Triassic magmatism of the Dinarides in Yugoslavia

273

T~,c,,o,lo~/!~src.r. 109 (1984) 273- 307 Elsevier Science Publashers B.V.. Amsterdam

TRIASSIC

JAKOB

MAGMATISM

- Printed in The Netherlands

OF THE DINARIDES

IN YUGOSLAVIA

J. PAMIC

Suchsor u ,7,4 IO00

GcwlosX~ :uwJ, (Received

February

ZU~ivh ( ~rrgo.slrcw)

8, 1984; revised version accepted April

18. 1984)

ABSTRACT

Pamid. J.J., 1984. Triassic magmatism

of the Dinarides

The Triassic magmatism of the Dinarides

in Yugoslavia.

T~,c,/o,loph~.oc.s. 109: 273 -307.

had a polyphase character.

It took place during a period of

ahout 50 Ma during the initial stages of the Mesozoic Wilson cycle. Their earliest phases might have heen connected with rifting processes. and the subsequent ones preceeded directly the opening of the Dinaridic part of the Tethys

and the formation

basic, and more commonly affinity.

The Triassic

calc-alkaline immobile

of a spreading

by intermediate

magmatic

rock association

rocks of recent convergent

ridge. The Triassic magmatism

and acid plutonic

and volcanic

can be correlated

plate margins.

However.

the Dinarldes

by rocks of the continental

was influenced

by partial

on maJor element

field relationships

trace elements indicate that lavas poured out over Triawc

which was underlain

is represented

by

rocks with talc-alkaline evidence

with

and the data on

sediments on a carbonate

platform

crust. The basic diversltv of the Triassic magmatism

melting.

Other

processes (crystallization.

contamination

of and

others) must have played a secondary role.

INTRODUCTION

Triassic plutonic and volcanic rocks are frequently found in the Dinarides. They are of metallogenetic interest because they are associated with numerous economically important mineral deposits of Fe, Mn, Pb. Zn, Sb, Hg and Ba. Triassic igneous rocks and adjacent Triassic sediments stretch without a break further to the northwest

in the Southern

Alps (Martinis,

Albania in the Hellenides, (Dede, 1970). Triassic igneous rocks have been studied

1975)

and

in detail

further

to the southeast

in numerous

localities,

in

and a

comprehensive list of papers published mostly by Yugoslavian geologists can be found in a separate paper (Pam?, 1982a). Some of the authors carried out regional petrologic studies for some parts of the Dinarides: Grafenauer (1978) for their most northwestern parts in Slovenia, PamiC (1963, 1974) for their central parts in Bosnia and KneieviC (1975) for their southeastern parts in Montenegro. Recently a group of French scientists (Bebien et al., 1978) published a paper in this journal on the Triassic volcanism of the central and southeastern parts of the Dinarides. 0040-l 951/84/$03.00

‘L) 1984 Elsevier Science Publishers B.V.

214

The aim of this paper is to give a realistic of the Dinarides

(TMD)

earliest

phases

during

the initial

range

of plutonic,

genetical nantly

might

have been connected

stages of the Mesozoic

relation

presentation

volcanic

and

character

with rifting Wilson

hypabyssal

with carbonate

of intermediate

of the Triassic

as a whole on the basis of all data

platform

processes which

sediments.

but with very distinct

Its

which took place

cycle. The TMD rocks

magmatism

so far available. produced

a wide

originated

in a close

The magmatism

was domi-

basic to acid differentiation

trends. GEOLOGY

Regional geological setting The Dinarides

represent

a typical

erogenic

belt located

along

the northeastern

margin of the Adriatic microplate (Dewey et al.. 1973) or the Adriatic promontory (Channel et al., 1979). The belt can be divided in two main parts (Fig. 1): (a) the outer Dinarides (the karst dolomites, and (b) the inner

area) consisting mostly of Mesozoic limestones and Dinarides characterized mainly by Mesozoic ophiolites

which

siliceous

are associated

with

and

elastic

sediments.

These

25 ,

L-

0,

,

scheme

platform,

2 -transitional

Paleozoic

zone,

5-inner

7 -Balkan-Karpathides.

are

T

\\

Fig. 1. Geotectonic

two units

50,

,

190

km

of the Dinarides.

zone with predominant Dinaridic

belt,

modified

after

Petkovik

flysch sediments,

6-transitional

zone

(1958)

3 -central

between

I -Mesozoic ophiolite

the Dinarides

carbonate

zone, 4 -inner and

the Alps.

215

thought divided

to represent almost

1959) or “flysch mostly

platform

and open

ocean

by a zone of Mesozoic

Bosniaque”

of elastic

tinental

carbonate

symmetrically

of French

and carbonate

geologists

sediments

environments.

flysch-Durmitor

(Aubouin

which

They

et al., 1970) consisting

probably

originated

under

con-

slope conditions.

Triassic morphic

igneous

rocks are associated

rocks of the Younger

with Triassic

Paleozoic

(Herak,

sediments

and with semi-meta-

1962). The relationship

between

oldest Triassic rocks of the Mesozoic Wilson cycle and the underlying rocks of the Hercynian Wilson cycle has not yet been solved. The youngest

Hercynian

and Lower Permian and

are

flysch (Be%,

northwestern

units,

sandstones Dinarides

represented

commonly

and shales are overlain by “Groden”

by Upper

the

Paleozoic

Carboniferous

in many places in the western

deposits,

represented

mostly

by red

sandstones, shales and conglomerates without fossils. The Groden deposits are found within the Permian in the Lika region (Salopek. 1942, 1960: Kochansky-Devide, 1973) for which there is an opinion that continuous sedimentation took place during the Permian and that it went on without a break into the Triassic (Raffaelli and SCavniEar. 1968). ‘The only place where sedimentology of the Groden deposits has been studied in detail is the area of iirovski-vrh in the northwesternmost Dinarides. Omaljev (1982) identified the Groden deposits of the northwestern Dinarides as continental sediments, and he provided evidence of sedimentary textures characteristic of delta and continental

environments.

continental

sediments

The Lower

He also noted

in the adjacent

Triassic

is represented

a positive

Southern

correlation

with the analogous

Alps.

by red sandstones

shales,

marly

shales

and

limestones with marine fossils. The Lower Triassic sediments are conformably underlain in some areas by Belerophone limestones (Susnjara, pers. commun.. 1982). thus providing parts

evidence

of the Dinarides,

deposits in these areas limestones are commonly

that the Mesozoic in the Upper

Wilson

Permian.

cycle started,

Unfortunately,

at least in some

there are no Groden

but the Lower Triassic sediments and the Belerophone underlain by anhydrite and gypsum beds.

