The Ba~honjan and Callovianof the Northwest-IberianRange:

Stagesoffacial andpaleogeographlealdfferentiation on an epicontinentalpla<form

5. WILDE

Institutfúr Geologie, Ruhr-Universitdt, D-4630BOCHUM, W-Gern’zanyKornweg3, D-4630BOCHUM

ABSTRACT

The Bathonian and Callovian stages of the NW-Iberian Range. whichformations are newly defined, correspond approximately to two «macro-sequences» limited by wide-spread uncorformity horizons. During thistime the facial environmental conditions of this epicontinental shallow-marine depositional realm led into an obviously intensified regional diffe-rentiation. This is resulted by increasing tectonic activities causing a struc-tural paleogeographical framework with very variable subsidences, suppo-singly in connection with the initial Biscay spreading phase.

Key words: Jurassic, Bathonian, Callovian, Iberian Range, Stratigraphy,Paleogeography, Formation definitions, Facies differentiation, Epiconti-nental Platform. Spain, Soria, Logroño, Burgos, Zaragoza Provinces.

RESUMEN

El Bathonicnse y Calloviense de la parte NW de la Cordillera Ibérica,cuyas f¡ rmaciones son nuevamente definidas, corresponde aproximada-mente a dos «macro-secuencias» limitadas por discontinuidades muy ex-tensas. Durante estos pisos las condiciones faciales-ambientales de la pla-taforma marina epicontinental y poco profunda cambiaron, indicandouna diferenciación regional intensa. Una activación tectónica tuvo comoconsecuencia una articulación estructural paleogeográfica con subsiden-cias locales muy variables, posiblemente conectadas con la fase inicial dela apertura del Golfo de Vizcaya.

(‘,,adún¡o.~ cié Geología ¡hética Ni’ 14. II 3—142. M adri cl. 1990.Ld it. Universidad Co ¡np1 t¡tense.

114 5. Wilde

Palabras clave: Jurásico, Bathoniense. Calloviense, Cordillera Ibérica,Estratigrafía, Paleogeografía, Formaciones definidas. Diferenciación fa-cíal, Plataforma epicontinental, España, Prov. de Soria. Logroño, Burgos,Zaragoza.

ZUSAMMENFASSUNG

Das Bathonium und Callovium der NW-Iberischen Ketten, dessen For-mationen neu definiert wurden. bilden in etwa zwei «Makrosequenzen».dic durch weit verbreitete Diskontinuitáten begrcnzt sind. Wáhrend dieserStufen gelangten dic Faziesverháltnisse dieses epikontinentalen flach-mari-nen Ablagerungsraumes zu ciner starken regionalen Differenzierung. Emeverstiirkte tektonischc Aktiviemng verursachte cine interne paláogeographis-che Strukturierung mit unterschiedlichsten Subsidenzen. Em Zusammenhangmit der Initialphase des Biskaya-Spreading wird angenommen.

Sehliisselwúrter: Aíra, Bathonium, Callovium. Iberische Ketten, Stratigra-phie, Paldogeographic, Formations-Definitionen, Fazies-Oiffercnzierung.Epikontinental-Platform. Spanien. Provinz Soria, Logroño. Burgos. Zara-goza.

INTRODUCTION

During mostly of the Jurassic period in the territories of the NorthwestIberian Range an epicontinental shallow marine realm existed, situatedbetween thc deepcr open seas of the Proto-Biscay (Atlantic) and 4w BetieGcosynclinal (Tethys). The marine Jurassic mega-sequence can be dcvi-ded into six macro-sequences. beginning with the partially evaporitic Car-niolas of the late Triasic/early Lias and cnding with the start of tbe limnic-terrestrial Wealden in Upper Kimmeridgian age (Fig. 1).

The fourth and fifth of these macro-sequences, approximately corres-ponding to the Bathonian aud Callovian stages, play a special and impor-tant role in thc Jurassic depositional evolution. At these times obviouschanges of the sedimentary environment took place with destinct regionaldifferentiation of facies and paleogeography, after a longer period of anessentially uniform development.

The studied area consists of two main territories. the Sierra de la De-manda! de los Cameros and the Sierra del Madero! del Moncayo. Thethird, the Zaragoza region (Ricla to Belchite) is included as transitionalregion between the NW and SE Iberian Range (Aragonese-Levantinebranch).

The basal works on marine Jurassíc biostratigraphy and paleogeogra-phy of the NW-Iberian Range are done mainly by Mensink (1966) and

Th e Bathonian and Callovian ofthe Northwest-Iberian... 115

UNCONFOPMITIES PROFILE t-WIN LZTHOLOGY AGE

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116 S. Wilde

Bulard (1972). Since then several special and local studics about this sub-jecí are published. Particularly the Paleontology & Facies Working Groupof the Bochum University Institute of Geology, directed hy Prof Dr H.Mensink. are engaged in the NW-lberian Jurassic since more than a deca-de. Lower Dogger (Aalenian-Bajocian) sequences are studied by Mert-mann (1984/1986), Scheer (in prep.) and Gervais (in prep.). the LowerCallovian Unconformity by Mcnsink and Mertmann (1984). and the over-lying Oxfordian-Kimmeridgian by Benke (1981). Bcnke et al?, (1981). Con-ze eta!. (1984), Dragastan eraL, (1987), Errenst (¡984, 1987). Wnendt-Juber(1985) and Schudack (1984, 1985/1987). without mcntioning ihe maty Di-ploma works done in this regions. This contribution is based on the firstdetailled study of Bathonian-Callovian of this regions done in my thesis(Wilde 1987/1988).

1H11 LIMITING UNCONFORMITY HORIZONS

The two studied macro-sequences are limited hy ihe following maindepositional unconformities representing omission or lowest-rate sedimen-tation phases (Fig. 2).

Ihe Upper Bajocian «Unconformity» is a sequence of low thicknesscmbracing two or three ammonite zones (niortense, garantiana. parkinsonipp.) and is characterized by faunal condensation, hardgrounds, reworkedlayers. and ammonite enrichment horizons. It is defined as the basal guidelayer of the Bathonian macro-sequence.

At íhe boundary Lower/Middle Baihonian an unconformity of localsígnificance separates discontinuotísly the Neila from the Montenegro For-mation in the Demanda Basin regions.

[he Lower Callovian Unconíormity appears in thc greatest part of iheNW-Iberian as hardground or erosional horizon and divides the Batho-nian frorn the Callovian macro-sequence. Usually it is combined with aniron-oxide covering (ferricrust). The horizon is dated with niacrocephaluszone arnmonites (Bulard. 1972, Benkc ca a!, 1981. Mensink & Mertmann¡984).

The Dogger/Malm Boundary Ilinconformity as the most wide spread ofthe Jurassic guide horizons terminates thc Callovian,macro-sequence. It ischaracterized by a typically iron-oolitic, often sandy and bioclastic layer,with one or more generations of hardgrounds and/or erosive surfaces.Ammonite faunas verify tbe stratigraphical reach in the NW-Iberian rcalmfrom lambeni (late Upper Callovian) up to plicasilis zone (early MiddleOxfordian) (Benke, 1981; Bulard, 1972. and others). In the Aragonese andsorne othcr SE-Iberian regions the Fe-oolitic omission phase sets in oftencarlier in Lower or Middle Caíiovian (Geyer et al., 1974: «Upper Houndary

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(Fe-) Oolite»; Gomez. 1979: “Capas de Oolitos ferruginosos de Arroyo-frio»).

