GeolCarp_Vol66_No4_269

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Introduction

The Late Carnian levelling of the topography (Bosellini et al.
2003;  Breda  et  al.  2009;  Roghi  et  al.  2010;  Breda  &  Preto
2011) and the following relative sea level rise (Haas & Budai
1999; Gawlick & Böhm 2000; Gianolla et al. 2003; Berra et
al. 2010) created suitable conditions for the growth of one of
the  most  extensive  Mesozoic  carbonate  platforms  lining  the
western embayment of the Neotethys Ocean (Fig. 1,  Bosellini
1967; Gawlick 2000; Mandl 2000; Golonka 2002; Bosellini
2004; Haas 2004; Vlahović et al. 2005; Krystyn et al. 2009;

Paleogeographic significance of Upper Triassic basinal

succession of the Tamar Valley, northern Julian Alps

(Slovenia)

LUKA GALE

, BOGOMIR CELARC

, MARCELLO CAGGIATI

, TEA KOLAR-JURKOVŠEK

BOGDAN JURKOVŠEK

and PIERO GIANOLLA

University of Ljubljana, Faculty of Natural Sciences and Engineering, Department of Geology, Privoz 11, SI-1000 Ljubljana, Slovenia;

luka.gale@ntf.uni-lj.si

Geological Survey of Slovenia, Dimičeva ul. 14, SI-1000 Ljubljana, Slovenia;

tea.kolar@geo-zs.si; bogdan.jurkovsek@geo-zs.si; bogomir.celarc@geo-zs.si

University of Ferrara, Physics and Earth Sciences Department, Via Saragat 1, 44122 Ferrara, Italy;

piero.gianolla@unife.it; marcello.caggiati@unife.it

(Manuscript received November 7, 2014; accepted in revised form June 23, 2015)

Abstract: The Julian Alps (western Slovenia) structurally belong to the eastern Southern Alps. The Upper Triassic
succession mostly consists of shallow water platform carbonates of the Dolomia Principale-Dachstein Limestone sys-
tem and a deep water succession of the Slovenian Basin outcropping in the southern foothills of the Julian Alps. In
addition to the Slovenian Basin, a few other intraplatform basins were present, but they remain poorly researched and
virtually ignored in the existing paleogeographic reconstructions of the eastern Southern Alps. Herein, we describe a
deepening-upward succession from the Tamar Valley (north-western Slovenia), belonging to the Upper Triassic Tarvisio
Basin. The lower, Julian-Tuvalian part of the section comprises peritidal to shallow subtidal carbonates (Conzen Dolo-
mite and Portella Dolomite), and an intermediate carbonate-siliciclastic unit, reflecting increased terrigenous input and
storm-influenced deposition (Julian-lowermost Tuvalian shallow-water marlstone and marly limestone of the Tor For-
mation). Above the drowning unconformity at the top of the Portella Dolomite, Tuvalian well-bedded dolomite with
claystone intercalations follows (Carnitza Formation). The latter gradually passes into the uppermost Tuvalian—lower-
most Rhaetian bedded dolomite with chert and slump breccias, deposited on a slope and/or at the toe-of-slope (Bača
Dolomite). Finally, basinal thin-bedded bituminous limestone and marlstone of Rhaetian age follow (Frauenkogel For-
mation). The upper part of the Frauenkogel Formation contains meter-scale platform-derived limestone blocks, which
are signs of platform progradation. The Tarvisio Basin may have extended as far as the present Santo Stefano di Cadore
area, representing a notable paleogeographic unit at the western Neotethys margin.

Key words: Southern Alps, Late Triassic, paleogeography, Tarvisio Basin, carbonate platform.

Fig. 1. Paleogeographic position of the Southern Alps during Late
Triassic. A suggested position of the Tamar tectonic unit (as a sub-
unit of the Southern Alps) is marked by a black star. Modified after
Haas et al. (1995, 2010). TR – Transdanubian Range, SA – Sava
Unit,  BU  –  Bükk  Unit,  JA  –  Jadar  block,  DR  –  Drauzug,
BR  – Briançonnais Unit, HE – Helvetic Unit,  AA  –  Austroal-
pine units, BA – Bajuvaricum, TI – Tirolicum, HA – Hallstatt
Unit, TA – Tatricum,  HR – Hronicum.

