Examples of strike-slip tectonics on platform-basin margins

293

~~~O~~~~~~jC~, 156 (1988) 293-302 Elsevier Science Publishers B.V., Amsterdam - Printed in The Netherlands

Examples of strike-ship tectonics on p~at~~r~-~asin margins CARLO DOGLIONI

(Received October 1,1987; revised version accepted April 18, 1988)

Abstract Doglioni, C., 1988. Examples of strike-slip tectonics on platfo~-baby

margins. ~~crono~~,vs~cs,1%: 293-302.

Examples from the Southern Alps (North Italy) serve to illustrate the use of carbonate platform-basin relations to recognize strike-slip tectonics and to estimate amounts of displa~ments~ It is noted that two~dimensionai cross-sections across strike-slip faults cannot be balanced and three-dimensional reconstructions would be necessary to restore original p~~g~~ap~c shapes of platfo~-basin margins. The main ~haract~stics of strike-slip tectonics are: (a} tectonic omission of fragments of the original t%rbonate platform-basin system in tw~dimens~ona~ section; fb) subvertical dip of the fault; (c)juxtaposition of differing thicknesses and facies of equivalent formations across faults, when these differences cannot be explained by normal growth faults; (d) anomalous tectonic wedging of subvertical basinal ductile sediments in the core of the carbonate platform. Normal faults cutting inclined slope margins may simulate apparent horizontal displacements. Platfo~-basin margins influence ~~R-S~M~ thrust tectonics in that overthrust ramps may be guided by clinoforms, and oblique or lateral ramps may develop along margins that are at an angSe of O”-70* to the main compressional axis.

Introdnction The Southern Alps (North Italy) exhibit excellent examples of Triassic platform-basin relationships, e.g., in the Dolomites (Bosellini, 1984). Platform-basin margins are mechanical dishomogeneities that influence later tectonics in all kinds of structural regimes. Moreover their articulate shape may help to unrave1 the kinematic evolution of a region. This paper aims at illustrating two particul~ly striking examples (the Passe Feudo and Raibl structures) of strike-slip tectonics affecting carbonate platforms margins, The Passo Feudo example

The Neogene S-verging Valsugana overthrust is overlain by a huge basement syncline. Well pre~#-195~/8g/$~3.50

@ 1988 Elsevier Science Publishers B.V.

served within that syncline are the classical Triassic sequences of the Dolomites (Leonardi, 1967; Bose&n, 1984). These are characterized by 800-1000 m thick carbonate platforms (Bosellini and Rossi, 1974), equivalent basinal formations, and by igneous complexes emplaced during a 217-230 m.y. old magmatic event (Lucchini et al., 1982). Middle Triassic structural deformation has been reported from the Dolomites (Cros, 1974; Pisa et al., 1979; Bosellini et al., 1982; Castellarin et al., 1982a, b; Doglioni, 1982; 1984a, b). These structures have been recently interpreted as being due to sinistral strike-slip along a N70 “E alignment known as the Stava fault and the northern limb of the Cima Bocche Anticline (Fig. 1 and Doglioni, 1984~1,b). A Middle Triassic age of deformation has been proven by (1) Late Ladinian volcanic dykes cutting pre-existing folds and faults, (2) the intrusion of the Predazzo and Monzoni plutonic

F‘ig. 1. Schematic

gtwlogic

C‘rma Bocche Anticline

map of the central

of the cross-section

as shown

carbonate

4 = Ladinian

platform;

Western

Dolomitrs.

trend is cut by the Late Ladinian-Early on Fig.

3. I = Quaternary

Note that the Middle-Triaaaic

Camian cover;

Staw

Predavo

and Monzoni

magmatlc

.? = Upper

Ladinian-Early

Car&n

Livinallongo Formation (hasinal faciea); .F = Anixan. Scvthian 6 = Permian volcanies; ? ==crystalline basement.