The Middle and Upper Triassic of the Dinarides are represented for the most part by limestones and dolomites. The Lower parts of the Middle Triassic are represented only in some places in Lika and Montenegro by elastic sediments, and the Lower parts of the Upper Triassic by the Rabelian beds (Ciric, 1964/65; Sokac, 1973). The Middle

Triassic

and Lower parts of the Upper Triassic

places by volcanic-sedimentary sequences, volcanic rocks including pyroclastics. Igneous

rocks, mode of occurrence

Igneous complexes

are represented

i.e. sediments

are

in numerous

interlayered

with

and age

rocks are associated with two main groups of Late Paleozoic and Triassic within the Dinarides (Fig. 2). The first is connected with the outer

216

Dinarides-the crestal tively

Mesozoic

parts

of larger anticlines

autochthonous

Permian

and

underlain

character.

Triassic

occur

crust.

platform

(MCP)-where

or occur along Triassic

sediments

by continental

complexes

carbonate

which

were

The second

as allochthonous

larger faults

igneous

masses

rocks

deposited

group

they

make

and have a compara-

are here

associated

with

in a sedimentary

of late Paleozoic

over the geotectonic

Dinarides which originated on the oceanic crust masses are interpreted as nappes with southwestern

up the

basin

and

units

Triassic

of the inner

basement. The allochthonous convergence and, accordingly,

they represent parts of the Durmitor and Pannonian nappes (Nopcza, 1921; Miladinovic, 1974). Most recently Herak (1980) has explained the allochthonous L,ate Paleozoic and Triassic masses in Gorski kotar as a result of subcrustal (subduction according to Amstutz) with northeastern convergence. The boundary Triassic defining

between

the autochthonous

and allochthonous

flowage

Late Paleozoic

complexes is represented by the zone of Mesozoic flysch the northeastern margin of the MCP of the Dinarides.

and

most probably

Triassic igneous rocks are not evenly distributed throughout the Dinarides. Quite scarce occurrences of volcanics with more pyroclastics can be found throughout the MCP. The largest masses of igneous rocks are exposed along the outer margin of the MCP, particularly along its northeastern side. A zone of igneous rocks starts to the southeast of the boundary with the Hellenides and stretches along the northern Montenegro (Mts. Komovi-Bjelasica-Sinjajevina-Ljubisna) and further to the northeast in Bosnia (Mts. ZelengoraaTreskavicaaIgman-Zvijezda). The northwesternmost

extension

of the zone is in Slovenia

Bled. A second zone of Triassic side of the outer

margin

igneous

of the MCP.

Dinarides

and

connected

with the inner margin

in the area of the Julian

Alps and

rocks can be traced along the southwestern It follows

the KuCi fault in Montenegro.

the Voljevac

A further

fault

in the middle

zone of igneous

rocks

is

of the MCP, and it follows the Sinj-Velebit-Fuiine

fault (Sokac, 1973) to the northwest, whereas its southeasternmost extension lies along the Montenegro coast. Small occurrences of igneous rocks from the Dalmatian islands-Vis. Jabuka of the MCP.

and Svetac-are

probably

Triassic plutonic rocks are represented

also connected

by varieties

with the inner

of granite.

syenite,

margin

diorite

and

gabbro, and occur most frequently in the middle Dinarides. The largest is the Radovan body with a surface area of about 50 km*, and there are several smaller masses with a total surface of about 200 km2. They occur as stocks. sills and dykes that are intrusive in Permian, Permo-Triassic, Scythian and Anisian sediments. Isotope determinations on twelve monomineralic fractions and whole-rock samples of plutonic rocks from the middle Dinarides and the area of the Karawanken gave ages that ranged from 262 to 216 Ma pointing to the stratigraphic span between the Middle Permian and Middle Triassic (Table 1). Hypabyssal rocks commonly intrude the same country rocks. Diabase and albite diabase dykes and sills are particularly frequent in Permo-Triassic sediments of the middle and southeastern

P

r-

P

AUSTRIA

-

-P

/ 4

c

GCCTI]

70

6.

S..--___

lo’-’

pp. 277 280

281

TABLE

1

Isotope

ages of abyssal

rocks

Mineral-rock

Locality

Method

Age (Ma)

Reference

Quartz-albite

Mt. Radovan

Rb/Sr

223+7

Pam?

232il

LovriC (1980)

250+7

Pamit and

syenite Jablanica

Gabbro Gabbro Hornblende

Rb/Sr

and

(1980)

253+8

LovriC

252&S

PamiC and

Jablanica

Rb/Sr

262?8

Lovrid (1980)

Foea

K/Ar

190+6

Pamii- and

Karawanken

Rb/Sr

2241-9

(not fresh)

LovriC

from diorite Granodiorite

(1980)

Scharbert

(1975)

216+9 Hornblende

from

Karawanken

Lippolt

244+8

K/Ar

Biotite from

Karawanken

Lippolt

221+7

K/Ar

Karawanken

from

Lippolt

23Ok5

U/Pb

and

Pidgeon (1974)

diorite Hornblende

from

Cliff et al.

22459

K/Ar

Karawanken

(1974)

diorite pegmatite

Dinarides

in Bosnia and Montenegro (Buzaljko, 1974; Vujnovic, 1980). extrusiue rocks are represented by varieties of basalt, spilite,

Triassic

keratophyre,

dacite

and quartz

keratophyre

with pyroclastics,

frequent

and cover in total a surface area of about 500-1000

LjubiSna

and Bjelasica

area of about square

and

Pidgeon (1974)

diorite Titanite

and

Pidgeon (1974)

diorite

volcanic

bodies

in Montenegro,

100 km2. There are numerous

kilometres,

as for example,

Prijepolje and others. Extrusive rocks occur

bodies

flows which

they are more

km’. The largest are the

each of which has a surface

with surface

in the neighbourhood

as volcanic

and

andesite,

areas of a few ten

of Kalinovik,

lie conformably

Jajce. Vakuf. within

Triassic

sediments. Figure 3 illustrates the geological columns of several Triassic volcanic masses of medium size. The interlayering of volcanics with marine Triassic sediments indicates the submarine character of the volcanic activity. The age of volcanic rocks has been determined in numerous places in the Dinarides. Austrian geologists (Zollikofer, 1861; Katzer, 1906; Kerner, 1916) originally obtained Ladinian ages, but later it was found that the volcanism can be both younger and older than the Ladinian. Tuffs interlayered with Groden sandstones (Hinterlechner-Ravnik, 1965) and evaporites (Scavnicar, 1979), on the one hand, and with megalodon limestones, on the other hand, define precisely the stratigraphic span of the volcanic activity. Columnar

sections

(Fig. 4) synthesized

on the basis of 44 local columns

illustrate

V t103N313Z

I

,

Y

”

-e-s.-+

““I” VI

” ”

”

.,

-

”

”

”

-5 “Y

”

v

”

Y

”

Y

<-

Y

”

YYY

”

”

”

YY””

Y

“Y”

”

”

”

”

Y

Y

v

n

Y

”

”

Y

n

+

h

”

A.

h

“““-4

““V

h

k-__

Y

v

”

I

V3lAV3lS3111

-1

.*_

YY””

._

”

I

4

-

r-4

I-

;

284

the stratigraphic available

data

position suggest

some areas in Middle place during Dinarides; Triassic

and Upper

the Anisian

main and most intense (4) weak

of the volcanism

the following

Permian

magmatic volcanic

activity

activity

parts of the Dinarides.

