50th Anniversary of the IUGS

Vol.34 No.4 December 2011

Journal of International Geoscience

WI Articles

by Birger Schmitz l, Victoriano Pujaltel

, Eustaquio Molina1, Simonella Monechi4

, XabierOrue-Elxebarria1, Robert P. Speijer', Laia Alegrer, Estibaliz Apellanit, Ignacio Arenilla.,J,Marie·Pierre Aubry6, Juan-Ignacio Baceta1, William A. Berggrel/, Gilen Bernaola8

,

Fernando Caballerol , Alllle CfeJll11lensen9, Jaume Dinares-Turell lO

, Christian Dupuisll, Clatls

Heilmann-Clausen9, Asier Hilario OrLÍs l2

, Roben KIlOXI1• Maite Martín-Rubios, Silvia Ortir,

Aitor Payros2, Maria Rose Petrizzo14

• Katharilla von Salis15, Jorilule Sprong5

, Etielllle

Steurbautl6 and Erik Thomsen9

The Global Stratotype Sections and Points for thebases of the Selandian (Middie Paleocene) andThanetian (Upper Paleocene) stages at Zumaia,SpainI Ocpanmenl of Geology. Lund Uni\cn¡ity. 5E-22362 Lund. Swcden. E"I(IÍ/; birg~r.schlllj¡~@K~(}I.IU.S~

Oepanmcnt of Stratigraphy and Palcootok>gy. Uni,·et'"Sity of the Busque Country. E-48080 Bilbao. Spain,

Depanmcnt of Earth Scicnces. Zarag07.a Uni\cn;ity, E-50009 z.arJ.g01..a. Spain.

Depanment of Eanh Scicnces. Aorence Unil"cnit)'. 1-50121 Aorencc. It:lIy.~ 0ep.1nment of Ear1h aOO En"ironmcntal Scicnces. K.U. Leul"en. B·3<XJ1 Leu\'en. Belgium.• Depanment ofGeology. RUlgers Uni,·en¡ity. Pi!i("ataway. J 0885-l. USA,7 Dcpanment ofGeology aOO Gcophy!>ics. Woods Hole Occ:.lIlogrJphie In"litution. Woods Hok. MA 025-13. USA.

• Dcpanment of Mining aOO MelaJlurgie Engincering aOO Material Scicnces. Uni\ersity of the 8a'>que Counlry. E-48901 Barnkaldo. Sp.1in.~ Dcpartmenl of Eanh Sciences. rhus Univen¡ity. DK-8000 Árhus C. Dcnrnark.

nI Instituto NazionaJc di Geofiska e Vulcanologia. Via di Vigna MIlI,¡\t¡1 605. 1-00142 Rome. haly.11 LaborJtoire de Géologie Fondamentale el Appliquée. F:lculté Polytcchni(IUe de Mons. B-7000 Mons. l3c1gium.

Il Egu1.kiuldc 1]. E-20271 IrurJ, Gipuzkoa. Spain,11 Brilbh Gculogical Survcy. King,ley Durham Centre. KcywOrlh, Notlinghml1 NGI2 50G Uniled Kingdolll.I~ Dcp¡1I1rnC111 uf E¡trth Scicnces, Mihmo Univcrsity. 1-20133 Milano. haly.

l' Vi:! Maistra 9. C1-I-7513 Silvuplnna. Swilzcrhllld.lb Dcpanment of Paleontology. Royal Bclgi:m Institute of Natur:ll Scicnccs. 13-1000 Bl1.lsscls, Bclgium,

'11U! global slmrol)'pe ,~eclioJlsal/(Ipo;",sfor lile bases

of lile Se1cmdi{1/l (Middle Paleocelle) amI Thallel;all

(UtJper Paleocelle) stages lun'e beell defilled i1l lile

coasIal diff alollg Ihe Ii:urlm 8each al lhe /O\\'II of

Zumai{1 ill Ihe Basque ~olllltry, lIorlhen¡ Spaill. 111 Ihe

hemipelagie seelion e.xposed al Zumaia Ihe base of Ihe

Setwuliall SIage has beell plaeed al Ihe base of rhe11:Ilr1m Form(lfioll. ca. 49 m {Ibol'e lile Cretaceolls/

Paleogelle bOlmdary. Allhe l}{Ise ofrlle Selwldhm. mar!!J,'

replace Ihe SlIccessiOIl of Oalli(/11 red /imesf01Ie {md

limeslolle-marl eOllplels. The besI marille. global

correlarion crileriol/ for rhe basal Se/alldillll is Ihe.I'ecol/d I'lIdil11iol/ oflile imporrltll1 clIlClIreolfS f/(/1lJlOfossil

grollp. rhe fascicll1ilh.~. Specie.\' ,wch as Fasciculithus

ulii. F. billii. F. janii. F. involutus. F. pilei.llllS {//Id F.

tympanifomlis h{lI'e rheirfir.l'I appearance inlhe ;lIlen'al

from afew decimelres below up ro 1.1 m ahove Ihe base

oflhe Se/alldian. The marker!J,'l}(xiesfor1I111l1l0fossil ZolleNP5. F.lympanifonnis.jirsr occlIrs 1.1 m ahol'e rhe l}{Ise.

Excellelll cye/oslraligmphy amI mag1leroSlraligrap"y ill

I"e seclio1l cremes flln"er correlaliolltJOlell1ial, lI'il" rifebaseoflhe Selalldiall oc(:lIri1lg 30 precessiofl cre/es (630

kyr) abal'e rhe lOp of magl/eroc"ro/l C2711. Profolllulclumges ;1/ sed;mellf%gy relaled lO a II/ajor sea-/el'et

fall c"arl/cleri:e rhe f){lIIic",-Selc",d;lIIl lral/si/;O" ;1/seclio/lS alollg I"e lI/arg¡1Is of rife Norl" Allal/l;c.

r"e bll.5e ofllle Tlulllelian Srage;s placed i/l rhe ,WllI/e

seclioll ca. 78 11/ abolle I"e CrelllceOI/,~/Pateogelle

bOll/lt/ary. 11 i.l" defil1ed {/1 a letwl2,8 111 or eigll/ precesÚolI

(.')'cle,~ abol't! lile base of lile core (Jf rhe di.\'rillct day-rich

f)t'("f'm~r 101 I

il/lel"l'tll aS,WJÓaled IVilh Ihe Mid-Pa{eocelle JJiolic Evenl,

ami il corre,VJOl/ds lo tite bme olll/agl/eloclllvl/ C2611 ill

tlle ,~eetiol1. Tite !Ja,"e ollhe Tlwl/etiall is IlOt assoÓaled

lIIilh al/Y signijicclllt c!utllge ill marine micro-fil/llw 01'

flora. 11/e calcareol/s l/al1l1ofossil Zone NP6, l1Iarked by

lile jirsl oCClIrrel/ce 01 I-Icliolithus klcinpelli srar(s ca,

6.5 /JI belolllllle base olllle 11wl1elial/. The dejil/itiol/s oI

rlte global,\'r/"{/tolype poil/rs¡orIlle bases ofllle Selalldillll

al/d 71ul/lerial/ srage.\' are ill good agreemellls willl Ihe

dejil/iriol/.\' il/ lile hiSlOrical Slralotype secriol/.I' in

Dellll/ark alld EI/glal/d, respeclil'ely.

Paleocene GSSPs - introduction andbackground

In 1993 lhe Paleocene Working Group was eommissioncd by lhe

Inlernalional Suocommissiol1 on Paleogene Slratigmphy lo define

global slralOlype sections and poims for lhe bases of lhe Sclalldiall

alld Thalleliall slages (Sehmil:I.: 1994). A slage represenls lhe basie

chronoSlr.lligrJllhk unil in lhe global Geologic.lllirnescale. and lhe

base of eneh slage is de!1ned by a Globall3ollndary SIr;l\Olypc Seclioll

alld Poinl (GSSP) in ,m approprialc, ('onlinuous marine seelion. The

GSSP fepresents a poinl oolh in uncicnl time ,lIld in lhe rock record.

and ils definilioll facililates eürnmllnicmion among cal1h sdcntislS.

After fourtcen years 01' resc<lfeh and discllssiollS lhe melllbers nI' lhe

Pnlcoeene Worldng GrollP ngrced lInanimously in June 2007 on

forwarding lhe pmpOS;¡11hallhe b'1SCS Oflhc Selandian and Thanelian

slages should be pl'leed in lhe ZlIlllai,l seclion allhe Sp,ln¡sh CO¡ISl of

lhe Bay of Biscaye. Foliowing ;¡pproval.~ in 2008 by lhe Inlcm;llional

SlIOCOl1llllissíon on P:lleogclle Strmigraphy and lhe JlIlernational

Commission on SITaligraphy lhis suggeslion was acceplcd and

formaliy Talified by lhe Inlemlltiunal Uníon of Geologiclll Scicnees

on Selllcmbcr 23, 2008. This (Xlpcr gives a summary and background

of lhe research and considcrations lIndcrlying this decision.

The Selandian and Thanetian stageshistorical background

The divisioll 01' lhe PalcOl,:cnc Series imo lhree stllges. Danian,

Selandian :md Thanelian. was uecided by lhe Inlernalionll1

Subcommission on Palcogene Str;lligraphy allhc 1989lnlcrnalional

Gcologicnl Congrcss in Washington (Jcnkins and LlIlerbachcr 1992).

111e base oflhe 10wer stage. lhe I)anian, coincides with lhe Crelaeeousf

I'a[eogene boundary which 1l¡IS bccn formally dcfined in lhe El Kef

scelion in Tllllisia ¡¡(Ihe bascoflhc iridium-rich clay layer thal formed

aflcr a major asteroid or comel impact on Earlh (Molina el [jI. 2006.20(9).

Thc second Palcocenc stage. lhe Selandian, was origin'llly

describeú in Denrnark by RoscnkranlZ (1924) nnd consists of

fossiliferous glauconilie marls (Leliinge Grccnsand nnd KCrleminde

Mllr1) overlain by t1nfossiliferous grey day (now ~lIbdivided inlo

JEbcl¡, Forl1laliOIl. Holll1chus Form,uioll and 0s1errcllde Clay)

(Fig. 1), The sllcces~ion t1IK'onformably overlies Danian chalks .md

limeslones and conlains cl:lSts derived ffol1l these unilS in ils basal

part (pcrch-Nielscll and Hallsen 1981: Ikrggrcn 1994). In lhe original

121

Skema over del danske Paleocren.

o

~Rupélien Septarielero

.0'5

Lakune

Strerkl farvede, rede Lerlag Eo

Londinien ~-Lag med vulkansk Aske •ü

Graa Lerlag

Graa Mergeilag Eo

Sélandien o-o Gr0nsandslag ••u Üo.. Konglomeral (Iokalt)ro~

Lakune

• Kalksandskalk (Iokal)

~oE~ Kokolilkalk, Bryozokalk, Koralkalko

Danien o-•ü• Bryozokalk"•Lakune

Cerilhiumkalk

Lakuneoo

Maastrichtien Skrivekridlo•"'

"';gl/re l. Strat;grapJ¡ic ~'clleme lor lile I'(l/eorene ill lJelll1/l1rk byRm'e"krall/z (/924). TJ¡j,~ is lile flrst l/se 01 lile regiuJI(ll sl(lge"Sé/al/diell ".

l)'pc llle,l lhe Sclandiall deposils are o\'erlain by lhe ellr1icsl Eoeene

01s1 Formalion and Ftlr Formalion ("Mo Clay"). cOlllailling Ihe

nUl11erous. well-known '"nurnbcrcd"' n~h 1¡IYCrs (P<,.'Uen;cn ,md SlITlyk

1983). Jnlhe Norlh Sea rcgion lhe Danian/Selandiall bollnd:lry reneelS

lhe end of ca. 40 mili ion ye.lrs of conlintlotls deposilion 01' open­

marine cllrbonalcs. alld rcprcsenls a major ch'lI1gc in lhe leclonic

evolulion of lhe northcaslcrn Allllnlie (Ziegler 1990: Berggrcn el al.

1995: C1cml11cnsen ,md Thornscn 2005: Niclscn el al. 2007), 11 is

nOlable lhal ulllil lhe middlc of lhe 201h cClllury lhe Crelaceou~

Paleogenc boundary was slill oflen plaeed al lhe IOp of Ihe Danian

limeslone (see rcvicw in l3erggren 1971), Hu.~d on Dilnish OlltCrop

scclions, ¡he DmlianfSelandian bollndary has lr.ldilionalJy bccn plm:ed

neaf lhe pl.mklOnic fO[";ll1linifer.t zones P2IP3 bound,lIY (e.g.. Berggrcn

el ,11. 19(5), bUllhis renecls lhe c)(islcnce of mlljor 1I1lConforlllilies m

lhe Iimestone/greensand ooulldary. Lller sllldies of more eontinllolls

drill cores in lhc rcgion in(]ic¡¡lc a !llore gradual lilhological change

and [j signiJiennlly yOllllger age. in lhe middle of ¡he Zone P3 alld

dosc lo lhe ealcareous nannofossil zones NP4/NP5 boundary

(Thomscll aud Heilmanll-Clllllscn 1985: 111o!llscn 1994: Clcl11mensen

and 1110m.'\cn 2005).

111

The Thanelian Stage coocept was firsl u~ by Renevier (1873)"00 includcd the 11lanel S;mds with C.'1'rinu IIwrriI and lile Woolwichand Reading Beds with Cyrt'11l/ nmt'iforlllis. lis mcaning W3~

subsequcntly narrowed by Dollfus (1880)."00 induded ooly lheThanct Sands. theoriginallype-strnl3 on lhe Islc ofThanct in SOUlheastEnglaOO. Sil1e'e [880 lhe lenn Thanctian has consistenlly been usedwilh lhe restricled meaning of Dol1fu~ (Bignoc et al. 1997). Inlensi,cbl(). and magnetoslrnligr.lphic sludies and sequence slraligraphicanalysis 00 OUlcrops and wells in !he Iype area ha"e Icd lO a delailcdundecslanding of the e"'tenl of Ihe Thanetian with regard 10 lhcmagnelobiochronologie lime M:ale (Aubry 1994). The historiealThanetian slrata span calcarcous nannofossil zones NP6-Nf>9 ofManini (1971 l. polarity chrons C26n·C24r (AH and Jollc)' 1996) anddinonagcllulc /.Ones Viborg 4 and 5 uf Heilmann-Clausen (l9K5.1994). Studies of drill cores show lh:u lhe baM: of lhe hislOrieulThanetian SI:Jge lies in lhe upper pan of Zone NP6 :llld dose lO lhe

base ofChron C26n (Hine 1994; Kno", 1994a). A m¡¡jor incrc¡l<,C inIhe abundance of the dinonagellale Misocysw gipl'illgt'l/sis iscoosidered a useful e\'enl for l'\."'Cognizing lhe base of lhe Thanclian",ilhin lhe North Sea Basin. while Ihe last occurrence ofPO{lIrofxoridiniulII P.,·rotHIOn¡IFI aOO PlIfot'ocyswdillilflll alu/rt¡!imlllll

blllfifofflU! are late SclaOOian cvcnlS dUI are useful for inlerrcgionall.:orn:l¡¡lions (Heilmann-C1ausen 2(07).