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Haas et al. 2010). The peritidal Dolomia Principale/Hauptdo-
lomit/Main Dolomite deposited in its proximal part, towards
the present east passing into the peritidal to shallow subtidal
Dachstein Limestone (Kuerschner et al. 2007). Basins of dif-
ferent depths formed inside the platform area and along its
edge (Kuss 1983; Jadoul et al. 1992; Carulli et al. 1998; Haas
2002; Haas & Tardy-Filácz 2004; Hornung 2005; Ciarapica
2007; Pálfy et al. 2007; Jadoul et al. 2012). At least two such
basins are known from the eastern Southern Alps. The expo-
sures of the better known Ladinian to Upper Cretaceous Slo-
venian Basin form the southern foothills of the eastern Julian
Alps (Winkler 1923; Cousin 1981; Buser 1986, 1989, 1996;
Rožič et al. 2013). A Carnian—Lower Jurassic(?) deepening-
upward succession was described from the Hahnkogel (in

Slovenian  termed  Klek)  tectonic  block  of  the  Karavanke
Mountains  (Krystyn  et  al.  1994;  Lein  et  al.  1995;  Schlaf
1996), and Tuvalian deeper water carbonates were described
from the Cave del Predil (Lieberman 1978; De Zanche et al.
2000;  Gianolla  et  al.  2003),  Vrata  Valley  and  Martuljek
Mountain Group (Ramovš 1986; Schlaf et al. 1997; Ramovš
1998;  Sattler  1998;  Celarc  &  Kolar-Jurkovšek  2008)  in  the
northern  Julian  Alps  (Fig. 2).  These  basinal  facies  were  in-
cluded by Gianolla et al. (2010) among the remnants of the
much less known Tarvisio Basin, which has been considered
a distinct branch of the Slovenian Basin.

In this paper, a Carnian to Rhaetian deepening-upward suc-

cession from the Tamar Valley in the northern Julian Alps,
NW Slovenia (Fig. 2), is described for the first time. This sec-

Fig. 2. Position and geological setting of the studied area. a – Position of the area depicted in Fig. 2b (shaded), b – Detailed map with po-
sitions of the sections mentioned in the text, c – Structural subdivision of north-western Slovenia. Modified after Buser & Draksler
(1993), Placer (1999), and Goričan et al. (2013). HTB – Hahnkogel/Klek thrust block, kk – Krn-Kobla thrust, KTB – Krn thrust block,
PTB – Pokljuka thrust block, rvc – Resia-Val Coritenza backthrust, TTB – Tamar thrust block, ZK – Zlatna klippe.

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tion provides a clear link between the Cave del Predil and the
Mt Hahnkogel/Klek area. The  Tarvisio  Basin  is  now  recog-
nized as an important element of the eastern Southern Alps’
paleogeography.  Furthermore,  the  emerging  correlation  be-
tween  seemingly  disjunct  sections  is  a  further  step  towards
Late Triassic carbonate platform-margin reconstruction, sim-
ilar  to  those  described  from  the  Northern  Calcareous  Alps
(e.g. Mandl 1999; Krystyn et al. 2009) and the Oman Moun-
tains (Bernecker et al. 2005).

Geological setting

The eastern part of the Southern Alps geographically in-

cludes the Julian Alps, the southern Karavanke Mts and the
Kamnik-Savinja Alps (Placer 1999, 2008). The studied sec-
tion of the Tamar Valley is located in the northern part of the
eastern  Julian  Alps  (Fig. 2),  structurally  and  geographically
separated from the Karavanke Mountains to the north by the
Fella-Sava  line,  a  dextral  WNW-ESE  oriented  strike-slip
fault  (Venturini  1990;  Placer  1999,  2008;  Vrabec  &  Fodor
2006; Jamšek Rupnik et al. 2012).

Geological research on the valley and its closer surround-

ings  includes  work  by  Peters  (1856),  Diener  (1884),  Selli
(1963), Ramovš (1981), Ogorelec et al. (1984), and Jurkovšek
(1986,  1987).  The  geological  map  of  Jurkovšek  (1986)  was
later updated by Buser & Draksler (1993) and Buser (2009).
The  structure  of  this  region  is  rather  complex  due  to  the  Al-

pine tectonics (Doglioni & Bosellini 1987; Poli & Zanferarri
1995; Placer 1999; Castellarin & Cantelli 2000): the Late Cre-
taceous  to  Paleogene  NE-vergent  Dinaric  thrusts  partially
overlap  with  Neogene  N-verging  Alpine  thrusts  (Doglioni  &
Bosellini 1987; Placer 1999, 2008; Kastelic et al. 2008), both
being further cut and displaced by dextral strike-slip faults ac-
tive  since  the  Pliocene  (Castellarin  et  al.  2006;  Vrabec  &
Fodor 2006; Kastelic et al. 2008; Caputo et al. 2010; Bavec et
al.  2012;  Kastelic  &  Carafa  2012).  In  this  complex  array  of
structural features, the Tamar Valley area belongs to the infor-
mal  “Tamar”  tectonic  block  of  the  Southern  Alps,  which  is
separated  from  the  Krn  tectonic  block  by  the  Resia-Val
Coritenza backthrust (Cousin 1981; Venturini & Carulli 2002;
Figs. 2—3).

