GEOL. CROAT. 50/1 57·77 7 Figs. 6 Pis. ZAG REB 1997 

Tectonic Structure of the Island of Hvar (Southern Croatia) 

Stanko MARINCIC 

Key words: Kinematics of de formation, Tectonic pha­
ses, Is land of Hvar, Croat ia. 

Abstract 
SlruclUml dcfonnalion of Ihe island of Hvar allows three tangen­

tial tectonic phases to be determined: the Laramian (F I), the Pyre­
llC,Ul ( fo II) alld the Neotectonic phase (F 111 ) . Preserved relic s of 
Laramian and Pyrenean fold s with intact structura l clements, indi ­
cates tilal the Neotectonic orientat ion of st ruCllI rcs (E- \V) i ~ a conse­
quence of refolding of the older structural fabric, rather than horizon­
[;Ii rotatioll. 

1. INTRODUCTION 

Geological development of the is land o r Hvar [rom 
the Ncocomian to the Eocene-Oli gocene (Fi g. 1) indi­
cates severa l phases of tec ton ically induccd changes. 
Emersion of Apt ian and Albian deposits is a regionally 
widespread example of such tendencies, but the cause is 
indcterminaled. At the end of the Upper Cretaceous, 
during a relatively shon interrupti on in platform car­
bonate deposi tion, more important struc tura l deforma­
tion occurred. These were altributed to the so-cal led 
Laramian tec tonic phase. Similarly, the ef fects of the 
Lute tian -Oligoeene Py renean tangenti al phase, as wcll 
as the effects of the Neogene-Quate rnary Neotecton ic 
tangential phase were determined. 

This nomenclature has been kept because of its his­
torical establi shmcn l in Ihe Croatian geological litera­
ture. The Laramian phase, as the oldest tecton ic defor­
mation, will be referred to as F J, the Pyrenean phase as 
F II , and the youngest Neotectoni c phase as P ITI. 

2. KINEMATICS OF DEFORMATIO N AND 
TECTONIC PHASES 

T he 1110s t obvious influences of the tangentia l tec­
Ion ic phase on the sedimentary sys tem arc expressed by 
shorter or longer periods of non-deposition during the 
e ll1c rs ion phases, or by essen tial changes reco rded in 
the la rge sedimenta ry systems (e.g. succession from 
platform carbonates to fly sch to molasse) . Such phases 

Institu te of Geology, Sac hsov a 2, P.O. Box 268, IIR 10000 Zag reb, 
Croat ia 

Kljucnc rijeCi: kinematika deformacija, tektonske faze, 
otok Hvar, Hrva tska. 

Sazctak 
Na temelj u svojstava struklurn ih dc formacija oloka Hvara dCler­

minirane Sll tri lange ncijalne lek ions kc I;\zc: laramijska, pircnejska i 
nco lektonska faza koj c su uvj el rlo Olllace ne bo F I, r II 1 F ill. 
Sacuvani rclikti lararnij skih i pircncjskih bora s inlaklnim stru ktu rnirn 
ele rnentima, ukazuju da ncotcktonska orijenlacija struklUra Is lo k­
zapad nije posljedica horizontalnc rotacije vee prcborav<Ulja starijeg 
struklUTllog sklopa. 

were recorded as event s during certain periods of the 
geological time. However, it is incorrec t to undoubtedly 
connect each sed iment ary gap with tecton ics, until a 
clear tectonic cause has been determined. Without sllch 
c lear tec tonic evidence sedim entolog ical changes 
should be regarded on the levcl o f recogni tion of the 
characterist ic facies. 

Under the tangen tia l st ress, as a result of the kine­
matic cond itions, the longer axis (b-axi s) o j' the de for­
mati ona l fabri c is o riented normal to the stress. There­
fore, the b-axis of the fo ld , as a product o r optim al 
deformation, is also ori ented normal to the stress. Com­
plete fold geometry , includin g a ll deformati onal se ts 
(limbs, amplitude, span, index, b-ax is, vergence, joint 
se ts, e tc.) represents the k inematic record of' a g iven 
stress oricntation. In practice, under stress o r any orien­
tation , the development or the dcformation will result in 
stepwise changes, which cou ld be defined as ki nematic 
stages. From this point or view, kinematic stages reprc­
sen I a genera l paradi gm, which will be explained using 
the example of the Neotectonic st ructural fabric of the 
island of H va l'. 

A very important ractor for each geologica l body is 
it s spatia l position during the geologica l processes. 
Consequent ly, the most important factor fo r its defor­
mational rab ric is its s tructural orientation. Both aspects 
are controlled by geological time. Therefore, the prima­
ry deformations direc tl y indicale the orientation of lhe 
reg iona l s tress during the spec ifi c tangential tec tonic 
phase. 

The illCiuence of Ihe Laramiall tec tonic phase (F I) is 
indi catcd by lhe emersion at the end of the Upper Creta­
ceous, and sporadic relics of metre- to decamet re-scale 
fo lds. These rolds with a N-S b-axis st rike, and corre­
sponding join! se ts, could have been formed only under 



58 

I I 
I I I I I I 

I I 

f I 

1 
~ 

I 

[J 

Cd 

[J 
0 
~ 

~ 
~ 

0 
~ 
0 

- z-== 

Geologia Croalic.1 50/1 

Fig. 1 Schematic geological map of the island of 
Hvar. Legend: I - Malmian deposits (simplified); 
2 - Ncocomian platform deposits (dolomites with 
micrite lenses); 3 - Barremian-Aptian platform 
carbonates (rhythmic alternaliotl of micrites and 
bioclastic limestones with dasyc!adaceans); 4 -
Albian-Cenomanian plat form carbonalcs (cryptal­
gal laminites and lale-diagenetic dolomites); 5 -
Cenomanian platform carbonates (cryptulgaJ 
limestones containing fossil fish and reptiles, rud­
isl biostromes); 6 - Turonian-Santonian platform 
carbonates (micriles, oncoidal, crypt algal and 
rudist limestones); Campanian-Maastrichtian 
platform carbonates (homogenous micrites) ; 8 -
Palaeogene flysch; 9 - reverse fault; 10 - slrike­
slip fault. 

S1. I Pregledna geoloska karla otoka Hvara. Tumuc: 
I - malmske naslage (pretpostuvljeno); 2 
neokomski platformni karbonali (dolomili s 
lecama mikritnog vapnenca); 3 - barcm-aptski 
platfonnni karbonati (ritmicka izmjena mikrilnih 
i biok laSlicnih vapnenaca S dazikladacejama) ; 4-
albsko-ccnomanski platformni karbonati (kriptal­
galni vapncnci i kasnodijagcnclski dolomiti); 5 -
cCllomanski platformni karbonati (kriptalgalni 
vapnenci s fosilnim ribama i gmazovima, rudistnc 
biostrome): 6 - !uron-santOllski pla!forrnni kar­
bona!i (mikritni, onkoidni, kriptalgalni i ruciistni 
vapnellci); 7 - kampan-mastrihtski platformni 
karbonati (ho111ogcni mikritlli vapncnci): 8 - pa le­
ogenski nis; 9 - reverzni rasjcd (celo Ijuskc); 10-
rasjed s horizontalnirn krclunjem. 



