1. INTRODUCTION

The structural relationships of northwestern Croatia

and the adjacent regions of Slovenia and Bosnia were

and remain subject to different treatment. The main

approaches are as follows:

PETERS (1863) assumed the existence of an anci-

ent “Palaeolithic Land” within the Balkan Peninsula,

comprising the “crystalline cores of Slavonia and Sie-

benburgen”. This megastructure was not supposed to

have participated in tangential Alpine tectonics. SUESS

(1875) attributed northwestern Croatia (including Mt.

Medvednica) to the Southern Alps, while DIENER

(1903) regarded the area as part of the Eastern Alps.

MOJSISOVICS (1880) accepted the “Land” defined by

PETERS and introduced the name “Oriental Land”.

However, he experienced difficulty in defining its

boundaries. PILAR (1882) was involved with the geol-

ogy of western Bosnia and concluded that the “flysch”,

containing “eruptive rocks” (including ophiolites), con-

tinued into Croatia. Later, KI©PATI∆ (1899), studying

ophiolites, accepted the opinion that Mt. Medvednica

was a continuation of northern Bosnia (i.e., of the Inner

Dinarides), as did also GORJANOVI∆-KRAMBER-

GER (1907), with the exception of the part which was

Tectonic Interrelation of the Dinarides and the Southern Alps 

Milan HERAK

attributed to the “Oriental Land”. SALOPEK (1914),

analysing modern tectonic concepts, concluded that

autochthonous relationships characterize NW Croatia.

CVIJI∆ (1924) accepted the idea of the ancient land (he

called it the Rhodopian Mass) but considered its bound-

aries as ambiguous. Therefore, he proposed to distin-

guish transitional zones between the “Land” and its sur-

roundings. KOCH (1924) gave preference to the Dinar-

idic elements in the whole area, and included even the

Slavonian Mountains into the Dinarides. WINKLER

(1924) believed in north-vergent allochthony in the

adjacent area of the Slovenian “Sava Folds”, probably

under the influence of Suess’s concept of a northward

push of the Southern Alps.

In recent times, MIO» (1975, 1981) paid special

attention to the “Sava Folds” and to the area of the

Lower Carniolia (Dolenjska, eastern Slovenia). He defi-

ned a unit named the Sava Nappe which overlies the

Outer Dinarides, and is overlain by a south-vergent

nappe composed of elements of the Julian and Savinja

Alps. The extension of such relationships should be fol-

lowed towards Mt. Æumberak (comprising the area of

Samobor). PREMRU et al. (1977), by means of some

deep boreholes, established a well-marked allochthony

in Lower Carniola (Dolenjska) and in the adjacent Mt.

Æumberak. They considered the area as a part of the

Outer Dinarides. The “Litija anticline” was defined as

the Dolsko overthrust (PREMRU, 1983, and earlier).

GEOL.  CROAT. 52/1 83 - 98 4 Figs. ZAGREB 1999

Key words: Alps, Dinarides, Tisia, Slovenian Trough,

Sava Nappe, Pannonian Nappe, Mid-Transdanubian

Zone, Bosnian Zone, Tectogenesis and geotectonic

classification.

KljuËne rijeËi: Alpe, Dinaridi, Tisia, Slovenski jarek,

Savska navlaka, Panonska navlaka, Srednja transda-

nubijska zona, Bosanska zona, tektogeneza i tekto-

genetska klasifikacija.

Croatian Academy of Sciences and Arts, A. KovaËiÊa 5/II, HR-10000

Zagreb, Croatia.

Abstract
The study focuses on northwestern Croatia which, including the

Æumberak (ÆumberaËka gora), Medvednica (ZagrebaËka Gora),

Kalnik, IvanπËica, and Ravna Gora mountains, make a cross area of

the Slovenian “Sava Folds”, Southern Alps, Mid-Transdanubian

Zone, Tisia, and the Inner Dinarides. This is a complex structural

region and cannot be attributed merely to one of the units. Therefore,

a geotectonic interpretation is proposed which respects the diversifi-

cation and multiple superposition of basinal and platform elements.

This concept allows linkage of the Slovenian Trough with the Bosn-

ian Zone and its southeastern prolongation as a major coherent tec-

tonic unit overlain by different nappe elements. The possible linkage

with the Budva Zone beneath the carbonate nappe is also discussed.

Saæetak
Glavna je pozornost posveÊena sjeverozapadnoj Hrvatskoj, koja

ukljuËuje ÆumberaËku goru, Medvednicu, Kalnik, IvanπËicu i Ravnu

goru - presjeciπte susjednih slovenskih “Savskih bora”, Juænih Alpa,

Srednje transdanubijske zone, Tisije i Unutarnjih Dinarida. To je

sloæeno strukturno podruËje, pa ne moæe biti pribrojeno samo jednoj

jedinici. Zbog toga se predlaæe geotektonska interpretacija koja

uvaæava diverzifikaciju i viπestruku superpoziciju bazenskih i plat-

formskih elemenata. Ovaj koncept omoguÊuje povezivanje Sloven-

skog jarka s Bosanskom zonom i njezinim jugoistoËnim produæenjem

u jednu koherentnu tektonsku megajedinicu na kojoj leæe razliËiti

navlaËni elementi. Takoer se raspravlja o moguÊoj vezi s Budva-

zonom.



84 Geologia Croatica 52/1

The same unit has been subdivided in detail by MLA-

KAR (1987). ©IKI∆ et al. (1978, 1979), ©IMUNI∆

(1992), ©IMUNI∆ & HE∆IMOVI∆ (1979), etc., intro-

duced short distance overthrusting with different ver-

gences to explain the tectonic pattern of Mt. Æumberak

(with the area of Samobor) and Mt. Medvednica as well

as of Hrvatsko Zagorje. They contributed new data to

previous interpretations. MILADINOVI∆ (1981) argu-

ed for the existence of an extensive allochthonous unit,

called the Pannonian Nappe. The idea was born in 1974

(see: MILADINOVI∆, 1981) on the basis of the study

of many published papers and with insight from the

geologic mapping data. The maps have been made by

numerous authors who registered several inverse con-

tacts but did not evaluate them in a geotectonic sense.

MILADINOVI∆ has drawn his tectonic map in 1977

and elaborated in 1981. The nappe concerns only Upper

Palaeozoic and Triassic rocks, which overlie Creta-

ceous and Jurassic formations. The Nappe should cover

a broad region stretching from Italy through the Julian

Alps, South Karavanke and Savinja Alps, to the “Sava

Folds”, Mt. Æumberak, Banovina, North Bosnia, Uæice,

Prizren, Pljevlja, “Pelagonian Massif”, etc. Within this

megaunit, several tectonic windows and klippen were

identified, which include the “Zlatibor” window. Since

the most characteristic areas lie outside the Pannonian

Depression, the name of the assumed nappe has not

been generally accepted. Likewise, there are some regi-

ons that cannot be included into such a simple model of

this unit, especially the composite structure called the

“Pelagonian Massif”. As to the Western Dinarides, the

idea itself may be generally acceptable. However, the

details require refinement.

The possible connection of the Slovenian Trough

with the Bosnian Zone has been registered in several

papers. In Mt. Æumberak, TORNQUIST (1918) deter-

mined pelagic sediments of Late Tithonian, Berriasian

and Valanginian age. He considered them as a link bet-

ween analogous Slovenian and Bosnian deposits.

AUBOUIN et al. (1970), COUSIN (1973), and BABI∆

(1973, 1974) were concerned with the same problem,

speaking in favour of such a connection. AUBOUIN et

al. (1970) assumed the existence of a “Furrow”, in

which specific (“basinal”) formations have been depo-

sited since the Late Triassic. However, they do not

explain the type of boundary between this “Furrow”

and the oceanic realm of the Inner Dinarides, which is

characterized by ophiolites and is visible in their recon-

struction of the major structures where they propose a

direct overthrust of the ophiolitic complex upon the ele -

ments of the “Furrow”.

Later, BABI∆ & ZUPANI» (1978) again evaluated

the analogies between the Julian Alps and the Dinarides

and contributed some additional elements in favour of a

direct connection. However, they also called attention

to some difficulties. For instance, between the Tolmin -

Selπka Sora area and the Æumberak area, differences

exist in the timing of their aquisition of basinal charac-

ter. In the Tolmin - Selπka Sora region, the basin may be

formed during the Triassic, while in the Æumberak area

this occurred no earlier than the end of the Lower Juras-

sic. In contrast, DIMITRIJEVI∆ (1982) accepted the

existence of a homogenous zone extending from the

Julian Alps, over the “Sava Folds” and “Zagreb Zone”

(i.e., Mid-Transdanubian Zone in the current terminolo-

gy), but he placed a sharp boundary towards the Dinar-

ides (inclusive of the Vardar Zone, s . l .). Though aware

of great differences within the area of the so-called

Inner Dinarides, I preferred to attribute the area in ques-

tion to a common Inner Dinaric megaunit (S u p r a d i n a r -

i c u m) with possible interior differentiation (HERAK,

1986, 1991, 1995, 1997). For example, the structures

consisting of Late Palaeozoic and Triassic rocks were

considered as overthrusting parts of the bottom margin

of the Inner Dinarides. More recent explanation of the

origin of this nappe requires emendation as discussed

later. PAMI∆ (1993) was concerned with Eoalpine and

Neoalpine magmatic and metamorphic processes in the

northwestern Vardar Zone, the easternmost Periadriatic

Zone and the southwestern Pannonian Basin. He was of

the opinion that the mountains of Hrvatsko Zagorje

“can be interpreted as relics of the Sava and/or Julian -

Savinja nappes”. He proposed to introduce more Dinar-

idic elements when treating southern marginal parts of

the Pannonian Basin. The participation of Dinaridic ele-

ments in the Mid-Transdanubian Zone was also ackno-

wledged by BERCZI-MAKK et al. (1993). Authors

from the Institute of Geology in Zagreb use the term

Mid-Transdanubian Tectonic Zone, which is not delim-

ited towards the Inner Dinarides (©IKI∆, 1995), as did

many other authors, e.g. HAAS et al. (1995). However,

by some authors sharp tectonic limits towards the

Dinarides were assumed (e.g., DIMITRIJEVI∆, 1982).

