TheN eogene ofA lgarv e (Portu gal)

(

Ciencias da Terra (UNL) Lisboa N.o ₁₄ pp.277·2 88

₂₀₀₀

J

7 Figs.

The Neogene of Algarv e (Portugal)

J.

Pals"-'',

P.

Legoinh a'':",

H.

Elde rfi eld(b,3),

L.

8 0 U53(8,4)

&

M. Estevensv-"

Work supported by the Praxis XXI Proj ect "Necgenicc e Quatem aric da margem aua nuce da Iberia e trans fonn ao;&s g lobais" (FCT, MeT),

a - Centro de Estudos Geol6gicos, Faculdade de Cienciase Tccnologia. Quinta da Torre, P·2825·114 Caparica, Portugal.

b -Depa rtment ofEarth Sciences, University of Cambridge, Downing Street, Cambridge CB2 3EQ, UK.

t ,jjp@fct.unl.pt; 2 . pal@fct.unl.pt;3 · helOl@csc,cam.ac.uk; 4 . 1S@fct.urd,pt; S- eslevens@telcpac_pl

A BST RACT

K ey-w ord s: Neogene; Stratigra phy ; Algarve; Portugal.

A synthesis abou r rhe Neogene and Quaternary of Algarve (Southern Portugal) is presented. New isot op ic~ 7S r j86S r ages as well as biostratigraphic data about the Miocene deposits allow to present a new stratigraph ic frame for the previously characterized units. The Lagos- Pcrtimao Formation correspo nds to depo sits of "t emperate carbonate pla tform " sedimentological type, d evelope d dur-ing a long time span (Lower Burdigalian to Upper Serravallian). A major change in sed imentation conditions (carbonate to silic iclas tic environments) occurred in the Lower Tortonian with the depos ition of yellowish sands.

Spongoliths rich in microfoss ils are rep resentedin Algarve inland. Th eir age is not well estab lished ; calcareous nannofo ssils indicate the CN5a l one (Upper Serravall ian) whi le foraminifera point out at least Nl6zone (Lo wer Tortonian).

In the UpperTortonian, the sedimentation is widespread in Easte rn Algarve, related with the Guada lqui vir Basin infill. The deposits begin wi th detrital limestones, locall y very rich in Heterostegina ,passing to fossiliferous co nglomerates and siltston es (Cacela Fonnation).

Coarse-gra ined conglomerates at Galvana (Faro) pose some age pr oblems. K/Ar age on glauconite indicates 6. 72±O. 17 Ma. However, glauconites may be reworked from older deposits (Cac elaForm ation ). The Galvana Con glomerate could be re lated to Pliocen e deposits arc not well characterized . Olhos de Ague sands, with a thi n marin e intercalation rich in marine vertebrates (fishes, a crocodile, cetaceans, sircnians), may be Upper Pliocene; howeve r, the verte brates point out to a Serrav allian to Tortonian

age." S r ~ S r ages on oysters from above the level with vertebrates point ou t to 3.0( +2 .5-1. 0) Ma. Similar sand deposits occur at

Morgad inho (Luz de Tavira). These sands are ove rlain by marls, lign ite clays, lacustrine limestones and a silty calca reous crust. A small mammals association indicate an age span between Upper Pl iocene and Lower Middle Plei stocene (M N 17.M N20).ABiharian mamma l fauna (Lower Pleistocene) was collect ed at Algoz in similar depos its. In the present stale o f kno wledge, Mo rgad inho and

Algoz deposits may be correlative.

RESU MO

Palav r a s-ch a ver Neogen ico; Bstratigrafia; Algarve; Portugal.

Apresenta-se um a sintese sobre0Neoge nico do Algarve. Dataeccs de" S r ~ 6 S r , bern como dad os bio stra tigrafico s de unidad es

miocenicas, pennitiram 0 esta be lecimento de urn novo qua dro estratigrafico para as unidades liticas alg arvia s. A Formacao de Lagos -Portimao corrcsponde a depositos sedimentares de tipo "plataforma carbonatada tempera da" que se dcscnvolveu durante urn longo intervalo de tempo (Burdigal iano inferior a Serravaliano superior). Uma mudanca maie r na scdirnentacao (ambie nres silici clasticos) deu-se no Tortonian o inferior com a deposicao de areias finas amarel adas .

No interior do Algarve oco rrem espongolitos rieos de microfosseis. A idade nao este perfeitamente definida. Foraminiferos indieam a zon a N16 (Torton iano in ferior) e os Nanofosse is calce nos a zona CN5a (S erra valia no superior) .