Marinbc: Tectonic Stnlct ure of the 1~land of 1-1 var (Sou thern Croatia) 

Pig. 2 Neotectonic compression (F III) reactivating first generation of 
hOI joints of the Pyrencan phase (F II ) into tensional joints and 
axial plane joints. 

SI. 2 Ncotektollska komprcsija (F][[ ) reaktivira prvu generaciju hOI 
pllkotina pi rcncjske faze (FI! ) II tcnzijske pukotine i pllkotinc 
os nc ravnine. 

the influence of the E-W oriented regional stress, i.e . 
during the Laramian tectonic phase. 

Relics of the Laramian folds preserved their recog­
ni zable geometries although they were refolded during 
late r Pyrenean and Neotectonic phases. They were 
incorporated in the limbs of the Neotectonic folds, 
changing only the inclination of their B-axis (traces of 
the axial planes of the Laramian folds are parallel to the 
"a-lineations" in the limbs of the Neotectonic folds). 

Under the influence of the Pyrenean tangential tec­
tonic phase duri ng the Middle Eocene, a trough filled 
with fly sc h was formed within the former carbonate 
platform (MARINCIC, 1981). This even t marked the 
commencement of the disintegration of the former 
Mesozoic carbonate platform. Syntectonic sedimenta­
tion of the Eoce ne-Oli gocene flysch deposits was, 
under the influ ence of the SW-NE oriented Pyrenean 
stress, accompanied by the subduction of the Adriatic 
platform beneath the Dinarides. The Dinarides were 
folded , forming the famous structural phenomena, 
known as "t he Dinaric st rike" or " the Dinaric struc ­
tures". These structures are characterized by their NW­
SE st rike and SW vergence. 

On the island of Hvar, Pyrenean folds are only spo­
radically preservcd. Due to their origi nally diagonal ori­
entat ion (Fig. 2) they were unable to provide st rong 
resistancc to the neotectonic stress. Therefore, the only 
preserved part s of thc Pyrcnean folds are those which 
were in a favourable position to bccome incorporated 
into the limbs of thc Neotcctonic folds. These Pyrenean 
folds have only changcd the original inclination of their 
b-axis; they also sporadically preserved their Pyrenean 
SW vergence. The Neotectonic stress effici ently accept ­
ed each Pyrenean fracture which could have been ineor­
poratcd into its own deformational set. The left sliding 
joints of the first Pyrenean hOI generation joint sets 
formcd joints of the axial plane, and the right oncs for­
med tensional joints of tile Neotectonic fold s (Fig. 2). 

Although the re lics of Laramian and Pyrenean folds 
are not so frequent as thc predominant Neotectonic 

L 23055 L 25878 Sis (til 

-:-

~FI 

Fig. 3 Synoptic ~-diagram of the isl,Uld of HvaL 

SI. 3 Sinopti6ki ~-dijagram otoka Hvara. 

tI F III 

59 

folds, their presence is very important (Fig. 3). Under 
the influence of the Neotectonic stress they have only 
changed the inclination of thei r b-axis, but they pre­
served the original orientation. Therefore, their mutual 
arrangement is rather we!! preserved (Fig. 4). It must be 
noted that their original st ructural fabric was only 
refolded during the activity of the Neotectonic stress 
oriented N-S . Therefore, it was not hori zo ntally 
"counter-clockwise rotatcd" around the tectonic c-axis, 
which has recently become the usual explanation for 
each occurrence of " the Hvar strike" in the Dinarides 
(e.g. ALJINOVIC et aI., 1990). Only a rootless nappe 
could horizontally rotate, and the Hvar thrust-sheet or 
thrust-sheets are definitely not examples of these root­
less structures. Some locally observed horizontal rota­
tions along the strike-slip faults (hOI) arc of the outcrop­
scale. Even the remarkable sum of the ir differential left 
movements cannot contribute to the predominance of 
one direction over the other (i.e. rotation), since it is 
compensated by movements along the right strike-slip 
faults. Besides, these movements are inc luded into the 
deformations of the kinematic F-stage (the fourth hOl 
generation), which took place after th e formation of 
"the Hvar strike". Finally, at the frontal surfaces of the 
thrust -sheet s with south vcrgence all tectog lyphs are 
oriented perpendicularly - they are not oblique, neither 
do they generally indicate any aberra tion from thc 
North-South direct ion. 

With the appearance of a new global stress oriented 
North-South, a new Neogene-Quaternary Neotecton ic 
tangential phase (F III) began. Intens ified subduction 
continued, resulting in the di sintegration of the Adriatic 
Carbonate Platform in several parts (ALJINOVIC ct aI., 
1987). At the same tim e in the area of the Dinarides 
structural deformations of East-West strike ("the Hvar 
strike") and South vergence were formed. 

The specific gcological development and geotecto­
nic position of SW Istria and the islands of Lastovo and 
probably Vis , indicate that they represent rclics of the 
Adriatic Carbonate Platform. Therefore, the island of 



60 Geologia Croatica 5011 

SFI 

SF III 

Fig. 4 Relics of Laramian (F I) and Pyrenean (F II ) folds in limbs of the Neotecton ic fold (F III ) near Vrboska. 

SI. 4 Rclikli laramijskih (F I) i pircllcjskill ( F II) bora II krill! ncotcklOllske bore (F III ); Vrboska. 

Hvar represents a considerably protruded part of the 
great structural complex of the Dinaridcs in the vicinity 
of the Neotecton ic subduction zone. Consequently, it 
underwent st ronger contrac tion, whi ch resulted in 
remarkable defo rmation dur ing the Neotectonic tangen­
tial tectonic phase. 

Althou gh the direction of the stress is of primary 
importance for the determination of the tectonic phase 
and understanding of the geological developmen t of a 
certain area, it is not so substantial from the kinematic 
point of view. The idea l kinematic sequence of defor­
malion is iden tical under any stress orientation. There­
fore, the Neotectonic deformation of the island of Hvar 
cou ld be treated as a gene ral example. Kinematic 
changes are designated as six stages of kinematic devel­
opment: A, E, C, D, E and F (Fig. 5). They are defined 
on the criter ia of the succes sive appearance of the 
important tangential deformational sets. 

