Festa et al., 2013 - Draft

New insights on diapirism in the Adriatic Sea: the Tremiti salt

structure (Apulia offshore, southeastern Italy)

Vincenzo Festa, Gianvito Teofilo, Marcello Tropeano, Luisa Sabato and Luigi SpallutoDipartimento di Scienze della Terra e Geoambientali - via E. Orabona 4, Universit�a degli Studi “Aldo Moro” di Bari, Bari 70125, Italy

ABSTRACT

The reinterpretation of public seismic profiles in the Adriatic

offshore of Gargano (Apulia, southern Italy) allowed the

detection of a kilometre-scale salt-anticline, the Tremiti dia-

pir, within the larger Tremiti Structure. This anticline was

generated by diapirism of Upper Triassic anhydrites within a

thick Mesozoic to Quaternary basinal sedimentary succession.

Both internal stratal patterns and shapes of Plio-Quaternary

units, and the occurrence of an angular unconformity

between early Tortonian and Pliocene rocks on the Tremiti

Islands, suggest that halokinesis began during the late

Miocene and is still active today. An ancient extensional

SE-dipping fault, cutting an older Mesozoic low-amplitude an-

hydritic ridge, played an important role during salt mobiliza-

tion, which was promoted by NW-SE shortening. The diapir

grew in the footwall of this fault, causing its upward propa-

gation. In some places, the ancient fault served as a preferen-

tial channel for the upward migration of the anhydrites.

Terra Nova, 0, 1–10, 2013

Introduction

Triassic to Lower Jurassic evaporites

developed in the peri-Tethyan and

proto-Atlantic areas over epicratonic

platforms (e.g. Courel et al., 2003;

Alves et al., 2006; Hudec and Jack-

son, 2007). Near and along the

fronts of the Apennines, Dinarides-

Albanides and Hellenides orogens

(Mediterranean Sea region), these

evaporites migrated upwards to form

diapirs, mostly during the Neogene,

often inducing sea-floor deformation

in the form of ridges (e.g. Underhill,

1988; Zelilidis et al., 1998; Kamberis

et al., 2000; Kokinou et al., 2005;

Scrocca, 2006; Alves et al., 2007;

Geletti et al., 2008; Kokkalas et al.,

2013). Tectonic shortening associated

with the accretion of the orogens

enhanced salt mobilization within

both the external thrusts area (e.g.

Kokkalas et al., 2013) and the fore-

deep sensu stricto (i.e. the sector not

involved in thrusting; Scrocca, 2006).

Geletti et al. (2008, and references

therein) highlighted the occurrence of

several diapirs in the central Adriatic

Sea, between the opposite fronts of

the Apennines and Dinarides

(Fig. 1). Here, diapirs are character-

ized by elongated shapes, mostly

200 km

Adriatic

Platform

Apulian

Platform

TYRRHENIAN

SEA

GarganoPromontory

A P U L I A

Fig. 2SEA

SEA

ADRIATIC

AdriaticBasin

halokinetic

SE

NI

N

N

E

AP

ALB

AN

IDE

S

structuresTremitiIslands

IONIAN

N40°

N42°

N44°

E17

°

E19

°

E15

°

D

IN

AR

ID

S

E

Fig. 1 Schematic structural map of the region around the Adriatic Sea (after

Zappaterra, 1990, 1994; modified). In the area not involved in the Apennines and

Dinarides opposite orogens, the Meso-Cenozoic paleogeographic position of the

Adriatic Basin between the Apulian and Adriatic carbonate platforms is shown.

The fronts of the Apennines and Dinarides are according to Scrocca (2006), and

Fantoni and Franciosi (2010), respectively. The halokinetic structures inferred or

hypothesized (e.g. the SW–NE-striking structure along the Tremiti Islands) by

previous studies are also indicated (after Geletti et al., 2008; modified). The inset

indicates the study area.

