THE NEOGENE OF THE LOWER TAGUS BASIN (PORTUGAL)
Trabajo "resell/ado a las
XVIII l omadas de Paleomologra J
/I COllgreso Ibhico de PlIleQlIlo!og{a
UlliI'ers it!ad de Salamanca
Salamanca. 24-29 de Sep,iembre de 2002
l OGO PAIS
Centro de Estudos Geol6gicos. Departamento de Ciencias da Terra. Faculdade
de Ciencias e Tecnologia. Quinla da Torre. 2829-516 Caparica. Portugal.
http://www.dcl. fct. unl .pt/CEGnovo/CEG .html . Email: jjp @fcL unl .pl.
Pais. J . 2004. The Neoge ne of the Lower Tagus Basin (Portu gal ). lEI Neogeno de la C uenca del Bajo Tajo (Portugal ).] Rel'ista Espanola de Paleolllologfa. 19 (2), 229-242. ISSN 0213-6937.
ABSTRACT
The Tcniary Lower Tagus Basin (LTB ) occupi es a large area in Portuga l and constitu tes a sym metri c basin of
the ori e ntal hu ge Uppe r Tagus Basin. ce ntered at Madrid (Spa in).
The LTB was an c ildorre ic basin durin g th e Paleoge ne. Marine co nnecti on occ urred at lhe Lower Aquita ni an;
at the Lisbon - Setubal Pe nin sul a region th e sedimentation was in th e ocean/co ntin en t interface. with several
cha nges in the coast line. Apparentl y. th e first marin e tran sgression ca me from South . originating a gu lf with a
N-S coraJ reef that att ained the Li sbon area. Occidental communi ca ti on to the sea was established after the
Burdigalian.The sedime ntary and palaeonto logic record of the di sta l sec tor of th e LTB (Lisbon-Setubal Pe nin sula) is re lated to sea level c ha nges. It is poss ible to correlate levels with plancti c foram inifera and mamm a ls.
as well as to get isotopic ages (KlAr in glauconi tes; 87SrfK6Sr). Good bios trati graphi c data can be obt ai n fro m
contin e nt a l a nd coas tal depos its. The foss il richness - din oflage llates. spores. polle n, plant macrorrcmains.
foraminifera. ostracoda. molluscs. ec hinids. fi shes, rc ptilcs, mamilla Is - and 0 and C isotopes. co nstitut es a large
source of inform atio n for e nvironme ntal and palaeogeog raphical reconstillui ons. as we ll as fo r th e establishme nt of correl ati ons between mari nc a nd con tincn ta l deposits. The a nal ys is and the integration of a large a mount
o f litho logical a nd biostratigraphi cal data joined with iSOlopic ages (KlA r and 87SrfMSr). all ow the establishemenr
o f a chronostratigraphi c framewo rk for the distal part of th e Miocene of th e LTB and the de finiti on of 10
depositiona l seque nces. in part agreeing with the Haq' s 3rd order custati c cyclcs. C limatic evolUlion durin g th e
Mi ocene has been a lso characterized. At co ntin ental environm ents, the faunas and fl oras poi nt out to an altern ation of moist a nd dry e pisodes. th c dryest one at th c Langhi an.
For the in land. two secto rs can be characteri zed. Near the region direct ly affected by th e sea ( Ribatej o and
Alto A lentejo) deposits are relat ed with th e wa ndering of a Pre-Tag us in a large flu vial pla in . During the Lower
and Middle Mi oce ne detrita l sedimentati o n is we ll repre sent ed. Some marl s with oyste rs denounce hi gh eustati c
sea levels: brack ish watcrs attain reg ions 150 km far from the ex tant coast line. Some ve rteb rate fossils sites
allow the es tabl ishm elll of co rrelati o ns with th c Lisbon reg io n. na mely durin g the Mi dd le Mi ocene and Lower
Torto ni an. Sedime ntary co nditi ons changed at Lower Upper Mi oce ne. At th e right bank of th e Tagus. limes tones
acc umul ate in lac ustre and palu slre e nviron men ts: latteral y thi ck cla y deposits strecht out to th e left bank.
At th e proximal areas of th e LT B (Be ira Bai xa) the chro nostrati graphi cal co ntral e is poor. The OlitCropS are large ly
d iscont inuous. It on ly has been possible to de fin e a los trat ig raphic un its. bounded by regio na l un conformi ties.
resulting from tectonic cvents recognized at the Iberia scale. During Lower and Middle Mi ocene. a sandy bra ided
depositional sys te m was install ed . drainin g the flu via l plain o f the Pre-Tagu s from E to SW. Plant macro-remains indicate a wanner and moister c limate than today. HispoIIOlhel"iu111 111arritel1sis (steppe rhin oceros) is known
fro m East o f Caste lo Branco (Pl asenc ia. Spain); it is c harac teristi c o f M 5 zo ne (Astarac ian) and is also know n
from Lisbon's Langhi an. Younge r deposits (Upper TOrl oni an and Messinian) co rrespond to a llu vial fan sediment s
occ ur near tec toni c slopes . at th c base o f risin g mountain s ( Portu gucse cent ral c hai n): the thi c kn e ss a nd
gra nul ometry qui c kl y decrease dow nstream.
Pl iocene flu vial deposits ove rl ay through an erosion surface the marine TOrl onian (Setubal Peninsul a) and the
conti ne nt a l limes tones and c lay s of the Va llesian of Ribatejo (i nl and ). During the Zanclean th e co ntinental sedi me ntati on ca rried on onl y at the proximal part of th c basin ( Be ira Ba ixa) wi th the depositio n of endorrei c alluv ia l fan
conglomerates. Away o f the mOllntain feede r re lieves. the sedimentation show a dec rease of thi ckne ss: alte rn ating
cong lo mcra tes a nd sand y lu tit es were deposited. A tem perat e med ite rra nean cli mate with co ntrasting seasons
prevai lled. In th e Piacenz ian, allu vial fa ns and braided flu vial syste ms were installed drain ing to the Atl anti c, precedin g the actu a l hydrograp hi cal net. Feldspatic sa nds were deposited in the Se tubal Pe nin sula ; the coas t line was to
th e west of the actu a l. A lransgrcssion took placc ovcr the Occidental littoral, affecting the Lower Tag us (Setuba l
230
JOAO PAIS
Pe ninsula) a nd th e Mondego Basin s. Whithish co ng lomerates with quartzi te and quartz ro unded clasts overl ay (he
Piazencian sands oflhe Senlbal Peninsul a. They yie lded Pre-Ache ulian art ifacts allow ing co rrelali on with the Pl ioPle istoce ne bou nd ary. Basin inland cong lo merates with iro n cru sts point out to cold and dry environment s.
