives are widespread in the Algerian margin. Granodiorites
are exposed in Thenia (site 10a; sample T22), monzonites and diorites in Bejaia-Amizour (site n.
11; samples A12, A1, A9). Cordierite-granites (samples U3, L61), gabbros and rhyolites (sample
C1) crop out in the vulcano-plutonic complex of Cap Bougaroun-Collo (20 x 10 km; site 12),
rhyolites in El Milia (about 30 km to the south of site 12); and tholeiitic basalts in Dellys (site
19). The space-time distribution of volcanics and magmatics that are not coeval with the oceanic
openings is issue of Supplementary Info S2.
Figure 5. Histogram of age data (number of ages vs age data) of magmatics from the Provence-Corsica-SardiniaTyrrhenian-Peninsular Italy area since the Oligocene. a) = the age clusters of the Oligocene -mid Miocene (ca. 33/32
- 12 Ma), Pliocene (ca. 5.4 - 1.8 Ma) and Quaternary (ca. 1.2 - 0 Ma; see Fig. 6 and text); b) = the episodes of
oceanic spreading (OS) which formed the basins of Sardinia-Provence, Vavilov and Marsili. With respect to the
peripheral areas of the basins, volcanic activity has been abundant during OS1, and absent or scarce during OS2 and
OS3. Legend: th = tholeiites; grd = granitoids.
Relationships between oceanic opening and peri-basinal magmas
Age distribution
An age histogram illustrates the distribution of geochronology data of magmatics from the
Provence-Corsica-Sardinia-Tyrrhenian region and the peninsular Italy since the Oligocene (Fig.
5/a). Figure part (b) shows that intra-basin magmatics were present during the Tyrrhenian
spreading episodes of the late Miocene (Vavilov basin, OS2) and the late Pliocene (Marsili basin,
OS3). In the Burdigalian, seafloor spreading of the Sardinia-Provence basin (OS1) occurred in
concomitance with strong eruptive activity of the margins. By the same period, also the opening
of the north Algeria basin of the west Mediterranean OAA was accompanied by intense eruptive
activity of the margins (Fig. 2). The late Miocene and late Pliocene episodes of oceanic opening
of the bathyal plains of Vavilov and Marsili occurred, on the contrary, when volcanism has been
absent or scarce in the Tyrrhenian Sea margins.
The Oligocene magmatics show up to ca. 400 km transversely to the SW-NE trend of the
submerged OAA and European margin, and along the CTFZ (see the distance between the sites
n. 2/4 and 11/13 of Fig. 2/A) on one hand. On the other hand, the SE-NW trending volcanics of
the rotated Tyrrhenian margin (< 1 Ma) are no more than 100-200 km wide in across-arc
direction (Fig. 6). In the Burdigalian, basalts of tholeiitic type (Figs. 2, 5) erupted during peak
volcanism. On the other hand, seafloor arc tholeiites (ca. 1 Ma) pre-date the acme of the Aeolian
island volcanism (ca. 0.2 Ma).
Figure 6. Distribution scheme showing the “in situ” magmatics of the Tyrrhenian region and surroundings. Legend:
1 = calc-alkaline volcanics erupted between ca. 33/32 and 12 Ma; 2 = oceanic spreading of Vavilov bathyal plain
(ca. 7.5 - 6.3 Ma; DSDP site 373, see *); 3 = post-orogenic granitoids of the north Tyrrhenian (ca. 8 to 6 Ma, late
Miocene); 4 = magmatics erupted between ca. 5 and 2 Ma (Pliocene); 5 = oceanic spreading of Marsili bathyal plain
(ca. 1.87 - 1.67 Ma; ODP site 650, see *); 6 = <1.2 Ma volcanics (Quaternary). an = magmatics exhibiting alkaline
(intraplate, OIB) character, and Pliocene to Quaternary age. In Capraia island, Nefza area and Iblei mounts are
present also volcanics of late Miocene age. Abbreviations: A = Algeria, Ace = seamount Aceste, Anc= seamount
Anchise, Ca = Capraia island, Co = Corsica, E = Elba island, G = Gortani ridge (ODP site 655), Gi = Giglio island,
M-O = Montecatini V/C - Orciatico, Mag = seamount Magnaghi, MB = Marsili basin, Ne = Nefza area, P = oceanfloor peridotite (ODP site 651), Po = Ponza and Palmarola islands, Pr = Provence, S = Sardinia, Si = Sisco; T =
Tunisia, To = Tolfa, V = Vercelli seamount, VB = Vavilov basin, Ves = Vesuvius - Campi Flegrei, Vul = M.
Vulture. Dotted line shows the position of lithosphere-asthenosphere section of Fig. 7/B.
Figure 7. Schematic lithosphere-scale cross sections: A), from Provence (France) to the Ionian area (location in Fig.
3/B); the oceanic spreading of Burdigalian age (between ca. 20 and 16 Ma) produced the Sardinia-Provencal basin
(Sa-Pr; European plate); B), from Sardinia to the Vavilov - Marsili oceanic basins and the Ionian (location in Fig.
6). AM = asthenospheric mantle, LM = lithospheric mantle, MORB = Mid-Ocean-Ridge-Basalt magma source in
AM, ANOR = Anorogenic (intraplate, ocean-island-basalt) magma source in AM. It has here been assumed that the
past lithosphere thickness of the Alpine-Betic orogen was comparable to that of nowadays Alps. Emplacement of the
calc-alkaline magmas before start of WNW-directed subduction implies that the metasomatic modification of the
corresponding igneous sources has been produced by lithosphere shortening of Hercynian or Alpine age. Because
the orogenic accretion processes are repeated in time, Hercynian remnants are likely present in the metasomatized
bodies of Alpine-age, and Alpine remnants in the bodies of Apennine-age.
Start of WNW-directed subduction
The above mentioned space-time aspects indicate that the Burdigalian opening on one
side, and those of the late Miocene and late Pliocene on the other, are probably linked to clearly
distinct tectonic environment. This reconstruction considers that the WNW subduction was
commenced at ca. 16/15 Ma (Burdigalian-Langhian transition; Fig. 2/B), after the clearly distinct
episodes of post-orogenic rifting (Oligocene-Aquitanian) and seafloor spreading (Burdigalian).
The waning of allochthonous volcanoclastic deposits of the Apennines occurred possibly at the
nascence of WNW subduction of lithosphere belonging to the African plate under the retroverging portion of the Tyrrhenian OAA (see Supplementary Info S3). The embryonic slab went
with eruption of volcanics of less common type (comendites of SW Sardinia, European plate,
and lamproites of NE Corsica, the Tyrrhenian part of the OAA; Supplementary Dataset S4). The
slab origin may be useful for recognizing the early formation of the Maghrebid-Apennine thrust
belt.
Discussion
Overall, rift tectonism is either of “failed” (incomplete) or “mature” type: the former is
linked to continental lithosphere thinning typically characterized by horst-graben structure, the
latter reaches the stage of oceanic basin opening. In the west Mediterranean and surroundings
Tertiary-Quaternary rifting of “failed” type produced thinning and stretching of various regions
such as Valencia basin, Alboran Sea, Sicily Channel, Aegean Sea, Rheintal, Rhone Valley,
Limagne-Massif-Central-Bresse. “Mature” rift can be distinguished from aborted rift spatially or
temporally. A spatial distinction is found in the Tyrrhenian as late Miocene rift activity of
“failed” and “mature” type occurs respectively to the north and the south of the 41° parallel
lineation zone. In fact, modest extension (incomplete rift) accompanied the magmatism of
granitoid nature of the north Tyrrhenian seafloor (Fig. 6). On the other hand, strong extensional
deformation went with the Vavilov plain volcanism of MORB type (mature rift) to the south of
the lineation. Granitoid magmas are widespread in the north Tyrrhenian, whereas basalt
volcanism appears limited to the eastern rim of Vavilov plain (DSDP 373A; Fig. 4). Spatial
distinction is also manifest in the Mediterranean OAA during the Burdigalian. In fact, rifting of
“failed” and “mature” type in the absence of subduction occur respectively to the east (future
Tyrrhenian sea) and west (north Algerian basin) of the Catalan-Tunisian fracture zone. More in
the past, the Permo-Triassic “failed” rift of the southern Alps could have been associated with
the distant opening of the Permo-Triassic Tethys. Regarding the temporal distinction,
rift/spreading transition of the Mediterranean OAA occurred in Burdigalian, late-Miocene and
late Pliocene time.
Pre-Oligocene (> 33/32 Ma) lithosphere thickening above SE-subduction of European
lithosphere produced the Mediterranean-Tyrrhenian OAA. Structurally, the orogen was made of
fore- and retro-belt. WNW-directed subduction of African plate beneath the retro-belt
commenced, most likely, at the Burdigalian-Langhian transition (ca. 16/15 Ma) was favoured by
vergence similarity with the nascent Maghrebid-Apennines. The Oligo-Burdigalian stage of
rifting in concert with volcanism of the Tyrrhenian OAA was possibly akin to the post-Laramide
rifting and volcanism of the Basin and Range. Overall, intramontain lithosphere rupture and
volcanism of calc-alkaline nature produce fault-bounded horst, exposing crystallinemetamorphic and volcanic rocks, and alternating with grabens that contain thick deposits of
volcanoclastic and siliciclastic nature. Calc-alkaline volcanoclastic deposits of Oligocene –
Burdigalian age are found as allochthonous bodies in the Apennines in the absence of the
emission centres (see the Supplementary Info S3, and Dataset S5, S6). At the nascence of WNW
subduction and Apennine thrusting, the upper plate source area of the allochthonous
volcanoclastics was probably affected by inversion tectonics in which a compressional stage
follows the extension-dominated stage. The fate of the volcanoclastics could have been
determined by the significant change of tectonic mode of their sites of origin in the former
Tyrrhenian OAA. By the start of WNW subduction, inversion tectonics could initiate the downfaulting of the original horst volcanoes (past topographic highs) and the thrusting of the faultbounded grabens bearing volcanoclastic deposits (former lows). In the more orthodox concept of
West-Mediterranean-Tyrrhenian evolution, the persistent WNW subduction of the last 33/32 Ma
excludes horst-graben inversion. Also the thick siliciclastic graben successions of the Apennines
and the nonappearance of the past structural highs could be a consequence of inversion tectonics.
The connection of volcanism of calc-alkaline type far from subduction zone most probably
implies that igneous sources have been metasomatized by crustal material brought downwards
during clearly past lithosphere shortening and plate convergence. Overall, the geological
literature indicates that the temporal gap intervening between tectonic mode linked to
metasomatic modification and igneous activity of calc-alkaline type can be highly variable.
The study area may have had important geological connections with the Alps. The
compression tectonics of the Alps has been interrupted and supplanted by extension during the
Oligocene - early Miocene. The high geothermal gradient due to extension and necking caused
generation and uprise of calc-alkaline melts28, 29. By the end of early Miocene, igneous activity
and extension ceased and the orogenic accretion of the Alps resumed. The resumption of
lithosphere shortening in the Alps appears to be penecontemporaneous with the start of oceanic
opening of the West Mediterranean.
