GeolCarp_Vol53_No1_37

GEOLOGICA CARPATHICA, 53, 1, BRATISLAVA, FEBRUARY 2002

37 — 44

POSITION OF THE MIDDLE TRIASSIC TYROS BEDS IN THE

GAVROVO-TRIPOLIS UNIT

(RHODES ISLAND, DODECANESE, GREECE)

EUTHIMIOS LEKKAS

, GEORGE DANAMOS

, EMMANOUIL SKOURTSOS

and

DIMITRIOS SAKELLARIOU

University of Athens, Department of Geology, Panepistimioupoli, 15784 Athens, Greece; elekkas@geol.uoa.gr

National Center Marine Research, Fleming 14, Vari, Greece

(Manuscript received January 3, 2001; accepted in revised form December 13, 2001)

Abstract: We describe a Middle Triassic volcano-sedimentary sequence, which outcrops on Rhodes Island at the south-
eastern edge of the Aegean Arc. The sequence is tectonically overlain by the Mesozoic calcareous platform of the local
Archangelos Unit. The latter is regarded as equivalent to the Gavrovo-Tripolis Unit of mainland Greece and Crete. We
propose that the volcano-sedimentary sequence described here is homologue to the Tyros Beds of Peloponnesus or the
Ravdoucha Beds of Crete, which mark the stratigraphic base of the Gavrovo-Tripolis calcareous platform. Consequently
we suggest that Tyros Beds characterize the base of the Gavrovo-Tripolis Unit all along the southern Hellenic Arc, from
Peloponnesus through Kythira and Crete to Rhodes Island.

Key words: Middle Triassic, Hellenides, Gavrovo-Tripolis Unit, Tyros Beds, volcanoclastic sedimentation.

Introduction

The Hellenic Arc is a multi-phase orogenic structure charac-
terized  mainly  by  extended  nappes  and  thrust  sheets.  The
present distribution of the various tectonic units (Hellenides)
is the result of two successive orogenic phases, the Eohellenic
phase  in  the  Late  Jurassic—Early  Cretaceous  and  the  Alpine
phase in Late Eocene—Early Miocene. The imprint of the Eo-
hellenic phase on some of the Hellenides has been used to dis-
tinguish  them  in  Internal,  which  have  been  affected  by  that
phase, and External, which have not been affected.

The paleogeographical distribution of the Hellenides has

been for a long time and still is a matter of controversy among
geologists, while the number of oceanic sutures still remains
obscure (Robertson & Dixon 1984; Dercourt et al. 1986; Pa-
panikolaou 1989). The correlation of the tectonic units, which
outcrop in continental Greece with similar units outcropping
on the Aegean islands, is another weak point in the geological
interpretation of the Alpine structure. Recently new aspects on
the  paleogeographical  organization  of  the  Hellenides  in  the
Late  Paleozoic—Early  Triassic  came  to  light  (Stampfli  et  al.
1998). The main question for that period is whether the vari-
ous  Triassic  volcano-sedimentary  sequences,  which  occur  in
the lower part of the lithostratigraphic columns of several tec-
tonic units, represent passive margin volcanism and are related
to the opening of Tethys or they are related to older consuming
plate margins.

Rhodes Island is located at the southeastern edge of the Hel-

lenic Arc (Fig. 1) and is characterized by a rather complicated
Alpine geotectonic structure. Although numerous geologists
have worked on the island since the beginning of the 20

cen-

tury, fundamental aspects of the Alpine structure of Rhodes
still remain obscure. The number and the origin of the Alpine
units, the time span covered by their litho-stratigraphic col-
umns, the tectonic relation between them as well as their cor-

relation with similar units occurring in continental Greece and
Crete are still a matter of debate. Consequently, the role of the
Alpine units of Rhodes Island in the paleogeographical config-
uration of the Hellenides is not well understood.

In the present paper we describe a volcano-sedimentary se-

quence of Middle to Late Triassic age and we attempt to corre-
late it with known and geodynamically equivalent volcano-
sedimentary sequences of the External Hellenides.