TELE FORMATIONS

In íhe Levantine part of the SE-Iberian Range the Chelva Formation(«Formación Carbonatada de Chelva») has been nominated by Gomez(1978, 1979) comprising the Toarcian to Oxfordian. His proposal to apply itto the whole Iberian is nol to follow. His definition ranges stratigrapbicallytoo wide: the major unconformities of the Lias/Dogger as of the Doggcr/Malm boundary exists well recognizably also in the Levantine. but unfor-tunately are not regarded as formation limits. On the other hand in theNW-Iberian the Jurassic is facially more differentiated and thicker. So tomy opinion it is useful to establish new formations for the NW-IberianBathonian-Callovian (Wilde 1987/1988). They are deñned by its strati-graphy, local distribution, lithology and facies types (Fig. 3).

Demanda - Cameros Territory (Fig. 3a, b)

Neila SpongeTuberoliteLiniestone Formation

Formación Calizas Espongio-tuberolíticas de Neila

Typeloca/Uy—Sierrade Neila (S-Demanda).Limiration.—BetweenUpper Bajocian Arntnonite Horizons and beginning

of sandy-marly Montenegro Fm.Stratigraphy.—LatestUpper Bajocian (upper parkinsoni zone) and early

Lower Bathonian (zigzag zone. convergens subzone).Lithologv.—Mainly tuberoid-rich calcarenites with siliceous spongcs («spon-

giotuberolites»); sorne silex nodtíLe horizons; thicknesses mostly 15-30 rn.Dktribution.—Whole Demanda-Cameros except marginal NE and SW parts.Facies types:N-1 Sponge TnberoidLimestone.—(Bio)tuheromicr(ud)ite with sponges and

its fragments, echinoderms, bryozoans, foraminifers. fllaments. Mainfacies.

N-2 Fe/oid Lnís¡.—Biopelmicr(ospar)ite. Locally in E-.NE-Demanda, 5W-Cameros.

N-3 Tuberoidic Calcilutitic Limestone. — Biomicrite with some tuberoids. Up-per part in the SW-Cameros.

N-4 Pc/oid TuheroidLmst.—Biopeltuberomicrite. Top layers in S-Dcmanda.N-5 Coated-grain Tuberoid Lms¡. —(Tubero)(micro)sparite (coated-grains =

micritie-enveloped hioclasts). Top layers in 5-. 5W-Demanda.N-6 Jhberoidic Bioc/ast Peloid Limevtone («Va/gaño Mernherx¡).—(tuhe-

ro)biopelmicr (ospar)ite. Transitional beds to following Montenegro Fm.in N-Dcmanda.

The Baihonian and Callovian of theNorthwest-lberian...

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The Bathonian and Callovian ofthe Northwest-Iberian... 121

Torreci//a (JoIUic LiniestoneFormation.Formación Calizas Oolíticas de Torrecilla

litre loca/iw—Areaaround Torrecilla en Cameros (E-Demanda).Limitation.—BetweenUpper Bajocian Ammonite Horizons and the Lower

Callovian Unconformity (ferricmst).Stratigraphy—WholeBathonian, including Latest Upper Bajocian (upper

parkinsonizone) and early Lower Callovian (macrocephalus zone).Litho/ogy.—Mainly oolitic calcarenites; about 50-150 m.Distribution.—SE-. E-Demanda, N-. NE-Cameros regions.lñizc¡es types:TI Pe//etoid/Ooid Limestone.—Oo(bio)sparite. with echinodermal clasts

(pelletoids = fully micritized ooids aud echinoderms). Ihe main facies.T-2 Echinoderni Bioclast Fe/oid Limestone.—Biopcl(micro)sparite.T-3 S/ightlv Sandy Bioclast Fe/oid Liniestone.—Biopelmicr(ospar)ite.T4 Slightly Sandy Qoid Bioclast Fe/oid Limestone.—(Oo)biopel(micro)spari-

te.rs 8kg/it/y SandyCoated-grainQoid Limestone.—Oobiosparite.T-2 to rs («Santa Inés Membera>) are transitional heds to the following

Montenegro Fm. in N- and SE-Demanda.

Doña SantosLimestoneForniation.Formación Calizas de Doña Santos

Type /oca/i~.—Doña Santos area (Duero Basin border)Limitation.—Substitute partially the upper Neila Fm.Stratigraphy— Lower Bathonian?Litho/o~y.—Sponge-free,quartzless limestones; up to 60 m.Distribution.—Only in parts of SW-Cameros.Facies ~p¿s:D-I Jiioc/asticí Calcilutitic Limestone.—(Bio)micritewith some fine bioclasts.D-2 Coated-grain Ca/carenitic Limestona—Bio(intra)pelmicrite/sparite, with

sorne peloids, bioclasts and lumps.

Fig. 3.—Synoptic seheme of thc stratigraphical and regional distribution of thc Bathonianand Callovian formations of the NW Iberian realm (region numbers sea [ig. 2). its mainli¡l¡Ology and ¡hicknesscs (little nunabers>. inck¡di¡ig thc aol jacení stages. ½. Den¡=¡n¡.la—(a¡neros territoro (regions l—4y31~, liernanúla—Canteros tcrritorv continued ( rcgions 5—91.3c,Madero-Moncayo territory (regions 10-12). 3d. Madero-Moncayo continuad (13-14) and Za-ragoza territory (15-16).[ig. 3.—Esquama sinóptico estratigráfico-regional de las formaciones del Bathoniensa y Ca-lloviense del NW de la Cordillera Ibérica (números da las regiones, véase [ig. 2). con las lito-logias principales y los espesores (números pequeños), incluyendo los pisos adyacentes. 3a.Territorio da Demanda-Carneros (regiones ¡-4). 3b. Territorio de Demanda-Camems. cont.(regiones 5-9). 3c. Territorio de Ma-daro-Moncayo (regiones 10-li). 3d. Territorio de Ma-dero-Moncayo, cont. (13-14) y de Zaragoza (15-16).

122 £ Wilde

Espejón Sant/yOo/itic LimestoneFormation.Formación Calizas Arenosas Oolíticas de Espejón

Type /oca/i¡y.—Espejón area (Duero Basin border).Limitation.—Followsthe Doña Santos Fm. (or Neila Fm. resp.). substitu-

ting Ihe MontenegroFm., Iocally only Ihe Iowest part of it.

Stratigraphy—Middleto UpperBathonian.Litho/o~.—Ooid/eoated-graincalcarenites witb quartz; up lo 45 m.Distribution.—Aboutthe sameas the Doña Santos Fm.Facies types:E-] 5/iglú/y Sant/y Ocid Limestone.—Oo(hio)sparite/micrite with coated-

grains, bioclasts and some quartz (f¡ne-sand).E-2 Sant/y Coated-grain Limestone.— fine/medium-sandy biosparite.E-3 Sandstone ~fine/medium,).—With quarzitic lithoclasts. Local intercala-

tions.