bodies along the N70” E alignment, and (3) volcaniclastic Ladinian and Camian deposits covering unconformably pre-existing overthrusts, folds and diapiric anticlines (Fig. 2). The Passe Feudo structure

The Passo Feudo structure (Fig. 3) is located in the western Dolomites (Fig. 1) along the Stava alignment. Positive flower structures have been described between the Stava and Trodena faults (Dogiioni, 1984a). East of Passe Feudo, the Stava Line is cut by the Upper Ladinian Predazzo magmatic body, proving the Middle Triassic age of that line. To the west, the Stava line joins with the Trodena line. The dip of the Stava fault changes

Line--northern centers.

‘4-A’

volcanics:

and Upper

Permian

limb of the ih the trace .i = Ladinian formations:

along strike, a common feature of wrench faults (e.g. Harding and Lowell, 1979). The most important observations on the Stava fault in the area shown as Fig. 3 are: (1) The Stava fault dips X5o to the north suggesting an uplifted hangingwall: (2) basinal sediments (Livinallongo Formation) are vertical on the north side of the fault and attached to the sub-horizontal undeformed core of the co-eval Ladinian carbonate platform (Marmolada Limestone); (3) the same basinal Livinaliongo Formation is thinner underneath the subhorizontal platform than in the vertical slice that is associated with the Stava fault; (4) Anisian Eacies and thicknesses differ on both sides of the Stava fault. i.e. the Moena Formation (basinal debris-flows) to the north and the Lower Serla and

295

Fig. 2. San Nicolo valley, central overlapping Permian

and “sealing” Bellerophon

unconformably

of volcanics

Werfen

formation

Conglomerato corresponding are aligned

Formation,

by an Upper

pebbles

and limestone. Marmolada

the N70°E

at the right)

conglomerate,

In the photograph (M).

Contrin The

of the Cima Bocche Anticline.

In this valley

not visible

(IV) and the Anisian

della

northward

tectonics.

Ladinian

to the outcropping along

Dolomites,

Ladinian

a diapiric and

the so-called

fault

Caotico

diapiric

(A) beneath

anticline

belt Stava fault and the northern Stava

the Lower

we see the northern

formation

and positive

Triassic

has

been

(CE).

eroded

are common.

and

anticline on

unconformity

in the core (Upper

subsequently

involving

The CE is overlain

superimposed

of the underlying

and shales

The CE is a debris

limb of the diapiric the unconformity.

of a Middle Triassic

gypsum

limb of the Cima Bocche anticline.

transpression

Contrin Formation (platform limestones) to the south (C. Net-i, pers. commun., 1987); (5) a cross section across the Stava fault cannot be balanced; (6) the thicknesses of two Ladinian carbonate platforms on either side of the fault differ by about 300 m, i.e. about 1000 m at M. Agnello, and 700 m at Latemar (R. Goldhammer, pers. commun., 1987); (7) Late Ladinian volcanic dykes cut the deformation. In the field these dykes clearly cut the chevron folds of the Livinallongo Formation at Passo Feudo. However, later Alpine folding deforms dykes as well as folds near the Stava line; (8) the chevron folds have an inclined axis and an en-echelon disposition with respect to the left-lateral Stava fault; (9) combined field map and facies analysis suggests that the Latemar platform to the north of the Stava fault apparently is displaced by 4-5 km from another platform fragment that is located on the south-side of the fault farther east (M. Harris, pers. commun., 1986).

An example

involving

eterogeneo

is presumably

flower geometries

(1984a, b) as due to sinistral

anticline

covered

flow that contains the lower Scythian

by the volcaniclastic

a deep-seated

basement

Many such diapiric

These have been interpreted

fault

anticlines

by Doglioni

basement.