Geotectonic structure of Rhodes Island

Thick Neogene sedimentary sequences have been deposited

in large, fault-controlled basins created during the post-Alpine
period. The Alpine rocks built up mainly the mountainous ar-
eas of the island, which are surrounded by low relief areas
covered by post-Alpine sediments (Fig. 2).

According to most of the researchers, the metamorphic Lin-

dos Unit is the lowermost tectonic unit outcropping on Rhodes
Island (Aubouin & Dercourt 1970) (Fig. 2). It is composed of
dark  bluish  marbles,  which  develop  upwards  to  thin-bedded
marbles and ends with a metaflysch. The transition from cal-
careous  sedimentation  to  flysch  deposition  occurs  in  late
Eocene—Early Oligocene (Leboulenger & Matesco 1975). The
geotectonic position of the Lindos Unit within the Hellenides
is  a  matter  of  controversy  among  the  various  researchers.
Some support its correlation either with the Ionian (or the Plat-
tenkalk)  Unit  (Pozzi  &  Orombelli  1965;  Leboulenger  &
Matesco 1975; Papanikolaou et al. 1995). Others, as Mutti et
al. (1970) and Aubouin & Dercourt (1970) regard it as equiva-
lent of the Preapulian Unit, because of its contents in shallow
water fauna.

Lindos Unit is overlain by a mélange-type formation, which

consists of pelites, clays, sandstones and bioclastic or con-
glomeratic limestone. Exotic blocks of volcanic rocks, pelagic

38 LEKKAS et al.

and brecciated limestones are included within this formation.
The age of the formation, which is known as “Laerma wild
flysch” (Papanikolaou et al. 1995), is Early Oligocene (Mutti
et al. 1970).

Attavyros-Akramites Unit is the lowest among the alloch-

thon units, which overlie the Laerma wild flysch (Fig. 2). The
succession of the litho- and biofacies of this unit is very simi-
lar to those of the Ionian Unit in continental Greece and Crete
Island (Renz 1929; Renz 1955; Orombelli & Pozzi 1967; Mut-
ti et al. 1970; Aubouin & Dercourt 1970; Leboulenger &
Matesco 1975). On the contrary, Harbury & Hall (1988) sup-
port a paleogeographical position of the Attavyros-Akramites
Unit between the Gavrovo-Tripolis platform and the Pindos
Basin.

The Archangelos Unit is constituted of a thick sequence of

massive to thick-bedded limestone and dolomites of Late Tri-
assic—Early Eocene age and Middle—Late Eocene flysch (Mut-
ti et al. 1970; Leboulenger & Matesco 1975). Like the previ-
ous unit, the Archangelos Unit overlies tectonically the
Laerma wild flysch (Papanikolaou et al. 1995) (Fig. 2). Renz
(1929, 1955) considered that it corresponds to the Parnassos-
Giona Unit of continental Greece, though Orombelli & Pozzi
(1967) suggested a paleogeographical position near the Gavro-
vo Zone. On the contrary Aubouin & Dercourt (1970), Lebou-

lenger & Matesco (1975) and Papanikolaou et al. (1995) corre-
spond the Archangelos Unit with Gavrovo-Tripolis Unit, be-
cause of its tectonic position below the Profitis Ilias Unit
(equivalent of the Pindos Unit), and the Eocene age of the up-
permost horizons of its calcareous sequence.

The Profitis Ilias Unit is constituted exclusively of pelagic

sediments, like thin-bedded limestones with silex, red marls and
red radiolarites of Late Triassic—Early Cretaceous age (Mutti et
al. 1970), and corresponds undoubtedly to the Pindos Unit.

The uppermost nappe on the island of Rhodes is constituted

of ophiolite rocks. According to Aubouin & Dercourt (1970),
Leboulenger  &  Matesco  (1975)  and  Papanikolaou  et  al.
(1995), they tectonically overlie the Profitis Ilias Unit. Mutti et
al. (1970) on the contrary believe, that the ophiolites are tec-
tonically  intercalated  between  the  Archangelos  Unit  below
and  the  Profitis  Ilias  Unit  above.  These  ophiolite  outcrops
have been interpreted as remnants either of the Vardar—Axios
oceanic  basin  (Aubouin  &  Dercourt  1970),  or  of  the  Pindos
oceanic basin (Papanikolaou et al. 1995).

