RENDICONTl DELLA SOCIETA ITALlANA 01 MINERALOGtA. E PETROLOGIA, 1989. VQI. 43.3. pp. 817.S29

Late hercynian intrusives from the Southern Cataloniancoastal ranges (NE Spain), and their epiplutonic

to subvolcanic level of magma emplacement

PERE RAMON SERRA, PERE ENRlQUE

Dpt. Geoquirnica, Petrologia y Prospecd6 GeolOgica. Facultat de Geologia.Universitat de Barcelona. Zona Universitaria de Pedralbes, 08028 . BARCELONA

ABSTRACT. _ The intrusive from the southernCatalonian Coastal Ranges form a Late.Hercynian I-typecalc·alkaline association with a set of features that suggestthey wen: emplaced in a very low-pressure, subvolcanicenvironmem. These inferences are based on thefollowing evidence: (i) the contact of the plutonics withtheir host·rock is sharp, cross.cutting and angular.to-polygonal in morphology; (ii) the plutons are roofed bytheir host with subhorizontal contact surfaces turninginto steeply dipping ones towards the border of theplucons; (iii) the host-rock is an anchimetamorphicsedimentary sequence with well.developed contactmetamorphic aureoles around the intrusions; (iv) theolder plutonic units have normal equigranular textures,whereas the younger ones are mostly inequigranular andtypically developed well·defined chilled margins in thecomact with their host: (v) miarolitic cavities are scarcebut widespn:ad; (vi) the dyke-swarm accompanying theplutons is very weU developed and in some areas isparticularly dense: (vii) columnar joiming of hexagonalsymmetry is present in some dykes: (viii) explosivehreccias are scarce but their occurrence is regularthroughout the complex.

The following conclusions are drawn from all theseobservations: (i) the environmem of magma emplacementwas suhvoleanic (pn:sence of breedas and columnarjointing) and brittle; (ii) this environment was inprominent thermal disharmony with the intrudingmagma; and (iii) the present.day outcrop levelcorresponds to the top of the complex.

Although magma venting cannot be demonstrated (norelated volcanic cover is present), it cannot be rejected,since it is compatible with observed relationships andcoincides in age (Stephano-Permian) with those of thewell·known calc·a1kaline volcanism occurring in severalplaces of the Hercynian fold·belt.

Mineral indicators reveal that the magmas were dryand hot enough to have a deep source and to ascend doseto the surface.

Key words: magma emplacement, subvoleanicenvironment, plutons, Late-Hercynian, cale-alkaline.

LES INTRUSIONS TARDI·HERCYNIENNES DELA PARTIE SUD DES CHAiNES COTIERESCATALANNES (NE DE L'ESPAGNE), ET SONNIVEAU DE MISE EN PLACE EPIPLUTONIQUEA SUBVOLCANIQUE

ReSUME: - Les roches intrusives de la partie Sud desChaines C6tihcs Catalannes constituent une associationcalco·alealine tardi.hercynienne. Ceue associationpr6ente des caracteristique typiques d'une mise en placesous conditions de pression faible, possihlementsuhvolcanique. Toutefois, il faut noter I'ahsence d'unecouverture voleanique en liason. Si celte couverturevoleanique a existe, elle a du, sans doute, ctre demameleepar I'erosion.

Les prindpaux arguments appuyant celte hypothesesont les suivants: (j) les contacts entre les plutons et leutencaissant sont tres nelS, recoupant les structures de cedemier et montrant des formes angulaires; (ii) parendroits, il est possible d'ohserver I'encaissant formantle chapeau des plutons et reposant sur des surfacespresque horizontales qui deviennent brusquementinclinees vets la hordure des masses pluconiques; (iii)I'encaissant est forme par une serie sedimentaireanchimetamorphique qui developpe des aureoles decontact autour des intrusions; (iv) les plutons les plusanciens montrem des fades avec des texturesisogranulain:s alors que les plus tardifs sont formes defades 11. texture heterogranulaire montrant des horduresfigm au contact de I'encaissant; (v) la presence de cavitesmiarolitiques est generalisee; (vi) il existe un cortegefilonien associe tres important et dans certaines zonessa distribution est particulierement dense; (vii) certainsfilons montrent une prismat ion neue; (viii) la presencede breches d'explosion regulierement distrihuees dansla complexe est indicative d'une pression lithostatiqueassez faible et inferieur ). la pression des fluides.

