ACTA GGM DEBRECINA Geology, Geomorphology, Physical Geography Series
DEBRECEN Vol. 3, 121–125
2008
Basic geomorphological characteristics of the Dinarides Mountain System
A Dinaridák f bb geomorfológiai jellemz i
András Bognár
University of Zagreb, Department of Geography, Maruli!ev trg 19., 10000 Zagreb, Croatia
Abstract – The mountain system of Dinarides, representing a part of the Alpine-Himalayan mountain belt, was characterized by complex
geotectonic development, marked by changing regimes. Geosyncline and especially orogenic evolution stages have played the most
significant role in the creation of present structural-morphologic characteristics of Dinaric relief. Namely, specific orogenic development
of the area (collision) defined the basic structural-genetic properties of existing morphostructures.
Dinarides are typical episubductional mountain systems having domed structure with internal abundance of structural-genetic type of
morphostructures: folded, folded-block, domed-folded-block, folded-block-thrust, etc. Three morphostructural zones are identified:
Inner, Central and Outer Dinarides. They are mutually different according to properties of their structure as well as the grade of
conformity between relief and geologic structure. As a significant element of relief shaped in folded-thrust-nappe morphostructures
polygenetic erosional surfaces should be distinguished (so-called karst plateau like South-Istria, Northern Dalmatian-Kistanje, BrotnjoDubrave, Zadvarje, plateau around Cista, Imotsko and Sinjsko poljes, etc.). They have fluvial-corrosive origin, but probably have been
predisposed additionally by allochtonous tectonics.
Összefoglalás – A tanulmányban a szerz összegzi kutatásait a Dinári-hegylánc morfológiájával kapcsolatban. Az Eurázsiaihegységrendszer részeként számon tartott hegységívet komplex geológiai-tektonikai szerkezet jellemzi, mely az id k folyamán többször is
módosult. A geoszinklinális és orogén folyamatok játszották a legfontosabb szerepet a tipikusan episzubdukciós Dinári-hegység
szerkezetmorfológiájának alakításában. A morfostruktúrát gy!r dések, blokkos feltolódások, töréses-gy!rt szerkezetek jellemzik, melyek 3
szerkezetmorfológiai régiót alkotnak: a Bels -, Központi- és Küls -Dinaridákat. Geológiájuk, reliefjük és szerkezetmorfológiájuk eltér . A
gy!rt-feltolódásos-takaróred s struktúrákon különféle poligenetikus eróziós felszínek különíthet k el, melyek zömmel fluviális-korróziós
eredet!ek, de vélhet en allochton tektonika is szerepet kapott átformálásukban.
Keywords – Dinarides Mountain system, folded-thrust-nappe morphostructures, polygenetic erosional surfaces, allochtonous tectonism
Tárgyszavak – Dinári-hegység, gy!rt-feltotlódásos-takaróred s szerkezet, poligenetikus eróziós felszínek, allochton tektonika
Introduction
Relief structures are represented by mutually parallel
mountain ranges, massifs and ridges, which, owing to the
stress interchange in a more recent neotectonic stage
(Pliocene, Quaternary), experienced deformations as a
consequence of strike-slip faults, rotations of particular
blocks and tectonic inversions. In an orographic sense,
these are all linear or arched elevations generally elongated
towards the NW-SE. As a step-like outline dominates in
the transversal profile of elevations, it is evident that the
uplift (T>D) and planation (T=<D) stages interchanged
during their development. Consequently, geomorphologic
specifics of the Dinarides mountain system are reflected in
the great energy amplitude of morphogenetic processes,
which causes a contrast relief development (according to its
sign and amplitude) in time and space. Although there are
no major deviations in the general structural make up of
the Dinarides in relation to other mountain chains of the
Alpine-Himalayan belt (PÉCSI 1975, BOGNÁR 2001), some
differences have been identified in the characteristics of the
Dinarides’ inner structure. Evidence has been supported by
the characteristic direction of the morphostructures (NWSE), the zonal orientation of structural-genetic entities and
their position within the mountain system of the Dinarides;
specifically, geomorphologic development of particular
morphostructural zones is substantially influenced by either
their “inner” or “outer” position within the mountain
system. This could be related to the properties of the
Dinarides’ geo-tectonic evolution. Consequently, two
structural-morphologic zones should be considered: the
Inner and the Outer Dinarides.
