GEOLOGIJA 40, 305-323 (1997), Ljubljana 1998
Structure of Mt. Blegoš between the Inner and the Outer
Dinarides
Zgradba Blegoša med Notranjimi in Zunanjimi Dinaridi
Ladislav Placer
Geološki zavod Ljubljana
Inštitut za geologijo, geotehniko in geofiziko
Dimičeva 14, 1000 Ljubljana, Slovenija
Jože Čar
Univerza v Ljubljani, Naravoslovnotehniška fakulteta. Oddelek za geologijo
Aškerčeva 12, 1000 Ljubljana, Slovenija
Key words: boundary Inner-Outer Dinarides, Slovenia
Ključne besede: meja Notranji-Zunanji Dinaridi, Slovenija
Abstract
The boundary between the Inner and the Outer Dinarides in the sense of B u s e r
(1987b) west of the Zagreb lineament is predominantly of overthrust character. The
Inner Dinarides are ovethrusted on the Outer Dinarides. Mt. Blegoš, situated in the
Outer Dinarides west of Ljubljana, on the boundary with the Inner Dinarides, con-
sists of horses that were formed during overthrusting of the Outer Dinarides from
the direction of the Dinaric carbonate platform towards the Adriatic platform, i.e.
in the present sense from northeast to southwest, probably during the Upper Eoce-
ne. After Sarmatian time these horses were first folded and then rotated around the
W-E axis owing to the overthrusting of the Inner Dinarides and Southern Alps from
north towards south on the Outer Dinarides. The footwall nappe plane along which
the Inner Dinarides in the Blegoš area were overthrusted southwards on the Outer
Dinarides is besides the footwall nappe plane of the Southern Alps the most impor-
tant nappe line south of the Periadriatic lineament. In the area from Ljubljana ba-
sin to Tolmin this boundary is clearly expressed, whereas westwards and eastwards
it has not been uniformly defined. Along the considered footwall nappe plain the
Outer Dinarides were clearly rotated towards the Inner Dinarides and the Southern
Alps for 30° to 45°, and thrusted under them.
Kratka vsebina
Meja med Notranjimi in Zunanjimi Dinaridi v Buserjevem smislu (1987b)
zahodno od Zagrebškega lineamenta je pretežno narivna. Notranji Dinaridi so nari-
njeni na Zunanje Dinaride. Blegoš v Zunanjih Dinaridih na meji z Notranjimi Dina-
ridi zahodno od Ljubljane je zgrajen iz lusk, ki so nastale med krovnim narivanjem
Zunanjih Dinaridov iz smeri od Dinarske karbonatne platforme proti Jadranski plat-
formi, kar pomeni v današnjem smislu od severovzhoda proti jugozahodu, verjetno v
zgornjem eocenu. Te luske so bile po sarmatski dobi zaradi narivanja Notranjih
306
Ladislav Placer & Jože Čar
Dinaridov in Južnih Alp od severa proti jugu na Zunanje Dinaride najprej naguba-
ne, nato pa zarotirane okoli osi W-E. Osnovna krovna narivna ploskev, ob kateri so
bili Notranji Dinaridi na območju Blegoša narinjeni proti jugu na Zunanje Dinari-
de, je poleg osnovne krovne narivne ploskve Južnih Alp najpomembnejša krovna
narivna črta južno od Periadriatskega lineamenta. Na prostoru od Ljubljanske ko-
tline do Tolmina je ta meja jasna, medtem ko zahodno in vzhodno od tod še ni ne-
dvoumno definirana. Ob obravnavani osnovni krovni narivni ploskvi so Zunanji Di-
naridi jasno zasukani nasproti Notranjim Dinaridom in Južnim Alpam za 30° do 45°
in pod le-te podrinjeni.
Introduction
In the hinterland of the Triest bay, west of the Zagreb lineament, the terms Alpine
(W-E) and Binarie (NW-SE) directions, or Alpine and Binarie structural elements,
obtained their right of existence in the geological professional jargon. They certainly
cannot be used along the global extension of the Alpides, but they have a considera-
ble value for local communication, since they efficiently illustrate the circumstances
at the contact of Outer Binari des with the Inner Binarides (Fig. 1). On the spatially
Fig. 1. Slovenia. Synthetic geotectonic sketch-map of the contact of
Eastern Alps and Dinarides, after Buser (1987b), Premru (1989), Kazmer
and Kovacs (1989), Csontos et al. (1992), Ravnik et al. (1995)
1 Eastern Alps; 2 Southern Alps; 3 Inner Dinarides; 4 Outer Dinarides;
5 Tisa unit
SI. 1. Slovenija. Sintetična geotektonska skica stika Vzhodnih Alp in Dina-
ridov. Po predlogah: Buser (1987b), Premru (1980), Kazmer in Kovacs
(1989), Csontos s sodelavci (1992), Ravnik s sodelavci (1985)
1 Vzhodne Alpe; 2 Južne Alpe; 3 Notranji Dinaridi; 4 Zunanji Dinaridi;
5 Enota Tisa
structure of Mt. Blegoš between the Inner and the Outer Dinarides_307
limited territory of Slovenia the structures strike in the alpine direction in the Sou-
thern Alps and the predominant part of the Inner Dinarides, while the structures in
the Outer Dinarides have the dinaric direction. Only in the belt along the Inner Dina-
rides the dinaric structures are in places masked by the alpine trending directions,
especially in areas where the Outer Dinarides consist of softer Lower Triassic and
Paleozoic rocks. In this paper we are interested in the boundary between the Inner
and the Outer Dinarides in western Slovenia, and its geometric and kinematic cha-
racteristics that shall be described at the example of the structure of Mt. Blegoš (1562
m) west of Ljubljana (Fig. 2), as well as the significance of these findings for the
study of genesis of the present structure of the Dinarides. This research is based on
geological mapping partially performed by Čar, and on kinematic analysis that was
done by Placer.