I" Ccogressc sobre 0 Cenozcic o de Portugal

o

conglomeradogrosscirode Galvana (Faro) poe alguns problemas.

uatecees

KJAr de glauconite indicam6.72±O. 17Ma. Todavia, a glauconi te podc tcr sido remobilizada a partir de niveis mais antigos (Formacao de Cacela). Parecem ester relacio nados com memento de forte instabilidade tectcruca como0da instalacao do olistostroma do Guadalquivir.

o

Plio cenico nao csta bern caracrcrizado . As areias de Olhos de Ague com uma intcrcalacao marinha pouco espcssa , rica de vertebrados marinhos (peixes, urn crocodile. cetaceos, sircnidoos) possivelmcntc redepositados, pede corrcs pondcr ac inicio do P fiocenico superior; eontudo , os pcixcs, marnlferos marinhos e0 crocodile apontam para0 Serravaliano a Tortoniano inferior. Datacc es 17SrJ1"Sr cfecruadas em ostra s e em dentes de pcixc fom cccram vatores de 3.0(+2.5- 1.0) Ma. Arcias do mesmo tipo ocorrem em Morgadinho {Luz de Tavira). Sao sobrepostas pe r margas, argilites lignitosos, calcarios lacustres e uma crc sta carbonatada. Os argilites lignitoscs fomeceram fauna de pcqucnos mamiferos corrcspondcnte eo intervale Plioccnico superior a parte inferior do Plis roccnico medic(tvrN17-MN20). Em Algoz foi recolhida uma fauna datada do Pllstocenlco inferior (Bihar iano) em depos itos sernelhantes.

E

possivcl que as jazidas de Morgadinho e de Algoz sejam correlat ives.

FOREWORD

The first studies abou t the Cenozoic of Algarve dealt only with some fossil localities and deposits (Pereira da Costa , 1866 ; Dollfus et at., 1903·1904 ; Bou rcan & Zbyszcwski, 1940; Chavan, 1940; Zbyszewski, 1948; 1950).

In 19 79, M.T. Ant une s and 1. Pa is, carried out stratigraphic studies on the Neogene of Algarve (Research lin e n" I of the former "Centr o d e Estratigrafia c Paleobiologia da Universidade Nova de Lisboa"}, Some synthetic interpretati ons have been published (Antunes

et

aI.,1981; Antuneset aI.,1990; Antuneset al., 1992). New developments have been achieved concerning mainly87Srl

!IIISr isotopic dati ng at the Department of Earth Sciences of Cambridge University (Table 1, Fig. 1). A revision is under way tak ing into accoun t all the available data, and specially isotopic ages, micropaleontology and sequence stratigraphy analysis.

At the present status of knowledge, the Neogene units characterized so far are mainly of Miocene age and mostly marine. They range from Lower to Uppermost Miocene. However, there are lithological differences. Olhos de Agua sands could be ascribed to the Pliocene based on~ 7Sr fl6Sr

da ting, bu t this needs to be con fir med . T hose of Morgadinho (Antuneset at.;1986e) may (at least in part) be Pliocene in age.

The Neogene units so far recognized in Algarve are shown in the Fig. 7, and will be discussed by chronologi-cal order.

Pereira de Sousa (1917; 1918; 1922) admitted the pres-ence of Miocene igneous rocks in Algarve although these were not found later. In 1971, a small basanite outcrop enclosed by Miocene biocalcarcnites was detected, show-ing clear evidence of low grade thermal effects on the sedi-mentary rocks along the contact with the igneous dike. This rock represents the latest volcanic activity in Portugal (Pin to Coelho & Brav o, 1983 ). Ho wever, Cen ozoic volcanic activity is well known in Southern Spain, since Langhian-Scrravallian till the Quaternary.

Tectonic struc tures concerning the Mesozoic and Cenozoic deposits of the Algarve basin allow to recog-nize the following alpine orogenic events : Jurassic (Upper Triassic at least) - Lo wer Cretaceous N-S distension; E·W distension during Lower to Upper Cretaceous; N-S co mpressio n during the setting -up of the Monchiq uc syenite dome at the uppermost Cretac eous; Paleogene

compression (only locally? - at the Albufeira salt dome); Lower and Middle Miocene N-S and E-W distension; Tortonian N-S co mp res s io n; post -Messini an E·W compression; N-S compression dur ing the Quaternary .

Table I • n SrJ1"Sr resu lts.

Louli l.