Thc Zumaia scction - gcography andphysical gcology

Thc Zumaia SlXlion is pan of an essenlially l"Onlinuotls lowerSantonian 10 lowcr Eoccnc sea-eliff oUlcropping along lhe coastuf lhe GipuZku¡} province hulfway betwecn Bilbao and S:mSebasti:m (Fig. 2). The P¡lIeocenc p¡ln of lhe ~cction is represcnted

(1) Lower Maastrichllan: medJum-beddedturbidles.

(11) Upper Maaslrichtiln: purple mlns. greymarly limestonea ancl thin-bedded lurbidrtn.

(111) Aitzgorri Limestone Fm. pink-grey~meslOne$and mam.

20 Km

Cinco villasmassif

road lo Ihesection

GipuzJ<oahomocline

",",",....,"",..,..,.,"

San Sebaslian

300 m

BAY OF BISCAY

Biscay syncllnorlum

to Bilbao

oBilbao

Marianlonheadland

• EOCENE

B PALEOCENE

D UPPER CRETACEOUS

D PALEOZOIC

Itzurunbeaeh

~

Iberia Ü_Marine OTerreslrial

(IV) Itzurun Fm. grey Irnettones. mlM Ind lhin­bedded t~bicnes

<V) Lowul Eocene. red-dlrk grey Iuliln (roreof Ihe elE). tollowed by Ihin-bedded ailiclClaslicIurbidilea.

(VII Lower Eocene. Ihlck-bedded lurbldiles.

~'

e

figure 2. (A) Gelleralized eady f'a/eu¡;cl/f! pafcogeogropllic ma,} (if WeYlerll Ellrope: (B) Simp{i/ie(f geu{ugic I/UlP (Jf Ihe y/mly regioll.

sfllJ ....illg lile most importalll I'u{eocelle olllcro{JS ulld '"e {oc(l/iol/ of Ihe ZimUlio beadl seetioll; (C) Geofagic III(IJI of tlle UfJf'er Crelflcemu

- f.,l)K"er f'o/eogene {l/(lcr(Jp.~ in lile Z/lmoio (lrt!(j.

l1J

by a ca. 165 m Ihid. cssentially complele f'CC<lI'"d exposcd along lhe

main bcach.lhc It..:urun Bea<:h. oflhe eoaslallOwn Zumaia (Ialiludc/

Ioogilude4)O IT57.1~ N/2° IS'39.6~W;Spanh.h...pcllingis "Zumaya".

bul we u;,e here lhe original Basquc: narne). 1ñe bull: of lhe Paleocene

is represcnled by rhYlhmk allemaliolls of hemipelagic dcposits in

lhe fOll1l of indur.lIcd limestooes. marly limcslones and marlsloncs.

plus numerous inlercal;nions of Ihin-beddcd lurbidilCS (Pujalte el al.

1995; Bacela 1996: Pujahe el al. 1998a). 1ñe dislinct stnl.ligmphie

e)'ClicilY has becn altribuled lO orbilal forcing (Ten Kale and Sprengcr

1993: Bacela 1996: Oin3.fts-Turell et al. 2002. 2003. 2007. 2(10).

1ñc scdiments werc deposilcd al an l$Iilllalt.'d waler dcpth of I())) m

col1'C!>ponding loa middk lO Iower balhyal selling (Pujallcet al. 1998a:

Arcllitla.~et al. 200S). Scdimentation was hClllipclagic wilh a lerreslrial

eOlllpOllenl supplied axially from !he emergillg prolo-Pyrences and

rnarginally from shallow ('urbomlle plmforms 10 lhe soulh :md nonh

(rig. 3). Olher Ilearby scclions such as Ul Ermuu. ca. 25 km 10 lhe

snulhwcst. Ilrovide records of lhe scdilllcnlaliol1 in lhe base 01' slopc

allron fringing lhe soulhem earbon:'lle plalform (Fig. 3). and conlain

a higher fmelion of lerrigenous maller. and also curbonale 51uml)

dcposil.\o ¡¡nd eakilul'bidilcs (Baceta 1996: Pujalte et ¡tI. 1998a; SChlllilz

el 1\1. 2001). Oue 10 lhe supcrb qualilY of ils exposure. lhe Zumaia

S<.'Clion alrcady :.lIIracled Ihe attention of piooeerworkers in Ihe regioo

(e.g.. Gómez de L1arcna 1946). 1ñe Zumaia <óCCtiOll was also subjecl

lO imponant ichnological sludies. e.g. lhe c1assic Sludy of lurbidiles

and Iheir associaled pre- and po!Jdeposition:allfXe fossils by Scilacher

(1962). h was I:uer lhe subjccI of );eneral sludies of planklOllic

für.lminifera (Hillebr.mdl 1965). cakareous nannofossils (Kapcllos

1974: Van Vlicl 1982). deposilional scuing (Van Vliel 1982) or"C<Iueoce Slrali);mphy (Bacela 1996; Pujalte el al. 1998a.b). lO

menlion a few. Several papers ha\'c focused on lhe Crelaecousl

Paleogene aOO lhe PalcoccnclEoccTlC bound.1rics. inc1uding Ah'arez

et al. (1982). Wicdman (1986), Smil and Ten Kale (1982). Canudo

and f\.'lolina (1992). Goroslidi (1993). Ward and Kennedy (1993).

Canudo el al. (1995). Oniz (1995), Kuhll1 and Kaminski (1997).

SChmill el al. (l997a). Molina el al. (1998.1999). Knox (1998).

Apdlani~ (1998). Arenilla~ et al. (1998. 20(4). An el al. (1999).

Adaue el al. (2000). Arenillas aOO Molina (2()))). Bcmaola (2002),

Orue·Elxebarria el al. (2()().l) and Caballero (2007). These 11.\'0

importanl boundarics. lhe base and lhe top of lhe Palcocene. are

cxcellentl)' exposcd aOO prescrycd in lhe secliOll along lhe Itzurun

Beaeh c1iffs. Zumaia was in fael the main ehallenger for hostin! the

GSSPs for bolh lhe CrelaceouslPaleogeflC and lhe PalcoccnclEoccflCboundaries, Ihal were e\'entually placed al El Ker (Tunisia) and

I)ababiya (Egypt). respecti\'e1y (Molina el al. 2006. 2009: Aubry el

al. 2007).

The GSSP for the Selandian - position,stratigraphy and completeness

Precise posilioll

The base of Ihe Selandian StllgC, lhe second or middle stage in

the Puleocene Series. is placed al lhe base of lhe Itzunm Fonnation

in Ihe SCClion al hzurun Beach in Zumaia (Arcnillus el al. 2008;

Bcmaola el al. 2009).lbc str:lIotypc point for lhe basal Selandian ¡s

equivalen! lO lhe base ofllle marls o\'crlying lhe uppennosllill1C.\olOne

Ix."d of lhe ca. 10 mctcrs of limeslone·marl couplelS in lhe uppcr panof lhe Aitzgoni LinlC:'ilonc ronn:nion (Figs. 4-9). 1bc base of lhe

Sclandian is Ihus ca. 49 melcrs above lhe Crelaceous/P-dleogcne

boundary. fol1owing lhe log of Oinalts·Turcll el al. (2003).

LirllOsrrotigraphy

lñe Ai11.gorri Limeslone r-ormaliOll is dominamly made up of

reddish ¡imestone. wilh varying amounts of rhythmicall)' appcaring

marl inlercalalions. wheteas lhe dominant lilhology in Ihe lower pan

~.

Rlpoll ...

•

• Tremp

~."...~'-- .

REFERENCE SECTIONSZu: Zumaia, Er: Ermua

Un: Unanu, Lz: Lizarraga, Kr. Korres

~''-

'o 'Huesca

I~base·of·-- Slope aprons·_

(hemi)pelagicbasln

1,""\1 outcrops

"

': • " ~oulouse '-~.....~•• ,;<"

~.

. ~,

;:;;.~~ ""'->

LEGEND

I ' 1continental areas.... .... (fluvial-Iacustrine)

p:::;:::r::::;:: shallow-marinel:!:::::::I::::::: carbonate plalforms

I Ireefal& constructions

~. 100 Km~~11

tunan

'<e?

[ LATE DANlAN (-60 Ma)

Figl/re J. tale f)alliall pafeugeugrllflllY afilie /'yrellellll domoill willl rcferellcl! .\'ecliall.~ amI IOCll/ifie.~. //mlll /JaccUt el 01. (1004).

t.¡modes lh/.].I. 110. 4

124

f-igllfe -l. (AJ Tlle IIpper IRlIIia" lO lowu TI/auelia" see/io" iu lile clifJs al 11:,Ilnlll Beaell,The bas#')' /Jf lile Se1tJIIlli(1II (/lid TlulIIelÜ(II stllges ure morked by bJue ulld )'cllow U"es,

rcspeelil'ftr)', rile II'ltile sqlUlre is elll(fr~e(f ill Fig. 7. (U) (//Id (e:; rile GSSI) ;'gIJI(II~f1 sl,ike.~"

lI'ue pluec(1 al lile buse)' afilie Sc/(Jlldiall ami T/wllcliulI IJII May 6, 2010. (O) Tlle base oftheT//flllelitm Stage. (E) Tite /Hlse of lile Sefalldioll Stage.

,,

of lhe \lluron Foonalioo is greyish marlslOncs: howe\·er. color aOO

liloology \ary Ihroughoul lhe formalion. 1ñe Dani3nJSelaOOi:mboundary is dcliot:d at lhe abrupt liloological change belwccn lheIWO fonnalions(Figs. 4--9). In lhe uppcrpan oribe Ailzgoni UTT'IOIOfle

Fonll:llion. largcly of pin"-n.--ddish colon;. lhe lower "crow<k.'1I" aOOlhi..- uppcr "'tmlified" mcmbcrs can be distinguishcd (B:lecla el :11.2006). The cmwtled melllbcr is 7 m lhick and cOllsislS of IimeMones

amalgalll:lled or Wilh very lhin m¡lrly inlerbcd~. TIle Slntlified mCIllOCr.

9 Ullhiek.lakes ils name from Ihe wel! dcfincd rttYlhlllic bcdding alldIhe clcady di'linguishable marl-limcslOne altem:tlions. Some of lhebeS! exalllplc:. of so ¡'alled bundlcs repre,cnling the ea. lOO kyrecccntricilY cycles can be idcnti ned in Ihi:. pan uf lhe sa:lion (I)inares­

Turell el al. 2003). The lo\\<cr ca. 15 m of lnc overlying ItJ'UfOll

Formalion exhibi's higher \ertical \'ari3liun~ in boIh Ihe rel:nheproportlon' tlfhemipelagie -.cdimenl!> aOO lhe ffl"<luelll.~y oflUrbitlileintCrc31:tliOfl~. Dar\: lO lighl grey colon; dominate lhrough lhe 11IufOn

Fonmuion, bUl lhe basal 2.85 m interval of mllrls and marlslone" hasa characlcri.'li{· red color (Fig, 7) (Schmill el :11. 19(8). The Ail/.gorriLimC'lonc Form:nion has prc\'inlt~ly bcen rcfcrrcd 10 as lhe Danillll

LimeslOoe Formalion (e.g .. Apellani:r et al.

1983). howevCT. :K.'COfding lO lhe guidelinesof the lnlernation31 Commission on

SIr:l1igmphy. lhe n:Hne of formal slr:ttigmphkunil" (i.e.. group. fonnalion) should consi:'>t 01'¡U\ approprialc geogwphic n:lme combinctl

Wilh 'In appropriale leml indiealing lhe kind:md mnk of lhe unil (Bemaola el al. 2009).GeogrJphic name.~ should be t1erived fmm

pcmlanent naluroil or artificial fealure!> near lhe~lr:nigraphic featurc. If a liloologic !con is

:MkIt.'1I lO Inc name ofa lilOOsIr:tligrnphk unilil ~hould be a "imple aOO gencmlly acceptcdlenn Ih:!l indicllll::- lhe predoOlin:1Il1 lilhology

oflhe unil.Cureful e)wlllinulion of lhe Ailt.gorri

Limeslone/ltzunlll r0n1mlion:11 boundary ¡111he

Il:ruron Bcuch :'>CClion and in.lwo :tddilionalscclions in Zumaia IOCalcd closc lo lhe N634

ruad lO San Scha"tian. 00 lhe easlem hank oflhe Urola ri\er moulh (Fig. 2). iOOicates lhallhis lransilioo is elearly conformable. 1llcre i~

no evidcnce for llny erosional gap or omi.-.sioosurface al Ihis 1c\'Cl. Throughoul lhe DanianlSclandian bOllndary inlerval lirncl>Ione-marl

lfllllsilions are alW¡IYs gmtlual :md no evidencefol' hardgrounds or slmtigf:lphic dia,,\cms h:1S

bccn idcnlificd in lhc bcaeh cliff scclion or inother scclions afllund Zumuia. TI1C presenceof 1Urbidilt.~ (only fi\e Ie\'els obser...cd) <loes

TlOl il1volve erosiono since lhey Inol>Ily occur

lIS lhin or \'ery lhin plane layCN (0.5·5 cm) withTc·e 80um3 internal scqucnce~ and baseslacking evidenee of ch:lIlllCIHng or erosiooal

troncalion. Trace fossils. OO/llffiOn Ihrough lhewhole interval. mainly Zoophycos. I'/(moliles,111(1 CIllJlIllrile:'i. show no cvidcnce of

IIlUlClllion. Precise bcd-by-bed corrdlllion ispossible ;lCrosS lhe whole basin noor domain.

e\'en bcl.....ecn scctions 100 km ap3rt. such asSopclana aOO HcOOaia. funhcr iOOicaling loc!; of m3jorunoonformilies

(Bacela 1996: Puj3lte el al. 19983).

Ca/(:areolls IUIIIIIO!OssiJs

1llc exp.1nded n:lIUre ofthe Daniau-$el:tndianlr,msitiun ¡II Zunmia

is cvidel11 from lhe l;r:ldual sequenee offi~l 3ppearances oflhe Iypic:tlt¡t!c¡lrcOUS nunllofo",ib 01' lhe period (Fi~. 8. rrom Bcmaola el al.

