Up-to-date Spanish continental synthesis and paleoclimatic interpretation

1 2 2 4 J. P. CALV0 , R. DAAMS , J. MORALES , N. LOPEZ-MARTINEZ3, 1. AGUSTI , 6 6 6 P. ANADONS, 1. ARMENTEROS , L. CABRERN, J. CIVIS , A. CORROCHAN0 , 2 IO M. DIAZ- MOLINN, E. ELIZAGN, M. HOYOS , E. MARTIN-SUAREZ , J. MARTINEZ", I2 13 13 E. MOISSENET , A. MUNOZ , A. PEREZ-GARCIA , A. PEREZ-GONZALEZ'\ I6 I6 J. M. PORTER01S, F.ROBLES , C. SANTISTEBAN , 17 IO I9 T. TORRES , A. J. VAN DER MEULEN 18, J. A. VERA AND P. MEIN

I Dpto Petrolog{a, Fac.GeoI6gicas, Univ.Complutense. 28040 . 2 Museo Nacional Ciencias Naturales, CSIC. Jose Gutierrez Abascal, 2. 28006 MADRID. 3Dpto Paleontolog{a, Fac.GeoI6gicas, Univ.Complutense. 28040 MADRID. 4Institut Paleontologia "M. Crusafont". 08201 Sabadell, BARCELONA. 5Inst. "Jaume Almera ", CSIC. Mart{ i Franques sin. 08028 BARCELONA. 6Dpto Geolog{a, Fac.Ciencias, Univ.. 37008 SALAMANCA. 7 Dpto Geolog{a Dindmica, Fac.Geolog{a, Univ.Barcelona. 08028 BARCELONA. 8 Dpto Estratigrafla, Fac.GeoI6gicas, Univ.Complutense. 28040 MADRID. 9ITGE. Plaza del Temple, 1. 46003 VALENCIA. 10 Dpto Geolog{a, Fac.Ciencias, Univ.Granada. 18071 GRANADA.

11 EGEO. Gaztambide, 61. 28015 MADRID. 12 1 rue Voltaire. 75011 PARIS. 13 Dpto Geolog{a, Fac.Ciencias, Univ.Zaragoza. 50009 ZARAGOZA. 14 de Ciencias Medioambientales, CSIC. Serrano, 115. 28006 MADRID. 15 Compaii{a General de Sondeos (CGS). San Roque, 3. Majadahonda, MADRID. 16 Dpto Geolog{a, Fac.BioI6gicas, Univ. Valencia. Dr.Moliner sin, Burjassot, VALENCIA. 17 Esc.Tecn.Sup.Ingenieros de Minas. R{os , 21. 28003 MADRID. 18 Inst. v.Aarwetenschappen. Budapestlaan 4. 3508 TA UTRECHT. 19 Departement Sciences de la Terre. Universite Claude-Bernard, Lion 1, F-69622 Ville Urbanne, CEDEX France.

Abstract: A synthesis of the Spanish continental Neogene is presented by designing an integrated correlative chart of the Neo- c "gen-e -succes-siuns-ofthe -lberian-PeninsuIa-.-Ninemain-sedimentary-breaks-have-been -distinguished-in-most-of-the-basins~ -'I'hey are considered a valuable criteria for correlation as they occur in similar time intervals from basin to basin. The determined se­ dimentary breaks occur in the Agenian, Ramblian, Middle Aragonian, Late Aragonian, Late Vallesian, Middle , Late Turolian, Late Ruscinian-Early , and Villafranchian ages. The larger interior basins (Ebro, Tajo, Duero) show a fairly complete Neogene sedimentary record in which the above mentioned sedimentary breaks are usually well recognized. A good correlation may be established from basin to basin. Likewise, there is a fairly good correlation among the Upper Mioce­ ne- sedimentary record of basins spreading out in Levante and southeastern Spain. However, the correlation is not as clear in those basins located within the Iberian and Catalan Coastal Ranges, which usually do not show a similar sedimentary pattern. The comparison between Neogene stratigraphic logs in most of the Spanish continental basins and the pattern of global events from currently accepted Cenozoic Cycle Charts allows recognition of chronological coincidences, especially with re­ gard to the age of seven major sedimentary ruptures (those developed at about 24.5 Ma, 22 Ma, 16 Ma, 13.5 Ma, 9.5 Ma, 5.5 Ma, 3.3 Ma). Evolutionary sedimentary trends in both offshore Mediterranean areas and inland peripheral zones of the Iberian Peninsula show also striking coincidences regarding the chronology of major sedimentary breaks observed in continental suc­ cessions. Paleoclimatic curves for the Spanish continental Neogene display four relative temperature peaks indicative of warm climatic conditions (Late Agenian, Early-Middle Aragonian, Vallesian-Turolian, and Late Villafranchian) as well as five relati­ vely dry periods (Early Ramblian, Middle-Late Aragonian, Middle Turolian, Late Ruscinian, and Middle Villafranchian ages).

Key words: Neogene, Continental basins, Stratigraphic correlation, Sedimentary discontinuities, Paleoclimates, Spain.

Resumen: Se presenta en este trabajo una sintesis del Ne6geno continental espafiolmediante la elaboraci6n de un esquema de correlaci6n general de las sucesiones ne6genas en la Peninsula Ib€rica. Se reconocen nueve rupturas 0 discontinuidades mayo­ res dentro del registro sedimentario de un total de 16 areas que cubren la mayor parte de las cuencas continentales terciarias de la Peninsula. Las rupturas, denominadas de acuerdo con su posici6n crono16gica, son las siguientes: Ageniense, Rambliense, Aragoniense medio, Aragoniense superior, Vallesiense superior, Turoliense medio, Turoliense superior, Rusciniense superior­ Villafranquiense inferior y Villafranquiense. Las grandes cuencas interiores (Ebro, Tajo, Duero) presentan un registro muy completo de las sucesiones ne6genas y de las rupturas arriba sefialadas, las cuales tienen buena correlaci6n de una cuenca a otra. De igual modo, existe una correlaci6n notable entre los registros sedimentarios del Mioceno superior-Plioceno de las cuencas de Levante y el Sudeste. Sin embargo, la correlaci6n es menor con las cuencas situadas en la Cadena Ib€rica y la Ca-

Rev. Soc. Geol. Espaiia, 6 (3-4), 1993 30 J. P. CALVO Y OTROS

dena Costero Catalana. La comparacion entre el registro sedimentario Neogeno obtenido en gran parte de las cuencas continen­ tales espafiolas y la secuencia de eventos globales a partir de los cuadros de ciclicidad para el Cenozoico actuall11ente acepta­ dos permite reconocer coincidencias cronologicas entre ambos, especialmente en 10 que se refiere a siete de las rupturas sedi­ mentarias mayores (las definidas a 24.5 Ma, 22 Ma, 16 Ma, 13.5 Ma, 9.5 Ma, 5.5. Ma, 3.3 Ma). Las tendencias en la evolucion sedimentaria de las sucesiones Neogenas, tanto en areas del "offshore" Mediternineo como en zonas perifericas de la Penfnsula Iberica, muestran igualmente notables coincidencias en 10 que se refiere a la cronologfa de rupturas sedimentarias mayores ob­ servadas en sucesiones continentales. La interpretacion paleocIimatica, resumida en las curvas de humedad y temperatura que acompafian el cuadro de correlacion, permite definir varios cambios climliticos a 10 largo del Neogeno en Espafia. Destacan cuatro picos relativos de temperatura (Ageniense superior, Aragoniense inferior-medio, Vallesiense-TuroIiense y Villafran­ quiense superior), los tres primeros indicando posiblemente condiciones subtropicales. De igual modo, son detectables cinco perfodos de sequedad relativa (RambIiense inferior, Aragoniense medio-superior, Turoliense medio, Rusciniense superior y Vi­ llafranquiense medio). Estas tendencias paleocIimaticas son en buena parte contrastables con las observadas a partir de suce­ siones marinas.

Palabras clave: Neogeno, Cuencas continentales, Correlacion estratigrMica, Discontinuidades sedil11entarias, Paleoclimas, Espafia.

Calvo, J.P. et al. (1993): Up-to-date Spanish continental Neogene synthesis and paleocIil11atic interpretation. Rev. Soc. Geol. EspaFia, 6: 29 - 40.