Key wo rds: Lower Tag us Basin, Neoge ne, Portugal, Palaeogeography, Biostr atigrap hy, Palaeoclimatology.
RESUMEN
La C ue nca del Baja Tajo (LTB ) acupa una alllp li a extensi6n e n Portu gal. y consti tuye un a c uenca simel ri ca de
la amplia Cuenca del Tajo espanola.
LTB fu e una cuenca de canicter endorreico durante el Pal e6geno. Estuvo conectada con el mar durante el
Aquitaniense inferio r; e n la region de la Pe ninsula de Lisboa-Setubal , la sedi mentac ion IU vo caracter mi xto marinol
co ntin e ntal. con varios cambi os e n la Ifnea de cos ta. A parente ll1ente, la prill1era lran sgresi6n marin a procedi 6
de l S ur, ori gi nand o un golfo co n un arrecife de coral e longado en direcci6 n N-S que alcanz6 la zo na de Lisboa.
La co muni caci6 n marina par e l borde occiden tal se es tablec i6 despues de l Burdiga lie nse. EI registro sedi me ntari o
y paleon to l6g ico del sec tor di sta l de LTB (Peninsul a de Lisboa-Setubal) se ha relacio nado co n cambios del nivel
del ma r. Es posible la co rre lac i6n e ntre nive les can foraminfferos planct6nicos y co n mamlferos, y edades
isotopicas ( KIA I' e n g lauco ni tas . 87Sr/86Sr). Se puede n ob te ne r bue nos datos bi oes trali graficos a partir de
sedime ntos cont inenta les y costeros. La riqlleza en fosiles - dinonage lados. po len, esporas. macrorestos vegera les,
fo raminfferos, ostracodos, mo luscos, equfnidos, peces. reptil e s, ma mffe ros e isoto pos e stables de C y 0 constir-u ye una gran flle nte de informac ion para reco nstruccio nes ambi e nta les y paleogeografi cas, aSI como para
la correlac i6n en tre dep6sitos marinos y co ntinte nt a les. EI ana l isis y la integracion de un a gran cantidad de da tos
iito l6gicos y bioestrmigraficos, unidos a las datac iones isotopicas (KlAr, 87SrfK6Sr), ha pe nnitid o e l establecimiento
de la cronoestrati graffa para la pane di sta l de l Mi oceno de LTB , y la de finicion de 10 secllencias deposicionales,
en parte correlac ionadas con los ciclos eustaticos de tercer orden de Haq. Se ha caracteri zado tamb ien la evoluc ion
c1 imat ica durante el Mi oceno. En ambie ntes co ntinentales, las fa unas y noras sugieren un a altern anc ia de episodios
humedos y secos, produciendose e l mas seco durant e e l Langhi ense.
En direcc io n al contin e nte, se pueden caracteri zar dos sectores. Cerca de la region di recl.amente afecLada por e l
mar (Ribatejo y Alto Ale ntejo). los sedime lllos e stan re lacionados co n la mi grac ion de l pre-Tajo e n una ampl ia lI anura al uvia l. Du ran te e l Mi oceno inferior y medio , la sedime nt ac i6n detrft ica esta bien represen tada. La presencia
de algu nas margas con ostreidos se re lac ionan con period os de alto ni ve l de lmar: depositos deaguas salobres alcanzan
regione s situ adas a l SO km de la actua l !fnea de costa. Alg un os yaci mi e mos de ve rte brados f6 siles permiten e l
esta blec imi ento de correlaciones co n la regi6n de Li sbon. sobre todo durante e l Mioceno medio y el Tortoniense
inferior. Las condi c iones sed ime lllarias cambiaron e n e l Tonon ie nse inferio r. En la marge n de recha del Tajo se
acumularon cali zas lacu stres y palustres; potentes dep6sitos arci ll osos latera les seex ti ende n hasta la marge n izquierda.
En las zonas prox imales de LTB (Bei ra Baixa), e l co ntrol c ronoeslratigrafico es pobre. Los allo rami entos
son mu y di scontinuos. Un ica me nte ha side posible de finir unidades aloestrati graJi cas. lill1iwdas por di scont inuidades regionales. ariginadas por event os tec t6ni cos reconocidos a escala de toda Ibe ria. Dumnte el Mioceno
inferior y medio se instal 6 un sistema de posicio na l Lre nzado de carac ter are noso, qu e dre no la llanura a lu vial
de l pre-Tajo de sde e l NE hacia el SO. Los macro rrestos vegela les indican un cJi ma Illas calido y hum edo que el
actua l. HispanolheriullI I1IGrrilensis (rin oceronte de la estepa ) procedente del este de Castelo Branco (Pl asenc ia.
Espail a): es caracterfsti co de 1£1 zona MN5 (Astaraciense), y tam bien se cnc ucJ1lra en e l La ngilicnse de Lisboa.
Dep6sitos mas rec ientes (Torto ni ense superior y Messinie nse) co rrespond ie ntes a aban icos al uviales asociados
a pendi e nt es tect6 nicas, se enc ue ntran e n la base de c le vac iones 1ll0ntanosas (Cade na Ce ntral po rtu gllcsa); e l
espesor y e l tamano de gra no di sminu yen rap idamente hac ia sus tramos d istales.