Toutes ccs relations mettent en boidence: (i) un niveaud~ mise en place suhvolcanique (presence de hrkhes etde prismation); (ii) l'existence d'un fort contraste detemperature entre le magma ascendam et son encaissant,et (iii) un niveau d'exposition qui correspond au toit ducomplexe.

818 P.R. SERkA. P. ENRIQUE

Tout en reconaissanr qu'iJ n'est pas possibk de:demontn:r I'existence d'un volcanismc local aS$OCii:(absence de couvcrtU«' volc.niq~ rapporlee), on ne pcUlpas non plus ]'ecarter car [',ge Stephano.Pcrmien desintrusions ooincide avcc celle du volcanisme calco'lIkaJinqui est dej. I;Ollnue dans la Chainc Hercynicnnc.

I...c:s lracrors minCnIogiqucs suggerenl ['existence d'unou de plusieurs magmas d'origim: profondc sumsamenrsecs Cl 11 temperature ~lcv«-: capable de montcr • des11'''','''' (ri's sup..-rficicls

Moll def mise en place, environ subvolcanique,1,IUlons, tardi.hercynicn, caJco-aJc.lin.

5Km

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LATE HERCYNIAN INTRUSIVES FROM THE SOUTHERN CATALONIAN COASTAL RANGES. ETC. 819

lntroduc:tion

This pa~r deals with the Late Hercynianintrusive complex occurring in the SouthernCatalonian Coastal Ranges, including all thosetopics that are directly involved in their wayof building-up to level of final emplacement.Chiefly, these subjectes are: the distinctionamong different types of intrusions presentin the area, their sha~s and sizes, theirrelationships with the wall-rock on bothcontact and regional scales, their relativechronology of intrusion, the structures theydevelop, related bcecciation processes, and thetextural and mineralogical indicators of theirevolution.

All these observations not only confirm thehigh crustal level of emplacement of theCatalonian Coastal Ranges granitoids(ENRlQuE, 1984) but also clearly establish, forthe first time in the area, the fact that theintrusives reached a subvo!canic level.

Consequently. the studied complex mayhave rooted a v.olcanic association ofStephano-Permian age. similar to otherwidespread throughout the Hercynian fold-belt. although related volcanics have neverbeen found (for reasons outlined later).However caution must be taken whenconsidering the actual occurrence of magmaventing.

Geological set/ing

The complex examined here is an l-ty~calc-alkaline association of Late Hercynian agechat occurs in the Paleozoic basement of theSouthern Catalonian Coastal Ranged (Fig. O.unconformably covered by subhorizontal togently dipping Triassic sediments.

The Catalonian Coastal Ranges form a 250K~-Iong alignment of homs and grabens,with a NE-SW trend, parallel to the norch·eastern corner of the Iberian Peninsulashoreline.

Although the nature of the host of theintrusions will be outlined here. the reader isreferred to the previous works on the region(ASHAUER and TEICHMULLER. 1935;FONT BOTE and }ULIVERT. 1982; andMELGAREJo. 1987) for more detailed

information.According to the last author. the wall-rock

is a sedimentary sequence ranging fromOrdovician to Carboniferous in age, t~ lattercovering most of the area. A discordancebetween pre-Carboniferous and CarOOniferousformations distinguishes a spatially limitedbasal unit with a complex structure from anoverlying one characterized by NNW-SSE -trending intra·Carboniferous fold with a largeradius of curvature. A subsequent brittlephase formed a dominant NE-SW - trendingfracture system constituting the main dyke-bearing fracture family in the area (see later).

The outcrop of the intrusions is a roofexposition of the magma chambers. Theirhighest exposed stratigraphic level isanchimetamorphic Westphalian. made up ofdetricic. essentially turbidicic materials.