The Inner Dinarides
The structural-morphologic zone of the Inner
Dinarides represents a geo-tectonic and structuralmorphologic entity spreading among the Central Alps to
the north, the Pannonides to the south, the Moravides to
the east, and Central Dinarides to the south-west. In
structural genetic sense it represents the oldest part of the
mountain system originating from the Upper Jurassic. This
zone belongs to the subduction zone that was subdued to
the oldest folding and thrusting phenomena, being
probably accompanied by obduction processes. Today, a
well-developed zone of ophiolites and ophiolitic melange
strongly supports the above model.
The zone structure was created during the tectonicgenetic stages, when the folded block thrusts and plate
(Zlatibor) structural-genetic types of morphostructures
were formed. Ophiolitic bodies are identified as blocks and
plates being subdued to uncharacteristically horizontal
directions during the closing-phase of the geo-syncline and
the collision of the continental platforms. Joining folded
block thrusts of ophiolitic melange (olistholith, diabase,
serpentinite, peridotite, gabbro, etc.) are found as
allochtonous structures. Denudation-tectonic morphostructures formed by uplifting during the orogenic
(neotectonic) stage in the middle Miocene and onwards.
They are morphologically expressed as mountain massifs
(Kozara 978m, Uzlomac 1,018m, Borja 1,077m, Ozren
917m, Konjuh 1,328m, Zlatibor 1,496m, Maljen 1,013m,
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ACTA GGM DEBRECINA Geology, Geomorphology, Physical Geography Series Vol. 3
Suvobor 864m, Rudnik 1,132m, "emerno 1,579m,
Kopaonik 2,017m, etc.) having a predominantly radial and
arch-radial, and, to a lesser extent, linear (ridges) orography.
The shape of the massifs is commonly isometric. In
morpho-tectonic sense, they are classified as folded blockthrust mountain massifs belonging to the ophiolitic Dinaric
zone (BOGNAR, 1992) On some massifs, denudation levels
(i.e. pediments) and remnants of poly-genetic plateau
(Kopaonik, Zlatibor, etc.) are common. The pre-glacial
modelling, and subsequent glaciation of the highest
mountain zones, was the result of a large-scale uplifting of
the area. Evidence comes from the remnants of the
corresponding morphologic forms (cirques, moraines, etc.).
The domed folded block-massifs of so called DrinaIvanjica and Vlaši#-Blizonja anticlinorium are characterised
by a predominantly arch-radial orographic structure, and
they represent a significant structural-genetic element of
the mountain zone of the Inner Dinarides. HERAK in 1991
described them as a remobilised section of the AdriaticPuglia microplate, due to their allochtonous position; in
reality these massifs consist of a block characterised by a
continental basement. Block-folded and block structuralgenetic characteristics are typical of the moprhostructures
found along the flysch zones on the Inner Dinarides,
within the south-western limb of the North-Western
Croatian Basin, northern Bosnia, and northern Serbia.
Eocene flysch sediments deposited in the trough valley,
were partly folded during the younger Palaeogene, being
subsequently subdued to strong disjunctive deformations in
the neotectonic stage. Consequently, the formation of
horsts and horst-anticlinories (Zrinska Gora 616m, Vu$jak
368m, Trebovac 692m, Majevica 915m, and Kosmaj 626m)
followed. In morphological sense, they are expressed as
low and moderately high massifs having a radial ridge
orography.
In a morphostructural sense, the SW part of the Inner
Dinarides mountain zone represents a transitional area. It is
visible through the development of polycyclic compound
morphostructures. The exhumation of the Hercynian
basement, and re-preparation of the folded zones, took
place along the sections of the platform characterised by a
thin carbonate cover. Mountain massifs with domedfolded-block structure-genetic properties formed over
those structures during the neotectonic stage, as, for
instance, the Bosnian Schist Mountains, which have a
prevailing radial, radial-arch, and ridge orography (Vranica
2,110m, Raduša 1,955m, and Komar 1,510m). During the
neotectonic stage, faulting of blocks having different uplift
rates took place in the area, with the prevailing thrust cover
formed a gravitational platforms. Additionally, mountain
massifs and morphostructural ridges with predominantly
folded-block-thrust and block-folded-thrust structuregenetic properties (Bjelašnica 2,066m, Jahorina 1,900m,
Treskavica 2,086m, Viso$ica 1,927m, etc.) also emerged.