Structure of Mt. Blegoš
The environs of Blegoš were mapped geologically several times, first during the Au-
stro-Hungarian monarchy at the scale 1:75000 (K o s s m a t, 1910), then for the Basic
geological map of Yugoslavia at 1:100000 (Grad & Ferjančič, 1974,1976; B u s e r,
1986, 1987a), and finally in detail, at the scale 1:10000, in the frame of prospecting for
mercury, copper and uranium (unpublished reports by Mlakar, Placer and Čar), so that
the presented ideas on the structure of this area are founded on a large number of fac-
tographic data. This territory consists of three units that are all built of nappes (Fig. 1,
Fig. 2). These are the Southern Alps in the north, consisting of Mesozoic rocks of the
Julian carbonate platform, the Inner Dinarides, of pelagic Triassic, Jurassic and Cre-
taceous clastics, marl and platy limestones of the Slovenian basin and its basement,
and the Outer Dinarides that consist in the Blegoš area of the Tmovo and the Hrušica
nappes. Of the latter, the first nappe consists of Carboniferous and Permian clastics,
and more southwestwards of Triassic, Jurassic and Cretaceous carbonate rocks, and
the second one of Triassic carbonate rocks. The carbonate beds of the Trnovo and
Hrušica nappes form the marginal part of the Dinaric carbonate platform. The Hruši-
ca nappe appears in the studied territory in the tectonic halfwindow below the Trnovo
nappe, named in the geological-morphological sense the Poljane-Vrhnika region. The
latter divides the Trnovo nappe into the Idrija-Žiri region in southwest, and the Ško-
fja Loka-Polhov Gradec region in the northeast. The internal structural elements in
the Trnovo and Hrušica nappes are expressively dinaric, which is characteristic for
the strike of beds and of internal thrust planes. In nappes of the Inner Dinarides the
structures are generally of W-E direction. Kinematically the nappes of the Outer Di-
narides are older, and theay have been overthrusted in the present sense from north-
east towards southwest. The Tmovo nappe is overthrusted on the Eocene flysch of the
Vipava valley, and is therefore of Upper Eocene or Lower Eocene age. The Inner Dina-
rides are overthrusted from north towards south on the Tmovo and Hrušica nappes.
As indicated by Upper Miocene beds that were folded in the Eastern Sava folds in
connection with this overthrusting, these nappes are of Post-Miocene age. With res-
pect to the fact that the dinaric trending antiform of the Poljane-Vrhnika region repo-
sed on the footwall nappe plane of the Inner Dinarides which is not folded, it follows
that the antiform dates from time before forming of these nappes.
The general relationship between the alpine and dinaric trending overthrust struc-
tures in west Slovenia can be found in all works of earlier researchers of this territoiy,
308
Ladislav Placer & Jože Čar
Kossmat (1913, Plate V), Winkler (1923, Plate IV), Grad and Ferjančič
(1974, 1976), Premru (1980) and B u s e r (1986, 1987a). However, Premru deci-
dedly stated that the younger alpine trending overthrust sheets that were moved from
north to south during the Rhodanian orogeny, cover the older dinaric trending over-
thrust sheets that were overthrusted from northeast to southwest in the Illyric-Pyre-
nean orogeny, an observation that at present cannot be denied.
In all nappe units appears in the Blegos area an expressive structural geometric
anomaly the center of which is the carbonate massif of Blegoš in the extreme north-
western part of the Poljane-Vrhnika region, consequently in the place where the com-
petent carbonate rocks of the Hrušica nappe below the incompetent rocks of the Tr-
novo nappe come in contact with the Inner Dinarides.
Fig. 2. Nappe subdivision of wider Blegoš surroundings
SI. 2. Krovna rajonizacija širše okolice Blegoša
structure of Mt. Blegoš between the Inner and the Outer Dinarides
309
Fig. 3. Geological sketch-map of Blegoš. Used unpublished data of Mlakar (Škofje) and Čar
(Črni vrh, western part of Blegoš)
1 Jelovica nappe (Grad & Ferjančič, 1974, 1976); 2 Nappes of Inner Dinarides (Fig. 2),
Podmelec nappe (Fig. 3); 3 Tmovo nappe; 4 Hrušica nappe; 5 Plioquatemary and Quaternary;
6 More important subvertical fault; 7 Footwall nappe plane of Southern Alps and Inner
Dinarides; 8 Thrust plane of Tmovo nappe; 9 Thrust plane within the Hrušica nappe; 10 Blegoš
horses; 11 Bounda^ of uplift of eastern part of Blegoš; 12 Davča anticline; 13 Blegoš syncline;
14 Valovnik anticline; 15 Thermal spring in the Kopačnica Valley; 16 Inclined fold axis; 17 Ge-
neral directin of thnisting; 18 Noiraal beds; 19 Inverse beds; 20 Inverse horizontal beds
SI. 3. Geološka skica Blegoša. Uporabljeni so neobjavljeni podatki Mlakarja (Škofje) in Čarja
(Cmi vrh, zahodni del Blegoša)
1 Jelovški pokrov (Grad & Ferjančič, 1974, 1976); 2 Pokrovi Notranjih Dinaridov (si. 2),
Podmelški pokrov (si. 3); 3 Trnovski pokrov; 4 Hrušiški pokrov; 5 Pliokvartar in kvartar;
6 Pomembnejši sub vertikalni prelom; 7 Osnovna krovna narivna ploskev Južnih Alp in
Notranjih Dinaridov; 8 Krovna narivna ploskev Trnovskega pokrova; 9 Narivna ploskev zno-
traj Hrušiškega pokrova; 10 Blegoške krovne luske; 11 Meja dviga vzhodnega dela Blegoša;
12 Davška antiklinala; 13 Blegoška sinklinala; 14 Valovniška antiklinala; 15 Termalni izvir
ob Kopačnici; 16 Poševna os gube; 17 Generalna smer narivanja; 18 Normalne plasti; 19 In-
verzne plasti; 20 Inverzne horizontalne plasti
310
Ladislav Placer & Jože Čar
Fig. 4. Lithostratigraphic development of nappe units in the Blegoš area
SI. 4. Litostratigrafski razvoj krovnih enot na območju Blegoša
In naming the nappe units we used the terms that are not yet generally accepted,
since no consens was reached yet on the extent of individual units, and the differen-
ces in ideas usually also result in to different naming. The rocks of the Slovenian ba-
sin west of the Ljubljana basin were named, e.g. after Winkler (1923) the Julian
outer zone, after Grad and Ferjančič (1976) the Selce zone, they are included
after P r e m r u (1980) into the Sorica and Selce overthrusts, and according to B u s e r
(1986) into the Kobla, Rute and Podmelec nappes. As a curiosity it should be mentio-
ned that for the same unit the term Tolmin nappe was proposed by K r y s t i n et al.
(1994, 415). The nappe structure of the Southern Alps and Inner Dinarides was not
structure of Mt. Blegoš between the Inner and the Outer Dinarides_7
subdivided by us, since there is no need for it in this article. The Trnovo nappe is un-
derstood in the sense of Mlakar (1969, Žiri-Tmovo nappe), Grad and F e r j a n-
Č i č (1974, 1976, Škofja Loka-Trnovo nappe), and Placer (1981, Trnovo nappe),
and Hrušica nappe in the sense of Placer (1981).