2009). For examplc. lhe stnllignlphic di"lancc bctwecn Ihe firslt1ivcrsificalion of ""rl.\'dClffilllllS and Ihe fi~l occurrcnce (FO) (usedin lhe same sense 3S lowest O('currcnce) of ""(UciCflJiIIIflS

t.fmfNmifimlli.f 3l Zomaia io¡ aboul 1I 111. This is ca. 6 m lhicker lhanin lhe !>Cl:'lion al Qreiya in lhe Easlcrn l)eSCfl of Egypl (Moncchi 300

Rcale :!007: RlXlñgucl aOO Aubry 2(07). The e:o:p:lI1dcd fI:Ilurc uflhen.'(.'O«l al Zumai3 i.. 31so apparenl by lhe lhiekncss. 13.6 m. bclwccn

lhe FO uf SpflelU)lirllll.\ l,rilllllS lO lhe FO of F. IYlllfNlllifimllis. lñcb.1:'>C of nannofossil Zime NP5 according to lhe SChclllC 01' Maflini

(1971) i" ddined hy lhe FO of 1': IYllllxlllijtJrmis. which is localcd1.1 111 abo"c Ihe hase of lhc IIzurun FormUlioll, i.e. Ihe h:l"C of Ihe

1Jt'N'llI""r 20/1

115

Chill.mw/itlws I'I/ell//I/1I3, which

marks the base of 5ubzollc NTp7b of

Varol (1989). ca. 10 m below lhe lop

of lhe Aiugoni Limestonc r"Ollllalion

(Schmill el al. 1998: Bemaola el al.

20(9). In sumlllary. lhe scquence uf

ealcarcous nannofossil e\'cnts sho\\ s

Ihm lhe Zum.tia scclion is COlllinuous

o\'er lhe Danian-Sclalldian trnnsiliofl.

This is also confinned by compariloOll

wilh thccalcaR'OUS nannofossil recordofODPSile 12620fLeg208 at Walvis

Ridge (501l1h AlI¡lntic) whcrc an

cX]XllIdcd and conlinllolls Palcoccnc

dcep-sca scquence has been reco\'en.-d

(Agnini el al. 2007: Monechi and

Reale 2(07).

PlonklOl/ic (111(1 belllhic

foramillifera

A

11

The prese..,..alion of for.uuinifern

is mooer'3le in lhe Zumai:l seclion.

hence sorne l:lllOnOmie problcms arisco

Wilh different rescarehcrs using

differcnl 1¡I;wnomic eoncepls 'Ind

di:lgnostic eriteri:l. Problcms in Ihe

ddinilion of planllonie fornminifernl

zonc boundaries in lhe Zum:ai:l scctiOll

have bccn earcfully CvalU:lled by e.g.

Cabnllero (2007) ;md Orlle-Etll.cbama

el al. (2007a). Once Ihesc dcnnilions

are unlangled and agrecd upon.

bouooaries can be placed wilh high

precisiOll. giving strong support foe"

lhe conlinuilY of lhe Zumaia seclion

;Il:ru~s lhe mid-Paleocenc.

B¡lscJ 1m pl;mklonic and bcnlhÍ\,;

fornminifcrn. iSQ(opic and lilhologic

data. Arenillas el al. (2008) h:l\C

localed fh-e signirK.'1Inl c\'cnl horizons

lhal h¡l\'C bren l."()flsidcrcd a~ poIcnlial

(:orrelalion crileria for Ihe DanianlSclnndian bollndary (Fig~. 5 and

9). Thc sequcnce of foml11inifcm c\'ellls ¡¡¡ Zumaia and comparisons

wilh scclions c1scwherc also give support for Ihallhe lomaia SCClion

is continuous and ellpandOO. Levcl HDSI. ca. 13 m below lhe lopof

lhe Aillgoni Limc~looc Forma!ion. is characteri/.cd by increa~... in

ACllfi"ilw. KarrerulillO aOO Slnrot1!t!C/(lmm;'lO. aOO corresponds lO

Ihe lower boundary uf lhe IHom;:tI\·t'lIlI (/118111(/1/1 Zonc; somc aUlhors

formcrly placed lhe Dani¡m/5elandian bollndary al this biohoriwl1.

i.e. allhc P2IP3 zonal boundary (Bcrggren 1994: Berggren el al. 1995:

Sleurbaul el al. 2<XJO). HD52. ca. 9 m bclow the lop of the Ail:lgoni

Limcslonc Funualion. is charnctcri/.oo bY:ln iocrcase in Moro:PI·,.f1aaOO corrcsponds lO the lower boundary ofthe MIJfl1:1II·t!//tI d. lll1Wtlri

Z(me by Arenillas ;md Molina (1997). lllc lowcr bound¡lry of lhe

MOIV;¡ll'elfll (Jcdl/,m Zonc of üTtlc·Elxebarriu el al. (2007b) occun.

ca. 7 m bclow lhe top of lhe Ailzgorri Lirncstonc Fomlation. HDS3.

ca. 7.5 m bclow lhe lop of Ihe AilZgoni Lirne)lone Fonnation. i"

eharaclcril:ed by an incrcasc in Kar"nll;,w :md nwimum \'alues in

1l1JS.l

ItIIS I

Sf.I.ANUl"N

It"turun "'11\.

5cl;lIldi:1I1 (Sehmil7. el ;11. 1995: Bemaoln el al. 2()()1). AnOlhcr

importan! global n:lnnofossil evcnt is :1 major radialioll oC lhe

fasciculilhs. which slans slighlly below Ihe 10p of Ihe AillgOrri

lJmestone r"'Omlalion, v.here lhe Fü of F. Il/ii s.). is recordcd aOO

continues lhrough lhe base of tne Il7.uTtln Formation. where the FOs

oC F. hUm, F. ftmii. F. ¡m·O/llm.f. F. 1)"/IIptl/lifimllÜ and f: pi/(,(l/IIS are

recorcJed (Ikrnnola el al. 2009). This radiation is hcre nal11ed lhe

M:cond mdialion of lhe fascicllJilhs becausc an carlicr r..diation of

slllall Fascicll/illms is recordcd 10.2 m bclow lhe top of lhe Aillgoni

ümc:stone Fonllalion. An imponan! regional e\'cnt is lhe las¡ common

occurrcnce (LeO) (01' lhe eOO of lhe: :lCme) ofme BrtlarudospJ!(/t!m.This genus exhibilS an abTtlpl decline in lhe relalivc aOO absolulc

abundan<.'C in eonncction Wilh lhe shift fmm lhe Ail1.g0ni Limc.\IOIlC

Formalion lO lhe lt1.unU\ Form¡lliofl. Olhcr import.ml nannofossil

evenlS recorded in lhe slrntigr..phic scqucncc al Zumaia includc lhe

fil'!ot r.m: occurrence of NfflChiaslOZJglu '>t't/t!CIUS in lhe uppcm1OS1

parl of lhe Ail:lgorr; Limestone Formalion and Ihe Fü of

Figllrt! 5. I'QtlOramic pllOlOgraplls of 111t! I)(",io" olld /Jalliall·St!follditlll lrallsi/ioll al Zmlloio. rile,-,jtrt!IIU sur/ocn I/DSI lo II0S5 ore discusst!d i" lile tUI olld sllOM'tI in grMltr dewil ¡ti Fig. 9.SurfoCt! 1/054 co"t!spollds to tlft! defillt!d base of tire St!folldioll S/agt. mar/ud by orallgt! atTOM·.

(A) Stratigrapllic poSitjllllS oftlle IlOriUlIls UDS 1 lo 111)55 ill l!le Ilpper block of ti lIorll/tll falllt /llOtoffecb t/¡e f)(I"ioll·Selo"dioll IrtlllSilioll. (lJ) StrOligrapldc pa.~j¡jol/.~ (JJ lile Creltlceo/lsll'tlleogellt!bOlmdory tlI/d tlle IlOriUlllS 11051 fo I/IJS5 ill tlle fOM·t!T block oftlit fallft. 111 (A) ol/d (11), /lolt! lile

rt'pefilioll aftlle IIppt'T lNJllioll st!qut!lICt! OIOllg file sectio" buou$e ofllle foull. f'TOI1I Art'lIi11os t!1 al.(1(}(J8).

E"iwHft'~ \'<1/, J4. 11<).;/

116

Red MlIrI

C26

."

ZUMAIA 5ECTION

n __ •• u __

-"

AitzgorriIimestoneFormation

ItzurunFormation .5

-GSSP--...

./ Clowded F1i membel •/ (¡,

/-..... Aitzgorri lms. Fm

Itzurun Fm: __

m~t-' B" ---...- IIrMified¡ • mem_

... mem_A F2 ....

/ ./,' ...../ Y,l

.... ,••

Figu~ 6. (A) rOlloro"'¡~ ¡'¡ew of lhe Dollioll-Sdalldioll lrrlllsitioll: (B) SY/ltll~lit: sketcll of tlJe IJalliulI-Sdaudioll trrlllsitiollOlltCrop i" tlle /t:urull Beuch, sholll'ing tlfe distriblltiOlf of tlle moill litllOlogical u"itslm~",lHn olld tlle f01l11 sYSltlllS tllal

disrupl t'ft $lfccnsioll. (e) O~tailedIitllOlog ofIh~ IJa"iDlI-Selandian trol/sition, (x) alld (1) "ferellc~ le¡'t/s ill sketcll B alld C.Frofll Baceta el al, (1006) IlfId {lemaola et 01. (1009).

perccnlages of MIIIY!:.JJl'elfll. coinciticl1l wilh II shifl in color of Ihelimcslonc-marl couplcts from greyi~h lO more I'l..-.odi~h. HOS4. whichOCCUI'" al lhe D.1SC of lhe lt7.Uron Formalion. may COI'TC5pond lo lhe

10\locr boundary of lhc IgorillllllllsiJfll Zone. as dcfincd by Arenillasel al. (2(X)8), Ü\her fealurcs flOlOO allhis be! are a slighl dccrease in

Moro:Pl'l'lIa and increases of lrochamminid~aOO S"¡rol'{t'clll",,,,;nll.HOSS. ca, 3 m abovc the base of lhe IlZuron klrmalion, coincideswilh lhe ~hift fmm ~1!>.11 red lo grey Sclandian marls. Minimum valucs

in lhe percenlages of Mnro:(JI'I'lIlI :md maximul11 values for IJlfarillllare rccordcd hcrc.

Benthic foraminifcra givc dClailcd informal ion aboul 'hepalc0b3lhymelry al Zumaia. 1l1e presence or organically t:emcnlcdaOO calcareoos-eemellled agglulinated fOr.lminifern of lhe "nysch

I)'PC" fauna. suggesb a minimum walcrdeplh corro.ponding lO lower·middk: bathyal dcplhs. 1be benthic foraminifcral a~semblage~ al..;ocOlllain abundanllaxa lypical uf dcep oolhyal environmcnb such asHu/i",i,lll IfinilllII'II,\·is. Cibidllf/it!I'.\ hyplw/IH. Cibiddoillcs

I'('/as{'()('ltsis. Gyroidilll)ide,\' f.:/"IHJSIII', SI('luiOI'iIlO be/TlIriifol"mis.

Nlllla/fides Ifllemp,,;. OSllllf.:ll/lIrhl ,'dllS/'Oi'/I.Ús. NlIl/al/i"I'IIl1

flOIl'lI/Ü', GUlIllf)'illll I'yrtllllidllla and Spiropll'ClallllllitW SIH.'c/abifis.

M(KI oflhesc ~pecie~ are l)'pical uf lhe Ve!aSCO-I)'pe fauna (Berurenand AubcTt 1975). Thesc dala Qlpport deplhs of ca. 9(X}.1100 mcten.

or middlc lO lowcr slopc. in agrcemenl wilh Pujallc el al. (1995). In,pilc of lhc sea-leve! falllhal ha!\ becn documcnlcd fur Ihe base oflhe

SclaOOian (M."'C bclow). bcnthic fOrJminifern show no major ch:mgcsin coincidencc with thal!eI·c1. probably bccausc lheir dcep habitat (alhou~ meten¡ dcpth) \loould 001 be affected cven b) a majo!' "Ca­

leve! fall (Arenillas el al, 20(8).

Magneto- ami c)'clostrarigraphy

The Zurnaia .'>CCtion has providcd an unprccooenlcd inlcgr.ll,;.-J

biomagoelo- :lI1d c)'do~lraligr.Jph)' forlhe P-,¡Icoccne (Din~-Turellcl al. 2002. 2003. 2007. 2010), 1l1e M:C1ion now providcs the firsl

complelc aSlronomically derh ed Paleocene chronology \lo here allpolarity chrons nave been eSlablished. rendcring Ihis sect.ion a ma.'ICfreference sc:t:lion. 1l1e oose of lhe Sclandian occurs approximalely at

Ihe 101' uf Ihe lower lhird uf Chrtln C26r. The nexl luwcrmagnclochron. Ihe lap of Chron cnn oecurs ea. 9 m bclow and lhis

chmn sp;.U1.~ cil. 4.S 111 of sccliun (Fig. 8). Thecyclc-duralioll cslirnalC'f\lr lhe cólical dm:lIlO"lones across lhe uppcr Danian and lhe Dani:m­SclaOOian Ir.Ulsilion are lt., follows: C27r (50 preression c)'cles. lOSO

I..yr). cnn (IS prt.'CeSSion cydes. 31S k) r). and C26r (133 prece"sionc)·c1cs. 2793 kyr). 1l1e b:l'iC of lhe luurun Fonnalion jo¡ localed 30

127

Piglfre 7. rile trmlsilif", fmm 'he 1.85 111 Qf red morl.l· to 'he flrst

grey bed.l· ill lile fower parl of file 1tZIIfIIII POflllflfioll. see IIIhi,e

sqllare ill Pig. 4for l1fecise /ocatioll. Ref! bed~' occ/lr /lfJ lo ca. .1.51/1. afler II'hil;/¡ bedslllfll COI/lllfelely grey.

prccession cycles (630 kyr) aboye lhe 10p ofC27n. Precession cycles

can <lIso be useu for ;¡ppro.linl:lle cslilllatcs 01' rcl;llivc limc differcm:;c

belwccn uitTcrcnllilhologic and bioslraligraphic cvents. Forex;¡mplc.

lhe onscl 01' lhe second radial ion 01' Ihe fasciculilhs and lhe FO 01'F. l.rtlll)(fIIiflJrllli.~ oecur res¡x:clivcJy 21 kyr befure alld 84-105 kyr

atier lhe Danian/Sclandian boundary (Bemaolacl al. 20(9). According

lO some gCllcmlized slI":ltigraphic schel11es (e.g.. Berggrcn el ¡ll. 1995.