Los sed imentos Ou viales de l Pli oceno se situan de un modo di sconfo rme ta nt o sobre los del Tort oninese
mar ino (pe nIn sul a de Setu ba l) como sobre las ca li zas y arc illas cOlllinental es de l Va llesiense de Ri batejo (hac ia
e l co ntin e nt e). delimitandose e ntre ambos un a superfi c ie de erosion. Durante e l Za nc lie nse, la sed ime nt acion
contine nta l tu vo luga r so lo e n la zo na prox imal de la cuenca (Be ira Baixa ), con sedimentac io n de aban icos
a luvia le s co nglol1lenlticos de CaraC le r e nd orre ico. Di sta lmen te a los re lieves 11l0nt a nosos que propo rc ionan
material es. e l espesor de los sed ime nt os di sl1linu ye, a lLema ndo cong lo merad os y luti tas are nosas. EI cli ma ru e
de tipo med ite rran eo te mp lado co n alta es tacio nalid ad. En el Pi acenc ie nse, los aba nicos a lu via les y los siste mas
Illiviaies trenzados se instalaron drena ndo hac ia el oceano Atla nt ico, precedie nd o la actua l red hidrogrMica. Se
depositaron are nas ri cas e n fe ldespatos en la penInsul a de Setubal. y la linea de costa se SilUO mas al oeste qu e
la actu a l. Una tran sgresi6 n lU VO lugar sobre todo e l li tera l occ ide nta l. afecta nd o a las cue ncas del Bajo Tajo
(pe nfnsula de Setl,bal ) y del Mondego. Conglomerados blancuzcos ca n c lastos redondeados de c liarc it u y de
cuarZo se sob re im pone n a las a re nas de l Pi acencie nse de la penin sula de Setl, bal. Co nli enen arte fact os pre-
T H E NEOGENE OF THE LOWER TAGUS BASIN (PORTUGAL)
231
Achelenses que sugieren una correlaci6n con el Ifmite Plio-Pl eistoceno. La presencia hacia el centro de cuenca
de conglomerados con cortezas ferru ginosas sugieren ambientes Frias y secas.
Palabras clave: Cuenca del Bajo Tajo,
e6geno, Portugal, Paleogeografia, Biostratigrafia, Paleoclimatologfa.
INTROD UCTION
In I beria, several grabens we re opened duri ng th e
Paleogene, some of which evolved to large sedimentary
basins along th e Cenozoic.
After the Maastrichtian the sedimentati on took place
only in the Mo ndego Tertiary basin, no rth of the Nazare
fau lt (a NE-S W reacti vated hercyni an faull) a fossiliferous
level with mammals of Upper Paleocene to Lower Eocene
age occurs in Silveirinha (Ant un es and Russe ll. 1981:
Ant un es el al .. 1997). Paleocene and Lower Eocene seem
not to be represented in other region s.
The L ower Tagll s Basin (LTB ) occupies a large area in
Portugal, from the lilloral region of Lisbon-Seulbal Penin sula, to beyond spanish border near Castelo Branco (Beira
Baixa). T he LTB is a sy mmetrical. western counlerpart of
_
the oriental large U pper Tagu s Basi n, centered at Madrid
C.ambrl.an
JuraSilc
Proterozoic . Cam~n
Tnallic
Granlt"
_
C.rbonlleroos /"'" F.ult
Granodlorit"
_
De'lonl.n
(Spai n). Three di stinct sectors can be recog ni zed:
_
G.abros
- Soud westhern distal sector, in th e Li sbon and Setlibal
Peninsula. in close rela ti onship wi th the ocean;
_
Ophiolite.
- centra l secto r in Ribatejo e Alto Ale ntejo. with con-
/
Overthrust
- - - Probable leull
•
Cu.tem.ry
_
CretJiceous
SHurl.an
_
Ordovlcl.n
Tertiary
Figure I. Lower Tagus Basin.
tinental facies and some bracki sh episodes corre sponding
to the higher eustatic sea level s:
- Northem proximal sector in Beira Baixa. crossi ng the
Portugal-Spain border. with cOnlinental facies only (Fig I).
Li sbon and Setuba l Pe ninsula are located at the distal
part of the Basin . Miocene sedimentation corresponds to
lime and space shifting interfaces between marine and COI1-
tinental domai ns. Miocene beds were well exposed. It is not
surpri sing that geo logic observation has been carried on
since lo ng ago (A lmeida, 1762). An impo rt ant period of
Aust ri a we re based on molluscs. partly described by G.B.
Sowerby (ill Smith. 1847). There were nearl y no more British contributions ever since. They were succeded by papers
by Portuguese and other, mostly French researchers.
An increase in resea rch on Miocene bed s was accom-
plished by the 2nd Commissiio Geologica ( 1857-1868), by
Carlos Ri beiro (field wo rk) and F. Pereira da Costa (molluscs). The strat igrap hi c framewo rk was basically that of
Sharpe, whose Almada beds appeared und er " Mi ocene
research concerns early 19th century and Jose Bonifacio de
Andrada e Si lva. then in charge of Minin g and M eta llurgy.
Among hi s ac ti vili es there is th e reopening of go ld mining
at Adic;a , a former medi eva l exploitation. A n account of thi s,
moyen et superi eur/ lll.- Formation marine avec fo ssiles
analogues ceux du bassi n mediterran een et des enviro ns
inc ludin g the first descriptio n of secti o ns where Miocene
beds outcrop, was presented (S il va, 1817).
Go ld exp loitati o n at Adi~a went o n under Wilhelm-
marine Miocene by J.e. Berke ley COller. who was in charge
of the Tertiary at the Geologic Survey (COller, 1904 ill Doll l'us
el al., 1903- 1904; COller, 1956). His c1assitication of the Lisbon Miocene units is sti ll in use (l ithostratigraphic units designed " Di visions" from I to VII with some sub-lInits). Stratigraphic work was accompan ied by high-standard palaeontologic research by swiss (Oswald Heer) and mostl y by french
authors (P. de Loriol, Gusta ve Dollrlls, Frederic Roman).