There are many more papers with controversial con-

cepts, but all of them are within the frame of these ideas

and, therefore special commentary of them is omitted.

By comparison of the proven data in NW Croatia

and eastern Slovenia, the heterogeneity of the region

(called the Mid-Transdanubian Zone) is obvious, with

the consequence that Dinaridic and Alpine elements are

superimposed. However, the tectogenetic processes and

the interior organisation remain under discussion.

Despite the fact that within northwestern Croatia

numerous new data, concerning lithostratigraphy and

local tectonics, have been collected (©IMUNI∆ &

PAMI∆, 1989; HERAK et al., 1990; ©IMUNI∆, 1992;

©IKI∆, 1995; HALAMI∆ & GORI»AN, 1995, etc.), a

general comparative treatment concerning Dinaridic-

Alpine geotectonic relations remains elusive. Therefore,

the major aim of this paper is to rectify that problem.

2. MAJOR LITHOSTRATIGRAPHIC

SEQUENCES

Mt. Medvednica (ZagrebaËka Gora) and Mt. Æum-

berak (ÆumberaËka Gora) display the greatest diversity

of lithostratigraphic units. In a relatively small space



there are numerous inverse tectonic contacts indicating

piling up of various lithocomplexes that require palin-

spastic reconstruction of the primary environments.

Compiled stratigraphic data on Mt. Medvednica

(©IKI∆, 1995) include units ranging in age from the

Palaeozoic to the Quaternary. Since the main purpose

of this paper is the reconstruction of palaeotectonic

relationships, the discussion of Neogene and Quater-

nary deposits is omitted.

As there is a high degree of stratigraphic diversifica-

tion, the origin of different stratigraphic complexes can-

not be explained by means of lateral facies within sin-

gle consistent depositional areas. Usable data have been

published in numerous papers cited by ©IKI∆ (1995).

In this paper, only the most pertinent ones will be taken

into account.

Generally, several primarily consistent lithostrati-

graphic successions, characterized by features indicat-

ing complementary palaeogeographic and tectonic div-

ersification in space and time (Figs. 1-4), can be distin-

guished in the Alpino-Dinaridic realm, though these are

dispersed at the surface.

2.1. VARISCAN BASINAL FORMATIONS

The Palaeozoic, from the Silurian to the Middle

Carboniferous, displays prevailingly basinal type of

carbonate and clastic sediments. They are exposed in

85Herak: Tectonic Interrelation of the Dinarides and the Southern Alps

Fig. 1  Diversification

of Mesozoic events

in the adjacent are-

as of the Dinarides

and the Southern

Alps: U) Upper-

most platform dep-

osits; S) Supradi-

naric oceanic roc-

ks; D) Dinaric pla-

tform deposits; E)

Epiadriatic pelagic

deposits and for-

mations with pela-

gic components.



86 Geologia Croatica 52/1

Mt. Medvednica (–UR–ANOVI∆, 1973; SREMAC &

MIHAJLOVI∆-PAVLOVI∆, 1983). Some outcrops are

slightly metamorphosed with relatively well-preserved

graptolites, conodonts, etc. Even in cases when they are

included into the younger metamorphic complex, it is

possible to use them as evidence of primary basinal

sedimentary conditions. However, in Trgovska Gora W

of the Una River, SE of Zagreb, only non-metamorphic

outcrops of the Devonian and the Carboniferous with

conodonts are present (–UR–ANOVI∆, 1973) what

indicates that they do not belong to the same tectonic

unit. The change from basinal type of sedimentation in

Fig. 2  Proposal of an emended and generalized map of the Dinaridic - South Alpine joint realm for further considerations; subductional tectonic

model, based on selected outcrop-areas with simplified and partially enlarged contours: 1) Neogene and Quaternary cover; 2) Austroalpine;

3) Tisia; 4) Uppermost Nappe (with some tectonic windows); 5) Supradinaricum (s. str.); 6) Dinaricum; 7) Epiadriaticum (pelagic deposits

and clastics with pelagic components); 8) Adriaticum; 9) ? Ionian underthrust; K) Mt. Kalnik (see Fig. 3); M) Mt. Medvednica (see Fig. 3);

Æ) Mt. Æumberak with the Samobor area (see Fig. 4); Iv) Mt. IvanπËica.



87Herak: Tectonic Interrelation of the Dinarides and the Southern Alps

the Middle Carboniferous is due to the Variscan oroge-

ny which formed the structural basis for later molasse

sediments. However, Variscan megastructures (with so-

me older tectonic elements) are preserved only in the

adjacent Slavonian Mountains belonging to the Tisia

(JAMI»I∆, 1983; HERAK et al., 1990).

Palaeozoic fragments (together with Triassic exam-

ples) are poorly preserved as protoliths of the younger

metamorphics (greenschists and associated schist mem-

bers). This rock complex with changed mineral compo-

sition originated during the process of progressive low-

grade metamorphism (BELAK et al., 1995a, b). There-

fore, it may be treated as a consequence of the Alpine

tectonic deformations and metamorphism.

2.2. VARISCAN MOLASSE DEPOSITS

The Late Palaeozoic is represented by Carbonifer-

ous deposits with corals as well as clastics, which con-

tain the remains of land plants (Banovina, SE of Zag-

reb). Various plant fragments are also found in Mt.

Medvednica and Mt. Æumberak.

The molasse deposists in the region of Samobor are

most characteristic. They consist of Permian (possibly

also of some Carboniferous) clastics composed of qua-

rtz conglomerates, lithoclastic graywackes, siltites, sha-

les, and sporadic dolomites. The terrestrial origin of the

clastic components is further proven by the remains of

land plants Calamites and Sigillaria (JENKO, 1944).

Evaporites were deposited in the transition time

between the Permian and the Early Triassic. They are

followed continuously by variegated clastics, what may

be decisive in the interpretation of the Uppermost

Nappe (Fig. 2, U), unifying Palaeozoic and Triassic

deposits as an integral unit which overlies oceanic for-

mations of the Inner Dinarides.

Some isolated platform outcrops are “strange” with-

in Variscan molasse deposits. Possibly they can derive

from the subducted (?) Dinaric platform. In an Eocene

breccia in Hrvatsko Zagorje (Vinica and Viπnjica W of

Varaædin), MILANOVI∆ (1982) found Middle Car-

boniferous limestone fragments with foraminifera and

calcareous algae. He correlated them with analogous

deposits in Mt. Velebit, Banovina, etc. In the area

northwest of Samobor (near the Bregana Village), in a

small isolated carbonate area, calcareous algae (Gymno -

c o d i u m, A t r a c t y l i o p s i s, etc.) have been determined

(HERAK & ©KALEC, 1967). In Mt. Medvednica a

boulder has been found which contains remains of

N e o s c h w a g e r i n a ( D E V I D É - N E DĔLA & KOCHAN-

SKY-DEVIDÉ, 1990). ©IMUNI∆ (1979) registered

Lower Permian algae in a non-metamorphosed lime-

stone in Mt. Medvednica. 

2.3. TARDY-VARISCAN DYNAMICS AND

THE ORIGIN OF CARBONATE PLATFORMS

The main Lower Triassic components include: sand-

stones, siltites, marly limestones, oolitic limestones,

and some dolomites (in the upper part of the limestones

ammonites are preserved). The general tendency of

subsidence is obvious.

The Middle Triassic was a time of relative tectonic

disquiet, especially in the Anisian. Some rifting with

volcanism (mostly several types of basalts) and clastic

sedimentation occurred. However, generally dolomites

and dolomitized limestones prevail, continuing also into

the Ladinian. At several horizons of the Middle Trias-

sic, small areas of ammonitic limestones have been fou-

nd. The tectonic dynamics in the Middle Triassic was

tardy-Variscan (final), forming the basis for the origin

of later carbonate platform areas.

In the Upper Triassic, stromatolitic dolomites and

some limestones with megalodontids predominate. Car-

bonate sedimentation lasted until the Palaeogene with

some oscillations indicated by shallow water clastics

and small gaps (CRNJAKOVI∆, 1981).

2.4. MESOZOIC DEPOSITS WITH

PELAGIC INFLUENCES

The outcrops of Late Triassic pelagic deposits are

encircled either by platform or by oceanic facies from

which they can be distinguished: from the platform for-

mations by the type of sediments (platy limestones,

radiolarites, etc.), and from the oceanic formations by a

lack of a magmatic-sedimentary complex with ultra-

mafics and mafic intrusives. On the NW side they out-

crop in the Slovenian Trough (GRAD, 1961; COUSIN,

1973; LAPAJNE & ©RIBAR, 1973; PREMRU, 1975,

1983; BUSER, 1977, 1989; BABI∆ & ZUPANI»,

1978; BABI∆, 1980/81; JURKOV©EK et al., 1990,

etc.). Towards the E and SE they are present at many

isolated sites.

In recent times, very important dispersed pelagic

outcrops have been described on the northern slope of

Mt. Medvednica and on Mt. Kalnik (Fig. 3), and then

on Mt. Æumberak (Fig. 4).

At the localities of Mt. Kalnik the metabasalts,

shales and radiolarites outcrop. Primary contacts with

the surrounding facies are not clearly visible. Locally,

the outcrops are composed of heavily tectonized rocks.

The lower part of the succession is composed of calcit-

ized, porphyritic, ophitic metabasalts. The age of the

radiolarites corresponds to the Carnian-Norian time

interval (HALAMI∆ & GORI»AN, 1995).

On the northwest slope of Mt. Medvednica radiolar-

ian cherts alternate with silty shales. The sediments are

intensely folded, partially even overturned. Their base

is not known due to intensive tectonics, and they are

non-conformably overlain by Palaeocene calcitic silt-

stones. However, it is probable that the examined Trias -

sic radiolarites are partially overlain by similar silty

siliceous sediments (radiolarian cherts, shales, etc.) of

uncertain Jurassic age (HALAMI∆ & GORI»AN,

1995, p. 135).

