Bio and magnetostratigraphy oftwo Lower Miocene sections, Tagus basin ()

S. SEN * M. T. ANTUNES ** J. PAIS ** P. LEGOINHA**

.. - Laboratoire de Paleontologie des Vertcbres, Univ. Pierre et Marie Curie. 4. PI. Jussieu, F-75252 Paris cedex 05. France .... - Centro de Estratigrafia e Paleobiologia da U.N.L., Faculdade de Ciencias e'Tecnologia, Quinta da Torre, P-2825 Monte de , Portugal

pp. 173-184 Ciencias da Terra (UNL) Lisboa NQ 11 1992 7 fig.

de Foz da Fonte et chez 74 en provenance de la coupe de Trafaria. La succession des zones de polarite magnetique RESUMO reconnues a ete correlee avec la "Geomagnetic polarity time scale" (GPTS) en tenant compte des donnees Palavras-chave: Miocenico inferior-magnetostratigrafia biostratigraphiques fournies par I'etude des forarniniferes -Foraminiferos-Lisboa-Bacia do Tejo- Portugal. planctoniques. Les zones de foraminiferes planctoniques etcelles de Apresentam-se os resultados do estudo da polarite magnetiquereconnues dans les coupesenquestion magnetostratigrafiadedois cortes no Miocenico inferiorda peuvent etre correlees d'une facon satisfaisante avec la bacia do Tejo. Foi utilizada a desmagnetizacao termica partie de la GTPS [tabelle calibree par BERGGREN et al. para isolar a componente primaria de magnetizacao de 45 (1985)] correspondant aux anomalies 6 et 5E (Foz da amostras recolhidas no corte de Foz da Fonte e 74 no de Fonte)et 5D (Trafaria).Cescorrelations suggerentdesages Trafaria. A sucessao de zonas de polaridade magnetica entre 19,35 et 18,14 Mapourlacoupe de FozdaFonteetde reconhecidas foi correlacionada com a "geomagnetic po­ 17,90 a 16,98 Ma pour celle de Trafaria. larity time scale"(GPTS) com base em dados biostratigraficos fornecidos pelos foraminiferos planct6nicos. ABSTRACT As zonas de foraminiferos planct6nicos e as de polaridade rnagnetica reconhecidas nestes cortes podem Key-words: Lower Miocene - Magnetostratigraphy­ ser correlacionadas adequadamente com a parte da GPTS Foraminifera - Lisboa - Tagus Basin - Portugal. [tabela calibrada por BERGGREN et al, (1985)] correspondente as anomalias 6 e 5E (Foz da Fonte) e 5D The magnetostratigraphy of two sections in early (Trafaria). Estas correlacoes sugerem idades entre 19,35 a Miocene marine deposits of the Tagus Basin is studied. 18,14 MaparaocortedeFozdaFonteede 17,9a 16,98Ma Thermal demagnetization was used to isolate the primary para 0 de Trafaria. component of magnetization for 45 samples from the Foz da Fonte section, and for 74 others from Trafaria section. Thesuccession ofthe polarity zones found in thesesections RESUME is tentativelycorrelated with the geomagneticpolaritytime scale (GPTS) on the basis of the biostratigraphic data Mots-cles: Miocene inferieur-Magnetostratigraphie­ yielded by planktic Foraminifera. The planktic zones and Foraminiferes- Lisboa - Bassin du Tage - Portugal. magnetic polarities recognized in these sections can be adequately correlated with the part of the GPTS [table On presente les res ul tats de I'etude calibrated by BERGpRENet al. (1985)] corresponding to magnetostratigraphique de deux coupes concernant Ie the Anomalies 6 and 5E (Foz da Fonte) and 5D (Trafaria). Miocene inferieur du bassin du Tage. La desaimantation This correlations suggests ages between 19,35 and 18,14 thermiqueaeteemployeepourisolerla composanteprimaire Ma for Foz da Fonte section, and 17,90 to 16,98 Ma for d'aimantation chez 45 echantillons preleves dans la coupe Trafaria.

