revision of the messinian-early zanclean sediments from odp...

Hindawi Publishing CorporationPaleontology JournalVolume 2013 Article ID 947839 17 pageshttpdxdoiorg1011552013947839

Research ArticleRevision of the Messinian-Early Zanclean Sediments from ODPHole 953C (Canary Island Archipelago North-Eastern Atlantic)Biostratigraphy Cyclostratigraphy and Astronomical Tuning

Federica Riforgiato

Dipartimento di Scienze della Terra Universita di Siena Via Laterina 8 53100 Siena Italy

Correspondence should be addressed to Federica Riforgiato riforgiatogmailcom

Received 4 September 2012 Revised 22 January 2013 Accepted 23 January 2013

Academic Editor Matıas Reolid

Copyright copy 2013 Federica Riforgiato This is an open access article distributed under the Creative Commons Attribution Licensewhich permits unrestricted use distribution and reproduction in any medium provided the original work is properly cited

A quantitative study was performed on calcareous plankton of the Messinian-early Zanclean succession recovered at ODP Leg 157Hole 953C (Canary Island Archipelago North-Eastern Atlantic)This revision allowed to recognize some events typically recordedin the Mediterranean region highlighting affinities between the Mediterranean and North Atlantic Ocean in the consideredtime interval The presence of such events in an open-ocean succession provides the possibility to substantially improve thebiostratigraphic resolution and supplies useful correlation tools between theMediterranean and oceanic areasMoreover to unravelcyclical patterns of deposition and given that the investigated succession shows no evident lithological pattern cyclostratigraphicanalyses have been based on abundance fluctuations of Globigerinoides-Orbulina group neogloboquadrinids and warm-waterversus cool-water species ratio As a result forty-three precession-controlled cycles have been recognized spanning from 6457Mato 4799Ma

1 Introduction

The Messinian Salinity Crisis (MSC) affecting the Mediter-ranean area during the latest Miocene has been the focusof numerous studies (eg [1ndash18]) It is considered as oneof the catastrophic oceanographic events that occurred inthe last 20 million years [5 8 19] It was caused by thetemporary isolation of the Mediterranean basin from theAtlantic Ocean due to a combination of tectonic and climaticfactors (eg [19ndash21]) According to numerous authors theonset of the MSC was synchronous over the entire Mediter-ranean basin and its end corresponded to the catastrophicflooding of marine waters from the Atlantic Ocean (eg[19 20 22ndash34]) The sedimentary expression of this floodingis recorded everywhere both in land sections and in thedeep sea cores showing that the transition from continentalto marine environment across Miocene-Pliocene boundarywas (i) typified by continuous sedimentation (ii) geologicallyinstantaneous (iii) synchronous throughout the Mediter-ranean basin However the problem of the exact timing andorigin of the Pliocene flooding of theMediterranean is not yet

completely understood and the evidence is not irrefutableSome authors support the early Pliocene flooding of theMediterranean (eg [7 8 35]) while others support a lateMessinian re-flooding (eg [6 36ndash41]) Indeed during thesalinity crisis environmental conditions within the Mediter-ranean excluded most marine microfossil groups which aretraditionally used for biostratigraphic correlation

To understand the cause(s) and consequences of the onsetof the MSC in detail an age control is needed for the partof the Atlantic immediately adjacent to the MediterraneanIn this connection the ODP Leg 157 Hole 953C (CanaryIsland Archipelago North-Eastern Atlantic) is consideredfavourable to the aims of the work for (i) the location (ii)the excellent paleomagnetic data (iii) micropaleontologicalrecords despite intervals of no recovery

Recently an age control was obtained for the Messinianboth in the Mediterranean and in the low-latitude AtlanticOcean through integrated stratigraphic studies comple-mented by the astronomical tuning of sedimentary cycles orother cyclic variations in continuousmarine successions (eg[3 34 42ndash52]) Milankovitch cyclostratigraphy is nowadays

2 Paleontology Journal

considered one of the best tools to gain high-resolutionchronostratigraphy in different depositional environments(continental marginal marine and deep sea) The presenceof high-frequency cycles in deep-sea records and their tuningto the astronomical curve provide an accurate chronologyfor the stratigraphic events recognized through the studiedsedimentary successions Applications of cyclostratigraphyresulted in the construction of an accurate AstronomicalTuned Neogene Time Scale (ATNTS 2004) for the Qua-ternary Pliocene and late and middle Miocene [3 42ndash44 53ndash61] The classic high frequency cyclicity recognizedin most of the late Neogene Mediterranean sedimentaryrecord is manifested by the alternation of homogeneousmarl and sapropel (or sapropel equivalent) horizons pro-moted by astronomical forcing [3] In this paper since thesuccession investigated does not show rhythmic litholog-ical patterns the proposed cyclostratigraphic reconstruc-tion is mainly based on the quantitative distribution pat-terns of climate-sensitive planktonic foraminifera taxa (eg[62ndash66])

The aim of this paper is (i) to present an biostratigraphyfor the Messinian-early Zanclean of the Hole 953C basedon quantitative data of planktonic foraminifera (previousstudies by [67 68] are to be considered inadequate for thisresearch) (ii) to compare the bioevents recognized withthose occurring in other astronomically calibrated sections(iii) to recognize other cyclic patterns for using as furthercontrol of the obtained astronomical calibration

2 Material and Methods

21 Site Description During Ocean Drilling Program Leg157 four sites (Site 953 to 956 see [70]) were drilled in thevolcaniclastic apron of Gran Canaria in the Canary IslandArchipelago (North-Eastern Atlantic) (Figure 1) ODP Hole953C is situated at 28∘391015840012N 15∘081015840670W 68 kmnortheastof GranCanaria 90 kmwest of Fuerteventura and 98 km eastof Tenerife at water depth of 35778m It is the most distallylocated site on the flanks of Gran Canaria and thus seemsto have been spared some of the major slumped intervalsand unconformities present at Sites 954 955 and 956 Therecovered sedimentary succession spans the interval from themiddle Miocene to Holocene and the dominant nonvolcaniclithologies were divided into seven major units and threesubunits (see [69]) The present study focuses on a 5111mthick succession from the Unit III embracing cores 18R to13R from 34689 to 29578mbsf (Figure 1) and representingthe Messinian-early Zanclean time interval Core recoverywas generally over 50 and mainly consisting of gray tobrownish-gray clayey nannofossil ooze interbedded withminor graded nannofossil clay-silt foraminifer lithic silt andsands and foraminifer sands

22 Sample Preparation and Micropaleontological Analysis

221 Foraminifera Samples for foraminiferal analysis weredisaggregated in normal water and washed through a 63 120583msieve The residues were oven dried at 40∘C Qualitative

and quantitative planktonic foraminiferal analyses were per-formed using a stereoscopic microscope on 170 samples(average spacing 20 cm) The samples were divided with amicrosplitter to obtain unbiased aliquots with about 300planktonic foraminifera They were (1) picked (2) mountedonto faunal slides (3) determined at specific and supraspe-cific level and (4) counted (200ndash300 specimens) from thelarger than 125 120583m fraction of the washed residue to collectquantitative faunal data The assemblages are usually abun-dant and generally well preserved although at times they arepoor Very few samples show a very scarce faunal content

Raw data of microfossils were transformed into percent-ages over the total abundance and percentage abundancecurves were plotted Species with phylogenetic affinities andsimilar environmental significance were also grouped tobetter interpret distribution patterns

Furthermore a semiquantitative analysis from the largerthan 63 120583m fraction was carried out on all samples in orderto pinpoint the actual position of the bioevents

Benthic foraminifera were also counted to determineplanktonbenthos ratio which is expressed as P = 100 lowast[P(P + B)] (eg [71])

222 Calcareous Nannofossil Standard smear-slides wereprepared for the nannofossil analyses for the intervals encom-passing the principal bioevents (from core 17R Section 3 tocore 13R Section 5) Qualitative analyses on a total of 30samples have been performed byDr Baldassini N (SienaUni-versity) to determine additional biohorizons and bioevents toimprove the biostratigraphic resolution

3 Micropaleontological Data

Theanalysis of the planktonic foraminiferal fauna allowed theidentification of 45 taxa which sometimes were grouped intocategories on the basis of morphological phyletic or ecologi-cal affinities The categories are (Table 1) Dentoglobigerina gr(D altispira altispiraD altispira globosa)Globigerinita gr (Gglutinata G uvula) Globigerinoides obliquus gr (G bollii Gcf elongatus G emeisi G extremus G obliquus) Globigeri-noides quadrilobatus gr (G quadrilobatusG trilobusG sac-culifer)Globoturborotalita decoraperta gr (G cf apertura Gdecoraperta) Globorotalia menardii gr (G menardii G mul-ticamerata) Neogloboquadrina gr (N acostaensis N pachy-dermaN dutertrei humerosaN dutertrei blowi)Orbulina gr(O bilobataO suturalisO universa) and Sphaeroidinellopsisseminulina gr (S seminulina paenedehiscens S seminulinaseminulina) Most of the categories are self-explaining butthe labelling of some of them needs further explanation

Figure 2 shows the quantitative distribution of thosespecies (or categories) which generally display frequencieshigher than 15 The main components are Globoturboro-talita nepenthes and Neogloboquadrina gr which are contin-uously present throughout the investigated interval reachingmaxima frequencies of 90 and 80 respectively

Neogloboquadrina gr includes also small-sized speci-mens sometimes under poor preservation conditions thatwere difficult to distinguish Different coiling directions of

Paleontology Journal 3

28∘N

29∘N

350

340

330

320

310

300

Dep

th (m

bsf)