These observations lead to the following conclusions: (a) The deformation observed on both sides of the fault (i.e. vertical basinal facies and horizontal co-eval platform) cannot be interpreted in terms of either normal faults or else thrust faults (Fig. 7); needless to say, a simple cross section across the fault cannot be reconstructed in a balanced cross section; (b) the above-mentioned situation suggests strike-slip faulting; (c) the different carbonate platform thicknesses on either side of the strike slip fault (Agnello and Latemar) suggest that the fault was also active during the Ladinian with a Stava strike-slip fault separating two different subsidence domains (Doglioni, 1984a; R. Goldhammer, pers. commun., 1987); (d) accepting an original sub-circular shape of the Ladinian Agnello platform (Fig. 1) we can imagine that the sub-vertical Livinallongo beds associated with the Stava fault were located in a basin that was originally to the east of the Agnello

S LINE M. Agnello

I km Fig. 3. Cross section

across

Stava fault line (for tocation

dimensions,

A two-dimensional

cross section

(Liu)

interrupt

parts

that

LP-Ladinian volcanic

different

carbonate

dykes;

platform;

PC-Upper

Formation

and

Lower

B-Upper

Permian

Serla

Dolomite

see Fig. 1). Obviously,

a strike-slip

of the essentially Lit+-Ladinian

Ladinian

Bellerophon

across

horizontal

Livinallongo

lavas and volcaniclastics; (footwdl

Formation: volcanic

fault cannot

of Stava V-Upper

carbonate Formation

A -Upper fault,

Permian

Neri,

platform (Fig. 8A); such a sinistrai displacement along the Stava fault is further supported by the orientation of the en-echelon overthrusts and associated Riedel wedges, as well as by flower structures and striations (for this documentation see Doglioni, 1984a, b); and (e) the facies analysis of the Ladinian involved in the fault-ass~iated structures is therefore quite important for the kinematic understanding of these structures. Thus, Ladinian strike-slip tectonics are strongly supported by several observations. Earlier, Anisian movements have been postulated by Brandner (1984), Doglioni (1984a), and C. Neri (pers. commun., 1987). Even Permian deformation was proposed by Pichler (1962). In this perspective therefore it can be concluded that the Late Ladinian displacements re-activated pre-existing weakness zones. En-echelon overthrusts and other structures associated with the Passo Feudo structure (Pisa et

platform (heteropic

Anisian pets.

Moena

commun.,

Val Gardena

dykes have been omitted

this section

be balanced.

could

only be reconstructed

Note the vertical (LP).

For

equivalent

Sandstones:

further (north

Formation

discussion

of the platform);

formation 1987):

in three

Livinallogo

see text. D-Ladinian

of Stava fault), Contrin

W-Scythian

Werfen

P-Permian

ignimbrites.

Formation: Several

from the cross section.

al., 1979; Bosellini et al., 1982; Castellarin et al., 1982a. b; Doglioni, 1982; 1984a, b; 1985; 1987) all suggest that the Middle Triassic deformation of the Dolomites is due to sinistral transpression across a N70 “E direction (Doglioni, 1984a; R. Brandner, pers. commun., 1984). This transpression coincides with rna~rn~ subsidence rates in the area, which in turn are reflected by the growth of thick carbonate platforms. Local transpressions of this type are understood within the context of a general transtensive environment (Bernoulli, 1985). Overall Mesozoic sinistral strike-slip tectonics have been postulated for the Southern Alps by Doglioni (1984a) because the main Mesosoic swells and basins have an en-echelon orientation with respect to the proposed N70’E transpressional orientation (e.g. the NNE trends reported by BoseIIini, 1965). What is the geodynamic significance of the Triassic strike-slip tectonics observed in the

297

