Reassessing Depositional Conditions of the Pre-Apulian Zone Based on Synsedimentary Deformation Structures during Upper Paleocene to Lower Miocene Carbonate Sedimentation, from Paxoi and Anti-Paxoi Islands, Northwestern End of Greece

: of the SSD structures. The conﬁnement of the lower Miocene deposits, both northwards and southwards (in Anti-Paxoi Island), indicates the presence of active transfer faults, with ﬂower structure geometry, that were formed during sedimentation, producing highs and troughs. The present open anticline geometry of Paxoi Island indicates that the Island represents the forebulge area of the middle Miocene Ionian Foreland due to Ionian Thrust activity. regime to the compressional regime with the reactivation of normal faults as reverse faults (inverted tectonic) and the gradual change of the studied area from the Apulian platform margins to the forebulge area of the Ionian foreland. Stage ( c ) represents the present morphology of the studied area where the islands Paxoi and Anti-Paxoi formed an open anticline geometry due to the Ionian thrust movement.


Introduction
Soft sediment deformation (SSD) structures are mostly studied and identified in clastic deposits, in which soft-sediment deformation structures are saturated with water. The The Pre-Apulian (or Paxoi) zone is the continuation of the Apulian platform and its transition to the Ionian Basin through some edge-slope facies that are exposed in several Ionian Islands, mainly in the southwestern margins of the Hellenic FTB (e.g., Kefalonia, Zakynthos) and south of Corfu (Paxoi islands). This transitional zone is absent from the NW part (Corfu Island), suggesting that the Ionian formations are directly over-thrusting over the South Apulia basin [33].
Strike-slip faults have also controlled the regional tectonic setting. The South Salento-North Corfu fault system [34] and smaller scale strike-slip faults have dissected the Ionian Thrust [35,36]. Furthermore, the Kefalonia transfer fault (KTF) to the south separates Western Greece in an ocean-continent subduction and a continent-continent collision regime, whereas the Borsh-Khardhiqit strike-slip fault to the north of Corfu controls the evolution of the broader region ( Figure 2).
Based on seismic data, Kokkinou et al. [37] have suggested that normal faults that influenced Mesozoic deposits were reactivated as thrust faults during the Eocene to Miocene and were further reactivated as normal faults during the Plio-Quaternary. In addition, Basilone and Sulli [38] and Bourli et al. [36] suggested that Mesozoic normal and transfer faults were re-activated during the compressional stage as thrust or back-thrusts and strike-slip faults, respectively.
Lefkas, Kefalonia, and Zakynthos islands, in the Ionian Sea, where both the Ionian Thrust (IT) and the KTF are outcropped, are the keys for studying the regional structural evolution. This remote area has been the target of previous expeditions resulting in diverging structural interpretations [37]. Additionally, Paxoi and Anti-Paxoi islands are situated far from the interaction and influence of KTF, and only the Ionian thrust seems to be influencing the islands.
Furthermore, it has been observed that the thrusting activity of the branches of the main Ionian Thrust has led to the evolution of smaller, confined sub-basins, at least as it has been recorded on Kefalonia Island [39].
Collisional deformation across the Ionian Islands was recognized in seismic profiles, revealing the different structures near and far from the KTF [33,40,41].
The Ionian Basin (IB) is bounded westwards by the Ionian Thrust and eastwards by the Gavrovo Thrust ( Figure 2). The Pre-Apulian or Paxoi zone to the west of the Ionian Basin is regarded as the eastern margin of the Apulian platform, in Albania, Croatia, and Italy, where similar rocks occur [40,[42][43][44]. The APM consists of Triassic to Miocene deposits, mainly neritic carbonate rocks ( Figure 3).  According to Karakitsios et al. [46], a characteristic slump horizon was observed in the Anti-Paxoi Island (Pre-Apulian zone, Western Greece), which could be followed in a zone of about 2000 m, at the eastern coast of the Island, and is overlain and underlain by undeformed strata. This slump has an average thickness of 15 m and a width of 200 m. Deformation axes present an NNW-SSE direction, coinciding with the general direction According to Karakitsios et al. [46], a characteristic slump horizon was observed in the Anti-Paxoi Island (Pre-Apulian zone, Western Greece), which could be followed in a zone of about 2000 m, at the eastern coast of the Island, and is overlain and underlain by undeformed strata. This slump has an average thickness of 15 m and a width of 200 m. Deformation axes present an NNW-SSE direction, coinciding with the general direction of the Pre-Apulian zone. Based on their biostratigraphic analysis, they believe that the slump and the surrounding sediments have an Early Oligocene age.