The first reaction to compress ion is expressed by a 
tension parallel to the pl ane of the greates t and the 
inte rmediate princi pal s tress ( 0"1 - 0"2)' resulting in the 
opening of tensional gaping joints of the A-stage. These 
joint s arc small (centimetre to decimetre scal e), and 
usually they do not cut the entire thickness of a bed. 

They arc velY expressive due to their feather-like shape 
filled with white sparitic calcite. They are present only 
in the parts of the 0" 1 - 0"2 plane with the minimal diffe r­
ence be tween resistance and tangential pressure (in 
li mestones approximately 38° towards the direction of 
the main stress). 

During stage B the hOI zone was torn , with charac­
teristic sliding along the conjugated hOI joint sets (the 
first hOI generation). Joints are of the cen time ter to 
metre scale, usua lly cutting through the entire bcd, but 
they do not disturb other beds, since they terminate at 
the interbed djsconlinuity. Their dimensions are con­
trolled by the thickness of the bed, and, therefore, they 
cannot evolve into faults. Commonly they arc charac­
terised by small-scale left or right movements with 
small teetoglyphs parallel to the bedding. These small· 
scale movements also interrupt tensional joints of the A 
stage, which preceded them. U nfortunately, this 
desc ribed succession of events is often misinterpreted; 
as tensional joints are interpreted as bei ng of secondary 
origin (as a consequence of moving along the sliding 
hOljoints). 

The A and B stages represent a period of compensa­
tion of lhe main stress on the level of a single bed. The 

Fig. 5 Kincmatic stages of 
deformation development 
in the exmnple o f Neotec ­
tonic compressio n. 

SI. 5 Kinematski stadiji raz­
voja deformacija na prim­
jeru neotcktonske kompre­
sije (F III), 



MarinCic: Tecton ic Slnlcture of the Island or ]-]\'3T (Southern Cro;llia) 

.. :0C:.~'. 
r ig. 6 lrllcgration of thrust-sheets into a kinematicall y morc res i.~ tant 

larger thrust-shee t. 

$ 1. 6 I ntegrir~l!ljc Ijusaka II k incmatski otporniju vecu tj usku. 

continu atio n of stress leads to the substitut ion or the 
already ex hausled smail-scale resistance wit h a group 
o f beds. From thi s stage on, the res isting complex is 
striving fo r homogenization, which in th is way leads to 
the large-sca le deformation s. Durin g the res istance to 
the material di sintegration , a homogeneous group of 
beds is fac in g by it s wide r front toward s the main 
stress . This leads to the redistributi on or the int ermedi ­
at e and the least principle stress (a2 and a j ), resulting 
with the most e ffici ent consequence: bending of beds 
and folding. The folding is accom panied by the addi ­
ti onal compensation or stress in the form of re lease 
along the compression cleavage of the axial plane. 

The C stage is characteriscd by the comple te change 
o f geo logical rc la ti ons, since the most im portant con ­
tractional change resulted in tectonic transport paralle l 
with the least principal stress - (J3' Sedim entation 
ceased o r is cOlltinued under di fferent cond itio ns a t a 
different locatioll. During stage C of the Laramian t ec~ 

IOnic phase wide areas were uplifted and emerged (not 
onl y the area of the former carbonate platform ), whil e 
durin g the C stage of the Pyrenean pha se there was a 
shift from the shallow-water carbonate sedimentation to 
the deposition of flysch. The same kinematic stage dur­
ing the Neotectonic phase resulted in the final orogeny. 

Advancing deformation leads to the increase of the 
fo ld compression index, and a hi gher inclination o f the 
charac teris ti c southern verge nce of the Neotec tonic 
contracti on. The only remaining resistance to the main 
stress is re presented by the ductilit y of the fo ld mate­
rial. Overcoming the ducti li ty during the stage D leads 
to the re leas ing or [o lds, and their breaki ng alo ng the 
zone o f the least difference between the resistance and 
the tangential stress . Thi s zone is represented by the 
sliding set of the second hOI generation. In concordance 
with the large structural form s, kilometer-scale hOI sets 
of reverse fault s with perpendicular (N-S) cicci metre to 
metre-scale tectoglyphs, were formed. The most impre­
ssive consequence of the Neotectonic contracti on of the 
is land of I-I var was the formation of the thrust-shccts 
from the fo rmer fold s, wit h southern vergence (" the 
Hvar st ri ke") . 

6 1 

T hrust-s heets, instead of "the s ing le island thrust­
sheet" as usually quoted in the lite rature, therefore rep­
resent the structural essence of the island of Hvar. So 
far established opi nions on only one thrust-sheet were 
probabl y based on a very remarkable contact of the 
front or the southernmost thrust-sheet with fl ysch , and 
the apparently continuous succession between the core 
and the younger deposits. However, it should be noted 
that the flysch represents only the youngest deposi ts in 
the succession, not a continuous surface used for thrust­
shcet motion. By the nature or deformat ion of the wider 
structural fabric, it is only possible to conclude that this 
southernmost thrust-sheet represent s the first, i.e. the 
oldes t thrust-sheet structure. Towards the North succes­
sivel y younger thrust-sheets of the Neotectonic stage D 
could be found. Moreover, opinions on only one thrust­
sheet structu re imply that stage C consisted of a single, 
huge rold , which had reworked the entire o lder Pyre­
nean structural fabric (also supposed to be composed of 
a single, huge fold ). Existing re lics of older, Pre-Neo­
tecto nic fold s , indicate that thi s was definite ly not the 
case. The Neotectonic stage C fOfmed so many en eche­
lon fold s because it first re fo lded Ihe maj ority of the 
older structures, and then included them into the thrust­
sheet stru ct ures . The cau se for th e apparent integral 
core of the island (or apparent sin gle is land thrust­
sheet) could probably have been a very persistent and 
strong Neotectonic compress ion , resulting in contrac­
ti on or folds and formatio n of th rust-sheets, as well as 
in the in tegration of tectonically reduced corcs into the 
new, secondary core, and reduced frontal paris of folds 
int o the new, secondary front ( Fig. 6). T he k inemat ic 
succession from one stage to the other, therefore. repre­
sents substilUl ion of already "consumed" structural 
form s with the more resistant ones. Successively, "COI1 -

sumed" elements were integrated int o a large res istant 
st ructure, act ing like a sin gle thrust-sheet in contact 
with flysch. 