(1) magmatic

and Scythian;

only in the area of the inner

only in the western

Some paleogeogruphic

in different

conclusions:

activity

(2) magmatic margin

activity

in took

of the MCP: (3) the

took place in the Ladinian continued

All

started

throughout

up to the middle

the

of the Upper

Dinarides.

considerutions

Triassic magmatic processes must have been controlled by tectonic features, i.e. the existence of large and deep faults provided channels for magma emplacement. Karamata (1975) has presented the idea that the TMD might be connected with the processes of rifting and opening of the Dinaridic part of the Tethys which is consistent with the concept of aborted Triassic rifting in the Southern Alps (Dietrich, 1976; Bechstadt et al., 1978). According to new geodynamic ideas the initial phases of rifting can be explained as a result of large-scale uplift caused by magmatic phenomena and by the rise of a “thermal dome”, i.e. partially melted upper mantle (Keen and Hyndman, 1979). The uplift and thermal expansion give rise to the breaking of superficial brittle parts of the lithosphere, manifested in the formation of a system of subparallel rift-type faults. This made an additional rise of the thermal dome possible and in some higher levels, because of adiabatic decompression, magmas can be formed and they move upwards along deep rift fractures. The solidification of igneous bodies in turn gives rise to shrinking rifted margin

and a new type of deformation

which represents

a predisposition

the MCP, respectively (Fig. 5). The beginning of the Alpine rifting

shown in a slow subsidence for the formation

process cannot

be precisely

of the

of a shelf area and fixed because

the

relationship with the Hercynian basement has not been positively solved. It can be presumed that the boundary between the Hercynian and Alpine cycles is marked by a land phase when the Groden deposits were accumulated. If the existence

of the Adriatic

microplate

is accepted

(Dewey

et al.. 1973)

the

origin of first rift fractures might be considered as a part of complex geological processes which took place during the Late Permian in an area that was probably located not far from the present northern coast of Africa. First rifts might have been formed on account of the uplift of the thermal dome and they gave rise to the development of horst-graben structures. A slow subsidence then produced marine transgressions which in some places resulted in the deposition of gypsum-anhydrite beds. The initial phases are characterized in a few places by weak magmatic activity. Afterwards, in the Uppermost Permian and Scythian a stronger subsidence took place which gave rise to a larger influx of terrigeneous material and to a elastic sedimentation accompanied only in a few places by weak volcanic activity.

285

.

Fig.

5. Schematic

platform

sketch

(modified

crust. 4 = rift sediments,

Very strong the

Anisian,

map

showing

a possible

after Keen and Hyndman, 5 = marine

tectonic and

sediments,

movements

these

were

evolution

from

1979). I = upper mantle. 6 = thermal

dome,

rifting

to the origin

2 = continental

7 = igneous

of carbonate

crust, 3 = oceanic

rocks.

must have taken place at the very beginning

followed

by strong

climatic

changes.

A cycle

of of

carbonate sedimentation resulted which produced a “carbonate ramp” (Wilson, 1975) and this phase can be understood as a beginning of the existence of the MCP of the Dinarides. The only exception is the area of the inner margin of the MCP where carbonate and elastic sedimentation took place in some places with contemporaneous weak volcanic activity (Fig. 6). The strongest

magmatic

activity

in the area of the MCP took place during

the

Ladinian, particularly along its outer margin. Aborted rift faults again became active, and subsidence and uplift of separate blocks took place along them. The vertical movements gave rise to smaller, probably isolated basins in which sedimentation of cherts, pelites and limestones took place accompanied by submarine volcanic activity of variable intensity along reactivated rift faults. In the uplifted

*.I..

T

x

-

:

I

t

__

287

areas between emerged 1966).

the basins,

blocks Some

conditions. The volcanic exposures

bauxite

larger

deposits

bodies

activity

of plutonic

reef sedimentation formed

might

have

was accompanied

rocks point

during been

a short-lived partially

by plutonic

to the conclusion

only in the area of the outer margin The volcanic activity quantity of pyroclastics,

took place and on some uplifted land

erupted processes,

phase

under and

that the plutonism

and

(Burial, subaerial

the present was manifest

of the MCP.

with numerous explosive phases, represented by a large continued into the lower parts of the Upper Triassic, but

only in the western Dinarides. the upper parts of the Upper

No traces of magmatic Triassic.

activity

have been observed

in

It can thus be concluded that the upper parts of the Upper Triassic marked the end of the complex tectonic and magmatic processes that started with the rifting along the northern margin of the Africa plate, i.e. in the area of the southern margin of the future Tethys. PETKOLOGY

Triassic

magmatism

and hypabyssal but it produced

of the Dinarides

produced

a wide range of plutonic,

rocks. The magmatism was dominantly of intermediate numerous basic, intermediate and acid rock varieties.

volcanic character.

Plutonic and h~pa~~ssai rocks Plutonic igneous rocks are represented by varieties of gabbro, diorite, granodiorite, granite, albite syenite and albite granite. Endometamorphic zones are developed in the marginal parts of some plutonic bodies and exometamorphic zones in the surrounding Permian and Triassic sediments. Both plutonic masses and their country rocks are in some places invaded by vein rocks of equivalent composition. Mineral assemblages of the plutonic rocks comprise quartz, various feldspars (plagioclase, albite, orthoclase, microperthite and pegmatitic intergrowth of quartz and alkali feldspar), and various mafic minerals (predominant amphibole-mostly ferrohastingsitic

hornblende-with

subordinate

biotite

and

clinopyroxene,

and

occasionally orthopyroxene and olivine). All these minerals, and particularly the feldspars, are commonly altered to various degrees and contain secondary minerals including sericite, calcite and prehnite. Microprobe chemical compositions of some of these rock-forming minerals are presented in Table 2. Gahbro occurs as an individual intrusion at Jablanica, within the Radovan massif (MariC, 1927/28; PamiC, 1979) and in some other places. Its major minerals are plagiocfase (average compositions in two bodies: An,, and An,,,,) and hornblende with subordinate clinopyroxene and biotite, and very infrequently hypersthene and olivine. Diabase

occurs within

endometamo~hic

zones as chilled

margins

and as dykes

288

TABLE

2

Microprobe

chemical

plagiogranites

compositions

(%)

of

rock-forming

minerals

SiO 2

TiO,

Al 2%

Fe0

1

67.30

-

19.31

-

2

63.99

-

21.64

3

67.59

-

78.70

some

albite

syenites

K,O

_

13.09

-

2.19

-

11.60

0.58

-

_

13.65

-

4

66.99

-

18.99

0.68

-

67.12

-

20.61

-

_

6 7

67.45 66.77

-

17.77 18.93

-

-

8

66.29

-

20.87

9

42.71

-

36.19

10

63.93

-

20.43

11

44.91

-

42.25

_

-

and

-

0.64

31.83

11.24

0.28

9.35

36.48

3.52

14

56.22

-

0.89

21.16

7.74

15

32.81 33.35

-

30.77 29.35

10.06 11.79

0.20 0.18

transformed);