Lnra liti.. Sam p. .\ h "S rrSr

.,.

o·

,

9.g('d.5) 0,708903 0.000024

,

Alje,u '

,

12.6(+0.9· 0.g) 0,70n50 0.000020 Fu,oa Ama,e la

,

11.9(t{l ,8) 0 ,70 g ~67 0.0000t 8

a

AljJ lgreja Nc.'a 16.9(-'0.3) 0.708701 0.00001 8

a

Alje,u'

,

18.5(-'0 ,3) 0.70860S 0.000017 IG;mnodesponivo

,

19.5(+0.3 .0,2) 0,70gSn 0,000017

•

Sag' .. 12.0(+1.3·1.3) 0 ,70 g ~~6 0 .ססOO21

12.5(+0.S·0.7) 0,70gS50 0.000047

5 Za,;.1 16.2(+0.5' 0.5) 0.708734 0.00002 1

,

17.S(+0.7_0.7) 0,708653 0.00002 6

,

16.3( +0.S-0.3) 0,708737 0.000020

6 Praia do C.o", ;al

•

14.3(+0,S·0.5) 0.708 ~04 0.000017 s 15.l( +0. S.0.5) 0,108771 0 .ססOO1 8

,

Alb"de;ra 5.5(+4,1'0.1) 0,708959 0.ססOO1 8

a 12.2(+1.2.1.3) O,708S60 0.000018

a

P,aia d. Roeh

,

11.5(+0.8·0.5) 0,708815 0.000026

"

10.1(+0.8.1.2) 0,708SS6 0.000018

9 Albaodei..

W

,

15.5(-'0.4) 0.108763 0.000017

W

.

16.3{+0.4· 0,5) 0,108799 0.000017 rc Ga l'; 11.J{+0.9.1.3) 0.108n O 0.000024

"

P,.i. do C."elo 15.5{+0.8·0 ,3) 0.108759 0,000017

,

i9.5{+0.2-0,3) 0.70851S 0.000017

"

An iflo

,

19.2(+0.2_0,4) 0.108553 0.000018

,

14.2{+0.6-0.4) 0 .10 ~801 0,000020

•

8.3(+2.2-3.3) 0.708922 0,000021

,

14.4(+0.5-0 ,6) 0.10 8804 0.000017

u S' o,.Eul.lli. z 14.6(+0.5·0 ,6) 0.70 8799 0,000017

,

15,5(-'0.4) 0.70 876l 0,000017

"

110,el Au"m" z 9.S(+1.O.0.5) 0.708907 0.000016

"

Olho, de Asu' 14.6(_0,4+ 1.4) 0.708797 0,000020

"

Arei.,lOlhos 3,0(+2,S_1.0) 0.709044 0,000048

A . ,

,

5.2(+4,('{l.6) 0.70 896 1 0.000014

"

Quclfe,

,

5.2(+4.4. 1.1) 0.70 8971 0.000018

,

S.3(+4.3· 0.7 ) 0.7089S2 0.000018

"

Cacot,

,

5.7(+] ,9.1.1) 0.708 9S0 0,000014

•

8.3(+2.2-3.3) 0.70 8922 0.000021

rs Mem Moo;z Fo" m 12.5(_1.1+0.7) 0.7088)1 0.000016

-';" .j!i!

' ~

/

}

,

'<,

,

"

.

]

Fig I - Geological schematic map of Algarve. Numbers - Sr isotopes sampling localities.

Cuncias do Terra (UNL). 14

T he NE-S W frac t ures a ffecting th e Pa leozo ic basement are related to the first distension phases . Th e mesozoic N -S distension is the main ca use of the two

E-Wflexur es so far recogn ized . Th e tectonic inversi on

occurred after the setting up of the Mo nchique syenite. If th e Lo wer C re taceo us - Lo we r Mioc en e A lbu feira 's unconform ity is a loca l effect of halokinesis, then the true tectonic invers ion o f the A lgarve basin only took place in the Lower to Midd le Tortonian.

Th ese eve nts co rr e late well with those known 10

sout hern Spa in and Morocco (Ku llberget af., 1992).

L.AG O S - PORTIl\-1AO FORMATIO N

Th is Formation, first described by An tunes eral.

(1 98 1), is the most evi dent M iocene unit in western

Algarve. It makes up a siza ble portion of the costal sea

cliffs, an d is of conside rable sce nic interest. It overlies

Carboniferous, J urass ic, Cretaceo us an d p o ssi b ly Paleogene units. In some places a very cle ar angu lar unconformity can be obse rved, whereas stratigrap hical hiatuses or paraconformities may be recognized elsewhere. The whole successi on has been much affec ted by karst phenomena.