Hole 953C

Cor

e

Reco

very

Uni

t

Lith

olog

y

13R

14R

15R

16R

17R

18R

III

Nannofossilooze or chalkCalcareous sand orsandstone

2000

9553000

3000

956

2000

2000

1000

1000

Fu

953

954

GranCanaria

Tenerife

16∘W 15

∘W

16∘W 15

∘W

27∘N

28∘N

29∘N

27∘N

Figure 1 Location map of the ODP Leg 157 Sites 953ndash956 (Canary Islands) and simplified lithology of Site 953C based on the site descriptiontaken from Shipboard Scientific Party [69]

295

300

305

310

315

320

325

330

335

340

345

350

Dep

th (m

bsf)

1314

1518

1716

6CC

CC

CC

CC

CC

12345

1234

1234

5

12

12

123

3

6

Cor

eSe

ctio

nSa

mpl

ePo

larit

yCh

ron

ODP Hole 953C

C3n2r

C3n3nC3n3r

C3n4n

C3An

C3r

LO

LROSD

100

50 200 00 20 0 5 0 10 150 0 2 20 0 30 0 020 040 090 060 0 5 060 3030 0 40 00

ldquoFOrdquo

Den

toglo

bige

rina

gr

G fa

lcone

nsis

Glob

iger

inita

gr

Gob

liquu

s gr

G q

uadr

iloba

tus g

r

G ju

anai

G m

mar

garit

ae

G m

prim

itiva

G ci

baoe

nsis

G sc

itula

G m

enar

dii g

r

G m

iotu

mid

a

G d

ecor

aper

ta gr

G n

epen

thes

N a

costa

ensis

N p

achy

derm

a

Orb

ulin

a gr

Spha

eroi

dine

llops

is s

gr

119875 ()

Figure 2 ODPHole 953C abundance curves of selected planktonic foraminiferal (as a percentage of the total planktonic foraminiferal fauna)and position of most significant biohorizons Grey color in Globorotalia menardii gr Neogloboquadrina acostaensis and N pachydermadistributions indicates the percentage of sinistral formsThe red dotted line designates the hiatusThe following acronyms indicate bioeventsLO (Last Occurrence) FO (First Occurrence) LRO (Last Regular Occurrence) and SD (sinistraldextral coiling change)

the N acostaensis (average value of 17) have been countedseparately as far as the study time interval coiling-changeof this species has been proved to have potential biostrati-graphic significance Particularly in the lower part of thestudied interval sinistrally coiled specimens prevail up to34457mbsf and after this level the dextrally coiled increasesin abundance

N pachyderma comprises specimens with low trochos-piral test four to five and one-half chambers in the finalwhorl with the last chamber irregular often a kummer-form surface characterized by large euhedral calcite crystalsumbilicus from closed to open but always narrow andaperture umbilical-extraumbilical with a thick apertural rimThis species is present from the base of the investigated


Table 1 ODP Hole 953C planktonic foraminiferal groups used forthe quantitative analyses

Dentoglobigerina altispiraaltispira

Dentoglobigerina groupDentoglobigerina altispiraglobosa

Globigerinita glutinataGlobigerinita groupGlobigerinita uvula

Globigerinoides bollii

Globigerinoides obliquus group

Globigerinoides cfelongatusGlobigerinoides emeisiGlobigerinoides extremusGlobigerinoides obliquus

Globigerinoidesquadrilobatus

Globigerinoides quadrilobatus groupGlobigerinoides sacculiferGlobigerinoides trilobus

Globorotalia menardiiGloborotalia menardii groupGloborotalia

multicamerata

Globoturborotalita cfapertura

Globoturborotalita decoraperta groupGloboturborotalitadecoraperta

Neogloboquadrinaacostaensis

Neogloboquadrina group

Neogloboquadrinadutertreihumerosadutertrei blowiNeogloboquadrinapachyderma

Orbulina bilobata

Orbulina groupOrbulina suturalisOrbulina universa

Sphaeroidinellopsisseminulina paenedehiscens

Sphaeroidinellopsis seminulina groupSphaeroidinellopsisseminulina seminulina

interval showing abundances of about 30 with peaks ofabundance in the range of 40ndash60 The coiling directionof N pachyderma is prevalently sinistral

N dutertrei humerosaN dutertrei blowi (following theconcept of [72]) comprises specimens showing low tro-chospiral test with five or more chambers in final whorlsurface uniformly moderately perforate with the character-istic rosette pattern formed by concentric arrangement ofeuhedral crystals on each chamber umbilicus open and deepaperture umbilical-extraumbilical and a moderately high

arch bordered by a distinct rim (in N dutertrei humerosa)N dutertrei humerosaN dutertrei blowi first occurs at33647mbsf displaying low percentage value about 26Thecoiling direction of this phenotypic couple is prevalentlysinistral

G decoraperta gr and G obliquus gr show a continuouspresence along the investigated interval with high abundancevalue of approximately 355 and 33 respectively

Dentoglobigerina gr displays low frequencies (averagevalue of 21) intervals with isolated abundance peaks higherthan 15

Sphaeroidinellopsis seminulina gr shows a general trendvery similar to that of Dentoglobigerina gr displaying lowvalues (approximately 2) but a continuous distributionwithpeaks of abundance higher than 14

Keeled globorotalids are represented by GloborotaliamiotumidaG menardii grG margaritae margaritae andGcibaoensis

G miotumida which includes less inflated forms ispresent from the bottom of the studied interval with lowfrequencies (average value of 7) up to 34435mbsf where itdisappears From this depth three short influxes are recorded(average value of 05)The coiling direction ofGmiotumidais prevalently sinistral

G menardii gr includes the species G menardii and Gmulticamerata G menardii shows low and scattered occur-rence from the base of the investigated interval (average valueof 13)The coiling direction is prevalently dextral with shortsinistral influxesGmulticamerata which includes the formswith seven to ten chambers in the final whorl first occurs at34205mbsf and displays a low a discontinuous distributionwith a maximum of approximately 2 Throughout thestudied interval it is exclusively dextral

G margaritae margaritae occurs firstly at 33611mbsfdisplaying a continuous presence until the top of the studiedinterval with low percentage value (about 9) The coilingdirection of this species is prevalently sinistral

G cibaoensis first occurs at 32525mbsf showing low(about 2) and scattered distribution up to 29728mbsfwhere it disappears Throughout the studied interval it isprevalently sinistral

Unkeeled globorotalids are represented by Globorotaliajuanai G margaritae primitiva and G scitula G juanai ispresent from the base of the investigated interval showingabundance of about 5 that decreases until its disappearanceat 33766mbsf

G margaritae primitiva first occurs at 33749mbsf dis-playing low but continuous distribution (about 9) withisolated abundance peaks higher than 10 Throughout thestudied interval it is exclusively sinistral

G scitula shows low (about 14) and scattered occur-rences from the base The coiling direction of this species isexclusively dextral

Additional and significant taxa such as Globigerinafalconensis (about 16) Globigerinita gr (about 22) Gquadrilobatus gr (about 14) Orbulina gr (about 5) andSphaeroidinellopsis seminulina gr (about 21) are continu-ously present throughout the investigated interval


Table 2 ODP Hole 953C calcareous plankton bioevents The asterisk indicates that the bioevents occur within the hiatus which is an agespan about 6436 to 6252Ma

Bioevents Samples mbsf Chron Age (Ma)10 Amaurolithus bizzarus First Occurrence 14R-2 10ndash12 cm 304 C3n4n 50389 Triquetrorhabdulus rugosus Last Occurrence 15R-2 63ndash65 cm 31273 C3r 52448 Neogloboquadrina acostaensis first influx sx 15R-2 95ndash97 cm 31455 C3r 52977 Helicosphaera stalis ovata Last Occurrence 16R-3 91ndash93 cm 32578 C3r 56816 Nicklithus amplificus Last Occurrence 17R-3 42ndash44 cm 33452 C3r 59795 Globorotalia margaritae margaritae First Occurrence 17R-4 51ndash53 cm 33611 C3An 60174 Globorotalia juanai Last occurrence 17R-5 56ndash58 cm 33766 C3An 60583 Globorotalia miotumida Last Occurrence 18R-3 75ndash77 cm 34435 C3An lowast

2 Globorotalia miotumida Last Regular Occurrence 18R-3 965ndash985 cm 34457 C3An lowast

1 Neogloboquadrina acostaensis coiling change 18R-3 965ndash985 cm 34457 C3An lowast

4 Biostratigraphy

Calcareous plankton biostratigraphy of the Hole 953C isbased on the stratigraphic distribution of several LateMiocene-early Pliocene marker species Ten biostratigraphicevents which have previously been dated astronomicallyboth in the Atlantic Ocean and in the Mediterranean Sea arealso recognized in this work

In the following distribution patterns of the mainbiostratigraphic marker species are discussed in detail andcompared with other land or deep-sea successions both fromthe Mediterranean Sea and Atlantic Ocean The first lastregular and last occurrences (FO LRO and LO) are shownin Table 2