Correspondence: Dr. Vincenzo Festa,

Dipartimento di Scienze della Terra e

Geoambientali - via E. Orabona 4, Uni-

versit�a degli Studi “Aldo Moro” di Bari,

Bari 70125, Italy. Tel.: 0039 080 5443468;

e-mail: [email protected]

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© 2013 John Wiley & Sons Ltd 1

doi: 10.1111/ter.12082

T E R 1 2 0 8 2 Dispatch: 13.11.13 CE: Malarvizhi

Journal Code Manuscript No. No. of pages: 10 PE: Revathi-

NW–SE and secondly, NE–SW

trending. Geletti et al. (2008) also

hypothesized that the NE–SW-strik-

ing ridge, whose culmination forms

the Tremiti Islands, could represent a

halokinesis structure. The ridge,

about 15 km north of Gargano

(Apulia, southeastern Italy; Figs 1

and 2), corresponds to the Tremiti

Structure of Andr�e and Doulcet

(1991).

Several different interpretations

based on local seismicity and/or

seismic profiles and/or regional geo-

dynamic modelling have been sug-

gested for the origin of the Tremiti

Structure. It has been suggested to

be a pushed-up ridge, accommodat-

ing deformation occurring along

faults of regional extent characterized

by either E–W right-lateral kinemat-

ics (Mele et al., 1990; Argnani et al.,

1993; Favali et al., 1993; Doglioni

et al., 1994; Gambini and Tozzi,

1996) or NE–SW left strike-slip

movement (Finetti and Del Ben,

2005) or undefined kinematics lead-

ing to a compressional or transpres-

sional setting (Scisciani and

Calamita, 2009).

The diapiric origin hypothesized

by Geletti et al. (2008) can be sup-

ported by comparing sea-floor defor-

mation along the Tremiti Structure

with that induced by Plio-Quaternary

diapirism of the Triassic anhydrites

in the subsurface of the Adriatic Sea

(Scrocca, 2006; Nicolai and Gambini,

2007; Geletti et al., 2008; Grandic

and Kolbah, 2009). In addition, a

few kilometres south of the Tremiti

Islands, around Lesina Marina vil-

lage (Fig. 2), the cropping out of

exotic gypsum rocks that rose up

from the Triassic anhydrite source

(Bigazzi et al., 1996) could represent

further evidence supporting the

hypothesized diapiric origin for the

Tremiti Structure.

To verify this hypothesis, the seis-

mic reflection profile M13 of the

CROP Project (Scrocca et al., 2003),

and both free exploration wells and

seismic reflection profiles of the

ViDEPI Project (2012; Fig. 2) dating

back to the 1980–1990s, was inter-

preted. The profiles of the ViDEPI

Project have been scaled to make

times and distances consistent with

the M13 CROP Project line. Owing

to the low quality of these old, non-

migrated seismic profiles, which can

lead to different interpretations (e.g.

Finetti and Del Ben, 2005; Scisciani

and Calamita, 2009), particular

attention has been paid to those typi-

cal pre- to post-halokinesis geome-

tries and terminations of the

reflectors within the host-rock of a

salt-diapir (e.g. Pascucci et al., 1999;

Alves et al., 2002, 2009; Rowan

et al., 2003; Stewart, 2007).

Geological setting

During the Mesozoic, in the Adria

Plate (sensu Channell et al., 1979), a

narrow pelagic basin (the Adriatic

Basin), flanked by carbonate plat-

forms (Apulian, to the SW, and

Adriatic, to the NE), occupied

roughly the same position as the

present-day Adriatic Sea (Zappater-

ra, 1990, 1994; Bernoulli, 2001;

Fig. 1). This pelagic domain devel-

oped as a consequence of early

Jurassic rifting of an epeiric area

dominated by carbonates (Rhaetian

dolostones and overlying early Juras-

sic limestones of the Calcare Massic-

cio Fm, Fig. 3). The epeiric platform

was rooted on Norian anhydrites

and shallow-water limestones and

dolostones (Burano Fm; Foresta

Umbra1 well, Fig. 3), which overlie

Permian continental deposits (Verru-

cano Fm) draping the Hercynian

basement (Ricchetti et al., 1988). The

Adriatic Basin succession rests on

the Calcare Massiccio Fm and con-

sists mainly of Jurassic to late Mio-

cene pelagic limestones; thin

Messinian evaporites separate this

succession from the overlying

MESOZOICPLATFORM

MESOZOIC

SHELF MARGIN

MESOZOICBASINAL

DOMAIN

BR16

8-10

B42

8

B42

7

B441

BR169-32

B442

BR265

BR264

BR263

BR262

BR261

BR260

BR168-21

M13

Fig. 4

Fig. 5b

Fig. 5a

B43

0

1500

1000500

500

1000

500

BR12

7

B42

6

Famoso 1Eterno 1

Peschici 1

ForestaUmbra 1

LesinaMarina

TremitiIslands

Fig. 6

10 km

N

Fig. 7

15

°06

’13

”