There were also contributio ns by P. Choffat (C hoffat,
1950, posthumous paper; I :20000 geologic map of Lisbon). Hi s chapter abollt mar ine Mi ocene (ibid .) is large ly
Lud wig, baron von Eschwege. H is geologic, mining and
palaeontologic observa ti ons were publi shed (Esc hwege,
183 1; w ith ex tra plates about marine mi ocene vertebra te
fossils added by Alexandre Vandelli ). For the first time, a
genera li zed section between Sintra and Arrabida and con-
cernin g part of the Basi n was prod uced (Op. c il.).
The nex t step in the stud y of the Lower Tagus Basin 's
Neoge ne is du e to Da nie l Sharpe ( 1834, 184 1) who described units as the Almada beds that correspond 10 the
mostly marine Miocene in fi llin gs. Early corre latio n attempts with Miocene units in France, Switzerland , Ital y and
a
de Vie nne en Autri che" (Ribe iro. 1878).
An hallmark in portuguese stratigraphy is the sketch on the
an abridged ve rsion of Cotter 's.
Geo rges Zbyszewsk i res to red the s tudi es on th e
po rtu guese Tertiary s ince 1937. Among many o ther con-
232
JOAO PAIS
lower T.gus Basin Miocene
Facies correlation
~
Chamoca
ACe
~
Ma., tectonIC evenl 8t AmIIbtda chan
(angular uncontorrMy)
-
-
1-
-
Lignites
••• • Conglomerates
""'"
1
-~
'"•
~
~
S
u
:/
5 .Ec0
."'"
~
Paleoenvironments
: : :: Booclasts
• ___ . Mudstoroes
Sands and Sandstones
~
• .!!•
8•
c•
•• ~
~
.•
g
"
~
-
Uthology
::::: Marls
FIf'St arod last occurrence
~
"
-
<
j
-~-~~ ....
""'"
51' isoIopIc age and etror
AC'
(borehole) (borehole )
j
•
"""-
Ma mm a l,
-
Mammal.
..- .-
"" ....
"...
,,..~--.,-
M(IIWte 6UbtJclal
Mafine infrslittoral
Figure 2. Chro nostratigraphical framewo rk fo r the Mi ocene of the di stal seclor of the Lo wer Taglls Basin (A ntunes er a/. , 2000).
THE NEOGENE OF H I E LOWER TAGUS BAS IN (PORTUGA L)
tributio ns, there are some broad scope o nes (Z byszews ki ,
I 954a, 1957, 1962, 1963, 1964 a, I 964b, 1967).
The development of studi es on sedimentation led to new
concepts. Rythm ic sedimentation, erosion and sedimentation
cycles. sequences and corresponding types became in fashion. This had consequences for the Lower Tagus ba<;in. A high
resolution stratigraphic strategy was deviced (M .T. Antunes),
compri sing: (a) detai led studies on important secti on s
233
in the ocean/continent interface, with se vera l changes in
the coast line. Apparently, th e fi rst marine tran sgre ss ion
came from SOllth, ori ginati ng a gulf with a N-S cora l barri er reef that attain ed the Lisbon area. Wes th ern communi cati on to th e sea was establi shed after th e Burdi galian.
The sedi mentary and palaeoI1lologic record of the di stal
part of the LTB (Lisbon- Setubal Peninsula ) is re lated to
biochronologic research. mostly on mammals and planktic
sea level changes. Good biostrati graphic data can be obta ined from continental and coas tal deposits. It is possible to correlate levels with planktic foramin ifera and mammals, as we ll as to obta in iso topi C age s ( K / Ar in
I"o rmllinil"era, K-Ar and (later) Sr isotope ages. sedimcntology,
g lau conites; " Sr/" Sr ). The foss il ri c hness - d ino fl a-
palaeoecology, magnetostra ti graphy, etc. rendering possible
gellates, spores, pollen, plant m3crorremains. foraminifera,
os tracoda, molluscs, echinids, fi shes, reptiles, mammals
(Antunes and Torquato, 1969- 1970. and laller contributions);
(b) the improvement of data ti o n and other data by means of
the develop ment 01" regio nal synthesis and broad-scale correlations (Antunes el al., 1973. 1987, 1996a, I996b; Antunes
and Pais, 1992; 1993: a series of Notes about the Geology
and Palaeo ntology of the Miocene of Lisbon, Antunes el al. ,
since 1960). Azevedo ( 1983) stud ied mai nl y the Pliocene
deposits of Setubal Peninsula.
Fewer studies had been prod uced about the inland part of
the Lower Tagus Basin. Ribei ro ( 1880) described the strati gra ph y of thec011linental Tertiary of the Ribatejo. Roman and
Torres ( 1907) presented the first paleontologic data and a
s tratig rap hi c synthesis. Later wo rks were produced by
Zbyszewsk i ( 1941 , 1943. 1946, 1947, 1953. 1954b, I964a,
1964b. 1965, I967b, 1967c, 1968). Antu nes, alone or wi th
others, pursued studi es on the stratigraph y and the palaeontology of the Ribatejo area (Albcrdi el al., 1978; Antunes, 1984;
AntunesandMein. 1977. 1979:Antunes,mdMazo, 1983 ; Antunes el al.. 1983, 1987. 1992: Antunes and Zbyszewski, 1973).
Palaeobotanical studies were fi rst publi shed by Heel' ( 188 1)
and later pursued by Teixeira ( 1942a, 1942b, 1944a, I944b,
1944c, 1944- 1947, 1946, 1947a. 1947b, 1949, 1952a, 1952b,
1954. 1973, 1973-74. 1979): Pais followed these works ( 1972,
1973. 1978. 1979. 1981. 1986, 1987, 1989. 1991. 1999: Pais
el al.. 1999). Dini z ( 1967. 1984) and Diniz and Sivak ( 1979)
characteri zed the palynology of the Ri o Maior diatomites and
lig nites. Sed ime nto log ica l studies have been produced by
Carvalho ( 1968). Cun ha ( 1992. I992 b) characterized alostrati graphi c unities and latter descri bed the Cenozoic oi" the LTB
proxi mal area (Beira Baixa) (C unha. 1996): Barbosa ( 1995)
recognised the alostrati graph y and the litostratigraphy of the
Ribatejoc011linental deposits. More recen tl y. Cunha (2000) descri bed the alterat ion and cementation processes of the Teni -
ary deposits of Central POJ1ugal including those of the LTB .