Depositional Conditions and Age Determination
The depositional environment conditions of the carbonate sequence in Paxoi and Anti-Paxoi islands were based on the microfacies analysis, whereas the taphonomy and paleoecology of the microfauna were also used in order to find the depositional environments and dynamic conditions in different positions across the basin and to support the previous lithofacies results. Additionally, the results were used for the revision of the existing geological maps.
Biostratigraphic results of the studied thin sections showed that sedimentation of the studied sequences from the two Islands ranged from the upper Paleocene (Thanetian) to lower Miocene (Aquitanian) ( Table 1). It seems that the younger deposits are restricted in the northern part of the Paxoi Island and in the Anti-Paxoi Island as well as ( Figure 4). There is a transition from the Paleocene (in the central part of Paxoi Island, sample P25) to the Eocene, then to the Oligocene and finally to the lower Miocene (northwards or southwards) (Figures 4 and 5). The results indicate that during the Miocene, the basin was restricted both northwards and southwards.   The microfacies analysis (Table 1) showed that the standard microfacies that prevail in the studied area are SMF3,4,5, and in only one case SMF6 was determined, indicating deposition in zones FZ1, FZ3, and FZ4. In addition, one sample (P24) was determined as SMF18-19 that introduces FZ8 ( Figure 6). In general, depositional environments correspond to deep-sea, toe of slope, and slope environments. Sample P24 classified as FZ8 representing the platform interior and especially the restricted area of the platform is of late Eocene age ( Figure 4). The age determination was based on a detailed analysis, mainly on foraminifera, where characteristic fossils assemblages were determined.  The microfacies analysis (Table 1) showed that the standard microfacies that prevail in the studied area are SMF3,4,5, and in only one case SMF6 was determined, indicating deposition in zones FZ1, FZ3, and FZ4. In addition, one sample (P24) was determined as SMF18-19 that introduces FZ8 ( Figure 6). In general, depositional environments correspond to deep-sea, toe of slope, and slope environments. Sample P24 classified as FZ8 representing the platform interior and especially the restricted area of the platform is of late Eocene age ( Figure 4). The age determination was based on a detailed analysis, mainly  (a) Sample AP1 shows a pelagic wackestone with planktonic foraminifera, SMF3/FZ1 (X40); (b) Sample P3 shows a pelagic wackestone with planktonic foraminifera, SMF3/FZ3 (X40); (c) Sample P2 shows a bioclastic and lithoclastic packstone with planktonic and a few benthic foraminifera, SMF4/FZ3 (X40); (d) Sample P14 shows a bioclastic and lithoclastic packstone with planktonic and benthic foraminifera, SMF4/FZ4 (X40); (e) Sample P1 shows a bioclastic and lithoclastic packstone with planktonic and benthic foraminifera, SMF5/FZ4 (X40); (f) Sample P17 shows a packstone-rudstone with benthic foraminifera, mollusks and mollusk fragments, SMF6/FZ4 (X40).
The absence of lateral or vertical changes in the depositional conditions from the Paleocene to the Miocene, as facies zones changed independently with the age, introduce mostly the regional tectonic influence in this part of the APM than the total changes of the APM configuration, as it can be seen in Kefalonia Island (see their position in Figure 2).
The presence of an Eocene sample representing the platform Interior indicates the presence of a large exoclast, which supports the idea of the above-introduced regional tectonic influence but even more introduces the close position of the Apulian platform.