Before continuing the regional discussion, the structure of Blegoš should be descri-
bed in some more detail, as shown schematically on Fig. 3. Lithostratigraphy appears
on Fig. 4. The massif of the mountain consists of the extensive Blegoš syncline (B)
that steeply is inclined towards southwest. Northwards it passes over into the smaller
Davča anticline (D) just below the footwall nappe plane of the Inner Dinarides, and
southwards into the Valovnik anticline (V) that straightens out into the Poljane-
Vrhnika region of dinaric trending beds. The axes of these three folds are subparallel,
and the dip elements for the Davča anticline and the Blegoš syncline amount to
235/50, and for the Valovnik anticline 245/65. The Blegoš syncline consists of several
horses named the Blegoš horses that were folded together with beds. The angle bet-
ween the thrust plane of the horses and the beds is small, abot 5o only. The lowest
horse in the sequence is horse 1 consisting of normally lying Middle Triassic and Cor-
devolian beds of the Pseudozilja Formation in the sense of Placer and Kolar-
Jurkovšek (1990). Follows the horse 2 of normally lying Middle Triassic pyrocla-
stics of the lower part of Pseudozilja Formation that discordantly overly the Carbo-
niferous-Permian clastics and rocks of the Groden, Bellerophon and Werfen Formati-
on. Next is the horse 3 of normally lying beds of the Pseudozilja, Rabelj, Transition
and Main dolomite Formation the horse 4 of normally lying beds of the upper part of
Rabelj Formation and of the rocks of Transition, Main dolomite and Dachstein For-
mation. Above the 4th horse the horse 5 is overthrusted. It consist of beds of the Pseu-
dozilja Formation and lower part of Rabelj Formation in normal position, followed
by the horse 6 from the same rocks in inverse position, and finally horse 7 of Bellero-
phon and Werfen Formation and discordantly deposited Langobardian pyroclastics
in inverse position. The belt of overthrusted rocks at the bottom of the Podmelec nap-
pe is formed of the Pseudozilja and Amphiclina Formation rocks. This suggests a wi-
der overthrust zone, that structurally is not analysed yet. The internal structure of
horses with normally lying beds is best exposed in horse 3 where the normal boun-
dary between the variegated lower part of Rabelj clastics and transition beds in the
northern flank of the Blegoš syncline is cut by the hanging wall thrust plane, and in
the southern flank by the footwall thrust plane of the mentioned horse. Consequently,
a beautiful exposure of the oblique cut within the Hrušica nappe that was formed in
the stage of genesis of the nappe structure of the Outer Dinarides. The starting form
for the kinematic development of Blegoš horses can be illustrated by an overthrown
fold (Fig. 5) where the succession of appearing horses is well visible, and also the re-
lations between the horses with the normal and the inverse position of beds.
The second characteristics of the Blegoš structure is its northeastern, eastern, sou-
theastern and southern to southwestern boundary with the surrounding rocks that in-
dicates the extreme uplift of the eastern part of the Blegoš massif (Fig. 6). The uplift
can be explained by the tilt of the axes of folds towards southwest. This siginifies ro-
tation of the originally subhorizontal folded beds and horses into the present steep po-
sition. The uplift of the eastern part of Blegoš must have happened along pre-existing
sub vertical faults of various directions (Fig. 2) that are marked in Fig. 3 with a special
sign. The movements in question are consequently of the inherited character. East of
this boundary appear inversely lying beds of the Pseudozilja Formation in discordant
relationship with the Lower Triassic beds. Therefore they are compared with equal
312
Ladislav Placer & Jože Čar
Fig. 5. Initial structure of the Blegoš horses in the Hrušica nappe
1 Tmovo nappe; 2 Lithostratigraphic structure of horses on the surface, Fig. 3;
3 Thrust plane of Trnovo nappe; 4 Thrust plane within the Hrušica nappe; 5 Blegoš
horses; 6 Normal boundary; 7 Unconformity; D.F. Dachstein Formation; M.D.F.
Main dolomite Formation; T.F. Transition Formation; R.F. Rabelj Formation;
P.F. Pseudozilja Formation; M.F Mendola Formation; W.F Werfen Formation
SI. 5. Izhodiščna struktura blegoških lusk v Hrušiškem pokrovu
1 Trnovski pokrov; 2 Litostratigrafska zgradba lusk na površju, si. 3; 3 Krovna
narivna ploskev Trnovskega pokrova; 4 Narivna ploskev znotraj Hrušiškega
pokrova; 5 Blegoške luske; 6 Normalna meja; 7 Diskordanca; D.F. Dachsteinska
formacija; M.D.F Glavnodolomitna formacija; T.F. Prehodna formacija; R.F. Rabeljska
formacija; P.F Psevdoziljska formacija; M.F. Mendolska formacija; W.F. Werfenska
formacija
beds of horse 7 west of the Blegoš summit. This horse is covered east of Blegoš by the
Carboniferous-Permian beds of the Tmovo nappe. The nappe character of the Tmovo
structure is indicated in this area by the nearby tectonic window.
The folded structure of Blegoš continues south west ward also in the Tmovo nappe.
In the core of the Blegoš syncline occurs the structure of Škofje, and in the core of the
Valovnik anticline the tectonic halfwindow consisting of rocks of the Hrušica nappe
east of Škofje along Podplečica brook.
The geometric anomaly in the Blegoš area occurs also in the structure of the Inner
Dinardes. It is expressed by a deviation of its footwall nappe plane from the W-E di-
rection into the SW-NE direction, and with a parallel deviation of strike of beds. Tha
massif of Blegoš is represented consequently by a core of competent rocks of the Hru-
šica nappe surrounded by incompetent rocks of the Trnovo nappe and the Inner Di-
narides.
Interesting from the kinematic standpoint is certainly the question on the mecha-
nism that resulted into the Blegoš stmcture. Before defining the starting data the
structure of the Poljane-Vrhnika region should be reviewed somewhat more in detail
(Fig. 7). This structure is represented by an anticlinal arch of rocks of the Hrušica
nappe in the NW-SE direction in which occurs also the anticlinally arched thrust
plane of the Trnovo nappe. The nappe is proved by tectonic klippes of Carboniferous-
Permian clastics amidst the anticlinal arch, and by tectonic halfwindows in valleys
transversely to the anticlinal ridge, where the carbonate rocks of the Hrušica nappe
pass deeply below the clastics of the Tmovo nappe. In the C-D profile of the Basic ge-
ological map, sheet Kranj (Grad & Ferjančič, 1974) that passes across the
structure of Mt. Blegoš between the Inner and the Outer Dinarides
313
Fig. 6. Cross section across the summit of Blegoš SW-NE. Section 2. Position of the
section on Fig. 3
1 Trnovo nappe; 2 Podmelec nappe; 3 Footwall nappe plane of the Inner Dinerides;
4 Thrust plane of the Trnovo nappe; 5 Thrust plane within the Hrušica nappe; 6 Ble-
goš horses; 7 Normal beds; 8 Inverse beds; 9 Fault; 10 Boundary of uplift of eastern
part of Blegoš; 11 Virtual throw along to the boundary of uplift of eastern part of
Blegoš
SI. 6. Profil prek vrha Blegoša v smeri SW-NE. Profil 2. Lega profila na si. 3
1 Trnovski pokrov; 2 Podmelški pokrov; 3 Osnovna krovna narivna ploskev Notra-
njih Dinaridov; 4 Krovna narivna ploskev Trnovskega pokrova; 5 Narivna ploskev
znotraj Hrušiškega pokrova; 6 Blegoške luske; 7 Normalne plasti; 8 Inverzne plasti;
9 Prelom; 10 Meja dviga vzhodnega dela Blegoša; 11 Navidezni skok ob meji dviga
vzhodnega dela Blegoša
Poljane-Vrhnika region, no thrust planes appear that v^^ould cut beds at a small angle
of around 5 degrees. Hov^ever, these nappes in Blegoš exist, and w^e presume they are
either not everyv^here developed, or they were not mapped. The beds of the Poljane-
Vrhnika region are folded, but they are generally subhorizontal and dipping more or
less steeply towards southwest in the southwestern flank, and towards northeast in
the northeastern flank.