T he Lagos- Portimao Formati on comprises yellow or pi nk massive and very foss iliferous biocalcareni tcs o f " warm temperate" platform type . Th e unit end s by an erosion surface , and is overlain by laminated sandstones, poor in foss ils.

At O lhos deAgua-Praiade Santa Eulal ia, a lenticular

body of sa nds tones with sa nd waves ou tcro p. I'Sr/uSr isoto pic ages give 15.5(±OA) Ma taken for biocalcaren ites

und er th e sands to nes (Sa n ta Eu lali a b each ),

14 .6(+0 .5-0.6) M a for the sa nds tones an d, above it,

14.4(+0 .5-0.6) Ma .

In the lower part, well expose d at Praia do Cana vial (Fig. 3), mol luscs are p lentiful. As for the upper part, ther e are many sea-urchins, Bryo zoa, pcctinids and fishes. The loca lity of Ce rro das Mo s (Lagos), from where a large

crocodilian (Tomistoma) to oth was collected long ago

(Ant unes. 196 1; Antuneseral.,198 1), has also produced

some Odontoceti teeth . These may be dated from the Serravallian, which, cons titute the oldest marine mammal occ urrence in A lgarve (Estev ens, 2000 ).

Pla nktic Foram inifera from the up per levels includ e

Globigerinoides trilobus,Gsubquadratus.Gbisphericus, Gfoboquadrina baroemoenensis and

cr.

Praeorbulina transttor ia , w h ich po int o ut to N 7- N8( ? ) (U p pe r

Burdigali an to Langhian) (A ntune s et 01., 19 8 1). The

presen ce ofOrbulin a in b iocalcar eni tes at th e Faro

borehole indicate that the Serravallian is also rep resen ted

there (Antunes eraI.,1984 ; Antunes& Pais, 1992 ).

A 17Srf'liSr isot opic age indicate 19.5(+0.2.0.3 ) Ma

1°Ccngressosobre 0 CenozcicodePortugal

and 14.3(±0. 5) Ma (Burdigalian to Lower Serravallia n). The upper beds at Praia da Rocha (Fig. 4) gave a17 Srfl~Sr

age of 12.2(+1.2- 1.3) Ma and 11 .5(+0.8-0.5) Ma (Upper Serravallian). At Aljezur, the lower levels (s ands with oyes tcrs, outcroping at the "P avilhac Gimnodesportivo'') in d ic at e 19 .5 (+ 0 .3· 0 .2 ) a nd 18 .5 (±0 .3 ) Ma , thus corresponding to the Lower Burdigalian. At Igrej a Nova, marlswithbiocalcarenites gave 16.9(±0.3) Ma and upper levels. silstoncs and marls at Fum a Amarela, gave values between 12.6 and 9.8 Ma (Table 1).They may corres pond to the great Serra vallian transgre ssion .

Nannoplankto n(Reticulofenestra pseudoumbilicusand

Calcidiscus p remacin tyrez)from the upper part of the unit (Albardeira, Lagos), also po ints out to a Serravallian age (NN6 or CN5 a) (Cachao, 1995).

On the other hand, this unit is older than the K-Ar dated glauco nite fine sands from Praia da Gale ( 10. I±O.25 Ma), as well as the sandstones from Praia da Rocha [' 7SrJl6Sr: 10.7(+0.8- 1.2) MaJ.

MEM MONIZ SPONGOLITIIS

Overlying the Cretaceousinthe inner Algarve the re is an outc rop of wh ite spongo liths virtu all y de vo id o f macro fossils but cont aining microfauna. These depo sits were origina lly described by Romarizet al.( 1979. 1980b). They are unkno wn elsewhere in Portugal, but closely simi-lar ones are widespread around the Mediterranean. They seem to have accumula ted in upwelling conditions in a trough related to tectonic events .

Th e roc k is composed essentially of skeletal elements of sponges. They also yielded some fish remnants along with large numbers of micro fossi ls, including diatoms , calc areo us nann ofossils (am ong others, Helicosphera carteri, Recticulof enestra pseudoumb ilicus, Coccolith us pelag icus, Cyclococcolith us macintyrei, Sphenolithus

ab ies. Discolithin a m ultip ora )(An tunes et al.• 1981 ;

Cacbao, 1995) benthi c (Nonion boueanum, Ammon ia,

B u!imin ids , B o li vi nids, U v iger inids ) and p lan ktic Fo ram in ifera, an d Os trac o d a (Au rila zby sze wskii, No nurocythereis seminulum , Carinocyth ereis ga lilea)

(Antuneset al.,1981; 1990; 1992).