The complex consists of several plutonicbodies accompanied by a dense dyke-swarm.The plutonics have a batholithic multipleintrusion nature and are surrounded bycontact metamorphic aureoles that, at leastin some places in their inner parts. reach thepyroxene hornfds fades.

Volcanics related to the intrusives arelacking in the complex.

Since its age is Stephano-Permian (asevidenced by unpublished Rb-Sr isochrons.DEL MORO & SERRA). and since theWestphalian is the highest stratigraphic leveloutcropping in the area, erosion may be thereason for the non-presence of volanics, if theyever exisced. It must be borne in mind.however, that calc-alkaline volcanics of thesame age are widespread throughout theHercynian fold-belt and that their nearestoccurrence is in the Pyrenees.

Contact relationships. shape of plutons. andmechanism of magma emplacement

The plutonic masses show sharp contactswith their host rocks crosscutting the mainHercynian structures occurring in them. Indetail. the contact is controlled bydiscontinuities in the wall-rock, such asfractures and stratigraphic surfaces. giving itan angular to polygonaJ morphology. Host-rock blocks engulfed by magmatic material

820 P.R. SERRA. P. ENRIQUE

occur in some localized contact areas.On a larger scale the plutons are seen to

be roofed by their wall-rock. Roof exposureis good along the SE and SW edges of theAlforja massif (Fig. 2). Here the w:l.imentaryhost lies above the piutonics over a gentlydipping planar surface oUlcropping for somekHometers (Fig. 3). The rapid change of thesesubhorizontal contacts into ste(:ply dippingones is needed to explain the observedrdarionships between lopognlphy and contactsurfaces in some areas (Fig. 4).

In the Montroig region (southernmOSl partof the complex), there is an arcuate structureof ahoul 2 Km diameter consisting of andexternal ring of granodiorire withinequigranular texture intruded into an olderlonalitic unit (Fig. 5). The interior of this ringcontains a smaller arc of the older [onalitethat, at the same time, enclo~s youngergranodiorite in its central part. Contacts dipoutwards about 60 to 70 degrees.

All the~ relationships, together with amore or less generalized lack of mineralorientation in the plutoni~, indicate that themagma was emplaced in a shallow brittleenvironment through the action of passivemechanisms such as stoping or cauldronsubsidence.

Taking into consideration that: (i) engulfedhost blocks are scarce, (ii) the pIu tons areeffectively roofed, and (Hi) subhorizontalcontacts rapidly turn into steeply dippingones, it is reasonable to infer thatemplacement was essentially controlled by thesinking, into underlying chambers, of largeroof·rock pieces unsupported by magma, insome cauldron subsidence-related process. Insuch a context, piecemeal stoping must haveplayed a subordinate role.

The arcuate structure which outcrops in theMontroig area is believed to represent a goodexample of block foundering. Here the innertonalitic arc represents the outcrop of thesubsided block.

Nature and tomposition of plutonit bodies

Lithologies forming the plutonic mas~svary from gabbrodiotitic to leucogranitic.Tonalitic ones are the most widespread,

granodiotites are also abundant, butleucogranites and diorites area much morerestricted.

a) Chronological re14lionships

Contacts between plutonic indicate that thetonalite of the Borges-Vilaplana type (definedin AHorja, Fig. 2), predates granodioritic andleucogranitic units throughout the complex.The AHorja·I'AJeixar tonalite, however, iscoeval to the CoU de la Batalla granodiorite(Fig. 2), as indicated by the decametric tohectometric zone of gradual transitionbetween them. Both masses are believed toderive from the same magmatic pulse and maybe related by a differentiation process.Although the gabbrOOiorites may be the basicprecursors of the association, theirchronological relationships with the remainingplutonics have not been deftnitely established,due to poor contact exposures.

b) Mineralogy

Primary moscovite or any otherperaluminous mineral is always I~cking inbiotitic granitoids, with the exception of thevery occasional appearance of almandine-richgarnet in restricted volumes in the Cara delMoro leucogranitic unit (Fig. 2). Themineralogy of the leucogranites is generallysimple; in some cases they have a remarkablylow content of mafic phases (1 % modal orless).