In the adjacent area of Mt. Hum, NW of Mt. Med-

vednica (valley of Burnjak), limestones with intercala-



88 Geologia Croatica 52/1

tions and lenses of chert outcrop (©IKI∆, 1995). Dis-

continuous fragments of pelagic outcrops, belonging to

the transition between the Upper Triassic and the Lias

are also present, as well as pelagic limestones with radi-

olarians and lagenid foraminifera of Late Lias - Dogger

age. Some isolated outcrops belong to the Jurassic-Neo-

comian, others to the Tithonian-Berriasian, with a pos-

sible “hard ground” at the contact with Triassic dolomi-

tes (BABI∆ & ZUPANI», 1973; BABI∆, 1975; ©IKI∆,

1995, p. 15). The incompleteness of the columns is

ascribed to the condensed sedimentation. In Mt. Ivanπ-

Ëica, ZUPANI» et al. (1981), and ©IMUNI∆ (1992)

also emphasized that, due to the “hard ground”, Tithon-

ian-Valanginian deposits non-conformably overlie dif-

ferent stages of the Triassic. Explanation of such a phe-

nomenon in that way would anticipate intensive tecton-

ics at the end of the Triassic with the consequence that

the lack of sedimentation would last until the Late Tith-

onian. Such a hiatus there has not been substantiated.

Moreover, the origin of ophiolites, accompanied by

younger magmatic-sedimentary rocks in the same area,

argues in favour of intensive tectonics during the Juras-

sic and the Early Cretaceous. Besides, the Triassic in

question does not necessarily belong to the same tec-

tonic unit as the Triassic which constitutes the overly-

ing nappe.

Some other Lower Cretaceous outcrops also indi-

cate basinal sedimentation (with pelagic influences).

Such is the “Oπtrc formation” in Mt. IvanπËica descri-

bed by ZUPANI» et al. (1981). It overlies the afore

mentioned Tithonian-Valanginian pelagic deposits. The

formation consists of calcarenites, sandstones, marly

shale, and deposits with radiolaria and spicules. The

calcarenites frequently show silicification and recrystal-

lization phenomena. The authors concluded that the

part of the basin within the Mt. IvanπËica area originat-

ed upon the continental crust. Analogous relationships

also occur at Mt. Æumberak (BABI∆, 1974). Moreover,

correlation is assumed with the Vranduk area in Bosnia

belonging to the Bosnian Zone (defined by AUBOUIN

et al., 1970), which displays essential differences in

sediments beginning with the Late Triassic, and contin-

uing during the Jurassic and Cretaceous. The Zone may

be followed in Montenegro. In Western Serbia OBRA-

DOVI∆ & VASI∆ (1996, p. 191) speak of “isolated

bedded series” with radiolarites of different ages within

various complexes. Analogous deposits outcrop even in

Albania, however not as a continuous zone but as local-

Fig. 3  Simplified main tectonic units in the mountains Medvednica and Kalnik; basic data from ©IKI∆ (1995) and ©IMUNI∆ (pers. comm.),

reinterpreted: 1) Uppermost Nappe; 2) S u p r a d i n a r i c u m (with possible small Dinaric outcrops) disturbed by strong interior tectonism; 3)

pelagic deposits and formations with pelagic influences (interpreted as Epiadriaticum); 4) Neogene and Quaternary cover; 5) place of graph-

ical shortening of the terrain.



89Herak: Tectonic Interrelation of the Dinarides and the Southern Alps

ized “strange” bodies within the Mirdita Zone. All this

suggests that these deposits with pelagic elements are

tectonically emplaced within heterogeneous areas. 

Similar heterogeneity has been found even in other

morphotectonic units like the North Karavanke Alps

(MIO» & ©RIBAR, 1975), and in the Outer Dinarides.

The latter were discussed by many authors (cited in

HERAK, 1993). The age of dispersed pelagic deposits

within the Outer Dinarides range from the Triassic (out-

crops in the Budva Zone, and in the Slovenian Trough)

to the Late Cretaceous, with a predominance of Upper

Jurassic outcrops. At the margin towards the Inner

Dinarides even Palaeogene outcrops occur. They all

require a common provenance influenced by the same

open sea environment. The lack of both intrusives and

metamorphic rocks means that the distribution area of

pelagic components was outside the active orogenic re-

alm. Therefore, their recent position can only be expla-

ined by entangled tectonics, discussed later.

2.5. OCEANIC MEGAENVIRONMENT

The origin of a belt with oceanic components started

within the area most often called the Inner Dinarides.

According to GU©I∆ & BABI∆ (1972, p. 336), the

lithology and fossil contents of the fragments in the

Senonian breccia in Mt. Medvednica “show that the

Norian-Rhaetian limestones had been deposited in a

very shallow sea, whereas the Liassic sediments had

originated in a considerably deeper and quiet marine

environment”. It is important to mention that on the

northwestern slope of Mt. Medvednica a tectonically

delimited, narrow Upper Triassic - Dogger limestone

zone, partially dolomitized and recrystallized, is present

(©IKI∆, 1995). This means that, due to tectonic forces,

two major environments have been brought close to one

another. This fact requires additional investigation, as

pointed out by ©IKI∆ (1995, p. 14). For our purpose, it

seems acceptable that, in the area where the tectonic

dynamics later increased, the deepening within the Tri-

assic-Liassic carbonate platform started not earlier than

the end of the Lias. Consequently, the above mentio-

ned, tectonically delimited pelagic limestones with che-

rt of Upper Triassic age (HALAMI∆ & GORI»AN,

1995; ©IKI∆, 1995) should be “strange” in the areas

where they are outcropping.

The oceanic opening made possible the uplift of

ultramafic rocks. The isolated outcrops have been fou-

nd in Mt. Medvednica and in Mt. Kalnik, secondarily

emplaced into Cretaceous clastics. They are also pre-

sent in some deep bore-holes north-eastward of Mt.

Medvednica (©IMUNI∆ & PAMI∆, 1989; ©IKI∆,

1995; PAMI∆, 1997). Furthermore, a magmatic-sedi-

mentary complex originated, composed of clastics and

magmatic rocks: gabbro, diabases, spilites, etc. (CRN-

KOVI∆, 1963).

As to the origin of the adjacent Tisia, there are dif-

ferent opinions discussed in numerous papers (see:

CLOETINGH et al., 1993). Later, SZEDERKENY

Fig. 4  Simplified tectonic map of the east-

ern part of Mt. Æumberak (with the

area of Samobor), supplemented by J.

BUKOVAC: 1) Uppermost Nappe; 2)

S u p r a d i n a r i c u m (with possible small

Dinaric outcrops); 3) pelagic deposits

and formations with pelagic influences

(interpreted as E p i a d r i a t i c u m ); 4) Ne-

ogene and Quaternary cover.



90 Geologia Croatica 52/1

(1996) is of the opinion that during the Jurassic (Bath-

onian) the Tisia fragments were broken-off the southern

margin of the Variscan Europe and after a complicated

drifting, accompanied by rotation, came to their present

tectonic position. In this case, the general platform area

split into two branches. One is nowadays extended in

the Mid-Transdanubian Unit, Bükk Unit, etc., the other

remained southward of the Tisia. However, general

agreement does not yet exist. Anyhow, the oceanic for-

mations were subducted northward under the platform

elements, disintegrated them and, possibly, in a latter

phase even obducted upon the Slavonian part of the

Tisia (in contrast, MATEJ et al., 1997, assume the sub-

duction of Tisia). During the oceanic dynamics meta-

morphic rocks (greenschists, etc.) were formed (BEL-

AK et al., 1995a, b). Analogous rocks have been found

at places outside of our area, e.g. anchizonal metamor-

phism has been described in Hungary in the Mid-Trans-

danubian Unit. BERCZI-MAKK et al. (1993, p. 280)

accepts the opinion that it presumably belongs “to a

nappe unit of lower position” (i.e., to the S u p r a d i n a r -

icum, s. str., as it will be treated in this paper).

Tectonic consolidation processes, approximately at

the beginning of the Turonian interrupted the tectonic

dynamics, responsible for the origin of the magmatic-

sedimentary complex. The deposition was influenced

not only from the open sea, but also from the near-shore

and land surfaces due to oscillation of basin bottom

depth with changes of depositional environments, fol-

lowed by subduction processes within the crust. All this

changed the future sedimentation processes, which

included conglomerates, sandstones, siltites, shales,

rudist bioherms, platy limestones with globotruncanids,

turbidites (with slope and bottom influences), etc. They

are either in superposition or represent only lateral

facies. The true relationships are difficult to explain due

to subsequent tectonic disturbances.

2.6. PREDOMINANCE OF FLYSCH DEPOSITS

From the Senonian the “continental” and “oceanic”

troughs were not so well delimited being narrowed due

to subduction and bottom uplift. The transgression upon

the adjacent land surfaces is often mentioned because

flysch elements also overlie different platform surfaces.

Despite the interfingering with other facies, the pre-

dominance of the flysch in the time span from the Ma-

astrichtian to the Palaeocene is evident (CRNJA-

KOVI∆, 1981; DEVIDÉ-NEDĔLA et al., 1982; BUK-

OVAC, 1988; MARIN»I∆ et al., 1995; ©IKI∆, 1995,

etc.). 

2.7. FINAL TECTOGENETIC CONSEQUENCES

After the Palaeocene continental subduction proces-

ses caused piling up and squeezing of different tectonic

units, emplacement of granites, etc. Afterwards, uplift

occurred, followed by Oligocene and Neogene volcani-

sm, tilting, strike-slip faulting, rotation, and, possibly,

slow subduction and/or obduction. However, these eve-

nts are not the topic of this paper.