Pl ankti c fo raminifera (Gl obig erina bulloides, G.

quinqueloba ,G.druryi,G.glutinata, Neoglo boquadrina acostoensis, Globigerinoides bulloideus)date these beds at least fromN 16 (LowerTortonianHAntunesetal. , 198 1;

. 1990 ; 1992). Ca lcareous nannoplancton indicate zone

CN5a of Bukry (upper Serravalli an) (Cecbao, 1995). I7Srl " Sr age on planktic foraminifera is 12.5(+0.7-1. 7) Ma (Up per Serravallian) . Hence , the accurate age of these deposits is still open to discussion, albe it between rather narrow limits.

Benth ic Foraminifera point out to shallow environ-ments, rich in organ ic matter, and to low oxygen conte nts. Such facies are quite alike some Upper Miocene ones in Sou t hern Spa in th at o ve r ly th e Guada lq u ivir olistostrome.

FINE SANDS AND SANDSTONES

Th is un it is se pa rated from the Lagc s-P ortlms o Format ion through a disconformity ,

It marks a maj or change from carbonated to siliciclastic sedimentation. Taking into account the isotopic ages from the lower levels, this change canbecorrelated. with the beggining of the eustatic 2nd order cycle T B3 (Haqet al., 1987).

The lowermost level at Praia da Rocha (Fig. 4) is a conglomerate with phos pha tic c lasts and gla uconite.

Ostrea shells gave a 87SrJl6Sr isotopic age of 10.7(+0.8-1.2) Ma (Lower Tortonian).

Fine sa nds at the Hot el Au ramar bea c h [l7SrfUSr isotopic age 9.5(+ 1.0-0.5) Ma] are considered correlative of the unit Fine sands and sandstones.

At Praia da Gale. glauconite-ricb fine sands allowed K-Ar dat ing ( 1O.1±0.25 Me, Lowe r Tortonian) (Antunes

etaI.,1984). Boskiet al.( 1995) obtained K-Ar ages from the same region 8,15±O,29 and 7,54±O,27 Ma.

CAC ELA FORMATION

T he uppermost Miocene deposits arc wcll represented

ineastern Algarve, but they also outcrop near Lagos (west-em Algarve) .

At Campina de Faro and Quelfes there are fossili ferous carbo nate rocks rich in detrital quartz; in some places these deposits grad e into microconglomerates (Faro lime stones with quartz pebbles and conglomerat es). At the upper part of the Auramar Hotel beach there is a lower level of eon-glomerates with o ysters t hat gi ve a 17Sr/ IiiSr ag e o f 8 .3( +2.2-3 .3 ) M a . T hi s is in ag re emen t wi th th e biostratigraphic datation ofthe lower levels ofCacela river (NI6-N I 7) which beg in by a co ng lomerate d irectly overlying the Triassic (Fig. 5). The Auramar conglomerate

Legend

Ir~ ~~i1

Blccalcarenites Ph Phosphatic nodules ~ Ostreids

tst;