175

INTRODUCTION Characterizationoflithostratigraphic units was firstly attempted by SHARPE (1842) who included The Lower Tagus basin near is well Miocene beds in a single unitthathe named" known for its Miocene infilling, which comprises a beds". A detailed study was conducted muchlaterby broad variety of lithotypes corresponding to six J. C. Berkeley Cotter, which was best presented as a major transgressive events alternating with regres­ stratigraphic introduction to the study by Dollfus on sions. Except for the upper Tortonian and the miocene mollusks (DOLLFUS, COTTER & Messinian (which are not so well characterized), GOMES, 1903-1904).The units defined by Cotter stages from the Aquitanian to the Tortonian are ("divisions", as he called them) are still in use, represented by lithostratigraphical units that yielded although a thorough revision is needed. much palaeontological and sedimentological infor­ Despite some contributions by P. Choffat, re­ mation in addition to other data. searchnearly stopped until 1937withG.Zbyszewski, Furthermore, it must be stressed that the geo­ New investigationwas carriedon and promoted graphic position is specially interesting as this basin by M.T.Antunes since 1959, either directly or in offers an unique occasion to establish correlations collaboration with other researchers. betweenthe remaining Atlantic basins from western Europe (Aquitaine in France) and the Mediterranean basins, as well as between the North Atlantic conti­ PALAEOMAGNETIC STUDY nental margins (Europe plus western Africa-North and central America). Sampling Much work has been done in the Tagus basin since the first known geological observations ofT. During a field trip in April 1989, sections were D'ALMEIDA (1762). The first sections at Fonte da sampled for magnetostratigraphical study. The re­ Telha were described by the remarkable mineralo­ sults concerning two sections, Foz da Fonte and gist (and later politician, one of those who master­ Trafaria, are presented. For the situation of these minded Brazil's Independence), Jose Bonifacio de sections and their geologic and palaeogeographic ANDRADA E SILYA (1817), then occupied in the context see figure 1. reactivationofMediaevaland Arab times gold mines Oriented blocks, with azimuth and dip meas­ in these region. ured, were collected at 15 horizons in the Foz da Early palaeontologie and geologic work was Fonte section (thickness 29.7m) and 22 horizons in doneby Daniel SHARPE(1834, 1842), WILHELM­ Trafaria (thickness 21.5 m). The continuity of the LUDWIG,BaronYONESCHWEGEand Alexandre outcrops allows good stratigraphic control and the YANDELLI (both 1831). determination of vertical distances between sites Later on, excellent palaeontologie research on with an accuracy of10 em. In theTrafariasection,the mollusks was carried on by F. Pereira da COSTA sediments are quite homogeneous, consistingofsilts (1866-1867) during the period ofthe (2d) Comissao and silty clays. The Foz da Fonte section presents a Geologica. more diversified lithology includingclays, sandstones Field work was carried out, mostly by Carlos and limestones. Ribeiro, who presented a paper on the Tertiary for­ Blocks were drilled in the laboratory in orderto mations ofPortugal to the International Geological obtain 22 mm long cylindrical samplesofa standard Congress, in Paris (1878). volume. Compressed air was used to cool the corer

177 cases, the more coherent values are taken as declina­ is quite variable; this is probably a consequence of tions and inclinations, and the polarity was deduced the more diversified lithology found in this section. from the magnetic behaviour of samples during the In the two sites, the intensity of magnetization de­ successive steps ofdemagnetization. At least three creases sharply (morethan 50%)belowthe tempera­ samples from each site were demagnetized to deter­ ture of 150°C; it is then gradually cleaned up to a mine its polarity with accuracy. temperature of500°C, showing almost stable direc­ The magnetic behaviour, during demagnetiza­ tions. In the othersites, the cleaningofthe remanence tion, ofthe sediments from the Foz da Fonte section is more regularup to temperature of380°Cor450°C.