3. TECTONIC EVOLUTION

AND CLASSIFICATION

The recent general characteristic of the area under

discussion is intensive fragmentation of the previously

described lithostratigraphic complexes. They have been

disturbed by continental (A) subduction, oceanic (B)

subduction, then by more or less vertical movements

connected with gravitational displacements, and finally

by erosion. According to the presented lithostratigra-

phy, the main events should be the following.

Before the Late Triassic, the major events were

more or less uniform over the whole area, only display-

ing interior differentiations, sometimes of a high deg-

ree, but not specific enough to be used as diagnostic

features in recognizing single well defined megatecton-

ic units.

At the beginning of the Late Triassic, the new major

differentiation started. According to the afore men-

tioned lithostratigraphic sequences and their position

between two carbonate complexes visible at many pla-

ces, a labile (“miodynamic”) continental trough origi-

nated, being connected with the open sea. It enabled the

open sea to influence the platform areas. The first

deposits in this trough were Late Triassic pelagic sedi-

ments (limestones, cherts, etc.). The longitudinal distri-

bution of their outcrops suggests an adequate (longitu-

dinal) common “furrow”. It remains to be seen if it was

within the carbonate platforms (HERAK, 1986, 1991,

1995, 1997, etc.) or within the oceanic realm itself, at

the oceanic margin of the platform (AUBOUIN et al.,

1970). The latter opinion was common before the mobi-

listic concept was introduced. However, there are still

many adherents (e.g., PAMI∆ et al., 1998). My concept

is based on the fact that at several places the pelagic

deposits are emplaced between two carbonate platform

units (Budva Zone, Una spring area, Slovenian Trough,

etc.) which would be impossible if the “furrow” were

adjacent to the oceanic realm. Initially, the deposition

was confined to the “furrow” itself, then the surfaces

widened upon the platform margins, lagoons and basins

of clastic deposition.

After the Lias, within the northern (northeastern)

part of the platform a new deep oceanic trough was for-

med, being characterized by “eudynamic” processes

during the Jurassic and a larger part of the Cretaceous.

Later on, the events in all labile areas were characte-

rized predominantly by clastic deposits not only within

the basins but also upon the adjacent platforms.

According to the mentioned interrelationships, it is

obvious that the reconstruction of single major tectonic

zones is very difficult. However, this may be attempted,

taking into account their composition and recent posi-

tion. It is possible to distinguish several homogenous

nappe units. They will be differently named in order to



91Herak: Tectonic Interrelation of the Dinarides and the Southern Alps

distinguish them from the morphotectonic entities (Out-

er Dinarides, Inner Dinarides, Southern Alps, Mid-

Transdanubian Zone, etc.), which are usually heteroge-

neous, composed of elements of two or more subducted

(underthrusted) homogeneous units. As the names are a

question of convention, the possibility is open for new

proposals if they can be supported by better reasons.

3.1. THE UPPERMOST NAPPE (U)

The overlying components of the region under dis-

cussion (Figs. 1-4, U) form a nappe composed predomi-

nantly of Triassic dolomites with some limestones,

accompanied by Lower Triassic clastics including well-

bedded limestones, as well as by Upper Palaeozoic

molasse deposits (which do not derive from the Inner

Dinarides). They are characterized by west-east, or

southwest-northeast extension. The nappe is disintegra-

ted and it comprises elements which have been descri-

bed as the Pannonian Nappe (MILADINOVI∆, 1981,

and earlier), as well as the Sava Nappe (MIO», 1981,

and earlier), or the inverse basement of the Inner Dinar-

ides (HERAK, 1991) as a part of the S u p r a d i n a r i c u m .

Recent additional data (©IKI∆, 1995) justify the tecton-

ic distinction of this Uppermost Nappe deriving outside

the Dinaric realm (s. str.), i.e., from the Southern Alpi-

ne area, emplaced on the northern side of the Oceanic

Trough (S u p r a d i n a r i c u m , s. str.). This Nappe overlies

not only the oceanic S u p r a d i n a r i c u m , but also parts of

Jurassic and Cretaceous carbonate rocks of the Dinaric

carbonate platform (D i n a r i c u m), mostly in the form of

klippen. The final emplacement may be at least partly

caused by gravitation.

At this point, it is necessary to note that some Trias-

sic and Palaeozoic deposits may not belong to the

Uppermost Nappe but to Dinaridic major units as their

direct basement. Therefore, the utmost care is required

in interpretation of the tectonic position of different Tri-

assic and Palaeozoic outcrops.

3.2. THE SUPRADINARIC NAPPE

(Supradinaricum , s. str., S)

This Nappe (Figs. 1-4, S) comprises the oceanic part

of the S u p r a d i n a r i c u m (s. l.), overlain by the Upper-

most Nappe. The Nappe is characterized by formations

originated as a consequence of “eudynamics” from the

Lias to the Turonian. In the Senonian, differentiation

increased under pelagic and terrestrial influences.

Simultaneous uplifts widened the influences of this

basin upon adjacent platform margins, in the form of

extensions of flysch deposits (marginal flysch) which

hide the boundaries between the basin and the plat-

forms. Therefore, only flysch deposits, which are tec-

tonically connected with oceanic formations, belong to

this Nappe. The rest of it (the marginal epiplatform fly-

sch) is to be treated together with the next tectonic

megaunit (D i n a r i c u m). The Vardar elements are also

included in the S u p r a d i n a r i c u m . However, their frame

exceeds the frame of the Vardar Zone as defined by

KOSSMAT (1924). The western extension of the S u p -

radinaricum is covered by the Uppermost Nappe.

3.3. THE DINARIC NAPPE (Dinaricum, D)

At the southern (southwestern) side, the rocks of the

Dinaric carbonate platform (Figs. 1 and 2, D) bordered

the oceanic belt (S u p r a d i n a r i c u m , s. str.). As a major

tectonic unit, it is called Dinaricum and it underlies the

Supradinaric Nappe. Within the D i n a r i c u m s e v e r a l

“strange” outcrops of pelagic deposits have been found.

Their origin and tectonic position were repeatedly dis-

cussed (citations in HERAK, 1993). In the contact area

of the S u p r a d i n a r i c u m and D i n a r i c u m , including the

marginal flysch (with some karstifications in the base-

ment), the nappe relations are obvious (PREMRU et al.,

1977; HERAK, 1986; BUKOVAC, 1988). Consequent-

ly, “La sous-zone prékarstique” (BLANCHET et al.,

1970) is also included into this megaunit.

Previously, the contact zone of the Dinaric platform

and oceanic formations was treated as a “flexion” or

“bending” zone, making a slope of the platform towards

the basinal complexes including magmatites. It was

supposed that this zone existed probably since the Tri-

assic, representing “the Adriatic microplate toward the

Tethys ocean” (DIMITRIJEVI∆, 1982, p. 11). Howev-

er, it is obvious that this contact zone was created as a

consequence of two events. The first, was the opening

of the ocean after the Lias (more or less vertical con-

tacts). The second was continental subduction during

the Palaeogene, when the Dinaric carbonate platform,

together with the overlying marginal flysch, was sub-

ducted under the basinal “magmatic-sedimentary” com-

plex (S u p r a d i n a r i c u m ) and even under the Uppermost

Nappe. The corresponding contacts are inclined.

The opposite margin of this megaunit, together with

the underlying “strange” pelagic outcrops, are discussed

below.

3.4. THE INTERPLATFORM MEGAUNIT

(Epiadriaticum , E)

The range of the isolated outcrops of pelagic and

basinal deposits without ultramafic and mafic intrusions

range from the Upper Triassic to the Upper Cretaceous,

and are to be found as well in the Outer as in the Inner

Dinarides (Figs. 1-4, U). Their distribution is extremely

difficult to explain in a generally acceptable way. The

continuous outcrops extend only in the Budva-Krasta-

Pindus Zone on the southeastern side and in the Sloven-

ian Trough on the northwestern side. Between these

areas, numerous tectonically delimited outcrops may

indicate that their interconnection could be traced

beneath the nappes mentioned earlier. In such a case

even the Bosnian Zone (AUBOUIN et al., 1970) may

be connected with the Budva-Krasta-Pindus Zone

below the D i n a r i c u m due to continental subduction.

The indications of such a connection were noticed earli-



92 Geologia Croatica 52/1

er. MEDWENITSCH (1964, in SIKO©EK & MEDWE-

NITSCH, 1965) distinguished the Subdinaricum which

should consist of Budva, Mirdita and Raduπa elements

together with the central ophiolites. Their extension is

supposed to be beneath the carbonate Dinarides. In this

way, typical Inner Dinaric elements (Mirdita, Raduπa,

central ophiolites), which normally overlie the Outer

Dinarides, were connected with the Budva Zone which

underlies them and now can be interpreted as a subduct-

ed unit. On the contrary, PAMI∆ (1993, etc.), tried to

connect the Bosnian Zone with the Budva Zone (united

with the Mirdita Zone) upon the surface lithologic

analogies.

However, the main problem, concerning all the

pelagic outcrops, is that they are delimited to small

areas, which are dispersed and tectonically encircled

with deposits of different provenance, belonging to var-

ious morphostructural units. For instance, the deposits

in question in western Slovenia are in contact with the

Dinaric platform, the Julian Alps and the “Sava Folds”

(= Sava Nappe sensu MIO», 1981). In Mt. Æumberak,

Mt. Medvednica, Mt. IvanπËica and Mt. Kalnik pelagic

outcrops occur within “magmatic-sedimentary” forma-

tions and, exceptionally, within platform elements.

Likewise, the pelagic elements of the Bosnian Zone

(AUBOUIN et al., 1970) are mostly in tectonic contact

with different Inner Dinaric rocks, including the ophio-

lites. Also there are localities in Western Serbia (OBR-

ADOVI∆ & VASI∆, 1996), as well as in Albania,

where localized “strange” bodies (Rubik complex, Kal-

ur cherts, and Lumi i Zi sections) are distributed as iso-

lated bodies within the Mirdita Zone (CAROSI et al.,

1996; MARCUCCI & PRELA, 1996).