The herein described succession of the Tamar Valley pa-

leogeographically belongs to the Tarvisio Basin in Gianolla
et al. (2010).

Methods

The Upper Triassic lithological units of the Tamar Valley

were  investigated  in  two  successive  sections  (Fig. 3):  the
Črna  voda  section  (46°26’14.19” N,  13°42’48.82” E),
which  consists  of  the  lower  part  of  the  succession,  and  the
Travnik section (46°25’53.35” N, 13°42’36.24” E), which
spans the upper part. A portion of the succession is missing
due to faulting.

Fig. 3. Geological map of the Tamar Valley with the positions of the Črna voda (A) and Travnik (B) sections.

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Eleven conodont samples of 2.5—3 kg were taken to estab-

lish the basic biostratigraphy. Five of the samples were posi-
tive.  The  samples  were  crushed  and  treated  with  diluted
acetic  acid  following  standard  procedures.  The  conodont
supra-species  taxonomy  follows  Orchard  (1991a,b),  Kozur
(1989,  2003)  and  Orchard  (2007).  For  the  study  of  benthic
foraminifera, 26 thin sections 47

×28 and 75×49 mm in size

were prepared from 24 stratigraphic levels. The positions of
the collected samples are indicated in Fig. 4. Some foramin-
iferal species are shown in Fig. 5 according to their position
in  the  different  lithological  units,  whereas  conodonts  are
illustrated  in  Fig. 6.  Samples  are  stored  at  the  Geological
Survey of Slovenia, Department for Stratigraphy and Paleon-
tology.  In  addition  to  the  present  sampling,  Ogorelec  et  al.
(1984)  listed  several  species  of  dasycladacean  algae,  mol-
luscs and benthic foraminifera from the Črna voda section.

Description of the Tamar Valley succession

Lithological units of the Črna voda section

Conzen Dolomite

Description: Bedding is often poorly pronounced, re-

sulting in massive facies (Fig. 7.1). Light brown dolomitized
lime mudstone alternates with fenestral dolomite, laminated
stromatolitic and oncoid-bearing dolomite (Fig. 7.2) in deci-
meter to meter scale thick beds.

The foraminifera Aulotortus friedli (Kristan-Tollmann)

sensu Piller (1978), Turrispirillina minima Pantić and small
planispiral Involutinaceae were identified.

Discussion: This unit probably represents a time equiva-

lent of the Conzen Limestone described from the Cave del
Predil area (cf. De Zanche et al. 2000). The latter becomes
more dolomitized and increasingly more shallow-water east-
wards (Assereto et al. 1968; De Zanche et al. 2000). Aulotor-
tus friedli suggests a Ladinian to Rhaetian age (Piller 1978;
Senowbari-Daryan et al. 2010; Gale 2012).

Depositional setting: The presence of stromatolites and

oncoids points to peritidal sedimentation, and the dolo-
mitized mudstone suggests deposition in a shallow subtidal
zone (e.g. Ogorelec & Rothe 1993; Satterley 1996; Sattler &
Schlaf 1999; Haas 2004; Haas et al. 2007).

Tor Formation

Description: The Tor Formation lies on the Conzen Do-

lomite.  A  gradual  increase  in  siliciclastic  input  coincides
with the thinning of the dolomite beds (Fig. 7.3). The lower
part consists of siltstone, marly limestone with crinoid ossi-
cles, small gastropod shells and undetermined mollusc frag-
ments,  and  nodular  limestone.  Coalified  plant  debris  is
present. Brownish dolomite and bioclastic dolomite, bivalve
lumachelle,  and  micritic  limestone  with  crinoids  are  fol-
lowed by alternating micritic limestone and marlstone. Small
megalodontids  and  bivalve  lumachella  beds  and  lenses  are
present  (Fig. 7.5),  and  there  is  occasional  packstone  above
erosional  surfaces  (Fig. 7.6).  Bioturbation  is  common.  The

uppermost part, consisting of marly dolomite and claystone,
is in sharp contact with the overlying Portella Dolomite
(Fig. 7.4).