Soft Sediment Deformation Structures
The study of SSD structures is presented independently for the two islands, due to the fact that in the Anti-Paxoi Island there are only lower Miocene deposits, whereas in Paxoi Island there are SSD structures in Eocene to lower Miocene deposits ( Figure 4). Both Islands present an elongated geometry with a general NNW-SSE direction ( Figure 4). In both islands, there are cliffs at both the western and eastern coasts, with up to 80 m thick limestones, where the SSD structures are outcropping. These SSD structures could be (a) Sample AP1 shows a pelagic wackestone with planktonic foraminifera, SMF3/FZ1 (X40); (b) Sample P3 shows a pelagic wackestone with planktonic foraminifera, SMF3/FZ3 (X40); (c) Sample P2 shows a bioclastic and lithoclastic packstone with planktonic and a few benthic foraminifera, SMF4/FZ3 (X40); (d) Sample P14 shows a bioclastic and lithoclastic packstone with planktonic and benthic foraminifera, SMF4/FZ4 (X40); (e) Sample P1 shows a bioclastic and lithoclastic packstone with planktonic and benthic foraminifera, SMF5/FZ4 (X40); (f) Sample P17 shows a packstonerudstone with benthic foraminifera, mollusks and mollusk fragments, SMF6/FZ4 (X40).
The absence of lateral or vertical changes in the depositional conditions from the Paleocene to the Miocene, as facies zones changed independently with the age, introduce mostly the regional tectonic influence in this part of the APM than the total changes of the APM configuration, as it can be seen in Kefalonia Island (see their position in Figure 2).
The presence of an Eocene sample representing the platform Interior indicates the presence of a large exoclast, which supports the idea of the above-introduced regional tectonic influence but even more introduces the close position of the Apulian platform.

Soft Sediment Deformation Structures
The study of SSD structures is presented independently for the two islands, due to the fact that in the Anti-Paxoi Island there are only lower Miocene deposits, whereas in Paxoi Island there are SSD structures in Eocene to lower Miocene deposits ( Figure 4). Both Islands present an elongated geometry with a general NNW-SSE direction ( Figure 4). In both islands, there are cliffs at both the western and eastern coasts, with up to 80 m thick limestones, where the SSD structures are outcropping. These SSD structures could be traced for at least 2 km, although their appearance is interrupted by coasts with different directions. Most of the long coasts (up to 3 km long) have an NNW-SSE direction, parallel to the NNW-SSE directed normal faults. Shorter coasts (up to 800 m long) with an ENE-WSW direction were formed due to transfer faults with the same ENE-ESW directions (Figure 4). Figure 7 shows the used lines and symbols for the interpretation of all photos that are used for the depiction of structures in both islands.  Figure 4). Figure 7 shows the used lines and symbols for the interpretation of all photos that are used for the depiction of structures in both islands.     traced for at least 2 km, although their appearance is interrupted by coasts with different directions. Most of the long coasts (up to 3 km long) have an NNW-SSE direction, parallel to the NNW-SSE directed normal faults. Shorter coasts (up to 800 m long) with an ENE-WSW direction were formed due to transfer faults with the same ENE-ESW directions ( Figure 4). Figure 7 shows the used lines and symbols for the interpretation of all photos that are used for the depiction of structures in both islands.

Paxoi Island SSD Structures Description
SSD horizons have been observed either between undeformed horizons ( Figure 8) or with the one over the other (Figure 9), with strong erosional contacts, and which are related with normal fault activity, showing a westward progradation.   traced for at least 2 km, although their appearance is interrupted by coasts with different directions. Most of the long coasts (up to 3 km long) have an NNW-SSE direction, parallel to the NNW-SSE directed normal faults. Shorter coasts (up to 800 m long) with an ENE-WSW direction were formed due to transfer faults with the same ENE-ESW directions ( Figure 4). Figure 7 shows the used lines and symbols for the interpretation of all photos that are used for the depiction of structures in both islands.