In conclusion, after the pre-Oligocene Alpine accretion linked to SE polarity two most
probable episodes of tectonic and magmatic activity are recognized. The Oligocene-Burdigalian
episode (ca. 33/32 - 16 Ma) saw rift activity in the absence of subduction. Calc-alkaline acidic
magmatism of the Oligocene-Aquitanian (ca. 33/32 - 20 Ma) was followed by volcanism of
bimodal, basic – acidic nature linked to oceanic basin formation of the Burdigalian (ca. 20 - 16
Ma). In the Langhian to Recent (ca. 16/15 - 0 Ma) episode, the tectonic and magmatic activity
was linked to subduction showing WNW-direction. Following the view of this work, the tectonic
setting of the Apennine Macigno Formation showing pre-Langhian age (> 16/15 Ma) was of
graben-type whereas the post-Burdigalian (< 16/15 Ma) Marnoso-Arenacea had setting of
foredeep-type. The supra-subduction formation of the Tyrrhenian bathyal plains of Vavilov and
Marsili is a four stage process. The short-lived late Miocene and late Pliocene stages are
characterized by strong spreading. Hyperextension deformation was accompanied by horizontal
accretion of the low-seated oceanic crust. The Pliocene (5.33 – 1.87 Ma) and Quaternary (1 Ma
to Recent) episodes were affected by weak spreading (Supplementary Info S2). Weak, localized
extension was accompanied by vertical accretion which produced high-standing basaltic
seamounts. MORB-type lavas (ODP655) created the modest elevation of 4.3 Ma old30 Gortani
ridge, NW of DSDP373 (Fig. 4). Afterwards, MORB volcanism migrated ESE, towards the
hinge zone. In the course of migration, from Gortani ridge to the axial volcanoes of Vavilov (<
2.4 Ma) and Marsili (< 0.8 Ma), crest elevation increased. Eventually, large magma input formed
the over-fed Marsili volcano, the last of the “sui generis” spreading axes of the Tyrrhenian.
Weak horizontal deformation is linked to ascent and emplacement of < 0.5 Ma old basalt melts
of alkaline type in the crest of Vavilov volcano11.
As the Tyrrhenian part of OAA was affected by the late Miocene strong oceanic
spreading, hyperextension occurred also in the adjacent Hercynian margin of Sardinia. By
contrast, the north Algerian oceanic opening and that of Sardinia-Provence were entirely located
respectively in the OAA and the Hercynian European lithosphere. In this view, it appears that the
tectonic mode linked to the Tyrrhenian continent-ocean transition could be diverse from that of
the Burdigalian opening. The space-time analysis indicates that calc-alkaline volcanism and
extension occur also in the absence of subduction.
Acknowledgements. F. Guerrera generously contributed to the review of the salient
characteristics of the allochthonous volcanic sedimentary rocks of the Apennine-Maghrebid
thrusts. I thank one anonymous reviewer and E. Bonatti for insightful suggestions which allowed
to improve the quality of the article. There has been helpful exchange of ideas with H. Bellon, C.
Doglioni, E. Gueguen, K. Kastens, M. Ligi, M. Lustrino, A. Malinverno, M. Mattioli, N.
d’Oraye, J.G. Sclater and N. Zitellini. The report of the Pieve Santo Stefano buried volcanic
body was obtained by courtesy of ENI/AGIP, Exploration division. The article is dedicated to the
memory of Mario Fornaseri, Michele Deriu, Renato Funiciello, Fabrizio Innocenti, Raimondo
Selli. It would never have been possible without Maria Pia.
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SUPPLEMENTARY MATERIAL
The supplementary numerical Tables S4, and S6 are obtainable via request to the author.
Supplementary - S1: Brief description of previous tectonic reconstructions
It is generally considered that calc-alkaline volcanism, oceanic spreading and bending of
the Maghrebid-Apennines belt were linked to roll-back of WNW-directed subduction of African
plate from early Oligocene to Recent. For the most part, the authors call for the arc environment
on the assumption that calc-alkaline magmas and oceanic opening probably require concomitant
slab retreat extending from the north Apennines to western Maghreb (see, e.g., Malinverno and
Ryan, 1986; Lonergan and White, 1997; Carminati et al., 1998a; Wilson and Bianchini, 1999;
Argnani and. Savelli, 1999; Maury et al., 2000; Cibin et al., 2001; Barruol and Granet, 2002;
Rosenbaum et al., 2002; Spakman and Wortel, 2004; Martin, 2006; Scrocca et al., 2005; Heymes
et al., 2008; Vignaroli et. al., 2008). In the subduction-controlled environment has been
considered the occurrence of: slab break-off (Carminati et al., 1998a, b; Benito et al., 1999;
Hoernle et al., 1999; Maury et al., 2000; Cavazza et al., 2004), slab tear (Patacca et al., 1990;
Marani and Trua, 2002; Faccenna et al., 2004, 2007; Chiarabba et al., 2008; Rosenbaum et al.,
2008), inversion of subduction polarity (see, e.g., Boccaletti et al., 1971; Rehault et al., 1984;
Doglioni et al., 1998, 2004; Gueguen et al., 1998; Peccerillo, 1999; Savelli, 2002, 2011), slab
roll-back without polarity inversion (Beccaluva et al., 1994; Argnani et al.,1995; Lonergan and
White, 1997), and delamination of subducted lithosphere (Serri et al., 1993; Hoernle et al.,
1999). Among the extension-controlled processes, various authors consider convective thinning
of lithospheric mantle and orogenic collapse (see, e.g., Doglioni, 1995; Turner et al., 1999;
Doblas et al., 2007). Doglioni (1992) and Keller et al. (1994) propose that the eastward mantle
flow is at the origin of back-arc extension and consecutive oceanic opening. Doglioni et alii
(1999a, b) suggest that mantle flow results in the contrasting modes of the steep and flat
subduction zones. The “two subductions” concept considers that flat E-subduction zones are
associated to uplifting mountains (e.g., the western Alps) and steep W-subduction zones to small
elevation of the chain (the Apennines).
Lavecchia and Stoppa (1990, 1996) and Bell et alii (2006) believe that east-dipping
detachment faults of the Sardinia/Tyrrhenian region and volcanic activity associated with
eruption of carbonatite rocks and deep-seated CO2 emission of the Apennine region took place in
response to the ascent of intra-continental plume. Diverse, but not mutually exclusive processes,
occurred in the western passive and the eastern active margin (Kastens et al., 1988; Keller et al.,
1994; Sartori et al., 2004). While the passive continental Corsica-Sardinian margin is thinned
and stretched by detachment faults, back-arc extension and arc volcanism migrate eastwards.
This reconstruction might recall the idea of Tatsumi et alii (1990) that asthenosphere injection
into the mantle wedge forced slab steepening and back-arc extension. Some authors (Turner et
al., 1999; Doblas et al., 2007) consider that the post-collision Betic-Alboran magmatism was a
consequence of convective removal of lithospheric mantle and lower crust in the absence of
subduction. Local comenditic rocks from Sardinia and lamproitic rocks from Alpine Corsica are
thought to reflect a tectonic environment of continental extension rather than subduction (Morra
et al., 1994; Prelevic et al., 2007). Mantovani et alii (2002) and Viti et alii (2009) consider that
Africa-Europe plate motions drove wedge extrusion and formation of the trench-arc-back-arc
sequence.
The slab beneath the Gibraltar arc is regarded as the counterpart of the Calabrian arc at the
eastern termination of the WNW subduction beneath the Maghrebid-Apennines belt (Lonergan
and White, 1997; Gutscher et al., 2002; Faccenna et al., 2004; Doblas et al., 2007). In this view,
the former arc migrated to the west and the latter to the east. It has been proposed that the
Sardinia calc-alkaline magmas originate from igneous sources which were metasomatized during
plate convergence of Hercynian age (Rehault et al., 1984; Savelli, 2002, 2005). Figure 2 shows
that the pre-Oligocene (> 33.9 Ma; International Stratigraphic Chart, 2009) NW-verging front
of shortening due to collision of the European and African plates was accompanied by formation
of SE-verging back-thrusts which will be the hinge zone of future WNW subduction of African
lithosphere beneath the Maghrebid-Apennines belt. The similar SE-vergence of the inherited
back-thrusts of Mediterranean OAA and the thrusts of the Apennines (Keller et al., 1994;
Doglioni, 1998; Gueguen et al., 1998; Scrocca et al., 2005) causes difficulties in determining
initiation of the WNW subduction. Some authors (Carminati et al., 1998b; Cibin et al., 2001;
Faccenna et al., 2004; Rosenbaum et al., 2008; Conticelli et al., 2009) propose that subduction
started in early Oligocene (ca. 34/30 Ma), and some others (Gueguen et al., 1997, 1998;
Guerrera et al., 1993, 2004, 2005) in late Oligocene (ca. 25 - 23 Ma or late Oligocene-
Aquitanian time, ca. 25 – 20 Ma). Subduction beneath the northern part of the
Tyrrhenian/Apennine system initiated probably not earlier than ca. 20 – 14 Ma (early-middle
Miocene; Savelli 2000; Guerrera et al., 2012). Maury et alii (2000) propose 16 Ma for slab
break-off and commencement of calc-alkaline magmatism along the Maghreb margin. Given
spreading rate of ca. 5 cm/a and slab depth of ca. 500 km beneath the Tyrrhenian basin,
Francalanci and Manetti (1994) consider subduction duration of 10 Ma.
Supplementary - S2: Periods of weak extension and volcanism not coeval with the oceanic openings
Oligocene - Aquitanian (ca. 33/32 - 20 Ma)
European Plate
East of the Catalan-Tunisian fracture zone, the island of Sardinia saw intense rift activity. In the
west Sardinia graben (Fig. 3/A, main text), lava flows and domes - often intruded by dikes and
autobrecciated - are accompanied by ignimbrites, pyroclastics and pillow basalts. A series of individual
volcanic complexes is the typical product of Sardinia volcanism. Rock composition varies from basalt to
andesite dacite rhyolite, the serial type from tholeiitic and medium-K calc-alkaline to high-K calcalkaline/shoshonitic, and the age from ca. 29 to 12 Ma (Deriu, 1962; Coulon et al., 1974; Coulon and
Dupuy, 1975; Savelli et al., 1979; Dostal et al., 1982; Beccaluva et al., 1994; Argnani et al., 1995; Conte,
1997; Lustrino et al., 2004; Gattacceca et al., 2007). Andesitic lavas and ignimbritic rhyolites are the
prevailing lithotype of the island (Tab. 1). The Sarroch volcanic complex (site 5; Fig.3/A) is made of
basalts, basaltic andesites and andesites (samples SH-32, SH-55, SH-48 of Tab.1; Conte, 1997). Basalts
and andesites crop out in Cixerri (site n. 6; Savelli et al., 1979); microdiorites, rhyolitic ignombrites,
dacites and andesites in Alghero-Oniferi (site 7; Bellon, 1981, Gattacceca et al., 2007); basalts, basaltic
andesites and andesites in Bosano-Logudoro-Capo Marargiu (site 8). In Provence are present andesites,
dacites and subvolcanic microdiorites (sites 3, 4). Andesite and dacite are lava flows (samples 77S4F,
Est96-2, PR4), gabbro xenolith is present in dacite lava (sample PR7a from Esterel area), and andesite
clasts (in the Villeneuve-Loubet conglomerate near Nice (sample PR2) (see note at foot of a previous
page).