The geometry of the alpine and dinaric systems of nappes is presented in Fig. 8.
Circumstances in the surroundings of Blegoš are a variant of this scheme (Fig. 9).
From it the present structure of Blegoš can be derived. The starting structure is con-
sequently represented by: (1) strike and dip of the footwall nappe plane of the Inner
Dinarides, (2) strike and dip of beds in the Poljane-Vrhnika region and (3), strike and
dip of internal thrust planes in this unit. The direction of the footwall nappe plane of
the Inner Dinarides can be determined from the geological map, whereas the dip an-
gle can be measured directly. For this, the dips of the nappe planes in the Inner Dina-
rides themselves, as given by B u s e r (1987a) on the geological map, sheets Tolmin
314
Ladislav Placer & Jože Čar
Fig. 7. Cross section of the Poljane-Vrhnika region. Section 1. Position of the section on Fig 2.
Legend as on Fig. 5
SI. 7. Prečni profil Poljansko-Vrhniškega ozemlja. Profil 1. Lega profila na si. 2.
Legenda na si. 5
Fig. 8. Relationship between nappe thrusts of al-
pine and dinaric directions. Legend as on Fig. 9
SI. 8. Odnos med krovnimi narivi alpske in dinarske
smeri. Legenda na si. 9
and Videm, amount to about 20°. Hence, the dip elements of the footwall nappe plane
of the Inner Dinarides and their variation in the Blegoš area would be 310/20+10. The
average dip of beds and internal thrust planes in the Poljane-Vrhnika region can be
considered together, since the difference of around 5° between them is negligible in the
general analysis. The dips of beds on the basic geological map, sheet Kranj (Grad &
Ferjančič, 1974) vary widely, so in the analysis the dips towards southwest and
northeast up to 30° were taken into account, and the subhorizontal position.
The starting point for genetic analysis of the actual Blegoš structure is the as-
sumption that the beds and the formed horses within the Hrušica nappe owing to
overthrusting of the Inner Dinarides from north southwards were first folded, and
then rotated from north towards south. The axis of the peri-nappe folds is according
to theory the line of intersection between the beds of the Poljane-Vrhnika region and
the footwall nappe plane of the Inner Dinarides, and the rotation of the formed folds
took place around the axis in the W-E direction, conformingly with overthrusting of
the Inner Dinarides from north towards the south.
With respect to the enumerated variants of dips of beds exist several variants of
possible intersecting lines with the footwall nappe plane of the Inner Dinarides (Fig.
10). With the dip of the footwall nappe plane of the Inner Dinarides of 310/20±10 and
with variants of dips of beds (225/0-30, 45/0-30) two fields of lines of intersection re-
sult, and they are at the same time the axes of newly formed folds (fields 1 and 2).
structure of Mt. Blegoš between the Inner and the Outer Dinarides_315
Fig. 9. Relationship between the footwall nappe plane
of the Inner Dinarides and thrust plane of the Trnovo
nappe in the Blegoš area
1 Footwall nappe plane of the Inner Dinarides; 2 Thrust
plane of Trnovo nappe; 3 Variant of the primary posi-
tion of footwall nappe plane of Inner Dinarides
SI. 9. Odnos med osnovno krovno narivno ploskvijo
Notranjih Dinaridov in krovno narivno ploskvijo
Trnovskega pokrova na območju Blegoša
1 Osnovna krovna narivna ploskev Notranjih Dinari-
dov; 2 Krovna narivna ploskev Trnovskega pokrova;
3 Varianta prvotne lege osnovne krovne narivne
ploskve Notranjih Dinaridov
With regard to the mode of formation of the present positon of the Blegos folds (V, D,
B) by rotation of the lines of intersection around the W-E axis, it becomes at the first
look evident that the lines of intersection in field 1 cannot be rotated into the actual
position of the axes of the Blegoš folds. This can be performed only with the segment
of field 2, and this between the traces of rotation a and b that touch the external bo-
undaries of the limits of influence of the axes of Blegoš fods V, D, B (field 3). The data
on oleate show that at the selected variant of dip of the nappe basal plane 310/20+10
the dip of the beds in the Poljane-Vrhnika region in the initial phase of overthrusting
of the Inner Dinarides must have been between 45/1 to 45/13, or rounded at 45/0-15.
The difference between the original direction of folds (field 2) and the present positi-
on confirms the virtual uplift of the eastern part of Blegoš which amounts to around
3000 m according to construction from section across the summit of Blegoš in the
SW-NE direction (Fig. 6).
Besides the described model of reconstruction a second model ought to be mentio-
ned. In analysis on Fig. 10 the starting point was the primary anomalous position of
the footwall nappe plane of the Inner Dinarides in the 220-40 direction (line 1 on the
Fig. 9). However, if the general direction of the mentioned footwall nappe plane W-E
316
Ladislav Placer & Jože Čar
Fig. 10. Kinematic genesis of the structure of Blegoš,
variant
1 Footwall nappe plane of the Inner Dinarides; 2 Dip of
beds of the Poljane-Vrhnika region; 3 Field of dispersion
of lines of intersection between the footwall nappe plane
of the Inner Dinarides and beds in southwestern flank of
the Poljane-Vrhnika region; 4 Field of dispersion of lines
of intersection between the footwall nappe plane of the
Inner Dinarides and beds in northeastern flank of the Po-
ljane-Vrhnika region; 5 Field of dispersion of axes of Ble-
goš folds; 6 Boundary traces of rotation; 7 Extreme lines
of intersection in field 2
SI. 10. Kinematska geneza strukture Blegoša, 1. varianta
1	Osnovna krovna narivna ploskev Notranjih Dinaridov;
2	Vpad plasti Poljansko-Vrhniškega ozemlja; 3 Polje
sipanja presečnic med osnovno krovno narivno ploskvijo
Notranjih Dinaridov in plastmi v jugozahodnem krilu
Poljansko-Vrhniškega ozemlja; 4 Polje sipanja presečnic
med osnovno krovno narivno ploskvijo Notranjih Dina-
ridov in plastmi v severovzhodnem krilu Poljansko-
Vrhniškega ozemlja; 5 Polje sipanja osi blegoških gub;
6 Mejni trasi rotacije; 7 Skrajni presečnici v polju 2
is taken into account (line 3 on the Fig. 9), and the assumption is made of its later de-
formation owing to the hindrance of competent rocks of the Poljane-Vrhnika region,
then the starting point of kinematic analysis becomes somewhat different. With the
general direction of the footwall nappe plane of the Inner Dinarides 360/20+10 it is
possible to reconstruct the Blegoš structure at the condition of northeastern dip of
beds in the Poljane-Vrhnika region, which is identical with results of the first analy-
sis, with the difference in the starting dip of beds that is somewhat higher, amounting
to 45/8 to 45/28, or rounded 45/10-30 (Fig. 11).