LUlerbacher el al. 2(04) lhe IOp 01' Chron C27n is cOllsidered lO

coincide wilh lhe pl:lIlklonie foruminifera 1'2/1') 1.0n¡1I bound<lry. i.c.

Ihe levcl where also lhe Dallian/Sclandian boundary has been placed

by convcnlion in lhe pas\. In lhe Zumaia seclion Dinares-Turcll el al.

(2007) place Ihc P21P3 bolllldary ca. 8 111 bclow lhe 10p 01' C2711.

whereas Arenillas el al. (2008) place lhis boundal)' 9 111 higher. Le.

one meler aboye Ihe 10p uf C27n. This discrepancy in foraminifcral

zone bollndaries rcl:lles 10 lhe use 01' ditrerclll !axonomic conecpls

und il1uslrales Ihe general difficulty in placing precise boulldaries

in a graullul. cvolulionary scqllcnce uf l11orphologic¡t1 change

in foraminifera spccies (Caballero 2007: Orue-Elxebarria el al.

2007a).

A robusl Aslrollol11ical Polarity Time Scale (APTS) has bcCIl

conslrucled during lhe lasl lWO decaues. slarling al lhe young elld 01'lhe limc scale aud lhen l110ving progressively dcepcr in time. A recenl

¡1~'hie\'eI1lCnl in Ihis effor! has bccn Ihe completion 01' an a~lronomical

lime scalc for lhe Neogcnc. rcsulting in lhe "Aslronomical1y Tuned

Neogenc Tillle S~'¡j1c" (LollrcllS el :11. 2(04). TlIlling lhe P:tlcogellc

bccomes more cha!1engillg despile new full numerical solmiolls for

lhe Solar Syslcm (V¡¡r¡tdi el ¡jI. 2003: Lusk¡lr el ¡t!. 2()().¡) due \O

limilalions inherent lO lhe Ch:lOlic bchaviour of lhe Solar Syslem ¡¡nd

i

Id'

I

(al OIna.b-Tu.ell el'" 2003(b)loIlowlng Martlnl (1971)(ellollowlng Varol11989)

..J..J FO C. edentulus1st radiation of Fasclcullthus

..J FCO S. primus

..J FCtO S. primus

(e) MAlN BIOEVlONlS

..J fe T. eminens

..J fe T. tovaa

..J FRO S. primusNTph

Nlp8a ..J Fe N. perfectus

N"

f--+.",,~..J fe F. tympanlformis~~Nl ..J-, EA B. bigalowii

2nd radiation of Fasclculithus

~C26r

NP5 NTp9

(a) (b)

-,"

=

--

SAMP. MAGN. IOZOAATIO

.,

IIra1lt1~

member

R~Marl

.,.

."

¡'"mal iltonel

erowdedmembe.

---------·--10

GSSP--Om

ZUMAIA

AitzgorriIimestoneFormation(Danian)

ltzurunFormation +S

(Selandian)

Piglfre 8. llllegmled lititostraligmplty, mflgllelostmligmphy lllld ca/careO/U" I/flflIlOfossil hio.~tmligm/lhyofthe Dal/iull-Seflllldillfl Iral/sition

ofIhe ZUlI/aia sectiol1. l.ocfltioll oft!le maill bioel'ellts ami s)'lIt!lelic dislrihllliUII «lid ohul1I/allce rtll1ges ofSplll.'lIolilhus. Fasciculithus "lid

Branrudosllh::acrlL ¡:O"" First OCCl/rrellCe; FRO"" Fint Rare OccflrreflCe¡ PCtO"" Fint COl/tillllOIIS OCCf/rrel/ce; FCO= First COflllflOIl

OccllrrClIce; EA= ElId ofAcme. From lJemaol« et al. (2009).

UN

Din:u"Cs-Turell el al. (2003) luncd lhe

orbilally driven lilhological Danian bundlesal ZUlllai¡l (lhcir E-cycles) lO lhc Va03_R7cccenlricity SolUlion lurgel (Varoldi el :11.2(03). Tuning was S1artcd by correlating IV.O

consecutive I'rOminenl carbonate-richbundle eycles (E·3S and E-36). al aboul 38m aboye lhe Crelaceuus/Pateogene

boundary. lo respective ceccnlricity cyclcsal a peculiar low-arnpliludc eccelllricilYminima nade in the solution IMgel. which isrclaled to Ihe very long ca. 2.8 1o.1yr

eccentricity modulalion c)'c1c. 1ñc luning

subsequently I'rogrcssed by corrclalingsoccessivc ax.'cntrieilY bundles in lhe scctiolllO succcssive cccenlricilY minim'l. Following

thc lllning. Dinares·Turell cl al. (2003) arriveal an a!lC of 65.830 1o.1a for tl)e CrctaccouslPalcogene boundary. Kuipcr el al. (2008)instcad use an altemalive stralegy of cycle

panem rccognitioo and luning lo lhe lI'IC)re

slable 4OS-kyr long cecentricity cycle and

incorpor.Lle Ihe ul04 solulion (Laskar et al.20(4) as largct. lnfcrcnces fmm lIun1cric¡t1daling c1sewhere led Kuiper al al. (2008) lO

JlffiPOSC two ahemative luning schemes foreach astronomical largel ~olution. The

favorcd one. resulted idenlical lO lhe oneproposcd by Dinares-Turcll el al. (2003) formosl of lhe Danian. tI is only below

eccenlricilY bundlc E-14 (lIl aboUl 17 m

aoove Ihe CrelaC<.'OOslPaleogene bl.lundary).Ihal Ihcy ehoosc tO calibrate 10 one

ecccntricity cycle oldcr. reaching an age uf65.940 Ma for lhe CrelaceousIPaleogeneboundary in lhe Va03_R7 large!. I-lilgen et

al. (20 IU). while maintaining Iheir previollstuning f{lr ZUJll¡li:l. ¡uncnd al sevcral Icvels

Ihe Paleoccne a~lronomical calibralion

_HOS3

_HOS4

_HOS2

_HOS1

_HOSS

Mainforamlnlferal

events(Arenillas el aJ., 2008)

proposcd by Weslerhold el al. (2008) whichis bascd on differem gcochemical dala seIsfrom ODPIlODI) scdimcnls frum diffcrem

oceans and their own interpretalion and

atleml'l 10 correlale 10 Zumaia. In IUrn.Dinares-Turcll el al. (2010) refine Ihe IOp

posilion of Chron C27n (C27n...,,) by integl"oI1ing new magnelo­

straligl"oIphic dala frum Zumaia and lhe Ojala scclion in Bulgaria.C27n,.. is now placed four precession ~'ycles abm e lhe posilionoriginally reponed in Dinartli-Turell cl al. (2003). Dinarts-Turcll et

al. (2010) also rea~~ess lhe a~lronomical luning of Ihe Danian·Scl,lfldlan lnmsiliunal imerval in lhe liglll (lf lhe exprcssion uf Ihe405-kyr ~'Ccentricily cyclc bolh in Ihe hll1d-b:1SCd scclions and for

IODP Sile 1262. They provide a consislenl corrclalion of lhevarioll~ d:lla seIs thal challenge the prcvious inlerprclalion ofWeslerhold el al. (2008). A1> for the posilion of the basal Sclandian

GSSP at Zumaia il is kx:aled 30 I'recession cycles aboye C27n"", (ca.630 kyr) and can be a....~igncd an age of 61.641 ±O.o·m Ma un Ihe

La04 aslrunomicallargcl Solulion (scc Dinarh-Turcll el al. 2010. forfurther dClails).

'5

-15

.,.

Red Mari

greymarlstones

-5

straliliedmember

GSSP--Om

AitzgorrilimestoneFormation(Danian)

ItzurunFormation

(Selandian)

ZUMAIA SECTION

C27r

C26r

JXlOr radiui~olOllic agc control in the Paleocene in addilion lOuoccnainlies in lhe absolulc numerical age of lhe monilor slandafds

u'\Cd for lhe radioisOIopic daling mcthods (Kuiper el al. 2008).J-1ov.c\'er. aslronomicalluning bascd on lhe slable4(}.¡-kyreccenlricity

eycle b apl'ropriatc (WcMcrhold el al. 2008) :md should be Ihe finit­order apl'roach lO rc;lch <1 consiSlenl P,llcoccnc luncd chronology.Ahhollgh precise orbilal solutions fOl" ~horlcr cycles are lacking. a

~lIilable approach is lO eslablish an imegralcd rnagnCIO!olmtigraphicand orbital Iy charnclcri7.t.'d tcmlllalc (i .C. e)'cle-dul"oIlion estimalcs an<!

main phase relalionshiJK) in a gh·en SUCCCSSloll. E\en if dcfioilivcluning to ao orbital solution (an<! Ihcrefore "absoIUlc" age eslimales)1ll;ly be provisional. lhe lime duration and role of I'roces~es (i.e.

biologicaL p.1lcuclimmic ClC.) <lre rcadily cXlrilcted. MOTCover. lhepolclItial for 1,;10001 corrclaliOll i~ amply faÓlilaled.

Figllre 9. Ihtai/~d 1il11OIogicnllognaos! I¡'~ D(",inll·~/nlfdi11l1lronsition oft¡'~ Zmnaia s«IiOll14'¡¡1I positioll of rtft'rt1u:~ 'IOriZOllS IIDSJ lo IIDS5 (Ar~Il;lIa.t ~t al. 1(08). T"~se 'IOrizoft$ ared¡scllss~d ;1/ t¡'~ maill text (lIId SllOl4'lI il/ Fig. S. SlIrface JlJJS4 corrt'sp(mds /0 tllt bus~ of t"~Se/al/dial/. A!agl1clostrmi¡:rl1flJiy from JJinare.f·1ilrc/J et fI/. (2tJ03).

On-rmbrr 2011

129

BASIN SLOPE PLATFORM PLATFORMMARGIN INTERIOR

Zumaia Ermua Unanu liZa.aga Korresf f f f -,/'-

E P6a I,L-21 ~ ~SBZ.

O lLER- NP10 SBZ5e OtAN 24,

1I'L-11._.- ...._..

T P5IT~-21 SBZ4

H NP9ANE E 1- ~

T u. UJI ~

I c:_.

SBZ3A ::l ~

N ~ • ~ -::l .s::; tip

j 1::: 1-

A..Vl YkY YkY

L SElAN- TY TYCVoN NP5 1-

E UJ!'~~ 26, -'

O

re ~ ~

P3aE E

~ ~

N u. Da-2 ~

E o J!l ~ SBZ2A E

~

P1cN ...JI .¡:A ~

$N o ~

Ol ~

l:JP1b . r ~

~ ,,-,•••

IMa~DalSBZ1-....... ......... 29r ........... .............. . .........................

e MR , AE t A tT e S. t

1t DEPOSITIONAL SEQUENCES tL1THOSTRATIGRAPHY Shallow Benthic

Zonesmagnetostratigraphy I l:eófcalcareous nannofossils HIATUS

I I KIPplanktic foraminifers bowd¡,ry dIIy

Shallow marine deposits

eulochlonous

~ (hemi)pelagicliiiiiiiI IImeatones_

marls&marlstone

[ .... lreefa'oonstructions

lYfiIí deepL.rr..J karstificatlon

~ paleosoits

niouter platform limestonesc.::IJ ("shoals· & bioclastic accumulations)

¡¡:r:::::;q inner platform Iimestone/dolostonese:a (tagoon & tidal flals)

F""""'l snallow marine siliciclasticsL..J (beach. delta and open platform)

Slope and basín deposits

resedimented

~ síliciclastict==J turbiditesr---I calcareous~ turbidites1.,...1oonglomerates

3. breccias

Figure 10. B;oc//rfJllostrotigrop1lit;. lromU'ork 01 the PoJeoctllt to 1014'tr )j:m·s;olf (rtgio/lol JltrdiDlI) )'IlI;'USSiOll 01 the SW Pyrtlltes,sllol4';ng dtpositio/laf sequellcn and ma;" facits, Age datillg of tlle sequellcn based 0/1 plat/orm margil/. sJope alld basil/al stc!ialls, Far

{ocotiol' 01rtftrtnu SUljons. set Fig. J. Modifitd from BaUla ~I o/. (2J)()4).

]JO

Cllrboll isotope strlltigmphy

A detaile<! carbon iSOlOpe slraligraphy has becn established

lhrough lhe cmire PalL'otenc scction al Zumaia bascd on bull rocl...amples (Schmill. el al. 1997a, 1998). Thi, i~opic rerord show'i

lhe samc gencr.d a"c lrcnd as rerords measun.'d in .....ell-presel"\'e<!

ocoe¡>-.'>Ca malerial. such a.<¡ al o...'Cp Sea Drilling l>rojeet Silo.' 577. Thechar.lclcrislic global l"le Pakoccnc auc maximulIl (Corfield 1994:

WC'lerhold el :11. 2()11) is ""'0.'11 rcpre.'iClI1cd al Zunmia. Two m:tior andlWo minor negalivc al lC shirls are rcgislcred. '11C lWO rmtior ~hifls

(> l'ir,) are siwatcd ni lhe CrewccousWalcogene and Paleocencl

Eocenc OOund:lrics. The 1.....0 ll1inor shifls « 1'ifd are localed ncar IhcIOp of lhe Aill.gorri Limcslonc FOmla[ion and in lhe basal Ill.uRlIlFormalion.1llc fir-;t t.....o anomalies ha\'c also been fouOO in m:my

other scctions orld\\ ide, whereas il has becn generally diffieuh lOreproduce lhe [ 0 other anom:lIies dsev.here. For example. lhe

conlinuous mid·Paloocenc record al Deep Sea Drilling Projecl SilC384 in lhe north""~1 Atlanlic (Berggren el al. 2000) does not show aelear negative allc spike similar lO lhe one obscr...ed by Schmil" elal. (1997... I99K) al the base of the Selandinn :11 Zumaia. Al boIh

loculilies. howe\lcr. Ihe inO..-..:lion poim of lhe iocrcase in aPc lhatellelllu:llly cu!min:llcs in lhe unusually high ól'C lI:llues during lhe

long-lenn lale P:llcocene Ól'C maximum. occurs IICry close lO lheboundary bclween calcareous nannofossil zoncs NP4 :lnd NP5. ThisfC:llUre can ¡¡pparenlly be uscd iU lCllSI for fir.;l-order corrcl:llions

bel\\'ccn differenl sile~. We!>lerhold elul. (2011) in a carboll iSOlopcfC(.'ürd forllle Palcoccne fmm Ihe cclllrall'acific, shuw sm.all ncglllivc

anomalic.~ Ihul may c~poOO lO lhe smallcr anomalies al Zumaia,1be shon-lenn negmi\e spike in a r'c althe base oflhe Sclandian

al Zumaia mayal le:I!>1 ¡X1I11y be relaled lO IOClll fealures 3!osociale<!wilh lhe prominclll sea-lC\'cI fall at Ihis c\'cnl (see laler scclion). 11 is

clear tllal in surface waters ihere is a grndicnllowards more negalin~

al'c values landward bI,o(:ause of an incre;tsing comribUlion of lao<l­

deri\ixl organic dclnlUs. A.'>Ca-lcvel fall may ha\'e shiflOO lhe t.'OOsllilledosel' lo Zumaia. 1ñc small (ca. Q,7'1r.) ncgali\'c óflC :momaly of,hoft dUrJlion lhal occurs al ca. 10 m bclow Ihc base of lhc Ilzunm

Fonn;llion (Schmitz el ¡jI. 1997a). in lhe lowcr I)llrl of Chron C26r:lIld al HDS2 in Figs. 5 alld 9. may be corrclaled lo lhe Latesl Daniiln

Evcnl as obsen·t.-d in EgYPl (Bomemann el al. 2009: Sprong el al.2(09) :lnd the Indi,rn Occ:m (Quillévéré el al. 2002: Bomcmann Clal. 2009).