MontenegroSant/y Mar/y LimestoneFormation.Formación Calizas Margosas Arenosas de Montenegro

Type /oca/@.—Around Montenegrode Cameros (SE-Demanda).Limitation.—Representing the whole quartz-hearing Dogger, except the Es-

pejon and San Leonardo Formations.Ssratigraphy—Loweror Middle Bathonian (zigzag orsubcontractus zone) to

Lower or Middle Callovian (graci/is orjason/? coronatum zone) in Wes-tern part. Lower lo Upper Callovian (rnacrocephalus to athlera/lambenizone) in the East of the Demanda-Cameros territory.

Litho/ogy.—Rhythmicallyalternating. sandy marís and limestones with peloidsand bioclasts; partially fossil-rich; thickness 5-250 m, very variable.

Distribution.—Thcwhole Demanda-Cameros, except the extreme SW.FaciesIypes:M-I 5/iglú/y Filament Pc/oidLimestone//vfar/.—Biopelmicritewith somequariz

(silt to ftne-sand). Mainly lower part in 5- and SW-Demanda.M-2 5/iglú/y Si/ty Ca/ci/utitic Li,nestone/MarL—(Bio)micrite/microsparite with

some fine bioclasts and quartz (silt). Lowest part in SE-Demanda.M-3 Sant/y Fe/oid Limestone/Mar!—Biopelmicr(ospaflhtewith peloids, No-

clasts and quartz (well-sorted coarse-silt to fine-saand). Main facies inalí regions.

M-4 Sant/y Bioclast L/mestone/Mar!—Biopelmicrite/micrudite with luma-chelle layers, peloids, quartz. lntercalations in SW-Demanda and SW-Cameros.

M-S Bioc/ast Ve/oid Ca/careousSandstone:Biopelmicrit5c (fine-)sandstone.SW-Cameros. within the upper formation part.

M-6 Sandy Aggregate-/Coated-grainLiniestone («Morca/vi//o Mcmber»).—Bio(pel)-intramicritc/microsparitc (aggregate-grains = micritic lumps and

The Bathonion and Callovian ofthe Northwest-Iberian... 123

clasts), with peloids, quartz (siít Lo coarse-sand). Upper part in 5W-Cameros and 5W-Demanda.

M-7 Sandstor¡e.—Of mostly medium-sized quartz and quartzitic lithoclasts.Locally in SW-Cameros.

San LeonardoSand Formation.Formación Arenas de San Leonardo

ljipe localitv.—Aiong railway-line near San Leonardo (SW-Cameros).Li,nitation.—Between Montenegro resp. Espejón and an uncornformity sur-

face upon which the Talveila Fm. (marine Kimmeridgian) follows.Stratigraphy.—Ahottt Lower Callovian?Lithology—Sands and sandstones; up to 20 m or more.Distribution.—Only in parts of the 5W-Cameros.Facies ~pe.—SL Sand/Sandstone.—Mostlycarbonate-free or decalcified, of-

ten graded and cross-stratified, fine- to coarse-sand, locally gravel.

Madero-Moncayo Territory (Sg. 3c, d).

Soria SpongeTubero/iteLimestoneFormationFormación Calizas Espongio-tuberoliticas de Soria

Type /oca/ity.—Proftle near province capital Soria.Limitation. —Between Upper Bajocían Ammonite Horizons or equivalent

layers and the Pozalmuro or Olvega Fm. resp.Stratigraphy—LatestUpper Bajocian (,parkinsoni zone) and ]3athonian in

locally different ranges.Litho/ogp.—«Spongiotuberolites»similar Lo Neila Fm.; up Lo 65 m.Disstrihution.—Westand central Madero (Soria-Olvega area).FaciesIypes:S-J SpongeTuberoid Limestone.—(Bio)tuberomicrite with sponges. Main

facies.S-2 Tuberoidic Ca/cilutitie Li>nestone.—Bio(tubero)micritewith some tube-

roids, filaments and other bioclasis. Upper formation pan in the Ma-dero.

O/vegaCa/cilutitic LimestoneFormnationFormación Calizas Lutiticas de Olvega

Type/oca/Uy—Madero west of Olvega.Limitation. —To the top is Pozalmuro Fm.; limit to subjacent is indistinct

(proposal for extension down to Lias/Dogger Boundary Unconformity).

124 S. Wilde

Stratigrap/zy.—Locally diffcrent, about Bajocian-Bathonían.Litho/og—Calcilutites. partially limestone-marí alternations.Distribution.—Madero.NW- and E-Moncayo regions.FaciesIypes:0-] Pe/oidic Fi/ament Calcilutite.—(Hiopel)rnicrite. Madero, NW-Moncayo.0-2 511ghz/y Biogenic Ca/cilutite — Micrite. partially sorne biogenes. Pégado.0-3 5kg/it/ySilíy Filament Limestone/Marí. — Biomicr(ospar)itc. E-Moncayo.0-4 5kg/it/y Silty Ca/ci/utite/Mar!—Micr(ospar)ite. Upper part in E-. NW-

Moncayo.

Manub/esOolitic LimestonefórmationFormación Calizas Oolíticas de Manubles

Jipe /oca/i&’.—Ciria area. at Manubles creek.Limitation.—BetweenUppcr Bajocian and Lowcr Callovian Unconformí-

tíes.Sítratigrap/iy—Whole Bathonian, minor paris of adjacent sub-stagcs.Lit/io/ogy.—Massive calcarenitie oolitesz thickness up to 200 m.Distribufion.—Only in SW-Moncayo.Facies 4vpe:C-I Qoid Limestone—Qosparite, well-sortcd. partiaily with pci letoids, coated-

grains, echinodermal lumacheile.

Poza/muroCalcareousSands’toneFormation.Formación Areniscas Calizas de Pozaimuro

Type/oca/iq.—Madero area east of Pozalmuro.Limitation.—Between LowerCallovian Unconformity and Aldealpozo Fm.

(cyclic lagoonal Oxfordian-Kimmeridgian) or coral-bearing calcareousoolitic sandstonc (underlying the Kimíneridgian Coral Limestone).

Stratigraphy—Callovian;limit to Oxfordian not exactly known.Lithology—Mostlyarenites as sandstones. oolitic and peloidic calcareous

sandstones. sandy-oolitic limestones; Cina area: fosiliferous peloidiesandy limestone-marí alternations; thicknesses 35-185 m.

Distribution.—Centraland W-Madero. 5W-Moncayo.facies types:P-] Sant/y Ooid Limestone.—Sandy oo(biopel)sparite, ooids partially quartz-

cored. with sorne pelletoids, peloids, biogenes. Main facies in W- andcentral Madero.

9-2 Sant/y Filament Pc/oid Limestone/MarL—Coarse-silty/ ftne-sandy No-pelmicrite. Lowcr part in Cina and Noviercas area (Madero! 5W-Mon-cayo).

9-1/2 Alternationsof Sant/y Oo/itic and Sant/y Filament Pc/oid Limestone—

Th e Bathonian aná Cal/ovian of theNorthwest-Iberian... 125

Sandy oo(bio)- to biopelmicrite. Lower part in Pozalmuro area (Ma-dero).

P-3 Sant/yBiogenePc/oidLimestone/Mar/.—Fine-sandy/marly biopelmicri-te. fossiliferous (ammonites, pelecypods, brachiopods). Upper part inCina area.

P-4 Qoid Pe//etoid Ca/careous Sandstone.—Oosparitic f¡ne/medium-sandsto-ne. Upper pafl in Tajahuerce-Pozalmuro area (W-/ Central Madero).