In Valencia basin, to the west of Catalan-Tunisian fracture zone offshore exploration wells
sampled early Miocene sediments bearing pyroclastics of andesitic to rhyolitic composition (site 1; Marti’
et al., 1992). The DSDP hole 123 drilled pyroclastics (site 2; samples n. 2/6a and 2/6b) of dacitic and
rhyolitic composition which yielded K/Ar dates of 24.4, 21.9 and 20.8 Ma (Ryan et al., 1972).
Mediterranean Orogen of Alpine age
West of the Catalan-Tunisian fracture zone, ca. 24.8 to 20.8 Ma old leuco-granite clasts are
present in the Betic area (site 10; Bellon et al., 1983). Rhyolitic pyroclastics (22-21 Ma, site 9) and
volcanogenic turbidites show Aquitanian-Burdigalian age (Algeciras, site 2 - in italics, Fig. 3). In the
Algerian Maghreb, the granodiorite from Bejaja-Amizour (Great Kabylia) and the granitoid from Beni
Toufout (Little Kabylia) show late Oligocene (24.4 Ma; site 11) and Aquitanian age (22 Ma; site 12),
respectively (Bellon, 1981). These intrusions are slightly younger than the peak thermo-metamorphism of
the Kabylia crystalline basement which is dated at ca. 25 Ma (Monie’ et al., 1995).
Langhian - Tortonian (ca. 16 - 7.5 Ma)
European Plate
Ignimbritic rhyodacites and andesites (sites 42, 43), comendites (site 44), and andesites (near to
s. 6) crop out in northern, southwestern and southern Sardinia respectively. Shoshonites are found in the
Sardinian offshore (site 45; sample Sar1.03; Mascle et al., 2001) and andesites in the Ligurian offshore
(Rollet et al., 2002; p. -17).
Mediterranean Orogen of Alpine age
Alboran region West of the Catalan-Tunisian fracture zone, magmas erupted mostly along
lineation zones trending SW-NE (Hernandez et al., 1987; Duggen et al., 2004), W-E (Torres Roldan et
al., 1986) and WSW-ENE (Hoernle et al., 1999). The SW-NE lineation (Trans-Alboran fracture zone)
extends from the Trois Fourches promontory of Morocco to the Betic area of Cabo de Gata (sites 30, 26,
27). Along such lineation ODP Hole 977 (site 15) recovered gravel pebbles which have dacite, basalt
(sample 7523) and rhyolite composition (sample 7521) and ages between 12.1 and 9.3 Ma (Hoernle et al.,
1999; Duggen et al., 2004). Pebbles from Hole 978 (near to s. 15) exhibit composition from basalt to
rhyolite and serial type ranging from tholeiite to shoshonite (Hoernle et al., 1999). The pebbles below
early Pliocene sediment of ODP Holes 977 and 978 probably derived from the widespread late Miocene
erosion process. At the Yusuf ridge is present andesite (10.7 Ma; sample CYA 5-6) and at Mansour
seamount basaltic andesite (8.7 Ma: sample POS III-D-1; Duggen et al., 2004). Sea-floor rhyolites (9.49.3 Ma; site 26; sample CYA3-11) accompanied by subaerial tholeiitic lavas and andesitic pyroclastics
are present along the lineation trending WSW-ENE of the submerged ridge near to the Alboran island
(Duggen et al., 2004; Gill et al., 2004).
Betic region. Volcanic activity was intense in the Betic region between ca. 12 and 9 Ma. The 8.9,
8.8 Ma old basalt and latite of Mazarron (site 28) show high-K calc-alkaline and shoshonitic type,
respectively (samples B302 and MAZ8; Benito et al., 1999; Turner et al., 1999). Granodiorites, diorites,
rhyolites, dacites, andesites, basaltic andesites and basalts erupted in the time span from ca. 15 to 8-7 Ma
in the Cabo de Gata region (site 27; Bellon et al., 1983; Di Battistini et al., 1987; Hernandez et al., 1987;
Turner et al., 1999). The ca. 1000 m thick CA lavas of Cabo de Gata exhibit K/Ar age between 15.2 and
7.9 Ma (Bellon et al., 1983). Di Battistini et alii (1987) report that 12.1 to 9.2 Ma old amphibole-bearing
andesites dacites and rhyolites overlie pyroxene-bearing andesites (8.7 to 7.5 Ma; samples CG200 599-9,
Sp317, Sp333, Sp253).
Morocco Rif. Pyroclastics and block lavas of basaltic-andesitic and andesitic, medium-K calcalkaline composition from Ras Tarf (site 29; sample 116-72) yielded K/Ar dates of 15, 13.1, 12.1 Ma
(Bellon, 1981; El Azzouzi et al., 1999; Maury et al., 2000). More to the east at the southern end of
Transalboran shear zone, rhyolites crop out in the Trois Fourches promontory (9.8 Ma; site 30; sample
G44; El Bakkali et al., 1998). Rocks of high-K calc-alkaline, granodioritic and andesitic composition
(samples G8, G1, G15) from the adjacent volcano/plutonic complex of Gourougou show ages of 8.1, 7.9,
7.7 Ma respectively (El Bakkali et al., 1998; El Azouzi et al., 1999). In addition, the Gourougou area is
characterized by eruption of shoshonitic rocks showing composition from basalt to trachyte (samples
G47, G74) and K/Ar age older than the Tortonian (between ca. 7.0 and 5.4 Ma).
Algerian Maghreb. In the Great Kabilya region of Algeria (site 20) the pre-Langhian magmatics
were followed by emplacement of latite dikes with age of 12.4 Ma. Louni Hacini et al. (1995) report K/Ar
age of 15 Ma for the rhyolitic dome of Sahel of Oran (site 31) which was followed by high-K calcalkaline andesites and dacites with K/Ar ages between 11.7 and 7.2 Ma (dike sample OR10), and 7.5 Ma
old latites (site 32; latite dome of M’ Sirda; sample ORbd1). Rhyolitic dikes cutting the Thenia
granodiorite of Burdigalian age (site 10a; sample T 36) have been dated 14-12 Ma. Bellon (1981)
indicates 16-15 Ma for the rhyolites and rhyodacites from Menacer area (site 36), Maury et alii (2000) 1311 Ma for K-rich granites from the Cherchel area (site 34) and Belanteur et alii. (1995) 11.8 Ma for
basaltic andesite from the area of Dellys (near to site 19; sample DLBO). According to Bellon (1981)
andesites and shoshonites of the Cherchel area (site 35) gave K/Ar ages of 13.1/12.4 and 9.0 Ma
(respectively), and andesites of Kef Hahouner (site 39) 10.9/9.3 Ma. Ca. 15.3 Ma cordierite-bearing
granitoids of Djebel Filfill (Little Kabylia; site n. 37; sample II-6) are of K-rich type. Granite and diorite
crop out in Annaba (K/Ar age of 15.9 and 15.8 Ma; site 38, near to the western margin of Little Kabylia;
Bellon, 1981); gabbros in Cap de Fer-Annaba (sample VPE-271) and basalts in Cap Djinet (13.7 and 12.2
Ma; site 36; samples Dj2, Dj1; Fourcade et al., 2001).
Tunisia. The ca. 13 Ma old cordierite-bearing granitoid intrusion of Oued Belif (site 40; Nefza
region) was followed by eruption of dacites and rhyodacites between ca. 12.9 - 8.2 Ma; cordieritebearing, K-rich granitoids and rhyolites crop out in the island of La Galite (ca. 14.2 and 10 Ma; site n. 41;
Bellon, 1981; Maury et al., 2000).
NE Corsica. East of the Catalan-Tunisian fracture zone, at Sisco crops out a dike body showing
lamproitic composition and K/Ar age of ca. 15.0 Ma (site n. 46; Civetta et al., 1978; Savelli, 2000;
Conticelli et al., 2007, 2009). This rock has high contents of compatible (K, Rb, Th, Sr, Ba), incompatible
(Mg, Cr, Ni) and light rare earth elements, as well as high Sr (0.71228) and low Nd (0.51215/6) initial
isotopic ratios (Tab. 1).
Pliocene (ca. 5.4 - 1.8 Ma; Tyrrhenian area)
Major sources of detailed documentation for the Pliocene and Quaternary magmatic episodes in
and around the Tyrrhenian sea (Figs. 6, 7) are found in Selli et alii (1977), Savelli (1984, 2002), Serri et
alii (1993), Faggioni et alii (1995), Argnani and Savelli, (1999, 2001), Peccerillo (1999), Sartori et alii
(2004). After the calc-alkaline volcanic cycle of Oligocene - Langhian age and ca. 7 Ma of magmatic
quiescence, Sardinia was affected by basaltic volcanism showing alkaline nature and age from ca. 5.4 to
1.8 Ma (Beccaluva et al., 1977; Savelli, 2002; Lustrino et al., 2004; and references therein). Pliocene
basalt volcanism is widespread in the Tyrrhenian seafloor. Alkaline basalts (3.0-2.7 Ma) occur in
Magnaghi seamount, MORB-type lavas in the Gortani ridge (4.1 Ma; ODP site 655) and calc-alkaline
basalts (2.6 Ma) above ultramafic rock of ODP site 651A. The age of Vavilov volcano is < 2.4 Ma if its
magnetic anomaly belongs to the Matuyama chron. Figure 7 (main text) shows that Pliocene magmatics
are present to the west of the Tuscan-Roman-Campanian area of abundant Quaternary volcanism. In the
Aceste and Anchise seamounts are found volcanics respectively of alkaline and calc-alkaline type.
Quaternary (< 1.2 Ma – Recent; Tyrrhenian area)
Calc-alkaline basalt volcanism (< 0.8 Ma; Selli et al., 1977; Savelli and Gasparotto, 1994;
Faggioni et al., 1995; Marani and Trua, 2002) and high angle faulting produce vertical accretion of the
large axial seamount Marsili as fast subsidence affects the seamount itself and the contour bathyal plain.
Such Quaternary vertical tectonic mode replaces the low-angle detachment faulting of fast horizontal
spreading and basalt eruption at ODP site 650 of the late Pliocene. Cocchi et al. (2009) point out that
Marsili basin evolves from pure lateral spreading to a superinflated seamount. In the part of the basin to
the east of ODP site 650, the full spreading rate decreases from 3.1 cm/a since the post Olduvai part of the
Matuyama (< 1.67 Ma) to 1.8 cm/a since the Brunhes chron (< 0.8 Ma) and the start of the vertical growth
of the 3000 m high seafloor volcano.
In the Marsili basin, if the ca. 2 Ma age of opening for 110 km in WNW-ESE direction is true the
full spreading rate was ca. 5.8 cm/a. Nicolosi et al. (2006), indicate spreading rate of 19 cm/a for the
short-lived Olduvai chron. As the Marsili spreading should be restricted due to nearness of the continental
crust, the large above-mentioned rate can be an overestimation. The MORB-like basalt injection at ODP
site 650 represents initial oceanic spreading of localized punctiform nature in ambient shallow-water.