The foraminifera “Trochammina” almtalensis Koehn-Za-

ninetti,  Aulotortus  friedli,  small  planispiral  Involutinaceae
(?Triadodiscus  eomesozoicus  (Oberhauser)),  Angulodiscus
impressus  Kristan-Tollmann,  ?Glomospirella  vulgaris  Ho,
?Hoyenella  sinensis  Ho  and  “Frondicularia  woodwardii
Howchin” auct. were identified (Fig. 5.2—5). Ogorelec et al.
(1984)  identified,  among  other  fossils,  the  bivalve  Lopha
montiscaprilis  (Klipstein)  [Umbrostrea?  montiscaprilis  in
Szente  et  al.,  2010],  foraminifera  Pilamminella  kuthani
(Salaj),  and  dasyclads  Clypeina  besici  Pantić  and  Poiki-
loporella duplicata (Pia).

Discussion: Umbrostrea? montiscaprilis indicates the

topmost part of the Julian (Ruvinetti, 2004). The Carnian age
is  further  supported  by  Clypeina  besici  and  Poikiloporella
duplicata (see Senowbari-Daryan, 2003). The lower Tor For-
mation  in  Log  pod  Mangartom  (see  Fig. 2)  belongs  to  the
Patinasporites  densus  (Leschik)—Partitisporites  maljawkinae
(Klaus)  palinomorph  zone  (Ogorelec  et  al.,  1984).  The  ele-
ments of this zone can be found in the Lagenella martini as-
semblage in Roghi et al. (2010), suggesting a correlation with
the  Dibona  Member  of  the  Heiligkreuz  Formation  in  the
Dolomites (Roghi 2004; Preto et al. 2005).

Depositional setting: A shift to a more clastic sedimen-

tation in the uppermost Early Carnian is attributed to climate
change  towards  more  humid  conditions  (“Carnian  Pluvial
Event”;  Simms  &  Ruffell  1989).  Bivalve  coquinas  with  in-
ternal  erosional  surfaces  are  interpreted  as  tempestites
(Schlaf  1996;  Pérez-López  &  Pérez-Valera  2012),  and  they
support the idea of an episodically high-energy environment
above  the  storm  wave  base,  whereas  the  fossil  assemblage
suggests  normal  marine  conditions.  A  nearshore,  shallow
water depositional setting was suggested by De Zanche et al.
(2000) for the Tor Formation at Cave del Predil.

Portella Dolomite

Description: Crystalline dolomite over 4 m thick (Fig. 7.4)

is followed by thick to very thick bedded dolomite.

Discussion: A Early Tuvalian age is assumed on the ba-

sis of superposition.

Depositional setting: Loss of primary sedimentary

structures by dolomitization prevents interpretation of the
depositional environment. In the Cave del Predil area, stro-
matolites are visible in some parts (De Zanche et al. 2000),
and the Portella Dolomite has been interpreted as a carbonate
bank deposited in a shallow water environment (De Zanche
et al. 2000; Gianolla et al. 2003; Preto et al. 2005).

Carnitza Formation

Description: This formation is lithologically uniform,

consisting  of  slightly  marly  thin  to  medium  bedded  dolo-
mite. Bedding is planar or nodular, dolomite beds are often
separated  by  claystone  interbeds  a  few  centimeters  thick
(Fig. 7.7). In the dolomite, parallel lamination is sometimes
visible,  as  well  as  rare  micritic(?)  intraclasts  and  bioturba-

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tion. More coarsely crystalline dolomite horizons with sharp
lower boundaries were found in a few places above more
fine-grained dolomite.

The upper boundary of the Carnitza Formation is placed at

the last claystone intercalations, closely coinciding with an
increase in abundance of chert nodules.

The conodonts Paragondolella polygnathiformis (Bu-

durov  &  Stefanov),  Paragondolella  carpathica  (Mock)  and
Carnepigondolella aff. C. tuvalica were recovered from the
lowermost  10 m  of  the  Carnitza  Formation.  The  composite
sample from the uppermost 10 m of the Carnitza Formation
yielded  P.  polygnathiformis  and  Metapolygnathus  primitius
(Hayashi).