P-SPeloidCa/careous Sandstone.—Pelsparitic Sdst. Main facies in W-Madero.P-6 Qoid Coated-GrainCa/careousSandstone.—Oo(biopel)sparitic sandsto-

ne. Main facies in Bijuesca area (SW-Moncayo).9-7 Sandswne/QuartzC’ong/omerate.—Inlercalations in W-Madero.AgredaSandv Mar/y LimestoneFormaban

Formación Calizas Margosas Arenosas de Agreda

Type /oca/i/y.—Around Agreda. NW-MoncayoLimitation.—Between Lower Callovian and Dogger/Malm Unconformi-

ties. This replace per deL the Pozalmuro Fm. east of the Olvega-To-zanzo Swcll line.

Strau~rap/ry.—Neany the whole Callovian.Litho/ogy.—Mostlysilty/ fine-sandy limestone-marí alternations and finely

clastie calcareous sandstones; oolitic and coarsly clastie arenaceouslimestones are less frequent; thicknesses about 150-300 m.

Distribution.—NW-and E-Moncayo.Faciestypes:A-] Quartz-freeLchinot/ermLumac/ielle Limestone(<cAñavieja Member»).—

Echinoderm bío(pel)microsparite, with peloids/pelletoids. Lower partin Pégado area.

4-2 Slig/it/y Sant/y Ec/iinoderm Limestone.—Fine-sandy/coarse-silty bio-miente! sparite with fine echinoderm clasts. Basally in Agreda area(NW-Moncayo).

4-3 Sant/yPc/oid Fi/amentLimestone.—Fine-sandybiopelmicr(ospar)ite. Lo-wer formation part in soutbern NW-Moncayo (Cueva/Olvega anca).

4-4 4/ternationsof Biogene-bearingSi//y! Fine-sandyMar// Limestone¡o Ca/-careous Silt-/Finesands¡one. —Bio(pel)micrite. Typically in NW-Moncayo.

4-5 Aiternations as A-4 but mostly biogene-free. typically in E-Moncayo.4-6 Sihy Fi/amentLimestone/Mar/.—Biomicrosparite. Locally upper part.4-7 Sant/y Ve/oid Limestone!Mar/.—Fine-sandy/ coarse-silty bio(pel)-

micr(ospar)ite. Upper part in southern NW-Moncayo.4-8 Pelletoid (ioa¡ed-grain Ca/careous Sandstone.—Biopelsparitic sandstone.

Local intercalations in NW-Moncayo.4-9 Bimodal Ca/careous Sandstone.—With sorne peloids and biogenes. NW-

Mo ncayoA-JO SandstonefrAñan Member»).—Middlepanonly in Añon (E-Monca-

yo).

126 5. Wilde

Zaragoza Territory (transitional region to SE-Iberian Range) (Fig. 3d).

Ric/a Mar/y LimestoneFormadonFormación Calizas margosas de Ricla

Typelocakty.—Riclaprofile.Limitation.— Between Upper Bajocian Amrnonite Horizons and Dogger/

Malm Boundary Unconformity. The Lower Callovian Unconforrnitynot occurred in this region, therefore no formational differentiationbetween Bathonian and Callovian macro-sequences is possible here.

Stratigraphy—Whole Bathonian and Callovian; in southern pafl gaps inMiddle to Upper Callovian.

Litho/ogv.—Fossiliferous limestone! mari alternations with filaments andpeloids. partially sandy; thicknesses 35-140 m, increasing from SE toNW

Distribution —Regions W and 5 of Zaragoza (proposal to define the forma-tion fon the adjacent SE-Iberian because of facies similarities).

I4icies types:R-1 TuberoidicFi/amentFe/oid Limestone.— Biopel(tubero)micnites, quartz-

free.R-2 Fi/amentPc/oid Limestone.—Biopelmicrites, quartz-free.R-3Fi/amcnt Ve/oid Limestone/Mar!—Same. but moreargillaceous.R-4 Sant/y Fi/arnent Ve/oid Limestone/Mar!—Sa me. but with quartz.

ENVIRONMENTAL AND PALEOGEOGRAPHICALDEVELOPMENT

The petrographical and stratigraphical facts of the studied Formationslead to the following outline of the changing facies and paleogeographyduring Bathonian and Callovian time in the NW-Iberian epicontinentalnealm (Eigs. 4a-d).

During nearly the whole Uppen Bajocian in great parts of the con-cerning territories low sedimentation rates and omission phascs with hard-ground formation and faunal enrichments prevailed (the Upper Bajocian«Llnconformity» with «Ammonite Enrichtnent Horizons». (Fig. 4a. c[1]).

Hajocianfliathonian Houndary (after Upper Bajocian “Unconformityss).(Hg. 4a, e[2j).

Ar the end of the Bajocian stage ihe environmental conditions changeddisíinctively. The sedimentation rates inereased or set it again. Iliree diffe-rent shallow marine domains are formed in the NW-Iberian:

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The Bathonian and Callovian of the Northwest-Iberian... 129

MADERO MONCAYO

~g Soria AIO•aIpozo Olv.ga Agr.da TaISff,flt•S

O~v.ga-7 or.nz o

Spong,otub.rolitic Plaíform flntr¡ct.d Marglna¡ Basin

BOOÑOAPV

BATH

MaderoS•n~i-1agoon

______________ L O

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BATH. _____ 1 ____

4 7 $wll Exri.flB’On 7

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UnwlofCfffi¡ty surfc.S.¡ ‘y//A, 5.2 — 0 1 - ~ 1 tI’> o—¡—¡on (0robsbf.)

Fig. 4c.

Fig. 4.—Schematic and interpretativa facial-paleogeographical cross-sections through theNW Iberian epicontinental platform during Eathonian and Callovian. For facies types seetext. for he 1 ocations see Lic. 2. Subside nce di fkre nces betwee n bloc ks are marked witha rrows s howí ng rclat ve movemen t di reclions. 4a. Dem a n cía—Cameros tcrrito ¡~y d~~¡ ring Ha—thonian. 4b. Demanda-Cameros territory during Callovian. 4c. Madero-Moncayo territoryduring Bathonian. 4d. Madero-Moncayo territo¡y during Callovian.Fig. 4.—Cortes transversales esquemáticos a través de la plataforma epicontinenral del NWde la Ibérica, con la interpretación facial-paleogeográfica del Bathoniense y Calloviense.Para los tipos de facies, véase al texto; para la localización dc los cortes, véase Fig. 2. Lasdiferencias de subsidencia entre bloques se han marcado con flechas, indicando las direc-clones de los movimientos relativos. 4a. Territorio de Demanda-Cameros durante el Batho-niense. 4b. Territorio de Demanda-Cameros durante el Calloviense. 4e. Territorio cíe Ma-dero-Moncayodurante el Baihonianse.4d. Territorio cíe Madero-Moncayo durante cl Callo-víause.

130 Si Wilde

MADERO MONCAYO

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Fig. 4d.

A low-energetic «spongiotuberolitic» platform. extended between Bur-gos and Olvega, covering the greatest part of Demanda-Cameros and Made-no ‘egiutis wtt¡t dli tsuutiiuituusty uegiittiutg u’ utusttuiiiai sjui¡gc giuwtii

connected with an intense tuberoid formation (facies N-1, 5-1).High-energetic oolite platforms or bars started to form in edge posi-

tions of thc NW-lberian. both in the N-/NE-Cameros (T-l) and in thc SW-Moncayo region (C-1) with great sedimentation rates.