Such short-lived magmatic emplacement can accompany strong tectonic extension. To the west of the
ODP site 650, strong tectonic spreading could affect - hypothetically - the amagmatic thinned continental
lithosphere of the bathymetric saddle which separates the bathyal plain of Vavilov from that of Marsili. In
the Marsili basin as in the older Vavilov, lateral oceanic accretion evolves to vertical growth producing
basaltic seamounts to the detriment of the opening rate. The landlocked Marsili volcano grew up in a
more eastward position with respect to the early localized shallow-water spreading of the site ODP 650,
whereas the axial volcanoes of the Vavilov plain develop in a more westward position with respect to the
MORB-type basalts of the site DSDP 373A. In the Marsili basin, the transition from pure horizontal
magma-poor spreading to strong volcanism and vertical accretion of Marsili seamount can be cause or
effect, or both cause and effect, of strong slab instability. This geochronological recostruction of the
Tyrrhenian opening might show that the Gortani ridge and the seamounts of Vavilov and Marsili can
represent the evolution from pure lateral to vertical oceanic accretion with formation of short “sui
generis” spreading axis.
During the last 1 Ma, abundant calc-alkaline volcanism affected the Tyrrhenian margin from the
Aeolian islands and Vesuvius to the “Roman Province” and southern Tuscany (Main text Fig. 7). The
figure shows also that alkaline-olivine basalts are present in the top of Vavilov seamount showing < 0.5
Ma (Selli et al., 1977; Robin et al., 1987; Faggioni et al., 1995), and in NW Sardinia (between ca. 0.8 and
0.2 Ma; Savelli, 1984, 2002). Alkaline contamination of Quaternary peri-Tyrrhenian calc-alkaline
volcanics is described by various authors (see, e.g., Ellam et al., 1989; Serri et al., 1993; Francalanci and
Manetti, 1994; Argnani and Savelli, 1999, 2001; Peccerillo, 1999; Gasperini et al. 2002; Cadoux et al.,
2005; De Astis et al., 2006; Rosenbaum et al., 2008; Trua et al., 2004, 2010).
Supplementary – S3: Volcanogenic allochthons of the Apennines
Volcanoclastic sediments
The pervasive presence of allochthonous volcanoclastics in the absence of the corresponding
emission bodies has attracted the attention of various authors (Mezzetti et al., 1964; Riviere et al.,1977;
Borsetti et al., 1984; Critelli et al., 1990; Guerrera et al., 1993, 1998, 2005; Amorosi et al., 1994, 1995;
Campos Venuti et al., 1997; Cibin et al., 1998, 2001; Mattioli et al., 2002). The rocks show age from the
Oligocene to Burdigalian (Langhian), and calc-alkaline nature (Table 2). In Table 3 are listed the
literature geochemistry data of the samples cited in this chapter and Table 2. The dilemma whether the
source area was originally located in the Tyrrhenian OAA, to the east of the Catalan-Tunisian fracture
zone, is object of debate. The provenance area and the tectonics causing disappearance of the primary
emission bodies (the “lost” volcanoes) preservation of the volcanoclastics are related issues which are
going to be considered more below. On the whole, volcanogenic sediments from the Apennines were
associated to erosion, reworking and basinal slumping (mass-flow) of pyroclastic material and lava and
mineral grains. Volcanoclastic sandstones with abundant glass and mineral fragments, tuffaceous and
volcanolithic sandstones reflect sedimentation by turbidity currents and mixing with the terrigenous
derive mostly from erosion of crystalline-metamorphic basement. Fine-grained ash layers of pyroclastic
fall which are often altered to clay minerals are also present. Some authors proposed the volcanoclastics
derive from the coeval volcanism of western Sardinia (Tab. 3). Yet, due to its remote location the island is
not a likely site of origin; the turbidite and gravity flow characteristics, coarse grain size (from sand to
gravel and pebble) and thickness of volcanogenic sediments indicate a nearness of eruption and
deposition sites (Critelli et al., 1990; Campos-Venuti et al., 1997; De Capoa et al., 2002).
Early Oligocene.
Early Oligocene volcanoclastic beds are widespread in the northern Apennines (Tateo, 1993;
Cibin et al., 1998, 2001; Mattioli et al., 2002). The Ranzano formation (l.s., sites 23, 24, 25; Fig. 3, main
text) is made up mainly of sands containing plagioclase grains of andesine-labradorite composition
associated with glass shards and grains of amphibole, pyroxene, biotite and opaques which indicate
primary composition of dacitic-andesitic type (samples 34D, 94, 128 of Tab. 2; Cibin et al., 1998). The
detritus is present in “pure” beds which contain around 70-80 % volcanic material and “mixed” beds
where volcanic and non-volcanic grains are present in variable amount. Pebble-sized clasts from the
Aveto-Petrignacola formation (sites 23, 24) yielded amphibole Ar/Ar ages of 29.8-29 Ma which match
the early Oligocene biostratigraphic evidence (Mattioli et al., 2002). Clast composition varies from basalt
and basaltic andesite to andesite, dacite and rhyolite (twelve samples; from MM2 to MM114). The lavas
exhibit serial type from low- to medium- and high-K calc-alkaline, and the rhyolitic ignimbrites
shoshonitic type. The volcanic sand beds of Reitano-Tusa and Stilo-Capo d’Orlando turbiditic
successions (Calabro-Peloritani arc, sites n. 13, 14) show rhyolitic K-alkaline nature and early Oligocene
age (Faugeres et al., 1992; Balogh et al., 2001; Baruffini et al., 2002).
Oligocene - early Miocene.
Volcanogenic sands showing rhyolitic-rhyodacitic composition are found in the southern
Apennines (sites 15, 16, 17; Critelli et al., 1990; Guerrera et al., 1998, 2005; De Capoa et al., 2002).
Volcanic ash layers of the northern Apennines (Contignaco, Mongardino and Calderino; sites n. 25-26)
are associated with early Miocene clays (Mezzetti et al., 1964; Cibin et al., 2001). Sometimes, the
volcanic ashes were modified and altered to various extent: the alteration degree was studied by Mezzetti
et alii (1964). The geochemistry diversity between separated shards and whole rock indicates the
alteration of Calderino pyroclastics (sample 4). The alteration produced decrease of silica and alkalies,
and CaO increase. Conversely, the Mongardino glass (sample 5) was only slightly altered into clay
material. In volcanic arenites of the early Miocene San Mauro/Pollica formation (southern Apennines;
Crisci et al., 1988; Critelli and Le Pera, 1990) are present lava clasts of rhyodacitic - rhyolitic
composition (sites 19-20; samples S2, S3). The arenites contain fragments of plagioclase, quartz, sanidine
and biotite; fresh plagioclase with anorthite content of 15 – 40 % shows embayed rims of allotriomorphic
quartz.
Late Aquitanian – Burdigalian (Langhian)
Figure 3 shows that volcanogenic deposits of Late Aquitanian – Burdigalian age are scarce in Rif
and Betics (Maate et al., 1995; Guerrera et al., 1998) and abundant in the Apennines. Turbidite
sediments bearing fragments of rhyodacitic-andesitic rocks crop out in the Betic region (sites 1, 3
– in italics; Guerrera et al. 1998, 2005). Maate et al. (1995) report fragments of basalt and
andesite lava in turbidites from western Maghreb (sites 4, 5, 6). The “Bisciaro” formation
volcanoclastics of the north Apennine Umbria-Marche region (sites 27, 29) yielded K/Ar ages between
ca. 22.3 and 17.1 Ma (Balogh et al., 1993). Rhyolitic-rhyodacitic glass shards and plagioclase
phenocrysts are present in the “Bisciaro” type deposits of Montebello and Fossombrone (samples 3, B6/1,
B8/7; B6(2), B8(1), 80, 80 mc; Guerrera et al., 1986; Coccioni et al., 1988). Delle Rose et al. (1994a, b)
reported the occurrence of rhyolitic glass of shoshonitic type among the volcanoclastic layers of the
Vicchio marls (site 29). Vicchio glass shards are accompanied by altered andesite clasts and sand-sized
grains of fresh andesine, plagioclase, biotite. Conglomerate beds with pebble-size lava clasts of rhyolitic rhyodacitic composition (samples A II, C 13A, B 12), and volcanic arenites are present in the
Gorgoglione flysch (site 22; Le Pera and Ventura, 1994). The clasts contain phenocrysts of plagioclase
(An 5-30), K-feldspar, quartz and biotite. Langhian. Pyroclastics of Langhian biostratigraphic age which
bear rhyolitic glass shards and biotite crystals (site 11; samples 7, 14) crop out in central Sicily (Spadea
and Carmisciano; 1974).
The buried volcano of Pieve S. Stefano
In the northern Apennines (site 13a) the oil drilling of Pieve S. Stefano recovered calc-alkaline
volcanics (ENI/AGIP report - San Donato Milanese, June 1984; Anelli et al., 1994). The 850 m thick
igneous sequence ends at drilling depth of ca. 4900 m. The core samples m 3870-1 and -2 consist
respectively of pyroxene-bearing andesite lava and andesite pyroclastics. The presence of “brownred”colour surfaces likely suggests not less than ten eruptive events. The volcanic sequence was
interrupted by two large anhydrite slivers belonging to the Triassic Burano formation. The evaporitic
layers, up to one hundred meter thick were probably crucial for the strong tectonic displacement of this
igneous sequence. Pervasive alteration produced the replacement of primary mineralogy with
hydrothermal minerals. The increase with depth of epidote content and other hydrothermal alteration
products of the deep-seated Pieve S. Stefano volcano supports the idea that the original eruptive sequence
might have been preserved. Three samples of decalcified andesite grains from core interval 3864 – 3872
m yield radiogenic 40Ar contents of (1.333, 1.179, 1.012) x 10-3 mm3/gram. Apparent ages of 33.8, 30.0,
25.7 Ma are obtained by K2O content of 1.21 %. Precisely repeated datings are not to be expected from
the altered rocks of Pieve S. Stefano. If the average date of 29.8 Ma is a true date, it indicates the
approximate timing of alteration rather than that of eruption.
Start of WNW-directed subduction and the “lost volcanoes”.
Overall, postorogenic lithosphere rupture and volcanism of calc-alkaline nature produce
alternance of fault-bounded horst, exposing crystalline-metamorphic and volcanic rocks, and grabens that
contain thick deposits of volcanoclastic and siliciclastic nature (Stewart, 1978; Hawkesworth et al., 1995;
Hooper et al., 1995). Calc-alkaline volcanoclastic deposits of Oligocene – Burdigalian age are found as
allochthonous bodies in the Apennines in the absence of volcanic emission centres (Fig. 3). This
geotectonic reconstruction considers that, at the nascence of WNW subduction and thrusting beneath the
Apennines (ca. 16/15 Ma), the submerged Tyrrhenian OAA, source area of the allochthonous
volcanoclastics was probably affected by commencement of inversion tectonics in which compression
follows the extension-dominated phase. The fate of the volcanoclastics could have been determined by a
significant change of tectonic mode in their former sites of origin. By the start of WNW subduction,
inversion tectonics could initiate the down-faulting of the original horst volcanoes (past topographic
highs) and the thrusting of the fault-bounded grabens bearing volcanoclastic deposits (former lows).
Rupture of the original upper plate horst-graben architecture probably initiated gradual downdrag and
upthrust motions which were at the origin of the loss of the original topographic highs (volcanic horsts)
and preservation of the lows (fault-bounded grabens bearing volcanoclastic deposits). In the more
orthodox concept of West-Mediterranean-Tyrrhenian evolution, the persistent WNW subduction of the
last 33/32 Ma excludes horst-graben inversion in which a contractional phase follows the extensional
phase.