Discussion: In contrast to its type locality in the Cave del

Predil area (Lieberman 1978), the Carnitza Formation in the
Tamar Valley consists entirely of dolomite. This feature is
common in other outcrops of the Italian Julian Alps (De
Zanche et al. 2000; Caggiati 2014), and complete dolomitiza-
tion is also reported in the Southern Karavanke Mts (Krystyn
et al. 1994).

Paragondolella carpathica suggests a Tuvalian age for the

lower part of the Carnitza Formation (Kolar-Jurkovšek 1991;
Muttoni et al. 2001; Krystyn et al. 2002; Buser et al. 2008;
Mazza & Krystyn 2013). Metapolygnathus primitius in com-
bination with P. polygnathiformis from the uppermost part
indicates a Late Tuvalian age (Muttoni et al. 2001; Buser et
al. 2008; Mazza et al. 2012).

Depositional setting: As for the Portella Dolomite, do-

lomitization largely obscures the primary sedimentological
features and prevents undisputed interpretation of the depo-
sitional environment. Parallel lamination may suggest depo-
sition from distal turbidite currents, and the coarser horizons
are likely related to the coarse-grained sediment occasionally

deposited as distal turbidites or as grain flows (Gale 2010).
Its  position  between  the  peritidal/shallow  water  (?)Portella
Dolomite and the slope to base-of-slope Bača Dolomite (see
below),  is  in  agreement  with  a  progressive  deepening,  as  is
the  upward-increase  in  chert  nodules  observed  in  the  Črna
voda  section.  In  the  Cave  del  Predil  area  De  Zanche  et  al.
(2000) and Gianolla et al. (2003) interpreted the lower bound-
ary of the Carnitza Formation as a drowning unconformity.

Bača Dolomite

Description: The Bača Dolomite consists of thin to me-

dium-thick beds of dolomite with common chert nodules and
lenses.  The  sequence  continues  with  massive  dolomitized
mud-supported breccia with chert clasts and dolomite intrac-
lasts  (Fig. 8.1),  but  this  part  was  not  measured  due  to  inac-
cessibility  and  disruption  by  faults.  The  uppermost  part  of
the Bača Dolomite is accessible in the Travnik section, and
the  thickness  of  the  entire  formation  is  estimated  to  be  ap-
proximately 200 m.

The conodonts Paragondolella polygnathiformis and M.

primitius  were  recovered  from  the  basal  10 m  of  the  unit.
Epigondolella  abneptis  (Huckriede),  Epigondolella  aff.  E.
orchard  Kozur  and  Epigondolella  quadrata  Orchard  were
found  somewhat  higher  up  in  the  section.  The  uppermost
part of the Bača Dolomite, accessible in the Travnik section
(see  description  there),  yielded  Misikella  posthernsteini
Kozur & Mock.

Discussion: Paragondolella polygnathiformis and M.

primitius suggest a Late Tuvalian age for the lowermost part
of the Bača Dolomite. Epigondolella quadrata from a sam-
ple taken higher up indicates an Early Norian age (Muttoni
et al. 2001; Krystyn et al. 2002, 2009; Mazza et al. 2012).

Fig. 6. Conodonts from the Tamar Valley section. 1—2 – Paragondolella
polygnathiformis (Budurov & Stefanov), Carnitza Formation (Tuvalian),
sample GeoZS 4812; 3 – Carnepigondolella aff. C. tuvalica Mazza &
Rigo,  Carnitza  Formation  (Tuvalian),  sample  GeoZS  4812;  4  –  Epi-
gondolella  cf.  E.  quadrata  (Orchard),  Bača  Dolomite  (lowermost  La-
cian), sample GeoZS 4809; 5—6 – Epigondolella cf. E. orchardi Kozur,
Bača Dolomite (lowermost Lacian), sample GeoZS 4809; 7 – Misikella
posthernsteini  (Kozur  &  Mock),  uppermost  Bača  Dolomite  (Rhaetian),
sample GeoZS 4892.

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Misikella posthernsteini was recovered from the uppermost
Bača Dolomite, indicating proximity to the Norian-Rhaetian
boundary (e.g. Krystyn et al. 2008, 2009; Giordano et al.
2010; Hüsing et al. 2011).