14-actinolite;

14.80 14.31

_

_

2.02

10.81

8 and

16.27 10.50

3.52

4 slightly

_ _

_

39.88

(2 and

-

-

10.50

39.61

13-homblende;

0.43

12.27

11.46

12

12-- biotite;

12.92

-

10.12

13

* l-7-albites

CaO

Na,O

M&J

5

lb

of

*

9.60

0.20

0.05

13.21

0.07

0.18

26.36 25.51

_

_

10.84

IO-potassium

feldspars;

9 and

ll-illites;

15 and 16-epidotes.

and sills in the adjacent sediments. It is particularly frequent in the middle and southeastern Dinarides, but it is also found in Dalmacija and Slovenia (Hinterlechner, 1959; Buzaljko, 1974; Golub and Vragovic, 1975; Vujnovic, 1980). Diabase commonly contains calcic plagioclase and clinopyroxene albite and uralite with chlorite (albite diabase). Diorite (+ quartz) is more frequent than the gabbro

often

transformed

and occurs

into

as individual

masses in the neighbourhood of FoCa and on the slopes of the Mt. Visitor in the southeastern Dinarides, within the Karawanken massif in Slovenia and in some other places (Pam2 and Buzaljko. I978; Faninger, 1976). The major minerals are diorite) and hornblende; other andesine (An 35,h is the average of the Radovan minerals are orthoclase, quartz, pegmatitic intergrowth of quartz and alkali feldspars, clinopyroxene and biotite. Diorite porphyrite is also found in some places and it differs from the diorite in its porphyritic texture. Albite syenite (+ quartz) is the most frequent Triassic plutonic rock, and it was found most recently within the Radovan massif and in the neighbourhood of Jajce and cajnice in Bosnia (Pamic, 19’77, 1979, 1981). The major minerals are albite, hornblende and quartz and to a lesser extent orthoclase, microperthite, pegmatitic intergrowth of quartz and alkali feldspars and biotite. Albite syenite porphyry differs from the commonly associated albite syenite in

289

porphyritic varieties

to a few metre

by albitites

( rt quartz)

in thickness.

but some of them also contain

Granodiorite within

and in its more leucocratic

are represented

decimetre quartz,

texture

leucocratic

microperthite

albite

and calcite.

are quite subordinate

quartz. Albite granite (plagiogranite)

from the diorite

and they are found

only in the increased

is found in many places in the central

in Bosnia (Trubelja,

1963; Trubelja

from a

and to a lesser extent

body and as veins on the slopes of the Mt. LjubiSna

1975; PamiC, 1979). They differ

ern Dinarides

The extremely

which occur as veins ranging

They contain

and granodiorite porphyrite

the Radovan

character.

and Sibenik-Studen,

(Kneievid, quantity

of

and southeast1965; PamiC.

1977, 1979). It differs from albite syenite only in the increased quantity Normal granite is found only within the Karawanken body in Slovenia

of quartz. (Faninger,

1976). Albite granite porphyry differs from the commonly associated albite granite only in porphyritic texture. Aplite is scarce and it is found in the neighbourhood of cajniee and Jajce. and within the Radovan body in Bosnia (PamiC, 1977, 1979, 1981). It consists mostly of quartz and to a lesser extent albite and muscovite.

E.~o~~ta~or~hie

These intrusive

rocks

can be found along bodies and Permian

tectonically undisturbed contacts and Triassic country rocks. On

between Triassic the basis of the

primary composition of the country rocks, two main groups of exometamorphic rocks can be distinguished: (1) Permian and Lower Triassic sediments represented mostly by shale, marly shale and sandstones are metamorphosed into various low-grade schists containing mainly the following mineral associations: quartz-sericite-calcite; chloritequartz-sericite;

quartz-albite-sericite-chlorite

and

chlorite-epidote-albite-seri-

cite-quartz and mixed layered vermiculite and chlorite. The presence of albite, epidote, chlorite and mixed layered chlorite and vermiculite is evidence for the PT conditions of greenschist facies of the contact metamorphism. (2) Scythian and Anisian limestones are metamorphosed to marbles and calc-silicate rocks (skarns) consisting mainly of calcite, grossular-andradite garnet, epidote with minor clinopyroxene, hornblende, chlorite, mixed layered vermiculite and chlorite. and occasionally of quartz, prehnite, baryte, apatite, titanite and zeolite. The predominant metallic mineral is magnetite which in some places is concentrated in economic quantities. Mineral parageneses show variations from place to place and a zonation from greenschist to amphibolite facies parageneses which is best developed around the Jablanica gabbro mass. The problem of the Triassic contact metamo~hism is presented in a separate paper (Sarac and PamiC, 1978).

Gbhnic

rocks

Triassic

volcanic

rocks show more diversity

rocks are represented potassium

by varieties

keratophyre,

The volcanics

of basalt,

dacite, quartz keratophyre

are frequently

accompanied

than

spilite,

the intrusive

poeneite.

and potassium

by various

rocks.

andesite,

Volcanic

keratophyre.

quartz keratophyre.

pyroclastic

rocks.

and mafic minerals. The mineral constituents are quartz, various feldspars Feldspars are represented by plagioclase (mostly labradoriteebytownite and andesine) commonly fresh and zoned, but also metamorphosed into a fine-grained aggregate of secondary minerals. Albite is the most common alkali feldspar and it occurs either fresh without any inclusions of secondary minerals, or more frequently heterogeneous with moderate to large quantities of secondary calcite, prehnite, sericite. clinozoisite. chlorite and pumpellyite. In thin sections it was not possible to observe any transition from calcic plagioclase into albite. Potassium feldspar. represented by adularia, is not as common as the albite. Chnopyroxene, represented by augite, is the most frequent mafic mineral. It occurs as single grains but it is frequently feather-shaped. Hypersthene and biotite are scarce, but celadonite of strongly variable chemical composition is common. particularly in amygdales where it occurs with predominant calcite and chlorite and subordinate

pumpellyite,

quartz

and zeolites.