Paxoi Island SSD Structures Description
SSD horizons have been observed either between undeformed horizons ( Figure 8) or with the one over the other (Figure 9), with strong erosional contacts, and which are related with normal fault activity, showing a westward progradation.   Commonly, the SSD structures were produced from the uplifted footwall block and stopped their migration-progradation at the subsiding hanging wall block of a neighboring fault ( Figure 10). Commonly, the SSD structures were produced from the uplifted footwall block and stopped their migration-progradation at the subsiding hanging wall block of a neighboring fault (Figure 10). Synthetic and antithetic faults produced troughs and influenced the movements of the SSD structures ( Figure 11). The thin SSD horizons within the Eocene deposits are characterized by sharp contacts, both with the underlying and the overlying thin to medium bedded limestones (Figure 12). Synthetic and antithetic faults produced troughs and influenced the movements of the SSD structures ( Figure 11). Commonly, the SSD structures were produced from the uplifted footwall block and stopped their migration-progradation at the subsiding hanging wall block of a neighboring fault ( Figure 10).  The thin SSD horizons within the Eocene deposits are characterized by sharp contacts, both with the underlying and the overlying thin to medium bedded limestones (Figure 12). The thin SSD horizons within the Eocene deposits are characterized by sharp contacts, both with the underlying and the overlying thin to medium bedded limestones ( Figure 12).
Finally, there are characteristic horizons where the progradation of the deformation took place with an eastward direction, and within the same horizon undeformed limestones developed laterally (Figure 13).

Anti-Paxoi Island SSD Structures Description
In the small Anti-Paxoi Island where only lower Miocene deposits are outcropping, the SSD structures are very thick and strong (Figures 14-18) and were recognized in Miocene deposits. In detail, Most of the SSD structures showed eastward progradation directions with their movements towards the subsiding fault plane of normal faults that present westward dipping surface planes. The thickness of these strong SSD deformation structures are up to 10 m ( Figure 14a) and more than 250 m wide. The overlying deposits are characterized by erosional contacts with the SSD structures (Figure 14a).
Synthetic and antithetic faults produced troughs and influenced the movements of the SSD structures ( Figure 15). Normal faults are responsible for the instability of the basin floor and the SSD structures development, whereas the antithetic faults act as the barge where the movement stopped.

Anti-Paxoi Island SSD Structures Description
In the small Anti-Paxoi Island where only lower Miocene deposits are outcropping, the SSD structures are very thick and strong (Figures 14-18) and were recognized in Miocene deposits. In detail, Figure 12. (a,b) in both photos a thin SSD structure is presented, between undeformed, thin to medium bedded, limestones, and with no erosional contacts with the over-and the under-lying beds. SSD structures were recognized in Eocene deposits. Finally, there are characteristic horizons where the progradation of the deformation took place with an eastward direction, and within the same horizon undeformed limestones developed laterally ( Figure 13).

