360:
retreating oceanic slab had to adjust and deform in relation the large and buoyant continental sectors. Post-Pliocene migration was eventually driven through the narrow corridor (250 km) represented by the present Ionian Sea and thus separated the
Adriatic and Sicilian sectors. Changes in lithospheric composition may have also contributed to differences in subduction geometry. For instance, during the first episode of subduction, thinned continental lithosphere underlying the Apenninic margin subducted beneath the Eurasian plate. However, in the second episode of subduction, it was instead Ionian oceanic lithosphere that was involved in subduction. A transition from continental to oceanic lithosphere subduction could explain the late onset of arc volcanism (2-1.5 Ma) as well as the lack of arc volcanism in the central Tyrrhenian basin.
338:
basin occurred approximately between the late
Tortonian and the middle Pliocene. However, in the Marsili plain, the oldest basaltic crust was found to be 2.1 Ma. This lower age limit, along with the presence of a saddle containing continental crust (the "Issel bridge") between the Vavilov and Marsili plains, implies that there were two distinct episodes of back-arc extension.
62:
259:. This is the easternmost point on the margin where pre-rift, syn-rift, and post-rift sediments can be clearly discerned on seismic reflection profiles. A drill core to the base of the syn-rift sediments revealed 533 meters of thinly-bedded, calcareous, siltstone and sandstone with dispersed detrital gypsum grains and
312:. Overlaying the basement is 250 meters of calcareous mud and ooze with interbedded volcanoclastic layers. Benthic foraminifera and magnetic anomaly data from the base of this section constrain the terminus of rifting between 1.67 and 1.87 Ma. At the top of the stratigraphic section are 350 meters of volcanoclastic
294:
containing carbonate-filled veins. Nannofossils and planktonic foraminifera within the carbonate veins constrain the age of emplacement between 3.1 and 3.6 Ma. Immediately above the basalt is a 100-meter-thick section of
Pleistocene sedimentary cover, consisting primarily of nannofossil-rich mud with
263:
nodules. The entire sequence is reversely magnetized, which when placed in the context of the adjacent stratigraphy, suggests that it was deposited during the reversed polarity event of the
Gilbert epoch (between 4.79 and 5.41 Ma). The environment of deposition for this section is uncertain; however,
214:
with subrounded clasts derived from metamorphosed carbonate and quartzitic basement. It is inferred that this conglomerate formation was deposited in a high-energy subaerial environment like an alluvial fan. Overlying the conglomerate formation are oyster-bearing glauconitic sandstones deposited in a
337:
of peripheral oceanic basalts, drilled at the southeast edge of the
Vavilov plain, estimates the beginning of extension to be 7.3 ± 1.3 Ma. Basalts recovered near the spreading center, in middle of the Vavilov plain, yielded ages of 3.4–3.6 Ma. This means that back-arc extension in this part of the
368:
The full spreading rate of the
Tyrrhenian basin has been estimated to be 3–5 cm/yr based on kinematic reconstructions and magnetostratigraphy. This is a relatively slow spreading rate when compared to spreading rates in other back-arc basins like the East Scotia basin (5–7 cm/yr) and the
346:
Between the
Tortonian and middle Pliocene, W-E directed extension opened the Vavilov plain and Sardinia margin in the northwest portion of the present day basin. By the end of the Pliocene, extension rapidly turned to NW-SE and was limited to the southeastern Marsili plain. This rapid shift in the
359:
The
Pliocene-Pleistocene changes in Tyrrhenian back-arc extension may have also been influenced by the adjacent Adriatic and Sicilian forelands. These sectors were not thinned by rifting and are characterized by normal continental lithosphere. During its southeastward migration, the passively
226:
assemblages overlays the sandstone formation; this indicates that water depth increased, perhaps due to subsidence at the end of the syn-rift period. The boundary between the syn-rift and post-rift periods is believed to be located in a 50-meter section of late
Messinian
52:
and two distinct sub-basins - the
Vavilov and Marsili basins. The Vavilov deep plain contains the deepest point of the Tyrrhenian basin at approximately 3785 meters. The basin trends roughly northwest–southeast with the spreading axis trending northeast–southwest.
355:
and trench retreat in the underthrusting African plate, then extension should not occur in the back-arc region. However, if the velocity of slab rollback and trench retreat exceeds that of the overriding plate, then back-arc extension will occur.