Depositional setting: Mud-supported breccia with chert

clasts and dolomite intraclasts are interpreted as debris flow

Fig. 8. Field photographs and thin section photomicrographs of lithostratigraphic units of the Travnik section. 1 – Breccia with dolomitic
and chert intraclasts of the middle part of the Bača Dolomite (ex situ). Note brittle deformation of chert clasts (arrowhead), suggesting early
chertification of the sediment (D. Skaberne, pers. com.); 2 – Grainstone with abundant benthic foraminifera, mostly Triasina hantkeni
Majzon and Duostominidae (arrowheads); 3—4 – Thin-bedded to laminated bituminous limestone and claystone/marlstone of the Frauen-
kogel Formation; 5 – A large olistolith of Dachstein Limestone (C) embedded in the Frauenkogel Formation.

deposition on an inclined slope. The Bača Dolomite is better
characterized  in  the  Tolmin  Nappe  of  the  Southern  Alps
from the succession of the Slovenian Basin (Kossmat 1914;
Buse,  1986;  Gale  2010).  Sedimentological  analysis  of  the
non-dolomitized  horizons  within  the  Bača  Dolomite  from
the  proximal-most  preserved  part  of  the  Slovenian  Basin

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points to deposition on the slope and at the foot of the slope
(Gale 2010).

Lithological units of the Travnik section

Frauenkogel Formation

Description: The Frauenkogel Formation overlies the

Bača Dolomite with a sharp boundary. The Frauenkogel For-
mation  in  its  lowermost  part  contains  marlstone  and  a  few
graded and laminated fine- to medium- coarse rudstone and
grainstone beds (Fig. 8.2). A uniform sequence of dark bitu-
minous  and  laminated  platy  limestone  follows,  alternating
with marlstone (Fig. 8.3—4). Small nodules and thin lenses of
chert  are  rare.  Bedding  is  often  disrupted  by  slumps.  In  the
upper part of the sequence, boulders measuring up to 3 m of
beige wacke- to packstone and dark grey packstone lie among
platy limestones (Fig. 8.5). They contain peloids, ooids, a few
lumped clasts, and subordinate bioclasts (foraminifera, echi-
noderms,  brachiopods,  bivalves).  The  Travnik  section  is
truncated at the top by the Resia-Val Coritenza thrust, bring-
ing it in tectonic contact with subtidal to peritidal Dachstein
Limestone.

Rudstone from the basal part of the Frauenkogel Forma-

tion  yielded  a  rich  assemblage  of  benthic  foraminifera
(Fig. 5.6—15): Gandinella falsofriedli (Salaj et al.), “Trocham-
mina”  almtalensis,  Alpinophragmium  perforatum  Flügel,
“Tetrataxis”  inflata,  Triasina  hantkeni  Majzon,  Aulotortus
friedli,  Aulotortus  sinuosus,  Aulotortus  tumidus,  Aulotortus
tenuis  Kristan,  Trocholina  umbo  Frentzen,  Auloconus  per-
modiscoides  (Oberhauser),  Hoyenella  inconstans  (Michalik
et al.) or Hoyenella sinensis, “Orthotrinacria expansa” auct.,
Galeanella  tollmanni  (Kristan),  Decapoalina  schaeferae
(Zaninetti  et  al.),  Variostoma  cochlea  Kristan-Tollmann,
Variostoma  helicta  (Tappan),  Duostomina  biconvexa
Kristan-Tollmann  and  Lenticulina  sp.  From  the  olistoliths
we identified the following species: Aulotortus friedli, Aulo-
tortus  sinuosus,  Triasina  hantkeni  and  Hoyenella  sinensis.
Trocholina crassa Kristan, Involutinidae and Lenticulina sp.
were identified in the packstone bed 38 m above the base of
the section.

Discussion: Biostratigraphic data suggest a correlation

with  the  Frauenkogel  Formation  described  from  the  Hahn-
kogel/Klek  tectonic  block  of  the  Southern  Karavanke  Mts,
although  at  the  type  locality,  the  Frauenkogel  Formation
lacks marlstone and the limestone is often bioturbated and in
part contains chert nodules (Krystyn et al. 1994; Lein et al.
1995;  Schlaf  1996).  Foraminifera  from  the  Travnik  section
were  derived  in  majority  from  shallow  water  reef-rimmed
carbonate  platform  environments  (see  Gale  2012  and  refer-
ences  therein).  Triasina  hantkeni  from  the  basal  part  of  the
unit is an indicator for a Rhaetian age of this unit (see Gale et
al. 2012).