- and 0 and C iso topes, cons titu tes a large and broad
scope source of in formation for enviro nmental and palaeogeogri1phical recon sti tuti on s, as well as for correlations
betwecn marine and continental dcposits.
The analysis and the integ rati on o f large amount of li th olog ical and biostrati g raph ical da ta such as the first and
last occurrence of most significati ve taxa of foraminifera,
os tracoda and mammals, togeth er with isotopic ages ( K/ Ar
and 87Sr/86Sr) allow th e es tabli shcment of an acc urate
chronos trati graphic frame for the distal part of th e Miocene
of the LTB and the definition o f 10 depositional sequences
that. at least in part, seem to correspo nd to Haq 's 3rd o rder
eustatic cycles. For more detai lled data see Antunes el QI.
( 1996b, 1999,2000) and Legoinha (200 I). A ge neral strat ig raphi c fram e for the Mi ocene is presented (Fig. 2. Fi g. 3).
Climatic evoluti on during th e Miocene has also been
charact.cri zed. Tropical conditions prevailed in the sea. In the
Upper Burdigalian and Langhi an the temperature attained a
maxi mum, being similar to thm of today's Guinea gulf. T he
temperature decreased later, its values bei ng similar to those
of ex tant M orrocco sea waters. The continental faunas and
noras point out to altern ati on of moist and dry episodes, the
dryest one at the L.1nghi an (Antunes and Pais, 1984; LauriatRage el aI. , 1993: Pais 1999) (Fig. 4).
In th e Pliocene, a genera l regression occurred. Flu vial
depos its overla y through an erosion surface th e marine
To rt on ian in the Se tuba l Penin s ula . The rIu via l Sa nt a
Marttl Sands arri ved to Setuba l peninsul a. A short tran sgression took pl ace over th e wes thern littoral in the Lower
Tag us (Setuba l Pe nin s ul a ) and the Mondego Bas in s.
Brac kish waters entered the Setuba l Peninsula (Azevedo,
1 98 3)~
DISTAL SECTOR OF THE LOWER
TAGUS BASlN (LISBON A D SETUBAL
PE INS ULA REGIONS)
clays wi th gypsum , plant m<1croremains, oys ters,
and Dreissel/Q (ide ntilied by P. Callapez, Coimbra Univ. ,)
occur. Whiti sh conglo merates (Be lverde Conglo merate)
with rounded quartzi te and quart z clast and some wi nd-
blown clasts overl ay the Piazencian sands of the Setuba l
Pe nin sul a. These conglo merates yielded Pre-Ache ulian
artifac ts th at point out to an age close by the Pli o-
The LTB was an e ndorreic basin du rin g the Pa leoge ne.
Mari ne conect ion occurrcd at th e Lower Aq uitanian; at th e
Li sbon - Setubal Peninsula region the sedimen tation was
Ple istocene boundary.
The corre lati on of these units with th ose of the LTB
inland areas is presented (Fi gA).
FONTE DA TEL .....
fo,z fONU - " BEIIto\ DAiS LAGES
COIII'II)IOS
{Aell
CHAI'INECJ.
(AtI)
sw
_ _ _ _ _ _ _ 10 Km
AUlADA
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10 Km
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.....
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010 (Ii.SMa)
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Mammal , Jles (Anlunes el 0/1996)
6· C:heIas 2
7 · CheIu 1 (0\. cia F....",..... Ot cIIol Ram.-.gul.
Ct>amece do lumoar (0\. cia SiI¥6ria.. 0\. Grande 0IIvaI cia SusaN ..
6 . 0...111 do Poml>eifo
5 · CriMO Aei
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A.. l/...q.;aI. ~v C-al0IieI
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1 . Al Motorway· KIn 10
,
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7777 Marts
TIdal Hats
Dellal'Estua.y chamels and bass
Sands and Sandstones
0 3 {20M' J ~.
:::::::: Conglomerates
Maline subtidal
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_
Marine infralittDfal
Figure 3. Correlatio n chart between sections and bo reho les from Foz da FontelRibeira das Lages (Setubal Penin sula) and the Lisbon regio n (A ntu nes et al., 2000).
o>,
o
)i
in
THE N EOGENE OF THE LOWER TAG US BASIN (PORTUGA L)
CENTRAL SECTOR OF THE LOWER
TAGUS BASIN
(RIBATEJO AND ALTO ALENTEJO)
Two main sectors can be characterized inl and of the
LTB. To the NE of the the distal region (Ri batejo and Alto
Alentejo) deposits are related with the wanderi ng of a PreTagus in a large fl uvia l plai n (inte rmediate region). The
prox imal area of the basin is situ ated at Bei ra Baixa, cross-
ing the Portugal - Spain border. Coarse prox imal continental deposits occu r.
Paleoge ne de posits (G res de Mon sa nto ) (Barbosa,
1995) are the basemen t of the Neogene. They outcrop in
the borders of the basin and comprise coarse sandstones
and some conglomerates in metri c positi ve sequences.
Caleretes and lac ustre limestones (Quinta da Marquesa,
Alcanede Li mestones) occur at the top. Pa ligo rskite and
smectite predominate in the clay frac tions.
Duri ng the Lower and Mi dd le Miocene fl uvial sedimentatio n is well represented (Ota Formatio n) overlayi ng
the "Gres de Monsanto" through a regional uncon formity.
Some clays with oyste rs sugges t high eustatic sea levels;
brackish waters reach ing reg ions 150 km far fro m the extant coast line. Some vertebrate foss il sites w ith mammals
allow the esta bli shment of correlations with the Lisbon
region, namely during the M iddl e Miocene and Lower
Torto ni an. The main fossil localiti es are: Vi la Nova da
Rainha (MN5) (A lberdi el aI., 1978); P6voa de Santarem
(MN6) (So u li e- Marsh, 1978; Pa is, 1978; Antunes a nd
Mei n 1977 ; Truc, 1977; Gaudant, 1977); Casais da Formiga (MN7) (Alberdi el aI. , 1978); Archino (MN9) (Alberdi
el al., 1978); Azam bujeira inferior (MN9) (Antu nes el aI. ,
1983). At the top, faunas with H ippariol1 allow correlation with the zone MN9 (Lower Vallesian) (A ntunes, 1979;
Antun es and Gi ns burg, 1983; A ntu nes el aI., 1993 ).