The kinematic stage E represents an e ven more 
character istic fcature of th e is land of Hvar than it s 
strike. Although the loca l occurrences of the defonna­
tions of this stage were found a ll over the Dinarides , on 
the island of I-I var they are an inevitable feature of the 
complete Neotectonic structural fabric, down to outcrop 
level. T hese deformation s are partl y the result of the 
specific regional geotectonic position of the island (as a 
protruded segment of the Neotectonic overthrusting of 
the Dinarides on the Adria ti c pl atform ), but they are 
also a consequence of the inLe rna l structural fabric of 
the island of Hvar. Nu merous reduced thrus t-sheets, 
composing the apparent integral structure of the island , 
have under the inten sified strain begun to respond 
autonomously to the stress. Each thrust-sheet, from the 
smallest to the largest , was released alo ng the new 
deformationa l se t of hOI joint s and fau lt s of the kine­
mati c stage E. This third ge nerati on o f hOi reverse 
faulls, together with earlier ha l reverse rault s of stage 
D, formed a conjugated hOI se t. Thi s res ult ed in the 
conjugation of thrust-sheets of all scales, and complete 



62 

1 

2 

D 

Fi g. 7 The sequence of deformation from conlraction (I) to extension 
(2) and grav itati ona l joints (3). 

SI. 7 Slijed dcfonn inmja ad kOl1trakcijc (I.) do ckstcnzije (2.) i grav­
itacijskih hOI pukolinn (3.). 

conjugation of the integrated thrust-sheet of the is land 
of Hvar. Towards the south fold s and thrust-sheets are 
of southern vergence, and towards the north they are of 
the northern verge nce. The tangential stress was con­
sumed in both directions of the reverse movements, in 
this way increasing the tcctonical tran sport along the 
ax is of the leas t principle s tress (cr, ). Hinges of the 
st ructures were in the pos ition of the decreased lateral 
pressure, resulting with the opening of the older dis­
junctive se ts of the A. Band C stages. 

The kinemat ic stage F comprises the youngest set of 
the Neotecton ic tangent ial deformations on the island of 
HvaI'. The global s tress already overcame the resistance 
of the fo lds and thrust-sheets as deformation of stage E 
procecded. In this way, stage F could be compared with 
slage B, bu t of a higher de fomlational level: it is char­
acte rised by the reac ti vation of the stage B li rst genera­
tion of hOI fault se ts. The F stage represents, therefore, 
the fourth hOI generation, characterised by the intensive 
hori zonta l movements along the left and right s trike­
slip faults, usually c lltting all parts of the Hvar structur­
al fabric (Fig. 1). It comprises large-scale faults with 
limoniti zcd surfaces and dccimetre-scale subhorizontal 
teetoglyphs. 

In a complex structural fabric , like that of the island 
of Hvar, kinematic stages follow each 0 1 her according 
to the struc tural maturity of each st ru ctural segment. 
Therefore, duc to the progression of the Neotectonic 
s tress toward s the south, each zone is practically in a 
different kinematic stage at the salllC time. 

Geologia Cro:uicn 50/1 

The question of the inlluencc of extensional phases 
and extension was omitted in the above analys is. Their 
inllucnce is much more predic table than that o r contrac­
tional phases, becausc they certainly follow after each 
contractional phase. 

Folded deposits , when exempt from the tangential 
s tress and stimulated by the reg ional widening. aimed 
to rees tablish their primary form due to thei r preserved 
elasticity. However, soon they exceed their c lasticity 
limit, resu lting in the formation of the extensiona l joints 
in the zone of the b-axis. S ince tangential stress was 
subsequent ly completely substituted by the gravita tion­
a l force , ex tensional joints in the zone of the b-axis 
were reac tivated into the gravitational hOi set of conju­
gated s lid ing joints (Fig. 7). Along these jo int se ts 
ant iforllls ascended and synforllls descended, similar to 
the isostatic movements. 

Without this cyclic succession of the tangent ia l and 
rad ial tecton ic movements, the reestablishment of sedi ­
mentation at the same locality would not be possible. 
During the exte nsion al phase the upliftcd mountain 
ranges were Oattcned, and the erosion was lowercd 
enough for depos ition to become reestablished. Thus, 
on the island of Hvar the Aptian emergence was suc­
ceeded by the Upper Albian immersion, the A lbian 
emergence by the Cenomanian immersion, etc. 

The nex t tangent ial phase appeared only when the 
velocity of the horizontal movement of the African 
plate increased enough to dominate the rotational ve loc­
ity. Along a new vector of tota l movement a new com­
press ion of the global s tress was generated, be ing 
recogn ised as the new tectonic tangential phase. 

3. REFERENCES 

ALJJNOY IC, B. , PRELOGOYIC, E. & SKOKO, D. 
( 1987) : Novi podae i 0 dubinsko-geolos koj gradi i 
se izmotektonski aktivnim zonama u Jugoslaviji.­
Geol. vjesnik, 40, 255-263. 

ALJINOYIC, B., PR ELOGOY IC, E. & SKOKO, D. 
( 1990): Tectonic processes and the contac t of the 
Adria tic platform and Dinarides in the area of thc 
northern Dalm atia. - Proc. of the Int. Cont". on 
mechanics of jointed and faulted rocks, 179- 182, 
A.A. Balkema, Rotherdam-Brookfield. 

MARINCIC, S. (1981): Eoeenski f1is Jadranskog 
pojasa.- Geol. vjesnik, 34, 27-38. 



MarinciC: I'eclonic SlruClUre of the Island of Hvar (Soulhern Croal;a) 63 

Tektonska struktura otoka Hvara 

Stanko MARINCIC 

1. UVOD 

Razvoj gcolosk ih naslaga otoka I-Ivara, od neokoma do 
cocen-oligocena (SI. 1), svjedoe i daje ovo podrueje II vise 
navrata prctrpjclo promjenc izazvanc tektonskim pokreti­
ma. Dobro su npr. izrazene cmerzijc aptskih i albskih 
naslaga s lieno kao i si rom krskih Dinarida, ali ni u jed nom 
ni u drugolll s lucaju ove pojave nisu i spccifieki detcrmini­
rane. Za sada nisu prcpoznali bilo kakvi rclevanlni pokaza­
telji 0 lipu slrllkwrnih deformacija prema kojillli.t bi se 
Illoglo zak ljueiti 0 tcktonskoj naravi ov ih emerzija i nji­
hovoj uzrocnoj vezi s odredenilll tektonskim fazama. Tek 
su na kraju gornje krcde, za rclativno kratkotrajnog preki­
da sedilllcnlaeije platformnih karbonala, u dovoljnoj mjeri 
izrazenc strukturnc dcfonnacije svojstvcne Izv. laramijskoj 
tangencijalnoj tektonskoj Fazio Analogn im je postupkom 
jos dClerminiran ucinak djclovanja lutct-oligocenske tzv. 
pircnej skc tangencijalnc faze i neogensko-kvartarne 
ncolektonskc tangencijalnc faze. 