Hornblende commonly occurs in tonalitesand diorites but is scarce in granodiorites.However, well-developed biotitepseudomorphs after hornblende are a commonfeature of the Coil de la Batalla granodioritewhich, as mentioned above, may becomagmatic with the A1£orja-I' Aleixarhornblende-rich tonalite.

Small amounts of orthopyroxene, coexistingparagenetieally with other mafic phases suchas biotite and/or amphibole, occur in dioriticto granodioritic rock compositions. Twogroups of this mineral have beendistinguished, the first consisting of a verymagnesium-rich pyroxene, with large andautomorphous (sometimes corrocled) crystals,

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L.eoucogranilt'

Carbonift'rous hosl rock

Mostly porphyrific dykt's

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[ill][l]

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AUorja - l'Alt'iKar lonalite

Coil dt' la Batalla granodiorit~

El Moll6 granodior;te

Borges -Vilaplana. tonalite

Mas df' I'Aragonh granodioritt'

G]J

=~or:::J

l.'>, 'j,~'(:, ,~Wiiit'Y RiudfCOls quartzdiorite

FiB. 2. - Geologic.1 m.p of Alforj. massif.

822 P.R. SERRA, P. ENRIQUE

occasionally accompanied by other high-temperature phases such as diopside,phlogopite or allonhite accompanied :; othergrains, as microxenoliths (Fig. 6). The secondgroup consists of hyperstene showing texture

relationships which are bdieved 10 be formedby equilibrium crystallization from themagma.

Small amounts of cummingtonite alsooccur, represc=nting a hydrous alteration

Fig. j. _ Flat, nearly horizontal p1utonia (below) against their ~mentaryhost (above). SE edge of Alforia rnlUsif.

·.- A - A'-,r"'>-"·D,..::?"'''''--'--...,---:c."·~.~·:.~·,r;''''''''''''''''''''''1?'''''~~~'''''~_. . . . ..•

·- B - S'-, f5;;:"'c

LATE HERCYNIAN INTRUSIVES FROM THE SOUTHERN CATALONIAN COASTAL RANGES. ETC. 82}

product of the orthopyroxene. In some casescummingtonite form fibrous aggregates,regarded as subsolidus reaction products withwater. These fibrous aggregates may surroundpyroxene crystals.

Zircon, apatite, ilmenite and alIanite are themost abundant accessory phases. No primarymagnetite has been found and feldsparmegacrysts are lacking in the whole complex.

c) Textures

The main textures present in each plutonicunit are described in SERRA (1985) and SERRAand ENRIQUE (in press). Equigranular andinequigranular medium-grained granitoids are

the twO main textural groups distinguished inthe complex. The dioritic units and Borges-ViIaplana tonalites belong to the first groupand display normal equigranularsubidiomorphic textures.

All the granodioritic units. as well as theAIforja-I'AIeixar tonalite, belong to the secondgroup. These bodies tend to developunambiguous porphyritic chilled marginsagainst their host (either sedimentary orplutonic) (Fig. 7). Their inner parts are alsoinequigranular, but this feature may be muchless evident because of grain-size increases inthe groundmass. In these inner parts, quartzfrequently forms large crystals withidiomorphic bipyramidal habit and, locally,

o.............;'.oo.;............'.;;ooo.m.-' ••• ! • , •• !

Fig. 5. - Map of arcuate structure otcropping in Montroig area (southern border of compkx). Patterns: 1) Paleozoicsedimcntary host·rock; 2) Tonalitc; 3) Montroig granodiodite; 4) Porphyritic dykes; 5) Mesozoic sedimentary oover.

824 P.R. SERRA, P. ENRIQUE

sign of corrosion. Plagioclase, biotite andhornblende also form relatively large crystals.In the Alforja-I'Aleixar tona!ite hornblendepresents crystals from 10 to 20 mm indiameter in a groundmass of alx>ut 1 to 5 mm.

All these phases also occur as groundmassminerals, although felsic species such as alkali-feldspar, quartz and sodic plagiocla.se are mo~frequent. The inequigranularity in these rocksis sometimes not porphyritic but poikilitic; in

Fig. 6. - Microxenoli.th coniliting of anonhite III and Mg-rkh orthop)"rQx(ne (2), from a lonalilc of Boraes.Vilap.lana type.