Seqllellt:e straligrapllJ

1ñe dce¡>-walcr Zumaia emDa)ment wa.~ bordcrcd by shatlo",,­waler arcas in v.hich a 3(X).-SOO m Ihick carbonale M.lcrcs.~ion was

formed by the \·enical slad.:ing of conSl.."Culi\e carbonale plalfonm(Fig. 3). Dc\dopmCnl of Ihis carbonate slIccession was puoclllaled

by !>Ca-Ievel lowcring.\ or al leu~l regional cXlent. during ""'hich lheplmfonll IOp was I>uh¡¡criully exlXJSed. plnlform growlh (·ca..;cd andeXlensivc discominuily surfaces werc cn::lled (Ihcela 1996: Bacela

el al. 200 l. 2007). During lhe Paleocelle-early Ypresian interv,ll sixI,uch drops h,l\lc bccn idenlili..-d. Ihe inherenl disconlinuilies llallingbccn u-.ed 10 ~ulxIillidc lhe SlICcc.<¡sion into dcposilional M:quen(:cs.

codcd according lO lheir age (Fig. 10: Pujahe el al. 2000: Bacela elal. 200... 2007). Thc mosl prominem of lhcse discominuilics. lhe so­""31100 Mid-PaICOt.ocne UnconformilY (Bacela cl al. 2001), marks lhe

base of lhe Se/lñ-I l>ctJuence. h was crealoo dllnng a long-Ia."'ingpcriod of 10\\ sea lc\"C1 (of ca_ 2.5 1l.lyr acoording 10 bioslraligraphic

conslrainls. sce Bacela el al. 2005) lhal Inggcrcd large cl\»ional

collapses oflhe uppcr Danian slopcs aOO shclf margins aOO pronlpledlhe deep karo¡lirlCalÍon of lhe c'(poe.ed plalform carbonales acros.'( lhe""hule Pyrencan hasin margin (Baceta cl al. 2001. 2004. 2(07), TIlo.:basal Sclandian llerc rcpresenls Ihe corrclali\'e conformilY in lhebaJ.inal succesl>ion Oflhis major ullConfonnilY idcotilied in lheshallow

plalform areas. According lO .1 dctailcd .'ilrJligr.lphic reconslntetionof Ihe shelf margin arca cropping OUI in lhe Urbal>a-Andia platc:lU:lIla Ihrough lhe UM: of dcplh-indic:rling key focics bclow lrnd :roo\'e

Ihc Mid-Paleoccnc UnconrorrnilY il has been eSlim:ued lhm in lhePyrene,.n b,lsin lhe minilll:lI LJI,lgniwde lIf Ihe sea-Ie\'el fall of lhe

Danian-Selandian lrJnsilion was belwccn 80·90 m. The origin of lhispromincnl sea-b'c1 drop is still uoceT1ain bUI il mainly seems lO berelatoo lO a major Icctonic invcrsion across lhe inlerioroflhe Eumpcan

plale (Nicll>Cn el al. 2005), presumably lin"ed lO uplifl of lhe NonhAllanlic lilhosphere by the ke1and plume (White aOO I...o.....ell 1997).

The GSSP ror the Thanetian - position,stratigraphy and completeness

Precise posi(iol/

Thc hase of Ihe Th:lnclion Sl,¡gc. lhe Ihird or upper slagc in lhe

Paleocene Serie.s. is placed in lhe seclion al IlluRln Be:lCh in ZUlmLia:11 u level 2.8 III aoo\'c lhe base of Ihe core of lhe dislinCI clay.richinlef'\'al 3ssocialcd wilh lhe Mid-P:lleocene 8iOlic Evcnl (MPHE)(Figs. 11-15). 11.... base of lhe Thanelian oorresponds 10 lhe base of

magOClochron C26n (Le., C26rJC26n re\·crsall in !he scclion (Dinares­Turell el :11. 20(7). h also correspoods lO lhe 1c\el eighl pn:cession

cycles abO\e lhe oo.'Ie of the l"Ore of lhe MPBE (Figs. 11·15). :ln

c\'ent eharacterized by imporlanl cakareous nannofossil andrornminifcr asscmblagechanges (Bemaola el al. 2007: Din:lres-Turellet al. 2(07). l1lC base of ¡he Thallelian occurs ca. 29 m aoo"c lhe

base of lhe Selandian. and ca. 78 m aho\'c Ihe Cretat.'COU!JPaleogcnc

oound:iry.

Li(IIOS(mi ig raphy

The Illurun Fonnalion lhal sp:ln~ lhe entire Selandi:1lI :mdcontinues IIp Ihrough lhe lower Thanelian. shows highcr \eT1ical

varialion~ in boIh lhe rclali\'e proponion of hemipclagic sedimcnlSaOO ¡he amounl oflorbidile inlerealalioo!> l'Unlpared lO lhe undcrtyingAitzgoni LilllC!>IOOC Fonnalion (Baceta el al. 2006). Thc Io\\cr par!

of!he hl.uRln Fonnalion can be dh·ided in a 10wCf. ca. 24 111 thick.(infomlul) Mcmbcr A. and an upper. ca. 52 m lhick Membcr B (Fig.13). Membcr A is largely dominal..-d by mar[s. whereas Mcmlx.-r B

includes signifit.'anl proponion!> ofindurJlOO limeslone. Thc bouOO:lrybclwccn lhe two Illembcrs h3.'( bccn csl:lblishcd arbilrJrily allhe poilll

in which lirncslone bcds rcach lUId rnairn:lin CaCO] \'alues higherlhan 6O%.l1ii~ bound:lry is silualcd C:I. 6.5 m bclow lhe delined baseof lhe Thanelian. On a larger scale, IHembcrs A und 13 or Ihe lll.unm

Fonnalion rcconl a pmgrcssh'c increase in CaCO" after lhe :ibn.pldccreasc lhal Chal".lClcri1.cS lhe lowcr boundary or lhe ronnation. 'Tñe

CaCo, increaM: culrninales in lile upperpan of Membcr B .....ilh lIaluessimilar lO lhose of Ihe Aill.gorri Limel>IOne Formalion. Thecomposilion Oflhe limcstones in lhe It,..urun r-onnation is mlherl>imilarlO !hose in lhe underlying Aitzgorri Limcslone Formalion (mkritic

mud.~lone-w:lCl~loncwilh plan"looic for:ullinifera). bul occasionally

lJl

f"igl/re JI. "osit;oll of tlle bose of tlle TflOllr.tiall Slage 01 /tUlnlll Hr.ach. TI/e rdOliollship of Ihe

GSSP rdolil'r. to lI/oglle'oslraligraphy olld 1il1lOlogy;s empllOsi:J'd. Mogm'loslraligrapl,y occordil/glo O;'lOns·Tflrell et al. (2(}(}7).

pn.-dominalllly of silicicla1>lic nalUrc.

'" hercil.-~ in Mcmbcr B. whlch show, a

higher ntllubcr. (hcy are u'ually of

~ilicicla~lic 01" mixcd carbonalic·

,ilieiclaslic nalUre. Thc carbonale

grains mainl) COlTCSpond lO abr.KlcdteslS of planLlOnic foraminifera. Aboul

lhrce melcrs abo\e lhe limil bcly,een

the mcmbers A aOO B of the Itzurun

Form:alion. Ihc!\" il> a promincnl danca. I m thiek inlenal TC('or¡Jing a

drll,lic de~'rease in CaCO, :1111.1rel:uh'ely high \alues in tll<lgnclic

~u~ccplibility. This e1<lY inlcr\al i~

illlerpreled n~ lhe cxpre,sion of lhe

Mid·Palcoccne Simil: Evclll (Benlllola

el al. 2007).

Ca/C(II,(,oll,\' 1/{//lIlofossils

MPBE core

1

TIle ~(raligraphic internll spanning

lhe Sclandian Slage and the Sclandianl

Thancli:ln boundary i~ chameteril.c¡J

by u ~moolhly e\ohing succc"ion of

cakan.--ous nanoofossils (Figs. 13 and

ISI. similar 10 m:onJs in apparently

CJlpanded aOO eonlinuous 'llCCCS~ion"

ehewhere, "ueh al> in the deep M:a(Bernaola and Nuño-Arana 2006:

Din:u'Cs-Turell et al. 2007: 8emaola

el al. 2009), Closc to lhe boundary

bclwccn lIle bal>al 2.85 rn of red marl aOO (Ile o\'crlying grey marl

bcds (Membcr A) in lhe 100·\cr pan of lhe Ill.urun Formalion. oc'Cu.....

a slighl dccrease in 100al abundancc of eakarcous nannofossils. bol

no olher significanl change il> rccordcd. TIlC c;lIcan.--ou~ n;lI1nofo~~il

a,scmblage l1Cm~s lhe grey nmrl";[onel> (Member A) of lhe 11Iunm

Form:llion ¡,., ~irnilar lO llml foun¡J in ¡he Llndcrlying red marl and i~

I11llinly dOll1inaled by Co<:eulirIIllJ pel(j~iCIl.l", I'rillsills mlll'lillii, f~

C26n/C26r

1•

C25r/C26n

1i

lhey also contain minor amounts of ,ilHizcd qU:lnl. aOO gl:llIconile,

lhilo laller as sub-mm gmins and infillings of Ihe for.l.Ininifeml lesb

(Bllcel:1 el al. 2006).1lle lt7.urun Formalion rccords a progrcs1>ive

change from iIIile-rich lO il1ite/smeelite·rieh clays. Trace fossils.

dorninaled by 2ooph)'cO.f. are common, Thc ItI.UI\1Il Forlll<ltion differs

froll11hc Ail~gorri LimcslOlle Fonnmioll ;llso in lhe amOUlll and lypc

uf lurbidilc intercalalions. In lllc marly Member A (hcy are

"iXl/re 12. Posiliofl ofmagllewclmJIIs C26r, C2611 (///(/ C25r ill relfltiOlllo lilfw/og) i/l the '/meta ~'eclioll, II cO/J'I'lemellfMJ' referel/<'e sce/iu"

for fIIt1gl/f!I(J.~1rll1igrnp/'yUCr(J.\·,~ IlIc SclOlllfilll/-1'Jllllll!lioll IrnllsiliOIl. Maf,:lIc/(wrtlligrtl/llly f1CCO/'{!iIlf,: tu lJimtres·1ilrcll el 111, (2007).

1:."',i.~()(JI'.' Vol. J4. ,ro. 4

2Jl

Plo"klOIl;C foram;llifera

kle¡III't'IIi, 8oll/o/iIl/l1,'i COIlicll,f alld Di.\T/J/I.\'ll'r

bml/llellei. al110ng Olhers are also recorued(lkmaola and Nuño-Arnna 2006). 1l1c baseor Zone NPó. nl:Jrked by Ihe FO of lf.

klt';"pt'1Ii occu~ ca. 22 m abO\e lhe base oflhe Selandian Stagc and ca. 6.5 ni belo..... lhebases of Chron C26n :md lhe Thanelian Slagc(Dinares·Turell el al. 2007).

NP5

NP7

NP6

NP4

NP8

1--

1--

1--

P4

P3a

(e) (d) (e)

."2 P3b'"..J

f-'"

No significan! ehangc in lhe planklonicfor.uniniferal 'Iswcialion has bt."'Cn obscrved:Icross Ihe b;lse of Ihe Thaneli;lll slage.Ho.....el·cr. al Ihe onsel of Ihc Mid-PalcoceneBiOl:ic E\'(~nl. 2.8 m below Ihe base of lheThanelian. Ihere is a dC{;rease in bolh lheproportion of Ihe planklonic [oraminiferarcblh'c lO Ihe lolal fornminifern asscmbl:lgc(pl:mlaonic + bcmhic) and in lhe nUl11bcr 01'planklonic spccies. Al lhe gencric Je"ellhcreis an increase in the proponion or /g(}rino. anda dccrcase in !he relali\'e abundanccorall OIhcr!'>pcl·ies. 1ñc lo .....esl fl.'lalh'c propon ion ofplanklOnie fonllllinifcra ¡lIld Ihc minimumnumbcr of spccies occur in lhe uppcr p:1rt oflhe Mid-Paleocenc Biolic Evcnl inlcrval."here mosl oflhe spccimens prescrvcd belonglO lhc S,lbbmi,w genus. Thcs<: l-hangc~.

howcvcr. were Ir.msienl. a.. a relum lO lheeonl!ilion.. lhal prev:Jilcd before lhe Mid­P"It.'OCcne Biolic Evcnl is obscrved aboye lhcevenl. A nOliccable decrease in Ihc proportionof morozovcllids across lhe Danian1Selandianbuundary. frum 20-25'l of lhe lolala,'ltCmblage in lhe Danian samplcs. 10 1(Yl, Of

les~ in lhe ScI:lIldian ~mllples .....a.. reponcd byOrue-Elxebarria cl al. (2007b: 2010). Oruc­Elxcbarria Cl al. (2010) funhcr documcmcd:lIlrogresshe bUI syslcmalie ehllnge in lheeoiling direetion of MtJro:'QI'~1I0 ocdustl.

whieh evoh'es from having approxim:ucly50% sini~tr;Jl ..nd dcxlr,¡1 individuals in Dani;lllsamples lO bccoming progressivcly domimlledby a dexlral populalion i!llhe lowcr fcw loclc!"of the Selandian succC'.ssion. so Ihal 10 mabo,·c lhe base of lhe llzuron Fonnalion ca.80% of lhe les!.'> show a predominanl deXIr:lIcoiling. The FO of I,lIl1ril1a allw/lri. m¡lrker ofZone P3b by Bcrggrcn and Pearson (2005).

occun. e:l. 10 m :Jbo\'c Ihc base of lhe h:zurnn Fonnalion (Fig. 13)

according lO Arenillas and Malina (2000) and Orue-Etxebarria CI al.(2007a). The lowcrboundary oflhe Zone N by Ikrggren and Pcaf"<OO(2005). markcd by lhe FOof GIQ/)a,IOllll,fil,(j p~elld(}/II~Iltmlii.lXcurs

c.,. 16 m aboYe lhe base of lhc It/urun FOrtll:llion aecording lO Ome­ElxcbalTia el al. (2oo7a). Inlhe loVo'cr pan 01' lhe Zone 1'4 lllere i":lnincrease in planklonic forJminifera din:rsilY. e..pccially in acarininidsand globanorna1inids. Arenillas and Molin., (2000) ~uggeslcd lhallhe luwer boundary or!he Zone P-I •Of ÚJterbtlCh~ri(jpSf'lldOlIlt'l1tmlii

C27n

C26n

(b)

~

."NU

~

<DNU

(a)

-e: __ l H. ridielli

" pusilfa~S.primus

.--.J /. e/beari

...-J M. velascoensisM. occJusa

......-J F. tympaniformis

~ N. perfectus

"

."