Supplementary –Table S4: Table of revisited geochemistry and age data of calc-alkaline volcanics
showing Oligocene to Langhian/Tortonian age (west Mediterranean region); major oxides (weight %) and
trace elements (ppm). European plate; data source: 1) Ryan et al., 1972; 2) Civetta et al., 1978; 3)
courtesy of H. Bellon; 4) Savelli et al., 1979; 5) Bellon, 1981; 6) Montigny et al., 1981; 7) Marti' et al.,
1992; 8) Beccaluva et al., 1994; 9) Morra et al., 1994; 10) Argnani et al., 1995; 11) Conti, 1997; 12)
Morra et al., 1997; 13) Rossi et al., 1998; 14) Mattioli et al., 2000; 15) Downes et al., 2001; 16) Mascle et
al., 2001; 17) Ottaviani et al., 2001; 18) Franciosi et al., 2003; 19) Conticelli et al., 2007; 20) Conticelli et
al., 2009. Alboran-Betic segment of OAA; data source: 21) Torres Roldan et al., 1986; 22) Di Battistini et
al., 1987; 23) Benito et al., 1999; 24) Hoernle et al., 1999; 25) Turner et al., 1999; 26) Duggen et al.,
2004; 27) Gill et al., 2004. African segment of OAA; data source: 5) Bellon, 1981; 28) Belanteur et.,
1995; 29) Louni-Hacini etal., 1995; 30) El Bakkali et al., 1998; 31) El Azzouzi et al., 1999; 32) Fourcade
et al 2001; 33) Maury et al., 2000. Serial affinity: hK-CA = high potassic calc-alkaline; HAB = high
alumina basalt; HMB = high magnesium basalt; mK-CA = medium potassic calc-alkaline. OAA =
(Mediterranean) orogen of Alpine age. Geological age: Ol-Aq = Oligocene – Aquitanian (33/32-20 Ma);
Burd = Burdigalian (20-16 Ma); Bu/La = Burdigalian/Langhian transition (16-14 Ma); La - L. Mio =
Langhian - late Miocene (15-8 Ma).
Table S4. Location
Site, Fig. 3 Rock type
Note
Ser. affinity Sample
Age Data Wt.% SiO2
TiO2 Al2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O5
1
dacite
pyroclastic mK-CA
DSDP/
Ol-Aq
source
1
68,17
0,23 12,75
2,75
Valencia basin
1
rhyolite
pyroclastic
/123/2/6
Ol-Aq
1
70,47
0,24 12,37
1,99
Mallorca isl.
Provence, Esterel
"; Esterel
"; Agay
" ; Esterel
" , near Nice
18
3
3
3
3
4
rhyolite
andesite
dacite
dacite
gabbro
andesite
PO-5
77S4F
Est 96-2
PR4
PR7a
PR2
Burd
Ol-Aq
Ol-Aq
Ol-Aq
Ol-Aq
Ol-Aq
7
3; 5
3; 5
8
8
5; 8
71,00
61,60
63,00
64,67
46,59
58,80
0,21
0,39
0,43
0,44
2,13
0,96
12,08
18,20
18,00
17,56
16,68
19,16
0,47
4,45
4,25
0,50
1,61
0,72
18,48
18,05
17,99
20,18
16,84
16,06
14,39
17,90
15,21
14,1
15,26
17,14
15,19
16,55
16,29
18,37
14,9
14,47
11,80
17,94
14,53
18,45
10,8
4,18
2,47
2,61
1,21
7,88
5,30
10,49
1,49
9,76
10,35
9,51
1,16
10,43
11,40
0,92
0,84
4,10
3,04
4,39
2,17
European plate
Valencia basin
5
Sardinia; Sarroch
"; Sarroch
5
"; Sarroch
5
"; Bosano
8
"; Arcuentu
21
"; Arcuentu
21
"; Arcuentu
21
"; Arcuentu
21
"; Arcuentu
21
"; Villanovaforru
21
"; Villanovaforru
21
"; Marmilla
21
"; Montresta
21a
"; Montresta
21a
"; Anglona
22
"; Anglona
22
"; Anglona
22
Sulcis
22b
S. Antioco
44
"; SE offshore
45
23
Corsica; Balistra
"; SW offshore
24
Alpine Corsica Sisco
46
Alboran-Betic segment of OAA
Alboran region
ODP site 977
15
Alb. ridge
26
Alb. Island
"
Yusuf ridge
26
Mansour smt
"
ODP site 977
"
"
"
Betic region
Malaga
14
Malaga
Malaga
Malaga
Malaga
Malaga
14
Malaga
Mar Menor
17
Mazarron
28
Mazarron
Cabo de Gata
27
Cabo de Gata
Cabo de Gata
Cabo de Gata
African segment of OAA
Morocco, Rif
Ras Tarf
29
Trois Forches
30
Gourougou
close to
s. 30
Gourougou
Gourougou
Gourougou
Gourougou
Algeria
Sahel d'Oran
31
M'Sirda
32
Middle Tafta
33
Dellys
19
Dellys
Cap Djinet
36
Cap Djinet
"
Thenia
10a
Thenia
10a
Bejaia-Amizour
11
Bejaia-Amizour
11
SE of Amizour
11
Cap Bougaroun
12
12
"
"
12
"
12
Djebel Filfilla
32
Cap de Fer
38
"
38
Tunisia
41
La Galite isl
subvolcanic mK-CA
mK-CA
xenolith in dacite
lava clast
mK-CA
0,62 0,16 2,79
0,76 0,16 2,48
1,20 0,15 0,66
1,1
0,3 0,83
1,47 0,17 0,68
2,88 0,12 1,40
0,58 0,09 0,72
0,80 0,30 1,99
0,54 0,09 1,09
1,2 0,21 1,46
1
0,2 1,15
0,3 0,18 2,98
0,5 0,26 0,32
0,90 0,28 2,66
3,1 0,21 3,77
3,7 0,28 1,71
3,7
0,1
3,2
5,14 0,08 0,66
4,82 0,04 0,55
5,7 0,13 3,47
3,3
4,05 0,20 14,5
11 0,67 2,09
99,99
100,00
100,01
101,5
100,89
100,32
99,24
101,17
100,00
98,98
99,61
100,2
100,00
100,00
102,3
101,3
99,9
100,00
100,01
99,12
2.25
2.09
8.86
8.06
8.40
1.76
7.85
51,65 0,85
55,51 0,65
60,19 0,61
53,5 0,84
56,45 0,85
62,64 0,78
50,52 0,57
50,58 1,03
51,11 0,75
49,5 1,57
47,1 1,71
52,1 0,76
47,4 0,79
47,5 0,91
61,6 0,74
58,4 0,78
65,1
0,5
70,17 0,43
72,10 0,32
60,3 0,31
73,3
41,00 0,49
58,5 2,27
granite
rhyolite
bas. andesite
andesite
bas. andesite
rhyolite
basalt
7646
CYA3-11
2002
CYA 5-6
POS III-D-1
7521
7523
Burd
La-L. Mio
La-L. Mio
La-L. Mio
La-L. Mio
La-L. Mio
La-L. Mio
24; 26
27; 26
27
26
26
24; 26
24; 26
70,5
68,44
55,5
60,20
51,50
72,9
49,9
0,24
0,23
0,54
0,65
0,87
0,23
0,77
15,13
14,73
16,84
15,30
20,10
14,17
18,29
26
26
25
21
21
26
26
26
25
23
26
22
22
22
54,9
52,8
53,2
50,9
55,8
74,0
53,1
60,90
52
64,2
57,2
54,7
62,1
65,4
0,47
0,68
0,83
0,48
0,76
0,11
0,47
0,64
1,75
0,63
0,63
0,73
0,63
0,55
16,60 t. 5.88
16,70 t. 7.60
15,74 t. 9.62
15,53
2,07
15,62
1,43
14,4 t. 1.09
16,50 t. 5.54
15,70 t. 5.42
12,80 t. 14.50
16,22
0,81
15,80 t. 7.47
18,25
4,49
17,76
2,51
15,86
2,22
bas. andesite
dike
tholeiite
basalt
"
tholeiite
basalt
"
tholeiite
basalt
"
tholeiite
bas. andesite
"
tholeiite
granite
"
bas. andesite
"
dacite,
cordierite bear.