Anti-Paxoi Island SSD Structures Description
In the small Anti-Paxoi Island where only lower Miocene deposits are outcropping, the SSD structures are very thick and strong (Figures 14-18) and were recognized in Miocene deposits. In detail,      There are SSD structures, up to 3 m thick and up to 70 m wide, that are characterized by sharp contacts with the underlying undeformed deposits, erosional contacts with the overlying deposits ( Figure 16). Synthetic and antithetic normal faults acting synchronously with the deformation produced the necessary instability conditions for the slump triggering. Within these horizons, there are no clear evidences for the progradation direction, probably because they must have developed far away from the starting point and present a wide range of progradation.   Most of the SSD structures showed eastward progradation directions with their movements towards the subsiding fault plane of normal faults that present westward dipping surface planes. The thickness of these strong SSD deformation structures are up to 10 m (Figure 14a) and more than 250 m wide. The overlying deposits are characterized by erosional contacts with the SSD structures (Figure 14a).
Synthetic and antithetic faults produced troughs and influenced the movements of the SSD structures ( Figure 15). Normal faults are responsible for the instability of the basin floor and the SSD structures development, whereas the antithetic faults act as the barge where the movement stopped.
There are SSD structures, up to 3 m thick and up to 70 m wide, that are characterized by sharp contacts with the underlying undeformed deposits, erosional contacts with the overlying deposits ( Figure 16). Synthetic and antithetic normal faults acting synchronously with the deformation produced the necessary instability conditions for the slump triggering. Within these horizons, there are no clear evidences for the progradation direction, probably because they must have developed far away from the starting point and present a wide range of progradation.
There are also a few examples where the SSD structures, up to 4 m thick and 50 m wide, produced strong deformation to the underlying deposits, with high relief surfaces (up to 50 cm), whereas the erosional contact with the overlying deposits is seen with low relief surfaces (Figure 17).
It seems that when the SSD structures were strong and as they started their movement from the uplifted footwall of a normal fault, they could bypass the subsiding area of the hanging wall, overstepping the uplifted footwall of the neighboring normal fault, and There are also a few examples where the SSD structures, up to 4 m thick and 50 m wide, produced strong deformation to the underlying deposits, with high relief surfaces (up to 50 cm), whereas the erosional contact with the overlying deposits is seen with low relief surfaces (Figure 17).
It seems that when the SSD structures were strong and as they started their movement from the uplifted footwall of a normal fault, they could bypass the subsiding area of the hanging wall, overstepping the uplifted footwall of the neighboring normal fault, and progradating until they reached the next block ( Figure 18).
Finally, there are also a few cases where two SSD horizons show opposite progradation directions and which are situated close to normal faults and probably could be related with the normal fault activity, occupying the existing space in every case and following the direction of the basement surface inclination (Figure 19). The alternative idea that the normal fault acted later and after the SSD structures must be excluded, as after the development of SSD structures, the whole area was influenced by a compressional regime, and the expected faults must have been reverse faults. Figure 19. Two deformed horizons with undeformed deposits between them. It seems that the SSD structures were produced on the uplifted footwall of a normal fault. Notice the two internal deformation structures within the lower structure. It seems that each of them tried to fill up the existing space due to fault activity, giving the sense of two different directions of progradation.

General Results Based on the SSD Structures
The deformation structures (Figures 8 and 19) developed as gravity flows, during the rift stage, and presented thicker and stronger deformation within their final stage of development, as displayed by the lower Miocene deposits. There are at least five different SSD horizons, and most of them have been recognized in lower Miocene deposits; their thicknesses could reach 10 m, their width could be as wide as 300 m, and they could be traced across 2-3 km (see Figures 14,15 and 18).
As there are many synsedimentary faults and although SSD structures could be traced for many kilometers, it is not clear if the above SSD structures are different horizons or if they are the same. At least three different horizons, in lower Miocene deposits, and two in Eocene deposits, were recognized.

Discussion
The boundary-margins of the stable Apulian platform with the Ionian Basin are so far considered as the Pre-Apulian platform e.g., Refs. [40,53]. The platform was influenced by inverted tectonics and particularly by an extensional regime (Jurassic to middle Eocene to the east and the early Miocene to the west) ( Figure 20a) to a compressional regime (middle Eocene to middle Miocene, from east to west) (Figure 20b). This shift in the tectonic regime has revealed characteristic structures. The compressional regime migrated from east to west, started its activity during the middle Eocene in the eastern part and reaching during the middle Miocene the western parts of the Ionian Basin. During the above described change of the tectonic regime, the pre-existing normal faults were reactivated as thrust faults and the respective transfer faults as strike-slip faults, producing different structures [36]. The type of these structures depends on both the existing displacement of the marginal normal faults and the proximity of the IT to the KTF. Figure 19. Two deformed horizons with undeformed deposits between them. It seems that the SSD structures were produced on the uplifted footwall of a normal fault. Notice the two internal deformation structures within the lower structure. It seems that each of them tried to fill up the existing space due to fault activity, giving the sense of two different directions of progradation.