During the orogenic stage nearly all the uplifted mountain
massifs and ranges were exposed to glaciation and
periglacial modelling. The morphology of their highest
sections is marked by the corresponding glacial and
periglacial
morphosculpture
(Vranica,
Bjelašnica,
Treskavica, Zelengora, Magli#, etc.). In the neotectonic
period, besides the typical structure of parallel range
sequences, the block mountain massifs were also formed
2008
by the stress change from the direction NE-SW to the
general direction N-S under the influence of faulted
tectonics and rotation of particular blocks (mountain
massif of Risnjak, mountain massif of Li$ko Sredogorje,
and mountain massif of Poštak). The planated higher
regions of the tallest mountain structures (Dinara and
Velebit) correspond to the remains of a Mesozoic erosional
surface – the peneplain. As a consequence of the prevailing
carbonate composition (limestones and dolomites), the
morphosculpture of the mountain elevation surfaces is
marked by the domination of various types of karst and
fluviokarst relief. The mountain tops above 1,300 metres
are characterised by morphologic traces of the Pleistocene
glaciation (moraines, cirques, glacial waves – the mountain
structures of Risnjak, Velebit, Li$ka Plješivica, Dinara and
Kamešnica).
The Outer Dinarides
The Outer Dinarides geotectonic zone comprises
mountain ranges, mountain groups, and mountain ridges of
a folded-faulted-imbricated geologic structure. The Dinaric
direction (NW-SE) of the mountain structures, the dry
valleys, and smaller basins (pull-apart structures basin of
poljes in karst: Imotsko Polje, Sinjsko Polje, Livanjsko
Polje, Mostarsko Blato, Krbavsko Polje, Gacko Polje,
Glamo$, Grahovsko Polje, Biha#ka Zavala, etc.) parallel to
them, prevails. During the neotectonic period, the stress
change (from the direction NE-SW to the direction N-S)
caused changes in the expansion direction of certain
elevations by rotation of blocks into the N-S direction
(mountain range of U$ka, range of Promina). The coastal
mountain ranges and the ridges have mainly an
asymmetrical transversal outline. This is in accordance with
the dominant reverse tectonics and imbricated structure of
the elevations. Examples are the mountain ranges and
ridges of Boraja-Vilaja-Opor-Kozjak-Mosor-Perun-Omiška
Dinara-Biokovo-Rili# and the ridge of the Central
Dalmatia’s interior; here, a carbonate structure with various
types of karst is common. Dry valleys (in Ravni Kotari) and
basins (Dicmo, Imotsko-Bekijsko Polje) run parallel with
the elevations and they are filled with flysch and
Quaternary sediments. The present erosional surfaces on
the Dinarides (Fig. 1) can be found at various levels (SouthIstrian, North-Dalmatian, Zadvar’s, Brotnjo-Dubrava,
Lika’s, the erosional surface on Northern Velebit, on the
mountain massifs of "vrsnica, Bjelašnica, Treskavica,
Durmitor, etc:); consequently, nearly from sea level to
1,000m and more than 2,000m above sea-level, they
represent traces of one, once larger, complete, and older
planation surface. During the neotectonic development
stage, this surface was intensively disarranged and
fragmented, and its surviving sections were transported to
various hypsometric positions. Some evidence for this
model can be deduced by the observation of regionally
extensive bauxites, which can be treated as correlative
weathering sediments in tropic-equatorial climatic
conditions. The existence for such climatic regime has
never been proposed for the Cainozoic; consequently, this
model describes a unique peneplained planated surface of
the Mesozoic age.
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Bognár, A.: Basic geomorphologic characteristics of the Dinarides…
GENERAL GEOMORPHOLOGY
Figure 1 Erosional surfaces and pediments in the mountain zone of the Outer Dinarides.