Kao lin ite and illi te predomi nate in the clay minerals.
Sed imentary condi tio ns changed during earl y Up per
Miocene. At the right bank of the Tag us, lac ustrine and
pal ustrine limesto nes occur (Almoste r-Santarem Limestones); latte raly thick c lay deposits (To mar clays) strecht
out to the left bank also. Al moste r-San tarem Limesto nes
are gray to wh iti sh in colour; breccia structures are frequent; sand y and luti tic fac ies may occur. Smecti te and
illite predom inate in the clay fraction. Tomar clays are
rep resent ed by orange or red lutites w ith ill ite an d
kao linite. Both constitute the A lmoster Aloformatio n.
Duri ng Pliocene, fl uvial arkosic sands (Ul me Fomnation)
related with Ole wandering of the Pre-Tagus were deposited
mai nl y at the left bank or the ri ver. They overlay the Vallesian
conti nental limesto nes (Almoster-Santarem limestones) and
c lays (Tomar c lays) of Ri batejo and Alto Ale ntejo. T he
arkosic sands present some yellow to redish colour and a
medium to coarse granulo metry with low kao lini te and ill ite
contents. The sands can be followed to the Setubal Penin-
235
sula where they correspond to the Santa Mruta sands (Barbosa
and Pena dos Reis, 1989, 1996; Bru'bosa, 1995). Some plant
macroremai n localities are known.
Loca ll y, conglomerates occur (Ri o de Moin hos Conglomerates, Mart ins el al., 1998) over the Almoster A Ioformati on. Two sequences can be recogn ised. T he fi rst one
overlay the Monsanto Formatio n (Pa leogene) or the Paleozoic. The MPS changes from 80-90 cm to 35-40 c m. The
upper levels are lutitic. T he second conglomeratic sequence
is mai nl y quartzi tic. The MPS is aro und 50-40 cm. A 10m
luti tic deposits complete the sequence (Barra el aI., 2000).
To the NE of the intermediate area of the LTB , coarse
cong lomera tes (Cong lomerates of Serra de Al meiri m)
were deposited. The MPS changes fro m 45 c m in proximal areas to 10c m in the more distal ones (A lme irim).
Channel slruCLU res are frequent. Kao lini te prevails over
ill ite (Barbosa, 1995 ; Barra el aI., 2000).
The Vil a de Rei Conglomerates (Upper Pliocene to
Ple istocene), overlay by unconformity the Serra de AIm ei rim Co ngl o mera tes. T he cl asts are q uartz it i c,
heterometric, and poorl y ro unded. The matrix is sandylutitic orange to red in colour, pre senting iro n cementa-
tio n that suggests co ld and dry environme nts. They have
a fa n-li ke s truc tu re deve lop ped near th e Ord o vic ia n
quartzitic crests at the No rth border of the Lower Tagus
Basin (Barra el al. , 2000). Correlatio ns with distal and
prox imal regio ns are presented ( Fig. 5) .
THE NORTHERN PROXIMAL SECTOR
OF THE LOWER TAGUS BASIN
(BEIRA BAIXA)
The chro nostrati graphi cal contro le is poor in the LTB
prox imal areas (Beira Baixa). The outcrops are largely
discontinuous. It has been poss ible to define alostratig raphi c units bounded by regio na l unconformit ies (U BS)
related w ith tec toni c events recognized at iberian sca le
(Cunha, 1992a, I 992b, 1996, 2000).
ConglomeratiC and sandy arkosic deposits (Cabe~o do
Tn fa nte Formati on) (C un ha, I 992a, 1996) have been correlated with the Paleogene Benfica Format ion in the distal
and Monsanto Sandstones of the intermediate LTB areas.
During Lower and Middle Mi ocene, a sandy braided
depositional system was installed, draining the fl uvial plain
of the Pre-Tag us from NE to SW till the Ri batejo. Orange
sands and green luti tes with scarce fossils we re deposited
(Sil veirinha dos Figos Formati on) (Cun ha, 1992a ; 1996).
T hese de pos its over lay throug h an unco nfo rm ity th e
Ca be~o do ln ra nte Formati on or, by a n angular unco nform ity, the Paleozoic of the Hes peric massif. Large channe ls wi th one hundred meters are typical (C unha, 2000).
Pla nt macro-rema ins col leted at Ponte de Sor sugges t a
wann er and moister than today climate (Pais, 1973, 198 1,
JOAO PA IS
236
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Figure 4. Paicoc nvironmelllal conditions al the di stal region of the Lower Tngus Basin during the Miocene (Pai s. 1999).
1986). Si lic ifi ed wood belo nging
10
a Iropical arborea l
angiosperm indica tes a warmer than tod ay, and wet climate
(Pai s. 1973, 1983; Teixe ira and Pai s, 1976). To Ihe Easl of
C astelo Branco. at Plasencia (Caceres, Spain), conglomerates and orange to red clay s y ielded HispOIlOfheriu l1I
lIIal rilell sis (Hern andez- Pac heco and Crusafo nl, 1960), a
sleppe rhinoceros known al so al Lisbo n in Ihe L I deposilional seque nce (Div. Vb) (A nlunes, 1979; AnlUnes el al. ,
1999) and al Qu inlanelas and aI Amor (Leiria, Mondego
Basin) (An lUnes and Ginsbu rg 1983 ; Anlunes and Mei n,
198 1), M N5 mamma l zo ne (Middl e Arago ni an). These
arcosic deposils probab ly are corre lal ive of Ihe ala Formalio n of Ihe Ribalejo area (Ca rval ho, 1968; Antunes ill
Ribeiro el al., 1979; C unh a, 1992a ; Barbosa, 1995) .