General Results Based on the SSD Structures
The deformation structures (Figures 8 and 19) developed as gravity flows, during the rift stage, and presented thicker and stronger deformation within their final stage of development, as displayed by the lower Miocene deposits. There are at least five different SSD horizons, and most of them have been recognized in lower Miocene deposits; their thicknesses could reach 10 m, their width could be as wide as 300 m, and they could be traced across 2-3 km (see Figures 14,15 and 18).
As there are many synsedimentary faults and although SSD structures could be traced for many kilometers, it is not clear if the above SSD structures are different horizons or if they are the same. At least three different horizons, in lower Miocene deposits, and two in Eocene deposits, were recognized.

Discussion
The boundary-margins of the stable Apulian platform with the Ionian Basin are so far considered as the Pre-Apulian platform e.g., Refs. [40,53]. The platform was influenced by inverted tectonics and particularly by an extensional regime (Jurassic to middle Eocene to the east and the early Miocene to the west) ( Figure 20a) to a compressional regime (middle Eocene to middle Miocene, from east to west) (Figure 20b). This shift in the tectonic regime has revealed characteristic structures. The compressional regime migrated from east to west, started its activity during the middle Eocene in the eastern part and reaching during the middle Miocene the western parts of the Ionian Basin. During the above described change of the tectonic regime, the pre-existing normal faults were reactivated as thrust faults and the respective transfer faults as strike-slip faults, producing different structures [36]. The type of these structures depends on both the existing displacement of the marginal normal faults and the proximity of the IT to the KTF.
The presence of normal faults, cross cutting the SSD structures (Figures 14 and 21), indicates that at least until the lower Miocene, the studied area was influenced only by extensional tectonism, supporting the idea that the compressional regime in the studied area arrived after sedimentation was completed and probably during the middle Miocene.
The fact that there is a gradual restriction of the basin both northwards and southwards, and from the upper Paleocene to the early Miocene, indicate that this restriction took place during sedimentation and could be related with the activity of transfer faults. These transfer faults had a flower structure geometry with a positive structure in the central part of the Paxoi Island and a negative structure (Figures 21d and 22) between the two islands and in the northern side of Paxoi Island (Figure 23).
These transfer faults were reactivated during the compressional regime as strike-slip faults. These transfer faults with a negative flower structure geometry could be the reason for the outcropped Paleocene deposits in the central part of the Paxoi Island (Figure 4).
Relating the fact that the present geomorphology of the Paxoi Island shows an anticline geometry without any obvious activity of thrust faults, which could be related with the activity of the Ionian thrust. Thus, the activity of the Ionian thrust produced in the studied area the forebulge area, supporting the idea of the produced anticlinal geometry as a response to the shortening due to the Ionian thrust activity (Figure 20c). The presence of normal faults, cross cutting the SSD structures ( Figures 14 and 21), indicates that at least until the lower Miocene, the studied area was influenced only by extensional tectonism, supporting the idea that the compressional regime in the studied area arrived after sedimentation was completed and probably during the middle Miocene.  The presence of normal faults, cross cutting the SSD structures ( Figures 14 and 21), indicates that at least until the lower Miocene, the studied area was influenced only by extensional tectonism, supporting the idea that the compressional regime in the studied area arrived after sedimentation was completed and probably during the middle Miocene.  The fact that there is a gradual restriction of the basin both northwards and southwards, and from the upper Paleocene to the early Miocene, indicate that this restriction took place during sedimentation and could be related with the activity of transfer faults. These transfer faults had a flower structure geometry with a positive structure in the central part of the Paxoi Island and a negative structure (Figures 21d and 22) between the two islands and in the northern side of Paxoi Island (Figure 23).    The fact that there is a gradual restriction of the basin both northwards and southwards, and from the upper Paleocene to the early Miocene, indicate that this restriction took place during sedimentation and could be related with the activity of transfer faults. These transfer faults had a flower structure geometry with a positive structure in the central part of the Paxoi Island and a negative structure (Figures 21d and 22) between the two islands and in the northern side of Paxoi Island (Figure 23).    wards, and from the upper Paleocene to the early Miocene, indicate that this restriction took place during sedimentation and could be related with the activity of transfer faults. These transfer faults had a flower structure geometry with a positive structure in the central part of the Paxoi Island and a negative structure (Figures 21d and 22) between the two islands and in the northern side of Paxoi Island (Figure 23).    The presence of the platform interior (sample P24) could be related with the Apulian platform, which is indicated to be very close to the studied region.
According to the previously published results from the Ionian Basin [14], it seems that although the previous work referred to SSD structures developed internally to the Ionian Basin, during the Cretaceous to Paleocene, the mechanism remains the same. In both regions, the produced SSD structures were related to fault activity and were produced from the uplifted footwall block. They were flowed towards the subsided hanging wall of a neighboring normal fault, and many times when the deformation was very strong, they overstepped the space in between and continued progradating to the next hanging wall until either slumping ended.
According to the previous results by Karakitsios et al. [46], there are two subjects that should be mentioned. One is the thickness and the second is the age. In relation with the thickness (15 m thick), the difference could be explained with the fact that there are SSD structures one above the other, either with the presence of undeformed horizons between them or with an erosional contact between them. In relation to age, their age determination (early Oligocene) was based on nannofossils, whereas the present study (early Miocene for the selected samples from the northeastern part of the Anti-Paxoi Island) relied on a detailed analysis based mainly on foraminifera, where characteristic fossils assemblages (e.g., Paragloborotalia kugleri, Paragloborotalia mayeri, Trilobatus primordius, Trilobatus trilobus, Globigerinoides altiaperturus, Globoquadrina dehiscens) were found determining the lower Miocene age of the respective rocks.
Finally, the pre-existing geological map was changed due to the new findings. Cretaceous deposits were not determined, and thus the late Paleocene was only found as the lowermost part of the exposed outcrops. More details were added on the new map, showing the bedding directions, and the new proposed transfer faults ( Figure 24).
In order to redraw accurately the pre-existing geological map, more samples are required to cover all of the islands in order to add not only the different age deposits but also the faults that influenced their outcropping.