Microprobe

chemical

compositions

of

some of the rock-forming minerals in the volcanic rocks are presented in Table 3. Basalts are found in some places in the zone ZelengoraaTreskavica-Zvijezda in the central Dinarides, on the slopes of Mt. Velebit and in a few places in Slovenia in the western Dinarides (Poljak and Tajder, 1942; Hinterlechner, 1959: Pamid. 1982b). They are commonly aphyric (ophitic) and rarely porphyritic and contain a variable quantity of amygdales. labradorite-bytownite

The mineral composition of both varieties is nearly the same: and augite are the major minerals, and olivine and hyper-

sthene are scarce. Aphyric

basalts

a fine-grained aggregate of calcite, bite is found in the intersticies.

frequently prehnite

contain

plagioclase

and clinocoizite;

metamorphosed

to

in some places neoal-

Spilites are much more common than the basalts. Spilites are found in some places in Slovenia and Hrvatsko Zagorje in the western Dinarides and in Dalmatia and Montenegro coast in the southern Dinarides. But they are particularly frequent in the zone Zelengora-Treskavica-Zvijezda of the central Dinarides (Germovsek. 1959; Faninger, 1965; Karamata, 1960; Golub and Brajdic, 1969; Golub et al., 1970: Pamid, 1962b. 1972; Golub and Vragovid, 1975; Kneievic, 1975). Porphyritic and aphyric (mostly ophitic) varieties of spilite can be distinguished and both varieties contain amygdales filled mostly by calcite, chlorite and celadonite. They consist mainly of albite and augite. the latter being frequently feather-shaped only in the aphyric spilite. The albite in the spilites ranges from fresh to completely replaced by secondary minerals and it is frequently hard to distinguish between ophitic diabases with metamorphosed plagioclases and ophitic spilites

291

TABLE

3

Microprobe

chemical

SiO,

TiO,

analyses (%) of rock-forming AI,O,

Cr,O,

FePs

minerals from some extrusive Fe0

NiO

MnO

MgO

rock * Na,O

CaO

K,O

1

49.90

0.05

31.20

0.00

0.31

0.00

0.00

0.04

15.36

2.76

0.11

2

52.12

0.01

28.37

0.00

0.15

0.00

0.00

0.18

13.20

3.45

0.22

3

66.99

0.00

21.13

0.00

0.10

0.00

0.00

0.10

0.19

10.89

0.60

4

67.71

0.01

20.39

0.00

0.09

0.00

0.00

0.02

0.36

11.73

0.08

0.00

0.00

0.00

0.01

0.11

16.57

0.01

0.19

15.85

20.28

0.17

0.03

0.00

0.18

16.36

18.39

0.00

0.11

0.00

0.24

14.76

19.32

0.16

0.00

6.09

0.01

0.12

15.28

21.03

0.20

0.03

0.03

13.95

0.00

0.07

21.71

0.67

0.00

0.13

5

65.82

0.01

17.94

0.00

0.06

6

50.73

0.83

3.88

0.25

0.70

7

51.62

0.58

4.50

0.14

6.63

8

50.52

1.31

2.51

0.02

1.97

9

49.39

1.31

5.96

0.21

10

39.61

0.02

14.07

6.23 9.60

11

34.43

0.02

14.16

0.02

17.52

0.08

0.25

20.48

0.91

0.01

0.09

12

31.90

0.07

14.74

0.00

9.48

0.00

0.19

20.09

0.78

0.16

0.11

13

42.76

0.08

20.82

0.00

4.61

0.00

0.06

0.83

24.83

0.01

0.01

14

35.22

0.22

16.86

0.01

13.75

0.00

0.05

3.52

21.02

0.00

0.01

15

51.19

0.06

18.00

0.05

6.01

0.00

0.02

6.06

0.96

0.00

5.83

16

42.59

0.38

15.14

0.02

20.60

0.00

0.14

5.24

2.93

0.07

4.31

17

36.06

0.07

15.83

0.00

13.18

0.00

0.14

19.03

0.94

0.00

2.13

18

48.27

0.05

9.96

0.99

12.44

0.00

0.04

6.07

2.00

0.00

8.72

19

55.21

0.09

7.98

0.01

13.13

0.00

0.00

6.55

0.15

0.04

9.46

* Minerals

from

basalts,

spilites and poeneites

l-2-labradorite-bytownite;

3-4-albite;

13-14-clinozoisite-epidote;

of the zone Zelengora-Treskavica-Zvijezda 5-K-feldspar;

6-9-augite;

15519-celadonite.

containing albite with large quantities of secondary minerals. Poeneites, defined by DeRoewer (1942) as basic volcanics represented together

only by K-varieties, with

spilite.

glassy groundmass rocks transitional

in Bosma.

IO-12-chlorite;

Poeneites

and amygdales between

in which

is very scarce, and it is only found consist

of K-feldspar

(mostly

filled by calcite, chlorite

the poeneite

feldspar

adularia),

and celadonite.

and the spilite which contain

is

in some places chlorite. There are

both albite and

K-feldspar. Andesites are common, particularly in northern Montenegro, southeastern Bosnia and southwestern Serbia, and to a lesser extent on the coast of Montenegro, on the island Vis and in some places in Slovenia (Miladinovic and iivkovic, 1961; Pamic, 1962a;

Fanninger,

1965;

Marid

and

Golub,

1965;

Golub

and

Vragovic,

1975;

KneieviC et al., 1978). All andesites exhibit a porphyritic texture with plagioclase and augite phenotrysts. The plagioclase, commonly zoned, is mainly andesine, but can cover a large range of compositions (An,,_,,). Amygdales, filled mainly by calcite and chlorite. are not as frequent as in the basic volcanics. Keratophyres are also very common volcanics and they are found in nearly all

292

Triassic

volcanic

(Karamata, Golub,

areas of the Dinarides,

1957; Germovsek,

either with basalt-spilites,

1959; Pamic, 1961, 1962a; Trubelja,

1965; PamiC and Buzaljko,

phenocrysts.

1962; Marie and

1966, 1976, 1978; Sibenik-Studen

1967; PamiC and PapeS, 1969; Vragovid and Golub, 1969). Keratophyres are commonly porphyritic in texture and contain They can only be distinguished

of chemical analysis. but, generally, the

or with andesites

from the associated

and Trubelja, albite and augite

spilites on the basis

The albite in keratophyres can also contain secondary degree of alteration is decreased when compared

minerals, with the

associated spilites. They also contain, as a rule, a smaller quantity of amygdales. Potassium keratophyres are found only in a few places in the central and southern Dinarides,

but also in their westernmost

parts in Slovenia

1962b; Kneievic, 1967, 1975; Sibenik-Studen Kneievic, 1975). They have the same relation

(Germovsek,

1959; Pamic,

and Trubelja, 1967; Djordjevic and to the keratophyres as the poeneites

have to the spilites. They contain adularia as well as chlorite, quartz and calcite, and varieties transitional to keratophyres also contain some albite. Dacites are found in a few places, commonly together with the andesites, in Montenegro and in Slovenia (Germovsek, 1959; MariC and Golub, 1965; Kneievic, 1975). They are porphyritic rocks with labradorite, quartz and chloritized augite in Montenegro, and with quartz, andesine and biotite in Slovenia. Quartz keratophyres can be frequently found, particularly in northern Montenegro, and also in many places in Bosnia and in some places in Slovenia (Lukovid,