Depositional setting: Common slumping indicates dep-

osition  on  a  slope.  Coarse-grained,  graded  and  laminated
rudstone  and  grainstone  are  interpreted  as  turbidity  current
deposits  (Tucker  2001;  Flügel  2004).  Blocks  of  Dachstein
Limestone found in the upper part of the unit are interpreted
as  cipit  boulders  derived  from  the  adjacent  shallow  water

platform (Russo et al. 1997; Trombetta 2011), as suggested
by a foraminiferal assemblage typical of shallow water car-
bonate  platforms  (Triasina  hantkeni,  Aulotortidae).  Beds  in
which only horizontal lamination is observed could be related
to a low-energy setting, poorly ventilated water and suboxic
or  even  anoxic  conditions,  as  suggested  by  the  absence  of
bioturbation  and  the  smell  of  bitumen  (Carulli  et  al.  1997;
Brenchley  &  Harper  1998).  Such  conditions  can  occur  in  a
variety of depositional environments; however, deposition in
deeper water is suggested due to the presence of cipit boul-
ders and turbidite deposits.

Discussion

Although numerous occurrences of Upper Triassic deep wa-

ter successions are known from the eastern Southern Alps
(e.g. Ramovš 1989), only a handful of them have been studied
in detail, and their relationships are not completely under-
stood. The lateral extent of the Tarvisio Basin can be followed
to the western Julian Alps and the Southern Carnic Alps.

In the Cave del Predil massive and thick-bedded shallow

water  limestone  and  dolomite  of  the  Schlern  Formation  is
overlain  by  thin-bedded  dolomite,  doubtfully  attributed  to
the  Lower  Carnian  (Assereto  et  al.  1968;  Lieberman  1978;
De Zanche et al. 2000; Roghi 2004).

Massive clinobeds of the Schlern Dolomite are interfin-

gered  with  and  then  onlapped  by  the  thick  carbonate-silici-
clastic Julian sequence of the Predil Limestone and the Rio
del Lago Formation (Assereto et al. 1968). The latter passes
upward  to  the  Conzen  Formation,  followed  by  the  Upper
Julian  to  Lower  Tuvalian  Tor  Formation,  overlain  by  the
Portella Dolomite and the Lower to Upper Tuvalian Carnitza
Formation (Lieberman 1978; De Zanche et al. 2000).

The Hahnkogel/Klek tectonic block (see Fig. 2) is located

on  the  northern  side  of  the  Fella-Sava  fault  in  the  Southern
Karavanke  Mountains  (Ramovš  1993;  Krystyn  et  al.  1994;
Lein  et  al.  1995;  Schalf  1996).  The  Ladinian  (and  Julian?)
Schlern  Dolomite  is  followed  by  massive-  to  thick-bedded
dolomite  with  stromatolites  of  the  Conzen  Dolomite,  pre-
sumably Julian in age. The contact between the Conzen Do-
lomite  and  the  terrigenous  “Raibl  beds”  is  tectonically
disturbed. The latter consists of limestone, marlstone, marly
limestone and bivalve coquinas with features of tempestites
(Krystyn et al. 1994; Lein et al. 1995; Schlaf 1996), and they
are  coeval  to  the  Tor  Formation.  The  terrigenous  “Raibl
beds” terminate with Upper Carnian thin- to medium-bedded
dolomite with stromatolites, shallow water replacement chert
and  desiccation  cracks  (Krystyn  et  al.  1994)  coeval  to  the
Portella  Dolomite.  A  progressive  deepening  starts  with  the
Upper Tuvalian(?) Carnitza Formation (Krystyn et al. 1994;
Lein et al. 1995; Schlaf 1996) and the overlaying Lacian to
Alaunian Bača Dolomite (Krystyn et al. 1994). Synsedimen-
tary  tectonics  is  evident  through  slumps  and  debris-flow
breccias (Krystyn et al. 1994; Lein et al. 1995). The dolomitic
unit  grades  upwards  into  platy  and  thin  bedded  bioturbated
hemipelagic limestone with chert nodules of the Upper Seva-
tian to Rhaetian Frauenkogel Formation, featuring in its lower
part three massive mass-flow breccias (Krystyn et al. 1994).

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The youngest lithological unit of the Hahnkogel/Klek area
consists of medium thick beds of micritic limestone of Rha-
etian? and Early Jurassic age (Hahnkogel Formation) rich in
sponge spicules and radiolarians (Krystyn et al. 1994; Lein et
al. 1995; Schlaf 1996).