The overall stratigraphic and structural setting is best illustrated by a N-S cross section, located just to the east of the N-S strike-slip faults. On this section (Fig. 4) we note Middle and Late Triassic carbonate platforms prograding in different directions, often oblique to the orientation of the cross section. A map showing the Ladinian platform-slope-basin relationships, strongly suggests strike-slip movements (Fig. 5) which had been proposed by Di Cobertaldo (1948). Strike-slip movements are widely confirmed by horizontal striations both dextral and sinistral on N-S striking faults. On E-W cross-sections flower structures are very common (Fig. 6). From the preceding discussions it may be concluded that displaced platform-basin margins are particularly useful markers to indicate strike-slip displacement. Of course, two-dimensional sections across flower structures cannot be properly balanced but the discordant juxtaposition of co-eval platform and basin sediments across strike-slip faults is very characteristic. Platform basin margins are typically irregular and often very articulated (i.e. lobes, tongues, emba~ents etc.) and therefore paleogeographic restorations across strike-slip

Dolor&es? Taking a much wider view we can see that Africa and Europe were separated by sinistral transform faults, e.g. the Newfoun~and-foresGibraltar fracture zone (i.e. see Dewey et al., 1973; Brandner, 1984; Masson and Miles, 1986; Ziegler, 1987). Thus we view the segment of the southern Alps as a link between the transform domain of the opening Atlantic Ocean and the subduction domain of the Triassic Paleotethys beneath the Eurasian continental crust (see Sengijr et al., 1984; Ziegler, 1987). The Raibl example The famous Pb/Zn ore deposit of Raibl (Brig0 and Omenetto, 1979) is located in the Eastern Alps near the point where the boundaries of Austria, Yugoslavia, and Italy meet (Fig. 1). Raibl is just to the south of two import~t Neogene Alpine dextral transpressive faults: the Fella-Sava line and the Gail line (i.e. the eastern segment of the Insubric lineament). In this area N-S trending sinistral strike-slip faults that are viewed as antithetic Riedel shears to the Fella-Sava line, cross the Raibl valley.

N

Cinque

k _ Fig. 4. N-S cross section of the eastern Raibl area showing Middle-Late directions (both southward and northw~d). Ignimbrites; P-Calcare in age); DP-Dolomia

de1 Predil; R-Rio

S

M. Guarda

Punte

Dh4-Dolomia

Me~fera

de1 Lago Formation;

I

Triassic platforms and basins prograding in different

(Ladinian); B-basinal

C-Comen

I km

Buchenstein Formation, Rio Freddo

Dolomite; Z+--Tor Formation (P, R, C, T, Camian

Principale (Late Camian to Norian). The slope of the Dolomia Metalhfera (DM) is oriented about N55 o W, i.e. at an angle to the cross section. Its defomration is illustrated on Fig. 5.

29X

to multiple ceivable

Early Carnian

Brigo,

interpretations.

(see Assereto 1973) that

For instance,

et al., 1968; Assereto

syn-sedimentary

could have disrupted

the platform

one must

that

remember

could

Late Triassic

also be interpreted

that case, additional

structural valley

fault planes,

margin;

faulted

are in

subvertical

striations

monocline.

that

fault. In

observations

a few N-S

(in by a

a map picture

in fact, show normal

tilted by the regional

faults

surface

as a strike-slip

order;

in the Raibl

basinal

margin)

fault, may well provide

and

normal

an oblique

this case, the platform-basin normal

it is con-

slowly

We conclude

that

we have to be cautious when calculating strike-slip displacements in the possible presence of normal faults that intersect complex basin-margin shapes. Applied to the Raibl mining district this means that a pronounced re-entrant could have modified the overall ESE-WNW platform-basin margin. Thus normal faults would simulate an apparent dextral movement in the eastern part of the re-entrant and a sinistral displacement in the other side (Fig. 5). Be this as it may, in the Raibl area sinistral Neogene (South Alpine trend) faults are associated with NO “-30 o E striking faults and probably dextral Paleogene (Dinaric trends) (NO ’ -40 o E) strike-slip faults that intersected the platform-basin margin. Even allowing for synsedimentary Triassic normal faults and a lobate platform margin, the platform-basin margins can still be used to assess approximate Tertiary strike2 km

slip displacements. Fig. 5. Speculative the Raibl

area

distribution platform

sketch

based

maps of the structural

on structural

of platform-basin developed

(black arrows).

facies.