Ovakvo nazivlje tcktonskih faza je zadrzano zbog nji ­
hove pov ijcsnc ukorjcnjcnosti i prcpoznatljivosti u nasoj 
geoloskoj literaturi, pa i zalo sto ne postoji ncko drugo. 
I311duci cia SLl najstariji definirani tektonski pokreti ovog 
podrLlcja laramijski , oni su Llvjelno oznaccni kao prva Ick­
lonska faza - F I , pirenejska kao F II i neotektonska faza 
kaoFtlL 

2. KINEMATIKA DEFORMIRANJA I 
TEKTONSKE FAZE 

Najuocljivija posljedica djelovanja tangcncijalne tek­
tonske faze na sedimentacijsk i s ustav je duzi iIi kraci 
prekid scelimenlacije (emerzija) iIi pak, bitnc izmjcne 
velikih taloznih sustava (plalformni karbonati - flii; -
molasa). Po lome se zapazaju kao dogadaji u odredenom 
geo loskom vrcmcnu. Mecllltim, ne moze sc bas za svaki 
prekid Ll sedimentac iji a priori tvreliti da je izazvan tekto­
nikom dok sc ne clokazLl tektonski iIi ini uzroci. Bez 
u[vrdenih uzroka, scdimentacijskc promjcne os tajll samo 
na rangll konstatac ije prepoznatog facijesa. 

Pod tangcncijalnim stresom, silom kinematskih uvjeta 
duza os (b-os) defonnacijskog sklopa je u polozaju nor­
male na sIres. Takoder i bora, kao optimaln a referentna 
deformacija sklopa, ima B-os normalnll na strcs. Sva 
gcolllct rija bore i svi pripadajllci joj deformacijski sllsiavi 
(krila, amplituda, raspon , indeks, 8-os, vergeneija , pllko­
tine itd.) kincmatski Sll iskazi orijen l iranog slresa. 
Praklicki , pod stresom bilo kojc orijcntacije, deformiranje 
napreduje iclenticnirn kinematskim tijekom koji se manifc­
stira 11 kinematskim skokovima kao rang stanja eleforma­
cije iii kinematski stadij. U toj su mjeri kinematski stadiji 
opci obrazac koji ce se poblize obrazloziti na primjcru 
ncotcktonskog slrllktllrnog sklopa otoka I-Ivara. 

Koliko je za neko geolosko tijelo od prcsudne vaznosti 
prostorna lokacija , loliko je za njegov deronnacijski sklop 

prostorna orijcntacija. Dakako, oba su aspekla konlrolirana 
geo loskim vremcnom i bas zbog toga ce autenticne pri­
marne eleformaeije ncposredno svjedocili 0 pravcu regio­
nalnog stresa kao 0 prcpoznat ljivoj tangencijalnoj tekton­
skoj razi. 

Prislllnost uCinka laramijske fazc - F I, osim cmerzije 
konccm gornje krede, indiciraju mjcstimicni relikti rela­
tivno velikih, metarskih do dekametarskih bora. Qve bore 
s B-osima pruzanja sjever-jug i korcspondirajucim 
pllkotinskim sListavima, mogle su nastati sarno pod djclo­
vanjem regionalnog tangencijalnog strcsa na pravcu istok­
zapad, elakle, u la ramijskoj teklonskoj fazi. Ostaci lm'ami­
jskih bora sacuvali Sll prcpoznatljivu gcometri ju na taj 
nacin sto im je i pirenejska i neotektonska faza prcborala 
B-osi. Promjenom nagiba osi sacuvali Sll sc oni dijelovi 
laramijskih bora koji su kinemalski ugradeni II konstitLlcijll 
kri la dominantnih neotektonskih bora (trase osnih ravnina 
laramijskih bora paralclne su s neotcktonskim "a-lincaci­
jama" krila). 

Pod djelovanjem pirenejskc tangeneijalnc tcktonskc 
faze (F II ) II karbonatnoj se platformi Ll srednjem eocenll 
formira flisko korito i pocinje talozenje flisa (MARINCJC, 
1981). Ovom fazom pocinje dczintegracija mczozojske 
karbonatnc platfonne. Sinlektonsku scclimcntac iju eoccn­
oligocenskog flisa pod djelovanjem pirenejskog stresa na 
pravcLl jugozapad-sjeveroistok prati podvlaccnje Jadranskc 
platforme poel Dinaride. Dinaridi sc boraju tvoreei poznate 
struktllrne fenomcnc obuhvacene pojmovima "dinaridsko 
pruzanje", "dinaridskc struklllre" (pruzanja sjeverozapad­
jugoistok) s karakteristicnim jugozapadnim vcrgencijama. 

Pircnejske Sll bore na podrLlcju !-Ivara samo mje­
stimicno sacuvanc. Zbog izvorno dijagonalnog polozaja 
prema neotektonskom stresu njihove strllklurne geometrije 
nisu ni moglc pruziti maksimalni otpor (SI. 2). Sacuvani su 
tek oni dijelovi pircncjskih bora koji SLl bili u kinc­
malskom polozaju da postanu konstitlltivni clement kr ila 
veee ncotcktonskc bore. U tim Sll slucajcvima zadrzale i 
pirenejsku jugozapadnu vergcnciju. Dapace, neotektonski 
jc sIres ekonomicno koristio svaku zatecenLl pircnejskll 
pllkot inLl koja sc mogla ugraditi u njegov dcformacijski 
Slls tav. Promijcnila sc samo kinematska fllnkcija starijih 
pllkotina. Obicno lijeve smicne pukotine konjugiranih 
parova prvc pircncjske hOI generacije poprimaju fllnkciju 
pukotina osne ravnine, a desne postajll tenzijskc pllkotine 
neotektonskih bora (SI. 2). 

Relativno mali broj utvrdcnih relikata laramijskih i 
pirenejskih bora U odnosu na dominantne neotektonske 
bore (SI. 3), ne umanjllje principijclno znacenje njihove 
prisutnosli. Pod neotektonskim su strcsom promijenile 
salllo nagib 8-osi, ali su zadrzale osnovnu orijcntaciju, pa 
prema tome i medusobno bitno ncporcmeeene polozajc 
(SI. 4). Zato je pOlrcbno islaknllti da je zateceni strukturni 
prcdcrtcz pod djelovanjem neotcktonskog slresa (sjcvcr­
jug) prcboran, a nc horizonwlno "retrogradno rot iran" oko 
ncotcktonskc c-osi, kao slO se danas pokLlsava tlllllaciti 
svaka pojava "hvarskog pruzanja" II Dinaridima (uspore­
eliti: ALJINOVIC et aL, (990). Uostalom , koji bi to stru-



64 

kturni sklap mogao horizontal no rotirati osim navlakc 
odvoje nc ad korijcna? Hvarska ljuska iii Ijuskc, nisu u toj 
siluaciji. EvcIl tualnc lokalne horizontainc rotacijc duz 
transkurcntnih (hOI) rasjeda su pojavc na razini izdanka. 
N i velika SllIn<l njihovih difcrcncijaln ih lijcvih krctanja nc 
doprinosi prcvagi j cdnog smjcra pomaka (rotaciji) jer ih za 
slican iznos kompenziraju pomaci duz desnih transkurcnl­
nih rasjcda. Osim toga, ova krctanja spadaju u dcronnacijc 
kincmatskog F-stadija (celvrta hOI generacija) koji je llslje­
dio nakon formiranja "hvarskog pruzanja". Na konell, na 
plohama ce la Ijusaka juznih ycrgcncija svi su tcktoglifi 
ugradeni perpendiklliarno - niti su zakrivljeni, niti sumarno 
pokazLiju odstupanje od pravea sjever-jug. 