Seven years ago, an overview of the Neogene ba­ cording to the established marine-continental correla­ sins of Spain was presented at the VIIIth Congress of tion chart, the sedimentary breaks identified in conti­ the Regional Committee of the Mediterranean Neoge­ nental sedimentary sequences seem to be chronologi­ ne Stratigraphy in Budapest under the title "Approach cally equivalent to those related to major events in the to the Spanish Continental Neogene Synthesis and Pa­ marine realm. This latter observation is probably the leoclimatic Interpretation". This contribution was aut­ most controversial. hored by 16 researchers, specialists in different fields The aim of this present paper, which is conceived of the Neogene geology, who were helped by 23 other as an updating of the previous synthesis, is to test the researchers yielding specific information in some are­ current validity of that contribution in view of the new as. The workshop was instigated and coordinated by data provided by: 1) recent findings of mammallocali­ Dr. L6pez-Martfnez. The final draft of the Spanish Ne­ ties and the biostratigraphical information supplied by ogene Synthesis can be found in L6pez-Martfnez et al. them, 2) advances in our stratigraphic and sedimento­ (1987). logical knowledge of basins, and 3) new proposals on The methodology of the synthesis written in 1985 the Neogene structural evolution of the Iberian plate, was based on modern techniques of basin analysis, es­ considered either as a whole or in particular areas. Un­ pecially the conceptual background derived from the fortunately, available information from magnetostrati­ tectono-sedimentary basin analysis (Megfas, 1982) as graphy, radiochronology or systematic chronostrati­ well as the development of sequential stratigraphy of graphical studies is far from being sufficient to supple­ basins (Mitchum et al., 1977; Vail et aI., 1984). Later ment the fossil mammal biochronological background; contributions on this topic may be found in Wilgus et therefore, this information will be offered in a restric­ al. (1988) and Vera (1989), among others. The use of ted manner. these techniques allowed the overcome of previous An initial change with regard to the previous synt­ syntheses that had been outlined mainly on the basis of hesis concerns the division and terminology of the Ne­ vertebrate paleontology (e.g., Aguirre et al., 1976). As ogene Mammal Ages on which the stratigraphic chart a result, a general scheme of correlation was establis­ is based. For instance, the Ramblian (Daams et aI., hed among the Neogene stratigraphic records of seven 1987) and Alfambrian (Moissenet et al., 1990) conti­ major areas within the Iberian Peninsula which, in nental stages are included in the new chart in order to turn, grouped sixteen basins and/or sectors of larger integrate recent proposals for the biostratigraphy of the basins. Two curves indicative of the evolution of hu­ Lower and Lower Pliocene, respectively. Ot­ midity and temperature throughout the Neogene in her changes concern the chronology of the stratigraphi­ Spain accompanied the correlation chart. cal divisions as well as the correlation between Neoge­ Although the results of that paper seemed to be ne Mammal Ages and the Marine Neogene Mediterra­ conclusive and the correlation chart fairly well fixed, nean Chronostratigraphy. Such changes are considered the authors did not hesitate to offer this approach with provisional as they will surely undergo modifications criticism and assessed their work as a starting point in the future. which should be improved by future developments. We assume the validity of the methodology of ba­ However, some major conclusions could be pointed sin analysis used in the paper by L6pez-Martfnez et al. out as quite consistent: 1) the lack of coincidence bet­ (1987). Although this methodology is viewed with cri­ ween main sedimentary breaks and classic chronostra­ ticism by some researchers (see. Santanach,. 19.89), tigraphical limits (these limits being characteristically even by co-authors of this paper, the establishement located within Tectonosedimentary Units (TSU)); 2) li­ and further correlation of major stratigraphic events in mits between TSU are not coincident with limits bet­ the diverse basins supports it as an acceptable working ween mammal-based biostratigraphic zones; and 3) ac- method.

Rev. Soc. Geol. Espafia, 6 (3-4), 1993 SPANISH CONTINENTAL NEOGENE 31

We take into account some valuable suggestions on zones 7 and 8 are fused. Bruijn et al. (1992) suppressed problems for recognition of sedimentary breaks in con­ these subdivisions as they are not useful at european tinental basins (Gonzalez et al., 1988; Pardo et al., scale. Distinction between zone 7 and 8 is not possible 1989). Most of the sedimentary ruptures described in either at larger distance from the reference level. this paper fit with the major types (1, 2, or 3-types) of The local zones are those of Daams and Freudent­ sedimentary breaks defined by these authors. Accor­ hal (1981) who defined zones A to I in Calatayud - Te­ dingly, the breaks are outlined either by sharp erosio­ ruel basins; Daams and Van der Meulen (1984) who nal surfaces, unconformities, paleokarst surfaces or defined zones X, Y and Z in Ebro, Almazan and Cala­ significant changes of the evolutionary trend of the se­ tayud-Teruel basins, respectively; and Alvarez et al. dimentary filling in the basins. Overall, they constitute (1987) who defined zone W for the Upper Oligocene major sedimentary discontinuities which are related to in the Loranca basin. Most of the local zones are defi­ tectonic activity in the basin margins. Although some ned in the type areas of the Ramblian and Aragonian. ambiguity may remain, the term 'sedimentary break' The use of the proposed local fauna subdivisions allows will be used for major sedimentary discontinuities that a more precise correlation than the biochronological can be recognized in an entire basin. framework of the MN system (Daams and Freudenthal, 1990). The local zones can be used independently for both micromammal and macromammal faunas. Geochronology, bio- and chronostratigraphy

The geochronological scale presented in this paper Summary of the Spanish continental basins and is that of L6pez-Martinez et al. (1987) with some mo­ their neogene sedimentary record difications. First of all, we separated the left column of the marine chronostratigraphy from the continental General characteristics stratigraphy because there exist few points of correla­ tion between the marine and continental realm in Three main Tertiary continental basins are located Spain. Two dashed lines between the marine chronos­ in the interior of the Iberian Peninsula (Fig. 1). The tratigraphical scale and the continental one are drawn. Duero basin, in the north-central part, is bounded by The first dashed line represents the correlation between the Cantabrian Range, the Hesperic Massif and the the mammal locality of Crevillente 6 and the Globoro­ Central System. The Tajo basin is located exactly in talia conomiozea zone of the Lower (Bruijn the centre and is bordered by the Toledo Mountains, et al., 1975). The second dashed line represents the co­ the Iberian Range and the southern side of the Central rrelation between the mammal locality of La Alberca System. Finally, the Ebro basin is bordered by the Py­ from upper MN13, intercalated between marine sedi­ renees, the Iberian Range and the Catalan Coastal Ran­ ments, to the Late Messinian (Mein et al., 1973). Tie­ ge. Each of these basins exceeds 15,000 km2 in extent, points of lesser order are also taken into account for and together they occupy a large portion of the total the construction of our chronological framework. area of Spain. In addition to these large Tertiary ba­ Reinterpretation of the paleomagnetic data of Dijks­ sins, other minor intramountanous basins occur within man (1977) of the Armantes section near Calatayud si­ the bordering ranges or in areas which were covered tuates the Armantes 7 fauna (Zone F of the Upper Ara­ by the sea throughout most of the Neogene. This is the gonian) at 13.7 Ma (Daams et aI., in prep.). Another case of Late Neogene basins of the Betic domain and tie-point is that between the Early and the some other peripheral basins. upper part of Zone D of the Middle Aragonian. This The Neogene sedimentary record is fairly complete correlation is based on the first indications of a cooling in several Spanish basins. With regard to the continen­ of the surface waters of the Mediterranean (Chamley et tal Neogene, the sedimentary sequences are especially al., 1986) and the cooling on the continent interpreted well developed within the three large interior basins by Van der Meulen and Daams (1992). Another corre­ which were separated from the marine realm since lation is that of the Aragonian/Vallesian boundary as their formation in the Paleogene. The thickness of the evidenced by the Hipparion-datum in the Mediterrane­ continental Neogene successions in these basins ranges an area. Sen (1990) argues that there is no radiometric from 500m to 1,500m. In the other basins the thickness data available that can prove that the Hipparion-datum of the continental Neogene successions is highly varia­ is older than 11 Ma, and that magnetostratigraphical ble but in a few cases it reaches up 1,500 m, particu­ data situates its age at a maximum of 11.5 Ma. In this larly in those generated as a consequence of rifting paper we follow Sen's suggestion and we set the da­ processes (Anad6n et al., 1989a). tum at 11.5 Ma. The formation and evolution of the Tertiary basins In the following columns we prefer to distinguish in Spain are closely related to the upbuilding of the Py­ between truly defined continental stages and mammal renean and Betic orogens and the internal deformation ages, such as was done by Steininger et al. (1990), but which affected the Iberian microplate (Vegas and Ban­ again with a modification. These authors mention a da, 1982; Anad6n et al., 1989a). The Ebro basin deve­ gap between the and Astaracian, a sugges­ loped as a foreland basin resulting from the upthrus­ tion' not followed by us. ting of the southern Pyrenean zones. A rather similar The MN subdivision presented in this paper does situation is recognized in the northern margin of the not have afbsubdivisions of zones 2, 3, 4 and 16, and Duero basin whereas the Central System bounds the