1952; Duhovnik,

1962a, 1972; Trubelja,

1953; GermovSek,

1959; Karamata,

1962; MariC and Golub,

1961; Pamic,

1965; Kneievic,

1961,

1967, 1975; Djord-

jevic and Kneievic, 1969, 1973). They are porphyritic, commonly with only albite phenocrysts and with quartz, albite microlites, chlorite, and infrequently biotite in the groundmass. Potassium tophyres

quartz

keratophyres

and are mostly

found

are commonly in Slovenia

associated

and northern

with the quartz

Montenegro

kera-

and in some

places in Bosnia (Germovsek, 1953, 1959; Berce, 1954; Karamata, 1961; Pamic. 1961, 1962a: Trubelja and Sibenik-Studen, 1965; Kneievic, 1967, 1975; Djordjevic and Kneievic, 1972, 1973, 1975; PamiC and Vrhovcid, 1979). Potassium quartz keratophyres can be distinguished from the quartz keratophyres by the presence of K-feldspar, and there is a complete gradation between these two rock types. Pyroclastic rocks are very common and they occur either as interlayers within volcanic flows marking explosive phases of volcanic activity, or as interlayers within Triassic sediments. Two main groups of pyroclastic rocks can be distinguished: (1) Volcanic breccias and agglomerates, which are always associated with volcanic flows, consist of fragments of various volcanic rocks. Larger masses of agglomerates have been studied in detail in northern Montenegro, in the neighbourhood of VareS in Bosnia and on the island Vis (Golub and Vragovic, 1975; Kneievic. 1975; Karamata, 1978). (2) Tuffs are more widespread, and are represented by lithocrystal and crystal

293

varieties

containing

plagioclase in detail,

fragments

(basalt-andesite for example,

the neighbourhood

either of albite (spilite-keratophyre tuffs). Tuffs from many

from the coast of Montenegro

of Fo?a (PamiC and Buzaljko,

Main Triassic magmatic

(Obradovie

tuffs) or of calcic have been described et al., 1972)

from

1976) and elsewhere.

subprovinces

Despite the great diversity of Triassic igneous vinces characterized on the basis of the different within

localities

rocks, seven magmatic subprorock types can be distinguished

the Dinarides:

(1) The spilite-andesite islands. It is connected associated

subprovince of the coast of Montenegro and the Adriatic with the inner margin of the MCP. The volcanics are

with some diabase

(2) The Montenegro

dykes.

andesite-keratophyre-quartz keratophyre subprovince of northern and southeastern Bosnia which can be traced along the strike for about

150 km in frontal parts of the Durmitor nappe. The volcanics are associated with subordinate intrusive rocks: diorites in the neighbourhood of FoEa and on eastern slopes of the Mt. Visitor, granosyenites in the area of Cajnice and various vein rocks on slopes of the Mt. LjubiSna. (3) The andesite-keratophyre subprovince of western and southwestern Serbia and eastern Bosnia which is placed in central parts of the Durmitor nappe. (4) The basalt--spilite subprovince of southeastern and central Bosnia which can be traced along the strike for about with subordinate ophitic dykes are very common.

basalts

100 km. Spilites predominate and scarce

keratophyres

and are associated

and poeneites.

Diabase

(5) The basalt-andesite and spilite-keratophyre-quartz keratophyre subprovince of the middle Dinarides which can be traced along the strike for about 100 km in the area JablanicaaProzor-Vakuf-Jajce. subprovince of the Dinarides because with gabbro,

diorite,

diabase dykes. (6) The basalt-spilite comparatively the Pannonian.

albite

syenite

and albite

subprovince

small and covered

Petrologically it is the most the above mentioned volcanics granite

of Hrvatsko

mostly

and by numerous

zagorje

by Tertiary

heterogeneous are associated

and southern

and Quaternary

swarms

of

Slovenia

is

sediments

of

(7) The dacite-quartz keratophyre subprovince of Slovenia which can be traced along the strike for about 150 km is mainly included within the Sava nappe. Within this group it is possible to include granites and the associated plutonic rocks of the Karawanken Mts. stretching continuously into neighbouring Austria. There are also numerous but small occurrences of various volcanics associated with pyroclastics scattered in some other parts of the Dinarides, as for example, andesite-keratophyres and spilites in Gorski kotar and in the neighbourhood of Senj, diabases and spitites in Dalmatia and elsewhere.

294

GEOCHEMISTRY

It can be concluded different

solidification

Abyssal

that the TMD nearly shows the same variation

trends in three

levels:

level:

gabbro-diorite + quartz-granodiorite-granite albite syenite + quartz-albite granite Hypabyssal

level:

diabase-diorite porphyrin+granodiorite porphyrite albite diabase-albite syenite porphyry-albite granite aplite Extrusive

porphyry

and

albitite

and

level:

basalt-andesite-dacite spilite-keratophyre-quartz keratophyre poeneite-potassium keratophyre-potassium

quartz

The main rock types display great variations and this enables one to consider the comagmatic terms of magmatic rock series. Major-element

keratophyre

in major and trace element contents Triassic igneous rocks as a whole in

geochemistry

The average

major

Table 4. The averages rock analyses. Miyashiro’s (1978)

element

compositions

were obtained diagram

of the main

rock types are given

on the basis of more than 400 available

SiO, against

Na,O

+ K,O

(Fig.

7) illustrates

in

bulk the

transitional character of Triassic igneous rocks. Putting aside volcanic rocks containing albite, it can be seen that the averages of gabbro, diabase, basalt and dacite lie along the line dividing the fields of alkaline and subalkaline rocks, whereas the averages of diorite, andesite, granodiorite, albite syenite and albite granite display a distinct subalkaline character. Miyshiro’s (1974) diagrams (Fig. 8) also illustrate their transitional character. All basic and some intermediate rocks show tholeiitic affinity whereas some intermediate and all acid ones show a distinct talc-alkaline trend. But taken as a whole, the Triassic rock association has essentially talc-alkaline affinities. On the diagram SiO, against

FeO”/MgO

on which

all lines

are steep and subvertical,

they have

295

Fig. 7. (Na,O+

K,O)

a

b

rn 28 3EI

II q

LA

A

50

0

60

l

7+

0

versus SO2 diagram

cl

after Miyashiro

.?/I = albite diabase.

_7(,= diabase.

30 = poeneite,

syenite.

keratophyre.

6h = albite gram&

hu = quartz

c

(197X). Iu = basalt.

4u = andesite.

4h = diorite.

7u = dacite.

Ih = gabbro.

I’(( = spilitr.

.‘cr = keratophyre.

S/J = albite

7h = granodioritc.

trends that are similar to those of typical talc-alkaline rock series of Asame and Amagi (Miyashiro, 1974). The tholeiitic differentiation trends on the same diagram are on the other hand nearly horizontal. The same conclusion can be drawn from his diagram FeO‘ against FeO‘/MgO. The AFM diagram (Fig. 9) is the most diagrams direction

used.

Most

of the (Na,O

It can be concluded with the typical

of the points + K,O)

significant

fall in the centre

apex indicating

all the triangular

a typical talc-alkaline

that the TMD can be correlated

talc-alkaline

among

of the diagram

rock series of convergent

and affinity.

on major element plate margins.

peculiarities, as shown in the weakly pronounced transitional some of the members. The difference is also in the presence

tholeiitic

in the

evidence

But it has its character

of

of some predominant

rock types. as for example spilite-keratophyres and albite granosyenites which are not typical, as a rule, for the magmatic associations of convergent plate margins. Truw-element

geochemistry

The determination of trace elements was carried out on about 150 samples of plutonic and volcanic rocks, and the average contents are given in Table 4. Various diagrams proposed by Pearce and Cann (1973) and Floyd and Winchester (1978)

K,O

(29)

n.d.