40 ;1

""1=""'=

.10 1fI

l'm

E-cycle ---,

"m

'll G/. pseudomenardii

" 1---'- +-'15~

~~ 1'='T-."mClllbcr A 31

"00-

"¡¡ f--;:'--

'""s::!J...--••.•• --- ·unxl mar! :üGSSpom~

"

:zs~

"'--_..._---~'"

20~..,

AitzgorriFonnalion

ItzunmFOnnalion

r-­/

M. engulata

Hgun /J. lmegrotetf IitllOstrotigrapIJJ'. bioslrotigrop¡'y a"d lIIaglltlostratigrapllY oflhe ",id·Po/tocellt! ollht Zumaia su,ion. (A) lIIai" calcaruJIIs planklolf bjtn¡"ellts. (8) Magllttic:polarit)' stratigraphy. (e) PIÚllktOllit: fOMl1li/lifero bitr.•OIlQtioll. (D) Hio:tJllolil", of Buggrtllel ul. (/995). (E) Ca/cureoas "al/llOfo.~si/ biozlll/{ltioll. Bioslratigrapllic tl'tJllIJ represellf ftrstQCCllrrCllce.f. "rQlII IJflreta el (/1. (1006) al/d IJillflre.f·Tllrell el al. (2007).

hif{'/Il1u lUid TlJlrriu.1 fi'rrlu.olS. 1be mosl importanl change in Ihel'alcareou~ nannoros.~il assembla!,!cs 3CnKS lhe A and B nlcmbers oflhe hzurnn Formation i... lhe occurrencc and di\'c~ificalion or lIJegenus Hrfio/itlm.1 and lhe (irsl Ol,:l;urrenct' of Ihe genus Di.'icooster.

onc of lhe nllJsl importanl ca1carcous nannofossil grou]l" providingnumcrous bio~lnlligml)hic l11:Jrkers Ihroughoullhe Paleogenc. Acrosslhe uppcr A and l<Mer B I'1'leIllDeN of lhe h/urun r"OfTllalion Ihe r"Ús

or Coromx:"c1I1.1 nile.1crfl.1. Zrgooiscus brmnll'fft'i. TUlI'riln emillens,

lfrliolitll1u clmll,brillr. Spllenolillllu onorrtJl1/lS. Heli"fillws

f)er"m}¡a 2UII

133

Zumaia-Itzurun section Ibaeta section

Inclination

·90 O 90(degrees)

•NO

l'r"

'.

1 ;

• .

lN....

•NO

'" ""(degrees)

lITHOlOGY

l~imCSlone!urbidite

Declinalion

.-r;;-'¡.. u ...... - -'1

6ll'~.,~

7,;;"...........-::"'66 t:.n.......- _ $--'

" '..... GSSP --:" J ••: M

.:¡; 6J_____ .:~ 61

n)~

;-~.

· .. · ..... ····7¡j~

n .

E-eycle '.4­" .4)::'

"

Inclinalionu. TU.,"" I~ U.....

•

•:» :: ::::,¡ . :.

• I" ,J¡ .:llll~

'U 'Vu,

•

".~.

•""""" ~..."" •" o."•k.f•, ,• ,,•,•,

'N ..... GSSP

·90 , 90(degrees) (degrees)

"

.~

• samples

Declination

"'""'""

"

"""""

"E;F="'¡;;;;¡-

70~

"".~~

6ll~~

67,1-

•66 7C­_Ir65 j=.--,-

M

Figure 14. Dedillalioll alld ¡/ldillalioll of lile dwmelCristie remUl/e"t II/agl/etiu¡tioll (ChRM) eIJlllfJ(JIIe"t.~ al/d JilJlOlugie lug.l' fur Ihe

Zlllllaia-flzurllII (/lId Ibaeta seeliol/s. Ded;/Il/t;uII.IIor the ZUII/ail/ seelifm IWI'e been IlIIrolated b)' lO". Opell eirele:> dellole llllre!iable dalaalld eroue.~ mark lile f}fJ.~ilioll of wllll/Jfes II/(/t ¡¡nJl'ided /10 dala. The PO:>i/;OIl of bOl/¡ GSSl's, of CllrulI C1611 allll tOrrelMiol/ bel'Weell lile:>ect;IJ/I.~ l/re SIIllIl'II. MI'UE deuotes lile Mid-I'u/coec/le lJiolic Erenl (lJerl/l/ola el (If. 1006) l/mi da.~IIedUnes eorrelale SOl/U! (U.I·tillct rclatil'ely

ll¡iek carbo/late beds. NUlllberil/g oflile eccelltricity (110 kyr) re/ated E·e)'clesfo//oM's Ilumberillg for IIl/(lerlyillg Slmla/ltal slarls abol'e lileCreluceoll.I·!I'aletJgelle bmllldary a.~ reportel/ by Dillares-Tllre/l el al. (1003). N/lmberillg of 'he carbol/(lIe layers frol/l lile Jm.l'le col/pfels orIJrece.I·.I'iml I'-cycles arbitmrily sWrl~' lit tite MPlJE el'c/u (jrulII /JillarC,~-Tllre/l el n/. 1010, .I·/iglilfy IIIQ(fijic(I).

Epis/K/O' \',,/. 3-1. "0.-1

234

D. multiradiatus

C26n

~A. soldadoensis

; F3

~mJ H. riedelli

ID]

1El~

C25n

67 ~.e;;;;;;;;;;~

~~I¡==-----ESSP66 .165

64

73

72

71

81

?­80

?­79

?­78

?- m-77 ..!

?-~.~~76 ~

? - w-'-]¡¡¡¡¡¡¡¡75 _, .:- d3~'

74

l25~-'70 ;

?

~

'"NU

i ..

C26n

~ H. kleinpel/i

~ l. albeari

_ MPBE

...-J F. tympaniformis

lIlE GSSP 2nd radiationi .... of FasciculithusLeO Braarudosphaera

~ N. pertee/us

G/. pseudomenardii

~

]1m

nKllre 15, MaglleuJslraligrap/¡J', lIIai" lIiQslraligrapllie CI'CIIIS, lil/IO/ogy olld C)'cffJ,~traligrafJllyocros,~ lile mid'/'ll/eocelle ill lile Zml/llia

.veclillll. MI'UF: flelloles tlle Mid·/'u/eoce"e Bia/;c El'elll. Nf//llherillg oItlle eccell/riÓ/y (cu. l/O k)'r) refflled E-C)'c1e,\1o/loll's I/II/11beriugIor

IlIIf/er/)'illg ~'tm/ll t/IlII.I'/lIm· abol'e lile Crelaceomll'aleflgelle btllllldllry, relJOrled by f);ulIres-1itre1l ellll. (2003). Nlllllbcrillg o/tlle cllrbuml/e

Ill)'er~' Imm lile bus;c c(JllfJlel,~ 01 precessioll P.C)'c1es urbilrori/)' slart~· al/hc MPIJE. Uioslmtigmpllic el'ems represelll first OCCl/rrel/ce.\·

(FO~'J, Qtlierwise IlIey are illdieatelf m; fir~'t eOII1lIIf)1I (¡cel/rreuces (FCOs),firsl rare oeel/rrellce (FRo.~) Ilr /1l.1't COJIIIIIOII oeCllrrellces (LeOs).

From Dillllres·1ilref/ el al. (2007).

1Je<'t'mlH'f 201/

Znoe of Arenillas aOO Molina (1997) - shoukl be placcd close lO lhe

C26r1C26n boundary al l'.umaia.

Magneto- afUl cydosrratigraphy

Thc precise pOSilioll and dur:llion of Chron C26n has been

eSlablished by delailed p:lll'Ol1lugnetic work in lhe ZUl11aia seclion.und confirnlcd by complemcnt:lry work in lhe Ile:lrby lbacla seclion(Figs. 11-15) toinares-Turell el al. 2(07). The magneloslraligrJphy

ha~ been linlt.'t.!IO delaile<! cycloslraligraphy providing an cxcellcnlAS!f()flOmical Polarily Time Seale. The cyde..tfuralion ~Iimales for

Ihe mid-Paleoccne crilical chronozones whcre Ihe Sclandian­Thanelian lran~ilion oceUD are as follows: C26r (133 precessionC)'cles. 2793 kyr), C26n (11 prcccssion cycles, 231 tyr) aOO C25r

(69 prece.<¡sion cycles, 1449 kyrl, The base 01' lhe Th:melian SllIgc is

105 Im:ees~ion cycles above lhe b.1se 01' lhe Sehllldian Stage, whichindicales a lol¡i1 dllralion 01' 21 03 kyr 1'01' lhe Selandian Slage, Thercis no dislincl lilhological ch:lnge (e.g., in carbonate col11em orlurbidile

abundancc) or nOliceablc biologic,ll change in connCClion Wilh lheChron C26rlC26n re\'crsal. bullhe Ie\'d can be localoo and OO~I:lI(,-d

toolhcr basin~by refeTCIlCC lO lhe distincl Mid·P'Jlcoccne BiOlic E\'cnl(sec belo",,),

Cm'bon isotope sIrarigraphy

The b..1!>C ofChron C26roccurs in abollllhc middle oflhe imerval

wherc whule-roek I)"C values gradually increase lowartls l11axilll\llllvullles in the I:lte P¡¡k-ocenc. 11lere i,s no I)I'C annmaly as~ocialcd

wilh lhe b:lllC 01' Ihe Thanelian. In lhe clayey interval corrcspondin,g

lO lhe Mid-Palctx-cnc BiOlic Evenl. in addilion 10 a JO<.i. dttrcase incarbonale conlenl. a 1'1. negali\'c ólJC shifl is rcpont.'t.! by Bcmaola

el al. (2007). howc\cr. such iSOlnpie shiflS asS(x.-ialed wilh a ehangc

fmm limcslone lO mar! may not ncc~ly ref1ee1 originallrcOOs.lKx-ause diagelk:lic mincrab can fonn in thc sof! marls (Sehmilz el al.1997a). In lhe Zumaia scclion rcliable iSOlopic re.~uh;, can primanly

be rclriC\'OO from Ihe lime.~tonc bl.--ds. The...e bcd~ werc lilhified dllringeMly diagcnc,i, which rcslrictcd lhe eltclmnge of iSOlOpcS withpcrcolaling pore wlllers.

Seqllence srmrigraphy

According lO gcncrJI and dt..1ailed com.-Ialions carried out bcIwcen

basinaL slope and platform successions in thc wC"lcm Pyrencan basin(Bacela 1996: Pl.Ijalte el al. 1998a.b: Baceta el al. 2Ol).f, 20(5). lheTh11lClian GSSP occurs wilhin lhe IrJns~hc sy~lcms lrael (TST)

of depo~ilional sequcnee Scffh-l (Fig. 10). This ~yslems lmcl isrnarked al platfornl margin sellLngS by lhe onlap of shallow marine

uppcr Selandian :IIlU Thanclian ,'Irala onto lhe renwrkable Mid·Pale<x:ene Uncnnfonnily c:lpping lhe shclf Danian carbonale.s, lhu,n:cording Ihe progrcssivc marine re-nooding of lhe extensh'e 11:\1­10Ppcd Danian plalforms afler Ihc sea-Ievel drop al lhe Dani:m·Selandian lransilion (Pujalte el al. 1998a: 2000). This regional

renooding JlfOCOS i, rn'Ol'dcd in lhe ba~inal 'lICces~ionoflhe IlzunmNlrmalion by a progres;,i\e bul relalhely rapld \·CTtic-JI increase in

lhe calcite conlenl of bolh limcslones and marls. lhe apparilion andiocrease 01' aUlhigenic glaut.-onile.inlilled forJllIiniferJllesls :md lhe

apparilion of ca1caJ1,,'Ou~lurbidiles etllllaining plalfonll-derived fossils;j('ross lhe 10 Illlhick illlerv:t1lhal in lhc Zumaia scclion encompasses

lhe Mitl·Palcocene Bel1lhic Evem (see below) and lhe magnelochron

""¡Hwtks \iN. J4, ¡¡(J. 4

2Jj

C26n (Bacela 1996: Pujahe et al. 1998a,b: Bacela el al. 2006). Similar

fealUres are recorded in lhe ncarb)' lb3cta scclion. near S¡m Sebaslian,and in Iypical base-of-slopc sections such as Ennua (Bacela 1996). a

facl reneeling Ihe direcl innuence of lhe sca-Ievel signalurc ondeposilional proecsscs l:Iking place across Ihe Pyrenean baJoin,

Relatioll ro Mid-Paleocene Biotic Eve1lr

A fe"" melcrs bclow lhe base of Chron C26n a global !>hon·livede\'enl of e\Olulionary ;,ignificarx:c is recordoo aOO possibly relaled lOa hyperthemml evenl (Fig. 11) (Bernaola el al. 2(07). This :>o callcd

Mid-Paleocene BiOlic E\'enl is rcprcsc:nled al l'.umaia by a dislincl

c1ay-rich intcl"'a1 charJCleril.ed by imponan! calcarcous nannofossiland forarninifer as~lllbla,ge change.<¡. Thi~ inlcrval. which is alsocharaelcrized by a si};nificanl drOIl in carbonale conlclll and a

pronollllce<1 peak in Ilmgnclic susceptibiJity, is localed ca. 4.5 111 abtwelhe first occurrencc 01' N. kll'ill/Jelli.lhe IllMker spccics ofZollc NP6,and w¡¡hin lhe planklOnie foraminifera Zone 1'4. Thi!> is al a

slrati};rJphic Ie\'el equivalenllO lhe red day layeroflhe Mid·PalcocencBiotic E\'em foond al Shalsky Risc in Ihe Central Pacific and WalvisRidge in lhe Soulh AlIanlic (Bralowerel al. 2002: Zachos el al. 2()().¡).