41°47’07”

16

°03

’26

”

42°31’57”

Fig. 2 Map of the study area around the Tremiti Islands (after Google Earth,

2013; modified). White contour lines represent the isobaths of the base of the Plio-

cene deposits (after Andr�e and Doulcet, 1991; modified); the Tremiti Structure is

the narrow area where the base-Pliocene depth abruptly decreases. Analysed wells

(shown in Fig. 3) and the grid of the studied seismic profiles are indicated. Thicker

orange lines show the portions of the interpreted seismic profiles M13, BR169-32,

BR168-21 and B426, shown in Figs 4, 5a,b and 6, respectively.

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2 © 2013 John Wiley & Sons Ltd

Diapirism in the Adriatic Sea: the Tremiti salt structure • V. Festa et al. Terra Nova, Vol 0, No. 0, 1–10

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Foresta Umbra 1

Marne a Fucoidi

Late Lias

Aquit.-Langh.

Eterno 1

Plio

-Qu

ate

rna

ry

Schlier

Scaglia Cinerea Bisciaro

Gessoso-

Scaglia Calcarea

Maiolica

Calcari ad Aptici

Rosso Ammonitico

Corniola

Calcare Massiccio Fm

2270 m

0 m(–160 m)

Peschici 1

Maiolica

Marne a Fucoidi

Calcari ad Aptici

0 m(55 m)

1275 m

Aptian-Albian

Late

Ju

rass

icM

idd

le

Jura

ssic

Ea

rly

Jura

ssic

Ea

rly

Cre

tace

ou

sMiddle Lias

Dogger - Malm

Early Lias

La

te C

reta

ceo

us-

Eo

cen

e

Oligoc.

Serrav.-Torton.

Messin.

Rh

ae

tia

nN

ori

an

Bu

ran

o F

m

Ea

rly

-Mid

dle

Ju

rass

ic

Pe

rsis

ten

t sh

all

ow

-wa

ter

con

dit

ion

s th

rou

gh

th

e E

arl

y-M

idd

le J

ura

ssic

Late

Ju

rass

ic

Rip

e R

oss

e F

m

Ca

lca

ri a

d A

pti

ci

eq

uiv

. in

slo

pe

fa

cie

s

0 m(809 m)

5912 m

Lithology

Marly limestones and marls

Limestones

Cherty limestones

Dolostones

Anhydrites

?

Seismostratigraphic units

Base of Pliocene

Top of


Top of

Triassic anhydrites

A

B

C

D

Vp = 1800 m/s

Thickness: variable, up to 1400 m

Vp = 4100 m/s


Vp = 5900 m/s


Vp = 6400 m/s

0

300

600

900m

3290 m

Marne a Fucoidi

Famoso 1

Plio

-Qu

ate

rna

ry

Gessoso-

Schlier

Scaglia Cinerea

Scaglia Calcarea

Maiolica

Calcari ad Aptici

RossoAmmonitico

Corniola


Messinian

Ea

rly

Lia

sciss

air T et

aL

Middle Lias

Late Lias

Dogger -

Malm

Thitonian-Barremian

Aptian-Albian

Cenomanian-middle Eocene

Late Eocene-middle Oligocene

Tortonian

0 m(–143 m)

4303 m

3126 m

Fig. 3 Lithostratigraphic correlation between exploration wells drilled in the Adriatic offshore, i.e. Famoso 1 and Eterno 1,

and in the Gargano onshore, i.e. Peschici 1 and Foresta Umbra 1 (see Fig. 2 for location). Lithostratigraphy of the Gargano

wells is derived from the original data of the ViDEPI Project (2012) modified after Bosellini et al. (1993, 2000). Seismostrati-

graphic units and their maximum thicknesses computed using interval velocities (Vp) are indicated in the left part. Vp of Unit

A, after Geletti et al. (2008); average Vp of Units B, C and D, according to Bally et al. (1986). The correlation between seismo-

stratigraphic and lithostratigraphic units is also shown.