Rev. Soc. Geol. Espm1a. 6 (3-4), 1993 32 J. P. CALVO Y OTROS

tOO zoo km

Figure 1.- Map of the Iberian Peninsula with location of the Tertiary basins included in this synthesis. Larger Tertiary basins are written in ca­ pitals; the several subbasins or minor basins are indicated with italics. Encircled numbers indicate major structural chains bounding the basins: I, Cantabrian Range; 2, Pyrenees; 3, Central System; 4, Toledo Mountains; 5, Altomira Range; 6, Iberian Range; 7, Catalan Coastal Range; 8, Betic Ranges; 9, Hesperic Massif. basin to the south. This latter major structure has been Group, 1990). The infilling of the smaller basins (those interpreted as a big arch bounded by reverse faults re­ located in the Iberian Range, Betic domain or elsewhe­ sulting from the compressive deformation of rigid in­ re) displays different sedimentary patterns and a wider traplate areas (Vegas and Banda, 1982; Vegas et a!., spectrum of both alluvial and lacustrine facies. Nevert­ 1990) or as a crustal thickening due to basement thrus­ heless, many of the sedimentary breaks recognized ting (Warburton and Alvarez, 1989). Whichever the within these basins are chronologically equivalent to case, the Madrid basin, located to the south of the Cen­ those detected in the larger ones. tral System, received huge volumes of terrigenous de­ Figure 2 shows several simplified stratigraphic logs posits which account for Tertiary sediments nearly from all the basins included in this study. In practice, 3,500m thick. they cover most of the continental Neogene record in In general, all the compressional processes leading Spain (Fig. 1). Emphasis is put on the position of the to the formation of the large Spanish Tertiary basins sedimentary breaks. Some comments on these sedi­ were active throughout the Paleogene and, locally, into mentary breaks, ordered by time intervals, are given the Lower and Middle Miocene. Synchronously, seve­ below. Mammal sites included in Figure 2 are listed in ral minor or medium-size basins (Valles-Penedes, Ca­ Appendix A. latayud, Teruel, Rubielos de Mora, .. ) developed in the eastern part of Iberia as a result of extensional proces­ ses (Anad6n et a!., 1989b). In a similar way, a number Main Neogene sedimentary breaks of extensional or strike-slip small basins were formed in the Betic Zones during and after the emplacement of Agenian sedimentary break.- This sedimentary break the Betic nappes (Vegas and Banda, 1982; Sanz de has been recognized in the Ebro (both central and wes­ Ga1deano, 1990; Sanz de Galdeano and Vera, 1992). tern sectors) and Tajo basins. In this latter basin the se­ Most of these basins were filled with marine sediments dimentary break is recorded as Phase by in their first stages but in many cases show later conti­ Aguirre et al. (1976). The age of the sedimentary break nental successions of considerable thickness (Granada, has been well determined in the Loranca basin but ele­ Guadix-Baza, Fortuna,...) ments are lacking for a solid age determination of the In spite of the extreme complexity of the structural discontinuity throughout the Oligocene-Miocene boun­ framework of the Tertiary basins of Spain, some com­ dary in the Madrid basin. Rhodanomys faunas are pre­ mon trends in vertical evolution of terrestrial succes­ sent below and above the break. Its age corresponds to sions (both alluvial and lacustrine deposits) are obser­ the Y zone (Daams et a!., 1987) or to the limit between ved from basin to basin. Thus, in the Duero, Ebro and X and Y zones (probably to the Upper Oligocene) (L6­ Tajo basins the sequential evolution throughout the pez Martfnez and Torres, 1991). Neogene is marked by progradations and retreatments The sedimentary break is marked in the Ebro basin of the peripheral alluvial systems which show striking by a net progradation of alluvial systems over alluvial similarities in the three areas (IGCP-219 Spanish and laterally related lacustrine sequences which show a

Rev. Soc. Geol. Espaiia, 6 (3-4), 1993 NEOGENE M.a.I:~:~~:::~ VALLES-I MAMMAL TAJO BASIN DUERO- BASIN CALATAYUD - TERUEL LEVANTE BETICS HUMIDITY ITEMPERATURE INEOGENE CHRONOSTRATlGRA. AGE PENEDES DRY ... I~MOIST WARM ... I~CDLD MA:GMlL

I.S 1.6 I I 1 "zz ..J .... ~ P1AZENCIAN ..Jo:- 'V w :;:Ll.5 U I I o 15 ::;;z I :J ~~ ~s ~~ D.. ~z 14 ..Jo: ::J­ "ID o:Z 5 5.4 13 z w MESSINIAN z .. z Z .. 12 ..J w :J '" o o ..J u 0: 0: o o ::J ::J 0: :E ... 11 ... PIR ...::J HI 0: z z z .. 10 .. CJ 101~ u; VIC .. UJ i3 D.. ..J '" ::l :l 9 ..J J. CL ~ ~ ~ H CPO !i! ItS 0: I I 7/S CIl w Z UJ so Z .... G "'Z... ", ~ n. ",13 SERRA "'u n. ",,,, 6 Q "0:"' .. ::J F 0: ~ ::;: VALLlAN ::r: 5 ~-m n 151j W o o z ..J o o C :E LANGHIANI z '" C z ~ ::;; o 16.S '"0: '" '" 4 z w z z '" ~ w ffi f ELC '"UJ u '"UJ /\ Z ~ B ..J o ..J /\ gJ :E8LI1OIGALlAN 0: 0: /\ o 2010: o /\ "C ~ w 3 z A /\ ~ /\ tIl o '"..J /\ ID /\ ..J ::;; rvr AOUITANIAN .. 0: z z /\1 RA / z 23.2 2 II 1/\ NAV y z'" '"z UJ UJ rvr ~ '" Cl> 25 '" x '" :: CHATTIAN '" I PA I 0: 0: go UJz SY UJZ !"> o w >'"0:- 0:->'" a "'Z Cl> "'Z Cl I") LOCAL ZONES AFTER WESTERN CENTRAL lORANCA . MADRID DUE RO ALMAZAN CALATAYUD DAROCA- TERUEL VALLES- CABRIEL JUCAR ALBACETE- AUCANTE GUAOlx GRANADA ,.... EBRO EBRO CAAMS a FREUDENTHAL(190t .1.988) CALAMQCHA PENEOES PREBETICO -MunCIA -BAZA t>l DAAMS a VAN OER MEULEN (t.984) {J ALVAREZ SIERRA .t 01 (t.987) l:l :::, ~ DOMINANT TERRIGENOUS ~ DOMINANT EVAPORITE ~ ~ ~ MARINE FORMATIONS J'l SEDIMENTARY UNITS SEDIMENTARY UNITS -n MAGNETOSTRATlGRAPHIC 0\ INFORMATION p:=j==I=f DOMINANT CARBONATE rv SEDIMENTARY BREAKS ." PALEOKARST SURFACES __ll <:;:; I::::i::::::::: SEDIMENTARY UNITS CDISCONTINUITIES) ~ t£iA MAMMAL SITES WITHIN #I- RADIOMETRiC .... ~ KA~ST DE~O~ITS AGES \C Figure 2.- Integrated Correlation Chart of Spanish Neogene continental basins. Lithostratigraphic logs for some basins are separated in different sectors. The graphic is accompanied by paleoclimatic curves for ~ w the Spanish Neogene. Meaning of codes for fossil mammal sites is included in Appendix A. w 34 J. P. CALVO Y OTROS positive sedimentary trend (Gonzalez, 1989; Perez by L6pez-Martfnez et al. (1987). Further studies have Gm'da, 1989; MUlloz, 199 1).To the north of the central demonstrated that a Late Aragonian sedimentary bre­ Ebro area (Huesca province), this sedimentary break is ak, first observed in the Madrid basin, can be also re­ represented by an angular unconformity between mam­ cognized in western and central areas of the Ebro basin mal sites of zone X (Santa Cilia) and zone Y2-Z (San as well as in the Duero. In all these cases the sedimen­ Juan-La Galocha) (Alvarez et aI., 1990). In Loranca tary break is marked by a net progradation of coarser the sedimentary break resulted from the reactivation of alluvial deposits over alluvial and/or lacustrine sequen­ alluvial fan systems (Dfaz-Molina et al., 1989). ces showing a positive depositional trend. The sedimentary break is located between the F and Ramblian sedimentary break.- Formerly defined as La­ G zones as indicated by ParacueIIos-S and Paracuellos­ te Agenian-Early Aragonian (L6pez-Martfnez et al., 3 mammal sites in the Madrid basin, Villanueva de 1987), this sedimentary break has been clearly recog­ Huerva and Moyuela in the Ebro, and Valladolid-I and nized in the Loranca basin (Tajo) where it is dated by in the Duero. This event is correlated with a faunas of the Loranca and Naval6n mammal sites, be­ second tectonic pulse included in the Guadarrama Pha­ low and above the discontinuity, respectively. In AI­ se that affected the Central System in the northern mazan, the sedimentary break is marked by an angular margin of the Madrid basin (De Vicente et al., 1990). unconformity near the basin margin and by a drastic sedimentary change in central parts of the basin where Late Vallesian sedimentary break.- This is a relevant alluvial deposits overlie lacustrine carbonate sequences event because of two reasons: I) the sedimentary break which contain the Cetina mammal site. An intra Z zone can be accurately recognized in the large basins (Ebro, biostratigraphic position is postulated for this event. Duero and Tajo); 2) as some recent investigations se­ Ligerimys (one species) and Eucricetodon are recorded em to indicate (Sanz de Galdeano, 1990; De Vicente et below and above the sedimentary break. al., 1990), the Late Vallesian sedimentary break re­ The relative chronological proximity of the two cords a major change in the tectonic strains affecting aforementioned sedimentary breaks is consistent with the Iberian microplate by that period. A generalised the remarkable tectonic activity developed throughout extensional phase lead to the development of grabens the Late Paleogene and Early Miocene in the Iberian and strike-slip basins in both internal and external zo­ Plate and other zones of the western Mediterranean nes of the Betics (Calvo et al., 1978; Sanz de Galdea­ (Vegas and Banda, 1982; Letouzey, 1986; Anad6n et no, 1990). Likewise, a drastic change of the paleogeo­ al., 1989). Unfortunately, the available biostratigraphic graphy of the large interior basins (Ebro and Madrid) information from some ranges, such as a number of is recorded (Calvo et al., 1989; Perez Gm'da, 1989; De small basins of the Iberian Ranges, is not as complete Vicente et a!., 1990). as needed for dating accurately the periods of basin The precise age of this discontinuity is stilI a matter formation and initial evolutionary stages (Sim6n, of controversy. Both Lower and Upper Vallesian fau­ 1984). nas are recorded below the discontinuity in the Duero and Madrid basins (L6pez-Martfnez et al., 1987; Alva­ Middle Aragonian sedimentary break.- This sedimen­ rez et a!., 1990; Sese et a!., 1990) but there is a lack of tary break seems to be generalized in most of the agreement with regard to the Iithostratigraphic position analyzed basins. It has been recognized clearly in the of mammal sites of VaIIesian age in some areas, parti­ Ebro basin as well as in Loranca and Madrid basins. In cularly in the Duero basin (Corrochano and Armente­ this latter basin the discontinuity is recorded as Neo­ ros, 1989; Portero et al., 1991). castellana Phase by Aguirre et al. (1976). The biostra­ tigraphic position of the sedimentary break is fixed by Middle Turolian sedimentary break.- This sedimentary the occurrence of mammal sites containing Hispanot­ break is significant as it may be correlated with the in­ herium below and above the break. A significant litho­ tra-Messinian regional sedimentary break (Santisteban, logical change between thick lacustrine evaporite suc­ 1981; Megfas et a!., 1983; Agustf et aI., 1985a). The cessions and sequences dominated by alluvial, carbo­ relationships between continental and marine deposits nate and gypsum deposits is recognized in the Ebro can be observed in the AIicante-Murcia area. Therein, and Madrid basins. This change is related to the tecto­ the Middle TuroIian site of Casa del Acero overlies nic reactivation of the basin margins combined with marine deposits of Messinian age (Agustf et al., the exhaustion of previous evaporite source areas (Cal­ 1985b; L6pez-Martfnez et al., 1987). The correlation vo et aI., 1989; Anad6n et aI., I989a). In addition, the between marine-continental may be also established on discontinuity may be marked locally, e.g., in the Ma­ the basis of several mammal sites in CreviIIente. Para­ drid basin, by paleokarst surfaces (Calvo et al., 1984). podemus faunas are recorded both below and above the In areas where marine and continental interfinge­ sedimentary break. ring is recorded, such as the VaIIes-Penedes area, the An additional event related to the Middle TuroIian sedimentary break may correspond to the progradation sedimentary break is probably represented by relevant of continental clastic facies over Upper coas­ depositional changes recorded in lacustrine basins of tal marine sediments. the Prebetic area (EIizaga, 1990). Data from the Ca­ briel and Granada basins also support the existence of Late Aragonian sedimentary break.- This sedimen­ this discontinuity which may be dated as an intra tary break was not outlined in the previous synthesis MN12 zone. In the Cabriel basin, the Fuente Podrida