basalt
mK-CA
latite
shoshonite
andesite
breccia
mK-CA
bas. andesite pyroxene be mK-CA
andesite
amphibole b hK-CA
dacite
hK-CA
AM240699CB230699M2
IB 18
IB 44
MI22; 0699FG22; 0599-2
MM2703
B302
MAZ 8
CG200; 599
Sp317
Sp333
Sp253
andesite
rhyolite
granodiorite
andesite
andesite
shoshonite
absarokite
mK-CA
hK-CA
hK-CA
hK-CA
hK-CA
shoshonite
116-72
G44
G1
G8
G15
G47
G74
andesite
dike
dacite/latite
dome
alk. basalt
tholeiite
basaltic andesite
basalt
"
granodiorite
rhyolite
quartz-monzonite
granite
diorite
crd-granite
crd-granite
rhyolite
gabbro
crd-granite
gabbro
basalt
hK-CA
shoshonite
Na-alkaline
th/CA
low-K CA
granodiorite
Burd
Burd
Burd
Burd
Burd
La-L. Mio
0,04
0,04
0,16
0,15
0,15
0,01
0,07
6,13
6,99
3,26
0,71
4,10
5,01
5,06
10,7
7,98
3,13
4,45
4,75
5,02
2,32
3,81
4,84
1,71
1,21
1,28
0,33
1,38
0,01
0,17
0,19
0,24
0,53
0,29
Nb
Ba
99,17
99,09
53
37
46
6
37
335
350
383
290
367
7,8
8,2
7
35
28
39
54
68
104
104
12
14
21
17
8
630
472
501
183
431
16
284
12
33
367
18
54
315
21
26
325
20
47 263 28
132 180
31
18,1 193 15,4
19
291
20
13,3 192 17,5
19
396
15
9
413
20
11
302
17
7,1 450
16
21
394
19
18
253
26
137 414
23
155
191 139
42
258
11
96
100 156 7,5
138 123
12
58
78
13
380 803
27
88
92
105
75
142
168
37,0
58
50,4
41
35
51
38
51
107
171
230
442
1120
127
128
170
1309
5
6
4
6
8
11
1,8
5
2,4
5
8
5
2
5
9
12
13
31
132
13
8
5,1
63
307
383
495
203
599
545
128,0
143
153,0
61
59
177
49
120
373
353
678
872
103
412
74
189
26
48
59
178
83
10
12
<0.3
0,6
1,2
11
4
Th
La
Ce
Nd
Sm
Eu
73,9
148 57,5
10,9 0,20
58,2
115 44,5
8,6 0,11
31,2 65,2
2,4 15
2,4 16
5 12
2 18
5 10
126 45,2
26 11,4
30
13
40
37
24
0,20
0,7
0,8
16,2 31,7 14,8
3,5
3,98 24 44,7 23,5
5,2
2,76 20,1 39,7 18,1
3,9
2 11
29
7,3 25,3
55,3 26,9 5,0
11,8 27,4 57,0 26,1
5,0
2,2 4,6 11,4 6,4 1,79
7
16
2,2 6,55 14,10 7,91 2,20
0,5 18
14
13
15
2
8
20
1,1 4,2 10,5 7,93 2,26
6,9 16,5 10,6 2,86
5 23
51
13 26
54
34
74
6,9
61
109 54,3 11,2
111
210 94,9 21,1
35 59,8 19,7 2,79
11 22 37,9 12,4 2,12
226 21 42 77,3 28,9
5
1310
172
347 139
19
1,11 3,46
1,4 5,9
1,17 4,20
1,13 5,20
0,99 4,84 4,65
0,61
0,78 2,58 2,91
0,8
1
2,3
2,7
2,4
3,2
1,1
1,3 9,1 9,1
1,1 17,4 16,6
0,6
2 1,6
0,5 1,8 1,9
1,2 3,9 2,8
3,2
82
11
240
28
99
30
70
22
135
21
187 17,4
385 20,9
0,10 6,26
0,17 6,52
0,18 5,13
0,16 7,28
0,16 4,96
0,04 <0.03
0,10 9,09
0,08 4,75
0,1 4,6
0,1 1,6
0,15 5,77
0,2 4,9
0,1 1,4
0,2 1,5
8,83
9,84
9,45
11,9
8,76
0,66
10,3
4,96
8,38
2,57
9,21
8,9
3,54
1,03
2,97
2,41
2,43
2,41
2,78
2,67
1,76
1,61
3,72
2,25
1,87
2,14
3,76
1,78
0,65
0,65
0,30
0,36
0,76
5,20
0,94
2,24
0,8
4,4
0,94
0,8
5,4
8,1
0,06
0,07
0,08
0,06
0,08
0,18
0,07
0,15
0,24
0,42
0,11
0,15
0,17
0,13
2,84
2,39
3,05
2,67
1,91
0,49
1,68
2,25
1,00
3,39
0,83
0,61
1,91
1,86
99,60
99,90
100,05
100,00
100,02
98,90
99,50
98,70
99,89
99,80
99,90
100,00
100,02
100,00
23
20
14,4
9,5
35
455
60
127
28,3
227
46
29
195
352
237
231
170
155
161
50
196
162
305
581
185
310
230
108
20
62 1,9
135 2,7
7
15
56 1,7
79 0,7 3,3
19 37,5 1,9
50 0,7 2,9
18
64
0,6
72
72
0,9
12
47
105
35
62 11
113 13 34
23 133
331
36 15,5 10 1172 2,8 18
31 260 33 1310 64 64
19
76 4,1
134 3,32 11,1
20
56 5
334
2
24 145 7
473
8
32 190 9
383
9
15,3 7,92
8,02 5,4
7,63 6,54
3,3
9,4
2,04
1,68
2,11
0,6
0,6
0,8
2,2
2,1
2,8
2,4
2,4
3,1
71,9 31,7
6,88
0,9
6,2
5,9
39,0 23,6
137 68,2
23,5 12,4
5,81 1,8 6,7 3,3
12,4 2,3
2,98 0,73 3,03 3,18
1,24
0,99
4,54
3,24
1,88
0,05
3,02
100,03
99,06
99,37
100,31
99,62
100,36
100,52
51
148
85
280
191
118
74
280
162
410
540
380
564
545
20
25
26
24
21
26
20
110
159
127
212
203
124
106
6,8
685
13
774
14
974
15
18 1531
33
913
33
20
15 35
12 46,2
33
19 30
12 32,4
14 28,4
38
20
72,5 28,1
85,0
5,75
55
25
63,4 26,1
53,4 23,6
4,6 1,2
3,6
4,63 1,20 4,06 3,45
4,35 1,25 4,00 3,46
1,37 93,07
2,88 96,16
3,81 99,67
5,18 100,52
1,99 99,69
4,21
3,82 99,65
1,3 99,55
1,35 98,85
1,66 99,26
0,86 99,47
1,82 99,69
0,90 99,39
0,92 99,73
0,66 99,21
2,80 99,37
0,72 99,46
2,21 99,40
3,96 100,03
85
182
12
5
4,1
12,1
6,7
245
296
570
892
775
200
400
340
360
192
43
24
20
20
18
26
17
22
14
14
141
148
146
46
84
41
68
100
73
7,2
850
20 2300
21
655
3
77
3,7
127
2,5
106
4,1
113
7,4
235
9
361
43
63
24
5
9,1
5
8,4
18
21
87
37
123
60
54
31
12
7
21
13
12 8,5
19 11,5
33
30
16
219
226
139
175
23
17
148 11
143 14
361
300
30
27
71 29,9
62 26,9
5,5
5,1
1,1
1,1
4,7
4,2
27
427
111
56
269
60
197
294
15 45,5 1,4
13 125 17
9,2 42,9 1,8
14 70,5 2,9
182
226
159
149
5,6
25
7,7
12
12,7 7,4
65 28,6
15,4 7,1
24,3 11,2
2,08
5,5
1,72
2,4
0,7
0,6
0,5
0,8
2,3
4,6
1,8
2,4
16,4
13,65
14,75
16,50
16,35
17,06
17,10
t. 7.2
t. 2
t. 6.85
t. 4.65
t. 4.7
t. 8.19
t. 8.62
0,1 4,7 8,03 2,45 1,5
0 0,3 1,63 3,80 4,2
0,02 3,90 3,89 2,40 3,30
0,06 1,78 5,75 3,12 2,87
0,1 2,4
5,6 2,88 3,9
0,1 4,9 8,99 3,10 2,95
0,10 4,72 10,6 2,98 2,39
0,17
OR10
ORbd1
OR13
DLDR
DLBO
DJ1
DJ2
T22
T36
hK-CA/sho A12
A1
A9
U3
L61
hK-CA
C1
L44
II 6
VPE-271
mK-CA
VPE-21
La-L. Mio
La-L. Mio
La-L. Mio
Burd
La-L. Mio
La-L. Mio
La-L. Mio
Bu/La
La-L. Mio
Burd
29
29
29
28
28
28
28
28
28
32
32
32
32
32
32
32
32
32
32
56,70
61,60
45,90
46,90
55,70
46,30
47,80
64,20
73,20
62,00
68,20
63,20
69,2
69,4
73
47,6
72,2
47,80
51,4
0,68
0,70
1,49
0,76
0,98
0,78
1,00
0,45
0,18
0,69
0,42
0,6
0,44
0,42
0,12
0,73
0,28
0,35
0,58
14,90
16,65
15,68
0,68
18,00
16,80
17,15
16,6
12,95
16,1
14,85
15,28
15,06
15,83
14,68
17,11
14,62
14,8
16
t.
t.
t.
t.
t.
0,12
0,08
0,15
0,16
0,27
0,13
0,16
0,04
0,01
0,33
0,06
0,05
0,05
0,05
0,02
0,16
0,02
0,19
0,09
0,21
0,41
0,48
0,13
0,10
0,19
0,19
0,15
0,03
0,16
0,08
0,12
0,14
0,14
0,29
0,16
0,18
0,08
0,12
hK-CA
La-L. Mio
5,86
2,10
9,57
9,00
2,81
8,70
6,55
2,4
0,4
1,4
1,1
2,3
1,5
1,1
0,3
7,4
0,6
14
8,1
7,47
4,56
9,25
10,7
8,02
10,5
9,35
3,96
0,61
1,98
2,57
4,66
2,42
2,29
0,65
11,9
1,04
8,6
9,3
3,17
2,70
3,15
1,88
3,50
2,58
3,35
2,67
1,91
4,28
3,72
3,43
2,65
2,88
3,31
1,5
3,12
1,16
2,06
2,59
4,48
0,69
0,36
0,46
0,64
0,38
3,4
6,3
5,1
4,2
3,8
3,9
3,7
4,8
0,8
4,7
1,7
1,3
0,24
11,8
32
6,05
4,50
6,70
35,4
17,3
1,4
1,4
245
169
4
11
9
167
<4
0,65
0,27
0,57
0,75
0,70
1,05
1,29
28,2
72
6,5
4,90
8,90
88,6
39,7
Dy
1,01 99,76
3,72 99,85
0,53 99,95
0,76 99,90
1,37 99,80
0,56 100,10
2,24 98,80
57,60
72,3
59,15
61,00
61,00
53,97
49,70
168 8,5 13
796 18 35
21
2,5
14 0,50 1,80
27 0,80 3,80
880 19 44
82 6,6 13
Gd
0,08
0,05
0,16
0,07
0,08
0,07
0,15
31
30
30
30
30
30
30
33
Zr
3,86
4,1
0,22
0,3
0,4
4,62
0,28
Mio
Mio
Mio
Mio
Mio
Mio
Bu/La
Y
2,48
3,66
1,91
2,33
2,25
3,57
2,70
La-L.
La-L.
La-L.
La-L.
La-L.
La-L.
Bu/La
Burd
Sr
2,77
2,36
9,61
8,31
10,9
1,70
10,6
Mio
Mio
Mio
Mio
6.97
3.51
9.50
9.30
7.76
t. 9.4
t. 9.9
t. 4.41
t. 1.73
t. 5.55
t. 3.35
t. 4.44
t. 3.06
t. 3.01
t. 1.46
t. 9.17
t. 1.98
t. 8.62
t. 7.14
Rb
1,44
0,42
5,66
3,76
3,82
0,48
6,48
La-L.
La-L.
La-L.
La-L.
4,20
0,80
1,31
ppm
6,70 100,40
4,77 0,23 5,12 8,37 2,67
5,21 0,17 3,79 8,32 2,43
3,22 0,16 2,20 7,94 3,08
7,3 0,2 3,6 9,52 3,05
0,15 5,33 8,89 2,18
0,08 2,59 5,64 2,83
0,18 9,94 9,90 1,86
8,96 0,19 5,52 10,3 2,07
0,18 9,28 10,0 1,96
- 0,1
11 8,01 1,81
- 0,2
11 9,89 2,35
7 0,1 5,9 10,8 1,79
- 0,2
11 11,9 2,14
0,21 5,95 11,5 2,18
5,5 0,2 2,4
5,1 2,43
5,1 0,1 1,8 7,09 3,09
- 0,1 1,4
3,4 3,4
0,26 0,03 0,41 1,26 4,05
0,36 0,13 0,22 0,20 5,08
1,1 2,57 5,48
0,9 1,99 3,59
3,85
0,1 8,7 4,50 3,36
0,81 2,4 0,1 6,6 3,12 1,02
Ol-Aq
11
Ol-Aq
11
Ol-Aq
11
Ol-Aq
8
Burd
15
Burd
15
Burd
15
Burd 4; 10
Burd
18
Burd
14
Burd
14
Burd 4; 8
Burd 6; 12
Burd
14
Burd
8
Burd 4; 8
Burd
3
Burd
9
Bu/La
9
La-L. Mio
16
Burd
17
Burd
13
Bu/La 19, 20
0,24
1,70
1,69
2,12
9,19
2,28
Sum
99,82
99,82
100,20
101,80
102,52
101,39
SH-32
SH-55
SH-48
A530
ST81
ST138
ST46
AR2b; a501
AR 280
VF2B
VF2C
A 714-713
kb 24
kb2
A540
Al 1
SI-2
NU371
37/Fbis
Sar1.03
B13
DR02
sis04
t.
t.
t.
t.
t.
t.
t.