MMAX = .315 mAim MMAX ~ .257 mAim MMAX ~ .251 mAim 1.0 1.0 ------1.0 ------foz,1-2 foz, 5-3 foz.14-1B

0.5 0.5 ---- 0.5

o. 0 l---~_~_~_~_~ 0.0 '--~-~-~---~~ o 100 200 300 400 500 600 o 100 200 300 400 500 o 100 200 300 400 500 500 Step Step Step

MMAX = .153 mAim MMAX = .159 mAim 1.0 1.0 tr.6-4A ~ tr. 19-4 :::E ------<, :>:

0.5 ------0.5

tr.2-1A o. 0 l--~_~_~ ~~ o. 0 l--~_~_~ ~~ 0.0 '---~-~_~_~_~ o 100 200 300 400 500 600 o 100 200 300 400 500 600 o 100 200 300 400 500 Step Step Step

Fig. 3 - Decay curves of the intensity of magnetization during the thermal demagnetization for six samples from the Foz da Fonte and Trafaria sections.

As in the Trafaria samples, the remagnetization, along with an increaseofthe magnetic susceptibility, is observed in seven sites up to 380°C and in six others up to 450°C. Therefore, the directions of the primary component are presumably determined af­ ter the cleaning ofthe viscous component and/or the secondary component and priorto the occurrence of ----+'------11----'~~ the intensity increase (Fig.4). HI-3

StrllUgrllph:lcCoord:lnlltes StrllUgrllph1c CoorlUnlltes Sc"l,,· .02 mAl.. Polarities ..N N Declinations and inclinations of the presumed primary component of magnetization are shown in figures 5 and 6 for each sample. Altough we observe some clustering of the declinations around O°C or 180°C, the inclinations are not always as would be expected for the latitude of this region. A large TR4-2 number of samples having southerly declinations ------f---=-~ u:, Strllt1grllphlcCoordlnates Sc"l -.05mA/.. show positive or very low negative inclinations. However, for both declinations and inclinations, we Fig. 4 - Zijdcrveld diagrams for four samples from the can observe some pattern in their gathering in the Foz da Fonte and Trafaria sections.

179 specific parts ofthe sections. In all cases, the polarity of each sample during demagnetization. Moreover, of each site is inferred not only from the average in both sections, each polarity zone includes several directions of the presumable primary component, successive horizons because ofthe regularsampling but, more importantly, from the magnetic behaviour and the small distances between the horizons.

I ....'" ...,co co Q) ",..,cr"""c c ..., ::J 0 N .... c co », +J'" -..-1 co C coL: Q) 0 0 a. c ...;'" ...., ...; .Y 0 .Y co L: C Q) o "~ ru ..., '"0 L: ::: ...; ",.., -' >- -' c,

m z" 35 DECLINATION INCLINATION IVb *15 • • •• :l • • •• ••• • • * • • ••• * • • •• •

ID Z * •• • • IVa

* •• •• • * •• • •• * •• • • • • III * •• • •

II

* • •• •• • • • • • •• • • • • •• Cretaceous - 90 180 0 90 -90 0 90 FOZ DA FONTE

Fig. 5 - Declination and inclination of the caracteristic magnetization component in the Foz da Fonte section. The left part of the figure concerns stratigraphic data from this section.

From these results, the following sequence of sented by two horizons in the silty clays. At these polarities has been observed in the Foz da Fonte sites, the weak magnetization of sediments and the section (from the bottom to the top): one normal presence of a hard secondary component did not horizon, four reversed horizons, four more normal allow a primary direction to be clearly determined. horizons and six more reversed horizons. Thebound­ Therefore, more samples (five from each horizon) ary betweenthe first reversed and the second normal were examined. In most of the samples, the behav­ zones is approximate because of a gap in the sam­ iour of the remanent magnetization during the suc­ pling (about 8 m) between the sites FF5 and FF6. cessive steps of heating leave no doubt about the This part of the section is mainly composed of reverse polarity of these two horizons. In the other unconsolidated sands. horizons,the directionsofthe characteristicremanent In the Trafaria section, three polarity zones are magnetization are reasonably well grouped and al­ apparent: a normal zone 5 meters thick between two lowthedeterminationofnormal and reversepolarity reversed zones. The first reversed zone is repre- zones.