Rev. Soc. Geol. Espaiia, 6 (3-4), 1993 SPANISH CONTINENTAL NEOGENE 35 mammal site dated at 7.2 Ma (Opdyke et al., 1990) is occurs between the Alqueria and Orce-2 mammalloca­ located below the discontinuity. lities.

Late Turolian sedimentary break.- Whereas this sedi­ Discussion mentary break is not well defined within the large inte­ rior basins (the Madrid basin may be considered an ex­ Several preliminary conclusions may be deri­ ception as the Algora mammal site of Late Tur6lian ved from the correlative lithostratigraphic chart pre­ age would be located above the rupture), the peripheral sented in Fig.2: Levantine and Betic basins offer a good choice for de­ a) There is a fairly good correlation among main termining its chronostratigraphic position. Thus, a Late sedimentary sedimentary breaks recognized in the stu­ Turolian sedimentary break (intra-MN13) can be defi­ died basins. Moreover, the sedimentary evolutionary ned in the Granada, Guadix-Baza (Agusti et al., 1988), trends of lithostratigraphic units defined between sedi­ Prebetic, Cabriel and Valles-Penedes basins. Apode­ mentary breaks show, in general, similar patterns from mus faunas are recorded below and above the disconti­ basin to basin. In many cases, the morphological cha­ nuity. In most cases the sedimentary break is represen­ racteristics of the breaks (paleokarst surfaces, erosio­ ted by an erosional surface and/or the overlying of te­ nal surfaces) is similar in a same time slice for diffe­ rrigenous deposits on lacustrine carbonates. rent basins. This sedimentary break has a probable absolute age b) The correlation among sedimentary breaks is of about 5.7 +/-0.3 Ma as recorded by the Monagrillo clear in the largest interior basins, especially within the volcanic event (Bellon et al., 1981) in the Las Minas Lower and Middle Miocene.interval as well as the lo­ basin (Prebetic) (Elizaga and Calvo, 1989). This is also wer part of the Upper Miocene (Vallesian). However, supported by paleomagnethostratigraphic insight from the correlation is poor among these large basins and the Cabriel succession where the Venta del Moro those located within the Iberian and Catalonian Coastal mammal locality dated over 5.47 or 5.78 Ma (Opdyke Ranges. On the other hand, basins of the Levante and et al., 1990) is located below the discontinuity. Betic areas show fairly· good correlative patterns th­ rough Upper Miocene and Pliocene. c) L6pez-Martinez et al.(1987) made emphasis on Late Ruscinian - Early Villafranchian sedimentary the chronological coincidence of most of the sedimen­ break.- The sedimentary break is located approxima­ tary breaks in both marine and continental series by tely in the Ruscinian (Alfambrian) - Villafranchian comparing the Spanish continental Neogene record boundary. It has been related to the Ibero-Manchega I with previously established charts of Neogene Global phase (Perez-Gonzalez, 1979, 1982) in the Tajo, Jucar, Cycles (Vail and Handerbol, 1983; Keller and Barron, and La Mancha areas. The sedimentary break has been 1983; and, in a regional scale, Soler et al., 1983). The also recognized in Teruel, where the Alfambrian stage updated synthesis confirms this impression. Further re­ has been defined (Moissenet et al., 1990), and in ne­ fining based on sequence stratigraphy (Haq et al., arby interior basins. In all these cases the rupture is re­ 1987, 1988) has led to the proposal of modified Ceno­ lated to tectonic reactivation resulting on both tilting zoic Cycle Charts which are currently accepted as a re­ and, locally (e.g., Loranca basin), strong deformation ference by most of the authors. According Haq et of previously deposited Neogene formations. The re­ al.(l988), the Neogene marine series record a highly cognition of this sedimentary break in Guadix-Baza is complex history of sea level changes with marked rela­ controversial (Agusti et al., 1988). tive rises and falls in several periods. The timing of Mimomys ischus (Esteban and Martinez Salanova, these eustatic sea level changes has been precisely fi­ 1987) as well as the last Hipparion faunas have been xed in Haq et al.'s curves (Fig.3). recorded both below and above the discontinuity, The comparison between stratigraphic logs from which has been dated c.a. 3.5 +/- 0.3 Ma according to the Neogene in most of the Spanish continental basins the volcanic event of Campo de Calatrava (Alberdi et (Fig.2) and the pattern of global cycles allows to re~ al., 1984). This event may be correlated with the Las cognize chronological coincidences, especially with Higueruelas mammal locality. regard to the age of seven major sedimentary sedimen­ tary breaks (Fig.3). This conclusion is considered to be Villafranchian sedimentary break.- The Villafranchian valid even if uncertainities in continental biostrati­ sedimentary break is widespread in most of the basins, graphy and marine-continental correlations in Spain where it records the terminal Neogene event prior to oblige to make only a tentative assessment. the development of recent fluvial systems. This sedi­ The agreement in the sequence boundary correla­ mentary break has been related to the Ibero-Manchega tions between marine basins lies in most cases on ap­ II phase (Perez-Gonzalez, 1979, 1982) in the Tajo, Ju­ proximate chronological coincidence, as deduced from car and La Mancha areas. Equus and Mammuthus as biostratigraphic, paleomagnetic and isotopic data. well as the typical Villafranchian ruminant faunas (Ga­ Many authors use sequence boundary ages established zella, Gazellospira, Leptobos, Croizetoceros) occur in Global Cycle Charts as a chronological reference for both below and above the discontinuity. The biostrati­ dating discontinuities elsewhere. Instead of, we have graphic position of the discontinuity is well determined obtained independent evidence for regional disconti­ in Guadix-Baza basins (Agusti et al., 1988) where it nuity correlations as well as to date them.