Besides, numerous Jurassic and less numerous Cre-

taceous isolated pelagic outcrops, often in visible tec-

tonic contacts with shallow-water carbonate rocks, are

widespread within the Dinaric carbonate platform in

Slovenia, Croatia, Hercegovina and Montenegro, while

the Budva Zone is overthrust upon the Adriatic carbon-

ate platform (HERAK, 1986, with older citations). The-

se facts and opinions require comparison with other

possible alternative explanations, to determine which is

the most convincing.

The first possibility would concern the model with

facies differentiation. In that case, tectonic contacts

with adjacent facies would be uncommon. Besides, it is

impossible to assume that similar pelagic environments

would prevail at the same time within a basin, which is

influenced by magmatic activity and on a stabilized car-

bonate platform without influences from a common

source of the pelagic components. Comparing recent

and fossil global radiolarian localities, DE WEVER &

BAUDIN (1996) came to the following conclusions: (a)

“Distal basinal or oceanic environments are often opti-

mal sites for the preservation of siliceous and lipid-rich

organic material derived from plankton” (p. 310); (b)

“The long held assumption of a relationship between

abundance of radiolarians and volcanic processes is

largely erroneous” (p. 311). Even in the case when the

basins are separated from the ocean by a platform, they

have to be partially open to the ocean (p. 313). Howev-

er, due to oscillations the deposition itself, character-

ized by pelagic fossils, occurred in various depressions,

i.e. even upon the platforms (in lagoons). The only con-

dition is in the interference with the open sea (in our

case the eastern Tethys).

Consequently, the pelagic components had neither

oceanic nor platform characteristics. Within the deriva-

tion trough itself the pelagic column seems to be more

or less complete. Upon both the adjacent marginal parts

of the carbonate platforms the range and extension var-

ied. The peripheral common boundary (at different

horizons) has been characterized by the transition of

pelagic deposits to carbonate shallow-water sediments.

Such exposures are, in a tectonical sense, part of the

platforms, while, below the Dinaricum a consistent tec-

tonic complex is to be supposed.

The fragmental exposures require an explanation

introducing either erosion of a common overlying and

tectonically disintegrated megaunit or by numerous

localized uplifts of a consistent major unit outcropping

in tectonic windows which were afterwards slightly dis-

turbed, i.e. fractured, tilted, and eroded.

The erosion as a main factor, which would disinte-

grate a homogeneous pelagic major unit, cannot be

accepted, because, in that case, this unit should primari-

ly cover the deposits of different ages and environ-

ments. Such a case is improbable even when there were

no tectonic contacts of single outcrops with adjacent

deposits. However, in many cases the contacts are dis-

tinct. At some localities younger deposits outcrop

through the older ones, thus favouring allochthony. The

relationships within carbonate terrains are characterized

by a very important phenomenon: the rocks of the Adri-

atic carbonate platform primarily and tectonically

underlie the pelagic deposits. At the same time, the

D i n a r i c u m overlies the pelagic distal deposits (together

with the underlying rocks of the Adriatic platform) sug-

gesting nappe relationships. The participation of pelagic

deposits in the Dinaricum is not obvious due to subduc-

tional contact. In the subduction process within the con-

tinental crust, the ductile deposits were a detachment

level, making possible long-rate continental subduction

even under the “magmatic-sedimentary” formations,

indicating that the dispersed pelagic outcrops within

them are tectonic windows. Such a concept respects the

dispersion of pelagic and other deposits with open sea

influences within the belts of different provenance and

their contacts with platform and basinal formations.

The relationships of platform and pelagic deposits are

still hidden due to nappe relationships. The interior

reconstruction of their allochthonous disturbances are

omitted.

3.5. THE ADRIATIC NAPPE (Adriaticum, A)

The next lower tectonic major unit consists predom-

inantly of carbonate rocks with some pelagic sediments



93Herak: Tectonic Interrelation of the Dinarides and the Southern Alps

and flysch. It is extended on the southwestern side of

the overlying E p i a d r i a t i c u m (Fig. 2, A). There are also

some detached bodies of the D i n a r i c u m overlying the

A d r i a t i c u m (possibly, due to younger gravitational dis-

placements). The differences between them are difficult

to establish, and require detailed analyses and regional

correlations. Recently, DROBNE & TRUTIN (1997)

palaeontologically confirmed the existence of a tectonic

window of the marginal part of the A d r i a t i c u m t h r o u g h

the D i n a r i c u m at BuniÊ in the Lika. BLA©KOVI∆

(1999) proposed a major tectonic classification based

on the A d r i a t i c u m, E p i a d r i a t i c u m and D i n a r i c u m f o r

purpose of oil prospection. ROMANDI∆ & ALJINO-

VI∆ (1999) easily recognized the A d r i a t i c u m b e n e a t h

the D i n a r i c u m in strongly disturbed sedimentary sequ-

ences, with cumulative thickness of up to 17 km, using

geoelectric and palaeomagnetic methods.

The A d r i a t i c u m is delimited by the E p i a d r i a t i c u m

on one side and by (?)Ionian deposits on the other. Lon-

gitudinally it continues toward the southeast into the

Gavrovo-Tripolitza domain. Sporadically, it occurs wit-

hin the D i n a r i c u m as tectonic windows. Remarkable is

also the Hercegovinian half-window.

3.6. ?THE IONIAN UNDERTHRUST (?Ionicum, I)

The insular region of the Adriaticum is underlain by

Cretaceous-Palaeogene deposits (LAWRENCE et al.,

1995), possibly belonging to the Ionian Basin, and sub-

ducted under the Adriaticum (Fig. 2, I). This fact may

justify the distinguishing of the Adriatic and Apulian

platforms.

4. CONCLUSIONS

To avoid some discrepancies in the interpretation of

the Alpino-Dinaridic realm in a “geosynclinal” way,

one of the posibilities is to follow the partially emended

concept of continental subductions as accompanying

process of oceanic subduction, based upon new litho-

stratigraphic and structural notions previously cited.

The approach to the subduction mechanism encoun-

ters great difficulty due to the fact that the traces of the

oceanic subduction are quite hidden. Only the presence

of restricted outcrops of ultramafic rocks (©IMUNI∆ &

PAMI∆, 1989; PAMI∆, 1997), secondarily emplaced

into Cretaceous deposits, testifies such a process. The-

refore, they do not reflect primary relationships which

would define their origin and later tectonic displace-

ments. Even the essential problem related to our part of

Tethys is not obvious; it concerns the question of

whether we are dealing only with a branch of Tethys or

if there was a connection with the Penninic Belt below

the Southern Alps and the Austroalpine Nappes. Also,

the time of the tectonic emplacement of the Slavonian

Mountains (as a part of Tisia) is still under discussion.

The only certain geotectonic phenomena are the

consequences of continental subductions. Their traces

are preserved within all the major facies, indicating a

general northward (northeastward) movement (caused

by the movements in the asthenophere). All the com-

plexes of the Outer and Inner Dinarides behaved acco-

rding to their constitution, being either brittle or ductile.

Anyway, the rate of the disturbances suggests the exis-

tence of weak zones at several levels, which made a

strong allochtonous imbrication possible. The continen-

tal subductions were preceded by very complex dynam-

ics, and have been followed by uplift of the area (verti-

cal faulting), tilting, possible additional subduction and

obduction, rotation, and often neglected gravitational

displacements. The time relations of the tectogenetic

process are relatively easily distinguished.

1. During the Variscan orogeny, vast continental sur-

faces originated, upon which, later, intensive depo-

sition of terrigenous fragments occurred. However,

in that time the continental crust was not completely

stabilized. Rifting and magmatic processes in the

Middle Triassic (and at the beginning of the Late

Triassic) were renewed, and accompanied by ande-

sitic extrusions (tardy-Variscan dynamics). This dis-

quiet was relatively short and final, and it prepared

the basis for vast and temporally extensive sedimen-

tation of carbonate platform deposits. In the Upper

Triassic an oscillating interplatform trough was

formed. It remained directly connected with the

open sea, from which pelagic components were sup-

plied during the whole Mesozoic era. The oscilla-

tions within the trough caused periodic ingressions

of pelagic deposits upon the adjacent platforms,

especially in the Late Jurassic and the Late Creta-

ceous.

2. North of the interplatform trough, after the Lias, the

opening of the ocean (including our western branch)

occurred with simultaneous extrusions of already

consolidated mantle rocks (ultramafites). So, the

“miodynamics” and “eudynamics” were contempo-

raneous with mutual influences in their final phase.

After the extrusions of the mantle rocks (peridotites,

serpentinites), the equilibrium was disturbed and

northward movements of lithospheric complexes

were initiated (as a consequence of adequate dyna-

mics in the asthenosphere). All this resulted in oce-

anic subduction and the consuming of subducted

material, while the more resistent ultramafites rema-

ined on the surface, submitted to further distur-

bances.

3. The asthenospheric northward movements were not

only localised under the oceanic lithosphere, but

were also active under the continental part, includ-

ing the trough between the Adriatic and Dinaric

platforms. The influence was different upon the pla-

tform surfaces in comparison with the oscillating

trough, in which continental subduction started.

Therefore, the trough narrowed and the sea level

rose, with the ingression of pelagic material upon



94 Geologia Croatica 52/1

the marginal platform areas, overlying platform for-

mations and interfingering with them.

4. The Oceanic Trough was, in the Late Jurassic and

the Early Cretaceous, still a place of intensive

“eudynamics” accompanied by strong magmatism

and low to medium-grade metamorphism. The clo-

sure of the Trough, approximately in the Middle

Cretaceous, was followed by deposition of clastics

accompanied by small reefs, platy limestones, and

by flysch deposits. At that time, there were no sharp

boundaries of the sedimentary basins within the

frame of the Dinaridic part of the Tethys.