B

26

(7)

99.90

1.86

-

1.24

0.15

100.03

1.00

yses

of anal-

Number

Total

CO,

H2O

p205

0.18

2.74

1.03

8.35

3.52

10.84

Na,O

0.19

3.34

5.69

Fe0

Fe203

MgO CaO

Al 203

6.37

18.03

5.14

1.05

5.61

16.49

48.85

SiO

Ti*t

4.41

51.75

1.72

2

1

n.d.

(12)

100.00

0.19

3.29

0.31

1.20

4.50

7.62

4.76

4.18

5.16

17.76

1.24

49.81

3

13

1221

100.16

0.22

2.26

0.22

1.61

3.22

7.07

3.80

3.89

4.13

16.54

1.00

56.14

4

n.d.

(29)

99.87

0.31

2.25

0.19

2.17

4.09

4.38

3.41

2.56

2.90

16.19

0.80

60.55

5

-

2.36

0.43

0.22

7.01

4.78

0.10

0.58

1.45

14.79

0.68

67.62

7

n.d.

(3) n.d.

(3)

100.08 100.03

5.51

0.14

-

0.28

8.06

7.32

0.47

0.10

1.49

16.15

0.84

59.72

6

Average major and trace-element contents of main rock types *

TABLE 4

n.d.

(8)

99.79

0.73

1.15

0.11

2.39

2.88

3.26

1.66

1.79

2.27

15.54

0.71

67.26

8

25

(22)

99.80

0.25

1.78

0.17

1.81

4.06

2.72

2.01

1.I1

2.54

15.71

0.68

66.32

9

8

(22)

100.18

0.50

3.51

0.20

1.43

2.89

9.70

7.73

4.05

3.69

16.78

1.04

48.24

10

26

(60)

99.99

0.33

3.24

0.22

0.80

4.77

6.25

6.04

4.81

4.76

17.34

1.16

50.27

11

29

(151

99.98

0.33

4.16

0.29

3.98

2.53

5.25

6.22

2.70

5.50

17.52

1.02

50.35

12

39

(48)

100.04

0.23

3.26

0.12

1.34

2.89

5.81

3.51

3.24

3.80

16.73

0.67

58.00

13

n.d.

(11)

100.28

0.79

2.05

0.08

1.83

3.42

3.59

1.54

1.59

2.43

15.36

0.45

67.10

14

32

(441

99.93

0.23

2.96

0.14

0.98

5.31

3.30

3.96

3.14

3.84

17.09

0.77

58.19

15

0.19

1.93

0.10

1.02

4.64

1.94

1.91

1.67

2.21

15.63

0.39

68.56

17

n.d.

(12)

41

(25)

100.00 100.10

0.34

2.91

0.14

5.49

2.55

2.15

2.91

1.57

5.09

17.64

0.84

58.27

16

n.d.

(39)

100.11

0.17

1.72

0.12

4.89

3.00

1.32

1.11

1.26

2.14

14.33

0.29

69.70

18

5

n.d.

n.d.

213

(24)

Na-K

quartz

IO-basalt;

* I-gabbro;

ysis

of anal-

Number

14

Y

keratophyre.

11-spilite;

2-diabase;

(8)

13

42

41

Zr

(9)

16

137

208

12--poeneite;

3-albite

n.d.

n.d.

141

n.d.

271

82

195

V

nd.

40

26

17

28

15

n.d.

12

ad.

nd.

12

13

31

13

2

315

n.d.

n.d.

nd.

n.d.

n.d.

n.d.

15

12

13

45

171

26

3

I012

Zn

307

Sr

-

La

33

12

Ga

SC

11

cu

12

100

Cr

28

16

Co

Pb

nd.

Be

Ni

348

Ba

nd. n.d. nd. nd. nd.

n.d. n.d. n.d. nd. n.d.

246

94 _

13-andesite;

diabase;

(20)

25

14-dacite;

syenite:

(16)

26

170

32

30

229

17

15

31

13

12

3

30

9

2

800

IS-keratophyre;

(5)

17

128

-

21

115

6

17

7

-

9

4

15

4

-

750

5-albite

n.d.

nd.

17

4-diorite;

n.d.

n.d.

137

nd.

nd.

S

n.d.

nd.

14

32

n.d.

n.d.

29 n.d.

nd.

n.d.

26

nd.

n.d.

nd.

9

32

n.d.

n.d.

n.d.

nd.

540 _

92

(10)

26

250

110

117

126

29

27

35

I

15

36

141

21

3

840

albitite:

_

n.d.

n.d.

n.d.

n.d.

nd.

nd.

n.d.

n.d.

n.d.

n.d.

n.d.

n.d.

nd.

n.d.

n.d.

nd.

nd.

17-quartz

9-albite

(4)

18-K

and

granite;

n.d.

n.d.

10

n.d. 147

n.d.

n.d. nd.

n.d.

nd. 27

625

n.d.

15 n.d.

120

n.d. n.d.

n.d.

36

n.d.

25 15

n.d.

96

n.d.

3 lb

n.d.

n.d.

keratophyre;

8-granodiorite:

(151

43

352

94

164

n.d. n.d.

200

34

12

17

18

17

26

229

n.d.

n.d.

n.d.

nd.

nd.

n.d.

n.d.

n.d.

18

2

n.d. nd.

385

nd.

keratophyre;

7-quartz

(5)

19

135

16

81

30

15

4

22

10

15

9

209

7

187

and Na-K

albitite;

(21)

16

110

x5

153

16-K

b-calcite

(5)

14

143

16

143

57

23

40

35

24

2

12

27

329

20

1

204

40

7 _

19

273

10

80

b

a ’ SiOz

FeO*

74 -

70

66

62

I 58-

t/

I

TiU,

3

4’0

54.

P

Fig. 8. Diagrams (1914).

Legend

SiU, versus FeO’JMgO

versus FeO-‘/MgO

M!3O

NU,U*K,U Fig. 9. Diagram

(a) and FeO’

is the same as in Fig. 7.

AFM.

Legend

is the same as in Fig. 7_

and TiO, (b) after Miyashiro

299

64

8

t

52 .