Rev. Soc. Geol. Espaiia, 6 (3-4), 1993 ::tl W := Q\ ~ fl IJ) CHRONOSTRATIGRAPHY I SEQUENCE STRATIGRAPHY (HAQ ET AL.,19Be ~ «a: MAIN c I Iw>- ,.... w I I EVENTS S EDIMENTAR Y >- MEDITERRANEAN ICYCLES 00: t>:I Z« BREAKS IN NEOGENE {J :E IJ) wow EUSTATIC CURVES IN THE I:> MARINE RELATIVE CHANGES OF ;:<, a: a: :::>ZCl CONTINENTAL z W w w THE SPANISH .1:> a o O::::l« (HAQ ET AL., 1988) BETIC a: a: COASTAL ONLAP 0\ o wo CONTINENTAL CHRONOLOGY w a: o 1J)!Il CORDILLERA ~ ~ NEOGENE LANDWARD BASINWARD w NEOGENE ~ .... CHRONOSTRATIG.I ~ 0.5 0 150 100 50 OM ...... 0.- IJ) \Q o ~

~ I u~3.4--­ o -' ZANCLEIAN lL 5 51- III

TUROLlAN ..... :-c n ? INTRA r 'V'V' LATE VALLE. < 101- VALLESIAN 10 o -< o t--11.5-- -l o;;0 lJJ UPPER C/J Z z « --- z 151-- o 15 Cl « MIDDLE 0: ~ « -- LOWER

201- 20

INTRA RAMBLlAN },~=)~:""=":""=-':"":::"":"':":=-=-=-tl--II "\.fV'RAMBLIAN

INTRA AGENIAN 'V'V' AGENJAN 25

Figure 3.- Chart for comparison of the chronology of major sedimentary breaks determined in Spanish continental Neogene successions and curves showing relative changes of coastal onlap during the Neogene (Haq et aI., 1988). A comparison is also established with chronology of major events recorded in the Betic CordilIera (after Pascual et aI., 1991). SPANISH CONTINENTAL NEOGENE 37

The coincidence of discontinuity ages between the are those of Van del' Weerd and Daams (1978), Daams Spanish continental Neogene record and Global Mari­ and Van del' Meulen (1984), Daams et al.(1987), Sese ne Charts show even better fitness than was previously (1991), and Van del' Meulen and Daams (1992), and stated (L6pez-Martfnez et al., 1987). In the Spanish will not be repeated in this paper. The temperature and continental Neogene chart (Fig.2), major sedimentary humidity curves are precised with regard to the pre­ breaks are at about 24.5 Ma (intra-Agenian), 22 Ma vious ones in L6pez-Martfnez et al.(1987) which is (intra-Ramblian), 16 Ma (intra-Middle Aragonian), due to an increase of information and new treatment of 13.5 Ma (intra-Late Aragonian), 9.5 Ma (intra-Late data by Van del' Meulen and Daams (1992). Vallesian), 6.5 Ma (intra-Middle Turolian), 5.5 Ma (in­ The recognized climatic changes are demonstrated tra-Late Turolian), 3.3 Ma (Late Ruscinian-Early Vi­ by humidity and temperature oscillations. Humidity and llafranchian), and 2 Ma (intra-Villafranchian). Main si­ temperature trends are not necessarily simultaneous. milarities with Haq et al. (1988)'s curve are twofold Four relative high temperature peaks, of which the (Fig.3): a) increase in frequency of relative changes of first three may indicate (sub)tropical conditions, are re­ coastal onlap (i.e., reduction of the time spacing of cognized during the Spanish Neogene. The first one is eustatic events) and continental sedimentary breaks in that of the Early Agenian, during which tropical large more recent Neogene times, especially since the Mes­ mammals like tapirs and pangolins are present in va­ sinian (Middle to Late Turolian); b) chronological rious faunas in central Spain. The second one is that of coincidence between many sedimentary breaks in both the Early and Middle Aragonian, during which Deinot­ marine and continental series. This is particularly clear herium (a tropical African proboscidian) entered the for global changes recognized in the , Lang­ Iberian Peninsula and Hispanotherium (a running rhi­ hian, Middle Serravallian, Middle Tortonian, Messi­ noceros with cement-filled teeth) spread widely. The nian, and in several periods throughout the Pliocene. third relatively warm interval is that of the Vallesian­ Main sedimentary breaks defined within the Spanish Turolian. In the Lower Vallesian of Catalonia, Pongi­ continental Neogene record appear to be delayed in time dae (apes) and again tapirs are present and in the entire in relation to Neogene sequence boundaries (Fig.3). Alt­ Iberian Peninsula the tropical chevrotains (Tragulidae) hough this displacement might be unreal as precise da­ have their maximum abundance during the Early Va­ ting of the sedimentary ruptures in the continental realm llesian. The fourth warm interval is that of the Late Vi­ is difficult, a "cause-effect process" of the sea level falls llafranchian and it is previous to the inmigration of ro­ on inland basins (perhaps a climatic effect as well?) otless voles like Allophaiomys. Several of the tempera­ may be postulated for explaining this stratigraphic rela­ ture trends are recognized in the marine realm as well tionship..Whichever the case, our understanding of how (Muller, 1984; Demarcq et aL, 1990). global changes recorded from marine series would be Five relatively dry periods are recognized. The represented in the inland realm is so far incomplete. first one is that of the Early Ramblian during which Regional studies of the Neogene sedimentary record running rhinoceroses and hypsodont ruminants (giraf­ in offshore Mediterranean areas (Soler et aI., 1983) and fes) are abundant. The second dry period is that of the inland peripheral zones of the Iberian Peninsula (Pas­ Middle Aragonian characterized by the so-called His­ cual et al., 1991; Sanz de Galdeano and Vera, 1992) panotherium-faunas (see above) and those of the first provide evidence that the sedimentary breaks recogni­ hypsodont bovid (Caprotragoides). The third and the zed in these nearby areas may be interpreted as a result fourth dry periods are those of the Middle Turolian of eustatic and/or tectonic events (Sanz de Galdeano and Late Ruscinian, respectively, during which anti­ and Vera, 1992). This latter work makes emphasis on lopes (high-crowned savannah-dwellers) are abun­ tectonism (or tectonism associated with eustatism) as a dant. The fifth relatively dry period is that of the main cause for sequence boundaries through most of Middle Villafranchian during which the horse Equus the Lower, Middle and Upper Miocene in SE Spain; and the steppe-elephant Mammuthus inmigrated into eustatism would be properly a relevant factor for detec­ Europe. ted coastal onlap during Langhian. The Spanish conti­ nental basins, mostly having evolved like closed tenes­ trial basins, have had their sedimentary filling contro­ Conclusions lled by tectonic readjustments during the Miocene (IGCP-219 Spanish Group, 1990). In contrast, the geo­ This paper, based on that presented some years ago logic evolution of many basins, even the largest interior by L6pez-Martfnez et al. (1987) in Budapest, summa­ ones, during Late Miocene and Pliocene underwent rizes recent findings about the Neogene stratigraphy of changes from closed to open conditions that probably most of the continental basins in Spain an updates the made them more sensitive to frequent eustatic sea level conelative chart for Neogene stratigraphic units. New variations which are characteristic for this period. findings of mammal localities and some, though spar­ se, recent radiometric and magnetostratigraphic data have been included in the synthesis. Palaeoclimatology Some modifications have been introduced by com­ parison with the geochronological scale used by L6pez­ The palaeoclimatic interpretation of this synthesis Martfnez et aL (1987). Main changes have been made is based on the composition and compositional shift in in order to include new biostratigraphic terminology time of micromammal faunas. The followed criteria and more refined biostratigraphic local zones.