As mentioned above, the dominant hypothesis in the exist-

ing literature favours the correlation of the Archangelos Unit
with the Gavrovo-Tripolis Unit of continental Greece. The
correlation of these two stratigraphically and tectonically simi-
lar units is strongly supported by the occurrence of a volcano-

Fig. 1. a – Simplified geotectonic map of the Southern Aegean region (after Jacobshagen 1986) showing the geographical distribution
of the main tectonic units of the External Hellenides. The Preapulian Unit constitutes the foreland of the Hellenides. Tripali and Asterous-
sia Units occur only in western and central Crete respectively. The Phyllite-Quartzite Unit is a Permo-Triassic sequence tectonically em-
placed between the Plattenkalk and Tripolis Units, and is regarded by most authors as the metamorphic equivalent of the Tyros Beds. The
tectonic relationship between the main Units is shown in figure 1b.

GEODYNAMIC SIGNIFICANCE OF THE TYROS-BEDS ON RHODES ISLAND 39

sedimentary sequence at the base of the platform of Archange-
los Unit, which is very similar to the Tyros Beds.

Tectonic position and lithostratigraphy of the

Archangelos volcano-sedimentary sequence

Although the outcrop of the Archangelos volcano-sedimen-

tary sequence, southwest of the village with the same name,
has been very early reported by Migliorini & Venzo (1934) and
Mutti et al. (1970), its paleogeographical position and geody-
namic significance remained obscure.

Mutti et al. (1970) mention the presence of limestone beds

alternating with brown-green pelites on the slopes of the Mt
Karavos near Archangelos village. The thickness of the forma-
tion is barely 20 m. The authors also note that the lower con-
tact of the sequence to the calcareous beds of the Archangelos
Unit is faulted, while the upper one is characterized as normal
stratigraphic contact. Within this formation they determine
Diplopora sp., Balanocidaris scrobiculata (Bronn), Stefaninia
cf. ogilviae (Bittn.) and Mytilus sp. and ascribe it to Carnian.

The stratigraphically lower horizons of the Archangelos

Unit,  which  contain  the  volcano-sedimentary  formation,  out-
crop on the eastern slope of Mt Karavos, 500—600  m south-
west of the Archangelos village, in the central eastern part of
Rhodes Island (Figs. 3, 4a). They are tectonically emplaced in-
between  calcareous  sediments  of  the  Archangelos  carbonate
platform and are partly covered transgressionally by Quaterna-
ry coastal deposits (Fig. 3a,b). The profile presented below has
been described and studied along the road climbing the eastern
slope of Mt Karavos (Fig. 4a).

The strata of the sequence strike NW-SE and dip SW-wards

with 40°—70° (Fig. 4a,b). They lie tectonically on white to
pinkish, thick bedded or massive, micritic to microbreccia and
dolomitic limestones of the Archangelos Unit. The age of the
calcareous sediments remains unknown, since no fossils were
found but on the basis of their sedimentary character we as-
cribe them to the Upper Triassic—Lower Middle Jurassic.

The volcano-sedimentary formation itself is overlain tecton-

ically by white to pinkish, 1—1.5 m thick-bedded, microbrecci-
ated  or  endomicritic  limestones,  which  contain  angular  and
rounded limestone clasts and dip NE-wards (Figs. 3a,b, 4a,c).
Mutti et al. (1970) have found echinoid spines, bivalves, and
Dasycladaceae  within  these  calcareous  sediments.  Corals,
Cladocoropsis  mirabilis  (Felix),  echinoid  spines,  octracods,
Frondicularia sp., Trocholina sp. and many other fossils have
also been reported from younger horizons of the same forma-
tion located at a small distance to the east of the main outcrop.