structure of Mt. Blegoš between the Inner and the Outer Dinarides
317
Fig. 11. Kinematic genesis of the Blegoš structure,
variant. Legend as on figure 10
SI. 11. Kinematska geneza strukture Blegoša, 2. varian-
ta. Legenda na sliki 10
Discussion
The relationship between the Inner and the Outer Dinarides in the Blegoš area
suggests the contact of two different nappe systems: (1) the south alpine system that
comprises the Southern Alps and the Inner Dinarides west of the Ljubljana basin,
and (2), the dinaric system that consists of the Outer Dinarides. Deformations in the
alpine direction that occur in places in the dinaric system below the footwall nappe
plane of the Inner Dinarides were formed owing to overthrusting from north towards
the south. This signifies that the dinarically oriented structures are masked by the al-
pine directed structures, as witnessed by the actual structure of Blegoš and by W-E
folds in incompetent clastic beds of the Trnovo nappe. The boundary between the al-
pine and the dinaric system of overthrusting is clear in the Ljubljana basin - Tolmin
area. Less so in the west and east, where the dinaric nappe units are entirely permea-
ted with the secondary alpine structures.
It follows from our conclusions that the footwall nappe plane of the Inner Dinari-
des in the Blegoš area represents the southern boundary of the south alpine nappes.
This boundary has a deeper structural significance, since it does not involve local ro-
tation of a smaller block of the Outer Dinarides with respect to the Inner Dinarides
west of the Zagreb lineament, but the contact of two extensive units that had been
originally most likely veiy far apart, the reasoning which is in hypothetical discussi-
ons of genesis of the Dinarides much too little considered. Here we deal with the con-
tact zone whose geometry and genesis are not yet satisfactorily solved. The conside-
red footwall nappe plane in the hinterland of the Triest Bay represents besides the fo-
otwall nappe plane of the Southern Alps the most important overthrust structure so-
318_Ladislav Placer & Jože Čar
uth of the Periadriatic lineament. Along it the rotation of the Outer Dinarides with
respect to the Inner Dinarides and Southern Alps for 40° to 45° is well expressed.
The comparison of individual concepts on the structure of the boundary between
the Inner and the Outer Dinarides was not the object of this article.
Zgradba Blegoša med Notranjimi in Zunanjimi Dinaridi
Uvod
V zaledju Tržaškega zaliva zahodno od Zagrebškega lineamenta sta se v geološkem
strokovnem žargonu uveljavila termina alpska (W-E) in dinarska (NW-SE) smer ozi-
roma alpski in dinarski elementi strukture, ki ju seveda ne moremo uporabljati v
smislu planetarne razsežnosti Alpidov, temveč imata zgolj lokalni sporazumevalni
pomen, saj na tem prostoru dobro ponazarjata razmere na stiku Zunanjih z Notranji-
mi Dinaridi (si. 1). Na prostorsko omejenem ozemlju Slovenije potekajo strukture v
alpski smeri v Južnih Alpah in pretežnem delu Notranjih Dinaridov, dinarsko smer
pa imajo strukture v Zunanjih Dinaridih. Le v pasu ob Notranjih Dinaridih, pre-
dvsem tam, kjer grade Zunanje Dinaride mehkejše spodnjetriasne in paleozojske ka-
mnine, so dinarsko usmerjene strukture ponekod maskirane z alpsko usmerjenimi. V
tem prispevku nas zanima meja med Notranjimi in Zunanjimi Dinaridi v zahodni
Sloveniji oziroma njene geometrijske in kinematske karakteristike, ki jih bomo opi-
sali na primeru zgradbe Blegoša (1562 m) zahodno od Ljubljane (si. 2) in pomen teh
ugotovitev za študij geneze aktualne zgradbe Dinaridov. Prispevek Čar j a v tem član-
ku je kartografski, medtem ko je kinematska analiza Placer j evo delo.
Zgradba Blegoša
Okolica Blegoša je bila geološko kartirana večkrat, najprej v času avstro-ogrske
monarhije v merilu 1:75000 (K o s s m a t, 1910), nato za Osnovno geološko karto Ju-
goslavije v merilu 1:100000 (Grad & Ferjančič, 1974,1976; B u s e r, 1986,
1987a) in nazadnje podrobno v merilu 1:10000 v okviru raziskav na živo srebro, baker
in uran (neobjavljena poročila Mlakarja, Placer j a in Čar j a), tako, da temeljijo predlo-
žena spoznanja o zgradbi tega območja na velikem številu faktografskih podatkov. To
ozemlje sestavljajo tri enote, ki so vse zgrajene iz pokrovov (si. 1, si. 2). To so: Južne
Alpe na severu iz mezozojskih kamnin Julijske karbonatne platforme. Notranji Dina-
ridi iz pelagičnih, triasnih, jurskih in krednih klastitov, laporja in ploščnatih apnen-
cev Slovenskega bazena in njegove podlage ter Zunanji Dinaridi, ki jih na območju
Blegoša sestavljata Trnovski in Hrušiški pokrov. Prvi je iz karbonskih in permskih
klastitov ter bolj proti jugozahodu iz triasnih, jurskih in krednih karbonatov, drugi je
iz triasnih karbonatov. Karbonatne kamnine Trnovskega in Hrušiškega pokrova se-
stavljajo robni del Dinarske karbonatne platforme. Hrušiški pokrov oblikuje na pri-
kazanem ozemlju tektonsko polokno izpod Trnovskega pokrova, imenovano v geolo-
ško morfološkem smislu Poljansko-Vrhniško ozemlje, ki deli Trnovski pokrov na
Idrijsko-Žirovsko ozemlje na jugozahodu in Škofjeloško-Polhograjsko ozemlje na se-
verovzhodu. Notranji elementi strukture v Trnovskem in Hrušiškem pokrovu so izra-
zito dinarski, kar je značilno za smeri plasti in internih narivnih ploskev. V pokrovih
Zgradba Blegoša med Notranjimi in Zunanjimi Dinaridi_3J_9
Notranjih Dinaridov imajo strukture v splošnem alpsko smer. V kinematskem smislu
so pokrovi Zunanjih Dinaridov starejši in so narinjeni v današnjem smislu od seve-
rovzhoda proti jugozahodu. Trnovski pokrov je narinjen na eocenski fliš Vipavske do-
line, zato je zgornjeeocenske ali spodnjeoligocenske starosti. Notranji Dinaridi so na-
rinjeni od severa proti jugu na Trnovski in Hrušiški pokrov. Po zgornjemiocenskih
plasteh, ki so se v Vzhodnih Posavskih gubah nagubale v zvezi s tem narivanjem, so ti
pokrovi postmiocenske starosti. Glede na to, da se dinarsko usmerjena antiforma Po-
ljansko-Vrhniškega ozemlja naslanja na osnovno krovno narivno ploskev Notranjih
Dinaridov, ki ni nagubana, ugotavljamo, da je antiforma nastala že pred oblikova-
njem južnoalpskih pokrovov.