41 Planktonic Foraminifera

411 Neogloboquadrina acostaensis Coiling Change TheNeogloboquadrina acostaensis coiling change is defined by thefirst common occurrence of dextral forms after a long periodof dominance of sinistrally coiled specimens It has recordedin the preevaporite marls of many Mediterranean sections(eg [45 52 73 75ndash86]) and in the Atlantic Ocean succes-sions (eg [48 82 87ndash100]) slightly predating the onset ofthe latest Miocene glaciation [8 45 52 94 95 101 102] Thisevent always seems to be located within subchron C3An1r[84 97 103] it usually occurs prior to the disappearanceof Globorotalia miotumida ([82] and reference therein) andit is astronomically dated at 6358Ma in the Mediterraneanarea and at 6373Ma in the Atlantic one [56] At Hole 953Ca very prominent sinistral to dextral coiling change of Nacostaensis (Plate 1 Figures 5(1) 5(2a) 5(2b) and 5(2c))is recognized at 34457mbsf (sample 157-953C-18R-3 965ndash985 cm) Moreover this event is followed by pronouncedsinistral influxes of the group twelve in Ain el Beida section[48] while Benson and Rakic-El Beid [98] only recognizedfive influxes which are most likely related to a lower sampleresolution two sinistral influxes in Falconara section [52] andin Sorbas Basin [45] All influxes are located within subchronC3An1n In the ODP Hole 953C five sinistral influxes arerecognized between 34160 and 33280mbsf

Above the last sinistral shift the coiling of N acostaensisremains dominantly dextral up to the late part of Chron C3rwhere a sinistral coiling change of this taxon is recognizedat 31455mbsf (sample 157-953C-15R-2 95ndash97 cm) The pres-ence of this event referred as ldquofirst Pliocene N acostaensissinistral shiftsrdquo is identified both in the Atlantic and in theMediterranean succession (eg [25 28 29 33 34 53 66 99])

412 Last RegularOccurrence andLastOccurrence ofGloboro-talia miotumida Globorotalia miotumida is a typical LateMiocene species recorded in the Mediterranean area (eg[45 52 73 78 93 105 106]) and in the Atlantic Oceansuccessions (eg [48 87 89 92 96 107 108]) playing akey role in the correlations between the two areas At Hole953C G miotumida (Plate 2 Figures 6(10a) 6(10b) 6(12a)6(12b) and 6(12c)) is represented by a rich population fromthe bottom up to 34457mbsf (sample 157-953C-18R-3 965ndash985 cm) where it realizes the LRO In the overlying samplesG miotumida becomes rare up to its LO The last typicalspecimens were found at 34435mbsf (sample 18R-3 75ndash77 cm)

According to the literature these events directly postdatethe sinistral to dextral coiling change of N acostaensis Inthe Atlantic Ocean they have been recorded within subchronC3An1r the LRO in the Ain el Beida section was found inthe range of 6308ndash6311Ma [48] In the Mediterranean areathese events occur in the upper part of subchron C3An2n atFalconara section the LO was found at 6506Ma [52] and at651Ma by Blanc-Valleron et al [73] the LRO in the SorbasBasin at 6504Ma [45]

The progressively restricted connection between theAtlantic and Mediterranean during the Messinian was prob-ably responsible for the earlier disappearance of this speciesfrom the Mediterranean

Based on the previously mentioned micropaleontolog-ical observations (i) the change in coiling direction of Nacostaensis from left to right (637Ma [56]) and (ii) theLRO of G miotumida (631Ma [48]) occurred in the samelevel It follows that a hiatus is recorded in the Hole 953Cat 34457mbsf with an age span about 6436Ma to 6252MaAccording to Brunner et al [67] the top of Chron C3An2n


(6436Ma [56]) and the base of Chron C3An1n (6252Ma[56]) were apparently removed by slumping

413 First Occurrence of Globorotalia margaritae margaritaeThe First Occurrence of Globorotalia margaritae margaritaehas been more widely disputed because of the taxonomicalproblems related to its identification near the evolutionarytransition from its ancestor

It has been commonly used as marker for the earlyPliocene in the Mediterranean (eg [75 76 109ndash113]) inthe South Atlantic [114 115] and in the South Pacific [116ndash118] Also it was found in the uppermost Miocene of theMediterranean [98] North Atlantic [48 82 98 119] and East-ern Atlantic [91 92] within subchron C3An1r (immediatelyabove to disappearance of Globorotalia miotumida in theNorth Atlantic [82]) while Benson et al [97] reported theGmargaritae FO in themiddle of C3An2n in both Ain el Beidaand Sale cores Moreover Saito et al [120] recorded this eventwithin subchron C3An1n in theWestern Atlantic off Floridaequatorial Pacific and equatorial Indian Ocean

This event is astronomically dated at 608Ma [56] AtHole 953C G m margaritae (Plate 2 Figures 6(7a) 6(7b)6(8a) 6(8b) and 6(8c)) occurs firstly at 33611mbsf (sample17R-4 51ndash53 cm) but probably it is not the evolutive appear-ance of the taxon due to the underlying hiatus

Additional bioevent has been also recognized in theGloborotalia juanai LO at 33766mbsf which was recorded inthe Ain el Beida section in AEB 29 cycle by Krijgsman et al[48]

42 Calcareous Nannofossils

421 Last Occurrence of Nicklithus amplificus The impor-tance of the Last occurrence of Nicklithus amplificus as abiostratigraphic marker in the upper Miocene and its relia-bility for time stratigraphic correlation has been confirmedin studies of numerous deep-sea succession [8 121ndash123] theLO was found at 5978Ma in the ODP Site 925 and 926([124] and reference therein) at 5939Ma in the easternMediterranean ([124] and reference therein) and in the agerange of 5972ndash5975Ma in the Ain el Beida section [48]Thisevent occurs very close to the C3AnC3r Chron boundaryand marks the beginning of the Messinian Salinity Crisis [8]in the Mediterranean basins In the Hole 953C the LO of thisspecies is recorded at 33452mbsf (sample 157-953C-17R-342ndash44 cm)

422 Last Occurrence of Triquetrorhabdulus rugosus TheLast Occurrence of Triquetrorhabdulus rugosus is tradition-ally used for identifying the MiocenePliocene boundary inopen ocean areas and is considered an additional event torecognize the CN10aCN10b subzonal boundary [125] it isastronomically dated at 5279Ma and at 5255Ma in the low-latitude Atlantic [124] and in the Loulja section [34] respec-tively In the Mediterranean basin the T rugosus LO is notconsidered a useful biostratigraphic event because it is toorare in the samples Nevertheless it was identified in severalsuccessions just below the base of the Thvera subchron and

this bioevent is astronomically dated at 5279Ma [25 32124 126ndash129] According to the paleomagnetic stratigraphyT rugosus LO has a closely comparable stratigraphic positionin Atlantic and Mediterranean records and it can be usedto correlate the base of the Pliocene in its type area (EracleaMinoa sectionmdashSicily [130]) to the oceanic record At Hole953C the LO of this species occurred at 31273mbsf (samples157-953C-15R-2 63ndash65 cm)

Two additional bioevents have been also recognized (i)the Helicosphaera stalis ovata LO at 32578mbsf (sample 157-953C-16R-3 91ndash93 cm) that was recorded in the Ain el Beidasection between AEB38 and AEB 39 cycles by Krijgsman etal [48] and the (ii) Amaurolithus bizzarus FO at 304mbsf(sample 157-953C-14R-2 10ndash12 cm) astronomically dated at5033 in the Loulja section by van der Laan et al [34]

5 Cyclostratigraphy andAstronomical Calibration

51 Calcareous Plankton as Proxy for Identifying AstronomicalCyclicity According to Hilgen [54 55] and Hilgen et al [343] the high frequency alternations of different lithologiesrecognized throughout several Mediterranean land-basedsedimentary sequences have an origin related to the astro-nomical forcing For example the limestone-marl coupletswhich characterize the Lower Pliocene pelagic sediments(ldquoTrubi FmrdquoAuct Sicily) reflect the periodicity of the Earthrsquosprecession cycle (eg [53ndash55 127 128]) The marls wereconsidered as the ldquoequivalentrdquo of the sapropels characterizinghigher stratigraphic levels (ldquoM Narbonne Fmrdquo Auct Sicily)On this assumption Hilgen [54 55] proposed his astro-nomically calibrated time scale where marl layers (sapropelequivalents) are correlated to insolation maximaprecessionminima and limestones correspond to periods of higherproductivity induced by minima of the insolation curve(precession maxima)

In the absence of an evident lithological rhythm bioticproxies may be taken into account to highlight the astronom-ical cyclicity of a sedimentary succession In this frameworkcyclostratigraphy and astronomical tuning to the ATNTS[56] has been carried out by means of foraminifera-basedproxies (eg [62ndash66 131 132]) In particular the abundancescurves of GlobigerinoidesOrbulina gr neogloboquadrinidsand the ratio of warm-water versus cool-water species showMilankovitch periodicitiesThe relationship between selectedclimate-sensitive planktonic taxa and lithological cyclicitycorrelated in turn to astronomical cycles is well expressedin the lower Messinian deposits of Sicily Spain and Greece(Figure 3)

511 Globigerinoides In agreement with their unanimouslydeclared warm-climate affinity (eg [62ndash64 131]) the high-est abundances of the Globigerinoides population seem tocorrespond to maxima of the insolation cycles In the Sicil-ian ldquoTripoli Fmrdquo (Auct) consisting of a repetition of thesame lithological triplet (ldquosapropel typerdquo brown laminate-diatomite-marl) high frequencies of Globigerinoides grconcentrate within brown laminates and diatomitic layers


Insolationminus +

War

mc

old

Neog

lobo

quad

rinid

s

Glob

igerin

oide

sSicily

Marl

Diatomite

Sapropel

Marl

Diatomite

Sapropel

Marl

MarlDiatomite

Sapropel

Gavdos

SorbasGlobigerinoides+ orbulina

Figure 3 Relationship among astronomically forced lithologicalcycles abundances of selected planktonic foraminifera warmcoldratio and inferred insolation cycles in different Mediterraneansuccessions (Sicily Gavdos BasinmdashGreece Sorbas BasinmdashSpain)(Modified after [73 74])

corresponding to insolation maxima [73 133 134] whereaslowest frequencies fall within the middle part of the marlsA similar situation is recorded in the coeval sediments ofthe Gavdos Island (Greece [45 46 74 135]) where thebasic cycle is three-folded as well (sapropel-diatomite-marl)Here the highest abundances of Globigerinoides spp arerecorded within the sapropel and in lower-middle part ofthe diatomites In the Sorbas Basin (Southern Spain [46])the lower Messinian sediments of the upper Abad sectiondisplay quadruplet-type lithological cycles (sapropel-marl-diatomite-marl) In this case maxima abundances of Glo-bigerinoides spp + Orbulina spp are recorded in the middle-upper part of the sapropels or at the transition between thesapropel layers and the first marly horizons (Figure 3)