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Terra Nova, Vol 0, No. 0, 1–10 V. Festa et al. • Diapirism in the Adriatic Sea: the Tremiti salt structure

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Plio-Pleistocene foreland basin clays

(Santantonio et al., 2013; Famoso1

and Eterno1 wells, Fig. 3).

Seismic stratigraphy

Four main seismostratigraphic units

(A–D, from the bottom; Fig. 3) were

identified in the studied area by

reviewing seismic- and well-data in

accordance with the most recent liter-

ature (e.g. Santantonio et al., 2013).

Unit A, exhibiting a semi-transpar-

ent seismic facies topped by a high

amplitude reflector (e.g. Fig. 4), is

represented by the anhydritic portion

of the Burano Fm.

Unit B, topped by a strong reflec-

tor, exhibits discontinuous and

poorly defined reflectors (Figs 4, 5a,b

and 6), and consists of Burano Fm

limestones and dolostones, Rhaetian

dolostones and Calcare Massiccio

Fm limestones (Fig. 3).

Unit C groups middle Lias to

Messinian lithostratigraphic units

(Famoso 1 and Eterno 1 wells,

Fig. 3) corresponding to the Adriatic

Basin succession. It shows well-

defined, continuous, subparallel

reflectors and is topped by strong

reflectors of the Gessoso-Solfifera

Fm (Figs 4, 5a,b and 6). In the Tre-

miti Islands, the top of the unit crops

out, in the form of an angular

unconformity between tilted Palaeo-

cene, Eocene and Miocene (Langhian

to early Tortonian) rocks below and

thin Plio-Pleistocene deposits above

(Cremonini et al.,1971; Andriani

et al., 2005; Brozzetti et al., 2006;

Miccadei et al., 2011).

Finally, Unit D consists of Plio-

Quaternary emipelagites (Famoso 1,

Eterno 1 wells, Fig. 3), and is char-

acterized by some continuous reflec-

tors, and, locally, semi-transparent

seismic facies (Figs 4, 5a,b and 6).

Seismic interpretation of theTremiti Structure

The interpretation of seismic lines

along the Tremiti Structure required

first the identification of the top of

Unit A in poorly deformed areas. In

agreement with the literature (Finetti

and Del Ben, 2005; Geletti et al.,

2008; Scisciani and Calamita, 2009),

the top of Unit A around the Tremiti

Structure has been located at c. 3.5 s

in seismic profile M13 (Fig. 4). Con-

sidering the interval velocities (Vp) of

the overlying sedimentary rocks, a

depth of ca. 4500 m has been calcu-

lated for this high amplitude reflector.

Along the Tremiti Structure

(Figs 4 and 5a,b), seismic wave dif-

fractions, reflected refractions and

velocity distortion phenomena

strongly suggest halokinesis of the

Triassic anhydrites. In addition, and

as shown on seismic profile M13, the

same seismic record may result from

a fault located above the steeply

inclined eastern flank of a halokinesis

structure, i.e. the Tremiti diapir

(Fig. 4). A chaotic and poorly

defined seismic signal typically char-

acterizes the diapir, while the reflec-

tors of the wall-rock appear

generally continuous and better

developed. Often, the reflected refrac-

tions, in association with the steeply

inclined flanks of the diapir, can be

observed crosscutting the primary

reflections of the host Unit B and the

lowermost part of Unit C (Figs 4

and 5a,b). Due to the relatively high

Vp value of the anhydrites, the

reflections related to the interbedded

dolostones are affected by velocity

pull-up phenomena within the diapir.

The top of the diapir stands at c.

1.8 s in seismic profile M13 (Fig. 4),

and between c. 0.4 and 0.8 s in the

profiles BR168-21 and BR169-32

(Fig. 5a,b). Considering the Vp value

of the overlying sediments, the roof

is at a minimum depth of c. 750 m

from the sea bottom. Therefore, the

diapir has risen up to c. 3750 m from

the Triassic anhydrite source.

On the flanks of the diapir, reflec-

tors of Unit B, which has a nearly

constant thickness, and Unit A are

geometrically concordant. In con-

trast, the overlying units C and D

exhibit variable thickness. Unit C is

definitely thinner above the diapir,

while an abrupt increase in thickness

is observed laterally, especially on the

eastern and southeastern sides (Figs 4

and 5a,b). A local thickening of this

B428 B430

0

1

2

3

4

BR169-32

s

TWTW - E

Salt

diapir

Unit D

Unit B

Unit A - anhydrites

Unit C

0

1

2

3

4

5 km

Fig. 4 Uninterpreted (above) and interpreted (below) non-migrated and multi-chan-

nel stacked seismic profile M13 (see Fig. 2 for location).