A re-entrant

area

extension:

horizontal

during

displacements.

sinistral trends. provides

in the form the

Neogene,

strike-slip Note

and/or

normal

times the old zone of weakness tectonics

During

was probably

the Late Triassic

parent

evolution

and

how

an useful

main

faulting

tectonic

also produced

took

strike-slip

South place

the platform-basin reference

in the Raibl

Much later during

of a dextral the

present

was re-activated

for

Alpine along margin

a

Tectonics

of carbonate

platform

margins

in the

Dolomites

progradation

the Early Jurassic

faulting

of

the present

the Ladinian,

with an overall south-dipping

valley; during suffered

analysis

the ap-

Paleogene

during

Dinaric

fault.

Finally

deformation the old

fault

configuration

the reconstruction

of the

evolution.

faults must keep into account, as much as possible, the original platform shape. Furthermore, restorations that are based only on maps are subject

On

a map,

Dolomites

the

carbonate

are irregular

platforms

with many

curved,

of the elon-

gated and arcuate re-entrants and promontories (Bosellini, 1984). Carbonate platforms are typically composed of competent massive limestones and dolomites, while incompetent lithologies of well-bedded limestones, marls and shales are characteristic for the off-platform basins. This leads to the observation that, in general, platforms are more protected from the effects of compressional tectonics than the adjacent basins (Leonardi, 1967). Not surprisingly, platform slopes are then preferred positions for overthrust-related ramp

299

Fig. 6. Positive flower structure in the Ladinian carbonate platform of Raibl (Dolomia Metallifera) that is related to a N-S trending sinistral Neogene shear zone. Photograph taken of the western cliffs of the Cinque Punte mountain.

structures. Thus, clinoforms associated with prograding sequences (Bosellini, 1984) are being used as ramps for overthrusts (Doglioni, 1985). Schematically a platform-basin sequence may be deformed by three tectonic processes i.e. extension, strike-slip and compression. Figure 7 illustrates that both compression and extension permits construction of balanced cross sections and reconstructions. On the other hand strike-faults do

not allow for simple Z-D balancing. Instead, strike-slip tectonics can only be reconstructed if one allows for the third dimension. Note therefore, in the strike-slip diagram, (Fig. 7) that the platform margin has been omitted and that the basinal facies has no equivalent on the right side of the fault. Figure 7 is only schematic, but the strike-slip illustration applies particularly well to the Passo Feudo structure that is located along the

Fig. 7. Cartoons showing, in principle, how different types of deformation may affect a carbonate platfo~-b~in margin; normal faulting or thrusting produce restorable cross-sections; note that thrusting can follow pre-existing clinoforms; strike-slip displacements produce a cross section that typically cannot be balanced on two-dimensional cross sections. Note that on this diagram the distal wedge of the platform is missing and that basinal sediments are directly juxtaposed across the fault plane.

Latemar

3 km _--_~-

Fig. 8. Two examples

of tectonics

Feudo

structure

(north

thrust

tectonics:

oblique

Paleogene

structure

deforming

platform-basin

to the left). The Late Ladinian and lateral

(north

ramps

at the right)

may occur where

margins.

magmatism

at the platform

the structure

fault,

i.e. a sinistral

Triassic

transpressive

tectonics;

along

margins;

is further

explanations

Stava

A. Strike-slip occurred

this example

could explain

this example

complicated

could

by later

be applied

Neogene

The Passo

Feudo

and Raibl

placement

fine example

a few kilometers

of strike-tectonics

(Fig. 8A).

to faulting

has

been the subject of many recent papers, particularly some that were illustrated by seismic profiles (Harding and Lowell, 1979; Reading, 1980; 1982; Harding, 1985). In the Passo Feudo case, criteria indicating strike-slip tectonics include the distribution of basinal sediments with respect to the platform core, their vertical attitude and differing thicknesses of basinal sediments on either side of the fault, omission of platform segments on profiles and the subvertical attitude of the fault. Platform-basin relations offer useful regional tectonic insights and may suggest amounts of displacements particularly if the original shape of the platform can be inferred with confidence.