Generalno razmerje med alpsko in dinarsko usmerjenimi narivnimi strukturami
v zahodni Sloveniji je razvidno v vseh delih dosedanjih raziskovalcev tega ozemlja
pri Kossmatu (1913, tabla V), W i n k 1 e r j u (1923, tabla IV), Gradu in
Ferjančiču (1974, 1976), P r e m r u j u (1980) in B u s e r j u (1986, 1987a).
Vendar je le Premru določno zapisal, da mlajše alpsko usmerjene narivne enote, nari-
njene od severa proti jugu v rodanski fazi, prekrivajo starejše dinarsko usmerjene na-
rivne enote narinjene od severovzhoda proti jugozahodu v ilirsko-pirenejski fazi, če-
mur danes ne moremo oporekati.
V vseh krovnih enotah nastopa na območju Blegoša izrazita strukturna geometrij-
ska anomalija, katere središče je karbonatni masiv Blegoša v skrajnem severozaho-
dnem delu Poljansko-Vrhniškega ozemlja, torej tam, kjer se kompetentne karbonatne
kamnine Hrušiškega pokrova izpod nekompetentnih kamnin Trnovskega pokrova do-
tikajo Notranjih Dinaridov.
Pri poimenovanju krovnih enot smo uporabili izraze, ki še niso splošno sprejeti, ker
še ni enotnega mnenja o obsegu posameznih enot, razlika v pojmovanju pa pomeni
običajno tudi drugačno poimenovanje. Kamnine Slovenskega bazena zahodno od Lju-
bljanske kotline so npr. po Winklerju (1923) Julijska zunanja cona, po Gradu
in Ferjančiču (1976) Selška cona, po Premruju (1980) so vključene v Sori-
ški in Selški nariv, po B u s e r j u (1986) pa v Koblanski, Rutarski in Podmelški
pokrov. Kot zanimivost naj navedemo, da za isto enoto predlagajo Krystyn in
sodelavci (1994, 415) termin Tolminski pokrov. Krovne zgradbe Južnih Alp in No-
tranjih Dinaridov nismo razčlenjevali, ker v tem prispevku to ni potrebno. Trnovski
pokrov razumemo v smislu Mlakarja (1969, Žirovsko-Trnovski pokrov). Grada
in Ferjančiča (1974, 1976, Škofjeloško-Tmovski pokrov) in P 1 a c e r j a (1981,
Trnovski pokrov); Hrušiški pokrov v smislu Placerja (1981).
Preden nadaljujemo z regionalnimi razglabljanji naj podrobneje opišemo struktu-
ro Blegoša, ki je shematizirano podana na si. 3. Litostratigrafija je podana na si. 4.
Sam masiv gore gradi obsežna Blegoška sinklinala (B), ki strmo tone proti jugozaho-
du. Ta se proti severu tik pod osnovno krovno narivno ploskvijo Notranjih Dinaridov
previje v neznatnejšo Davško antiklinalo (D), proti jugu pa v Valovniško antiklinalo
(V), ki se izravna v Poljansko-Vrhniško ozemlje z dinarsko usmerjenimi plastmi. Osi
vseh treh gub so subparalelne, elementi vpada znašajo za Davško antiklinalo in Ble-
goško sinklinalo 235/50, za Valovniško antiklinalo 245/65. Blegoška sinklinala je iz
več lusk, imenovanih blegoške luske, ki so nagubane skupaj s plastmi. Kot med na-
rivno ploskvijo lusk in plastmi je neznaten in znaša 5°. Najnižja v skladovnici lusk je
luska 1 iz normalno ležečih plasti Psevdoziljske formacije srednjetriasne in cordevol-
ske starosti v smislu Placerja in Kolar-Jurkovškove (1990). Sledi ji
luska 2 iz normalno ležečih srednjetriasnih piroklastitov iz spodnjega dela Psevdo-
ziljske formacije, ki ležijo diskordantno na karbonsko-permskih klastitih in kamni-
320_Ladislav Placer & Jože Čar
nah Grödenske, Bellerophonske in Werfenske formacije. Nato sledijo luska 3 iz nor-
malno ležečih plasti Psevdoziljske formacije ter kamnin Rabeljske, Prehodne in
Glavnodolomitne formacije, luska 4 iz normalnih plasti zgornjega dela Rabeljske for-
macije in iz kamnin Prehodne, Glavnodolomitne in Dachsteinske formacije, na 4. lu-
sko so narinjene luska 5 iz plasti Psevdoziljske formacije in spodnjega dela Rabeljske
formacije v normalni legi, nato luska 6 iz enakih plasti v inverzni legi in končno lu-
ska 7 iz Bellerophonske in Werfenske formacije ter diskordantno odloženih lango-
bardskih piroklastitov spodnjega dela Psevdoziljske formacije v inverzni legi. Pas na-
rinjenih kamnin v dnu Podmelškega pokrova grade kamnine Psevdoziljske in Amphi-
clinske formacije, kar kaže na širšo narivno cono, ki pa strukturno še ni razčlenjena.
Notranja struktura lusk z normalno ležečimi plastmi je najlepše razvidna v luski 3,
kjer je normalna meja med pisanim zgornjim delom Rabeljskih klastitov in prehodni-
mi plastmi v severnem krilu Blegoške sinklinale odrezana s krovninsko, v južnem
krilu pa s talninsko narivno ploskvijo omenjene luske. Gre torej za lepo viden pošev-
ni rez znotraj Hrušiškega pokrova, ki je nastal v stadiju geneze krovne zgradbe Zuna-
njih Dinaridov. Izhodno formo za kinematski razvoj blegoških lusk je mogoče prika-
zati s poleglo gubo (si. 5), kjer je nazorno razvidno zaporedje nastopajočih lusk in
odnosov med luskami z normalno in inverzno lego plasti.