Pojavom novog smjera g lobalnog slresa na pravcu 
sjevcr-jug, artikulira se neoge nsko-kvartarna neotcktonska 
tangeneijalna fa za (F III). Podvlaccnje se naslavlja i inten­
zivira, pa se i sama Jadranska karbonatna pial forma dezin­
tegrira na nekoliko scgmenala (ALJ INOVIC ct aI., 1987), 
dok sc u Dinaridima pojavljLljLl strukturne deformacijc 
pruzanja iSlok -zapad ("hvarsko pruzanje") s juznim ver­
gene ijama. 

Specifieni geoloski razvoj i gcolektonski po 1 oz.aj 
jugozapadnc ISlre, otoka Lastova i, vjcrojalno, Visa, 
ukazujLl da su oni re likli Jadranske karbonalne platformc. 
Otok Hvar je, prema tome, diD vrlo isturenog navlacnog 
ozemlja vel ike slrukturnc elaze Dinarida blizu zone 
neo\ck\ol1skog podvlaeenja. U toj je mjcri prctrpio i jaeu 
kontrakciju koja se odrazila u bogalom sadrzajll slrll ­
ktLlrnih dcf"orlllacija neolektonske tangcnc ijalne faze. 

Mada je pravac djclovanja stresa od presudne vaznosti 
za razllmijevanje geoloskog razvoja [lekog podrueja, s 
kinclllatskog je aspekla od sekundamog znacaja. Idealni 

(polpuni ) kinematski slijed napredovanja deformacija je 
identican LI bilo kojoj orijentaeiji stresa pa i u neotckton­
skolll primjeru Hvara ima vrijednosti opeeg obrase<.t. 
Promjene su llvjclno oznaccnc kao A, B, C, D, E, F - stadi ­
ji kincmatskog razvoja, deriniranog prema kriteriju progre­
sijc pojavljivanja bilnih tangeneijalnih defonnaeijskih sus­
(a va (Sl. 5). 

Prva reakcija na komprcsiju j e tenzija koja paralelno s 
ravninom g lavnog i srednjeg slresa (0 1 - O2) otvara tcnzi­
jske zjapecc pukoline kinematskog A-stadija. Ove puko­
tine imaju malo prOslorIlo protezanje (eentimelarskih do 
decimetarsk ih velieina) pa o bicllO ne presjecaju ni eijelu 
dcbljinu sloja. Porcd toga se dobro isticu zbog karakle­
risticnih pcrastih obJika ispunjenih bijclim sparikaic itom. 
Znaeajno jc cia se Be pojavljuju na bilo kojelll mjeslLi 11 

ravnini 01 - 0 2' vec samo u zonama na koj ima je razlika 
olpornosti i langeneijalnog prit iska najmanja (hO[-zona 
poel kutolll od 45° prema praveu glavnog slresa, modifici­
rana za kUl unutrasnjeg trenja Ll vapnelleima iznosi eea 
38°). 

U kinematskolll B-stadiju dolazi clo kidanja hOI-zone i 
sm ieanja po konjugiranom paru hOI pukotina (prva hOI 
gcneraeija). Pukotine su ecntimctarskih do Illctarsk ih duzi ­
na, potpuno presjeeaju sloj al i nc penetriraju u drugi sloj; 
zastaju na meciuslojnolll diskontinuiletu. Velieinu il11 
zapravo kontrolira debljina sloja, pa se ne mogu razviti do 
kvalitcte rasjeda. Cesto iskazuju mil imctarska lijeva, 
odnosno ciesna kretanja s lllalim tekloglifima koji su para­
lelni sa slojem. Ovi mali pomaci, clakako, razmicu i tenzi­
jske pukotinc kinemalskog A-stadija kojc SLi U istoj zoni 
prethodile smienim pukolinama. Nazalost, kod lih sc 
slueajeva brka redoslijed dogadaja, pa se uSlalilo kao pra-

Geologia Croalica 50/! 

vilo, da Sll sl11icne hOI pukoline krctanjelll izazvalc sekun­
darnu pojavu tenzijskih pllkotina (lad a ill razlikuju kao 
"peraste pukotine"). 

A i B stad ijcm jc g lavni s tres kompenziran na razini 
otpora sto ga je pruzao svaki sloj zasebno. Naslavkom 
djelovanja stresa, u C-stadiju, potroseni ustroj olpora 
zamjenjujc krupniji sklop, skup slojeva (pakel). C-staclijem 
opiruea mas a teii hOlllogenizaciji, okrupnjavanju, pa su od 
ovog slaclija i sve defonnacijc krupnije. OpirLici se materi­
jalnoj dezintegraeiji, homogcni sc sk lop slojeva postavlja 
sirom frol1tom prema glavnom stresu. Na OVll rcakcijll 
olpora, glavni sIres redistribuira sporcdne st resove (G2 i ( 3) 

slo je rezultiralo minimalno 1110g11com posljed ieolll - savi­
j anjem slojcva i boranjem. Boranje je jos popraeeno doda­
tnom kompenzacijom stresa "popustanjcm" po komprcsi­
jskom klivazu osne ravnine. 

C-sladij donosi najznacajniju kontrakcijsku promjenu . 
Na sirem planu ovaj strukturni doseg naznaeava i pro­
mjellu ukupnih geoloskih odnosa. Dominantan geoloski 
proces postaje tektonski transport (na praveu najslabijeg 
strcsa - 03). Sedimentacija prestaje, odnosno nastavlja se u 
izmijenjcnilll uvjetima na nekom drugol11 mjestu. U kine­
matskom C-staciijll laramijske tektons ke faze izdizu se i 
okopnjavaju siroki prostori (ne salllo karbonatne plat­
forme), a u C-stadijLl pirenej ske faze mijenja se velik i scd i­
mentacijski sustav platrorTnskih karbonata II flis. Ncolek­
lonskim C-sladijem, mog lo bi se ree i, pocinje pos ljednje 
izclizanje gOlja . 