A. Parts of the erosional surfaces of the Mesozoic age
1. Fragments of denudational erosional surface on autochthonous structures (Adriatic platform) – exhumed and disturbed during the Tertiary and
Quaternary – several times exposed to denudational processes during the younger Palaeogene and in Neogene (South Istrian erosional surface).
2. Fragment of erosional surface on allochthonous structures
21 Fragments of denudational erosional surfaces – disturbed in the Palaeogene, Tertiary and Quaternary and exposed to repeated
denudational processes during particular time intervals of the quoted geologic periods with traces of partly exhumed peripedimentation (erosional
surfaces Brotnja, Dubrava, etc.).
22 Fragments of denudation-accumulation planation surfaces – disturbed and partly exhumed, as well as exposed to the repeated
denudational planation processes with peripedimentation traces – less expressed relative relieves (Northern Dalmatian erosional surface).
23 Fragments of denudational planation surfaces – intensively disturbed and elevated to various heights above sea-level with a prominent
relative relief (even to 300m/km2) – exposed to the repeated denudational processes during the Tertiary and Quaternary with traces of
pedimentation, probably exhumed (most of high erosional surfaces).
B. Younger pediments formed by the end of the Miocene, and with the traces of the Quaternary denudational planation processes in the Pliocene –
partly disturbed and destroyed – elevated to various heights.
C. Uplifting
1. ábra Eróziós felszínek és pedimentek a Küls -Dinaridák hegységi zónájában.
A. Mezozóos eróziós felszínek
1. Dnudációval átformált, a harmad- és negyedid szakban exhumált eróziós felszínmaradványok Autochton szerkezeteken (Adriai-platform),
melyek a paleogén végén és a neogén során többször voltak kitéve denudációs folyamatoknak (dél-isztriai eróziós felszín).
2. Allochton szerkezeteken kialakult eróziós felszínmaradványok
21 Paleogénben, a harmadid szakban és a negyedid szakban bolygatott, majd az említett korokban ismételt denudációs folymatoknak kitett
és szemiexhumált, peripedimentáció nyomait mutató denudációs felszínmaradványok (Brotnja, Dubrava eróziós felszínek stb).
22 Denudációs-akkumulációs elegyengetett térszínek maradványai, részben exhumáltak, bolygatottak és ismételt denudációs folyamatoknak
voltak kitéve peripedimentációs nyomokkal (észak-dalmáciai eróziós felszín).
23 Denudációval elegyengetett felszínmaradványok, intenzíven átformált és különböz magasságokba kiemelt, helyenként igen jelentékeny
relativ relieffel (akár 300m/km2) bíró felszínek a harmad- és negyedid szak során ismételt denudációs folyamatoknak kitéve, feltehet en
exhumált magas eróziós felszínek.
B. Miocénben kiformálódott pliocén elegyengetés által érintett, részben megsemmisült, különböz magasságokra kiemelt fiatal pedimentek.
C. kiemelkedés
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2008
Figure 2 Morphological and structural genetic profile of Dinarides range
2. ábra A dinári vonulat morfológiai és szerkezeti genetikai szelvénye
Erosional surfaces can be observed on the majority of
the mountain ranges and massifs of folded-thrust and
folded-imbricated structural-genetic material in the Outer
Dinarides mountain zone. These are characterised by a
specific step-like outline of their transversal profiles (Fig.
2). This scenario supports their complex geomorphologic
124
Bognár, A.: Basic geomorphologic characteristics of the Dinarides…
evolution marked by the alternation of uplift stages with
those of relative tectonic inactivity favourable to
denudational-planation processes, relations proved by the
existence of two clearly marked steps-pediments.
Exceptions are the fragments of older erosional levels, i.e.
the surface, which are, in view of their morphologic
position, connected with the mountain ranges’ tops and
massifs, then with the parts of the karst poljes bottoms, the
marginal parts of the Outer Dinarides towards the Adriatic
basin, and with the Pannonian basisn.