Sarta A idas ¡pozo

1zz

L.CALL.

Qú¿srtz—ooiitlcPistfors

<II.

Fue Bathonian and Cal/ovian of Ihe No>-thwest-Jherian.., 131

A somcwhat restricted, semi-lagoonal and mostly biogene-poor margi-nal basin lay in NW- to E-Moncayo, limited to thc east from (he platformsby the Olvega-Toranzo Swell, continuing similarly the previous facialconditions of the UpperBajocian times (0-1. 0-4). Ihe least faunal influen-ces existed in the northern basin part, the Pegado area (0-2). Some terrige-nous silt supplies are made conspicuous only in the more marginal partsin the E-Moncayo and Agreda areas (0-3/4). The sponge growth in the cen-tral Madero probably ended before the begin of Bathonian and the envi-ronment then changed also into a more abiogenie micritic one (0-1).

An open-marine aud faunally rich, nearly pelagie basin were situatedtransitionally to the SE-Iberian realm (Zaragoza Basin) without quartz-detritic influx. In the Ricla and Aguilon areas some sponge growth tookplace (14-1), but without contact to the Demanda-Madero spongiotuberoli-tic platform. The Belchite-Jaulin anca remained sponge-free (R-2).

Lower Bathonian (Fig. 4a, cL3l).

During its final development the spongiotuberolitic platform partially(S-SW-Demanda) gct into higher-energetic and possibly shallowen influ-ences (N-4/5) rendering its hiostromal gmwtb more difftcult or impossible.The sponge environment in most of the regions (5-, SW-Demanda, 5W-Cameros) ended isochronously. possibly following by a short omxssionphase with local erosíons.

Añer it die sedimentation set in again with an entire different facies of adeeper subtidal qtiartz-detritic and peloidic basin environment (M-1). Oniyin Ihe N-Demanda dic sponge tuberoid sedimentation remained longen(N-1).

This facial unconformity is restnicted on thc Demanda regions. TheDemanda basin subsidence is connected with an uplift phase of the adja-cenÉ Meseta forclands with dic consequence of beginning quartz supphes.First the marginal, but fully marine 5W-Demanda regions are detriticallyinfluenced. Parts of Ihe S-Dcmanda, the present-day Canales Graben,retnained initially as a local «Canales Swell» with possibly omitted sedi-mentation.

In the 5W-Cameros. from Espejón! Hortezuclos to Las Fraguas. a na-rrow coasí-parallel zone with scmi-lagoonal micritie sediments withoutsponge growth. alternating with reworked biogene influx wcre formed (D-1/2). Near Doña Santos solitary and stock corals growed. Similar abiogenieconditions encroached locally on thc adjacent San Leonardo Strip duringits final sponge platform development.

Thc ooliíe regions of the Cameros spread until the Montenegro! SantaInés anca (o its maximal expansion displacing the marginal sponge tube-roid sedimentation (N-l > T-l).

132 S. Wilde

Middie Bathonian (Hg. 4 a, c [4]).

Thc 5W- and S-Dcmanda were now fully included into the quartz-detnitie basin sedimentation. During its initial phase it is characterizedmainly by less quartz and greater fdament influxes (M-l), but ten conti-nuously leading to more sand percentages (M-3). In the Canales Grabenanca dic sedimentañon rates dilfered locally very much, the «Canales Swell» inte west and the «Mansilla Trough» in its eastern part can be separated. Inthe 5-Demanda locally iron-oolites were formed.

In thc San Leonardo Srip anca the sedimentation started at once withthe «normal» sandy basin facies (M-3). but soon leading to increasingquartz and lumachelle contents as sign of a more shallow position (M-4/5).In (he more marginal areas of the Demanda basin, the present DueroBasin borden, highcr agitated near-shore bioclastic (coated-grain) and ooli-tic bars developped (E-l/2). In the N-Demanda the spongiotuberojitic pha-se continued, but with lower sedimentation rates and incneasing open-marine influences (N-6).

Thc facial and palcogeographical conditions of 4w Madero-Moncayoterrhory is not too well to define because of (he extended stratigraphic gapor (he lack of guiding fauna. Middle Bathonian is biostratigraphicallyproved only near Noviercas with a micnitie restnicted environment (0-1).which total extension is unknown.

Seetningly in the arcas around Olvega/Agreda/Cueva de Agreda thesedimentation came to a standstiil, interpretable as an extension of theOlvega-Toranzo Swell. But a laten erosion, during dic Lower CallovianUnconformity phase, of primarily deposited Iayers can noÉ be excludedhere. In te E- Moncayo the facies likely continued unchanged (0-4).

In te W-Madero the sponge platform get negionally deminished. pro-bably remaining with greated sedimentation rates only around Soria (5-1);near Aldealpozo sponge deposits are minitnal (S-2) possibly in a swellposition. On te contrary in (he oolite bar anca around Cina (5W-Monca-yo) the thickncsses were proportionally very high (C-l).

¡Jpper Bathonian (up to Ihe Lower Callovian Uneonform¡ty) (Fig. 4a, c[5J).

The 5-Demanda central basin facies. including the formen Canalesswell anca (M-l/3), get more uniform with higher sedimentation rates, whilein the marginal 5W Demanda-Cameros regions the terrestnial influencestncreased distinctively tnore. Thcre three parallel facies bclts are formed:first, in (he 5W-Demanda, with lumachelle ennichments intercalating (henormal sandy basin facies (M-3/4); second. in the San Leonardo Strip andadjacent Castrovido area, a higher-energetic zone with greater supplies ofquartz sand and reworkcd carbonate particles as aggregate- and coated-

The Bathonian and Callovian of the Northwest-Jberian... 133

gnains (M-4/5/6), including local little quartz deltas (M-7); and third, as themost near-shore, the further existing coated-grain oolite belt (E-1/2).

The shallow oolitic platfonm arcas of the Demanda were reduced infavour of the eastward expanding deeper sandy basin. Between these wodiffercnt environmen(s the transitional «slope» facies is found aroundMontenegro/Santa mes and Anguiano (T-3/4/5). ALo the N-Demandawere now included in the sandy basin realm afien a continuous transitionfroín the spongiotuberolitic facies (N-6 > M-3).

In (he Madero-Moncayo territory Uppen Bathonian nowhere is proved;a snatigraphic gap consisted at leas from Aldealpozo (W-Madero) to thcAgreda anca (NW-Moncayo), as a sign of sedimen(ary omission, supposingsmall quantities of later erosion. Probably only the 5W-Moncayo oolites(C-l). the sponge tuberolites near Soria (5-1) and the slightly detritie mscri-(es of dic E-Moncayo (0-4) continued sedimentation until beginning ofLower Callovian.

The regression reached its maximum in Lower Callovian with a sedi-men(ary standstill in most ncgions of (he NW Iberian realm, from the SE-Demanda over dic whole Cameros and Madero to (he SW-Moncayo, con-nected with (he formation of ferruginous crusts and hardgrounds (LowerCallovian Unconformity). On the contnary (he sedimentation did not in-kmrupt in the Demanda Basin, same as in the Zaragoza Basin as in thewhole Aragonese tenritory.