Balanids

~

Sandstones

G

Glauconite ~ Other bivalves

~

Eehinids

~~~

Conglomerates ~ _{Disconlorm ity}

"il

_Bryozoans

₆

_Gastropods

Ciencia$ da Terra (UNL), 14

Praia do Canavial section

m

Note: carsUIcaUon affectsthewhole sectlon, 'romtopto bottom.

Includingthecretaceousb. .ement

..

35

Y :;:;:::

~ :

:I:r.i :::::::1::

:::: :,:::,t"":

: f. ~ : : ~: ~ :

::

:::: ::::;:: :V:

Compact biocalcareniterich inIergesizepectinids

: [ ",,~ : : :, ::

:-: :-: :-: :-: I:-: ~:-::-: ~ : ~ : 1 : ~ :t:: : :: :: I ::

,:,:I:

::" ;<1 :,:, :

.

'n; .'

:-:-:.,-:

:~ : . :: :..r. : .: . :I:.

:::,t: :::::]:-;"

:: ,: : f.::;;;' :I ::

~

:::::::1:::::

30

c

.!!

'ii

>

m

~

~

rll

25

e

:2

'"

c

j

Cretac. 20

Biocalcaremewithbivalves(pedinidsand ostreids)andechink1s

(lessabundart than thebivalves. exceptlor thelastmeter where

echinidspredominate).

_ 1 4 .3( ~ .5 ) M a

• • • :0.,,;, .

arcceeereone. more compactthan the previous levels, with bryoz oans, bivalves (peclinids and osl reids ), gastropods and

fragmentsof BChinids . ReddiSh ferrug inou s concretions.

c

o

10

E

t1.

o

.m

E

t:

~

'"

o

j

1°Congresso sobre0Cenozcicc de Portugal

Praia da Rocha section

Fine yellow sandstone, with thin greyish, carbonaled crossed beds.

h contains veryscarcefragments of pectinidsand echinids.

Reddish biocalcarenite.

Biocalcarenite with echinids, pec1inids , balanids and abund ant large ostre lds.

Yellowish sandstone.

Compact greyish biocalcarenite,with more rossns thanthe previou s

level (balanids and pectin Ids more abundant; large echinids) , but in

lesser numbers than atthebasa l lev el. Ther e are yellowish

sandstone Inter calations

Fine yellowish-orange, carbonate-cemented sa nd stone , with

scattered and scarce fos sils (pe ctinidandechinid fragme nts , balan ids

and bryozoans) .

Compact , yel lowish-orange biocalcarenitewithabundant fossils :

large pecti nids and echinids (fhe latter reaching 15 em in diameter) , ostreid s, vertebra le ocoee, corals, gastropods , etc . It also shows biOturbations and some ferruginized bival ve shells.

...

._

....

.'. .

'

.

·

.. .

'

·

. ....

Fineyellowsandstone, with fossi ls similar to thoseofthesecood

level butlessfrequent.

Wiff f'ff -

11.5{+O.S-O.S)Ma

;;;;;; ·· ···; ;;;;;;; ;;;;; ~ i f;

::::::::%:;:::::::::;.::::::

Fine yellowish-orange sandstone with intercalated ferrugi nous beds.

: : : :: ;: : ::::: :::: ::.::::: ~ :: hcon tains pectinidsandscattered small echinid fragments.

illl i·lllllfd:::I-

12 .~ +1. 2 -1. 3 ) M a

"-. Cong lo merate with ph osphatic nodulesandgl aucon ite

1 ~i

li .m:

-

10.7(+O.S-1.2)Ma

_ Biocalcarenite with echinidsandlarge sized pectinids.

10

20

1 5

,..

"

.!!

J::

01 C

j

5

_.

•

. ~ .

m

_·

_{. ' ;}

"

C

·

8

.!!

..

:ii

01

~

'6

.,

~

~

III

"

....

m

25

.,

e

.,

"

"

~

0

_c

:ii

0

~ 1::

.,

₀

eL t-eL

:>

.

.

is interpre ted her e as correlative ofthe lowermost deposits of Caccia Formation, which comprise mainly yellow, ora nge, or gree n glauconite silts.

The lower conglomerates at Cacela (Fig. 5) and the directly ove rlying silts yielded the richest and best pre-served Miocene mollusk fauna in Portugal. Th is fauna was des cribed by Pereira da Costa ( 1866, 1867) and Dollfuset al. (19 03, 1904), and revised by Chavan ( 1940) and Bourcart & Zbysz ewski (1940). Glycym eris, Cardium, Megacardita , Panopea , Pelecyora, Callista ,Turritellids, Naticids, and Conus are common. T here are also some Vertebrata. Amon g theselacians,Carcharocles megalodon

has been recorded but no Carcharodoncarcharias(both species coexist in Pliocene when the latter appears for the first time, this association being known in Southern Spain

- Elche ,etc.) (info rm .of M. T. Antunes). Also, a few

previo usl y unr eported cetacean rema in s have been co ll ecte d lo ng ago at Caeela supp osedly from the yellowish silt levels. These consist of vertebrae , rostrum and mandible fragments of large-siz ed Myst iceti, which are deposited at the Geological and Mining Institut e.

O lho s de Ague and Ce rro das Ma s occ urr ences (refe rred to elsewher e), are the on ly localities in Algarve that yielded fossils of marine mammals. Moreover, Caccia is one of the younges t records of marine mammals in Portugal; it is on ly a little older than the late Messinian remains from the Esbarrondadoiro Formation in Alvalade Basin, Alentej o (Antuneset al.,1986).