Fig. 7. - M.iaoscopic detail of • chilkd margin devdopcd in contllCt of AHor;.-I'AJeinr lonalite with its sedimmtaryhost. Note openly porphyritic texture.

LATE HERCYN!AN INTRUSIVES FROM THE SOUTHERN CATALONIAN COASTAL RANGES, ETC, 825

this case, alkali-feldspar is the only oikocrystalphase.

Miarolitic cavilies are a textural featurecommon to almost all the igneous bodies ofthe complex, but they clearly predominate inthe most acidic ones. They are usually filledby pegmatitic material.

The textures of the first group indicate thatcrystallization developed in plutonicconditions, whereas those of the second groupreveal interruplions that quenched the

I

to a loss of volatiles, it is likely that theconfining pressure was low enough to permitvolatile expansion in fractures or escape to thesurface.

The dyke swarm

Porphyritic dykes compositionallyequivalent to the piu tonics form a well-developed swarm in' which the largestindividuals have extensions of several

o SOO IOOOrn, , , , , , ,

Fig. 8. - Map of dyke swarm in I'Argentera area. Porphytitic masses consist of multiple dykes of varied compositionintruded into onc: another and covering 60% of surface. Patterns: 1) Palcowic sedimentary host.rock; 2) Porphyriticdykes; J) Mesozoic sedimentary cover.

remaining liquid in the crystallizing magmachambers, especially in their marginal parts.This quenching may have been induced notonly by thermal contrasts between the magmaand its host, but also by the loss of volatilesvia fractures. Since chilled margins have notbeen found in the first group of granitoids,cooling of the environment is expected beforethe emplacement of the second group, ifquenching was thermal. If queching was due

kilometers and reach thicknesses of severalhundreds of meters.

NE-SW dyke trends predominate over allother orientations. They are subparellel to theCatalonian Coastal Range alignment and areemplaced in a penetralive joint family that,according to MALGAREjO (l987), results froma brittle event corresponding to the lastdeformational Hercynian pulse. NW-SE-trending dykes are also important and have

826 PR SERM. P. ENRIQUE

directions that, according to the same author,were imposed by the intra-Carboniferousfolding. Th~ dykes are usually concordantwith the wall-rock stratification.

Fine-grained chilled margins and coarserporphyritic interiors characterize almost everydyke. They may show rhyolitic banding in the

aphanitic margins of the acidic dykes, whichmay affect the thinnest ones completely.

Dike abundance in the AIforja massif (Fig.2) is repre~ntalive of the development of theswarm throughout the complex. The"Argentera area, however, (Fig. 8) isabnormally dense and represents the highest

Fig. 9. - Columnar ;ointing in a porphyrilic dyke (I'Argenttr1l ....u).

Fig. 10. - View of southern part of Alforja breeda body in which only largest leuo;ogranilic blocks are distinguishable.

LATE HERCYNIAN INTRUSIVES FROM THE SOlm-lERN CATALONIAN COASTAL RANGES, ETC. 827

dyke concentration of the ~gion. He~ dykesform thick NE·SW-trending compositeswarms, made up of many single dykes ofvariable composition (from dioritic togranitic), intruding into one another andgenerally confining their host to thin scrttns

betwttn dykes. In the I'Argemera area, dykescover 60% of the surface.

Columnar jointing of hexagonal symmetryis a very significant structure of some dykes(Fig. 9), Prisms are perpendicular to the dyke-walls and show especially good development

Fig. 11. - Detail of inte:rior of a pe:bbk-dyke 2 m thick in Escornalboo CI$t1e, «Insisting of clam of both igneousand sedimentary origin.

Fig. 12. - Detail of rounded clam forming Alfotfa breeda body.

828 P.R. SERRA. P. ENRlQUE

on the: chilled margins. Columnar jointingrequires such a shallow environment offormation that thermally induced stressesresponsible for tensile cracking of the coolingmagma are not significantly affected by theload pressure.