Druga značilnost strukture Blegoša je njena severovzhodna, vzhodna in jugovzho-
dna do južna in jugozahodna meja nasproti okolnim kamninam, ki kaže na ekstremni
dvig vzhodnega dela masiva Blegoša (si. 6). Dvig je razviden iz nagnjenosti osi gub
proti jugozahodu, kar pomeni, da gre za rotacijo prvotno subhorizontalnih nagubanih
plasti in lusk v strmo lego. Dvig vzhodnega dela Blegoša se je moral zgoditi ob že prej
obstoječih subvertikalnih prelomih različnih smeri (si. 2), ki so na si. 3 označeni s po-
sebno oznako. Gre torej za nasledstvene premike. Vzhodno od te meje se javljajo in-
verzno ležeče plasti Psevdoziljske formacije v diskordantnem odnosu s spodnjetriasni-
mi skladi, zaradi česar jih vzporejamo z enakimi plastmi luske 7 zahodno od vrha Ble-
goša. To lusko prekrivajo vzhodno od Blegoša karbonsko-permske plasti Trnovskega
pokrova. Tektonsko okno nedaleč od tod dokazuje krovni značaj Trnovskega pokrova.
Nagubana zgradba Blegoša se nadaljuje proti jugozahodu tudi v Trnovskem po-
krovu. V jedru Blegoške sinklinale je struktura Škofjega, v jedru Valovniške antikli-
nale pa tektonsko polokno iz kamnin Hrušiškega pokrova jugovzhodno od Škofjega
ob Podplečici.
Geometrijska anomalija na območju Blegoša nastopa tudi v zgradbi Notranjih Di-
naridov. Izražena je z odklonom njihove osnovne krovne narivne ploskve od smeri W-
E v smer SW-NE in z vzporednim odklonom smeri plasti. Masiv Blegoša predstavlja
potemtakem jedro kompetentnih kamnin Hrušiškega pokrova, obdano z nekompe-
tentnimi kamninami Trnovskega pokrova in Notranjih Dinaridov.
V kinematskem smislu nas seveda zanima, kakšen mehanizem je ustvaril strukturo
Blegoša. Za določitev izhodiščnih podatkov si nekoliko podrobneje oglejmo zgradbo
Poljansko-Vrhniškega ozemlja (si. 7), ki predstavlja antiklinalni svod iz kamnin Hru-
šiškega pokrova v smeri NW-SE, v katerem je antiklinalno usločena tudi narivna plo-
skev Trnovskega pokrova. Pokrov dokazujejo tektonske krpe karbonsko-permskih
klastitov sredi antiklinalnega hrbta in tektonska polokna v dolinah prečno na anti-
klinalni hrbet, kjer se karbonati Hrušiškega pokrova zajedajo globoko pod Mastite
Trnovskega pokrova. V profilu C-D na osnovni geološki karti, list Kranj (Grad &
Ferjančič, 1974), ki poteka prek Poljansko-Vrhniškega ozemlja, sicer ni narivnih
ploskev, ki bi blago sekale plasti pod kotom okoli 5°, vendar te na Blegošu obstajajo,
zato sklepamo, da niso povsod razvite ali pa niso bile kartirane. Plasti na Poljansko-
Zgradba Blegoša med Notranjimi in Zunanjimi Dinaridi_3J_9
Vrhniškem ozemlju so sicer nagubane, vendar so v generalnem smislu subhorizontal-
ne in vpadajo ponekod bolj, ponekod manj strmo proti jugozahodu v jugozahodnem
krilu in proti severovzhodu v severovzhodnem krilu.
Geometrija alpskega in dinarskega sistema krovnih narivov je razvidna na si. 8.
Razmere v okolici Blegoša so varianta te sheme (si. 9). Iz te je mogoče izpeljati seda-
njo strukturo Blegoša. Izhodno strukturo torej predstavljajo: 1. smer in vpad osnovne
krovne narivne ploskve Notranjih Dinaridov, 2. smer in vpad plasti na Poljansko-Vr-
hniškem ozemlju in 3. smer in vpad internih narivnih ploskev v tej enoti. Smer
osnovne krovne narivne ploskve Notranjih Dinaridov je mogoče določiti po geološki
karti, velikosti vpada pa se ne da izmeriti neposredno. Nasloniti se je treba na vpade
krovnih narivnih ploskev v samih Notranjih Dinaridih, ki jih posreduje B u s e r
(1987a) na geološki karti, lista Tolmin in Videm, in znašajo okoli 20°. Tako bi elemen-
ti vpada osnovne krovne narivne ploskve Notranjih Dinaridov in njegove variacije na
območju Blegoša znašali 310/20+10. Povprečni vpad plasti in internih narivnih plo-
skev na Poljansko-Vrhniškem ozemlju lahko obravnavamo skupaj, saj je razlika med
njima 5° za generalno analizo zanemarljiva. Vpadi plasti na osnovni geološki karti,
list Kranj (Grad & Ferjančič, 1974) močno nihajo, zato smo pri analizi upoš-
tevali vpade proti jugozahodu in severovzhodu do 30° in subhorizontalno lego.
Izhodišče za analizo geneze sedanje strukture Blegoša je podmena, da so se plasti
in že formirane luske znotraj Hrušiškega pokrova zaradi narivanja Notranjih Dinari-
dov od severa proti jugu najprej nagubale in nato zasukale od severa proti jugu. Os
obnarivnih gub je po teoriji presečnica med plastmi Poljansko-Vrhniškega ozemlja in
osnovno krovno narivno ploskvijo Notranjih Dinaridov, sukanje nastalih gub pa se je
zgodilo okoli osi v smeri W-E skladno z narivanjem Notranjih Dinaridov od severa
proti jugu.
Glede na naštete variante vpadov plasti obstaja več variant možnih presečnic z
osnovno krovno narivno ploskvijo Notranjih Dinaridov (si. 10). Pri vpadu osnovne
krovne narivne ploskve Notranjih Dinaridov 310/20±10 in pri variantah vpadov pla-
sti (225/0-30, 45/0-30) dobimo dve polji presečnic, ki so hkrati možne smeri osi novo-
nastalih gub (polji 1 in 2). Glede na to, da je današnja lega osi blegoških gub (V, B, D)
nastala z rotacijo presečnic okoli osi W-E, je že na prvi pogled očitno, da presečnic v
polju 1 ne moremo zarotirati v aktualno lego osi blegoških gub. To lahko opravimo le
s segmentom polja 2, in sicer med trasama rotacije a in b, ki se dotikata zunanjih mej
vplivnega polja osi blegoških gub V, B, D (polje 3). Iz oleate je razvidno, da je bil pri
izbrani varianti vpada krovne narivne ploskve 310/20±10 vpad plasti na Poljansko-
Vrhniškem ozemlju v začetni fazi narivanja Notranjih Dinaridov med 45/1 do 45/13
ali zaokroženo 45/0-15. Razlika med prvotno smerjo gub (polje 2) in sedanjo lego po-
trjuje navidezni dvig vzhodnega dela Blegoša, ki znaša po konstrukciji v profilu prek
vrha Blegoša v smeri SW-NE (si. 6) okoli 3000 m.