The mountain ranges, massifs, and the mountain
groups of folded-faulted-thrust geologic structure of the
Dinaric mountain system were formed during the Alpine
orogeny. In geotectonic sense, they represent a part of the
Outer Dinarides zone. It is important to note the prevailing
specific Dinaric direction (NW-SE) of the expansion of
mutually parallel, linearly elongated or arched mountain
elevations (Risnjak – V. Kapela – M. Kapela – Li$ka
Plješivica; Uilica – Dinara – Kamešnica; Tuhobi# –
Medve%ak – Kobiljak – Range of Veljun – Velebit; Kozjak
– Svilaja), and intermontane basins and uvalas. Generally,
we find a strong relation between the orographic and
geologic structure (elevations-anticlines, anticlinoria;
recesses – synclines, depressions, synclinoria), but some
deviations of discomforming features have also been
determined (elevations – synclinorium of Dinara and
Svilaja, successions of the upper Cetina flow basins –
anticline –anticlinorium). The insular relief of the NE part
of the Adriatic Sea maritime zone commenced during the
post-Pleistocene by glacio-eustatic rising of the sea level by
around 100 metres. Geo-tectonically, it belongs to the zone
of the Outer Dinarides with a prevailing folded-faultedimbricated geologic structure. An identical folded-blockimbricated geologic structure was mainly comfortably
reflected in the relief. The Dinaric direction (NW-SE)
dominated the extension of the islands, the mutually
parallel mountain ridges, and the ranges formed on them,
as well as those dry valleys and basins which consequently
became channels, bays, gulfs, and straits as a result of sea
transgression in the post-Pleistocene. In the neotectonic
period, the stress change from the NE-SW direction to the
general N-S direction, and rotation of certain smaller
tectonic blocks, resulted into the change of the expanding
direction of some relief entities: the Central Adriatic Islands
(the islands of Drvenik, Šolta, Bra$ and Hvar – so called
Block of Hvar) to the E-W direction, a part of the
Dalmatian Island to the E-W and WNW-ESE direction
(Kor$ula) (Mljet), and the Kvarner Islands (Unije, V. and
GENERAL GEOMORPHOLOGY
M. Srakane, Cres, Lošinj, Plavnik, Rab, Krk and Prvi#) into
a fan-shaped (radial) extension outline.
Conclusions
The mountain system of Dinarides, representing a part
of Alpine-Himalayan mountain belt, was characterized by
complex geotectonic development, marked by changing
regimes. Geosyncline and especially orogenic evolution
stages have played the most significant role to creation of
present structural-morphologic characteristics of Dinaric
relief. Namely, specific orogenic development of the area
(collision) was defined the basic structural-genetic
properties of existing morphostructures.
Dinarides are typical episubductional mountain system
having domed structure with internal abundance of
structural-genetic type of morphostructures: folded, foldedblock, domed-folded-block, folded-block-thrust, etc. Three
morphostructural zones are identified: Inner, Central and
Outer Dinarides. They are mutually different according to
properties of their structure as well as a rate of conformity
between relief and geologic structure. As a significant
element of relief shaped in folded-thrust-nappe
morphostructures polygenetic erosional surfaces should be
distinguished (so-called karst plateau like South-Istrian,
Northern Dalmatian-Kistanje, Brotnjo-Dubrave, Zadvarje,
plateau around Cista, Imotsko and Sinjsko poljes, etc.).
They have fluvial-corrosive origin, but probably have been
predisposed additionally by allochtonous tectonics.
References
BOGNAR, A., 2001: Geomorphological Regionalisation of
Croatia. Acta Geographica Croatia, 34
BOGNAR, A., 1992: Basic Structural-Morphological
Characteristics of the Dinarides. – Proceedings of the
international symposium “Geomorphology and Sea”
and the meeting of the Geomorphological
Commission of the Carpatho-Balcan Countries,
Department of Geography, Faculty of Science
HERAK, M., 1991: Dinarides – Mobilistic View of the
Genesis and Structure. Acta Geologica, 21,
PÉCSI, M., (special consultant Bognar, A.) 1975:
Geomorphological Map of the Carpathian and
Balcan Regions (1:1.000 000). – Geographical
Research Institute of Hungarian Academy of
Sciences, Budapest.
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