Description of the profile

The volcano-sedimentary formation near Archangelos vil-

lage has the following litho-stratigraphy from the stratigraphi-
cally lower to the higher levels (Fig. 3c).

a. The stratigraphically lower horizons are composed of al-

ternations of pelites and tuffs with rare intercalations of sand-
stone and limestone horizons. Green and pink layers or round-
ed  bodies  of  igneous  rocks,  as  well  as  foliated  and  strongly
altered  pillow  lavas  are  usually  observed  within  the  clastic
sediments. Quartz, plagioclase, green amphibole, chlorite and
opaque minerals have been observed in thin sections from the
volcanoclastic, tuff layers. Mineralogical analysis of thin sec-
tions from the lava layers and rounded bodies revealed andes-
itic to diabasic composition with diopside phenocrystals flow-
ing  within  microlithic  matrix  composed  of  plagioclase,
chlorite, epidote, calcite and opaque minerals. The sandstone
and  limestone  horizons  become  more  abundant  toward  the
higher  stratigraphic  levels.  The  calcareous  layers  are  endo-
biomicritic to bioclastic limestones and contain fragments of
algae,  echinoderms  and  corals.  Their  thickness  does  not  ex-
ceed 40 cm. The total thickness of this part of the sequence
reaches 250—300 m. This formation overlies tectonically mas-
sive and thick-bedded dolomitic limestones of unknown age.

b. Upwards follows a 4—5 m thick sequence of yellowish

sandstones and pelites within which greenish tuffs and grey,
brecciated limestone beds of 10—12 cm thickness are interca-
lated. The limestone beds become thicker (up to 40—50 cm)
upwards and contain fragments of algae and echinoid spines.
Large calcareous clasts of up to 1.5 m in diameter have been
deposited within the clastic sediments.

c. Alternations of thin green-grey pelites and yellow-grey-

ish limestones of 15 m total thickness follow. The thickness of
the  limestone  horizons  increases  towards  the  top  of  the  se-
quence from 1—15 cm to 10—30 cm. They are microbrecciated
and contain fragments of corals and bryozoa, unilinear fora-
minifers, algae and crinoides (Encrinus liliiformis) of Middle
Triassic age. At the top of the sequence, a 30 cm thick micro-
breccia  to  bioclastic  limestone  horizon  contains  coral  frag-
ments,  bryozoa,  crinoides  (Encrinus  liliiformis),  algae

Fig. 2. Simplified geotectonic map of Rhodes Island according to
Papanikolaou et al. (1995). See text for explanation and their cor-
relation with the units of Fig. 1.

40 LEKKAS et al.

(Diplopora sp.), foraminifers and echinoid spines of the Mid-
dle Triassic (Fig. 4d).

d. Thickness 30—32 m. Limestones and pelites with rare in-

tercalations of 20—40 cm thick green tuffs and 12—15 cm thick
yellow  sandstones.  Two  facies  of  limestone  horizons  have
been observed within this sequence. The first one corresponds
to  grey  micritic  limestones  of  1—6  cm  thickness,  containing
echinoid spines. The second facies corresponds to brecciated
bioclastic  limestone  horizons  of  10—40  cm  thickness  with
some algae fragments and recrystallized coral fragments.

e. Thickness 5 m. Limestones with rare intercalations of

green and yellow pelites. The thickness of the individual cal-
careous beds reaches 60 cm.

f. 1 m thick green pelites and tuffs.
g. Thickness 45 m. Alternations of up to 1 m thick limestone

beds  with  up  to  30—35  cm  thick  pelites  and  yellow  to  green
tuffitic  horizons  with  rare  intercalations  of  sandstones.  The
brecciated limestone layers contain big fragments of crinoides
(Encrinus  liliiformis),  recrystallized  algae  fragments,
(Diplopora sp.), rounded and angular micritic pebbles and bry-
ozoa. Their age is Middle Triassic.

h. Thickness 10 m. Alternations of 5—25 cm thick limestone

beds and 5—10 cm thick pelitic horizons. The micritic facies
become more rare.

The upper contact of that series to the overlying limestones

of the Archangelos platform is of tectonic origin. The contact

Fig. 3. a – Geological map of the area southwest of Archangelos village. See Fig. 2 for location. b – Geological cross-section A—A´. c –
Stratigraphic column of the Archangelos volcano-sedimentary sequence. See “Description of the profile” for explanations on a—h.

GEODYNAMIC SIGNIFICANCE OF THE TYROS-BEDS ON RHODES ISLAND 41

at the southern part of the outcrop dips relatively steeply while
at the eastern and western part it becomes subhorizontal and
crosscuts the stratigraphic horizons of the underlying volcano-
sedimentary sequence (Figs. 3a,b, 4a).