512 Neogloboquadrina Usually reported as cool taxa [136ndash138] neogloboquadrinids show an evident preference forstratified waters within high-productivity zone associatedwith the deep chlorophyll maximum (DCM) at the base ofthe euphotic zone [139ndash141]

The neogloboquadrinids show maxima frequencies incorrespondence of the topmost part of the diatomite andmarllayers in the Sicilian Tripoli [73 134] they generally reachthe highest percentages at the base of the first marl layer inthe upper Abad section [46 142] and within the diatomites

at Gavdos [74] (Figure 3) thus implying different parametersthan temperature controlling theirs distribution

513 WarmCold Ratio The ratio of warm-water ver-sus cool-water taxa using modern habitat characteristicsdescribed by Pujol and Grazzini [138] Lourens et al [53]Perez-Folgado et al [74] and Sierro et al [46] herein followsWarm-water taxa includeG decoraperta grG quadrilobatusgr G obliquus and O universa while Neogloboquadrina grG falconensis and G glutinata were taken as representativeof cool condition

G decoraperta gr (G decoraperta and G apertura) isnot living today but its descendant G rubescens is currentlyliving in subtropical and tropical environments This speciesusually grows in the surface nutrient-depleted waters ofthe mixed layer in oceanographic settings with a strongstratification in the water column [136 143 144]

In the Sorbas basin this group is abundant in the upperpart of the sapropels and the lower part of the diatomites onGavdos [74]

O universa behaves as G rubescens in the Sorbas basinand on Gavdos [74]

G falconensis is a species whose geographic depth andseasonal distribution patterns are poorly known because inthe literature it is grouped withG bulloides However studiesof planktonic foraminiferal assemblages from the westernNorth Atlantic [145] surface sediment data from the SouthAtlantic [146] and southern Indian Ocean [147] indicate thatthis species prefers to live in the cool subtropical regions

G glutinata is a ubiquitous species living in subarcticto subantarctic waters low in absolute amount but with ahigh percentage in waters with very low total foraminiferalconcentrations [143] This species is abundant in the homo-geneous marl-sapropel transitions both in the western andeastern Messinian Mediterranean [46 74]

Generally planktonic taxa indicative of warm nutrient-poor superficial waters are abundant in sapropels or sapro-pelitic layers whereas cold eutrophic deep-water forms char-acterize the homogeneousmarls or the diatomites [46 73 102148ndash150]

A close dependence between lithofacies and microfossilassemblages has been proved for sapropel-bearing succes-sions with by definition and the same microfossil assem-blages can be considered as sensitive to astronomical period-icity also in successions lacking sapropels Consequently theabundance variations of the after-mentioned taxa allowed theastronomically tunedwith the insolation curve of Laskar et al([104] La04

11solution)

Particularly insolation maxima-precession minima cor-respond to (i) maxima in the distribution patterns ofboth GlobigerinoidesOrbulina gr and warmcold ratio (ii)minima in the distribution patterns of neogloboquadrinids(Figure 4)

52 Astronomical Tuning The magnetic polarity reversal([67 70] and reference therein) and the bioevents recognizedin the Hole 953C have been used to correlate the studiedsedimentary records with Ain el Beida and Loulja sections


800

494

504

514

524

534

544

554

564

574

584

594

604

614

624

634

644

654

664

674

684

694

704

714

0 007400 5200 40 1000295

300

305

310

315

320

325

330

335

340

345

350

355

360

365

370

12345

6cc 12

cc

12

3cc

123

cc

12345

123

12

12345

6

13

Dep

th (m

bsf)

Core

Secti

on

14

15

16

17

18cc

cc19

20

ODP Hole 953C

Polar

ity

Chro

n

C3r

C3An

C3Ar

C3n4n

C3n3r

C3n3n

C3n2r

Eccentricity Insolation

4

14

59

101315

22

23

28

29

34

35

383940414243

(a)

(b)

(c)

(d)(e)

(f)

Ain el beidasection

A1A2A3A4A5A6A7A8A9A10A11A12A13A14A15A16A17A18A19

A20

A21

A22

A23

A24

A25

A26

A27

B1

B2

B3

B4

B5

B6

B7

B8

B9

C3r

AEB1AEB0AEB2AEB3AEB4AEB5AEB6AEB7AEB8AEB9AEB10AEB11AEB12

AEB13AEB14AEB15AEB16AEB17AEB18AEB19AEB20AEB21AEB22AEB23AEB24AEB25AEB26AEB27

AEB28AEB29AEB30AEB31

AEB32

AEB33AEB34AEB35

AEB37

AEB38

AEB36

AEB39

AEB40

AEB41

AEB42

AEB43

484 Ma

Neogloboquadrina grGlobigerinoidesorbulina gr Warmcold

Louljasections

La04 11 solution

[68 65]

Figure 4 Cartoon showing the tuning of the ODP Hole 953C with the insolation and eccentricity curves of La0411

solution [104] and thecorrelation to Ain el Beida and Loulja sections ([34 48] resp) Grey dotted lines represent the tendency lines of selected taxa and warmcoldratio curves The numbers from 1 to 43 refer to the lithological cycles Position of calcareous plankton bioevents (a) Neogloboquadrinaacostaensis coiling change andGloborotalia miotumida Last Regular Occurrence (b)Nicklithus amplificus Last Occurrence (c)Helicosphaerastalis ovata Last Occurrence (d)N acostaensis first influx sx (e) Triquetrorhabdulus rugosus Last Occurrence (f)Amaurolithus bizzarus FirstOccurrence

(Morocco) astronomically calibrated by Krijgsman et al [48]and van der Laan et al [34] respectivelyThe sinistraldextralN acostaensis coiling change the LO ofN amplificus and theLO of T rugosus are considered synchronous events whichwere used as tie points to calibrate astronomically the Hole953C sedimentary sequence The SD N acostaensis and theLO of N amplificus calibrated at 6378Ma and 5975Ma byKrijgsman et al [48] and the LO of T rugosus calibrated at5255Ma in cycle LA 15R (and [34]) were used as the startingpoint for tuning the sedimentary cycles at the Hole 953C Inaddition the LO ofHelicosphaera stalis ovata LO (recorded inthe Ain el Beida section by [48]) and the first sinistral influxofN acostaensis (recorded in Loulja section by [34]) are hereconsidered

Forty-three sedimentary cycles were recognized in theHole 953C (Figure 4) and are informally and progressivelynumbered from the base to the top of the studied interval

521 Chron C3An According to the literature the ChronC3An (6733Mandash6033Ma [56]) comprises thirty-two sedi-mentary cycles and corresponds to 700 kyrs At Hole 953C

only thirteen precession cycles (1ndash13) were recognized dueto (i) the 192m thick no-recovery interval in the core 17Rwhich covers a time interval of 0088Ma (ii) the hiatusidentified at 34457mbsf with an age span about 6436Ma to6252Ma The cycles are highlighted by positive fluctuationsof GlobigerinoidesOrbulina gr-warmcold ratio which arein opposite phase respect to the fluctuations of Neoglobo-quadrina gr Cycles 6 to 8 fit excellently with the high-amplitude fluctuations of the eccentricity curve According toKrijgsman et al [48] maxima in eccentricity enhance climatefluctuations on a precessional scale because the eccentricitymodulates the precession amplitude favouring the formationof distinct cycles

522 Chron C3r The Chron C3r (5235Mandash6033Ma [56])comprises a total number of twenty-seven sedimentary cyclesand corresponds to 798 kyrs in according to the ATNTS2004[56] Twenty precession cycles (14ndash33) are recognized owingto the no-recovery interval in the cores 16 (486m thick)and 15 (602m thick) that covers a time interval of 01578Maand 0208Ma respectively The cycles are highlighted by the


Figure 5

abundance peaks of GlobigerinoidesOrbulina gr-warmcoldratio signal which are in opposite phase with Neoglobo-quadrina gr distribution (except the cycles 20 and 22)Moreover cycles 14 17 and 20 fit excellently with the high-amplitude fluctuations of the eccentricity curveThe increasein thickness of cycles 24 and 27 has been interpreted as a

change in the sedimentation rate Additionally the cycle 27is interpreted as ldquodouble cyclerdquo due by the fluctuations of thefaunal proxies like cycle AEB 41 from Ain el Beida [48]

In this interval the recorded bioevents are (i) the LOof N amplificus in the cycle 17 at the astronomical age of5979Ma (ii) the LO of H stalis ovata in the cycle 24 at the


Figure 6

astronomical age of 5681Ma (iii) the presence of Discoasterquinqueramus in the cycle 28 which corresponds to cycleAEB 42 of Ain el Beida section [48] (iv) the first sinistralinflux of N acostaensis in the cycle 30 at the astronomicalage of 5297Ma (v) the LO of T rugosus in the cycle 33 atthe astronomical age of 5244Ma The recognition of theselast two bioevents and the base of the Thvera magnetic eventare a useful guide to identify theMiocenePliocene boundaryin the interval studied Since from a cyclostratigraphic

perspective the boundary fallswithin the insolation cycle 510five precessional cycles below theThveramagnetic event andhas an astrochronological age of 5332Ma [53]