For

further

see text.

structive examples of strike-slip across carbonate platform-basin

of perhaps

to the Falzarego

tectonics.

fault. As previously stated, the Passo Feudo structure can only be explained by a strike-slip disThe relationship

the Passo

the shear zone in a later event. B. Thin-skinned

is the Ladinian

situations

are in-

tectonics cutting settings. Another

Costabella

platform

that has also been intersected by the Stava fault in the Dolor&es (Doglioni, 1984b). In the Falzarego area of the central Dolomites. W-vergent Dinaric (probably Paleogene in age) thrusts shortened the sedimentary cover (Doglioni, 1987). In that area the paleogeographic setting influences thrust planes: lateral and oblique ramps are developed along platform-basin margins (Fig. 8B) both in the hangingwall and in the footwall. We can consider a lateral ramp as a superficial strike-slip (tear) fault. In the Falzarego structure a WSW-vergent, N30” W trending overthrust placed a Camian platform (Lagazuoi) over another Camian platform (Sass0 di Stria). The overthrust continues into an oblique and lateral ramp at the southern

301

platform stance

margins

and

at a point

changes

into

were

can

the strike

a N90”-1OO”E

Falzarego

valley.

tectonics

overprinted

The

be observed

later

for in-

Acknowledgements

of the thrust

direction S-vergent

along

the

Neogene

Thanks

to A.W. Bally, A. Bosellini,

Trtimpy

and two anonymous

cal reading

this geometry.

text. Thanks

the useful

suggestions

Lallemant,

D. Bernoulli,

toration

of the paleogeography

forms and basins, sion

across strike-slip faults require analysis for an adequate res-

of the

Passo

of carbonate

as we indicated Feudo

and

plat-

with the discusRaibl

examples.

Platform-basin relations may be very useful to estimate the amount of displacement along strikeslip faults. In the two cases presented in this paper the main features indicative of strike-slip faulting are: (1) the subvertical dip of the fault, which cannot be explained normal fault;

in context of a thrust fault (2) the omission of significant

or a por-

tion of the platform on two-dimensional cross sections; (3) vertical dips in basinal sediments along the fault and their anomalous position with respect to the core of the platform. (4) The platform cores are offset. (5) Widely different thicknesses and facies on either sides of the fault that cannot be explained in terms of a normal growth fault. Normal faults may cut inclined platformslope margins and with inadequate outcrops suggest apparent horizontal displacements. It is noted that thin-skinned may be associated with oblique

thrust tectonics or lateral ramps

along platform-basin margins that are oriented at an angle of 0 “-70 ’ with respect to the main compressional axis. Finally, at least conceptually, it can be imagined that during the development of platformbasin margin complexes the syn-sedimentary response to strike-slip faulting may well lead to platform developments in transpressional settings (or push together, A.W. Bally, pers. commun., 1988) and the drowning of platforms and/or the formation small basins coinciding with pull-apart segments: these paleogeographic elements can invert their nature along the path of undulate strike-slip zones.

M. Harris,

A. Castellarin,

H.P. Laubscher,

M. Zerbato.

Italian

AvC

G.V. Dal L. Hardie,

D. Masetti,

F. Massari,

J. Platt, D. Rossi, F. Sabat

Supported

Minister0

for

H.G.

R. Goldhammer,

C. Neri, P. Omenetto, and

also to the following or discussions:

Piaz, M. Friedman, Reconstructions a three-dimensional

for the criti-

of the text. A.W. Bally also re-edited

the English Concluding remarks

L. Brigo, R.

referees

della

by a grant

Pubblica

from the

Istruzione

(40%

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