Breeda. and explosive phenomena

As indicated in SERRA (1987), the AIforjabreecia body (Fig. 10) is the best example ofthis kind of formation in the complex, andits origin is believed to be due to an explosiverelease of energy as a consequence of volatileexsolution in an epiplutonic magma chamberundergoing boiling. This is not, however. anisolated occurrence, and although breedabodies are sparse, they have bttn found inseveral places.

A poorly exposed breeda similar to theprevious one, is found along the Montroig-Vilanova d'Escornalbou road. There isanother interesting breecia outcropping in theVilanova d'Escomalbou area. It is an ellipticalmass of about two hundred meters in itswidest point, located at the intersection of twoporphyritic dykes with another irregularlyshaped porphyritic body which intrudesPaleozoic sediments. Lithologically it isformed by angular-to-rounded fragments witha matrix consisting of either igneous materialor ground rock in a patchy arrangement Thereis a small pebble-dyke about two meters thickin Escornalbou Castle. It is also hosted byPaleozoic sediments against which it showsa sharp cross-cuning contact. The level of theoutcrop is about one or two hundred metersabove the inferred position of the plutonicroof. It is formed by some centimeter-sizedrounded fragments of sediments, as well asby tonalite fragments belonging to the Barges-Vilaplana type, embedded in ground rock (Fig.11).

All these br«"das can also be attributed toexplosive degasification of magmas in veryshallow environments. A fluidized gas-solidsystem is invoked to explain the roundedshapes of the dasts (Fig. 12).

Summary and c:.onc.!usions

High crustallevels reached by magmas may

be inferred from these exposed data. Someobservations indicate that this level is asubvokanic one: (i) the sparse but regularoccurrence of explosive brecdas, and (ii) thedevelopment of columnar jointing in somedykes. The important energy disharmon.yexisting between the magmas and the.lrenvironment of final emplacement resulted 10the development of contact metamorphicaureoles that, at least in some places, reachedhigh grade. The chilled margins of someplutonic masses may have been by the samephenomenon if they were thermally induced.

The brittle behaviour of the host isindicated by the contact relationships. Magmaemplacement may be accounted for by largeblock-sinking mechanisms like cauldronsubsidence, whereas piecemeal stoping isconsidered of secondary importance.

The presence of miarolitic cavities alsodenotes low pressure, when gas exsolutionfrom liquids forces the formation of bubbles.

Magma emplacement at such a high crustallevel can only be explained if the magmasessentially behaved as mobile liquids withminor amounts of suspended solids. Since thepresence of ortophyroxene characterizes thegranitoids of the complex, it is inferred thatthe magmas were water-deficient, to the pointthat not enough water was available to hydrateall the femic components of the magma, andthat their water fugacity was buffered by theassemblage of this anhydrous mineral withother hydrous ones, such as biotite and/oramphibole. To forfT'! water-de:ficient granitoidmagmas relatively high temperatures, usuallyoccurring at the base of the crust or in theupper mantle, are required. It is believed,therefore, that these magmas formed at sucha depht and that they were hot and dryenough to ascend dose to the surface.

U the magmas ever reached~ surface, thedyke swarm may have provided very goodmagmatic vents, especially in the l'Argemeraarea where is is so dense.

Acknowldg~enfJ. - We are indebted to Dr. Aldo De!Moro and Pro£. Giorgio Ferrara of the lstituto dlGeocronoIosia e Gcochimka Isotopica dd CNR di Pisa,for their helpful collabontion and sciemific support inthe Rb-Sr isotopic analyses.

LATE HERCYNIAN lNTRUSIVES FROM THE SOUTHERN CATALON1AN COASTAL RANGES. ETe. 829

P.rt of Ihis work WllS SUpporled by • CIRIT gram(Semr principii investigalorl, and by lhe Savei~icde C.t-.Juny•.

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FONTllOTEj.M., JUUVERT M. (1952) - Algu1llls prtcisionC's

sobre la cro1lo/otUJ tk /os p/q,llmimtos hcd1fu1IOf mCIltllbtflll.XV Congr. GC'OI. Intern. Alger. I. XIV·XV:H5.

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