523 Chron C3n4n The Chron C3n4n (4997Mandash5235Ma [56]) comprises a total number of ten sedimentarycycles corresponding to 238 kyrs according to theATNTS2004 In this interval the relation betweenwarmcoldratio maxima versus neogloboquadrinids minima allowed


to identified only five precession cycles (35ndash39) becauseof no-recovery interval in the core 14 (697m thick) thatcovers a time interval of 012Ma In particular cycles36-37 fit excellently with the high-amplitude fluctuationsof the eccentricity curve In this interval the Globigeri-noidesOrbulina gr signal is not clear or completely absentIn the cycle 37 the FO of A bizzarus is recognized and it hasan astronomical age of 5038Ma corresponding to cycle LB2R of Loulja section [34]

524 Chron C3n3r In the literature the Chron C3n3r(4896Mandash4997Ma [56]) comprises a total number of 45sedimentary cycles and corresponds to 101 Kyrs accordingto the ATNTS2004 Three precession cycles (39ndash41) arerecognized owing to the 143m thick no-recovery interval inthe core 13 cover a time interval of 0044Ma The cycles arehighlighted by two negative fluctuations ofNeogloboquadrinagr that are in opposite phase with those of the warmcoldratio GlobigerinoidesOrbulina gr signals In the cycle 39 thepresence of H sellii suggests a correspondence to cycle LB 6of Loulja section [34]

525 Chron C3n3n In the literature the Chron C3n3n(4799Mandash4896Ma [56]) comprises a total number of 25sedimentary cycles and corresponds to 97 kyrs accordingto the ATNTS2004 The cycles (42-43) are highlighted bytwo negative fluctuations of Neogloboquadrina gr whichare in opposite phase with those of the warmcold ratioGlobigerinoidesOrbulina gr signals Finally the increase inthickness of the cycles has been interpreted as a change in thesedimentation rate

6 Conclusion

This paper presents the results of qualitative and quantitativeanalyses of the calcareous plankton assemblages carriedout in tract of the Hole 953C succession encompassing theMessinian to early Zanclean The study allowed to recognizeten important bioevents well calibrated and widely usedin the Mediterranean and Atlantic correlation Moreover acyclostratigraphic approach has been attempted to obtain adetailed chronostratigraphic subdivision Lacking any evi-dent lithological cyclicity and the no-recovery intervalsalong the succession the combination of climate sensitiverecords allowed to extract signals of the astronomical cyclic-ities The fluctuations curves of GlobigerinoidesOrbulinagr neogloboquadrinids and the ratio of warm-water ver-sus cool-water species highlight a frequency indicative ofthe Earthrsquos precession periodicity Particularly the insola-tion curve is in phase with the GlobigerinoidesOrbulinagr and warmcold ratio distribution and is in antiphasewith the Neogloboquadrina gr curve As result forty-threeprecession-controlled cycles have been recognized spanningfrom 6457Ma to 4799Ma

Description of Plates 1 and 2

Plate 1 (see Figure 5)

(1) Neogloboquadrina acostaensis (Blow) umbilical viewsample 953C-13R-3 8ndash10 cm

(2) Neogloboquadrina acostaensis (Blow) (a) umbilicalview (b) spiral view (c) ultrastructure sample 953C-13R-3 8ndash10 cm

(3) Neogloboquadrina pachyderma (Ehrenberg) (a) um-bilical view (b) spiral view sample 953C-18R-2 98ndash100 cm

(4) Neogloboquadrina pachyderma (Ehrenberg) (a) um-bilical view (b) spiral view (c) ultrastructure sample953C-19R-1 245ndash265 cm


(6) Neogloboquadrina pachyderma (Ehrenberg) umbili-cal view sample 953C-17R-3 57ndash59 cm

(7) Neogloboquadrina dutertrei humerosa (Takayanagiand Saito) umbilical view sample 953C-13R-2 1405ndash1425 cm

(8) Neogloboquadrina dutertrei humerosa (Takayanagiand Saito) (a) umbilical view (b) spiral view (c)ultrastructure sample 953C-13R-3 26ndash28 cm

(9) Neogloboquadrina dutertrei humerosa (Takayanagiand Saito) (a) umbilical view (b) spiral view sample953C-12R-2 415ndash435 cm

(10) Neogloboquadrina dutertrei blowi Rogl and Bolli um-bilical view sample 953C-13R-3 91ndash93 cm

(11) Neogloboquadrina dutertrei blowi Rogl and Bolli (a)umbilical view (b) spiral view (c) ultrastructuresample 953C-16R-1 38ndash40 cm


(1) Globorotalia scitula (Brady) (a) umbilical view (b)side view (c) spiral view sample 953C-17R-2 12ndash14 cm

(2) Globorotalia juanaiBermudez and Bolli (a) umbilicalview (b) side view (c) spiral view sample 953C-18R-375ndash77 cm



(5) Globorotalia margaritae primitiva Cita (a) umbilicalview (b) side view (c) spiral view sample 953C-17R-1 80ndash82 cm


(7) Globorotalia margaritae margaritae Bolli and Ber-mudez (a) umbilical view (b) side view sample 953C-16R-3 745ndash765 cm


(8) Globorotalia margaritae margaritae Bolli and Ber-mudez (a) umbilical view (b) side view (c) spiralview sample 953C-13R-4 147ndash149

(9) Globorotalia cibaoensis Bermudez (a) umbilical view(b) side view (c) spiral view sample 953C-16R-1 128ndash130 cm

(10) Globorotalia miotumida Jenkins (a) umbilical view(b) spiral view


(12) Globorotalia miotumida Jenkins (a) umbilical view(b) side view (c) spiral view

(13) Globorotalia menardii (Parker Jones and Brady) (a)umbilical view (b) side view (c) spiral view sample953C-16R-2 1445ndash1465 cm

(14) Globorotalia multicamerata Cushman and Jarvis (a)umbilical view (b) side view (c) spiral view sample953C-13R-3 415ndash435 cm


For quantitative data of ODP Hole 953C planktonicforaminifera see Tables 1 and 2 of the Supplementary Mate-rial available online at httpdxdoiorg1011552013947839

Acknowledgments

The author is particularly grateful to Gianfranco Salvatorinifor discussing data for his helpful comments support andencouragement She thanks Niccolo Baldassini for calcareousnannoplankton analyses She is grateful toHugoCorbı and ananonymous reviewer for their critical reading of the paperSamples for this study were obtained through the courtesyof the Integrated Ocean Drilling Program This paper isdedicated to whom is no longer with us and to whom willcome soon

References

[1] W B F Ryan ldquoQuantitative evaluation of the depth of the west-ern Mediterranean before during and after the late Miocenesalinity crisisrdquo Sedimentology vol 23 pp 791ndash813 1976

[2] R W H Butler W H Lickorish M Grasso H M Pedley andL Ramberti ldquoTectonics and sequence stratigraphy inMessinianbasins Sicily constraints on the initiation and termination ofthe Mediterranean salinity crisisrdquo Geological Society of AmericaBulletin vol 107 no 4 pp 425ndash439 1995

[3] F J Hilgen W Krijgsman C G Langereis L J Lourens ASantarelli and W J Zachariasse ldquoExtending the astronomical(polarity) time scale into the Miocenerdquo Earth and PlanetaryScience Letters vol 136 no 3-4 pp 495ndash510 1995

[4] J P Suc D Violanti L Londeix et al ldquoEvolution of theMessinianMediterranean environments the Tripoli Formationat Capodarso (Sicily Italy)rdquo Review of Palaeobotany and Paly-nology vol 87 no 1 pp 51ndash79 1995

[5] G Clauzon J P Suc F Gautier A Berger and M F LoutreldquoAlternate interpretation of the Messinian salinity crisis con-troversy resolvedrdquo Geology vol 24 no 4 pp 363ndash366 1996

[6] R Riding J C Braga J M Martın and I M Sanchez-AlmazoldquoMediterranean Messinian salinity crisis constraints from acoeval marginal basin Sorbas southeastern Spainrdquo MarineGeology vol 146 no 1ndash4 pp 1ndash20 1998

[7] W Krijgsman F J Hilgen S Marabini and G B Vai ldquoNewpaleomagnetic and cyclostratigraphic age constraints on theMessinian of the Northern Apennines (Vena del Gesso BasinItaly)rdquoMemorie della Societa Geologica Italiana vol 54 pp 25ndash33 1999

[8] W Krijgsman F J Hilgen I Raffi F J Sierro and D S WilsonldquoChronology causes and progression of the Messinian salinitycrisisrdquo Nature vol 400 no 6745 pp 652ndash655 1999

[9] M Roveri M A Bassetti and F Ricci Lucchi ldquoThe mediter-raneanMessinian salinity crisis anApennine foredeep perspec-tiverdquo Sedimentary Geology vol 140 no 3-4 pp 201ndash214 2001

[10] M Roveri V Manzi F Ricci Lucchi and S Rogledi ldquoSedi-mentary and tectonic evolution of the Vena del Gesso basin(Northern Apennines Italy) implications for the onset of theMessinian salinity crisisrdquoGeological Society of America Bulletinvol 115 pp 387ndash405 2003

[11] M Roveri S Lugli V Manzi and B C Schreiber ldquoTheMessinian Salinity Crisis a sequence-stratigraphy approachrdquoGeoActa Special Publication vol 1 pp 117ndash138 2008

[12] J Lofi C Gorini S Berne et al ldquoErosional processes andpaleo-environmental changes in theWestern Gulf of Lions (SWFrance) during the Messinian Salinity Crisisrdquo Marine Geologyvol 217 no 1-2 pp 1ndash30 2005