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unit can be appreciated in the western

sector of seismic profile M13, i.e. on

the hangingwalls of synsedimentary

faults showing a dip-slip component

(Fig. 4). These faults belong to a sys-

tem of NE-dipping extensional faults

(Fig. 6), which determined thickness

variations in the lower part of Unit C

(Figs 4 and 6) and likely of Unit B

(Fig. 6) during the Mesozoic exten-

sional stage linked to the Jurassic rif-

ting. The abrupt increase in thickness

observed on the eastern side of the

Tremiti Structure along seismic pro-

file M13 (Fig. 4) is additional evi-

dence of extensional tectonics.

Furthermore, a low-amplitude ridge

structure, involving the NE-dipping

faults (Fig. 6), developed with a NW–

SE trend (Fig. 7).

On the flanks of the Tremiti Struc-

ture, reflectors show that gentle drag

folds involve both Unit B (Fig. 5a,b)

and the lower part of Unit C (Figs 4

and 5a,b), which were upturned by

rising anhydrite. From the sides to

the roof of the diapir, the geometries

of reflectors within the wall-rock are

compatible with an open, asymmet-

ric anticline affecting both Unit B

and Unit C (Figs 4 and 5a,b), which

is thinner in its uppermost portion

(e.g. Fig. 5a). As shown on seismic

profile M13 (Fig. 4), compressive

minor faults have been recognized in

the eastern side of the diapir. In

Unit D, internal unconformities, and

reflectors recording upturned strata,

are locally observed. Furthermore,

the unit exhibits a decrease in thick-

ness approaching the anticline,

whose crest is truncated by an

erosional surface (Figs 4 and 5a,b).

The latter corresponds to an

unconformity below the apparently

undisturbed Plio-Quaternary sedi-

ments.

According to well-known shape

classifications of salt structures (Jack-

son and Talbot, 1991; Stewart, 2007;

Guerra and Underhill, 2012), a salt-

anticline-type geometry may be

inferred from the seismic profiles of

the Tremiti diapir, which is c. 7–

8 km wide (Fig. 5a,b). In map view,

the salt-anticline is developed for c.

30 km and its axial-plane trace is

arched with a gentle concavity

towards the NW; northwards, it

strikes NNE–SSW, whereas south-

wards, it curves towards an ENE–

WSW trend (Fig. 7). A strong

asymmetry of this salt-anticline can

be appreciated in seismic profile M13

(Fig. 4), i.e. along the intermediate

part of the NE–SW-striking Tremiti

diapir (Fig. 7).

Discussion: age and mode ofhalokinesis

Two stages of halokinesis of the Tri-

assic anhydrites can be recognized in

the Tremiti Islands area.

0

1

2

BR127

NW - SE

Salt

diapir

s

TWT

5 km

0

1

2

NW - SE

BR168-10B428M13

s

TWT

Salt

diapir

0

1

2

5 km

BR168-10

Unit D

Unit B

Unit C

Unit D

Unit B

Unit C

(a)

(b)

Fig. 5 (a) Uninterpreted (above) and interpreted (below) non-migrated and multi-

channel stacked seismic profile BR169-32 (see Fig. 2 for location). (b) Uninter-

preted (left) and interpreted (right) non-migrated and multi-channel stacked seismic

profile BR168-21 (see Fig. 2 for location).

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The older one is characterized by a

low-amplitude ridge structure

(Fig. 6), striking parallel to the

ancient, extensional NE-dipping

faults (Figs 6 and 7), and related to

the early Jurassic rifting (Santantonio

et al., 2013). The ridge is bordered to

the NE by the fault that records the

maximum dip-slip displacement

(Fig. 6). In accordance with several

models of diapirism in extensional

tectonic settings (e.g. Vandeville and

Jackson, 1992; Schultz-Ela and Jack-

son, 1996; Rowan et al., 1999; Stew-

art, 2007; Guerra and Underhill,

2012), this kind of fault could have

promoted migration of the salt

towards the hangingwall. Here, the

low-amplitude ridge likely developed

in Unit B during the deposition of

Unit C, namely during the regional

subsidence that followed the main

fault displacement (Fig. 8).