Above the Sil veirinha dos Figos Formation, allu vi al fan
sediments occur near tectonic slopes, at the piedmont of the
rising mountains of the Portuguese central chain (Murracha
Group, Upper Miocene
10
Pliocene); Ihe Ihickness and
granu lometry quickly decrease downstream.The Murracha
Group corresponds to two positives megasequcnces fol lowed
by a negati ve one, bounded by sedi mentary unconformities
(alostratigraphic un ils UBS II. UBS 12 and UBS 13; Cunh a.
1992b, 1996, 2000). From Ihe botlom 10 Ihe lOp, il includes
the Torre, M onfOitinho and Falagueira Fonnations.
T orre Form ati on presents conglomerates at th e base
and grayish green to yell owish mi caceolls silndy- Iuti tes to
the top, locall y cemented
by sili ca and green to redish in
colour. The Formali o n di sa ppears progress ively 10 SE;
T HE NEOGENE OF T HE LOWER TAG US BASIN (PORTUGAL)
Smectite with some ill ite predomina te. Torre Form a ti on
correspo nd s to the UBS II and was interpreted as a n a llu via l e ndorrei c system (C unha , 1996, 2000).
During the Zanc lea n th e co ntin en ta l sedimen tation is
we ll docu me nted at th e prox im a l pan o f the bas in (B ei ra
Ba ixa) with th e depo siti on o f endorre ic a llu via l fan cong lome ra tes ( M o nfo ninh o Fo rm a ti on) . Away fro m the
mou ntains, there is a decrease o f thi c kn ess: conglo mera tes and sand y lutites a lternate. A tem pe ra te medite rranea n
c limate with co ntrastin g seasons prevailed . Mo nfor tinho
Formation is represe nted by red a llu vial fan depos its w ith
conglo merates an d sandy- Iutites fac ies. lilite and kao linite
predominate. It co rresponds to the UB S 12 (C un ha, 2000).
Falag ue ira Fo rma ti o n ( Pi azencia n) is re presented by
oc re to red ish or w hiti sh coarse de pos it s with a sa ndy to
si lt y mat ri x. It consti tut es a negative seque nce re fl ec ting
the progradati on of coa lesce nt a ll uvia l a nd braided sandy
fl uvia l syste ms dra ining to the Atl a nti c and precedin g the
exta nt hyd rograph ica l ne t (C unha el al., 1993). Kao li n ite
a nd so me illite are re presellled in the c lay frac ti o n. The
Falag ue ira Fo rm a ti on co rres pond to th e UBS 13 (C unha.
1996,2000) a nd ca n be co rre la ted w ith the Serra de A lme irim Co ng lo mera tes (Barbosa and Pe na do s Re is . 1989).
Correlati o ns with di sta l and intermedia te regions are
prese nted in fi g ure 5.
PALAEOGEOGRAPHIC EVOLUTION
First pa leogeog raph ic reco nstitutio ns fo r th e LTB d ista l
area was presellle d by Anlll nes (ill Ri beiro el al., 1979).
New data, includ ing those fro m the Be lverde Borehole (pais
el al., 2002; Legoinha el al., 2002) a nd the c ha racterization of alostrati graphi c un its in the in te rmed iat e and proxima l areas, allow the e stab lishe me nt of new paleogeographi c
sc he mati c maps for th e evolution of th e LTB (Fig 7).
During the first Miocene tra nsgressio n eve nt the sea attai ned the in ner pa l1 of the Settibal Penin sul a; a gulf. reaching Lisbon area. was deve loped. Seismi c profiles and the data
conce rnin g th e Be lve rde Borehole, suggests that the sea e ntran ce was made from the south. A N-S coral reef barrier
developed sho l1l y afterward s. The westwru'ds opening of the
Tag lls gul f only happe ned in Lower Burdiga lian (begining
of the B I depositio nal seque nce). A marine N-S bank, correspo nding to the exta nt coastal area. protected the inner re g ion of the Setubal Penin su la: the subsidence allowed th e
de position of ci rca 1000 m of Neogene sedi ments, although
in th e N-S sea ba nk , onl y around 200 111 arc known.
During hig h sea leve l eve nt s ( Burdi ga li a n and Se rraval lian ), brac kish waters ex te nded ti ll 150 km inla nd 10
th e inte rmed ia te regio n. Arrabida beca me an is la nd during the Burdiga lia n a nd the Serrava lli an tra nsgressions: the
sa me occ ured w ith S in tra igneolls mass if (W of Lisbon )
du rin g th e Serravallia n ( Figs. 7B. 7C).
In land. the Tag ll s wan dered through a large a llu vial
237
plain during Lower and Middle Miocene (Fig. 6, A, B a nd
C ). At th e Lower Tortoni an (C), a large marsh area developed in th e Ri batejo. Lac ustrin e and pa lustrine limestone s (A lmoster-Sa nta re m Limes tones) as we ll as ma rls
and clays (To mar C lays) were th e resulting ma in de posits.
Durin g th e Pli oce ne, a ge ne ra l regress ion occll red.
Fl uv ia l sa nd s a rri ved to th e Se tub a l Pe nin s ul a (U lme
sand s) . In the more proxima l areas coarse conglo me ra tes
prograded to SW (Serra de A lmeirim and Fa lag ue ira Co ng lomerates) (Fi g. 6D).
AKNOWLEDGEMENTS
M.T Antunes. P. Legoi nha and P. Cu nha helped in the rev ision o f the tex t and are gratefu ll y ac kn owledged.
Projec ts aprave d by the " FlInda ~ao para a C icllcia e a
Tecnologia" and by 'he paCT] cofund ed by the EC FEDER
Prog ram: " POCTII3234S /CTAl2000 - Recognit ion o f the
Miocene of the distal region of the Lower Tagus Basin through
a borehole wit h conti nuous sa mpl ing and " POCT I/CTAJ38659/
200 I - Th e Tertiary of centra l-northern Port ugal basin analysis,
straligraphy a nd reso urces"
REFERENCES
Albe rdi. M.T. , A ntunes. M.T.. Sondaar. P. Y. et Zbyszews ki,
G. 1978. Les Hippariol/ du Portugal. Ciel1cias da Terra
(UNL), 4. 129- 156.