A hypothetical Cave del Predil-Tamar Valley-Mt Hahnko-

gel/Klek transect depicts a progressive deepening towards the
present northeast (Fig. 9). The most proximal position of the
Cave del Predil area can be assumed on the basis of a stronger
terrigenous influence in the pre-Tuvalian units and according
to  the  early  sealing  of  the  basin  by  the  Dolomia  Principale
clinobeds.  The  distal-most  position  of  the  Hahnkogel/Klek
section is finally supported by the continued deep water sedi-
mentation in the Early Jurassic and the diminishing supply of
the  platform  derived  carbonate,  reflected  in  a  shorter  strati-
graphic time span of the Bača Dolomite.

Evidence of a western extension of the Tarvisio Basin is

found at least up to the upper Dogna Valley (Sompodogna)
where the Carnitza Formation overlays the Portella Dolomite
(Preto et al. 2005). In the same place, there is evidence of a
margin-slope system connected to a shallow inner lagoon
area (Monticello Member of Dolomia Principale – Roghi &
Dalla Vecchia 1997; Preto et al. 2005; Caggiati 2014). Fur-

ther to the west, basinal conditions in the Late Tuvalian are
only  reported  in  the  Santo  Stefano  di  Cadore  area  (Geyer
1900;  Gianolla  et  al.  1998,  2010;  Caggiati  2014),  but  the
spatial  connection  with  the  Tarvisio  Basin  can  only  be  as-
sumed due to the lack of Upper Triassic successions in most
of the Carnic Alps.

Towards the present east Gianolla et al. (2010) proposed a

link  between  the  Tarvisio  Basin  and  the  Slovenian  Basin.
Such  a  connection  was  also  envisaged  by  Krystyn  et  al.
(1994),  who  considered  the  Hahnkogel/Klek  succession  as
part  of  the  Slovenian  Basin.  However,  there  is  currently  no
evidence for or against this connection.

Conclusions

The Tamar Valley (NW Slovenia) structurally belongs to

the Tamar tectonic block of the eastern Southern Alps and is
bordered by the Resia-Val Coritenza backthrust to the south-
east and the Fella-Sava line to the north (Placer 1999; Ven-
turini & Carulli 2002). The Upper Triassic succession of the
Tamar Valley is composed of Julian peritidal to shallow
subtidal dolomite (the Conzen Dolomite), Julian to Lower

Fig. 9. Correlation chart for Upper Triassic basinal successions of the Southern Alps. Note that in the majority of cases (especially for the
Norian to Rhaetian interval; dotted lines), stratigraphic resolution based on the present knowledge does not allow exact correlation of the
formation boundaries.

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Tuvalian  marlstone  and  marly  limestone,  deposited  above
the  storm  wave-base  (the  Tor  Formation),  Lower  Tuvalian
peritidal to shallow subtidal dolomite bank (the Portella Dolo-
mite),  Upper  Tuvalian  well-bedded  dolomite  with  claystone
intercalations  (the  Carnitza  Formation),  Upper  Tuvalian  to
lowermost  Rhaetian  bedded  dolomite  with  chert  and  slump
breccias  (the  Bača  Dolomite),  and  Rhaetian  thin-bedded,
slightly  bituminous  and  laminated  limestone  and  marlstone
(the  Frauenkogel  Formation).  This  succession,  ending  at  a
thrust plane, records platform drowning during the Tuvalian
(top  of  the  Portella  Dolomite)  and  a  progressive  deepening
of the area during the Norian.

According to the deduced paleobathymetric setting, the

Tamar Valley succession was deposited in deeper water with
respect  to  the  Cave  del  Predil  succession,  belonging  to  the
same structural unit (i.e. the Tamar tectonic block). Both of
these, however, were deposited in shallower setting with re-
spect  to  the  Hahnkogel/Klek  section  (belonging  to  the
Hahnkogel/Klek  tectonic  block),  suggesting  a  bathimetric
trend among these three successions. This trend probably re-
flects  a  proximal  to  distal  evolution  along  a  section  of  the
passive  margin  of  the  Neotethys  Ocean,  preserved  in  the
eastern Southern Alps.

Acknowledgments:  This  study  was  financially  supported
by  the  Slovenian  Research  Agency  (Project  No. P1-0011),
and  by  the  Italian  PRIN  2010-2011  funds (Project
No. 20107ESMX9_004).  Thin  sections  and  conodont  sam-
ples were prepared by the laboratory staff of the Geological
Survey of Slovenia. The manuscript has been improved fol-
lowing constructive remarks by J. Pálfy, N. Preto and an un-
named third reviewer. Their help in improving the manuscript
is greatly appreciated.

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