The younger halokinesis stage

began during the late Miocene. The

internal unconformities in Unit D

and its thinning approaching the Tre-

miti diapir (e.g. Fig. 4) indicate that

the salt-anticline grew during the

Plio-Quaternary due to the upward

movement of the Triassic anhydrites

(Fig. 9). However, on the Tremiti

Islands, the angular unconformity

separating early Tortonian deformed

rocks from less-deformed Pliocene

deposits indicates that this halokinesis

deformation began before the Plio-

cene. Moreover, the diapirism seems

to be still active as, on high-resolution

seismic profiles, deposits of the post-

last glacial interval show weak defor-

mations that also involve the sea floor

(Ridente and Trincardi, 2006).

Late Paleogene–Neogene halokine-

sis structures found in the Adriatic

Sea, north of the Tremiti Islands, by

Geletti et al. (2008, and references

therein; Fig. 1) could have been

enhanced by horizontal shortening

linked to either the Apenninic or Din-

aric orogenesis (Scrocca, 2006; Gran-

dic and Kolbah, 2009). In such a

setting, the axes of salt-anticlines

strike perpendicular to the regional

shortening direction, as demonstrated

also by Jahani et al. (2009) in the Per-

sian Gulf (i.e. the foreland basin of

the Zagros orogen). In the Adriatic

Sea, these NW–SE-striking salt-anti-

clines developed mainly on top of

pre-existing NW–SE-striking diapirs,

elongated like the old low-amplitude

salt ridge in the Tremiti area.

In contrast, despite the presence of

the old salt ridge, the axis of the

younger Tremiti salt-anticline strikes

roughly NE–SW, and is perpendicu-

lar to the Apennines front. This

geometry is coherent with NW–SE

shortening (Fig. 7), whose occurrence

in the area could be related to the

presence of an active tectonic bound-

ary deduced by seismicity and sepa-

rating the Adriatic into north and

south blocks with different velocity

motions (Oldow et al., 2002). In

addition, this shortening is in accor-

dance with the local component of

the E-W right-lateral simple shear

inferred by several authors (Mele

et al., 1990; Argnani et al., 1993; Fa-

vali et al., 1993; Doglioni et al.,

1994; Gambini and Tozzi, 1996).

The mode of emplacement of the

Tremiti diapir, reconstructed in

accordance with the NW–SE short-

ening direction (Fig. 9), is mainly

constrained by the interpretation of

seismic profile M13 (Fig. 4). The

emplacement needed a NE–SW-ori-

ented zone of weakness for the

upward migration of the anhydrites

(Figs 7 and 9). The abrupt increase

in thickness of Unit C on the south-

eastern side of the Tremiti diapir

(Figs 4 and 5a,b) strongly supports

the presence of an ancient NE–SW-

striking extensional fault (Figs 7 and

9). This inferred fault strikes subpar-

allel to the normal faults accompany-

ing the widespread NW–SE dip-slip

faults activated during the Jurassic–

0

1

2

3

4

1

2

3

4

5 km

s

TWTSW - NE

Unit D

Unit B

Unit A - anhydrites

Unit C

Fig. 6 (a) Uninterpreted (above) and interpreted (below) non-migrated and multi-

channel stacked seismic profile B426 (see Fig. 2 for location).

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Cretaceous (Festa, 2003; Santantonio

et al., 2013). Much later, during the

NW-SE shortening, the anhydrites

migrated in the footwall of the fault,

beneath Unit B (Fig. 9). Above the

southeastern flank of the diapir, the

growth of the anhydritic body deter-

mined an upward propagation, with

a dip-slip displacement, of the

ancient fault (Fig. 9). Drape upbend-

ing of Units B and C occurred, and

an asymmetric salt-anticline devel-

oped (Figs 4 and 9). In addition, the

NW–SE shortening may have led to

the arching of this fault, which has a

gentle concavity towards the NW

(Fig. 7).

Towards the north-east and south-

west terminations of the salt-anticline

(Fig. 7), the anhydrites simply used

the weakened zone of the ancient

fault as a preferential channel for

their upward migration through Unit

B (e.g. Fig. 10). Upward dragging of

Unit B, piercing of the lower part of

Unit C, and folding of the intermedi-

ate and upper parts of this unit also

occurred (Fig. 5a,b). In addition, in

the south-west termination of the

salt-anticline, an inversion of the

ancient dip-slip fault, which occurred

during piercing of the anhydrites,

would explain both the highest posi-

tion of Unit C, and the thinness of

Unit D in the hangingwall, compared

with the footwall (Fig. 10).