198:
surveys across the Upper Sardinia Margin exhibit a stratigraphic geometry suggestive of pre-rift, syn-rift, and post-rift sequences. Drill cores penetrating to the base of the syn-rift sediments identified a transgressive sequence related to
93:
to join a seismogenic slab that extends down to 500 km beneath the Tyrrhenian basin. Between the upper slope of the trench and Calabria are a number of small fore-arc basins that developed through extensional listric faulting during the
333:, as shown by the recognition in seismic reflection profiles of pre-evaporitic (i.e. pre-Messinian) sediments in the western Tyrrhenian and by age estimates based on the overall lithospheric thickness, basement relief, and heat flow.
307:
The basement rock of the Marsili Basin is vesicular basalt. Due to the abundance (10–30% of rock volume) and size (up to 3 or 4 mm) of the vesicles, it is likely that the basalt was emplaced as a flow rather than a
121:
of the convergent system. The volcanism associated with these islands occurs at the northeast closure of the downgoing slab and began approximately during the late Pliocene to early Pleistocene (1.5–1.7 Ma).
826:
Barberi, F., Bizouard, H., Capaldi, G., Ferrara, G., Gasparini, P., Innocenti, F., Jordon, J., Lambert, B., Treuil, M., and Allegre, C. (1978). "Age and nature of basalts from the Tyrrhenian abyssal plain".
369:
Manus basin (13 cm/yr). The ratio between the initial crustal thickness and final crustal thickness, also known as the beta factor, is estimated to be 3.3 for the Tyrrhenian basin.
580:
Malinverno, A., and Ryan, W. (1986). "Extension in the Tyrrhenian Sea and shortening in the Apennines as result of arc migration driven by sinking of the lithosphere".
937:
846:
812:
718:
664:
615:
557:
69:
The Tyrrhenian basin is located in a geologically complex portion of the Mediterranean Sea. The basin is partially encircled by several orogenic belts, including the
683:
Sartori, R., Carrara, G., Torelli, L., and Zitellini, N. (2001). "Neogene evolution of the southwestern Tyrrhenian Sea (Sardinia Basin and western Bathyal plain)".
275:
with intermittent volcanic glass. This sediment layer is believed to be deposited after the end of rifting due to its subhorizontal seismic reflection profile.
1131:
1126:
264:
due to the presence of thin, well-graded layers and a lack of marine fossils, it is possible that the formation was deposited in a closed
467:
1087:
389:
which pushes the oil window to very shallow depths where structural and stratigraphic traps are uncommon. There is, however, active
777:
Kastens, K. and Mascle, J. (1988). "ODP Leg 107 in the Tyrrhenian Sea: Insights into passive margin and back-arc basin evolution".
351:
change over time. For example, if the horizontal velocity of the overriding Eurasian plate exceeds the velocity of
629:
Della Vedova, B., Pellis, G., Foucher, J., and Rehault, J. (1984). "Geothermal structure of the Tyrrhenian Sea".
798:
207:
during the rifting stage of the Tyrrhenian Basin opening. At the base of the syn-rift sequence are 60 meters of
972:
390:
1010:
211:
987:
931:
840:
806:
712:
658:
609:
551:
232:
896:
Philosophical Transactions of the Royal Society of London. Series A, Mathematical and Physical Sciences
287:
with both high and low-temperature phases of deformation. The peridotite is overlain by 120 meters of
1002:
960:
903:
786:
692:
638:
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522:
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accumulation in most of the Tyrrhenian basin is very poor. This is primarily due to the basin's high
347:
direction and spatial location of extension may be due to how the relative velocities of interacting
1015:
386:
142:
86:
85:
and associated trench to the southeast. Deep reflection seismic lines near the trench clearly show
82:
919:
195:
138:
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21:
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272:
114:
78:
964:
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48:
to the northeast. The Tyrrhenian basin displays an irregular seafloor marked by several
535:
397:. Here, the small Narciso and Nilde fields produce sulphur-rich, light to medium-grade
394:
309:
191:
174:
162:
134:
126:
29:
704:
243:
post-rift sediment containing calcareous mud with occasional terrigenous clastics and
173:. Basement rocks in the southeastern portion of the basin were reactivated during the
137:. Similar to other back-arc basins, the Tyrrhenian basin displays a shallowing of the
1120:
1024:
923:
650:
421:
352:
291:
268:
setting. Overlaying the syn-rift sediments are 200 meters of Pliocene to Pleistocene
256:
150:
130:
244:
125:
The Tyrrhenian basin lies to the northwest of the Aeolian Islands and represents a
118:
402:
382:
334:
269:
240:
405:
ranging between 21 and 39). The primary reservoirs in these fields are Miocene
377:
Although there are numerous petroleum plays in mainland Italy and the northern
409:
378:
313:
288:
284:
231:
that overlays the calcareous ooze and claystone formations. At the top of the
200:
107:
103:
1102:
1089:
329:
It is widely agreed that extension in the Tyrrhenian basin began in the late
129:
formed from tensional forces associated with the northwest subduction of the
601:
398:
260:
216:
208:
166:
146:
95:
70:
49:
915:
255:
The Lower Sardinia Margin lies near the transition between continental and
283:
The basement rock in the Vavilov Basin consists of strongly serpentinized
417:
236:
99:
90:
33:
894:
Barker, P. and Hill, I. (1981). "Back-arc extension in the Scotia Sea".