Rev. Soc. Geol. Espaiia, 6 (3-4),.1993 38 J. P. CALVO Y OTROS

Nine main sedimentary breaks have been recogni­ tive temperature peaks indicative of either (sub)tropi­ zed as widespread occurring in the different basins. A cal conditions or less marked warm intervals. Five re­ good correlation is observed among the Neogene sedi­ latively dry periods are inferred from the palaeoclima­ mentary record of the largest interior basins (Tajo, tic curves. Duero, Ebro) through a time interval spanning Lower This paper fully corraborates most of the results Miocene to Vallesian. In a similar way, a fairly good achieved by L6pez-Martinez et at. (1987), in particular correlation has been determined for the Late Neogene the use of tectono-sedimentary analysis as a valid geo­ sedimentary record in eastern and southern basins. logical tool for this Neogene synthesis. On the other However, the correlation is poorer in those basins lo­ hand, this up-to-date confirms a main conclusion con­ cated within the Iberian and Catalan Coastal Ranges, cerning the non-coincidence of global discontinuities which usually do not show a similar sedimentary with classic chronostratigraphic limits. pattern. There is chronological coincidence between the se­ dimentary breaks recognized within the Spanish conti­ Main achievements of this paper are indebted to several resear­ nental Neogene record and sedimentary discontinuities chers who have furnished very valuable data to the authors. Accor­ dingly, they are considered analysis authors. We acknowledge the fo­ resulting from global sea-level changes. The compari­ llowing researchers for their contributions: L.Alcahi, M.T.Alberdi, son with currently accepted Cenozoic Global Cycle A.M.Alonso Zarza, M.A.Alvarez Sierra, B.Azanza, M.Belinch6n, Charts indicates that sedimentary disccontinuities oc­ J.Carballeira, G.Cuenca, J.Fermindez, M.Freudenthal, E.Garcfa, 1.Gi­ cur at about 24.5 Ma, 22 Ma, 16 Ma, 13.5 Ma, 9.5 Ma, bert. A.Gonzalez, F.Junco, J.I.Lacomba, F.L6pez Olmedo, A.V.Mazo, P.Mein, J.Montesinos, S.Moya, A.Olive, S.Ordoiiez, M.de Renzi, 5.5. Ma, and 3.3 Ma in both marine and continental J.Rodrfguez-Fernandez, A.Ruiz-Bustos, M.A.Sacristan, C.Sese, successions. The chronological coincidence is also re­ M.O.Soria, J., M.Valle, C.Viseras, and J.L.Zapata. We thank markable at a regional scale by comparing Spanish Ne­ Paula Bayard for the improvement of the engIish in the text, A.Garcfa ogene continental successions with those observed in Blanco for his help in drawing figures included in the paper, as well as offshore Mediterranean areas and inland peripheral zo­ V.Martfn for his assistance in typing the manuscript. One of the authors (Dr. Emilio Elizaga) died during the nes of the Iberian Peninsula. time in which this paper was written. All of us wish to devo­ The palaeoclimatic curves inferred from mammal te this work for his memory, permanently reminding him as assemblages throughout the Neogene display four rela- the best friend and scientific collaborator.

APPENDIX A LH - Las Higueruelas ESC - Escorihuela SQ - San Quirce LO - Loranca List offossil mammal sites F - Fuentes VIC - Viladecabals LU - Lupiana GL4 - La Gloria4 Ebro basin LY - Layna GL6 - La Gloria 6 AN - Arnedo MN - Moncalvillo Ll - Libros I Levante NAL - Naval6n AU - Autol LCI - Loma de Casares I - O'Oonnell BE - Bergasa 00 LP4 - Las Planas 4 B- Balneario BO - Borja PA - Pm-rales LPV - La Puebla de CM - Cuestas de Mahora PA3 - Paracuellos 3 BU - El Buste LR - La Roma ER - El Rinc6n PA5 - Paracuellos 5 CR - Carretil MA - Manchones FP - Fuente Podrida - Pineda CUR - Cura PI MAN - Los Mansuetos FV - Fuente del Viso - Retama F7 - Fraga 7 RE MB - Masfa del Barbo LPO - La Portera - Sayat6n FM - Fuenmayor SY MOL - Mas del Olmo MRI - Marmota I IL - Islallana TO - Torija NAV - Navarrete TL - Tolosa VC2 - Valverde de Calatrava 2 LA - Los Agudos NO - Nombrevilla VG3 - Valdeganga 3 VJ - Vallejo LC - La Ciesma P5 - Peralejos 5 VM - Venta del Moro MO - Moyuela ZZ - Zafra de Zancara PM - Puente Minero SC - Santa Cilia RAI - Ramblar I SJ - San Juan-La Galocha Duel'o basin SO - La Solera Beties TA - Tarazona TR - Torralba de Ribota ARZ - Ariza AC - Casa del Acero TC - Torrent de Cinca VA - Villalba Alta C - Cetina ALB - La Alberca TU - Tudela VAI - Valdemoros I CS - Carr.Soria ALQ - Alquerfa VH - Villanueva de Huerva VA3 - Valdemoros 3 DU - Dueiias AR - Arenas del Rey VR - Villarroya VAT - Valtorres EC - Escobosa de Calataiiazor BOC - Botardo YM - Yesos de Monteagudo VLL - Velilia LVF - Los Valles de Fuenti- CI-3 - Crevillente 1,2,3 dueiia VRC - Villarroya del Campo C4-5 - Crevillente 4,5 Tajo basin MV - Montejo de la Vega VT - Valalto C6 - Crevillente 6 ALG - AIgora SI - Simancas CCI - Caiiada del Castaiio ALM - Almendros TMI - Torremormoj6n I CJU - Canteras de Jun AO - Arroyo del Olivar TM4 - Torremormoj6n 4 Valles Penedes CLl - Cerro Limones ARB - Arbancones VI - Valladolid I CN - Cenajo BAT - Batallones CAL - Can Almirall CP - Cerro Parejo CIB - Canteras de Iberia CJ - Can Jofressa CU - Cuarterones Calatayud - Teruel CO - C6rcoles CL - Can Llobateras GO - GOl'afe CT - Cendejas de la Torre ARM7 - Armantes 7 CPO - Can Ponsic H3 - Huescar 3 ES - Escamilla AT3 - Ateca3 ELC - EIs Casots HI - Hfjal' HE2 - Henares 2 BR! - Brito LF - La Fortesa HU - Huelago HO - Huerta ObispaHa CA - Casas Altas MC - MoH Calopa LB - Librilla IS - CES - Concud Estaci6n PIR - Piera LJ - La Juliana LD - Ledanca DH - La Dehesa SM - San Mamet 02 - Orce 2