180 (J) Q) c a N .>, en c a a .-\ ..., a .Y (J) ....,s: C Q) --I ....;"-1"'..., ...J a.. U1

m 25 DECLINATION INCLINATION

"2 IVb :1 * * " * Z * * * ...... * * * IVa * ? * * *

lC Z ;1 *1

TRAFARIA 90 180 o 90 -90 o 90

Fig. 6 - Declination and inclination ofthe characteristic magnetization component in the Trafaria section. The left part of the figure concerns stratigraphic data from this section.

BIOSTRATIGRAPHY dissimilis zone with Blow's N5 and N6 zones, No Catapsydrax dissimilis forms have been Both Foz da Fonte and Trafaria sections, al­ found at Foz da Fonte. This makes it difficult to ready sampled for magnetostratigraphy, were also correlate the upperpartofthe sectionto any biozones. studied undera biostratigraphic viewpoint, specially Thelastoccurrenceofthis species is an usefuldatum as far as planktic Foraminifera are concerned. to characterize the passage from Globigerinoides altiaperturus - Catapsydrax dissimilis subzone to Globigerinoides trilobus zone (IACCARINO, 1985), Foz da Fonte section which corresponds to Blow's N7 zone. Otherwise Praeorbulina glomerosa s. 1. seems A sample collected 205m from the bottom of entirely absent. This excludes ascribing the Foz da this section yielded the first Globigerinoides Fonte Foraminiferaassociations to the Praeorbulina altiaperturus. The first appearence ofthis species is glomerosa s. 1. zone (IACCARINO, 1985), which a datum that has been used as marker for the lower may be correlated to Blow's N8 zone. boundary of Globigerinoides altiaperturus ­ Summingup, Foz da Fonte sectioncorresponds Catapsydrax dissimilis subzone from the essentially to BLOW'S N5-N7 zones, evenifits upper Globoquadrinadehiscens dehiscens-s--Catapsydrax levels may be correlated to the lower part ofBlow's dissimilis zone (IACCARINO, 1985). The same N7 zone. datum is also employedto recognizethe Aquitanian­ Burdigalian boundary (BIZON & BIZON, 1972; DEMARCQ et al., 1974; BIZON, 1984; Trafaria section IACCARINO & SALV ATORINI, 1982; IACCARINO,1985). All the samples studied are enriched in IACCARINO (1985) correlates the Globigerinoides trilobus and Globigerinoides Globigerinoides altiaperturus - Catapsydrax immaturus. Other species - Globigerinoides

181 obliquus, Globigerinoides altiaperturus and from Artenay,France; that may be ascribedto Mein's Globorotalia obesa are common. All samples yield mammal Neogene unitMN4a, which corresponds to someforms ascribedto Globigerinoidesbisphericus. the N6 and the main part of N7 Blow's zones This association allow a rathersatisfactory cor­ (STEININGER et al. 1990),UpperBurdigalian(part) relationofTrafariasectionto Globigerinoides trilobus or to the late Orleanian Faunal unit (also in part), or zone (lACCARINO 1985) or to its equivalent N7 to the early Aragonian continental stage. zone from BLOW (1969). Calcareous nannoplankton from Palenca sec­ tion (about 6 kilometers East from Trafaria's) al­ lowedFONSECA(1977) to ascribethe higherlevels CORRELATION from IVa division - corresponding to those of Trafaria section - to MARTINI's NN4 zone. Ac­ Based primarilyon plankticForaminifera,some cording to BERGGREN et al. (1985), this zone biostratigraphic zones have been identified for both begins at the lowerpart ofN7 and ends in the midlle the Foz da Fonte and the Trafaria sections. part ofN8 zone (Blow); however, the viewpoints of According to these data, the first section in­ STEININGER et al. (1990) are notidentical as to its cludes the planktic zones1ying betweenthetop ofN5 upper boundary, which they regard as ending just and, may be, the base ofN7. In the Trafaria section, after the beginning ofN8. N7 zone is well characterized for almost all the Another upper boundary for IV-a unit is given section. Thecentral columnoffigure 7 comparesthe by the mammalian fauna from overlying IV-b unit ranges of the early Miocene planktic zones as pro­ (Lisboa, Cristo-Rei), characterized by the first ap­ posed by BERGGREN et al. (1985) and by pearanceofmastodonts and the lastofanthracotherids STEININGER et al. (1990), along with their corre­ (Brachyodus); this fauna is quite close in age to that lations to the geomagneticpolari ty time scale(GPTS)