Al Zumaia lhe calcarcous nannofos<¡il. planllonic and bcnthicfornminifcra experienccd a rapid and ren\arkabJc lransfonnalion(Bcrnaola el al. 20(7). Calcarcous nannofossil a~scmbla};c chan};es

suggest a shift from rclali\'cly cool mcsolrophic lO warmer, more

oligolrophic condilions. Al lhc sea noor, lhc di\'crsilY of bcnlhicforal11inifcral assembluges, and lhe pcrccnlagc 01' buliminids :md of

cllifalln:r1 !>uspcnsion feedcrs decreased. whereas low food untlopporlUnislic laxa (c.g. rr"r,ropJ¡rllg/lloi(/es. Karreflllil/(I ¡¡nd

Rt'{'lln'oirli's) show quantilati\'t.' peak!> al the day.rich la)'er. These

faunal chan};cs are ~imilar 10 lhose reponed ffOm othcr carly Eocencdccp--waler dislUrbcd en\ ironments during h)"lX'nhennal eplsodcs......hich possibly affected mctabolic rales of dccp--sea fauna.s (Thotnas

2(05). Thc eaJcarcous nannofo~sil antl planllonic foraminiferalIUmO\CD !>laned carlier lhan lhe bcnthic foraminiferal ch:lIlges,

indicatin,g Ilml Ihe environmenlal change al lhe sea noor occurrcdafter lhe changes il1 Ihe surface wa!ers, This p¡lllCm is consistenl wilha lop-doWIl w:lrIlling of lhe ot.-can, and i~ ~imilar lO th:ll repol1ed by

BrJlowcr el al. (2002) for lhe PalcOt.-cnclEocene Ihenoal ma.~imum.

The ""lid·Palcoccne BiOlic Evem was shorl·li\'ed: according lOpreccs.<¡ion cycles lhe e\cnlla.<¡led for ca. 52-53 kyr, wjlh lhe {'OA: of

lhe c\'ent rc~nling ca. 10-11 kyr (Bernaola el al. 2001).

Correlation to the historical stralotypeareasBase of Selol1diol/

In al! OUICrop sccliollS in Dcnmarl, lhe hislorical lypc region forlhe ScI:mdi:m Slage. lhe DanianlSelandian boundary is marlcd by :In

uneonformilY wilh a variable number of biozoocs mbsing {8eq!gren1971: Thomsen and Hcilmann·Clauscn 1985: sce funher re\'iew inCJcmmenscn 0100 lltomscn 20051. 11 hM lherefore becn dilTlCuh lOdelcnnine lhe exaet biostmligraphic po!>ilion of lhe hislorical Danianl

SelaOOian boundary. Thcsc difficu1ties are e~acerbalcd by lhe faet

lhallhc relevam index f""si" uo;OO in internalional zonation schemcsare mre 01' lIb!>l:nl in lhe Nonh Sea Basin (lJcq!gren 1971: Percho

Nielscn 1979: King 1989: Thomscn alld 1-lcillllann-C1auo,cll 1985:Varol 1(89), The b:lsal Selantli:m is genemlly corrcl:tlcd wilh

116

plankltlllic for.lIuinifcra Zonc P3¡1. while lhe uppcrmOSl D¡¡nian is

rcferred lO lOnes Pie or 1'2. TIlC!<oC l'Orrclations are primarily based(Xl a sin.@le(lC("urrence of lhe planklonie fOr.Iminifcl1l Mom:tJI·t'I/(1

(lIlglll(lf(l. irKlcx f05$il of Zone P3a. in lhe SelaOOian :11 Copcnhólgen

(Hanscn 1968). ¡md on lhe presente of G/obocOlIll.m (/(mbjergell.\¡.f

in lhe uppcrrn()~l Dunian ul 1l1()~t oollndary IOC:llities. The highesloceurrcncc of G (itmbjt'rgt'lI.fis is widely 1I ....-d lO ¡¡pproximale lhe 10p

of Zone Pk (Obson el al. 1999). Bcrggren el al. (1995. 2000)prollO"'---U lo place lhe Danial1lSclaOOian bouOOary (arbilrarily) allhe

P2IP3lonul bollndary eom:laling. approximulely, wilh lhe milldle oflhe Cale¡lrcous n¡l1\nofos~il Zonc NP4 and wilh the base of Chron

C26r.A~ predieted by Bermlren (1971). youngcr I>.lf1ian dcposils which

narrow the slrilligr.Jphie gap in lhe suñace exposurcs are prcsenl in

lhe subsurfaee of lhe D¡mish Basin. With lhe f\."<:(jvcry of moreeonlinuous drill cnrcs, ineluding ~Olne from lhe SlOreba:1t arca, a

gr.ldu:lt and eomplele sucl·cssion oflhc Danian·Selandian lmnsiliuneould be studied in greal delail, Thc sueeession of cakarcousnannofossils in Ihcse cores. and panicularly Ihe appcar.mee of

Nt'Q('IIifls/o::.ygIlJ /Jt'rft'CIIIS clase lO lhe boondary. indicales lhal lheDani¡ll1 lO Setandi¡1ll c1mngc from limestonc lO CI¡IY oceurs in lhe

upper pan llfZllllC NP4. c10se lO lhe NP4/NP5 boundary Cl1lOmSCIland Hcilmann·C1ausen 1985;nlOlll~n 1994; von Sulis Pcrch-Nicbcn

1994; Clemmensen :ll1d Tholllscn 20(5). Aeeording 10 Berggrcll el

al. (1995) lhe NN/NP5 boundary is silualed in Ihe lower part 01'planklonic foraminifcrJ ZOne P3b, ~uggesling lhallhc uppemlOSl part

of lhe Danian dcposilS in lhe Sloreb:eh cores should be referrcd lO

7..om: P3a. This agn:cs weU wilh magnclOslr.Jligr.Jpl1ie swdics of lhe

Slorcb:clt eorc 8604A showing lhallhc D:llIi¡ll1/Sclnndian ooundaryoccurs a short diSlancc up in Chron C26r (Ali el al. 199-1).

Thc dclailcd sequencc ofC'Jlcarcous nanoofossil al>pcarJoccs aOOlhe magnelochronology al Zumaiasuggest mal lhe lilhological changefrorn lhe Aillgorri Linle'\IOOC FormaliOll 10 lhe marls of thc ItzunmFonnation reneels lhe sarne p:11cogl'Ogr.lphie cvcnl lha! callscd lhefacies shift from Dunian lirnc.~lones lo Selandian gn:cnsands. daysand murl~ in Dcnmark. Sueh a rclalionship was firsl proposed by

Schmilz el al. (1998) who foond lhe ro of N. ~if«lIls in Zumaiac10se lO Ihe Aillgorri Limc5londlt.lUrun formalional boundary.

SubSCl:IUCnl m:lgneloslr.Jligr.tphic and bioslrnl igmphie sllldies refcrrcdlu alxwe givc fllrlhcr supporl for sucll a corrdalion (c.g.. Arcnillusand Molina 2000: Dinares-TlIrcll Cl al. 2003. 2007; Arenillas el al.

2Q08: Bcmaola el al. 2(09). This included a relocalion of lhe FO ofN. /}~rf~CIfjS lO ca. 3 m below Ihe AitJ;gorri LimestonelltlUrunforrnalional boundary (Fig. 16). Considering Ihe slrong regionalevidcn(;c for u .'>C:.-Icvcl f¡lll c10se lO Ihe NP4/NP5 bound¡¡ry ¡md in

lhe lower pm1 of magnclochron C26rbolh in Denm'lrk aOO the l3asque

Clemmensen & Thomsen, 2005 Bemaola et al. 2009 Rodriguez & Aubry, 2006

North Sea Zumaia

*

GSSP•

e ......

,,'¡--,

FD 1"F. tympan;fonnis

Qreiya

* O/S boundary accordingto previous studies

.. 12--_ ...,----"0 !.o/.._- -

26 bedding ,

couplets Feto r-,:;s. primus .~ ...-~'1 ""u-_.'" " ......

" ""__FO C. edentulus 2......

"'iiif 1st rad~tiono, (m) OJ.i"'""D

~ Fascicullthu$

(b)(a)

NTp9

EA B. bigelowii ~JAIS:

ss.••

FO N. perfectus NT....

/..;;' .........~

.".. ryNTp7b

FO C. edentulus

FigJlr~ '6. Biostroligropllic CDrTdot;Oll oll/¡e ZUIIIO;O tectioll ",'ji" Soul/¡ T~I/lyJ (Qr~i.)'o) alld l)o,,;sll secliolls. (o) Colcorrous 1IOI/IIOI0ssiJ

ZOIU,~ loUv""jllg lile bj('ZOllOlioll 01 1'arol (1989). 01111 (h) maglleIVSlri/ligrap"y aJier lJillaris·Tflrel1 ~t al. (1007). 111 Nvrtll Sta log:

(1)= Ilr}'vwII Limes/flllt', (1)= Ctl/Ú,'illite, (3)= Le/Jillgc GreclI.\·{wd, (4)= Kertemi//(Ie Mad, (5)= ""'be/II Farmotioll. "rolll Ilernoufi/ el tl/.(2009). 711t ptlfCUIIIOglIClic di/to fr,r Ihe Nort/¡ Sea be/vl\' lile 1'0 01 N. l)Crfcc.lus are 01/0"" qlltlfily allt/ ¡IIterprem/iolU' are I/l/cerloill,

region (Knm I994b: B¡¡Cela clal. 2007). "nd lhe facllhallhcsc regionsare on Ihc order of only 1500 km a¡X1f1 ¡¡Iung lhe nol1heaslern Allanli('margino makcs il likely lh:n lhe S:llllC cvelll has bccn rcgislcred.

TIICsc conclu~ions are further supportcd by a recenl sludy uf lhc

Bidan alld Loubieng oUlcrop scctions in A<luilaine in soulhwcSICrrlFranee (Slellrl)aul :md SZlr.1kos 2008). High-resolulion ea1careous

n:mnofossil and foraminiferal invesligalÍons oflhcse sCclions dcfincd<l limc calibraled ~cquencc of 47 bio-evellls wilhin lhe Danian­ScI;llIdian lnlll,iliun inlerval. The Dall;an/Sel;mdian ooundary. a~

originally defillcd in Dcllmar\.;. is cocv¡11 wilh Ihe lilholugie change

from limCSlOnc-dominalcd (Lasscubc Formalion) lO marly."CdimcnulIion (Lalapy Mcmber uf lhe POIll-Labau Formalion) in

soUlhwi.'Slern Aquilainc. This horizon is also eocv¡¡1 Wilh lhc AilzgorriLimcslOllcfllzurun f0rl11¡llional ooundary ¡ll ZUfllaia. The Dimi;lIIf

Selandian boundary in lhese areas is markcd by Ihe end of lhe :lemeof lhe nannofossil family Braarudosphaeraceac. possibly due lO lhedisruplion 01' frcsh walcr illnux rclmcd lO c1imatie ehanges (Steurbaul

amI S/.lrákus 2008: Bernaula el al. 20(9). Sludies of S<.."X:lions aerosslhe upper Dani:1Il and 10wer Sel¡lIldian in Bclgium indiclIle:l similar

>ea-Ievcl hi~lory in rclalion 10 bio,lmligraphy as in Dcnrnark and lheBay of Bisc¡lY rcgioll (Sleurb¡Ull ¡uld SZln¡ko~ 2008). TIle sea-leve!changes lhercfore arc cilher cU~lalie or relaled lO large-scale leClonic

evenls affccling lhe enlirc norlhweslern Europe. Cyc1o- andmagneloslmligmphic sludies oflhe Loubieng scrlion wilh corrcl:llions

lO ZlImaia have fllrther refincd lhe slmligraphic schcme aeross lheD¡¡nian-Sclalldian lmnsilioll (Dinarh-Turell el al. 2(10).

Base of Thalletitlfl

Corrclalion lo lhe hislorie:ll1Ype area is slraighlforward w;lh lhehclp of rnagncloSlmligmphy (base 01' Chroll C26n) aud calcareous

n:Jnnofossils (uppcrZone NP6) (Aubry 1')94: Hine 1')94: Knox 1994a:

Ali and Jolley 1996). TIle basal Thanelian in ilS original lype arcaand ils ellslem prulongalion in Belgiul1l. as wcll as al Zumaia and inshallow-waler sectiolls in lhe Pyrenecs retlcets a major lransgression.

mnsl likely rclaled lO lhe same euslalic or regional isoslalic eve!11(Knox 1994l1.b: Sleurbaul 1998: Puj¡¡11e el ¡ll, I998a.b. 2000).

Correlation lo lhe TelhysIn lhe soulhern TClhyan re;lIm (e.g. Egypl. Tunisia. l¡,m(1)

sedirnenlalion condilions in lhe early and middle Paleucenc arc \'ery

difTerent fromlhe weSlcm Europcan b:lsins. Seclions in Ihe soulhemTClhys over lhis irllcrval are lypic:JlIy eharaelerized by monolonOllSbrownish grey marls. One particular mid-Pa!cocenc evenl levcl.

represenled eilher by an uneOnf0rt11ilY (in severa! Tunisian sccions)oro as ¡l promincnl organic-rich,.bcd.laminalcd and rich in tish debris

(in several EgY]Jli.rn seelions). has been considered lo possiblyrepresem a Danian/Selandian boundary cvenl (SleurbaUl el al. 2000:Spcijer 2000. 2003: GuaSli el ;11. 2006: Van IUerbceck el al. 2007:

Obaidalla el al. 2009: Soliman and Obaidalla 2010). This leve! haspreviously bcen lhoughllO correspond lO lhe now dclined base of lheSe1:mdian al Zunmi¡¡ (e.g.. Spcijer 2003). bul recenl ca1carcousnannofossil and fomminifeml ~tudies ,how lhat lhis evenl is ca. 4()(}­

600 kyr oldcr (Bcrnaola 2007: Slcurbaul and SZiriÍkos 2008: Sprongel al. 2(09) and is now lenlled lhe L;llesl Danian Event (Borncmannel al. 2(09). In lhe Qreiya scclion lhe organie-rich I¡¡yer OC('urs

appro:"¡lIHllcly 1 m lIbove lhe FOs 01' C. ('ll('IlW/I/S ¡¡lid lhe smallfasciclllilhs (Sprong el al. 2(X)')). According lO lhe cycloslrmignrphie

t¡,¡sodes \i>/. j.¡. l/O. 4

237

sludie.~ al Zunmi:l lhe FO of C. edl;'lrlll/I/,\' :lnd \he lirsl cnnlinunusQCcurrem:c 01' SI'!lellu/il/III.\' ¡¡re 32 and 22. re~pcclively. bedding

COuplclsfprecession cycles bclo\\' Ihe IOp 01' lhe AilzgOni Limeslone

Fonnalion (Bcmaola 2007: 13emaola el nI. 2009). Assuming a II\cunpcriod 01'21 kyr rur lhe precession cyc1es lhis means lhallhe* e\'ent~

are respcclivcly 672 and 462 kyr older lhan Ihe 10]J 01' lhe Danian

limeslones. Al Qreiya lhe organie-rieh layer is silualed belween lheselWO events. and il is appro:l:ill1alc1y 570 kyr older Ihan lhe IOp 01' lhe

Ailzgorri Limc~lonc Formalion in ZUl11aia and lhe OunianfSclandianboundary in lhe originallYpe arca 01' Denmark.