Rev. Soc. Geol. Espaiia, 6 (3-4), 1993 SPANISH CONTINENTAL NEOGENE 39

References Daams, R. and Freudenthal, M. (1990): The Ramblian and the Ara­ gonian: limits, subdivision, geographical and temporal extension. Aguirre, E., Dfaz-Molina, M. and Perez-Gonzalez, A. (1976): Datos In: European Neogene Mammal Chronology (E.H.Lindsay et a!. paleomastol6gicos y fases tect6nicas en el Ne6geno de la Meseta Eds), Plenum Press, New York, 51-59. sur espaiiola. Trabajos Neogeno-Cuaternario, 5: 7-29. Daams, R. and van der Meulen, A. (1984): Paleoenvironmental and Agustf, J., Cabrera, L. and Moya, S. (1985a): Sinopsis estratigrafiea paleoclimatic interpretation of micromammal faunal successions del Ne6geno de la fosa del Valles-Penedes. Faleontologfa i Evo­ in the Upper Oligocene and Miocene of North Central Spain. Pa­ luciD, 18: 57-81. teobiologie continentale, 14: 241-257. Agustf, J., Martfn Suarez, E. and Vera, J. A. (1988): Contribuci6n a Daams, R., Freudenthal, M. and Alvarez Sierra, M. A. (1987): Ram­ la sfntesis del Ne6geno continental de Espaiia e interpretaci6n blian; a new stage for continental deposits of early Miocene age. paleoclimatica. II Congr.GeoI.Espmia, Granada, Comunicacio­ Geol. Mijnbow, 65: 297-308. nes, 1: 241-244. Daams, R., Langereis,C. and van der Meulen, A. (in press): A rein­ Agustf, J., Moya-Sola, S., Gibert, J., Guillen, J. and Labrador, M. terpretation of the paleomagnetic dating of the Middle to Late (l985b): Nuevos datos sobre la bioestratigraffa del Ne6geno con­ Aragonian Calatayud Section (province of Zaragoza, Spain). tinental de Murcia. Paleont. Evol., 18: 83-94. Earth Planet. Se£. (in press). Alberdi, M. T., Hoyos, M., Junco, E, L6pez-Martfnez, N:, Morales, Demarcq, G., Gourinard, Y., Magne, J. and Wallez, M. J. (1990): J., Sese, C. and Soria, D. (1984): Biostratigraphy and sedimen­ Temperature des eaux marines du bassin rhodanien au Miocene tary evolution of continental Neogene in the Madrid area. Pateo­ inferieur et moyen: megafaunes et datations. Pateobiologie Con­ biologie Continentale, 14: 47-68. tinentale, 17: 205-214. Alvarez, M. A., Daams, R., Lacomba, J. 1., L6pez-Martfnez, N. and De Vieente, G., Calvo, J. P. and Alonso Zarza, A. M. (1990): Main Sacristan, M. A. (1987): Succession of micromammal faunas in sedimentary units and related strain fields of the Madrid Basin the Oligocene of Spain. Munchner Geowiss.Abh., A, 10: 43-48. (Central Spain) during the Neogene. IXth RCMNS Congress, Alvarez, M. A., Daams, R, Lacomba, J. 1., L6pez-Martfnez, N., Van Barcelona, Abstracts: 121-122. der Meulen, A., Sese, C. and Visser, J. de (1990): Paleontology Dfaz Molina, M., Arribas, J. and Bustillo, M. A. (1989): The T6rtola and biostratigraphy (micromammals) of the continental Oligoce­ and Villalba de la Sierra Fans: Late Oligocene - Early Miocene ne-Miocene deposits of the North-Central Ebro Basin (Huesca, Loranca Basin, Central Spain. 4th Intern. Conf.Fluvial Sedimen­ Spain). Scripta Geologica, 94: 1-77. tation, Barcelona-Sitges, Field-Trip 7: 74pp. Anad6n, P., Cabrera, L. and Roca, E. (l989a): Contexto estructural y Dijksman, A. A. (1977): Geomagnetic reversals as recorded in the paleogeografico de los sistemas cenozoicos de Espaiia. Acta Ge­ Miocene Red Beds of the Calatayud-Teruel Basin (Central 01. Hisptinica, 24: 167-184. Spain).Ph.D.Thesis, Univ.Utrecht, 156pp. Anad6n, P., Cabrera, L., Julia, R., Roca, E. and Rosell, L. (1989b): Elizaga, E. (1990): Antilisis de facies sedimentarias y petrologfa de Lacustrine oil-shale basins in Tertiary grabens from NE Spain los depositos lacustres de edad Neogeno superior,Zona Prebeti­ (Western European Rift System). Palaeogeogr., Palaeoclimat., ca, Albacete, Espmia. Tesis Doctoral, Univ.Complutense, Ma­ Palaeoecol., 70: 7-28. drid, 268pp. Bellon, H., Bizon, G., Calvo, J. P., Elizaga, E., Gaudant, J. and L6­ Elizaga, E. and Calvo, J. P. (1989): Evoluci6n sedimentarfa de las pez-Martfnez, N. (1981): Le volcan du Cerro del Monagrillo cuencas lacustres Ne6genas de la Zona PreMtica (Albacete, Es­ (province de Murcia): age radiometrique et correlations avec les paiia). Relaci6n, posici6n y efectos del vUlcanismo durante la sediments neogenes du bassin de Hellfn (Espagne). evoluci6n. Bol.Geol.Minero, 94: 837-846. C.R.Acad.Sci.Paris, 292: 1035-1038. Esteban, J. M. and Martfnez Salanova, J. (1987): Mimomys ischus Bruijn, H. de, Daams, R., Fahlbusch, V., Ginsburg, L., Daxner­ n.sp. y M.realensis n.sp., dos nuevos Arvic61idos (Rodentia, Hock, G., Mein, P. and Morales, J. (1992): Report of the Mammalia) del Plioceno de la Cuenca del Jucar (Albacete). Es­ RCMNS Working Group on Fossil Mammals (four appendices), tudios geol., 43: 299-308. Reisensburg 1990. Newsl. Stratigr, 26: 65-118. Gonzalez, A. (1989): Antilisis tectosedimentario del Terciario del bor~ Bruijn, H. de, Mein, P., Montenat, C. and van de Weerd, A. (1975): de SE de la Depresion del Ebro (sector bajoaragones) y de las cu­ Correlations entre les gisements de rongeurs et les formations mari­ betas ibericas marginales. Tesis Doctoral, Univ. Zaragoza, 507pp. nes du Miocene terminal d'Espagne meridionale (provinces d'Ali­ Gonzalez, A., Pardci, G., Villena, J. and Perez, A. (1988): El amllisis cante et de Murcia). Proc.Kon.Ned.Akad. Wetensc.,B, 78: 1-32. tectosedimentario como instrumento de correlaci6n entre cuen­ Calvo, J. P., Elizaga, E., L6pez-Martfnez, N., Robles, F. and Usera, J. cas. II Congr. Geol. Espmia, Granada, Simposios: 175-184. (1978): El Mioceno superior continental del Prebetico Externo: Haq, B. U., Hardenbol, 1. and Vail, P. R (1987): The new chronostra­ Evoluci6n del estrecho nord-betieo. BoI.Geol.Minero., 5: 9-32. tigraphie basis of Cenozoic and Mesozoie sea level cycles. Cush­ Calvo, J. P., Ord6iiez, S., Garcfa del Cura, M. A., Hoyos, M., Alonso man Found. for Foraminiferal Research, Spec.Pub!. 24, 4 figures. Zarza, A. M., Sanz, E. and Rodrfguez Aranda, J. P. (1989): Sedi­ Haq, B.U., Hardenbol, J. and Vail, P. R. (1988): Mesozoic and Ceno­ mentologfa de los complejos lacustres miocenos de la Cuenca de zoic Chronostratigraphy and Eustatic Cycles. In: Sea-level Chan­ Madrid. Acta Geol. Hisptinica, 24: 281-298. ges. An integrated approach. (C.K.Wilgus, Hastings,B.S., Ken­ Calvo, J. P., Ord6iiez, S., Hoyos, M. and Garcfa del Cura, M. A. dall,C.G.S.C., Posamentier,H., Ross,C.A. and Van Vagoner,J.C., (1984): Caracterizaci6n sedimentol6giea de la Unidad Interme­ Eds). Spec.Pub.Soc.Econ.Paleont.Miner., Tulsa, 42: 71-108. dia del Mioceno de la zona sur de Madrid. Rev. Mat. Proc. Geol., IGCP-219 Spanish Group, Tertiary Basins (1990): Tertiary lacustri­ 2: 145-176. ne systems in Spain. I: Tectonosedimentary and paleoclimatic Chamley, H., Meulenkamp, J. E., Zachariasse, W. J. and van de We­ constraints; Il: Megasequential arrangement and mineral resour­ erd, A. (1986): Middle to Late Miocene marine ecostratigraphy: ces. 13th Inter.Sedim.Congress, Nottingham, Abstracts: 236-237. clay minerals, planktonie foraminifera and stable isotopes from Keller, G. and Barron, J. A. (1983): Paleoceanographic implication Sicily. Oceanologica Acta, 9: 227-238. of Miocene deep-sea hiatuses. GeoI.Soc.Am.Bull., 940: 590-613. Corrochano, A. and Armenteros, 1. (1989): Los sistemas lacustres de Letouzey, J. (1986): Cenozoic paleo-stress pattern in the Alpine Fo­ la Cuenca Terciaria del Duero. Acta Geol.Hispanica, 24: 259-280. reland and structural interpretation in a platform basin. Tecto­ Daams, R. and Freudenthal, M. (1981): Aragonian: the Stage con­ nophysics, 132: 215-231. cept versus Neogene Mammal Zones. Scripta Geol., 62: 1-17. L6pez-Martfnez, N., Agustf, J., Cabrera, L., Calvo, J. P., Civis, J., Daams, R. and Freudenthal, M. (1988): Synopsis of the Dutch-Spanish Corrochano, A., Daams, R, Dfaz, M., Elizaga,. E., Hoyos, M., collaboration program in the Neogene of the Calatayud-Teruel Ba­ Martfnez, J., Morales, J., Portero, J.M., Robles, F., Santisteban, sin. 1976-1986. In: Biostratigraphy and paleoecology ofthe Neo­ C. and Torres, T. (1987): Approach to the Spanish continental gene micromammalian faunas from the Calatayud-Teruel Basin Neogene synthesis and paleoclimatic interpretation. Ann. Inst. (Spain).(M.Freudenthal, Ed.). Scripta Geol.,Spec.lss.l: 3-18. Geol. Publ. Hung., 70, 383-391.