[13] J Lofi F Sage J Deverchere et al ldquoRefining our knowledgeof the Messinian salinity crisis records in the offshore domainthrough multi-site seismic analysisrdquo Bulletin de la SocieteGeologique de France vol 182 no 2 pp 163ndash180 2011

[14] V Manzi S Lugli F R Lucchi and M Roveri ldquoDeep-waterclastic evaporites deposition in theMessinian Adriatic foredeep(northern Apennines Italy) did the Mediterranean ever dryoutrdquo Sedimentology vol 52 no 4 pp 875ndash902 2005

[15] F Sage G Von Gronefeld J Deverchere V Gaullier AMaillard and C Gorini ldquoSeismic evidence for Messiniandetrital deposits at the western Sardinia margin northwesternMediterraneanrdquoMarine and Petroleum Geology vol 22 no 6-7pp 757ndash773 2005

[16] A Maillard C Gorini A Mauffret F Sage J Lofi andV Gaullier ldquoOffshore evidence of polyphase erosion in theValencia Basin (Northwestern Mediterranean) scenario for theMessinian Salinity Crisisrdquo Sedimentary Geology vol 188-189pp 69ndash91 2006

[17] F Orszag-Sperber ldquoChanging perspectives in the concept ofldquoLago-Marerdquo in Mediterranean Late Miocene evolutionrdquo Sedi-mentary Geology vol 188-189 pp 259ndash277 2006

[18] C Bertoni and J A Cartwright ldquoMajor erosion at the end ofthe Messinian salinity crisis evidence from the Levant basineastern Mediterraneanrdquo Basin Research vol 19 no 1 pp 1365ndash2117 2007

[19] K J Hsu W B F Ryan and M B Cita ldquoLate miocenedesiccation of themediterraneanrdquoNature vol 242 no 5395 pp240ndash244 1973

[20] M B Cita R C Wright W B F Ryan and A LonginellildquoMessinian paleoenvironmentsrdquo in Initial Reports of the DeepSea Drilling Project K J Hsu L Montadert D Bernoulli et alEds vol 42 pp 1003ndash1035 1978


[21] K J Hsu L Montadert D Bernouilli et al ldquoHistory of theMediterranean salinity crisisrdquo in Initial Reports of the Deep SeaDrilling Project K J Hsu LMontadert D Bernoulli et al Edsvol 42A pp 1053ndash1078 1978

[22] A Bossio L Giannelli R Mazzanti R Mazzei and G Salva-torini ldquoGli strati alti del Messiniano il passaggio MiocenemdashPliocene e la sezione plio-pleistocenica di Nugola nelle collinea NE dei Monti Livornesirdquo in IX Convegno della SocietaPaleontologica Italiana pp 55ndash90 Pacini Pisa Italy 1981

[23] J AMcKenzie and R Sprovieri ldquoPaleoceanographic conditionsfollowing the earliest Pliocene flooding of the Tyrrhenian Seardquoin Proceedings of the Ocean Drilling Program Scientific ResultsK A Kastens J Mascle C Auroux et al Eds vol 107 pp 405ndash414 1990

[24] A R Fortuin J M D Kelling and T B Roep ldquoThe enigmaticMessinian-Pliocene section of Cuevas del Almanzora (VeraBasin SE Spain) revisited-erosional features and strontiumisotope agesrdquo Sedimentary Geology vol 97 no 3-4 pp 177ndash2011995

[25] E Di Stefano R Sprovieri and S Scarantino ldquoChronology ofbiostratigraphic events at the base of the PliocenerdquoPaleopelagosvol 6 pp 401ndash414 1996

[26] F Sgarrella R Sprovierp E Di Stefano and A CarusoldquoPaleoceanographic conditions at the base of the Pliocene in theSouthern Mediterranean Basinrdquo Rivista Italiana di Paleontolo-gia e Stratigrafia vol 103 no 2 pp 207ndash220 1997

[27] S Spezzaferri M B Cita and J A McKenzie ldquoThe MiocenemdashPliocene boundary in the eastern Mediterranean results fromODP Leg 160 Sites 967 and 969rdquo in Proceedings of the OceanDrilling Program Scientific Results A H F Robertson K-CEmeis C Richter and A Camerlenghi Eds vol 160 pp 9ndash281998

[28] S Iaccarino D Castradori M B Cita et al ldquoTheMiocenePliocene boundary and the significance of theearliest Pliocene flooding in the MediterraneanrdquoMemorie dellaSocieta Geologica Italiana vol 54 pp 109ndash131 1999

[29] S M Iaccarino M B Cita S Gaboardi and G M Grup-pini ldquoHigh-resolution biostratigraphy at the MiocenePlioceneboundary in Holes 974B and 975B Western Mediterraneanrdquo inProceedings of the Ocean Drilling Program Scientific Results RZahn M C Comas and A Klaus Eds vol 161 pp 197ndash2211999

[30] SM Iaccarino andA Bossio ldquoPaleoenvironment of uppermostMessinian sequences in the western Mediterranean (sites 974975 and 978)rdquo in Proceedings of the Ocean Drilling ProgramScientific Results R ZahnM C Comas and A Klaus Eds vol161 pp 529ndash540 1999

[31] E Di Stefano M B Cita S Spezzaferri and R SprovierildquoThe Messinian-Zanclean Pissouri Section (Cyprus easternMediterranean)rdquoMemorie della Societa Geologica Italiana vol118 pp 133ndash144 1999

[32] F Sgarrella R Sprovieri E Di Stefano A Caruso M Sprovieriand G Bonaduce ldquoThe Capo Rossello bore-hole (AgrigentoSicily) cyclostratigraphic and paleoceanographic reconstruc-tions from quantitative analyses of the Zanclean foraminiferalassemblagesrdquo Rivista Italiana di Paleontologia e Stratigrafia vol105 no 2 pp 303ndash322 1999

[33] C Pierre A Caruso M M Blanc-Valleron J M Rouchy andF Orzsag-Sperber ldquoReconstruction of the paleoenvironmentalchanges around the Miocene-Pliocene boundary along a West-East transect across the Mediterraneanrdquo Sedimentary Geologyvol 188-189 pp 319ndash340 2006

[34] E Van Der Laan E Snel E De Kaenel F J Hilgen andW Krijgsman ldquoNo major deglaciation across the Miocene-Pliocene boundary integrated stratigraphy and astronomicaltuning of the Loulja sections (Bou Regreg area NWMorocco)rdquoPaleoceanography vol 21 no 3 Article ID PA3011 2006

[35] C Pierre J M Rouchy and M M Blanc-Valleron ldquoSedimen-tological and stable isotope changes at the MessinianPlioceneboundary in the eastern Mediterranean Holes 968A 969Aand 969Brdquo Proceedings of the Ocean Drilling Program ScientificResults vol 160 pp 3ndash8 1998

[36] J Aguirre and I M Sanchez-Almazo ldquoThe Messinian post-evaporitic deposits of the Gafares area (Almerıa-Nıjar basinSE Spain) A new view of the ldquoLago-Marerdquo faciesrdquo SedimentaryGeology vol 168 no 1-2 pp 71ndash95 2004

[37] J C Braga J M Martın R Riding J Aguirre I MSanchez-Almazo and J Dinares-Turell ldquoTesting models for theMessinian salinity crisis the Messinian record in Almerıa SESpainrdquo Sedimentary Geology vol 188-189 pp 131ndash154 2006

[38] G Carnevale W Landini and G Sarti ldquoMare versus Largo-mare marine fishes and the Mediterranean environment at theend of the Messinian Salinity Crisisrdquo Journal of the GeologicalSociety vol 163 no 1 pp 75ndash80 2006

[39] F Bache J L Olivet C Gorini et al ldquoMessinian erosional andsalinity crises view from the Provence Basin (Gulf of LionsWestern Mediterranean)rdquo Earth and Planetary Science Lettersvol 286 no 1-2 pp 139ndash157 2009

[40] F Bache S-M Popescu M Rabineau et al ldquoA two-step processfor the reflooding of the Mediterranean after the MessinianSalinity Crisisrdquo Basin Research vol 24 pp 125ndash153 2012

[41] S M Popescu F Dalesme G Jouannic et al ldquoGaleacystaetrusca complex dinoflagellate cyst marker of Paratethyaninfluxes into the Mediterranean Sea before and after the peakof the Messinian Salinity Crisisrdquo Palynology vol 33 no 2 pp105ndash134 2009

[42] F J Hilgen L Bissoli S Iaccarino et al ldquoIntegrated stratigraphyand astrochronology of the Messinian GSSP at Oued Akrech(Atlantic Morocco)rdquo Earth and Planetary Science Letters vol182 no 3-4 pp 237ndash251 2000

[43] F J Hilgen W Krijgsman I Raffi E Turco and W JZachariasse ldquoIntegrated stratigraphy and astronomical calibra-tion of the SerravallianTortonian boundary section at MonteGibliscemi (Sicily Italy)rdquoMarineMicropaleontology vol 38 no3-4 pp 181ndash211 2000

[44] N J Shackleton and S Crowhurst ldquoSediment fluxes based onorbital tuned time scale 5 Ma to 14 Ma Site 926rdquo in Proceedingsof the OceanDrilling Program Scientific Results N J ShackletonW B Curry et al Eds vol 154 pp 69ndash82 1997

[45] F J Sierro F J Hilgen W Krijgsman and J A Flores ldquoTheAbad composite (SE Spain) a Messinian reference section forthe Mediterranean and the APTSrdquo Palaeogeography Palaeocli-matology Palaeoecology vol 168 no 1-2 pp 141ndash169 2001