864:
468:"The Tyrrhenian back-arc basin and subduction of the Ionian lithosphere"
406:
330:
296:
220:
37:
228:
41:
416:. The source of the hydrocarbons is unknown but is inferred to be
413:
223:
45:
951:
Taylor, B. (1979). "Bismark Sea: Evolution of a back-arc basin".
865:"Episodicity, sequence, and style at convergent plate boundaries"
74:
61:
1056:"Structural setting of petroleum exploration plays in Italy"
420:
limestone. Traps are structural in nature and are primarily
799:
10.1130/0016-7606(1988)100<1140:olitts>2.3.co;2
973:
10.1130/0091-7613(1979)7<171:bseoab>2.0.co;2
149:(exceeding 200 mW/m in some places), and an active
988:"Some remarks on the development of sedimentary basins"
98:. These basins subsequently subsided between the late
32:. It covers a 231,000 km area that is bounded by
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1063:Special Volume of the Italian Geological Society
215:nearshore environment. Late Tortonian to Early
177:while those to the northwest were undisturbed.
190:The Upper Sardinia Margin is a fault-bounded
8:
936:: CS1 maint: multiple names: authors list (
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614:: CS1 maint: multiple names: authors list (
556:: CS1 maint: multiple names: authors list (
511:"The deep seismicity of the Tyrrhenian Sea"
424:related to the Tunisian Atlas thrust belt.
117:north of Calabria and Sicily represent the
869:Geological Society of Canada Special Paper
678:
676:
674:
461:
459:
457:
81:to the southwest. It is also bounded by a
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829:Deep Sea Drilling Project Initial Reports
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486:
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141:towards the central part of the basin, a
393:on the south edge of the basin near the
194:located northwest of the Vavilov Basin.
60:
858:
856:
433:
89:from the African plate flexing beneath
929:
838:
804:
779:Geological Society of America Bulletin
710:
656:
607:
549:
509:Anderson, H. and Jackson, J. (1987).
7:
995:Earth and Planetary Science Letters
219:calcareous ooze and claystone with
153:on the arc-ward edge of the basin.
536:10.1111/j.1365-246x.1987.tb01661.x
14:
515:Geophysical Journal International
364:Rates of extension and subsidence
44:to the southeast, and peninsular
1132:Landforms of the Tyrrhenian Sea
488:10.18814/epiiugs/2003/v26i3/011
1:
705:10.1016/S0025-3227(01)00116-5
320:Basin tectonics and evolution
1127:Sedimentary basins of Europe
1025:10.1016/0012-821x(78)90071-7
651:10.1016/0025-3227(84)90072-0
412:that are sealed by Pliocene
1148:
169:granites derived from the
106:and are now infilled with
325:Temporal onset of rifting
57:Regional geologic setting
342:Mechanism of development
1007:1978E&PSL..40...25M
602:10.1029/tc005i002p00227
391:hydrocarbon exploration
24:located in the western
916:10.1098/rsta.1981.0063
77:to the north, and the
73:to the northeast, the
66:
986:McKenzie, D. (1978).
251:Lower Sardinia Margin
233:stratigraphic section
186:Upper Sardinia Margin
64:
466:Sartori, R. (2003).
381:, the potential for
295:occasional reworked
1099: /
1054:Casero, P. (2004).