Almeida, T. 1762. Recreasao Filozojica. 0/./ Dialogo Sabre
a Fifozojia Natural para instrusao de pesoas cllriozas,
que lIao f requent6rao as aulas. TOil/a VI e II/limo. Trow
dos Ceos e do MIIlldo. Na Ofic ina de Mi gue l Rod ri gues.
Li sboa, Tarde XXXV, 400-4 18.
Antunes, M. T.
J
979. " H ispalIoth eriul1I fa una" in l" berian
Middle Mi oce ne, its import ance a nd paleogeographical
mean ing. AI/Hales. Geologie des Pays Heltelliques. 1. hors
ser. I. 19-26.
Al1lunes. M.T. 1984. Essa i de sy nthese sur les mammi feres du
Mi ocene du Port ugal. Vol. d'hol1lmage CUl gio/aglle C. ZJ)Js;.elVski. Ed. Recherche sur les Civilisat ions. Paris. 30 1-323.
Alllll ncs, M.T., Casa novas, M .L. , C uesta, M.A .. Checa, L. .
Sanlafe, J. V. and Ag ustf, J. 1997. Eocene Mammals fro m
Iberian Pe nin sula. I II: ACles du s Conge Bi oc hro M '97
(Edit. J.P. Ag uilar. S. Lege ndre a nd J. Mi chaux). M el1loires
clu TravClllx E. P H. E. , IlIsrillll de MOlllepel/ier. 21. 337 -352.
A ntunes . M.T.. Calvo, J .P., Hoyos. M .. Morales. J.. Ordonez.
S .. Pais. J. y Sese, C. 1987. Ensayo de correlaci6 n en tre
e l Ne6geno de las areas de Mad ri d y Li sboa (C ue ncas
Al ta y Baj a de l rio Tajo). C0l11IlnicCl90es dos Servi90s
Ceol6gicos de Portuga l, 73, 85-102.
Antunes. M.T.. Civis. 1.. Gon za lez-Delgado, J .A .. Legoinha.
P. Nasci men to, A. and Pais, J . I996a. Mi ocene stab le isotopes (0 180. OUC) bioslratigraphy an d e nvironme nt s in the
southe rn limb of th e Alb ufeira sy ncline (Setubal Pen insula, Port uga l). Ceogaceta, 21. 21 -24.
Lithostratigraphy
(SW)
Chronostratigraphy
Distal region
OS oJ,OiVn
Antunes
Cotter,
1956
et aI.,2tXIJ
Intermediate region
I
Belverde Fm.
1-- - - -
Almeirim Fm.
Pliocene
1_ _ _ _ -
Beira Baixa
~
Ulme Fm.
~
..
c:JLTI
- - - - - - - - -- - - - CongoRio de Moinhos
Torre Fm.
SDT2
V Ub Areias de Cabo Ruivo
SOT1
Vila Areias de
SOS2
Vic
Calcflrios de Ma rvila
Vlb
Via
Vc
Gres dos Grilos
Langhian
Casais da Formiga (M N7)
P 6voa de Santa rem (MN6)
Arg ilas azuis de Xabregas
Calcarios da Q uinta das Con chas
SOB2
Va2 Areias com Pfacuna miocenicB
Va1 Calcarios do Casa l Vistoso
SOB1
IVb
a
D
Sands and sandstones
1'" 1
D
Vallesian
~
is
»,
o
----- ----
Ota Formation
Orleanian
III I I
SLD 9
Agenian
- - - - - - - -f - - - - - - - - - - - - - - - Monsan to Formation
Benfica Formation
Conglomerates
Turolian
Astaracian
W, I~~~~~s ~!~iS do Areeiro
SOBO
Areias da Esle fania
II
SOAl
~D~ ~ Camadas co~enus ribeiroi _ . _
Eocene
Ruscinian
SLD10
1! SilveirinhaFm.dos Fi gos
Vila N. da Ra inha (MN5?)
Areias da Quinta do 8acalhau
1I]f~,.
Villanian
Archino , Azambujeira int. (MN9)
Vb Areias do Vale de Chelas
Va3 Ca lcarios da Musaueira
Oligocene
D
SLD11
,,- I Fms. (tl MN10)
de Prata
SOL1
Burdigalian
Aquitanian
Bar~
unities
-- -- --
- - - - - - - c : f- - - - - - - - - - - - -- - - - - - - - - - Iii"l
Almoster I Tomar .
SOS1
Miocene
SLD1 2
~..
1.. .1
Faunal
".,
r - - - - - - - .--- - - - - - - - - - Monfortinho Fm.
Messinian
Serravallian
SLD13
-=m
c::::J
IV
W
00
SLD14
Taberna Seca Congo
Falagueira Fm.
Zanclean
Tortonian
A lostrati g raphic
unities
(UBS)
(Cunha, 1992)
r - - - - - - - ' -- - - - - - - - - - - -
I
Santa Marta F m.
I
Piazencian
Proximal region
Ribatejo
Lisboa I Almada
Gelasian
(NE)
~
Arkosic sandstontes
Figure 5. Lithostratigraph ic co rrelati on of the Lower Tag us Basi n units.
•
Lutites
Cabeyo do Infante
Fm.
SLD 8
-=m
III
Limestones
'if
Inland mammal localities
~
in
T HE NEOGENE O F THE LOWER TAGUS BAS IN (PORTUGAL)
239
RioMaiof
.
Akk~doSaI
Dcorals
~ Lacustrine and palustrine limestones
o
t- _.j
Gd
~ Continental conglomerates
Marine lutites
Continental days
Continental sands and sandstones
Figure 6. Paleogeog raphic maps co nce rning the Aquita ni an (A). Uppe r Burdigalian (B). Serrava ll ian
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10
Lower TOrlonian (C) and
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JOAo PAtS
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Mallll scrito recibido: 20 de febrero. 2003
Mallll serito aeeptado: 2 de sepliembre. 2004