N apredovanjem dcformiranja raste indcks sl isnutosti 
bora, a zalim i naglaseni nagib karaklc ristiene juzne ver­
gencije neotektonske kontrakeije . Olpor glavl10m slrcsu 
jos pruza duktilnost matc rijalne grade bora. Nadvladava­
njcm duktilnosti, u kinelllatskom D-stadiju, bore popustaju 
i kidaju se po zon i na kojimaje razlika otpornosti i langen­
cijalnog stresa najmanja - po smienom hOI sustavu drllge 
gcncraeije. Suglasno velikim strukturnim formama, nasla ­
.ill kilomct arski hOI - sllstavi rcverznih rasjeda s per­
pendikLllarno llgradenim (sjevcr-jug) dec illlelarskim do 
metarskim tektoglifima. Od bora se formirajll Ijuske juznih 
vergeneija kao najslikovitiji odraz ncotektonskc kontra­
keij e otoka Hvara ("hvarsko pruzanje"). 

Ljuskc su, dakle, strukturna sustina oloka Hvara , a ne 
"otoena Ijuska" kako se rcclovito opisllje u geoloskoj lilera­
turi. Moze sc prctpostaviti cia j e oejeni 0 j ednoj Ijuski 
doprinio markantni kontakt ecla najjuzn ije Ijuske s fiisom, 
kao i privid 0 re lativno kontinuiranom zatvaranjLl naslaga 
integrirane jczgre s mladim naslagam<l. Prvo: rJis sc ovdje 
pojavljuje samo kao najmladi sediment i nije u funkeiji 
suvisle pod loge po kojoj se Ijuska krece. Po prirodi kinc­
matskih uvjeta napredovanja derormiranja sireg s trll­
kturnog sklopa, moze sc reci jeciino to da jc ova najjuznija 
Ijuska ujcdno i prva pojava Ijuskanja. Sjcvcrnije od njc 
sljede sve mladc Ijuske kinematskog D-staclija neotek ­
tonskc kompresije. Drugo: ideja 0 jcclnoj Ijuski podrazlImi­
jeva kinclllatski predstadij (C) jednc jedine goicmc bore s 
kojom je preraden eijcli zateeeni pirenejski strukturni 
sklop, kao da se i on sastojao salllo od jednc goleme borc. 
Relikti bora ranijih, predneotektonskih faza, ukazuju dOl to 
nijc tocno. Neoteklonski C-stadij forrnirao je brojnc 
csalonirane bore jcr j e morae prcborati veCinu zaleeeni h 
struktura starijih tektonskih faza i tek ih potom med iti II 

Ijuskc. Sto je dakle uzrok prividno integralne jezgre, 
odnosno inlegralne olocne Ijuske? Moglo bi se reci upoma 
i snazna ncoteklonska kompresija koja sabija i ljuska bore 



MarinCic: Tectonic SlnKlure of the [s[;llld or H var (Southern Croali;l) 

do clubokog tektonskog kontakta jczgre s jezgrom i spaja­
nja rcduciranih cela bora u jedno sekundarno te lo (SI. 6). 
Kincmatski put oel staclija do stadija ustvari je put zamjena 
svladan ih o pi rucih formi s otpornijom geomctrijskom 
graclom . Od "potrosenih" se elemcnata sastavlja, integrira , 
vcl ika otporna slruktura koja na koncu runkcionira, a tako 
sc i dozivljava, kao jedna ve lika otocna Ijuska s aktualn im 
celom u kontaktu s rIi som. 

Za kinematski E-staclij bi se moglo reci cia je vjerodo­
stojn ije hvarsko svojslvo i od sarnog "hvarskog pruzanja". 
lako SLI sirom Dinaricla poznate lokalne pojave E-deforma­
eija, one su nezaob ilazni ci nilac ukupnog neotcktonskog 
sklopa c ij clog podrucja Hvara, do razine izdanka. One su 
zapravo puni odraz specificnog rcgionalnog geotektonskog 
polozaja otoka Hvara (kOla islurcnog segment a neotekton ­
skog navlacenja Dinarida na laclransku pl atfo rmu) ali 
takoder i odraz int ernog stanja stru kturnog ustroj a 
hvarskog sklopa. Naime, brojne reducirane Ij uskc kojc sas­
tav lj aj u priviclno hom ogenll otocnu struktu ru, pod 
pojacani m naprczanjem poc inju iskazivat i autonornnc 
odgovorc na sIres . Svaka se osnovna Ijuska ponaosob, ocl 
najvece do naj rnanj c, os lobada pri tiska popll stanj em po 
novom deforrnaeijskom sustavu hOI pukotina i rasjeda 
kinemalskog E-stadija. Ova sc trcca gcneracija hOi 
reverzni h rasjcda prikljucuje ranijcrn hOI rcvcrznom sus­
lav u D-slad ija u konjugirani hOI pa r. Pos ljediea jc konjugi ­
ranje Ijusaka sv ih podrucja vc lic ina i ukupno konjug iranje 
hvars kc integriranc Ijuske. Juz.no oel njezi ne si met ra lne 
ravn inc su bore i Iju ske ju zne vergeneije s nav lacenjern 
prema j ugu, dok se sjeverno od simetralne ravnine It E­
stadiju fOrTnirajll sjevernc ve rgcncijc bora i Ijusaka prellla 
sjeveru. Tangeneija lni se stres trosi na oba revcrzna kre­
tanja slo udvosl rucuj e te ktonski transport na praveu cry 
Tjcmena struktura do laz i u polozaj smanjcnog bocllog pri ­
liska, pa se s ire i otvaraj ll sta riji disjunklivni sllstavi A, B i 
C-stad ij a. 

Kinelllatski F-st ad ij obuh vaca najmladi suslav ncolek­
tonskih tangcncijalnih dcformaeija otoka Hvara. Globalni 
je stres fakticki sv ladao kinematsku sust inu otpora bore -
Ijuske, pa sc dcformiranjc E-s klopa nasta vlja , Ltvjetno 
receno, s licno ponavljanju ll -s tacl ij a vise cl e form acijskc 

65 

razine, odnosno F-s tad ijem . U bi ti se reakti v ira prva hOI 
gcneracija konjugiranih parova rasjecla B-stadija. F-stadij 
se pojav ljuje kao cetvrta hOI generae ija s naglasellim hori­
zontalnim kreta njem duz lij ev ih i desn ih tran skurentnih 
rasjeda koji ces to presjecaju sve strukturnc form e 
hvarskog sklopa (S I. I ). Isti cu se ve likim rasjed ima s 
limonitiziranim plohama i dccimetarskim subhorizontal­
nim Icktoglirima. 