Primary and secondary markers

Base 01 'he Se/alldiall

The besl c\'ent for global. marine corrc!alion is lhe second

radial ion 01' lhe il11pol'l<lnl c¡¡lcarcous n:rnnofossil group. lhefaseiculilhs (charaCleril.ed by lhe lir~l OCeurren('c of rasl'Ículil/lfls

u/ii s.s.). CycloSlr.tligmphy combined wilh rnagnelOslrm¡graphy lmlYalso be crud;ll. for e:l:lllJlple. in correJalion lO caminenl:ll scclions.For regional marine eorrclalion. al leasl in nul1hweslcm Eum~. lheend 01' lhc acme of lhe nallnofo,~il farnily 13nt:1rudosphacnlCC¡le

logelhcr wilh Ihe cess:uion of long-Icrm c¡lrbonale deposilion and

evidcnce uf sea-leve! fall ean also be used.

Base DI fhe Tlwlleliafl

The C26rfC26n magnelOchron reversal is lhe besl globalcorrclalioll 1001 ;md can be applicd lO a varielY of f¡Kies.

Cycloslr:lligraphy logelher wilh lhe posilion of lhe Mid-Paleocene13i01ie Evenl ean be used for delailed rn¡lrine correl:llion.

Accessibilily, conservalion andprOleclion

Considering lhe exposure ¡¡long lhe main "playa" of lhe lownZumai¡¡ aecessibililY lO lhe GSSPs is oplirmll. There is cvcn ¡l holel

loealed on 101' uf lhe c1iff seclion (on lhe uppcr Thanelian pan of lheslrala). TIle lihed nmurc of lhe sImia ulJows cxccllcnt access along

Ihe be;leh ul lhe sall1c lime as one ascends ()J' descends lhrough Ihegeologic record. Aecess is limiloo during high lide ;md slmng 1,1I1dwardwaves. howevcr. bolh GSSPs arc aboye lhe highesllevcl whcre wave

:lclion normally erodes lhe cliffs. and lherc is no risk lhm the scclionwill be 10Sl beeausc of erosion. TIle ditl's and lhe beach are major

lourisl allnlc1Íons aud lhe loe¡¡l eomrmrnilY llnderswnds lhe "alue ofpreserving Ihe arca frolll exploilalion lhal may dam:rgc lhe GSSPs.Morcover. lhe enlirc oulcrop was prolccled by lhe Basque Govemmenl

in FebruMY 2009 wilh lhe "Deba Zumaia Coaslal 13iolOpC"'. adcclamlion lhirl guarantces lhe conscrvalion of lhe oulcrop. 11 is lhet1rsl gcological oUlcrop prolecled by law ill lhe Basque Counlry. The

managemel1l of lhe l3iolOpC. incJuding lhe Palcocene seclion. is ineharge of lhe COUlllY Council of Gipu~.ko¡l. which has crealed apal1icular "scienlifie rnanagcmen¡" 10 ensure Ihe pcrforrll¡lncc of lhe

lhree lllain objeclives 01' lhe nalural reservc: lhe proleclion 01' lheoulcrop. lhe prornolion and coordinalion of the scienlÍfic rcscarch

amllhe popul;lrizaÜon 01' the gcologieal V¡¡llle 01' lhe area. Therc areno rcslriclions lO salllllling. bUl il is advis;lble lO conlacllhe scienlitkmanagemenl orlhe scrlion (flysch@gipuzkoa.nel)IOOblainlhespccial

238

~ ... t....-",.

~"'" .pcnnil dial is rcqum:d lO worl. in the arca. It i~ also imponam 10 note

lhal lhere i.. an Inlerprelation Ccnler in Zumaia caUed Algorri and

that 3 complele progrom ""ilh geologieal guirJed cxcursion:. has bcendc\'elopcd lO promote Ihe knowledge of lhe section among scholaTSand \'i~itors. TIIC Zumaia M:Clion also contains excellcnl records oflhe CrclaceomJPaleogene and PalcoccnefEocelle bounuaries. :jdtlillg

lO ilS gcological significan<.-c.

bl ContnD.lI_.."""

--._--

...... _1 _ bI.l \herw " lT>I poultldity 10

-...~WIltl c:ycIottmigr~

v_ n.llUII:r<lp. n:l"*' no ... Oooez........ e-.I 8o<*Ille, _ jo -.g 10~ _ promohIlhIo oarUic-=tMtyn .... _ An~Io'm,*,~_

frcm~""'__ ~1íIed

10 __., 1*fTI1S""" 1O_.,1hIo HCl"""

Ya ThlIIClIDI'1" -..;no lhIo rt__al ..~ ••~

t'1- ThlloelIl vo-m-na..---a...._,...... .. ~....,.IO~.

. -_......__...._._.1l~"'_,_-o.'1

"-

lWO jeeps plus desen pcrmils. The ZUmai¡1 scelion is abo more

exp.1nded Ihan Ihc Qrciya seclion. alleaSl across the Dani:m-Sel:mdianIr.Jnsilion. An importunl <'·onsider.llion is Ihc facllh31 high.resolUlioncyclrn.lr.Jligraphy aOO good magnelostr.lligrophy exisl for Zumai¡¡.

wlw:reas lhese parameters canOOl be uscd al Qreiya. This i$ a very'ilrong argumem in fa\'or of Zumai;). Prescn"alion of fOl"3lllinifem

and calC".lreous oannofossils is superior al Qrciya rclatl\'e 10 Zumaia.bul preservalioo al Zumaia is slill sumeienl for csl¡¡blishing a high~

resolUlioo bioslrotigrJphy. Al Zumai:l cOlTclalions and ('olllpamti\'c

sludies eunl:e madc Wilh nearby coeval scdimenl scctions rcprescminga wiuc mnge of facies and envimnmenls. including base of slopeapron. inner and OUler shelf. deep-sc¡j ch:mnels and even cOntinenlal

f¡leics in Ihe Trcmp Basin lO thc southe¡ISI (Schmilz and Pujalte 2003).TI,is correlation pOlcntial opens the prospccl for del¡¡iled Icmporo'

and spalial reconslruclions of sea-Ievel changes al Ihe DanianlSel300ian aOO $ebndianffhanelian boundaries. Al Qrciya llw:re isalso subSlantial eorrelalion pOlenlial. bul lhe speetrum of

paleoenvironments is 001 as wide as in lhe Pyrenean regioo. Al lhefinal nt<.'Cling of lhe Palcocenc Working Gmup. held in Zumai¡¡ in

June 2007. lhesc issuc:. were discus.~ed in delail. and based onevalu:llion.~ of eXlensivc ¡jnd detailed dalu SCIS lhe Zumaia scclionwas unanimously considercd Ihe mosl suitable seclion lO host lhe

II)F__ larlongrro;. TelhyIVES

-9"Ill!'oc~""" _OCMnVESNom~.... YES

.....................................1 ..

,) ""*-Y'"-

"'ig/ln J7. SUII/I1Itlry ofelYlJualiol/ oftlle ZIII1Itlio sectiollfor 1I0ldil/glile Se/OIldiQII O/Id T/J(I/u!lioll GSSI's ill re/aliOli 10 lilerecommellllaliol/s by the IlIlematiOllll1 COlllmissioll (JI/ Slr(lligropl!J.

lllCre was a general rttOgnilion early in lhe !toCleclion procedurc

lhat Zum:lia would be onc of lhe prime caOOidatcs for GSSPs.. butne\'erthclcs.., (klaik-d orpilot :.Iudics have becn madc of ¡¡ large numbcrof set1ion, mainly in the COUnlrics ¡¡rounu lhe Medilerrnnean. ll1c

following ahemalive seclionl> halle been l>Criou'>ly considcr\:d: GebclAwcina. Gebel Duwi and Gebel Qreiya in thc E;l'>te01 Desert of Egypl

(e.g.. Charisi and Schmil~ 1995. 1995: Speijer and Schmilz 1998;Spcijer2000. 2003: Sprong el ul. 20(9). Sen Gurion in Israel (Schlllilzel al. 1997b; Churisi :md &hmilz 1998). Ihe Sidi Nasscur und Ain$eltar.l seclions near Kalaat Senan in Tunisi¡¡ (Sleumaul el ¡¡l. 2000:

Guasti CI al. 2())6; Van hterbceck el al. 2007: Sprong el al. 2Ol9).Botlacciooe Gorge and Conlcss:l Highway in haly (Corficld et al.

1991). aOO Carav0C3 in Spain (Arenilla~ and Molilla 1997). In ilsfinal stage lhe sclcetion proccdure was naITOwcd down 10 a comparison

of lWO ~tions. Zum¡¡ia. anu Ihe Qrciya seclion in lhe Eastcm OcSCr1of Egypt. Beeuu'>e of lheir cxedlenl records both s..:clions halle beC11Sludied in uetail by several groups aud cnll~iderable dala elli.,t. A

delailed profile ueross Ihe Qreiyu section was sumpled by B. Schl\1iv;.

R. Knox. N. Obaidal1ah and M. Solim:lll in 2004. Thc.~ sumpleswere di:.lribuled wilhin Ihe Paleocene Working Group and ha\'crcsulu:d in sc\"crol detailed :.Iudies (e.g.. Bemaola 2007; Monedli

aOO Reale 2007: Oruc-Et~ebaniact al. 2007a.b: Rodríguez and Aubry2(07). Slr.lligr.lphy aOO p:lleoeo\irooments were also intensi\"e1y

sludied in sc\·cral parallel sectioo!> al Gcbel Qrciya (e.g.. Spcijer2000. 2003; Bornemann et al. 2009; Sprong el al. 2009).

One major ¡¡dvanlage of ZUIll¡¡i" is il!> poo:.ition interrnedi:llebclwccn lhe North Se:l (or borc¡ll) region. whcrc lhe original slr.Jlotypcseetion:. for Ihe Selandian and ·nmnetian were detined. :md lhe more

southerly Tethys region. e.g. Egypt. Tllllisia and South Spain (SchrnilJ;et 31. 1998)" 11lc Zum3ia seclion contains faunal and nor.J1 clernenl.'>

represcnlati\"c of both regions aOO this facililalcs corrclalioo belwccnlile Nonh Sea aOO lhe resl of lhe world. During lhe P3lcoccne lheZumaia sile appear.¡ to ha\'e been alTecled by the <;ame sea-1e\"el ¡md

lilhology ch¡¡ngcs as other northwCSlern European siles. Placiog lheGSSPforlhc bascoflhe$clandian allhcshifi fmm limeSlooc lO marl

in the upper NP"¡ Zone P.1YS homage lO Alfrcd R<bCnkrontz's origin:lldefinilion of Ihe Selandian (1924) al Ihe ,>hifl frorn lime.~lone lO grey

marl illlhe Danish Basin. beC:lUSC mosllikely lhe change in lilhologyal Zumuia regislers the sarne regional evenl. The lirncstoncfmarl shiftofZumai:1 has :llso becn irJcnlificd in Ihe Loubieng scction in Aquilainc(SW Fmnce) (Steurbaul ¡¡nd SIIr.1kos 2008). Both scclioos are markcd

by a (:ommon dcposilional hislory. as shown by lhe ¡¡Irnosl idcnlicalstrotal QlCCcssion and scqueoce ofbio-ncnts. Zumaia excels IhrOlJgh

ilS beller aOO more pennancnl acccssibility of lhe OUIcn>p (roastalSttlion \eISUS quarry) and lhe wider gamul of sciemific informalion(preseoce of magoctoslroligrophic and cyclosllmigrophic sludies). bUl

Loubieng i!> :LlI excellent auxiliary seclion. The Zumaia scclion isalso superior rclative 10 Qrei)'a bccause ofits mllch bellcr aCl.:cssibility.

A visillO lhe Qreiya '>ection rcquires a smal! expedition wilh al leasl

Summary of selection procedures

GSS~ for lhe Selandian ¡¡nd Thanelian Slal;c.... 1ñe .....orking group

earefulJ) cvalualcd lhe slanding of lhe Zumaia M.'t:tion in rclalion \O

lhe requiremenls for a GSSP according lO Ihc I",croalional

Commission on Slruligrnphy. and foond lhm Zumaia is c10se lO idealfor placing Ihe GSSPs lhere (see fUl1her rompilalion in Fig. 17). 1ñeInlemational Union of Gcological Scienees rnlified lhe propo:.cd

GSSPs forthc Sclandian :mdlllanetian slab'CS al Zurnaiaon Scpternhcr23.2008.

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.' ....••~" ~

.' ~Membcrs of lhe r-.. leoccnc Worl:jng Group in fmm of lhe basal Sel:mdian oUlerop 31 h7urun Beach. Junc 2007. From left lO righl; RobenSpeijer. Jorindc Sprong. Enk lbomscn. Annc Clemmcnscn. Bill Bcrggren. Fernando Caballero. EUSloquio Molina. Xabier Oruc-Elxebarria.

M:uia Rose Pclriu:O. Aitor Payros. Ignacio Arenillas. Robcrt KIlO" VICtoriano Pujallc. Marie·Pierre Aubry. Birgcr Schmilz. Gilen Bcmaola.Maile Manín-Rubio. Simonc:lla MOIllochi. CI;¡us Heilmann-Clau"Cn. Elienne Sleumaut. and Christian Dupui~. Memben not shown in photoare: Laia AI~gre1. Eslibalil Apellani/_ Juan-Ignacio Bxet3. burne Dinares·Turell. Asier Hil;¡rio Orús. Sih'ia Ortiz 300 Kalharina \00 Salis.