Conclusions
The known Pre-Apulian platform represents the Apulian platform margin (APM) to the Ionian Basin (IB) and was formed because of normal fault activity until the early Miocene (Aquitanian) Epoch. SSD structures in Paxoi and Anti-Paxoi islands document the presence of gravity flow processes. Gravity flows developed due to an inclined basin floor where the instability was responsible for the slumping. SSD structures were cross-cut by normal faults, indicating their development during the rift stage since the early Miocene. Most of the SSD structures progradate either eastwards (especially to Anti-Paxoi Island) or westwards (in the northern part of Paxoi Island), all of them moved towards the subsided fault planes of normal faults.
SSD structures are classified into four (4) different types of deformations: (1) Thick synclines and anticlines, formed due to strong synsedimentary deformation, which were produced mostly from N-S directed normal faults or from the interaction between normal and transfer faults, are situated between undeformed horizons. The movement of the deformation seems to have started from the uplifted footwall of a normal fault. (2) Strong and thick SSD structures, due to their strong power, produced erosional contacts both with the underlying and overlying undeformed horizons. (3) Thin slumps, with sharp contacts with the underlying undeformed horizons and erosional contacts with the overlying undeformed horizons. The upper erosional contact was formed due to the existing relief of the SSD structures with the end of the deformation. (4) Thin slump horizons passing laterally to undeformed deposits in the same horizon, show the short distance of movement. Finally, it seems that the SSD structures are stronger and thicker in the lower Miocene deposits in relation to the SSD structures within the Eocene deposits, indicating more intense tectonic activity during the early Miocene than during the Eocene.

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