Lower Callovian (after the Lower Callovían Unconformity) (Fig. 4b, dI71).

In (he Demanda basin (he facial belÑ continued exisdng: The 5-De-manda remained as (he basin centre with neanly unchanged peloidic quartz-detritic sedimentation (M-3); also, (he N-Demanda ge( adjusted to (hisfacies. The 5W-Demanda region shallowed aud now came into a higher-cnengetic, more near-coas( aggregate- and coated-grains environment (M-6); (he facies obviously shiftcd to N-NE indicating the rcgressive trends. Inthe San Leonardo Strip and Espejón! Doña Santos areas duning LowerCallovian, on perhaps alrcady in Upper Bathonian, a sand bar was formedparallelly to the coastline. slightly marine influenced (facies SL). Thequartz sands wcre terminated by a fernuginous crust which formation ageis un-certain.

In te 5W-, N-Demanda and 5W- Cameros regions at least in earlyLower Callovian the preserved marine development ends. In the 5-De-manda (he sandy basin sedimentation continued, biostratigraphically pro-ven, fur(hen on.

After (he omission phase of (he Lower Callovian tJnconformity the E-Demanda and N-Cameros regions were also included in (he sandy peloi-dic environment of (he Demanda territory (M-3), then resulting a unitaryDemanda-Cameros basin np to (he coastal domains of dic Ebro Massif.

134 S. Wilde

In the most marginal zone (N-, NE-Cameros - at the present EbroBasin border) (he sedimentation set in somewhat laten or with reducedrates after (he omission phase. In the E-Demanda a special «Santa mesTrough»were formed with higher subsidence and less detnitie influx (M-2).

ANo nearly in the whole Madero-Moncayo territory the sedimentationstarted after the hiatus witli more or less sandy deposits. The strongestquartz sand influxes took place around Soria (P-5), likely in a vcry near-shore position bu completely marine. In the remaining West and centralMadero regions up to Olvega a shallow wave-agitated more calcareousplatform spread forming quartz-cored oolites (P-l).

The thickest deposits with correspondingly high subsidence nates weresedimented in (he greater par of the Madero-Moncayo tcrnitory duringLower Callovian, obviously more than in the later substages. Only thecoastal arcas around Bijuesca (southern 5W-Moncayo) remained in thatpeniod unaffected by the great subsidences and is characterized by reducedsedimentation. The terrestrial proximity specially near Torrelapaja wcrcsignificant with pure quartz sands directly after the omission phase. Incontrary te Cina area as the only par of the Madero-Moncayo tenritory ischaracterized by fauna-rich open-marine basin-like conditions (P-2/3). Pos-stbly there wcre a direct connection with the facially similar Zaragozabasin.

Open-marine influences reached (A-2/3) in (he beginning of the trans-gressive phase up to E of Olvega (NW-Moncayo). Ihen regressive trendsasserted aud lead prevailingly around Olvega-Agneda (o fine-detritie alter-nations of a very shallow sub- to intentidal coastal plain with sorne endo-benthonic life. named as «Agreda watt» or «tidal-fiat» (A-4). Thc E-Mon-cayo remained probably somewhat deeper and less agitated by tides, butmore abiogenie and restricted as a sandy marginal basin (A-5).

Only in the Pégado area primarily a locally restnicted echinoderm-richenvironment without any quartz influx were formed. interpreted as a «crí-noid lagoon» (A-l). After an omission this region were also included in thesandy realm.

Middle Callovian (Fig. 4b, dj8]).

In the Demanda-Cameros territory sedimentation continued with tlicrclatively uniform open sandy basin enviroment (M-3), now with an exten-sion at least from the S-Demanda to the present Ebro Basin border Lo-cally different subsidences however lead to very variable thicknesses. Wc-ther or not a (later eroded) sedimentation took place in the westem rcgions.(SW-Cameros. N-, 5W-Demanda and partially 5-Demanda) during Midd-le Ca-llovian is uncertain, corrcsponding dcposits are definitely missing.

Furtheron (he greater par of the W-Madero were dominated by intense

The Baiñonian ant] Callo vian oftire Nw-t/rwest-lberian... 135

siliciclastic sedimentation (P-5/7). Pure carbonate-free quartz sands werespnead in some arcas from the W-Madero to the Pégado. probably origina-ted from a deltaic bay of the Ebro Massif in the NE (Cervera-Fitero re-gion). Also the quartz-cored oolite platform of the Madero get more sandy(P-4) andexpanded up to the coastal anca of Bijuesca (5W-Moncayo) (P-6).tu conrary to these environments the Cina area remained as a fully man-nc influenced basin with open faunal exehanges (o the south (P-3).

In the NW-Moncayo around Agreda the «tidal fiat» deposition conti-nued (A-4). Its southern parE the Olvega/Cueva area, were influenced aswell from the southern more marine environment (A-7) as from the ternes-tnial clastic (A-8) of libe west. The E- Moncayo marginal basin stayedunchanged with abiogenie fine-detritie sedimenis, except a locally builtsand delta at Añón (A-lo)

The open-marine Zaragoza Basin came in its western part into quantz-dctnitic influences (R-4). In thc eastern pant (he sedimentation ended dur-ing the Middlc Callovian leading to an omission phase with iron-oolites.Thegeneral regression Idi thc Ebro mainlands expand (o SE narrowing (heNW-Iberian Strait.

Upper Callovian (up to tbe Dogger/Malm Bonndary Unconf.) (Fig. 4b,d[9j).

The real extension of (he Demanda-Cameros basin to (he wcst is un-knowun for the Uppen Callovian. because of the lack of (he concerningdcposit in its western pan. including now also the 5-Demanda. Unchangedquartz-detnitic peloidie deposits (M-3) were formed at least from Montene-gro area (SE-Demanda) to the marginal region of dic Ebro Massif (NE-Cameros),continuing cari) (be Dogger/Malm Boundary Unconformityphase.

The Madero-Moncayo facies got generally more regressive and is cha-racterized by an increase of quarliz detritus in connection with a shallo-wing of (he sea. In (he West and central Madero (he environment changedrelatively less (P-4/5). Probably about dic end of (he Callovian macro-sequence a mostly tbin sand plain covered aH tbis regions. partially alsothicken-bedded sand deltas set in somewhat carlier from (he N/NE (P-7).

Thequartz-oolitic platform were extended comprising Ihe regions fromsouthern Madero to (he 5W-Moncayo (P-6), including now the Cina area.To (he east it did not pass over (he Olvega-Toranzo Swell. More quartzsand were intercalated also in the MV-Moncayo region, in the northernmore tidal Agreda area (A-4/9) as in its southern pan (A-7/8). On the othenhand local open-marine influences are recognizable in (he E-Moncayo (A-6/7).

In accordance to the general rcgressive trend also (he Zaragoza Basinwere narrowed. At Belchite no sedimentation took place duning UpperCaflovian. a Aguilón lowest-rate deposits with iron-oolites were presení.

136 Si Wilde

Only in the Ricla area (W-Zaragoza) the open-marine and fauna-richbasin environment continued unchanged until (he late Upper Callovian(R-4).

About (he final Upper Callovian the regression got (o its peak and themacrosequence to an end. In the whole remaining sedimentation area anomission phase followed, from late tJpper Callovian to early Middle Ox-fordian, with hardground and iron-oolite formation, ami faunal condensa-tions (Dogger/Malm Boundary Unconformity (cf. Benkc, 1981).