[46] F J Sierro J A Flores G Frances et al ldquoOrbitally-controlledoscillations in planktic communities and cyclic changes inwestern Mediterranean hydrography during the MessinianrdquoPalaeogeography Palaeoclimatology Palaeoecology vol 190 pp289ndash316 2003

[47] L Vidal T Bickert GWefer and U Rohl ldquoLate Miocene stableisotope stratigraphy of SE Atlantic ODP Site 1085 relation toMessinian eventsrdquoMarine Geology vol 180 no 1ndash4 pp 71ndash852002

[48] W Krijgsman S Gaboardi F J Hilgen S Iaccarino E DeKaenel and E van der Laan ldquoRevised astrochronology for the


Ain el Beida section (AtlanticMorocco) no glacio-eustatic con-trol for the onset of the Messinian salinity crisisrdquo Stratigraphyvol 1 no 1 pp 87ndash101 2004

[49] J C Larrasoana J A Gonzalez-Delgado J Civis F J Sierro GAlonso-Gavilan and J Pais ldquoMagnetobiostratigraphic datingand environmental magnetism of Late Neogene marine sedi-ments recovered at the Huelva-1 and Montemayor-1 boreholes(lowerGuadalquivir basin Spain)rdquoGeo-Temas vol 10 pp 1175ndash1178 2008

[50] J N Perez-Asensio J Aguirre G Schmiedl and J CivisldquoMessinian paleoenvironmental evolution in the lowerGuadalquivir Basin (SW Spain) based on benthic foraminiferardquoPalaeogeography Palaeoclimatology Palaeoecology vol 326ndash328 pp 135ndash151 2012

[51] J N Perez-Asensio J Aguirre G Schmiedl and J CivisldquoImpact of restriction of the Atlantic-Mediterranean gatewayon the Mediterranean Outflow Water and eastern Atlanticcirculation during the Messinianrdquo Paleoceanography vol 272012

[52] F J Hilgen and W Krijgsman ldquoCyclostratigraphy andastrochronology of the Tripoli diatomite formation (pre-evaporite Messinian Sicily Italy)rdquo Terra Nova vol 11 no 1 pp16ndash22 1999

[53] L J Lourens A Antonarakou F J Hilgen A A M Van HoofC Vergnaud-Grazzini and W J Zachariasse ldquoEvaluation ofthe Plio-Pleistocene astronomical timescalerdquoPaleoceanographyvol 11 no 4 pp 391ndash413 1996

[54] F J Hilgen ldquoAstronomical calibration of Gauss to Matuyamasapropels in the Mediterranean and implication for the Geo-magnetic Polarity Time Scalerdquo Earth and Planetary ScienceLetters vol 104 no 2ndash4 pp 226ndash244 1991

[55] F J Hilgen ldquoExtension of the astronomically calibrated (polar-ity) time scale to the MiocenePliocene boundaryrdquo Earth andPlanetary Science Letters vol 104 pp 211ndash225 1991

[56] L Lourens F Hilgen N J Shackleton J Laskar and J WilsonldquoOrbital tuning calibrations and conversions for the NeogenePeriodrdquo in A Geological Timescale 2004 F Gradstein J Oggand A Smith Eds pp 469ndash484 Cambridge University PressCambridge UK 2004

[57] N J Shackleton J G Baldauf J A Flores T C Moore I Raffiand E Vincent ldquoBiostratigraphic summary for LEG 138rdquo inProceedings of the Ocean Drilling Program Scientific Results NG Pias L A Mayer T R Janecek et al Eds vol 138 pp 517ndash533 1995

[58] F J Hilgen H Abdul Aziz W Krijgsman I Raffi and ETurco ldquoIntegrated stratigraphy and astronomical tuning of theSerravallian and lower Tortonian at Monte dei Corvi (Middle-Upper Miocene northern Italy)rdquo Palaeogeography Palaeocli-matology Palaeoecology vol 199 no 3-4 pp 229ndash264 2003

[59] F Hilgen H Brinkhuis and W J Zachariasse ldquoUnit strato-types for global stages the Neogene perspectiverdquo Earth-ScienceReviews vol 74 no 1-2 pp 113ndash125 2006

[60] S K Husing F J Hilgen H Abdul Aziz and W KrijgsmanldquoCompleting theNeogene geological time scale between 85 and125 Mardquo Earth and Planetary Science Letters vol 253 no 3-4pp 340ndash358 2007

[61] F J Hilgen H Abdul Aziz W Krijgsman et al ldquoPresent statusof the astronomical (polarity) time-scale for the MediterraneanLateNeogenerdquo Philosophical Transactions of the Royal Society Avol 357 no 1757 pp 1931ndash1947 1999

[62] R Sprovieri ldquoMediterranean Pliocene biochronology an highresolution record based on quantitative planktonic foraminifera

distributionrdquo Rivista Italiana di Paleontologia e Stratigrafia vol98 no 1 pp 61ndash100 1992

[63] R Sprovieri ldquoPliocene-early Pleistocene astronomically forcedplanktonic foraminifera abundance fluctuations and chronol-ogy of Mediterranean calcareous plankton bio-eventsrdquo RivistaItaliana di Paleontologia e Stratigrafia vol 99 no 3 pp 371ndash4141993

[64] A Caruso ldquoClimatic Change During Upper PlioceneLowerPleistocene at Capo Rossello (Sicily Italy) a plankticforaminifers approachrdquo in Proceedings of the 1st ItalianMeeting on Environmental Micropaleontology GrybowskiFoundation Special Pubblication R Coccioni S Galeotti andF Lirer Eds vol 9 pp 17ndash36 2004

[65] F Riforgiato L M Foresi M Aldinucci et al ldquoForaminiferalrecord and astronomical cycles an example from theMessinianpre-evaporitic Gello composite section (Tuscany Italy)rdquo Stratig-raphy vol 5 no 3-4 pp 265ndash280 2008

[66] F Riforgiato L M Foresi A Di Stefano et al ldquoTheMiocenePliocene boundary in the Mediterranean area newinsights from a high-resolution micropalaeontological andcyclostratigraphical study (Cava Serredi section Central Italy)rdquoPalaeogeography Palaeoclimatology Palaeoecology vol 305 no1ndash4 pp 310ndash328 2011

[67] C Brunner J Sblendorio-Levy R Maniscalco et al ldquoBios-tratigraphic and Magnetostratigraphic evaluation of Sites 953954 955 and 956 Canary Islandsrdquo in Proceedings of theOcean Drilling Program Initial Reports P P E Weaver H-USchmincke J V Firth and W Duffield Eds vol 157 pp 97ndash114 1998

[68] R Maniscalco and C A Brunner ldquoNeogene and Quaternaryplanktonic foraminiferal biostratigraphy of the Canary Islandregionrdquo in Proceedings of the Ocean Drilling Program InitialReports P P E Weaver H-U Schmincke J V Firth and WDuffield Eds vol 157 pp 115ndash124 1998

[69] ldquoShipboard Scientific Party Site 953rdquo in Proceedings of theOcean Drilling Program Initial Reports H-U Schminke P P EWeaver J V Firth et al Eds vol 157 pp 317ndash394 1995

[70] H-U Schmincke P P E Weaver and J V Firth Proceedings oftheOceanDrilling Program Initial Reports vol 157ODPCollegeStation Tex USA 1995

[71] T J Kouwenhoven C Morigi A Negri S Giunta W Kri-jgsman and J M Rouchy ldquoPaleoenvironmental evolution ofthe eastern Mediterranean during the Messinian constraintsfrom integratedmicrofossil data of the Pissouri Basin (Cyprus)rdquoMarine Micropaleontology vol 60 no 1 pp 17ndash44 2006

[72] F Rogl and H M Bolli ldquoHolocene to Pleistocene planktonicforaminifera of Leg 15 Site 147 (Cariaco Basin (Trench)Caribbean Sea) and their climatic interrelationrdquo Initial Reportsof the Deep Sea Drilling Project vol 15 pp 553ndash615 1973

[73] MM Blanc-Valleron C Pierre J P Caulet et al ldquoSedimentarystable isotope and micropaleontological records of paleoceano-graphic change in the Messinian Tripoli Formation (sicilyItaly)rdquo Palaeogeography Palaeoclimatology Palaeoecology vol185 no 3-4 pp 255ndash286 2002

[74] M Perez-Folgado F J Sierro M A Barcena et al ldquoWest-ern versus eastern Mediterranean paleoceanographic responseto astronomical forcing a high-resolution microplanktonstudy of precession-controlled sedimentary cycles during theMessinianrdquo Palaeogeography Palaeoclimatology Palaeoecologyvol 190 pp 317ndash334 2003


[75] W J Zachariasse ldquoPlanktonic foraminiferal biostratigraphy ofthe Late Neogene of Crete (Greece)rdquo Utrecht MicropaleontologyBulletin vol 11 1975

[76] C Montenat G Bizon and J J Bizon ldquoContinuite oudiscontinuite de sedimentation marine mio-pliocene enMediterranee occidentale Lrsquoexemple du bassin de Vera(Espagne meridionale)rdquo Revue de lrsquoInstitut Francais du Petrolevol 31 pp 613ndash663 1976

[77] J Civis J Martinell and J de Porta ldquoMicrofauna del Miocenoterminal de la Rambla de Arejos (Almeria)rdquo Studia Geologicavol 15 pp 37ndash55 1979

[78] M L Colalongo A Di-Grande S DrsquoOnofrio et al ldquoStratig-raphy of Late Miocene Italian sections straddling the Torto-nianMessinian boundaryrdquo Bollettino della Societa Paleontolog-ica Italiana vol 18 no 2 pp 258ndash302 1979