Poleg opisanega modela rekonstrukcije je treba omeniti še enega. Pri analizi na si.
10 smo izhajali iz primarne anomalne lege osnovne krovne narivne ploskve Notranjih
Dinaridov v smeri 220-40. Če pa upoštevamo generalno smer omenjene krovne nariv-
ne ploskve W-E (si. 9) in postavimo, da se je le-ta deformirala pozneje zaradi ovire iz
kompetentnih kamnin Poljansko-Vrhniškega ozemlja, je izhodišče kinematske anali-
ze nekoliko drugačno. Pri generalni smeri osnovne krovne narivne ploskve Notranjih
Dinaridov 360/20±10 je mogoče rekonstruirati zgradbo Blegoša pri pogoju, da vpada-
jo plasti na Poljansko-Vrhniškem ozemlju proti severovzhodu, kar je identično z re-
zultati prve analize, le da je izhodiščni vpad plasti nekoliko večji in znaša 45/8 do
45/28 ali zaokroženo 45/10-30 (si. 11).
322_Ladislav Placer & Jože Čar
Razprava
Odnos med Notranjimi in Zunanjimi Dinaridi na območju Blegoša kaže na stik
dveh različnih krovnih sistemov: 1. južnoalpskega, ki zajema Južne Alpe in Notranje
Dinaride zahodno od Ljubljanske kotline in 2. dinarskega, ki zajema Zunanje Dina-
ride. Deformacije v alpski smeri, ki nastopajo ponekod v dinarskem sistemu pod
osnovno krovno narivno ploskvijo Notranjih Dinaridov, so nastale zaradi narivanja
od severa proti jugu. To pomeni, da so dinarsko usmerjene strukture prekrite z alpsko
usmerjenimi strukturami, na kar kažejo aktualna zgradba Blegoša in gube v smeri
W-E v nekompetentnih klastičnih kamninah Trnovskega pokrova. Meja med alpskim
in dinarskim sistemom narivanja je od Ljubljanske kotline do Tolmina jasna, medtem
ko proti zahodu in vzhodu ni tako; tu so dinarske krovne enote povsem preparirane s
sekundarnimi alpskimi strukturami.
Iz naših ugotovitev izhaja, da predstavlja osnovna krovna narivna ploskev Notra-
njih Dinaridov na območju Blegoša južno mejo južnoalpskih pokrovov, ki ima globlji
strukturni pomen, saj ne gre za lokalno rotacijo manjšega bloka Zunanjih Dinaridov
nasproti Notranjim Dinaridom zahodno od Zagrebškega lineamenta, temveč za stik
dveh obsežnih enot, ki sta bili prvotno po vsej verjetnosti daleč narazen, kar je v ge-
nezi Dinaridov v dosedanjih hipotetičnih razglabljanjih premalo prisotno. Gre za sti-
čno cono, ki geometrijsko in genetsko še ni zadovoljivo rešena. Obravnavana krovna
narivna ploskev v zaledju Tržaškega zaliva predstavlja poleg osnovne krovne narivne
ploskve Južnih Alp najpomembnejšo narivno strukturo južno od Periadriatskega li-
neamenta. Ob njej je jasno izražena rotacija Zunanjih Dinaridov nasproti Notranjim
Dinaridom in Južnim Alpam za 30° do 45°.
Primerjava posameznih idej o zgradbi meje med Notranjimi in Zunanjimi Dinaridi
ni predmet tega prispevka.
Zgradba Blegoša med Notranjimi in Zunanjimi Dinaridi_3J_9
References
B u s e r, S. 1986: Tolmač listov Tolmin in Videm (Udine), Osnovna geološka karta SFRJ,
1:100.000. Zvezni geološki zavod, Beograd, pp. 103.
B u s e r, S. 1987a: Osnovna geološka karta SFRJ, Lista Tolmin in Videm (Udine) 1:100.000.
Zvezni geološki zavod, Beograd.
B u s e r, S. 1987b: Development of the Dinaric and the Julian Carbonate Platforms and of
the Intermediate Slovenian Basin (NW Yugoslavia). - Mem. Soc. Geol. It. 40, 313-320.
Grad, K. & Ferjančič, L. 1974: Osnovna geološka karta SFRJ, List Kranj, 1:100.000.
Zvezni geološki zavod, Beograd.
Grad, K. & Ferjančič, L. 1976: Tolmač lista Kranj, Osnovna geološka karta SFRJ,
1:100.000. Zvezni geološki zavod, Beograd, pp. 70.
Kazmer, M. & Kovač s, S. 1989: Ћ-iassic and Jurassic oceanic/paraoceanic belts in the
Carpathian-Pannonian Region and its surroundings. Tectonic Evolution of the Tethyan Region,
NATO ASI Series, Springer - Verlag, 77-92.
K o s s m a t, F. 1910: Erläuterungen zur geologischen Karte Bischoflack und Idria. - Geol. Ra.,
Wien, pp. 101.
K o s s m a t, F. 1913: Die adriatische Umrandung in der alpinen Faltenregion. - Mitt. Geol.
Ges. 6, 61-165, Wien.
K r y s t y n. L., Lein, R., Schlaf, J. & Bauer, F. 1994: Über ein neues obertria-
disch-jurassisches Intraplattformbecken in den Südkarawanken. - Jubiläumschrift 20 Jahre
Geol. Zusammenarbeit Òster. - Ung. 2, 409-416, Wien.
Mlakar, L 1969: Krovna zgradba Idrijsko-Žirovskega ozemlja. - Geologija 12, 5-72, Ljub-
ljana.
Placer, L. 1981: Tektonska zgradba jugozahodne Slovenije. - Geologija 24, 27-60, Ljub-
ljana.
Placer, L. & Kolar-Jurkovšek, T. 1990: O starosti psevdoziljskih skladov v vzho-
dnih Posavskih gubah. - Rud.-met. zbornik 37/4, Ljubljana.
P r e m r u, U. 1980: Geološka zgradba osrednje Slovenije. - Geologija 23/2, 226-273, Ljub-
ljana.
Ravnik, D., R a j v e r. D., Poljak, M. & Ž i v č i d, M. 1995: Overview of the geo-
thermal field of Slovenia in the area between the Alps, the Dinarides and the Pannonian basin.
- Tectonophysics 250, 135-149.
Winkler, A. 1923: Ueber den Bau der östlichen Südalpen. - Mitt. Geol. Ges. 16, 1-272,
Wien.