U komplcksnom st rukturnom skloPll kao sto je 
podrucj e Hvara , kinematski se stadiji pojavljuju s ljedorn 
strukturne zrelost i svakog strukturnog segmenta. Zbog 
loga se, na pl anu progresijc ncotektonskog stresa prcma 
jugu, od zone do zone prakticki istovrerneno nalazc 
razliciti kinematski stadiji. 

U ovom je prikazu zapostavljeno pitanje sudjelovanja 
ekstcnzijsk ih faza i ekstenzijskih tektonskih pokrcta c iji jc 
uc inak , za razliku od kontrakeijskih (tangcncijalnih) faza, 
redov ito prcdvid iv. Nairne, one nezaobilazno s ljecle 
prestanak djclovanja svakc kontrakcijske faze. 

Borane naslage oslobodene tangcncijalnog sl resa i pot­
pomognute s irenj em prostora, sac uvanim e last ic itetom 
tcie vracanju prema prvotnom stanju formc. Medutim , 
ubrzo prelazc g ranicu elasticiteta zbog cega se LI zoni b-osi 
otvaraju ekstenzijske pllkotine. Bllduci cia tangcnc ij a lni 
stres u potpunosti smje njujc s ila grav itacije, ckstenzijske 
sc pukotine zone b-osi akli viraj u u gravi tacijski hal sll stav 
konjugiranih parova kliznih pukotina (S I. 7). Po njima sc, 
popu t izos tat skog krctanja, antiformc g ravit acijski 
spustaju, a sinforlllne izdizu. 

Bez ove cik licne kornplementarne izmjene tangeneija­
lnih i radijalnih lekton skih pokrcta, ne bi bila Illoguca 
obnova seciimentacijc na istom mj cstll. Faza ekstenz ije 
poravnava izd ignuto gorjc i sni zava crozijsku bazu do 
razine obnove uvjeta sccl imentae ije. Tako na I-Ivaru na apt ­
skoj emerz ij i sl ijed i irnerzija gornjeg alba, nakon emerzije 
alba c10lazi imcrzija ccnomana itd. 

Nova sc tangenc ijalna faza pojavljuje tek kada brzilla 
kretanja Africke ploce poslaje izrazito veca od brz inc 
rOlacije. Po nc izbjcz.llo novolll vek toru ukupnog kretanja , 
generira se nova kompresija g lobalnog slresa kao prepo­
znatljiva tcktonska langencijalna faza. 

Manuscript received April 3, 1995. 
Revised manuscript accepted April 28, 1997. 



66 Geolog i;l Croalica 5011 

PLATE! 

Fig. I Relics of the Laramian fold (1' I, B 180/20) in the southern limb of the central Neotectonic anticline (1' 1Il , 
B 270/1 0) of the island of l-lvar; vicini ty of lel sa. 

Fig. 2 Relics of the Laramian fold (F I, B 5/10) near Vrboska. 

TABLA 1 

SI. I Relikt laramijske bore (1' I, B 180/20) u juinom hilu sreclisnje neote~10nske antikl inale (1' Ill , B 270/10) 
otoka T-Ivara; poclrucje Jclsc. 

SI. 2 Relikt laramijske bore (1' I, B 5/ 10) kod Vrboskc. 



Marincic PLAT E I 67 

BFI 

1 



68 Geologia Croatica 50/1 

PLATE 11 

Fig. I Relics of the Pyrenean fold (F 11, B 297/8) with preserved south-western vergence; Vrboska. 

Fig. 2 Neotectonic fold (F III) of the northern coast of the island of Hvar with secondary northern vergencc of the 
E stage; Mala Stiniva cove. 

TABLA II 

Sl. I Relikt pirenejske bore (F II , B 297/8) sa sacuvanom jugozapadnom vcrgencijom; Vrboska. 

SI. 2 Neotektonska (F Ill) bora sjeverne obalc atoka Hvara sa sckundarnom sjcvcrnol11 vcrgcncijom E-stad ija; 
uvala Mala Stin iva. 



M:lrillcic 

, .' 
I 

-------

PLATE II 

, 
" " , 

.~.-""~' ' 

"\ ~... ~ 

...... :.\~:". 
.; 

69 



70 Geologia Croatica 50/1 

PLATE III 

Fi gs. I and 2 Small-scale Neotectonic folds (F III) with the northern vergence of the E stage; Stari grad. 

TABLA 1II 

SI. I i 2 Male neotcktonske (F III) bore sjevernc vergcncijc kinematskog E-stadija; Stari grad. 



PLAT E !!! 71 



72 GcOlogi;l Croatica 501 1 

PLATE IV 

Fig. I hOI joints of the B stage in the kinematic fabric of the fold (C stage); northern limb of the anticline in the 
Dubac cove. 

Fig.2 Identical kinematic stages in the core or the syncline in the Zavala cove (near Stari grad). 

TABLA IV 

SI. I hOI pukotine B-stadija u kinematskom sklopu bore (C-s tadij); sjeverno krilo antiklinale u uvali Dubae. 

SI. 2 Idcnt icno kincmatsko stanjc u dnu sinklinalc u uvali Zavala (Slarigraciski zaJjcv). 



Marin6': PLATE IV 

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" --

73 



Geolog ia Croa!ica 5011 

PLATE V 

Fig. 1 Conjugated hOI joints or the kinematic stage B; bedding surface near Vrboska. 

Fig. 2 Frontal part of the Ncotcctoni c(F III) thrust-shect of the Uppcr Cretaceous limestone overlhrusling Palaeo­
gene flysch. Metre-scale "a"- lineat ions (Iccloglyphs) with movement towards the South; city of Hvar. 

TABLA V 

Sl. I Konjugirane hOI pukotine kinclllatskog B-stadija; slojna ploha kod Vrboskc. 

SI. 2 CeJo neotcklonske (F Ill) Ijuskc gornjokrednog vapnenca navucenog na palcogcnski rIis. Mctarske "a" lin­
eacije (tcktoglifi) s krclanjem prcma jugll; grad Hvar. 



PLATE V 75 



76 Geologia Croalica 50/1 

PLATE VI 

Fig. 1 Tensional joints of the kinematic stage A (feather-like shaped joints) appearing in the hOI zone before hOI 
joints. Bedding surface in Carnian limestones in the Samoborska Gora Mt. 

TABLA VI 

SI. I Tcnzijskc pukotine kinematskog A-stadija ("perastc pukoline"). Pojavljuju se u ha l zoni prijc hOi pukotina; 
slojna ploha karnickog vapnenca Samoborske gore. 



Marincic PLATE VI 77 

hot 



78 Geologia Croatica 50/1