5. Due to the closure of epicontinental and oceanic

belts, the crust generally coalesced and afterwards

behaved more or less as a single major unit com-

posed of rigid and weak domains. This fact deter-

mined the future behaviour in respect to the north-

ward movement in the asthenosphere, which contin-

ued. The multiple continental subductions were inf-

luenced by ductile horizons. In this way a complex

allochthonous structural pattern has originated. Alo-

ng the Interplatform Trough, the subduction was

most intensive, resulting in the carbonate rocks with

the flysch of the Adriatic platform (A d r i a t i c u m)

underlying not only the pelagic elements (of Epi-

adriatic provenance), but elsewhere are also directly

overlain by the carbonate rocks of the Dinaric plat-

form (D i n a r i c u m). The D i n a r i c u m has been sub-

ducted under the oceanic formations (S u p r a d i n a r -

icum, s. str.) which underlie Palaeozoic and Triassic

platform elements of the Uppermost Nappe. More-

over, in the frames of the major nappes imbrication

is also present. Delimitation and gradation of tecton-

ic units is difficult due to the fact that parts of pelag-

ic and flysch deposits primarily overlie platform

margins, and are, in the tectonic sense, only parts of

the platform nappe units. Along the major contact

zones, the underthrusting character of contacts is

obvious, though not necessarily equal to one anoth-

er. Then, subduction process increased towards the

west (northwest) and, therefore, the zones wedge

out. In this way the Dinaric strike (SE-NW) was

finally established. Only the elements of the Upper-

most Nappe have not been essentially influenced,

and so the difference in strike between this Nappe

and the Dinaridic structural units (nappes) could be

explained. Such a dynamics lasted approximately

until the end of the Oligocene and, thus, the basis

for the Neogene indentation process was prepared.

The consequences of the process itself have been

interpreted in several papers (e.g., RATSCHBACH-

ER et al., 1991), though the moving forces were not

well defined. According to this proposal, they shou-

ld be represented by continental subductions.

6. Simultaneously, in the main Alpine and Carpathian

domains, the subductions were directed generally

toward the south. Therefore, our region was squeez-

ed and the thickness of sedimentary complexes

increased, not only due to piling up of subducted

units but also due to the rise of the Cretaceous-

Palaeogene S-granites, final volcanism, etc.

7. The concentrated thermal “diapirism” was distrib-

uted within all the tectonic units, and in this way

numerous tectonic windows originated, predomi-

nantly of the ductile flysch and pelagic deposits. At

such places the chaotic carbonate breccias on the

northern slope of Mt. Medvednica (“Horvatove

stube”, Pronjak), as well as in Mt. Kalnik and Mt.

Ravna Gora, have been interesting to many authors

(e.g. BABI∆ et al., 1973; ©IMUNI∆ et al., 1993;

PRTOLJAN et al., 1995), but a final explanation

has not yet been found. Their emplacement is char-

acterized by tectonic contacts with the adjacent

rocks. The age of the fragments belong to different

horizons of the Mesozoic, with a matrix of Campan-

ian age. ©IMUNI∆ et al. (1993, p. 614) assume that

the upper boundary of these “exotic breccias” is

post-Palaeocene, and suggest “that they might have

been originated along subduction zones”. It could be

added that also localized rise of parts belonging to

different subducted nappes contributed to the gene-

sis of the breccias, making in fact the (additionally

disturbed) tectonic windows. I am conscious that

such an unconfirmed opinion might be considered

as too courageous, but it should be taken into acco-

unt in future discussions.

8. The mentioned vertical diversification was intensifi -

ed during the Neogene, and caused disintegration,

tilting, rotation and gravitational displacements of

parts of the nappes. Therefore, fragments with dif-

ferent vergencies are to be found even upon Neo-

gene sediments. The process itself is considered as

very complicated (possibly combined with slight

subductions), and an explanation exceeds the topic

of this paper.

9. The proposed model can be understood on the basis

of the mobilistic interpretation of geotectonic prob-

lems. The assumption of continental subductions

helps to explain not only major structures but also

“strange”, “uncommon”, “isolated”, and “exotic”

phenomena, as single constituents of major tectonic

units, within logical, though not anticipated structur-

al frameworks.

10. Due to a nappe system, it is necessary to distinguish

not only the previously discussed homogeneous tec-

togenetic units (Uppermost Nappe, Supradinaricum ,

s. str., D i n a r i c u m, E p i a d r i a t i c u m , A d r i a t i c u m a n d

(?)Ionian underthrust) but also some more or less

individualized morphotectonic complexes, e.g., the

Adriatic area, High Karst Belt, Outer Dinarides,

Inner Dinarides, the Pannonian Basin, etc. To this

category of terms also belong the Mid-Transdanu-

bian Zone, Zagreb Zone, and “Sava Folds”. They all

are characterized by a heterogeneous, composite



95Herak: Tectonic Interrelation of the Dinarides and the Southern Alps

constitution terminated during neotectonic dynam-

ics, and are used in the regional geology and geo-

morphology.

11. I hope that the intention of this paper to explain the

tectonic setting of the Alpino-Dinaridic realm in a

mobilistic sense may be generally acceptable base

for further discussions. Therefore, the concept may

not be considered as final. Many pecularities remain

open to further confrontations, based upon addition-

al, more accurate (confirming or emending) data. 

Acknowledgements

The preparation of the manuscript required addition-

al discussions of some elementary data with experts of

different research fields, e.g., with Ljubomir BABI∆,

Stjepan BAHUN, Mirko BELAK, Josip BUKOVAC,

Ivan GU©I∆, Domagoj JAMI»I∆, Vladimir JELASKA,

Vladimir MAJER, Pero MIO», Jakob PAMI∆, Branko

SOKA», Antun ©IMUNI∆, Marko ©PARICA, Ivo VE-

LI∆, etc. The drawings have been executed by Miroslav

KLADNI»KI. To all of them I express my sincere gra-

titude.

5. REFERENCES

AUBOUIN, J., BLANCHET, R., CADET, J.-P., CEL-

ET, P., CHARVET, J., CHOROWICZ, J., COUSIN,

M. & RAMPNOUX, J.-P. (1970): Essai sur la géo-

logie des Dinarides.- Bull. Soc. géol. de France, 12,

1060-1095.

BABI∆, Lj. (1973): Bazenski sedimenti gornjeg titona i

valendisa zapadno od Bregane (Upper Tithonian to

Valanginian basinal sediments west of Bregana).-

Geol. vjesnik, 26, 11-27.

BABI∆, Lj. (1974): Razdoblje otriv-cenoman u Æum-

berku: stratigrafija, postanak sedimenata i razvoj

prostora (Hauterivian to Cenomanian time in the

region of Æumberak, Northwestern Croatia: stratig-

raphy, sediments, paleogeographic, paleotectonic

evolution).- Geol. vjesnik, 27, 11-33.

BABI∆, Lj. (1975): Kondenzirani lijas Medvednice i

IvanπËice i njegovo znaËenje za interpretaciju paleo-

geografskog razvoja unutarnje dinarske regije (Con-

densed Liassic sedimentation on Mt. Medvednica

and Mt. IvanπËica - northern Croatia - and its signi-

ficance for the interpretation of the paleogeographic

evolution of the Inner Dinaric belt).- Geol. vjesnik,

Zagreb, 28, 11-18.

BABI∆, Lj. (1980/81): The origin of “Krn Breccia” and

the role of the Krn area in the Upper Triassic and

Jurassic history of the Julian Alps (Postanak “BreËe

Krna” i uloga predjela Krna u povijesti Julijskih

Alpa u gornjem trijasu i juri).- Vesnik Zav. geol.

geofiz. istraæ., (A), Beograd, 38-39, 59-75.

BABI∆, Lj. & ZUPANI», J. (1973): Najmlaa jura i

najstarija donja kreda u IvanπËici (uppermost Juras-

sic and Early Cretaceous deposits on Mt. IvanπËica -

northern Croatia).- Geol. vjesnik, 26 (1972), 267-

272.

BABI∆, Lj. & ZUPANI», J. (1978): Kossmatovi “Æele-

znikarski vapnenci i dolomiti” i “Zaliloπki krovni

πkriljavci” u predgorju Julijskih Alpa; podaci o

stratigrafiji, facijesu i paleogeografskom znaËenju

(Kossmat’s “Kalke und Dolomite von Eisnern” and

“Dachschiefer von Salilog” in the Julian Prealps:

data about stratigraphy, facies and paleogeogra-

phy).- Geol. vjesnik, 30/1, 21-42.

BABI∆, Lj., GU©I∆, I., & DEVIDÉ-NEDĔLA, D.

(1973): Senonski krπnici na Medvednici i njihova

krovina (Senonian breccias and overlying deposits

on Mt. Medvednica - northern Croatia).- Geol. vjes-

nik, 25 (1971), 11-27.

BELAK, M., PAMI∆, J., KOLAR-JURKOV©EK, T.,

PECSKAY, Z. & KARAN, D. (1995a): Alpinski

regionalnometamorfni kompleks Medvednice - sje-

verozapadna Hrvatska.- 1. hrv. geol. kongres (Opa-

tija, 1995), Zbornik radova, 1, 67-70, Zagreb.

BELAK, M., SREMAC, J., CRNKO, J. & KOLAR-

JURKOV©EK, T. (1995b): Paleozojske stijene nis-

kog stupnja metamorfizma na jugoistoËnoj strani

Medvednice (sjeverozapadna Hrvatska).- 1. hrv. ge-

ol. kongres (Opatija, 1995), Zbornik radova, 1, 71-

74, Zagreb.

BERCZI-MAKK, A., HAAS, J., RALISCH-FELGEN-

HAUER, E., & ORAVECZ-SCHEFFER, A. (1993):

Upper Paleozoic-Mesozoic formations of the Mid-

Transdanubian Unit and their relationships.- Acta

geol. Hungar., 36/3, 263-296.

BLANCHET, R., CADET, J.P. & CHARVET, J.

(1970): Sur l’existence d’unités intermediaires entre

la Zone Haut-Karst l’unité du flysch bosniaque, en

Yougoslavie: la sous-zone prékarstique.- Bull. Soc.

géol. de France, 12, 227-236.