As no accura tely dated post-lower Tortonian miocene deposits are known in the Lower Tagus Basin (where the remainder of the series is very well repres ented), the imp orta nce o f the Cac ela reco rd b ecome s obv ious . Fo ramin ifera and Ostracoda[Audia (Cy mbaurila) diecci,

A . gr. sem ilun ata, Cartn ocyihereis g alilea a nd

Nonuracythereissem inulum]are p lentiful.

Pl an kt ic foram in ifers a re su ita ble fo r dat ing :

G lo big e rina b ullo ides , Globorotalia scuuta , G.

pseudomiocenica,G menardii, G humerosa, Galtisp ira

andNeogloboq uadrina acostaen sisindicate N 16-17 zones o f B low (U pp er Torton ian-Lo wer Messin ian). T he p r e sen ce ofSp iroplectam ina ca rin ata (a b en thi c foraminifer) excludes a Messinian age for the lower levels of the CacelaFormation(Antuneset al. ,1981;1990; 1992). Calcareous nannop lancton from the lower beds include

Discoaster berggrenii, Heli cosphaera sta lls, Miny litha convalisandTriquetrorhabdu lus rug osus(?)that also point to the sa me UpperTortonianage (CN9 a zone of Bukry) (Cachao, 1995).

Somewhat higher levels (a tFabrica)yielded calcare-ous nanno pla nc ton (Coccoli thus p elag ic us , Re ucu lof enestra pseudoumbilica , R. minuta , R. minu uda, R. haqii,

Diayococcnes

antarct icus, Sphenolithus abies,

S. morifo rm is , He lic osp hae ra ca rteri, E udiscoaster surculus , E. icarus, E. intercalaris, E. pseudovariabilis, Triquetrorhabdulus rug osus) and plankt ic Forami nifera

[Glob ig erina bulio ideus , G. ap ert ura , G. dru ry i, G.

quinquelob a, Globigerinoides extrem us, G seigliei, G

quadrilobatus, Globig erinita gl utinata, Orbulina universa,

O. su turalis , Globoq uadrina g lo bosa , Gl oborotalia (Hirsutella) scitula, Neogloboquadrina acos taensis sin.]

Cu nctas da Terra (UNL) , 14

that may be ascribed to Late Tortonian-Messinian (Antunes

et al. , 199 0 ) . B e nt hic Fo r am in ife ra (B olivi nids , Bulimini ds) indicate oxigen-poor environments (Antunes

etal.,1990).

These beds are overlain by si lty or fine sand beds in stratigraphical continuity with scarce , poorly preserv ed fossils including so me plant remna nts. Upper bedsmay be Messinian in age .

The middl e, also silty, levels of CacelaFormationare ric h in gla uconite that gave ages o f 6.90± 0 . 18 Ma (Galvana) , 6.88±O.5 (Q uelfes)and 7.03±O.4 Ma (near Luz de Tavira), uppermo st Tortonian (Antunes et al., 1984,

1986d ; 1990 ; 1992).i7Srl"Sr ages from the Qu elfes silts are 5.3(+ 4.3 -0.7); 5.2(+4.4- 1.1) and 5.2(+4 .4-0 .6) Ma (Fig. 7) . At Q uelfe s, above the gla uco nite lev el, the occurrence of Glob orotalia men ardii (100% dext.) and

Globorotalia miotum ida( 100% sinist.) allow correla tion with the event 3 from the Guadalquivir basin (Sicrro et al., 1985, 1993, 1996). This event has been correlated with the Torto nia n/ Messi n ian bo u nda ry. Glo borotalia

conorniozea (FAD7 . 12 Ma, Messinian) was found at the

uppermostlevels fro m Quelfes region.

The upper deposits of the Cacela Format ion overlie ferruginous hardgr ound. T hey correspo nd to confined marine environmen ts, fossi ls being sca rce and poorly preserved . Th e age ma ybeMessinian to Lower Pliocene.

',G ALVAN AC O NG LO M ERAT E

Th e stratigraphic position of the spectacular G alvana conglomerate, with striate blocks exceeding one meter, and interbeddedglauconiferoussilts (Antuneset aI.,1984),

is not clear. Glauconiferous silts indicate aK-Arage of 6.72±0. 17 Ma; however, the glauconite may have been reworked from the Ca mp ina de Faro silts (Antunes

et

al.,

1984 ; 1990; 1992).

Conglomeratesare relatedtostrong tectonic instability and were p rob ab ly form ed in the sub-masi ne slop es associated to the Algarve southern flexure . TheK- Arage is com p atible with that o f the Guada lqu ivir basin olistostrome, although this is far away and correspo nds to South-North sedimen tmassmovements (the Ga lvana con-glomerate has been generated by North-South sediment movements).

Conglomerates ov er lying glauconitic silts in a borehole at Campina de Faro, may correspond to the Galv ana conglom erate. If so , this is younge r than the silts and its age could be Messinian or Pliocene.

OLIIOSDEAGUASA NDS

A thic k sand series out crop s ncar Olhos de Ag ue between the Sand sto nes with sand waves and the Faro-Quarteira Fonnation .

1· Congressc sobre 0Cenoz6icode Portugal

Cacela section