Concluding remarks

The occurrence of the Tremiti ridge

and its outstanding size are the

result of late Miocene to present-day

salt tectonics overprinting a Meso-

zoic low-amplitude salt ridge. A

halokinesis structure, the Tremiti

diapir, made up of Triassic anhy-

drites, is located beneath this ridge.

The Tremiti diapir forms an anti-

cline whose axis is approximately

perpendicular to both the elonga-

tions of most of the Neogene dia-

pirs, and the Apenninic and Dinaric

fronts, which strike NW–SE in the

sector of the Adriatic Sea north of

Gargano Promontory. The develop-

ment of this diapir required NW–SE

shortening, and occurred along a

pre-existing SE-dipping extensional

fault, whose origin dates back to the

Jurassic–Cretaceous. In its central

part, the diapir was emplaced in the

footwall of this fault. Both shorten-

Shortening

BR169-32

BR168-21

M13

Fig. 4

Fig. 5b

B42

6

Fig. 6

10 km

N

dip-slip faultsMesozoic

15°1

3’2

4”

42°02’38”

15°5

8’4

9”

42°26’09”

AnticlineaxisM

esozoic low-am

plitude ascent of the

Fault

Tremiti diapir

Fig. 9

Fig. 9

anhydritic ridge

Fig.

8

favouring the

Saltanticline,i.e. Tremitidiapir

Fig. 10Tremitidiapir

Tremitiridge

Fig. 5a

TremitiIslands

Fig. 7 Structural sketch map of the Tremiti Islands area, where the old Mesozoic

anhydritic low-amplitude ridge and the younger Neogene Tremiti diapir (roughly

corresponding to the Tremiti ridge) are emphasized in grey. Note the geometric

relationships between the dip-slip Mesozoic faults and the coeval salt low-ampli-

tude ridge, and between the Tremiti diapir and the fault that favoured its rising up.

Unit B

Unit C

Early Jurassic

Unit C

Cretaceous

Unit A

5 km NESW

s.l.

s.l.

Fig. 8 2D frames summarizing the mode of emplacement of the low-amplitude

ridge, from early Jurassic to Cretaceous. Reconstruction is based on the interpreta-

tion of the seismic reflection profile in Fig. 6, and is perpendicular to the elonga-

tion of the Mesozoic anhydritic low-amplitude ridge (see Fig. 7).

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ing and upward growth of the diapir

were able to uplift the entire foot-

wall. As a consequence, upward

propagation of the fault with dip-

slip kinematics occurred. Towards

the terminations of the diapir, the

fault, which was locally reactivated

with reverse kinematics, represented

a path for the upward migration

and squeezing of the anhydrites,

which pierced and folded the above

wall-rock.

These results could represent an

interpretive key for the scattered

halokinetic structures occurring in

the Adriatic Basin, north of the

Tremiti Islands. NW-SE-elongated

diapirs originally developed during

the Mesozoic in the form of low-

amplitude ridges, whose geometric

features were driven by the activity

of extensional faults. During the

Neogene, two sets of diapirs with

opposite elongations developed. The

most representative set consists of

halokinesis structures that grew on

top of, and parallel to, the pre-exist-

ing low-amplitude diapirs. Their fold

axes strike NW–SE, i.e. perpendicu-

lar to the shortening direction due to

the opposite propagation of the

Apenninic and Dinaric fronts. In

contrast, NW–SE shortening could

have locally promoted both salt

mobilization and NE–SW-elongated

salt-anticlines representing the other

set. These halokinesis structures

developed parallel to the Tremiti dia-

pir, likely along Jurassic–Cretaceous

faults.

Acknowledegments

This study was supported by “Convenzi-

one tra Autorit�a di Bacino della Puglia e

Dipartimento Geomineralogico dell’Uni-

versit�a degli Studi di Bari per studi

Pleistocene

Present-days.l.

s.l.

Unit D

Late Miocene

Pliocene

Unit C

Unit B

Unit A

10 km SENW

s.l.

s.l.