Discussion

Up to now the Archangelos Unit was regarded by most re-

searchers  as  equivalent  to  the  Gavrovo-Tripolis  Unit  mainly
because of the following two aspects: (a) the age of the Arch-
angelos Unit calcareous sequence, which is compatible to the
continuous Late Triassic—Upper Eocene calcareous sedimenta-
tion  of  the  Gavrovo-Tripolis  shallow  water  platform  and  (b)
the tectonic position of the Archangelos Unit below the pelag-
ic  unit  of  Profitis  Ilias,  which  is  attributed  by  almost  all  re-
searchers to the Pindos Unit.

The new data presented in this work support that hypothesis.

We suggest, that the above-described volcano-sedimentary se-
quence of the Archangelos Unit is equivalent to the lower part
of the litho-stratigraphic column of the Gavrovo-Tripolis Unit,
meaning the Tyros Beds in the Peloponnesus or their equiva-
lent Ravdoucha Beds in Crete Island.

Our hypothesis is supported by a) the lithological similarity

between the Archangelos volcano-sedimentary sequence and
the Tyros Beds; b) the age of the sequence, which has been

also reported from several places in Peloponnesus and Crete
for the upper part of the Tyros Beds and c) the tectonic posi-
tion of the sequence below the Archangelos Unit carbonate
platform, similar to the position of Tyros Beds below the
Gavrovo-Tripolis platform.

The Upper Paleozoic—Lower Triassic volcano-sedimentary

formation  at  the  base  of  the  Gavrovo-Tripolis  shallow  plat-
form was recognized very early (Ktenas 1926) and repeatedly
described since then. The Tyros Beds are characterized by a
lower clastic formation and an upper volcano-sedimentary se-
quence (Fig. 5) (Skarpelis 1982). The lower part is constituted
of  pelites  and  sandstones,  that  often  form  turbite  sequences
within  which  calcareous  lenses  intercalate.  Carboniferous,
Permian  and  Early  Triassic  ages  have  been  reported  for  the
lower part of the Tyros Beds (Ktenas 1926; Lys & Thiebault
1971; Panagos et al. 1979; Thiebault 1982).

The majority of the Tyros Beds outcrops in the Peloponne-

sus and Crete are dominated by the upper volcano-sedimentary
part. It is composed of lava horizons, pyroclastics, tuffs and
clastic and calcareous sediments that intercalate within volca-
no-sedimentary deposits (Skarpelis 1982). Numerous fossils
such as ostracods, echinoids, ammonites and conodonts, found
within the calcareous beds, are evidence of a Carnian—Norian
and in some places also Rhaetian age for the upper part of Ty-
ros Beds (Sannemann & Siedel 1976; Kopp & Ott 1977; Thie-
bault 1982; Brauer et al. 1980; Thorbecke 1987; Gerolymatos

Fig. 4. a – View of the Archangelos volcano-sedimentary sequence outcrop from the east. b – Alternation of brecciated limestones,
pelites, sandstones and tuff horizons. c – The tectonic contact between the Archangelos carbonate platform and the volcano-sedimentary
sequence. d – Encrinus lilliformis within brecciated limestone. The location of the pictures of Fig. 4b,c and d are shown in Fig. 4a.

42 LEKKAS et al.

Fig. 5. Schematic presentation of the geological evolution of the Tripolis Unit in the Late Carboniferous—Early Jurassic.

1994). According to the synthetic litho-stratigraphic columns
proposed by Gerolymatos (1994) and Dornsiepen & Manutso-
glu (1994) for the Tyros Beds, a stratigraphic hiatus occurs in
the Middle Triassic (Ladinian) (Fig. 5). It is possible that this
hiatus represents the limit between the lower, clastic formation
and the upper, volcano-sedimentary sequence of the Tyros
Beds (Fig. 5).