965:1979Geo.....7..171T
908:1981RSPTA.300..249B
791:1988GSAB..100.1140K
697:2001MGeol.175...47S
643:1984MGeol..55..271D
594:1986Tecto...5..227M
527:1987GeoJ...91..613A
387:geothermal gradient
373:Petroleum resources
143:Wadati Benioff zone
87:oceanic lithosphere
83:convergent boundary
65:The Aeolian Islands
863:Dewey, J. (1980).
235:are 243 meters of
196:Seismic reflection
157:Basement structure
145:, abnormally high
139:Moho discontinuity
67:
40:to the northwest,
1103:39.933°N 12.233°E
902:(1454): 249–261.
303:Marsili Sub-Basin
279:Vavilov Sub-Basin
205:continental crust
171:Hercynian orogeny
26:Mediterranean Sea
22:sedimentary basin
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785:(7): 1140–1156.
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18:Tyrrhenian Basin
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1016:10.1.1.459.4779
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349:tectonic plates
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273:marine sediment
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115:Aeolian Islands
79:Atlas Mountains
59:
12:
11:
5:
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1135:
1134:
1129:
1119:
1118:
1108:39.933; 12.233
1081:
1080:
1037:
978:
959:(4): 171–174.
943:
886:
852:
818:
724:
691:(1–4): 47–66.
685:Marine Geology
670:
631:Marine Geology
621:
588:(2): 227–245.
563:
521:(3): 613–637.
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481:(3): 217–221.
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395:Sicily Channel
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192:passive margin
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175:Alpine orogeny
163:basement rocks
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135:Eurasian Plate
127:back-arc basin
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30:Tyrrhenian Sea
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835:(1): 509–514.
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151:volcanic belt
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131:African Plate
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36:to the west,
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1084:
1071:. Retrieved
1066:
1062:
1028:. Retrieved
1001:(1): 25–32.
998:
994:
981:
956:
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946:
932:cite journal
899:
895:
889:
877:. Retrieved
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841:cite journal
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807:cite journal
782:
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713:cite journal
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659:cite journal
634:
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610:cite journal
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552:cite journal
540:. Retrieved
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514:
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478:
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297:volcanogenic
282:
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245:volcanic ash
212:conglomerate
189:
181:Stratigraphy
160:
133:beneath the
124:
119:volcanic arc
112:
68:
17:
15:
1106: /
1073:23 February
879:27 February
542:17 February
494:15 February
403:API gravity
383:hydrocarbon
335:K-Ar dating
270:hemipelagic
241:Pleistocene
161:Tyrrhenian
1121:Categories
428:References
410:limestones
379:Ionian Sea
314:turbidites
289:tholeiitic
285:peridotite
266:lacustrine
201:subsidence
104:Quaternary
28:under the
1069:: 189–204
1011:CiteSeerX
924:121280138
875:: 555–573
582:Tectonics
399:crude oil
261:anhydrite
217:Messinian
209:Tortonian
167:Paleozoic
147:heat flow
96:Tortonian
71:Apennines
50:seamounts
475:Episodes
418:Mesozoic
299:debris.
237:Pliocene
100:Pliocene
91:Calabria
34:Sardinia
1094:12°14′E
1091:39°56′N
1030:1 March
1003:Bibcode
961:Bibcode
953:Geology
904:Bibcode
787:Bibcode
693:Bibcode
639:Bibcode
590:Bibcode
523:Bibcode
407:karstic
331:Miocene
221:benthic
203:of the
108:mélange
38:Corsica
1013:
922:
229:gypsum
42:Sicily
1059:(PDF)
991:(PDF)
920:S2CID
471:(PDF)
414:clays
224:foram
46:Italy
20:is a
1075:2015
1032:2015
938:link
881:2015
847:link
813:link
719:link
665:link
616:link
558:link
544:2015
496:2015
310:sill
113:The
102:and
75:Alps
16:The
1021:doi
969:doi
912:doi
900:300
795:doi
783:100
701:doi
689:175
647:doi
598:doi
531:doi
483:doi
239:to
1123::
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1061:.
1040:^
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999:40
997:.
993:.
967:.
955:.
934:}}
930:{{
918:.
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898:.
873:20
871:.
867:.
855:^
843:}}
839:{{
833:42
831:.
809:}}
805:{{
793:.
781:.
727:^
715:}}
711:{{
699:.
687:.
673:^
661:}}
657:{{
645:.
635:55
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