The thickest iron-oolites were found in a marginal position near Jubera(NE-Cameros). In the W-Madero between Soria, Olvega and Noviercas ashallow intertidal lagoon with charadteristie cycles established (Aldealpo-zo Formaúon. cf. Oragastan el aL. 1987. see also further Colloquium con-tribution).

THE FACIAL-SIRUCTURAL FRAMEWORK

The facies variety of the studied formations is mainly caused by the in-fluences of the both sides adjacent emerged mainlands and highs. as wellby the internal structural framework of the depositional area.

The sedimentary territory is limited (o (he NE by the Ebro Massif andto (he 5W by dic Meseta and its forelands, especially thc Burgos and thcSoria-Ateca Highs, forming a strait trending NW-SE. same as the prcsent-time Ibenian Range.

Thc internal fragmentation of thc NW Iberian carbonate platform andthe facies boundaries connected with it, follow lines and siructures con-trolled by the main directions NNW/NW-SSE/SE and NNE/NE-SW. Such«lincamenis» are compiled in the structure maps (Fig. 5a. b). Many ofihese structural elemenlis can also be recognized ye( in the pnescnt-timetectonical framework.

In dic 5W Cameros sorne NW-SE striking lineamenlis (BQL = Barbadi-lío-Quintanar L., SLL = San Leonardo L.. HEL = Hortezuelos-Espejon L.)formed facies belts during Middlc Baihonian to Lowen Callovian. One ofthcse lineamens get reinforced during dic Wealden Basin developmcntforming one of lihe main marginal faults. The Alpide Orogeny inverted thisstnucture (o (he present-day San Leonardo Fault.

The East Demanda Line (EDL) separated as a N-S trending transitio-nal zone (he oolitic platform of the northern Cameros with i(s greatersubsidences from the spongiotuberolitic one and laten from (he sandyDemanda Basin.

A special (rough with higher subsidences formed in the Demanda Ba-stn centre during Upper Bathonian/Lower Callovian (MTr = MansillaTrough).shifting to (he East in Midd¡c/Upper Callovian (SITr=San(a mesTrough).

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TheBathonian ant] Callovian of the Northwest-Jberian... 139

Ihe negion of the Ebro Basin borden is charactenized by a complexlineament and fault system (Jubera-FiteroZone. Tischer, 1966). Alreadyduring Bathonian and Callovian diis anca, 1am marginally to the EbroMassif, was fragmentated into several blocks with different subsidences.Similarly the fault system of (he North Cameros (Torrecilla-Leza Zone)were active already during the siudied stages. Ihe NE-SW sriking NonthCameros Lineament (NCL) laten played an important role, as a main stri-ke-slip fault of the Wealden Basin.

The central area of the Madero-Moncayo territory is characterized bythe Olvega-Toranzo Swell (OTS) recognizable by an extended stratigraphi-cal gap of differcnt spaces of time. The omission phase ranges from LowerHaihonian up to Lower Callovian at the centre, and in the outer pan star-tung somewhat later in Middle or Upper Baihonian. Presumably the swellexpanded successively during the Bathonian and had its peak along (hefacies Iimiting Olvega-Toranzo Lineament (OTL). Its course is obviouslyconformable (o a present main fault. Another parallel stniking lincamcnt(ATL = Aldealpozo-Torrelapaja L.) separated blocks of different faciesand subsidences.

Fig. 5,—Structural framework of the NW lberían realm w¡th the fac;ally recogn¡zed «Li-neamenís» (sea text) and the possibla Iocations of tha limiting emerged mainlands (EbroMassi f and Meseta with its foreland «highs»).The numbers refer to thicknesses for thelt¡thottiaoi of (i¡llowi:o¡i ¡1tacro—seql¡ertce rc-sltectivel\’. Sa. Structr¡ralmap of the Hatbo¡iian—l)ot signatura begin of sandy facies in Lower Bathonian (closely dotted) or Middle Balbo- -

nian (widely dotted). Vertical unas: Stratigraphical gap in thc Madero-Moncayoarea withthe centied Olvega4oranzo swell (OTS). beginning in Lower (close unes), Middle (widelines). or t..tpper Bathonian (interrupted lines). partially presumed. Double numbers refer tosandy (upper) and quartz-free (lower number) portion of Bathonian. 5b. Structural map ofthe Caltovian. Horizontal tinas: .Fnd of presarved marine facies. before Callovian (closeunes). in Lower (wide Unes) or Middle Callovian (interrupted lines). Vertical and diagonalunes: Presi¡mably longer omission phases (gaps) during Lower Callovian (vertical) or UpperCallovian (diagonal) respeetively.lig. 5.—Lscjoe¡na tectón¡co-estroctural del NW cíe la Cordillera tbérica. con los «Alinea-mientos» rcconoc¡dos lhcialmente (véase el texto) y las localizaciones su-puestas de los terri-torios emergidos (Macizo del Ebro y la Meseta con «Altos» adyacentes). Los números serefieren a los espesores cíe la macro-secuancia del Bathonianse respecto a la del Calloviense.Sa. Mapa estructural del Bathoniense. Puntos: comienzo de la facies arenosa durante elBathoniense Inferior (punteado denso) o Bathoniense Medio (punteado ligero). Lineas verti-cales: Laguna estratigráfica en el área del Madero-Moncayo con eí Umbral de Olvega-Toranzo (OTS) situado en el centro que comienza durante el Bathoniense Inferior (lineas

ttret¡dl¡s). Medio (li¡ieas continuas) o Sc¡íterior (lineas discontinuas), parcialmente sc¡pc¡e.>la. Númerosdobles: espesores de la parte arenosa (número de arriba) y parte sin cuarzo(numero de abajo) del Bathoniense. 5b. Mapa estructural del Calloviense. Lineas horizonta-les: Fin al cíe la facies ¡it arin a con servada antes cíe Cali ovien se (líneas apretadas), durante el(allovie,tse Interior (lineas eflfltifldulsj ci Medio (li¡íetcs discontinuas). Las l¡¡íeics vertieaIes~diagonales: Fases de omisión (lagunas estratigráficas) presuntamente prolongadas duranteel Cal loviense 1 feriar (verticales) o durante el Calloviense Superior (diagonales).

140 S. Wilde

CONCLUSION

The intensified facies variability during Bathonian and Callovian timein the NW-Iherian is caused mainly by wo factors:

Firstly, global sea level changes gaye the main sequencial rhythmsleading in the shallow NW-Iberian platform to more facial divcrsity thanin (he gcnerally more deeper and more open-manine neighbouring Canta-bnian and SE-Iberian realms.

Sccondly. tectonie activities set in or intensify during these stagcs. Whi-le during most of (he Liassic and lowen Dogger the depositional environ-tnents are relatively more or less uniform. (he Bathonian and Callovian ischaracterized by an increasingly regional differenta(ion of facies. The acti-vities lcd lo a stnucural framework of dic marine platform, dividing it intoseveral blocks with very different subsidence histories. which lcd conse-quently huio lihe manifold envinonments. Ihe sanie tectonie movemeniscaused (he uplift phases of the adjacen( emerged mainlands which supplythose huge amouns of quartz detritus into (he marine realm. in thc De-manda Basin hcginning at Lower/Middle Bathonian and (ben cvcrywhereat Lowcr Callovian time. The regional influenced developmcnts overprintoften the general trend of ncgression.