Rev. Soc. Geol. Espaiia, 6 (3-4), 1993 40 J. P. CALVO Y OTROS

Lopez-Martfnez, N. and Torres, T. (1991): La microfauna de los Santanach, P. (1989): Reflexiones sobre los mecanismos de inciden­ sondeos de ENUSA en la Depresion Intermedia (provincias de cia de la Tectonica en la divission estratigrMica de rellenos de Cuenca y Guadalajara). Rev.Esp.Micropaleoll/olog{a, 24, 117­ cuenca. Implicaciones en la correlacion estratigrafica. 140. Rev.Soc.GeoI.Espwia, 2: 223-234. Megfas, A. G. (1982): Introduccion al amllisis tectosedimentario: Santisteban, C. (1981): Petrolog{a y sedimell/olog{a de los materia­ aplicacion al estudio dim'imico de cuencas. Quillto COllgr. Lati­ les del Mioceno superior de la Cuenca de ForlUna (Murcia) a la Iloamer/cano Geolog{a, Buenos Aires, Actas, I: 385-402. luz de la "Teorfa de la crisis de salinidad". Tesis Doctoral, Uni­ Megfas, A. G., Leret, G., Martfnez del Olmo, W. and SoleI', R. versidad de Barcelona, 725pp. (1983): La sedimentacion Neogena en las Betica: am\lisis tecto­ Sanz de Galdeano, C. (1990): Geologic evolution of the Betic Cordi­ sedimentario. Mediterrdnea, Ser.Geol., 1: 83-103. Ileras in the Western Mediterranean, Miocene to the present, Mein, P., Bizon, G., Bizon, J. J. and Montenat, C. (1973): Le gise­ Teclonophysiscs, 172: 107-119. ment de Mammiferes de la Alberca (Murcie, Espagne Meridio­ Sanz de Galdeano, C. and Vera, J. A. (1992): Stratigraphic record nale). Correlations avec les formations marines du Miocene ter­ and palaeogeographical context of the Neogene basin in the Be­ minal. C.R.Acad.Sci.Paris, seLD, 276: 3077-3080. tic Cordillera, Spain. Basin Research, 4: 21-36. Meulen, van del' A. 1. and Damns, R. (1992): Evolution of Early­ Scn, S. (1990): Hipparion Datum and its chronologic evidence in the Middle Miocene rodent communities in relation to long tcrm pa­ Mediterranean area. Ill: European Neollene Mammal Chronology leoenvironmental changes. Palaeolleollr. Palaeoclimat. Palaeoe­ (E.H.Lindsay et aI., Eds.), Plenum Press, New York, 495-505. col., 93, 227-253. Scse, C. (1991): Interpretacion paleoclimatica de las faunas de mi­ Mitchum, R. M., Vail, P. R. and Thompson, S. (1977): Scismic slra­ cromamffcros dcl Mioceno, Plioceno y Plcistoceno de la Cuenca tigraphy and global changes of sea level. Part 2: Thc depositional de Guadix-Baza (Granada, Espafia). £.I'tudios 111'01., 47: 73-83. sequence as a basic unit for stratigraphic analysis. In: Seismic Sese, C., Alonso-Zarza, A. M. and Calvo, J. P. (1990): Nuevas fau­ stratillraphy. Applications to hydrocarbon exploration. nas de micromamffcros del Terciario contincntal del NE de la (C.E.Payton, Ed.). AAPG Mcm.26: 53-62. Cucnca de Madrid (prov. dc Guadalajara, Espafia). Estudios ge­ Moisscnct, E., Lindsay, E., Mcin, P., Opdykc, N. and Percz-Gonza­ 01.,46: 433-45 I. lez, A. (1990): The Alfambrian: a new continental stage for thc SoleI', 1., Martfncz dcl Olmo, W. and Mcgfas, A. G. (1983): Rasgos Plioccne formations of Tcrucl Basin. Biostratigraphy, Magnetos­ basicos del Neogcno dcl Mcditcrraneo espafiol. Mediterrdllea, tratigraphy, referenced sections. IX RCMNS Conllress, Barcelo­ I: 71-82. lW, Abstracts: 245-247. Simon, J. L. (1984): Compresion y distension alpinas en la Cadena Muller, G. (1984): Climatic evolution during the Neogene and Qua­ Iberica Oriental. Inst.Estudios Turolcnses, CSIC, 268pp. tcrnary cvidcnccd by marinc microfossil assemblages. Paleobio­ Steininger, F. F., Bernor, R. L. and Fahlbusch, V. (1990): European IOllie ContinentalI', 14: 359-369. Neogene marine/contincntal chronologic correlation. In: Europe­ Mufioz, A. (1991): Alldlisis tectosedimenrario del Terciario del sec­ un Neogene Mamll1al Clmmolo!l.V (E.I-1.Lindsay el aI., Eds), Plc­ tor occidental de la Cuenca del Ebro (Conumidad de La Rioja). num Press, New York, 15-46. Tesis Doctoral. Univ. de Zaragoza, 496pp. Vail, P. R. and I-1anderbol, J. (1983): Sca-levcl changes during the Opdyke, N., Mein, P., Moissenet, E., Perez-Gonzalez, A., Lindsay, Tertiary. Oceanus, 22: 71-79. E. and Petko, M. (1990): The magnetic stratigraphy of thc Late Vail, P. R., Hardenbol, J. and Todd, R. G. (1984): Jurassic unconfor­ Miocene sediments of the Cabriel Basin, Spain. Ill: Europeall mities, chronostratigraphy, and sea-level changes from seismic Neollene Mammal ChrollolollY (E.H.Lindsay ct aI., Eds), Plenum stratigraphy and biostratigraphy. In: IntelTelliona! Unc0l1!orll1i­ Press, New York, 507-514. ties ami Hydrocarhon Accull1ulation (J.S.Schlec, Ed.), AAPG Pardo, G., Villena, J. and Gonzalez, A. (1989): Contribuci6n a los Mem.36: 129-137. conceptos y a la aplicacion del analisis tectosedimentario. Ruptu­ Vegas, R. and Banda, E. (1982): Tectonic framework and alpine ras y unidades tectosedimentarias como fundamcnto de corrcla­ evolution of thc Iberian Peninsula. Earth Evol.Sci., 4: 320-342. ciones estratigraficas. Rev. Soc. Geol. Esp£llia, 2: 199-221. Vegas, R., Vazquez, J. I., Surinach, E. and Marcos, A. (1990): Mo­ Pascual, A., Rodrfgucz, J., Sanz de Galdeano, C. and Vcra, J. A. del of distributed deformation, block rotations and crustal thicke­ (1991): Relacion entre tectonica y sedimentacion en las cuencas ning for the deformation of the Spanish Central System. Tecto­ neogenas de Granada, Alpujarras y Tabernas (Cordilleras Beti­ nophysics, 184: 367-378. cas). I Congr.Esp.Terciario, Vic, Barcelona, Libro Gula Excur­ Vera, J. A. (Ed.) (1989): Division de unidades estratigni!icas en 1'1 siones (F.Colombo, Ed.), 147pp. iIIuilisi.l' de cuencas. Rev.Soc.GeoI.Espafia, 2: 40 Ipp. Perez Garcfa, A. (1989): Estratillraj/a y sedimentololl(a del Tercia­ Warburton, J. and Alvarcz, C. (1989): A thrust tcctonic interprcta­ rio del borde meridional de la Depresion del Ebro (sector r/oja­ tion of the Guadarrama Mountains, Spanish Central System. In: no-aragol1l!s) Y cubetas de Muniesa y Montalbdn. Tesis Docto­ Libro Homenaje a Rafaef Soler, AGGEP, Madrid: 147-155. ral, Univ. Zaragoza, 525pp. WeeI'd, A. van de and Daams, R. (1978): Quantitative composition Perez-Gonzalez, A. (1979): EIlfmite Plioceno-Pleistoceno en la sub­ of rodent faunas in the spanish Neogene and paleoecological im­ meseta meridional en base a los datos geomorfol6gicos y estrati­ plications. Proc.Kon.Ned.Akad. Wet.,B, 81: 448-473. grMicos. Trabajos Neogeno-Cuatemario, 9: 23-26. Wilgus, C. K., Hastings, B. S., Kendall, C. G. S. G., Posamentier, Perez-Gonzalez, A. (1982): Ne6geno y Cuatemario de la Llanura H., Ross, C. A. and Van Wagoner, J. C. (Eds) (1988): Sea-level Manchega y sus relaciones con la cuenca del Tajo. Tesis docto­ changes -An integrated approach. SEPM Spec.Publ.42: 408pp. ral, Univ. Complutense, Madrid, 787 pp. Portero, J. M., Ortega, L. I. and Portero, G. (1991): Hoja y Memoria Geologica de Guadalajara (n° 21-21). Mapa GeoI.Nac.Espwia, 2a Recibido 1'1 9 de diciembree de 1992; aceptado elmanuscrito Serie, 1aEdic., ITGE, Madrid. revisado 1'12 dejunio de 1993

Rev. Soc. Geol. Espaiia, 6 (3-4), 1993