0,02 1,19 0,69 2,98 3,76
0,84 0,01
0,10
0,19
2,99 0,11
9,63 0,29
4,32 0,28
LOI
8,37 100,66
6,28
2,95
1,49
1,81
2,53
1,41
basalt
amphibolebas. andesite bearing
andesite
bas. andesite
mK-CA
bas. andesite
breccia
mK-CA
andesite
hK-CA
basalt
dike
tholeiite
"
tholeiite
"
tholeiite
"
porphyric low-K CA
"
doleritic low-K CA
"
tholeiite
"
thol./HMB
"
HAB/mK-C
andesite
hK-CA
latite
hK-CA
rhyolite
ignimbrite
rhyol/com
"
comendite
comendite
shoshonite
shoshonite
rhyolite
pyroclastic hK-CA
andesite
amphibole+biotite bear.
lamproite
sill
lamproite
hK-CA
tholeiite
tholeiite
tholeiite
0,02 2,02 0,73 2,40 3,22
2,95 0,6 2,7 2,2
5,91
1 4,5 4,4
2,13 0,7 3,1 4,2
1,76 0,62 2,66 3,56
2,23 0,83 2,88 3,57
6,58 1,2
5 3,8
4,6 1,2 4,6 4,5
1
1,4
2,15
1,70
0,8
1,1
0,8
1,1
0,9
0,5
5,9
3,5
4,6
1,50 3,90
3,90
3,40
2,8
4
2,5
3,5
2,6
2,7
1,6
2,3
Supplementary – Table S5: Table of site, formation, age and stratigraphic data of calc-alkaline volcanogenic
allochthonous sediments from the Apennines and the Maghrebid-Betic region. Key: SIV, stratigraphic interval
with volcanogenic sediments (meters); VTT, total thickness of volcanoclastic beds; TVB, thickest
volcanogenic bed. Fig. 3: elongated triangles without black rim of red, gray and yellow colour indicate beds of
Oligocene-Aquitanian, Burdigalian and Langhian-Tortonian age. References.- [1] Guerrera et al. 1998 and
references therein; [2] Guerrera et al. 2005 and references therein; [3] Critelli et al., 1990; [4] Maate et al.,
1995; [5] Riviere et al., 1977; [6] Balogh et al. 1993 and references therein; [6a] Critelli et al., 1990a; [7]
Spadea et al. 1974; [8] Le Pera et al., 1994; [9] Balogh et al., 2001; [10] Borsetti et al., 1984; [11] Guerrera et
al., 1993 and references therein; [11a] Perrone, 1987; [12] de Capoa et al., 2002; [13] Baruffini et al., 2002;
[14] Faugères et al., 1992; [15] Delle Rose et al.,1994a and references therein; [16] Crisci et al., 1988; [17]
Mattioli et al. 2002; [18] Cibin et al., 1998; [19] Tateo, 1993; [20] Mezzetti et al., 1964; [21] Cibin et al.,
2001; [22] Amorosi et al., 1994; [23] Coccioni et al., 1988; [24] Guerrera, 1977; [25] Guerrera et al.,1986;
[26] Delle Rose et al., 1994b; [27] Guerrera et al., 2004; [28] Mattioli et al., 2000.
SECTOR,
VOLCANOCLA
VOLCANIC
VOLCANIC
MAIN
SOURCE
REFER
HYPOTH.
-ENCE
SEDIMENTARY
DOMAIN, SITE
FORMATION
AGE
STIC ROCK
LAYERS (type, SIV,
PROCESSES
(Fig. 3)
TYPE
Betic
Viñuela
Cordillera/ 1
Group
andesite, rhyolite-
(meters)
mineral
grains and
pyroclastic fallout;
rhyodacite
glass- shards; SIV: 45;
epiclastic mass-flow
fragments
VTT: 3;
(turbiditic)
andesite, rhyolite
TVB: 0.5
felsitic lava and mineral clasts
epiclastic mass-
fragments
(up to 7% vol.)
flow (turbiditic)
early
[1]
Burdigali
----
an
Aquitanian
Betic
VTT, TVB
Algeciras
----
Burdigalian
Cordillera/ 2
Flysch
[2]
p.p.
[1]
Almidar, Río
Submarine
Betic
Fardes-Mencal
early
rhyodacite
glass-shards and
Epiclastic mass-
Cordillera/ 3
Succ.b
Burdigalian
fragments
mineral grains; TVB: 0.25
flow (turbiditic)
volcanic
emissions
(Subbetic)
Sidi Abdeslam
Early
Rif / 4
mainly mineral clasts, SIV:
epiclastic mass-flow
Internal
[1]
10; VTT: 0.5; TVB:0.15
(turbiditic)
zones
[4]
andesite, basalt
–Boujarrah Fm
Burdigalian
syn- and/or postlate Aquitanian
Beni Ider
Rif / 5
[1]
andesite,
-early
Flysch
eruptive epiclastic
Internal
mass-flow
zones
lava clasts
basalt fragments
[6]
Burdigalian
[2]
(turbiditic)
Talaa Lakra
late Aquitanian
syn- and/or postandesite
Rif / 6
(Mixed
-early
Successions)
Burdigalian
lava clasts
Internal
[1]
zones
[6]
Western
[11]
Mediterran
[5]
Mesomedi-
[2]
terranean
[1]
Microplate
[12, 13]
epiclastic mass-flow
Mesomedit.
[2]
(turbiditic)
Microplate
[6]
eruptive epiclastic
fragments
Algerian
mass-flow (turb.)
Oligo-Miocène Burdigalian p.p
glass-shards; grains of quartz, epiclastic mass-flow
rhyolite
Tell/ 7, 8
Kabylia
(19.1±1.0 Ma)
plagioclase, sanidine, biotite
Tusa
early
andesite to dacite
Tuffites
Oligocene
fragments
(turbiditic)
lava clasts (80-85% vol.),
Sicily/ 9
epiclastic mass-flow
grain size up to 2.5 mm, SIV:
(turbiditic)
600; VTT: 200; TVB: 1.5-2
;
Troina
andesite
up to 40 % volcanic clasts,
Sandstones /
fragments /
grain size >2 mm; SIV: 150,
Poggio Maria
volcanic glass,
VTT: 30-40; TVB: 0’5-1 /
Sandstones
andesite-dacite
lava and mineral clasts (30-
fragments
35% vol.), grain size >2
Sicily/ 10
Burdigalian pp.
[12]
mm;
SIV: 200; VTT: 30-35; TVB:
0’5-1,5bentonite
shards, biotite;
Case Liardo,
Sicily/ 11*
M. Ugliarella;
C. Biticchie
mid Miocene rhyodacitic glass
clays (TVB: 1-1.5);
rhyodacitic tuff (TVB: 0.51.5)
Volcanic arc
[7]
mixed
late
rhyolite, andesite,
mainly lava clasts, grain
epiclastic mass-flow
Sicily/ 12
successions
Reitano flysch;
Sicily/ 13*
mixed
Aquitanian
early
basalt fragments
arenitic beds;
early
Burdigal.
Oligoce
successions
Stilo-Capo
Peloritani
d’Orlando,
size>2 mm, SIV:43;
TVB:1
lava and mineral clasts,
[11]
(turbiditic)
epiclastic mass-flow
[9]
----
andesite & basalt
glass-shards, pumices,
[11,14]
(turbiditic)
fragments
ne
Calabria-
SIV:20
andesite & basalt
early
rock fragments;
Paludi
epiclastic mass-flow
Internal
[1]
(turbiditic)
zones
[2]
epiclastic mass-flow
Active
(turbiditic)
volcanic arc
epiclastic mass-flow
Active
(turbiditic)
volcanic arc
lava and mineral clasts
Oligoce
Arc / 14
[1]
---
crystals
ne
Calabroandesite, basalt,
S. Apennines
rhyodacite
/ 15
Lava and mineral clasts,
late
Lucano
Liguridi
Oligoce
Complex)
ne
fragments
glass-shards (andesite,
[15]
qz- andesite
tuffites),TVB:1.5
Saraceno
andesite to dacite
S. Apennines
early
(Liguridi
/ 16
[1]
lava and mineral clasts
[2]
fragments; mineral
Mioce
Complex)
(andesite, qz andesite
[3]
clasts
ne
tuff)
lava and mineral clasts
Tusa Tuffites
epiclastic mass-flow
S. Apennines
complex
early
andesite, basalt,
(80%vol.), pelites with
(Sicilide
Oligoce
dacite fragments
pumices, glass-
Complex)
ne
(turbiditic) and ash
/ 17
[11]
Sardinia
[2, 3]
turbidites
shards;SIV:54;
VTT:46;TVB:5
late
S. Apennines
Numidian
Burdigalia
glass-shards, mineral
rhyolite
/ 18
Flysch
n-
Pyroclastic fallout
[11]
Sardinia
[6, 6a]
Sardinia-
[16]
clasts
Langhi
S. Apennines
rhyolite,
(Cilento
Sardinia
grains, pumices, lava
-early
Pollica
[13
an
Burdigalian-
/ 19
epiclastic mass-flow
lava and tuff clasts, TVB: 3
rhyodacite
(turbiditic)
Group)
S. Apennines
/ 20*
San Mauro/
Burdigalian
lava and mineral clasts; SIV:
mass-flow short-
rhyodacite
15-20
distance (turbiditic)
-Corsica
pyroclastic fall-out,
Volcanic
late
andesite and/or
3-15 % lava clasts; mineral
epiclastic mass-flow
Arc
Burdigalian
basalt fragments
grains, glass-shards; TVB: 5
(turbiditic)
(Sardinia)
Pollica
rhyolite,
[11]
(Cilento)
Mt. Soprano
S. Apennines
(Daunia
/ 21
Complex)
Macchialupo;
S. Apennines
andesite and/or
Burdigalian
Gorgoglione
/ 22*
Volcanic
lava clasts (70-90 % vol.),
epiclastic mass-flow
basalt fragments;
p.p.; Miocene
(Daunia comp)
[6]
Arc
SIV: 80; TVB: 4
rhyolite clasts
[11a]
(turbiditic)
[8]
(Sardinia)
N. Apennines
basalt, andesite,
lava clasts
Sub-Ligure
Val Aveto;
Early
Continental
epiclastic mass-flow
dacite, dacite(up to > 80 vol. %)
Domain / 23
Ranzano
Oligocene
[17]
arc (near the
(turbiditic)
rhyol. ignimbrite
SIV: 490
[18]
graben)
clasts
[*]
basalt, andesite,
N. Apennines
early
Petrignacola;
Sub-Ligure
Continental
dacite;
volcanic clasts
epiclastic mass-flow
rhyodacite,
(up to > 80 vol. %); SIV: 255
(turbiditic)
Oligocene;
Ranzano
Domain / 24*
arc (near the
32-30 Ma
[17]
graben)
ignimbrite clasts
andesite, dacite;
N. Apennines
Antognola
early
Ranzano
Oligocene;
Mongardino
32-30 Ma
[19]
lava and mineral clasts; glassepiclastic mass-flow
glass-shards
Epi-Ligure
shards; SIV: 15; VTT: 5;
(turbiditic)
(rhyoliteDomain / 25*
[20]
---[1]
TVB: 5
[21]
rhyodacite)
N. Apennines
glass-shards (< 90% vol.),
pyroclastic fallout,
rhyodacite-dacite
mineral clasts (grain size <
and/or epiclastic
clasts
0,5 mm), SIV: 15; VTT: 15;
mass -flow,
TVB: 10
hyaloclastic
AquitanianEpi-Ligure
Tripoli di
[6]
Burdigalian
Domain /
Contignaco
----
p.p.; 22.4 Ma
[10]
[22]
26/*
Bisciaro
glass-shards, mineral and lava epiclastic mass-flow Intern. volc.