, ~j ~ , cr·~ ID c: C -:;;~ ro~~'" "'.~ ID c-, 2 .~ c: '" .~ ~ -:;;~ .::: ~ tn c-, ~ ",.c ~ a. ID ~u ~ c-, c ~.~ c-, .x ~ ~ c ro ~ ID ro "'.c '"ID ~'" o .~ '" ~ a. .3 s ~ .§ ~ GPTS ro 0 .3 f= ~ 0- ~ .~ '"ID ro '" ~ :5 ;5 ~ ~ '" ~ N9 N9

N8 N8

_ *15 :1 11 N7 N7 * IVb * N6 - N6 IVa -

* N5 * N5 IVa * III *

II a b TRAFARIA

FOZ DA FONTE

Fig. 7 - Stratigraphic and magnetostratigraphic data from the Foz da Fonte and Trafaria sections, and the calibration ofthe planktic Foraminifera chronology as proposed by BERGGREN et al., 1985 (a) and STEININGER et al., 1990 (b). Note the age difference for the N5-N6 boundary.

182 afterBERGGRENet al. (1985). We mustemphasize bottom ofthe section, the N5 zone is represented and, that the majordifference between these two calibra­ otherwise, the N7 zone should be represented from tions concerns the age ofthe N5 - N6 boundary: 19 the middle of the section but this seems not to be Ma according to the first authors, but 18 Ma accord­ supported by the Foraminifera data. ing to BERGGRENet al. (1985). In this lastcalibra­ In the Trafaria section, the palaeontological tion, the span of the zone N6 is very brief, e.g. less data allows to correlate the palaeomagnetic anoma­ than 0.5 Ma. lies with the reverse and uppernormal periods ofthe The range of the planktic zones after Anomaly 5D and to the lower reverse anomaly of BERGGREN et al. (1985) implies that the Foz da C5C. The correlation is betterusing BERGGRENet Fonte section should include the polarity chrons al. (1985) scale. This correlation implies ages be­ from the top of the Anomaly 6 to the top of the tween 17,90 and 16,98 Ma for the Trafaria section. Anomaly 5D. The four polarity zones found in this Taking into accountthis lastcorrelation, a sedi­ section are less than the number that would be mentation rate of2.1 cm/Ka can be estimated for the required by this. Several hypothesis would explain two complete polarity zones of the Foz da Fonte this discrepancy: 1) insufficient sampling to record section. If we estimate the sedimentation rate by all polarity zones concerned by the interval ofdepo­ dividing the total thickness of the Foz da Fonte sition; 2) occurrence ofsome unconformities and/or section (29.7m) by the suggested interval of time very low sedimentation rate; 3) the top ofN6 and the (19,35-18,14 Ma), this rate will be 2.7cm/ka. In any N7 zones are not represented. In spite of these case, these are quite reasonable amounts oftenfound difficulties, the only possibility of correlation with in such marine deposits (SEN, 1988). the BERGGREN et al. (1985) calibration would be thatthe complete normal zone found in Fozda Fonte section corresponds to the Anomaly 5E. This corre­ ACKNOWLEDGEMENTS lation implies ages between 19.35 and 18.14 Ma for the Foz da Fonte section. The present work has been supported by CNRS In the STEININGER et al. (1990) correlation (France) and INIC (Portugal) grants. S.Sen is grateful to his colleagues from the Laboratoire de Paleornagnetisme table, the planktic zone N6 is very short and it is de l'IPG (Paris) for discussions and comments. Ms.V.Lee approximately time equivalent to the Anomaly 5D Hagee kindly helped to improve the English. F. Sierro, (fig.?). The polarity zones of the Foz da Fonte from Salamanca University, kindly gave some informa­ section fit worth with this calibration, since in the tions about Foraminifera from the Trafaria section.

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