The continuous transition from the volcano-clastic sedi-

ments of the “Tyros Beds” to the Gavrovo-Tripolis platform
sedimentation has already been described from various places
in the Peloponnesus (Tataris & Maragoudakis 1967; Fytrolakis
1971;  Lekkas  &  Papanikolaou  1978;  Thiebault  1982)  and
Crete (Kopp & Ott 1977; Bonneau & Karakitsios 1979; Fytro-
lakis  1980).  This  transition  has  usually  been  found  to  take
place in the Late Carnian—Rhaetian, while Lias age is also re-
ported  by  Alexopoulos  (1990)  in  central  Crete.  Danamos
(1991,  1992)  and  Gerolymatos  (1994)  report  a  tectonic  rela-
tionship between the underlying Tyros Beds and the overlying
shallow water carbonates. Consequently, we suggest that the
volcano-sedimentary  Archangelos  sequence  may  easily  be
correlated with the upper part of the Tyros Beds.

There is a lot of incertitude regarding the origin of the Tyros

Beds  and  the  geotectonic  setting  of  the  Triassic  volcanism.
Thiebault  (1982)  &  Thiebault  et  al.  (1985)  suggest  that  the
shoshonitic composition of the Tyros volcanites is related to a
rifting  phase  though  Skarpelis  (1982)  and  Pe-Piper  (1982)
favour an above subduction zone character for the Tyros vol-
canism. Pe-Piper (1983a,b) notes the presence of tholeiites and
calcalkaline  basalts,  which   may  refer  to  an  old  subduction

zone, but describes also more alkaline types, which display
within-plate character. Therefore she suggested that the Trias-
sic volcanism occurred close to an old consuming plate bound-
ary and is also related to the initial stage of a back-arc rifting
process. Later the same author (Pe-Piper 1998) suggested, on
the basis of the geochemistry of Nd and Pb isotopes, that the
Triassic volcanisms are related to a general extension, which
affected the paleogeographical area of the Hellenides during
that period. Recently Stampfli et al. (1998) proposed that Ty-
ros Beds represent an accretionary prism created in front of the
subduction zone of the Paleotethys oceanic lithosphere below
the southern Eurasian margin.

Up to now there are no data from the volcanic rocks of the

Archangelos volcano-sedimentary sequence, which would al-
low  us  to  support  any  of  the  proposed  hypotheses  regarding
the geotectonic setting of the Triassic volcanism. The presence
of  pillow-lavas  and  the  alternations  described  suggest  a  se-
quence  rich  in  calcareous  redeposits  possibly  deposited  in
deep water conditions.

It is obvious, that a widespread volcanic activity occurred in

the Middle—Late Triassic within the paleogeographical area of
the  Gavrovo-Tripolis  Zone,  before  the  onset  of  the  shallow
platform calcareous sedimentation. The deposition of the vol-
canic  material  was  interfering  with  clastic  and  biochemical?
sedimentation  possibly  in  a  shallow  water  environment.  The
end of that volcanic phase marks the onset of the calcareous
sedimentation either in the Carnian—Norian or Rhaetian, or even
in the Lias in central Crete. The shallow water platform sedi-
mentation continued without any break until the Early Tertiary.

GEODYNAMIC SIGNIFICANCE OF THE TYROS-BEDS ON RHODES ISLAND 43

Conclusion

We propose that the Middle Triassic volcano-sedimentary

sequence, which outcrops near Archangelos village in eastern
Rhodes Island, is a homologue to the Tyros and Ravdoucha
Beds, which represent the stratigraphic base of the Gavrovo-
Tripolis carbonate platform in the Peloponnesus and Crete re-
spectively.

The correlation of the Archangelos volcano-sedimentary

formation with Tyros Beds indicates that the latter constitutes
a significant characteristic of the entire paleogeographical area
of the External Hellenides carbonate platform, from the
Peloponnesus through Kythira and Crete to Rhodes, before the
onset of the shallow water sedimentation in the Middle—Upper
Triassic.

The deposition of clastic sediments, accompanied by andes-

itic volcanism with lava flows and tuff layers, predates the on-
set of the shallow marine calcareous sedimentation of the
Gavrovo-Tripolis Unit and is present throughout the entire pa-
leogeographical area of the unit. It is noteworthy that the sedi-
mentary facies and the lithological characteristics of the Upper
Paleozoic—Upper Triassic volcano-sedimentary Tyros Beds
formation remain more or less constant all along the southern
Hellenic Arc.

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