CL01

1.00

0.10

Zr ITiO2

I

o*lQ

_ _ -

-

a

4 - - 0

I

5

10

15

20

25 Ga

wm

30

35

45

CO

b

301

have been setting

used in order

and magmatic

The Ti-Zr-Y

to consider

the questions

of magma

origin,

geotectonic

rock series.

diagram

(Pearce

and Cann,

1973) demonstrates

that most of the

Triassic basic volcanics fall in the field of within plate basalts (Fig. 10a). The same diagram was used for basic plutonic and hypabyssal rocks (Fig. lOc), i.e. for the rocks which Pearce and Cann

did not take into consideration;

a well defined

field

was obtained that covers the field of within plate basalts and extends further in the direction of the Ti apex. When the average contents of all Triassic plutonic and volcanic

rocks were plotted

on the same diagram

(Fig. lob),

a coherent

elongated

field was obtained which can be quite well correlated with that in Fig. 10a. The diagram of SiO, versus Zr/TiO, ratio (Winchester and Floyd, 1977; Floyd and Winchester, 1978) shows that the Triassic spilites partially fall in the field of basalts and partially in the field of andesites (Fig. lla). Consequently, one might presume

that

interesting

spilites

to note

might

that

have

the data

originated

from

for the average

basalts

and

Triassic

andesites.

plutonic

rocks

It is can be

correlated with the ones of volcanic equivalents. Their diagram Zr/TiO, versus Ga the points of spilites are located in the points mainly to the same conclusion; adjoining area of basalts and andesites. The trace-element diagrams presented here thus favour the conclusion that the igneous rocks of the TMD represent a peculiar rock association of talc-alkaline affinity which is, however, genetically related to the stable continental realms. DISCUSSION

The Triassic igneous rocks of the Dinarides are connected with a rifting episode of some 50 Ma duration which preceeded the opening of the Dinaridic part of the Tethys. The rifting processes took place in the Hercynian basement and they represent a part of contemporaneous rift events that took place in many other parts of Pangaea

(e.g., the Oslo graben-Oftedahl,

rift magmatism continental

coincide

1978). The last phases of the Dinaridic

with the first stages of the Atlantic

rift structures

all around

the Atlantic

margin

rifting (Burke,

which left relict 1976). Magmatic

rock associations of these and many identical areas mostly display a weak to strong alkaline affinity, as distinct from the ones of some continental rift structures which exhibit distinct tholeiitic to talc-alkaline affinities (Neumann and Ramberg, 1978). The Triassic magmatic association of the Dinarides is mostly of talc-alkaline affinity and shows a great variation in mineral and chemical composition, The

Fig. 11. Diagrams and

Floyd

2 -alkaline cite.

Zr/TiO,

versus SiO, (a) and Ga (b) after Floyd and Winchester

(1977).

Legend

basalt.

3 -bazanite,

8-ttrachyte.

2 -ttrachyandesite,

is the same

9-comendite 3 -dacite

as in Fig. 7. The left (a) diagram:

4 -andesite. and

5-ttrachyandesite.

pantelerite,

and rhyodacite,

IO-rhyolite.

4 --rhyolite,

6 -phonolite, The

S-pantelerite.

right

(1978) and Winchester I -sub-alkaline P-dacite

(b) diagram:

6 -phonolite

basalt.

and rhyoda1 -andesite. and trachyte.

302

question

is how to explain

such a diversity.

Bowen (1928) explains

the same and similar

zation

magma,

from a primary

also used in the genetic the Dinarides

(Pamic,

Most recently explained

commonly

interpretation

of partial

advanced

by fractional

composition.

volcanic

1969; Kneievic.

trend of the Dinaridic

melting

petrology

trends

of a basalt

of Triassic

1962a; Grafenauer,

the great variation

as a result

Traditional variation

by

crystalli-

This idea was

rocks from some parts of 1975). Triassic

of rocks of the earth

rocks has been

crust and/or

upper

mantle (Pamic, 1979). The conclusion is strongly supported by data from experimental petrology (Green and Ringwood, 1969; Boettcher, 1973 and others) and by some field relationships. It has been found that many intrusive and extrusive bodies are made up of only a single rock type, for example, of gabbro, andesite, or of plagiogranite pointing to the presumption that magmas of such compositions must have existed before their emplacement. In addition, the Miyashiro’s SiO,-FeO’/MgO diagram, commonly used as an indicator of the degree of differentiation, rock

shows

types.

that there is a definite

This

was

plagiogranite bodies definite composition

exemplified

relationship

by

the

between

nearly

all separated

gabbro-diorite-albiteesyenite

and

of Mt. Radovan, and it was presumed that each magma of a must have evolved independently (Pamic, 1979). Trace-element

contents, and particularly the metallogenetic diversity also strongly favour the idea of partial melting.

of the Triassic

magmatism,

It is very probable that each solidification level had its own peculiarities shown in some differences in the mineral composition. Amphibole is the most characteristic mafic mineral of intrusive rocks as distinguished from augite of extrusive rocks. This is probably caused by the difference in the content and pressure of water during crystallization. The composition of the volcanic rocks must have been influenced by a stronger contamination because of a longer transport of magmas on their way to the surface. This basically implies the contamination by elastic and particularly by carbonate having

country

given rise to a significant

Consequently, partial

rocks shown in the increased

melting.

the basic

quantity

of calcite

and amygdales

desilification.

diversity

of the TMD

Other processes (crystallization

must have played a secondary role. The diversity of the Triassic igneous

is fundamentally

conditions,

contamination

rocks of the Dinarides

influenced

by

and others)

must also have been

influenced by late-magmatic and post-magmatic processes. But before considering that, it must be stressed that some Triassic igneous rocks, although having the same mineral and chemical composition, originated at different solidification levels, as for example, diorite-dioriteporphyrite-andesite, albite syenite-albite syeniteporphyre-keratophyre and others. In such a situation it would be quite erroneous to separate only extrusive rocks with their genetic problem of albite origin from the mineralogically identical intrusive ones because different kinds of transformation are nearly equally reflected in both groups of rocks. Could we, for example, decisively state that all Triassic spilites and keratophyres originated by albitization of basalts

303

and andesites diabase,

when the latter,

albite

comparatively In single

of the

fact

of primary

genetic

the albitite

and

are associated albitite

at hypabyssal

veins,

and

in the

level by albite abyssal

one

by

larger bodies of albite syenite?

spite

albitization

in turn,

syeniteporphyre that

some

basalts

explanation,

of the

(Pamic,

as demonstrated

veins a few metres

evident

that

the genesis

spilites

by Amstutz

thick strongly

melts enriched in the albite component. lents of rocks of the spilite-keratophyre the TMD. It is quite

Triassic

originated

1982b), it seems at present suggests

from

the

that there is no

(1974). The occurrence

of

the idea of the existence

of

In addition, association

abyssal and hypabyssal equivaare very common products of

of Triassic

albite-bearing

volcanics

of the

Dinarides is much more complex then has been thought. It is possible that in this particular case there may exist “spilites and spilites” and “keratophyres and keratophyres”, or taking the volcanic and intrusive products of the TMD as a whole it is quite conceivable that there are “albites and albites”. But it must be said realistically that the question of albite genesis only represents a part of the very complex

petrogenesis

of the TMD,

and it will be discussed

in detail elsewhere.

ACKNOWLEDGMENT

The author is indebted to Drs. M. Herak of the Zagreb University, of the State University of New York and J.A. Pearce of the Open critical reading of a draft of the manuscript.

A. Miyashiro University for

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