m

10 -- - ~ ---- --

---- --- --- - --- ~

- - -

--l:

o

1i

E

02

..

g

o

FineyellOwish-orangesandstonewithlevelsof carbonated concretions.Fossils are scarce.

-,,-

---

-

-

--- --- ----

-~

- --- --- -

- -

-

-

-

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---.-~- :0;.:.1_-_ ~-

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FIrI8 yellowish-graysandstones.withabt.w1dantIosslls : :--...-It.1-...-_-""'. foramll"lItera.bryozoa, mollusks (bival vesand

.li!J-.v -.~-.,l\ _. "'. gastropods) ...

~~ ~~ --G '

.

. -0- . ":' ~ ~

..:

~ 5 . 7( +3 . 9- 1 .1) Ma

;:

~ ~

~ . . .

Fll"leyellowish-graysandstone

~ 'er. '

_ .'

Conglomeratewith abundantfossils: molluskS (otten

large-sized), cirripeds .

Triassic sandstones 5

l:

....

_~

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Z Z

C eb

₀

o

t: ~

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Trias.

Fig.S•Cacela section (Antuneset al., 1997).

gullies and are covered by red pel ites. The latter are overlain eit her by white sands or by the Faro-Quertcira Form ation (Q uaternary ). Over these white fluviatile sands there are bea ch sands and conglomerates with abraded remnan ts of aquatic Verteb rata (fish vertebrae and teeth, ce tacean bones, Sirenian teeth and bones). The majority of the fishes a re marine, often very large in s ize

(Carcharocles mego iodon.lsurus hastalis, Odontaspiscf

taurus, Hemipristis serra, Carcharhinus sp.). The degree of abrasion of the verte brate remnants suggests that the y

were rolled by wavesinshallow, sandy bottoms at a beach .

TheSirenians(Metaxytherium medium)point out to warm

shallow seashore environments, rich inaq uatic

vegeta-tion (algae, vascular plants) . The prese nce of fish like

Lares,also frequent in fresh water facies suggests (as well

as the feldspathic sands) the ex istence of a large river

whose mouth was quite close by.The prese nce of large

crocodil ians asTomistomacflusitanicacorroborates these

views and indicates tro pical to sub-tropical co nditions

(Antunes, 1979; Ant UReSet al., 1981; 1990, 1992 ).

Above these levels th ere are sands rich in oysters and

scarce p ectinids - incl udi ng the rar e Pa li o l/um

(Lissochlamys) excisum .Molluscs indicate estuarine. even brackish environments.

Vertebrata are compatible with a pos t-Langhian age; they are certainly pre-Plioce ne and they may correspond

to the Serravallian or to the Tcrt onian. T he mollusks are

not chro nologically charac teristic. However, Palio/lum

(Lissochlamys)exctsumis known both in Upper Miocene

and Pliocene (Demarcq, 1979) (it is co mmon in Upper

Pliocene in western Portu gal).11S_{rl"Sr age obta ined from}

oysters gave 3.0( +2.S· 1.0) Ma. However this value has to be taken caut iously since it corres ponds to a brackish environme nt, with broad errors.

M O RG ADI NIIO AND ALGOZ DEPOSITS

This unit com prises thick sandy deposits in assoc ia-tion (towards the lop) with marls, lign ite clays, lacustrine limestone and a silty ca lcareous ernst This unit is poorly exposed in outcrop, for which most observations have been carried out during the excavat ion of water wells.

At Morgadinho and Luzde Tavira these sands overly th e Caccia Formation and arc overlain by the Faro--Qliart:eira

sands , as at Algoz (where the basementisnot known).

At Morgadinho, the lignite clays yielded a few small

mammals (Ga/emys Icormosi, Prolagus cfcatpensis,

Mimomys sp. and M uridae undetermi ned), fres hwater

small cyprinidfisbes,gastropods,Ostracoda,pollens and

spore s (including An thoceros , Kesette rta . Pinus.

Cupressacea and Ericaceae) (AntunesetaI.,19 86c ). Th e

Ciencias da Terra (UNL) ,14

Olhos de Agua sect ion

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Verythn sandswiltlpelllic layers,

Dal1<redsandswiIhcross stratification andpebblelayers ,

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Coarsewhitish sandwiIh pebbles.

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Orange dayey micaceous sand,

La os- PortlmAo Format io n. - 14.4(.(1.6+0.5)Ma

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mammalian fauna ind ica tes an a ge span between the

Up-perP liocene an d the lo wer Mi dd le P le istocen e(MN 17to

MN 20mammal units).

In thep resent state of knowledge. M orga dinho and

Algoz deposits seem to beco rrelat ive . The Al go z

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