Thesc tectonie movements lead in thc following rnega-cycle of (he non-marine Wcaldcn to thc large Strike-slip Fault Basin wi(h ilis synsedimcn-tany marginal faul( systems and its grca( internal subsidences and bedthickncsscs. The dcvelopmcnt of the Cameros Wcalden Basin is intcrpre-ted by some authors (cg. Salomon. 1982; Wiedmann u a/.. 1983) as connec-(cd with or caused by (he main Initial Phase of thc Biscay Rifting. Butmany strucural clements of (he later Wcalden Basin already appearedeven during Baihonian-Callovian stages. as (he satdied facial paleogeo-graphical paerns indicae. So the initial phasc of Biscay Sprcading pos-sibly makcs thcmself evident alrcady during ibis lime.

BIBLIOGRAPHY

I3ENKF., K. (1981): Die Dogger/ MaIm-Wende in den NW-Keltibenischen Ketten(Spanien) und angrenzenden Cebieten. Sedimentologie, Stratigraphie und Pa-láogeographie. (Thesis Univ. Bochum, 1980). Facie’.s 4: 95-164.

BENKL. K.: DURKOOP, A: ERRENST, Ch., and MENSINI( ¡-1. (1981): Dic Ko-rallenkalke im Ober-Jura dar nordwestlichen Iberisehan Kctten (Spanien). Fa-cie.s 4: 27-94.

HULARO. P. E (1972): Le iurassique Moyen et Supérieun de la Chaina lbéniquesur la bordure du Bassin dc libre (Espagne).Thesis Univ. Nice. vol. 1: 702 Pp.,vol. II: 39 pl.. lOO fig.

CONZE, R.; ERRENSTCh.. and MENSINK, H. (1984): Dic Amrnoniten desObe¡--Callovium bis Unter-Kimmeridgium in dan Nordwestlichen Keltiberis-chen Katten. Palaeontographica A. 183 (4-6): 162-211.

The Bathonian ant] Callovian of Ña Northwest-Iberian... 141

DRAGASTAN, O.; MENSINK, H.; MERTMANN. D.. and WILDE, 5. (1987):Ktistennaha Sedimantationszyklen im Obar-Jura dan westlichen Madero. Nord-Spanian. Ni ib. Ceo!. Palñont. A/ib., 175 (1>: 377-398.

ERRENST. Ch. (1984): Dar marine Malm in dan nordwastiichen Kel(ibarischenKettan (Spanien). Z. Dt Geol. Ges., 135: 45-55.

ERRENST. Ch. (1987): Das korallenfúhrende Kimmaridgium den nordwestlichanlberischen Ketten und angrenzenden Gabiela. Fazies. Palaogeographie undBeschneibung dar Korallenfauna. Thesis Univ. Bochuni. 161 pp.. (pubí. in Pa-Iaeontographica A. in press).

GERVAIS. A. (in prep.): Das Ober-Bajocium den NW-Iberischan Kattan. ThesisUniv. Bochum.

GEYFR. O. E; BEUMEL. H., and HINKELBEIN, 1<. (1974): Die Granzoolithe imJura von Otspanien. N. ib. GeoL Paláonr. Abh., 145: 17-57.

GOMEZ., 3.1(1978): Características generales del Jurásico en facies carbonatadasde] sector Levantino de Ja cuenca ibérica (Valencia - Castellón - Cuenca).In:Grupo Españolde Mesozáico:Guía de las excursiones al Jurásico de la CordilleraIbérica. Dep. Paleont.& Estratigr., Fac. Cienc.Geol? Unir Complutense.VIII: 1-17.

(jOMEZ. J. J. (1979): El Jurásico en facies carbonatadas del sector Levantino dalaCordillera Ibérica. Sernin. Estratigr, Ser Monogr. Fact Ciene. GeoL Unir. Complu-tense, 4: 683 Pp.

(JOMEZ, J. 3., and GOY. A. (1979): Las unidades litoestratigraficas del Jurásicomedio y superior en facies carbonatadas de la Cordillera Ibérica. Estud. Geol.,35: 569-598.

MENSINK, H. (1966): Stratigraphia und Palaogeographie des marinen Jura in dennordwastlichan Ibarisehen Kattan (Spanien). Beih. Geol. ib.. 44: 55-102.

MENSINK, H., and MERTMANN, 0. (1984): Diskontinuitáten im Unten-Callo-vium dar nordwestlichen Keltibanischen Kettan. N. ib. GeoL Pa/áonít A bu., 167(2): 189-223.

MENSINK. H.. and MERTMANN, D. (1988): Dic Geologie der Juragabieta umOlvega (Sierra del Madero, del Moncayo und de Toranzo). BochumerOcaL u.Geotee/in.Arb...30: 99 pp.. with 1 gea>. mnap. 1:46.000.

MERTMANN, D. (1986): Die negressive Fazies-Entwicklung im Obar-Toarcium/Aalenium dar NW-Iberisehan Kattan, Spanien. (Thesis Univ. Bochum. 1984). N.ib. GeoL Paltonr Ab/i., 173; 1-46.

SALOMON. J. (1982): Les formations continentales du .lurassiqua supérleur -

Crétacé infériaur (Espagne du Nord - Chainas Cantabrique et NW Ibniques).Mém. (kot Unir. D~on. 6: 227 Pp.

SCHEER, U. (in prep.): Das Untar-Bajocium dar NW-lbarischen Ketten. ThesisUniv. Bochum.

SCHUDACK, M. (1984): Dic Jura/Waalden-Granzschichten in den nordwestli-chan Iberisehen Ketten (Spanian). Z. ¡It GeoL Ges., 135: 57-65

SCHLIDACK. M. (1987): Charophytanflora und fazialle Entwicklung dar (ireuz-schichten marinarJura/Wealden in dan nordwastliehen Ibarisehan Ketten (mitVergleichen zu Astunien und Kantabnien). (Thesis Univ. Bochum. 1985>. Pa-laeontographica. R, 204: 1-180.

TISCHER, G. (1966): Ubar die Wealdan-Ablagarungen und die Tektonik dar óst-lichen Sierra da los Cameros in den nordwastlichen Iharisehan Kattan (Spa-roen>.Reih. Ceo!? ib.. 44:123-164.

142 S. Wilde

WIEDMANN, J.. REITNER. Ji, ENGESER, 1, and SCHWENTKE, W. (1983):Plattentektonik. Fazias- und Subsidanzgasehichte das baskokantabrischanKontinantalrandes wahrand den Kraida und Alt(ertiár. Zitteliana, 10: 207-244.

WILDE, 5. (1988): Das Batlionium und Callovium den Nordwes-lbenischan kat-ten (Jura, Spanien). Sequenzen einer sich diffarenzierendan Epikontinental-Plattform. (Thasis Univ. Bochum, 1987). Bochumer Geo!? u. Geotechn. .4rb., 31: 1-222.

WNENDT-JUBER, E. (1985): Dic Mikrofauna und -flora dar Korallenkalka iniKimmeridgium dar NW-Tbarischen Ketten (Spanien). Thasis Univ. Bochum.92 pp. (pubí. in Palaeontographica A, in prcss).

Recibido: 13 marzo 1989Aceptado: 12 julio 1989.