[1] [5]
andesite –
N. Apennines
Formation
Burdigalian
/ 27[*]
clasts; SIV: >100; VTT:18;
(turbiditic) and
zone (near
[23]
TVB: 6.9
pyroclastic fallout
the graben)
[24, 25]
rhyolite
(s.s.)
mainly glass-shards, mineral
N. Apennines
Aquitanian/
andesite and
Cervarola
/ 28
epiclastic mass-flow
----
grains -vitric tuffs, SIV: 80;
Burdigalian
rhyolite
[15]
(turbiditic)
VTT: 10; TVB: 6
Vicchio Marls
late Aquitanian
internal
mineral grains, glass-shards
N. Apennines
(Cervarola
-Burdigalian
rhyolite
epiclastic mass-flow
volcanic
[15]
(turbiditic)
zone (near
[26]
and andesitic clasts; SIV: 450;
/ 29*
Unit; Bisciaro
p.p. (lower
-dacite glass
TVB: 0.3
form, l.s.)
portion)
the graben)
Villanovaforru
W-Sardinia
Burdigalian
Graben / 30
high-Mg basalt
large amount of reworked
epiclastic mass-flow
(tholeiitic/calc-
volcanic detritus, SIV: 640;
(turbiditic),
VTT>10; TVB: 0,6
pyroclastic fall.
Succession,
Marmilla
alkaline type)
Basin
close to the
[27]
source
[28]
Supplementary – Table S6: Table of revisited age and geochemistry data of Apenninic allochthonous
volcanoclastics and buried volcano beneath Pieve Santo Stefano; major elements (weight %) and trace
elements (ppm). Data source: 1) Eni (unpublished report, 1982; 2) Cibin et al., 1998; 3) Balogh et al., 2001; 4)
Baruffini et al., 2002; 5) Mattioli et al, 2002; 6) Mezzetti et al., 1964; 7) Guerrera et al., 1986; 8) Balogh et al.,
1993; 9) Delle Rose et al., 1994a; 10) Delle Rose et al., 1994b; 11) Spadea and Carmisciano, 1974; 12)
Guerrera et al., 1986; 13) Crisci et al., 1988; 14) Critelli and Le Pera, 1990a; 15) Le Pera and Ventura, 1994.
CA = calc-alkaline; glass sh. = glass shards; b.d. = below detectio.
Age (Ma) Location
Oligocene
North Apennines
29.8, 29.0 Aveto &
amphibole Petrignacola
Ar/Ar dates
((29.8)) Pieve S. Stefan
(oil drilling)
Oligocene Ranzano format
(32-30 Ma
"
NE Sicily
Reitano flysch
Miocene
early
Miocene
North Apennines
Contignaco
Mongardino
Site in Data Rock
Fig. 3 source type
25-24
13
26-25
13
26
25
Calderino
Burdigalian Bisciaro formation
(22.3) - 17 Montebello, Urb
27
Fossombrone
Vicchio
early
Miocene
Miocene
South Apennines
Cilento
San Mauro/
Pollica
Lucania
Gorgoglione
flysch
mid Mioce Sicily
Case Liardo
Monte Ugliarella
Case Biticchie
late Mioce North Apennines
Laga Formation
29
"
"
"
"
5
"
"
"
"
"
"
"
"
"
"
"
1
"
2
"
"
Note
basalt
"
basaltic
andesite
andesite
"
dacite
"
dacite
"
"
rhyolite
bas. andesite
andesite
andesiticdacite
"
3 & 4 rhyolite
"
6
"
"
"
"
8&6
7
"
"
"
9 & 10
"
"
"
"
rhyodaciterhyolite
"
"
"
"
"
"
"
"
"
"
"
"
"
19, 20 13 &14 rhyodacite
"
"
rhyolite
Sample Serial Whole Mineral
affinity rock grains
SiO2 TiO2 Al2O3 Fe2O3 FeO
Wt. % --->
lava clast
"
"
"
"
"
"
"
ignimbrite
clast
"
"
altered
rocks
volcanoclastic
"
MM72
MM15
MM5
MM2
MM61
MM109
MM54
MM89
MM29
MM112
MM113
MM114
3870-2
3870-1
34D
94
128
48,42
49,94
51,16
54,49
56,43
58,03
61,45
63,75
57,50
63,18
66,23
71,42
58
62,1
45,18
36,23
52,84
lava clast
5(24)
s2
Kalkaline
1
5
5
4
4
CA
volcanoclastic
"
"
"
"
"
"
"
"
"
"
"
"
"
"
CA wh. rock
"
"
"
"
"
"
"
"
"
"
"
CA
"
"
CA
amphibole
biotite
pyroxene
pyroxene
glass sh.
glass sh.
lava clast
"
S2
S3
LOI
Sum
18,02 9,11
0,14 5,85 9,41 3,49
18,57 11,84
0,14 9,34 1,36 4,13
18,38 10,73
0,14 7,75 1,59 5,15
16,44 6,54
0,13 3,84 10,41 3,02
19,71 5,19
0,12 3,83 5,16 3,36
17,67 4,91
0,13 3,17 5,67 3,53
17,68 4,21
0,11 3,14 3,19 4,17
16,47 4,59
0,12 3,49 3,88 2,16
16,65 7,07
0,15 5,36 4,02 5,90
19,02 3,03
0,10 1,26 2,93 4,44
15,61 3,78
0,12 2,07 4,11 3,59
12,66 1,50
0,12 2,50 2,40 5,27
21,2
3,2
0,02 1,30 3,89 3,83
15,2 4,54
0,04 1,62 5,02 2,09
9,19
15,73 0,47 12,82 10,98 1,63
14,53
12,49 0,16 16,04 0,03 0,84
2,10
8,77 0,77 14,21 22,15 0,28
0,94
0,30
0,42
1,15
2,60
2,84
3,61
3,42
0,34
3,50
2,45
1,43
1,63
2,24
0,55
8,56
0,00
0,14
0,23
0,20
0,17
0,21
0,16
0,21
0,18
0,16
0,17
0,18
0,21
0,12
0,11
3,43
3,11
3,49
2,90
2,59
3,26
1,38
1,39
2,50
1,63
1,41
2,33
6,30
6,78
100,00
100,00
100,00
100,00
100,00
100,00
100,00
100,00
100,00
100,00
100,00
100,00
20,2
1,75
0,08
0,57
9,84
0,16 0,11 2,44
0,55 14,99 20,06 0,31
11,58
0,25
1,34
1,71
0,80
1,66
1,02
3,82
3,75
2,12
3,30
4,50
2,60
2,44
3,23
2,20
3,20
3,51
3,04
2,87
1,96
6,80
7,69
8,64
8,17
12,85
100,47
99,83
100,53
100,08
100,46
glass sh.
65,8 0,58 13,6
"
67,2 0,28
14
"
64,2 0,51
14
plagioclas 59,1
27,7
"
50,5
30,5
glass sh.
70,6 0,36 14,9
"
75,4 0,53 13,3
K-feldspar 65,5 0,34 19,3
plagioclas 59,20
24,88
biotite
34,80 2,49 18,82
1,49
1,5
2,55
3,14
0,38
0,67
0,68
0,62
0,33
0,23
21,40
0,09
0,12
0,10
0,54
0,25
0,59
3,78
2,46
2,54
7,64
2,75
2,21
0,29
3,20
7,02
0,44
2,37
4,20
3,61
0,76
0,12
6,52
6,93
11,81
0,62
3,84
8,28
100,23
92,26
91,37
0,20
9,82
2,18
1,26
3,24
7,56
15,69
2,47
0,23
0,30
6,53
0,31
0,07
0,02
1,69
0,30
1,19
0,06
3,09
2,72
4,36
5,06
P2O5
0,13
-
2,44
1,37
0,04
0,05
0,03
68,1
76,3
0,35
0,05
15,3
13,1
3,27
1,01
69,6
71,2
75,1
0,62
0,36
0,19
15,3
13,6
13,1
1,99
1,8
0,66
1,30
1,30
0,46
0,67
0,70
0,78
3,11
3,39
3,57
4,44
5,51
4,65
0,23
0,12
0,07
2,06
1,51
1,01
68,60
41,44
38,15
70,04
0,23
3,32
3,56
0,20
13,41 0,72 0,92 0,03 0,60
16,05 5,04 11,82 0,17 9,43
15,75 11,01 7,09 0,14 10,54
13,34 0,49 0,87 0,05 0,35
1,85
0,40
0,41
1,69
2,96
0,73
0,25
3,11
3,06
7,50
7,30
2,86
0,12
0,07
7,55
3,86
5,86
6,87
0,96 2,17
7,29 7,26
11,39 5,14
2,48
0,78
0,35
rhyolite
lava clast
"
"
A II
C 13A
B 12
CA
11
"
"
"
11
"
"
"
rhyolite
volcanoclastic
"
"
7
"
"
14
CA
29a
"
"
12
"
"
rhyolite
volcanoclastic
"
F3/9
F3/3
F3/1
CA
"
"
"
glass sh.
biotite
biotite
glass sh.
glass sh.
70,84 0,13 13,69
andesine
61,50
24,58
labradorite 54,75
27,21
2,72
2,01
1,35
1,18
0,12
0,18
0,04
0,14
160
90
10
557
634
500
338
903
730
679
614
250
779
427
183
25
34
26
20
23
28
23
20
32
27
26
13
97,90
98,46
101,63
94,48
92,16
CA wh. rock
"
15
"
"
36
38
9
40
85
72
138
113
Y
100,6 (0.34%BaO)
100,36
0,06
0,14
0,15
0,09
0,04
0,05
0,88
0,06
Rb
Sr
ppm --->
93,04
101,29
0,55
4,28
2,83
1,31
0,98
glass sh.
70,60
57,87
58,80
65,1
60,7
K2O P2O5
1,74
2,97
3,96
1,69
3,15
wh. rock
3
CA
B6/1
B8/7
B6(2)
B8(b1)
80
shoshonitic
80a
80mc
80mc
80mc
64,6
52,46 0,40
CaO Na2O
0,08 11,67
0,89 14,82
0,99 14,19
0,48 14,2
0,56 13,1
wh. rock
22
"
"
rhyolite
"
1,04
1,05
1,00
0,92
0,79
0,62
0,84
0,56
0,37
0,74
0,44
0,17
0,85
0,62
1,44
4,18
0,18
MnO MgO
0,14
196
137
121
16
8
21
102,06
101,53
101,02
240
191
159
166
150
55
28
30
33
100,05
99,83
100,06
100,00
244
672
115
9
251
140
91,36
101,53
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