Fig. 9 2D frames summarizing the mode of emplacement of the Tremiti diapir, from late Miocene to present-day. Reconstruc-

tion is based on the interpretation of the seismic profile M13 (Fig. 4), and is subparallel to the elongation of the old Mesozoic

anhydritic low-amplitude ridge (see Fig. 7).

5 km SENW

s.l.

Unit C

Unit B

Unit A

Unit D

Fig. 10 2D schematic interpretation of the seismic profile BR169-32 (Fig. 5a),

crossing the southwestern termination of the Tremiti diapir (see Fig. 7 for loca-

tion). The path taken during upward migration and squeezing of the anhydrites is

indicated by the blue arrows, near the fault plane. Note in Unit C, piercing and

folding due to the Tremiti diapir. The inversion of the originally dip-slip fault is

indicated by the red arrow. The highest position of Unit C, and the thinness of

Unit D in the hangingwall, compared with the footwall, can be appreciated.

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petrografici e mineralogici, oltre che

geologico-strutturali, nell’area di Lesina

Marina (FG) – 2009” research funds, to

V. Festa. We are grateful to T. Alves, L.

Ferranti and an anonymous reviewer,

whose suggestions helped us to improve

the manuscript. Discussions with D.

Scrocca, J. Underhill and S. Nardon were

very useful.

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Received 4 June 2013; revised version

accepted 21 October 2013



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‚ Type the replacement text into the blue box that

appears.

This will open up a panel down the right side of the document. The majority of

tools you will use for annotating your proof will be in the Annotations section,

rkevwtgf"qrrqukvg0"YgÓxg"rkemgf"qwv"uqog"qh"vjgug"vqqnu"dgnqy<

2. Strikethrough (Del) Tool Î for deleting text.

Strikes a red line through text that is to be

deleted.

How to use it

‚ Highlight a word or sentence.

‚ Click on the Strikethrough (Del) icon in the

Annotations section.

3. Add note to text Tool Î for highlighting a section

to be changed to bold or italic.

Highlights text in yellow and opens up a text

box where comments can be entered.

How to use it

‚ Highlight the relevant section of text.

‚ Click on the Add note to text icon in the


‚ Type instruction on what should be changed

regarding the text into the yellow box that

appears.

4. Add sticky note Tool Î for making notes at

specific points in the text.

Marks a point in the proof where a comment

needs to be highlighted.

How to use it

‚ Click on the Add sticky note icon in the


‚ Click at the point in the proof where the comment

should be inserted.

‚ Type the comment into the yellow box that

appears.

http://get.adobe.com/reader/

USING e-ANNOTATION TOOLS FOR ELECTRONIC PROOF CORRECTION

For further information on how to annotate proofs, click on the Help menu to reveal a list of further options:

5. Attach File Tool Î for inserting large amounts of

text or replacement figures.

Inserts an icon linking to the attached file in the

appropriate pace in the text.

How to use it

‚ Click on the Attach File icon in the Annotations

section.

‚ Enkem"qp"vjg"rtqqh"vq"yjgtg"{qwÓf"nkmg"vjg"cvvcejgf"file to be linked.

‚ Select the file to be attached from your computer

or network.

‚ Select the colour and type of icon that will appear

in the proof. Click OK.

6. Add stamp Tool Î for approving a proof if no

corrections are required.

Inserts a selected stamp onto an appropriate

place in the proof.

How to use it

‚ Click on the Add stamp icon in the Annotations

section.

‚ Select the stamp you want to use. (The Approved

stamp is usually available directly in the menu that

appears).

‚ Enkem"qp"vjg"rtqqh"yjgtg"{qwÓf"nkmg"vjg"uvcor"vq"appear. (Where a proof is to be approved as it is,

this would normally be on the first page).

7. Drawing Markups Tools Î for drawing shapes, lines and freeform

annotations on proofs and commenting on these marks.

Allows shapes, lines and freeform annotations to be drawn on proofs and for

comment to be made on these marks..

How to use it

‚ Click on one of the shapes in the Drawing

Markups section.

‚ Click on the proof at the relevant point and

draw the selected shape with the cursor.

‚ To add a comment to the drawn shape,

move the cursor over the shape until an

arrowhead appears.

‚ Double click on the shape and type any

text in the red box that appears.

Education

Festa et al., 2013 - Draft