BLA©KOVI∆, I. (1999): Subsurface tectonic relations -

a basis for determination of the zones of petroleum-

geological prospectivity.- Working materials, 2nd

intern. Symposium of Petroleum Geology, Croat.

Acad of Sci. and Arts, Faculty of Mining, Geology

and Petroleum Engineering and INA, 133-145,

Zagreb. 

BUKOVAC, J. (1988): Tectonics of the contact zone of

the Dinaricum and Supradinaricum in the area of

Krnjak-BariloviÊ-Karlovac, Croatia, Yugoslavia

(Tektonski odnosi u kontaktnoj zoni Dinarika i

Supradinarika u podruËju Krnjak-BariloviÊ-Karlo-

vac, Hrvatska, Jugoslavija).- Acta geol., 18/1, 1-12,

Zagreb. 

BUSER, S. (1977): Osnovna geoloπka karta SFRJ

1:100.000. List Celje L33-67.- Geol. zavod Ljub-



96 Geologia Croatica 52/1

ljana (1972-1976), Savezni geoloπki zavod, Beo-

grad.

BUSER, S. (1989): Development of the Dinaric and the

Julian carbonate platforms and of the intermediate

Slovenian basin (NW Jugoslavia).- Mem. Soc. geol.

It., 40 (1987), 313-330. 

CAROSI, R., CODRA, A., MARRONI, M. & MUS-

TAFA, F. (1996): Deformation history of Jurassic

Kalur cherts from the Mirdita nappe, Albanian ophi-

olites.- Ofiolit, 21/1, 41-45, Pisa.

CLOETINGH, S., SASSI, W. & HORVÁTH, F. (eds.)

(1993): The origin of sedimentary basins: Interfer-

ences of the quantitative modelling and basin analy-

ses.- Tectonophysics, 226, Elsevier, 518 p. 

COUSIN, M. (1973): Le sillon Slovène: les formations

triassiques, jurassiques et neocomiennes au Nord-

Est de Tolmin (Slovenie occidentale, Alpes mérid-

ionales) et leur affinites dinariques.- Bull. Soc. géol.

France, 15/3-4, 326-338.

CRNKOVI∆, B. (1963): Petrografija i petrogeneza

magmatita sjeverne strane Medvednice (Petrogra-

phy and petrogenesis of the magmatites of the

northern part of Medvednica Mountain).- Geol.

vjesnik, 16 (1962), 63-160.

CRNJAKOVI∆, M. (1981): Mastrihtski fliπ jugoza-

padnog dijela Medvednice (Maastrichtian flysch

sediments in the southwest part of Mt. Medvedni-

ca).- Geol. vjesnik, 34, 47-61.

CVIJI∆, J. (1924): Geomorfologija.- Dræ. πtamparija,

Beograd, XXI+588 p.

D E V I D É - N E DĔLA, D. & KOCHANSKY-DEVIDÉ,

V. (1990): Neoschwagerinenfund in Medvednica-

Gebirge (ZagrebaËka gora).- Rad Jugosl. akad.

znan. i umjetn., 449, 29-34, Zagreb.

D E V I D É - N E DĔLA, D., BABI∆, Lj. & ZUPANI», J.

(1982): Mastrihtska starost fliπa Vivodine u Æum-

berku i kod Ozlja (zapadna Hrvatska) na temelju

planktonskih foraminifera (Age maestrichtien du

Flysch de Vivodina dans le Æumberak et des envi-

rons d’Ozalj en Croatie occidentale - Yougoslavie).-

Geol. vjesnik, 35, 21-36.

DE WEVER, P. & BAUDIN, F. (1996): Palaeogeogra-

phy of radiolarite and organic-rich deposits in

Mesozoic Tethys.- Geol. Rundschau, 85, 310-326,

Berlin.

DIENER, C. (1903): Bau und Bild der Ostalpen und

des Karstgebietes.- Bau und Bild Österreichs, Wien,

2, 1-328.

DIMITRIJEVI∆, M.D. (1982): “Pregib”, gledan mobi-

listiËki (“Flexion zone” - a mobilistic viewpoint).-

Radovi Znan. savjeta za naftu Jugosl. akad znan. i

umjetn., A, 10, 7-11, Zagreb.

DROBNE, K. & TRUTIN, M. (1997): Alveolinas from

the BuniÊ section.- Geol. Croatica, 50/2, 215-223.

–UR–ANOVI∆, Æ. (1973): O paleozoiku i trijasu

Medvednice (ZagrebaËke gore) i podruËja Dvora na

Uni na temelju konodonta (About the Paleozoic and

Triassic of Medvednica Mountain and the area near

Dvor na Uni on the basis of Conodonts).- Geol.

vjesnik, 25 (1971), 29-49.

GORJANOVI∆-KRAMBERGER, D. (1907): Geologi-

ja gore Samoborske i ÆumberaËke.- Rad Jugosl.

akad. znan. i umjetn., 120 (Matem.-prir, razred, 18),

1-82, Zagreb.

GRAD, K. (1961): Obavestilo o raziskavah krednih

sedimentov v Posavskih gubah (Note on the investi-

gation of Cretaceous sediments in the Sava folds).-

Geologija, 6 (1960), 313-315, Ljubljana.

GU©I∆, I. & BABI∆, Lj. (1972): Die Mikrofazies und

Mikrofauna der Obertrias und des Lias des Medved-

nica Gebirges (Nordkroatien).- Mitt. Ge. Geol.

Bergbaustud., 21, 327-340, Innsbruck.

HAAS, J., KOVÁCS, S., KRYSTYN, L. & LEIN, R.

(1995): Significance of Late Permian-Triassic facies

zones in terrane reconstruction of Alpine - North

Pannonian domain.- Tectonophysics, 242, 19-40.

HALAMI∆, J. & GORI»AN, ©. (1995): Triassic radio-

larites from Mts. Kalnik and Medvednica.- Geol.

Croat., 48/2, 129-146.

HERAK, M. (1986): A new concept of geotectonics of

the Dinarides (Nova koncepcija geotektonike Dinar-

ida).- Acta geol., 16/1, 1-42, Zagreb.

HERAK, M. (1991): Dinaridi - mobilistiËki osvrt na

genezu i strukturu (Dinarides - Mobilistic view of

the genesis and structure).- Acta geol., 21/2, 35-117,

Zagreb.

HERAK, M. (1993): Additional considerations on the

Epiadriaticum, Outer Dinarides.- Geol. Croat., 46/1,

165-168.

HERAK, M. (1995): Koncepcijski doseg geologije

Hrvatske (Conceptional scope of the geology of

Croatia).- 1. hrv. geol. kongres (Opatija, 1995),

Zbornik radova, 1, 25-33, Zagreb.

HERAK, M. (1997): Croatia.- In: MOORES, E.M. &

FAIRBRIDGE, R.W. (eds): Encyclopedia of Euro-

pean and Asian Regional Geology. Chapman &

Hall, London, 155-160.

HERAK, M., JAMI»I∆, D., ©IMUNI∆, A. & BUKO-

VAC, J. (1990): The northern boundary of the Dina-

rides (Sjeverna granica Dinarida).- Acta geol., 20/1,

(Prir. istraæ., 60), 5-27, Zagreb.

HERAK, M. & ©KALEC, D. (1967): VapnenaËke alge

u permu Samoborskog gorja (Kalkalgen im Perm

des Samoborer Gebirges).- Geol. vjesnik, 20, 37-40.

JAMI»I∆, D. (1983): Strukturni sklop metamorfnih sti-

jena Krndije i juænih padina Papuka (Structural fab-

ric of the metamorphosed rocks of Mt. Krndija and



97Herak: Tectonic Interrelation of the Dinarides and the Southern Alps

the eastern part of Mt. Papuk).- Geol. vjesnik, 36,

51-72.

JENKO, K. (1944): Geoloπki rad na listu Samobor

1:75000.- Vjesnik Hrv. dræ. geol. zav., 2/3, 19-23,

Zagreb.

JURKOV©EK, B., ©RIBAR, Lj. & KOLAR-JURKOV-

©EK, T. (1990): PelagiËke jurske in kredne plasti v

zahodnem delu Julijskih Alp (Pelagic Jurassic and

Cretaceous beds in the western part of the Julian

Alps).- Geologija, 31-32 (1988-89), 285-328, Ljub-

ljana.

KI©PATI∆, M. (1899): Nastavak bosanske serpentinske

zone u Hrvatskoj.- Rad. Jugosl. akad. znan. i umj-

etn., 139 (Matem.-prir. razred, 27), 44-73, Zagreb.

KOCH, F. (1924): Geotektonische Beobachtungen in

Alpino-Dinarischem Grenzgebiete.- Zbornik radova

posv. Jovanu CvijiÊu,341-358, Beograd.

KOSSMAT, F. (1924): Geologie ser zentralen Balkan-

halbinsel; mit einer Übersicht des dinarischen Geb-

irgsbaues. Die Kriegsschauplätze 1914-1916.- Born-

träger, Berlin, V+198 p.

LAPAJNE, V. & ©RIBAR, Lj. (1973): Zgornjokredni

sedimenti na obmoËju Posavskih gub (Upper Creta-

ceous deposits in the Sava folds).- Geologija, 16,

237-244, Ljubljana.

LAWRENCE, S.R., TARI-KOVA»I∆, V. & GJUKI∆,

B. (1995): Geological evolution model of the Dinar-

ides.- Nafta, 46/2, 103-113, Zagreb.

MARCUCCI, M. & PRELA, M. (1996): The Lumi i Zi

(Puke) section of the Kallur cherts: Radiolarian

assemblages and comparison with other sections in

northern Albania.- Ofioliti, 21, 71-84, Pisa.

MARIN»I∆, S., ©PARICA, M., BENI∆, J. & KORO-

LIJA, B. (1995): Sedimenti senona u dolini MikuliÊ

potoka.- In: ©IKI∆, K. (ed.): Geoloπki vodiË Med-

vednice. Inst. za geol. istraæ. & INA-Naftaplin, 73-

76, Zagreb.

MATEJ, S., NOVOSELEC, E. & TARI-KOVA»I∆, V.

(1997): Neogene extension and compression proces-

ses in the central part of the Sava Depression, South

Pannonian Basin, Croatia.- Dynamics of the Pan-

nonian-Carpathian-Dinaride System, Polish Acad.

of Sci., 1091, Krakow - Zakopane.

MILADINOVI∆, M. (1981): Pregled tektonske grae

zapadnog dela Jugoslavije (Vue sur la téctonique

des Dinarides occidentales Yougoslaves).- Geol.

glasnik, 9, 89-106, Titograd.

MILANOVI∆, M. (1982): Carboniferous microfossils

from Gorski kotar, Hrvatsko zagorje and Banija

(Karbonske mikrofosilne asocijacije Gorskog kota-

ra, Hrvatskog zagorja i Banije).- Palaeont. Jugosl.,

28, 1-34, Zagreb.

MIO», P. (1975): Prilog poznavanju tektonskih odnosa

graniËne zone istoËnih Posavskih bora i dinarskog

πelfa (Contribution to the knowledge of the tectonic

relations of the boundary zone of the eastern Sava

Folds and Dinaric shelf).- 2. god. znan. skup Sekcije

za primjenu geol., geofiz. i geokem. Znan. savjeta

za naftu Jugosl. akad. znan. i umjetn., 223-228, Zag-

reb.

MIO», P. (1981): Tektonski odnosi Savske navlake u

Sloveniji te njena veza sa πirim jugoslavenskim

podruËjem (Tectonic relationship of Sava thrust

compared to the adjacent units in Slovenia and its

relation with the broader Yugoslav area).- Nafta,

32/11, 543-548, Zagreb.

MIO», P. & ©RIBAR, Lj. (1975): Jurski skladi v Sev-

ernih Karavankah (The Jurassic beds in the North

Karavanke Mountains).- Geologija, 18, 87-97, Ljub-

ljana.

MLAKAR, I, (1987): Prispevek k poznavanju geoloπke

zgradbe Posavskih gub in njihovega juænega obrob-

ja (A contribution to the knowledge of the geologi-

cal structure of the Sava Folds and their southern

border).- Geologija, 28-29 (1985-86), 157-182,

Ljubljana.

MOJSISOVICS, E. (1880): West Bosnien und Tür-

kisch-Croatien.- In: MOJSISOVICS, E., TIETZE,

E. & BITTNER, A. (eds.): Grundlinien der Geolo-

gie von Bosnien-Herzegowina. Jahrb. Geol. Reich-

sanst., 30, 1-100, Wien.

OBRADOVI∆, J. & VASI∆, N. (1996): The signifi-

cance of the radiolarites in the evolution of deposi-

tional basins - some examples in Yugoslavia.- In:

Terranes of Serbia. Univ. of Belgrade & Serbian

Acad. of Sci. and Arts, 191-195, Beograd.

PAMI∆, J. (1993): Eoalpine to Neoalpine magmatic

processes in the northwestern Vardar Zone, the east-

ernmost Periadriatic Zone and the southwestern

Pannonian Basin.- Tectonophysics, 226, 503-518.

PAMI∆, J. (1997): The northwesternmost outcrops of

the Dinaric ophiolites: a case study of Mt. Kalnik

(North Croatia).- Acta geol. Hungar., 40/1, 37-56.

PAMI∆, J., GU©I∆, I. & JELASKA, V. (1998): Geody-

namic evolution of the Central Dinarides.- Tectono-

physics, 297, 251-264.

PETERS, F.K. (1863): Bemerkungen über die Bedeu-

tung der Balkan-Halbinsel als Festland in der Lias-

periode.- Sitzungsber. Akad. Wiss. (Matem.-natur-

wiss. Klasse), 6-10, 418-426, Wien.

PILAR, Gj. (1882): Geoloπka zapaæanja u zapadnoj

Bosni. Iztraæivanja od 1879.- Rad Jugosl. akad.

znan. i umjetn., 65, 1-68, Zagreb.

PREMRU, U. (1975): Starost ponikvastih skladov (Das

Alter der Ponikva-Schichten).- Geologija, 18, 75-

86, Ljubljana.

PREMRU, U. (1983): Osnovna geoloπka karta SFRJ

1:100.000. List Ljubljana L33-66.- Geol. zavod



98 Geologia Croatica 52/1

Ljubljana (1969-1978), Savezni geoloπki zavod,

Beograd.

PREMRU, U., OGORELEC, B. & ©RIBAR, Lj.

(1977): O geoloπkoj zgradbi Dolenjske (On the geo-

logical structure of the Lower Carniola).- Geologija,

20, 167-192, Ljubljana.

PRTOLJAN, B., O©TRI∆, N., FU»EK, L., VELI∆, I.

& TI©LJAR, J. (1995): Mezozojske vapnenaËke sti-

jene u predjelu Horvatove stube - Markov travnik.-

In: ©IKI∆, K. (ed.): Geoloπki vodiË Medvednice.-

Inst. geol. istraæ. & INA-Naftaplin, 137-139, Zag-

reb.

RATSCHBACHER, L., FRISCH, W., LINZER, H.G.

& MERLE, O. (1991): Lateral extrusion in the East-

ern Alps; Part 2: structural analysis.- Tectonics,

10/2, 257-271. 

ROMANDI∆, S. & ALJINOVI∆, B. (1999): Interpreta-

tion of geophysical data in SW part of Dinarides.-

Working materials, 2nd Intern. Symposium of

Petroleum Geology. Croat. Acad. of Sci. and Arts,

Faculty of Mining, Geology and Petroleum Engi-

neering & INA, 195-205, Zagreb. 

SALOPEK, M. (1914): Moderna alpinska tektonika i

geologija Hrvatske i Slavonije.- Glasnik Hrv. prir.

druπtva, 26/2, 85-109, Zagreb.

SIKO©EK, B. & MEDWENITSCH, W. (1965): Neue

daten zur fazies und tektonik der Dinariden.- Verh.

Geol. Bundesanst., Sonderheft G, 86-102, Wien.

SREMAC, J. & MIHAJLOVI∆-PAVLOVI∆, M.

(1983): Graptoliti Medvednice (ZagrebaËke gore)

(Graptolites of Mt. Medvednica - ZagrebaËka Go-

ra).- Rad Jugosl. akad. znan. i umjetn., 404, (Razr.

prir. znan., 19), 65-68, Zagreb.

SUESS, E. (1875): Die Entstehung der Alpen.- Born-

träger, Berlin, 158 p.

SZEDERKENY, T. (1996): Metamorphic formations

and their correlation in the Hungarian part of Tisia

Megaunit (Tisia composite terrane).- In: Terranes of

Serbia. Univ. of Belgrade & Serbian Acad. of Sci.

and Arts, 229, Beograd.

©IKI∆, K. (ed.) (1995): Geoloπki vodiË Medvednice.-

Inst. za geol. istraæ. & INA, Zagreb, 199 p.

©IKI∆, K., BASCH, O. & ©IMUNI∆, A. (1978): Osno-

vna geoloπka karta SFRJ 1:100000. List Zagreb,

L38-80.- Inst. geol. istraæ. (1972), Savezni geol.

zavod, Beograd.

©IKI∆, K., BASCH, O. & ©IMUNI∆, A. (1979): Osno-

vna geol. karta SFRJ 1:100000. TumaË za list Zag-

reb, L38-80.- Inst. geol. istraæ. (1972), Savezni geol.

zavod, Beograd, 81 p.

©IMUNI∆, A. (1979): The deep marine development of

Paleozoic and Mesozoic in Northwestern Croatia.-

16th European micropaleont. colloquium, 107-111,

Ljubljana.

©IMUNI∆, A. (1992): Geoloπki odnosi srediπnjeg dijela

Hrvatskog zagorja.- Unpublished PhD Thesis, Uni-

versity of Zagreb, 193 p.

©IMUNI∆, A. & HE∆IMOVI∆, I. (1979): Tektonski

odnosi sjeverozapadne Hrvatske - IvanπËica, Kalnik

i Ravna gora (Tectonic relationships of the north-

west Croatia - IvanπËica, Kalnik and Ravna Gora).-

Zbornik radova 4. god. skupa Sekcije za primjenu

geol., geofiz. and geokem. Znan. savjeta za naftu,

StubiËke toplice, 1978, Jugosl. akad. znan. i umj-

etn., 187-198, Zagreb.

©IMUNI∆, A. & PAMI∆, J. (1989): Ultramafitne sti-

jene kod Gornjeg Oreπja na sjeveroistoËnim obron-

cima Medvednice (Ultramafic rocks on the north-

eastern flanks of Mt. Medvednica - northern Croat-

ia).- Geol. vjesnik, 42, 93-101.

©IMUNI∆, A., NAJDANOVSKI, J. & PAMI∆, J.

(1993): Chaotic rock-complexes, possible hydrocar-

bon accumulations in southwestern parts of the Pan-

nonian Basin (R. of Croatia).- Nafta, 44/11, 609-

616, Zagreb.

TORNQUIST, A. (1918): Das Erdbeben von Rann an

der Save.- Mitt. Erdbebenkommission, N.F., 52, 1-

117, Wien.

WINKLER, A. (1924): Über den Bau der östlichen

Südalpen.- Mitt. geol. Ges., 16 (1923), 1-272, Wien.

ZUPANI», J., BABI∆, Lj. & CRNJAKOVI∆, M.

(1981): Bazenski klastiti donje krede (Oπtrc forma-

cija) IvanπËice u sjeverozapadnoj Hrvatskoj (Lower

Cretaceous basinal clastics (Oπtrc formation) in Mt.

IvanπËica (northwestern Croatia)).- Acta geol., 11,

1-44, Zagreb.

Manuscript received February 3, 1998.

Revised manuscript accepted May 28, 1999.