[79] S Iaccarino and G Salvatorini ldquoA framework of plank-tonic foraminiferal biostratigraphy for Early Miocene to LatePliocene Mediterranean areardquo Paleontologia Stratigrafica edEvoluzione Quad vol 2 pp 115ndash125 1982

[80] S Iaccarino ldquoMediterranean Miocene and Pliocene plankticforaminiferardquo in Plankton Stratigraphy H M Bolli J BSaunders and K Perch-Nielsen Eds pp 283ndash314 CambridgeUniversity Press New York NY USA 1985

[81] H M Van De Poel ldquoMessinian stratigraphy of the Nijar Basin(SE Spain) and the origin of its gypsum-ghost limestonesrdquoGeologie en Mijnbouw vol 70 no 3 pp 215ndash234 1991

[82] F J Sierro J A Flores J Civis J A Gonzalez Delgado andG Frances ldquoLate Miocene globorotaliid event-stratigraphy andbiogeography in the NE-Atlantic and Mediterraneanrdquo MarineMicropaleontology vol 21 no 1ndash3 pp 143ndash167 1993

[83] F J Sierro J A Flores I Zamarreno et al ldquoAstronomicalcyclicity and sapropels in the pre-evaporitic Messinian of theSorbas Basin (Western Mediterranean)rdquo Geogaceta vol 21 pp131ndash134 1997

[84] F Gautier G Clauzon J P Suc J Cravatte andD Violanti ldquoAgeand duration of theMessinian salinity crisisrdquoComptes RendusmdashAcademie des Sciences Serie II vol 318 no 8 pp 1103ndash11091994

[85] R Sprovieri E Di Stefano A Caruso and S Bonomo ldquoHighresolution stratigraphy in the Messinian Tripoli Formation inSicilyrdquo Paleopelagos vol 6 pp 415ndash435 1996

[86] R Sprovieri E Di Stefano and M Sprovieri ldquoHigh resolu-tion chronology for late miocene mediterranean stratigraphiceventsrdquo Rivista Italiana di Paleontologia e Stratigrafia vol 102no 1 pp 77ndash104 1996

[87] H Feinberg and H G Lorenz ldquoNouvelles donnees strati-graphiques su le Miocene superieur et le Pliocene de Maroc-occidentalrdquo Notes et Memoires du Service Geologique du Marocvol 30 no 225 pp 21ndash26 1970

[88] R M Stainforth J L Lamb H Luterbacher J H Beard and RM Jeffords ldquoCenozoic Planktonic zonation and characteristicsof Index formsrdquo University of Kansas Paleontological Contribu-tions vol 62 1975

[89] A Bossio K Rakic El-Beid L Giannelli R Mazzei ARusso and G Salvatorini ldquoCorrelation de quelques sectionsstratigraphiques du Mio-Pliocene de la zone Atlantique duMaroc avec les stratotypes du Bassin Mediterraneen sur labase des Foraminiferes planctoniques Nannoplancton calcaireet Ostracodesrdquo Atti della Societa Toscana di Scienze NaturaliMemorie vol 83 pp 121ndash137 1976

[90] M B Cita and W B F Ryan ldquoThe Bou Regreg section of theAtlantic coast of Morocco evidence timing and significance of

a late Miocene regressive phaserdquo Rivista Italiana di Paleontolo-gia vol 84 pp 1051ndash1082 1978

[91] R Mazzei I Raffi D Rio N Hamilton and M B CitaldquoCalibration of the late Neogene calcareous plankton datumplaneswith the paleomagnetic record of Site 397 and correlationwith Moroccan and Mediterranean sectionsrdquo Initial Reports ofthe Deep Sea Drilling Project vol 47 no 1 pp 375ndash389 1979

[92] G Salvatorini and M B Cita ldquoMiocene foraminiferal stratig-raphy DSDP Site 397 (Cape Bojador North Atlantic)rdquo InitialReports of theDeep SeaDrilling Project vol 47 pp 317ndash373 1979

[93] F J Sierro Foraminiferos planctonicos y bioestratigrafıa delMioceno superior-Plioceno del borde occidental de la cuencadel Guadalquivir (SO de Espana) [dissertation] Universidad deSalamanca 1984

[94] D A Hodell R H Benson J P Kennett and K Rakic-ElBied ldquoStable isotope stratigraphy of latest Miocene sequencesin northwest Morocco the Bou Regreg Sectionrdquo Paleoceanog-raphy vol 4 no 4 pp 467ndash482 1989

[95] D A Hodell J H Curtis F J Sierro andM E Raymo ldquoCorre-lation of late Miocene to early Pliocene sequences between theMediterranean and North Atlanticrdquo Paleoceanography vol 16no 2 pp 164ndash178 2001

[96] R H Benson K Rakic-El Bied and G Bonaduce ldquoAnimportant current reversal (influx) in the Rifian Corridor(Morocco) at the Tortonian-Messinian boundary the end ofTethys Oceanrdquo Paleoceanography vol 6 no 1 pp 165ndash192 1991

[97] R H Benson L A C Hayek D A Hodell and K Rakic-ElBied ldquoExtending the climatic precession curve back into the lateMiocene by signature template comparisonrdquo Paleoceanographyvol 10 no 1 pp 5ndash20 1995

[98] R H Benson and K Rakic-El Bied ldquoThe Bou Regreg sectionMorocco proposed global boundary stratotype section andpoint of the PliocenerdquoNotes et Memoires du Service Geologiquevol 383 pp 51ndash150 1996

[99] J Zhang and D B Scott ldquoIntegrated stratigraphy and paleo-ceanography of theMessinian (latestMiocene) across theNorthAtlantic OceanrdquoMarine Micropaleontology vol 29 no 1 pp 1ndash36 1996

[100] C Morigi A Negri S Giunta et al ldquoIntegrated quantitativebiostratigraphy of the latest Tortonian-early Messinian Pissourisection (Cyprus) an evaluation of calcareous plankton bio-eventsrdquo Geobios vol 40 no 3 pp 267ndash279 2007

[101] D A Hodell R H Benson D V Kent A Boersma andK Rakic-El Bied ldquoMagnetostratigraphic biostratigraphic andstable isotope stratigraphy of an Upper Miocene drill core fromthe Sale Briqueterie (northwesternMorocco) a high-resolutionchronology for the Messinian stagerdquo Paleoceanography vol 9no 6 pp 835ndash855 1994

[102] W Krijgsman M M Blanc-Valleron R Flecker et al ldquoTheonset of the Messinian salinity crisis in the Eastern Mediter-ranean (Pissouri Basin Cyprus)rdquo Earth and Planetary ScienceLetters vol 194 no 3-4 pp 299ndash310 2002

[103] P W P Hooper and P P E Weaver ldquoPaleoceanographic signifi-cance of late Miocene to early Pliocene planktonic foraminifersat Deep Sea Drilling Project Site 609rdquo Initial Reports of the DeepSea Drilling Project vol 94 no 2 pp 925ndash934 1987

[104] J Laskar P Robutel F Joutel M Gastineau A C M Correiaand B Levrard ldquoA long-term numerical solution for theinsolation quantities of the Earthrdquo Astronomy and Astrophysicsvol 428 no 1 pp 261ndash285 2004


[105] F J Sierro ldquoThe replacement of the ldquoGloborotalia menardiirdquogroup by theGloborotaliamiotumida group an aid to recogniz-ing the Tortonian-Messinian boundary in the Mediterraneanand adjacent Atlanticrdquo Marine Micropaleontology vol 9 no 6pp 525ndash535 1985

[106] F J Sierro J A Flores J Civis and J A Gonzalez-DelgadoldquoNew criteria for the correlation of the Andalusian andMessinian stagesrdquoAnnales Instituti Geologici Publici Hungaricivol 70 pp 355ndash361 1987

[107] J A Flores and F J Sierro ldquoCalcareous nannoflora and plank-tonic foraminifera in the TortonianMessinian boundary inter-val of East Atlantic DSDP Sites and their relation to Spanish andMorroccan sectionsrdquo in Nannofossils and Their Applications SE van Heck and J Crux Eds British MicropaleontologicalSociety Series pp 249ndash266 1989

[108] R Z Poore ldquoTertiary Oligocene through Quaternary plank-tonic foraminiferal biostratigraphy of theNorth Atlantic DSDPLeg 49rdquo Initial Reports of the Deep Sea Drilling Project vol 49pp 447ndash518 1979

[109] M B Cita ldquoMediterranean evaporite paleontological argu-ments for a deep-basin desiccation modelrdquo inMessinian Eventsin the Mediterranean C W Drooger Ed pp 206ndash228 North-Holland Amsterdam The Netherland 1973

[110] M B Cita ldquoPlanktonic foraminiferal biozonation of theMediterranean Pliocene deep sea record A revision Studi sulPliocene e sugli strati di passaggio dal Miocene al PliocenerdquoRivista Italiana di Paleontologia vol 81 pp 527ndash544 1975

[111] M B Cita ldquoPlanktonic foraminiferal biostratigraphy of theMediterranean Neogenerdquo in Progress in MicropaleontologySpecial Pubblications Y Takayanagi and T Saito Eds pp 47ndash68 Micropaleontology Press 1976

[112] H M Bolli and J B Saunders ldquoOligocene to Holocene lowlatitude planktic foraminiferardquo in Plankton Stratigraphy H MBolli J B Saunders and K Perch-Nielsen Eds pp 283ndash314Cambridge University Press 1985

[113] C G Langereis and F J Hilgen ldquoThe Rossello composite aMediterranean and global reference section for the Early toearly Late Pliocenerdquo Earth and Planetary Science Letters vol104 no 2ndash4 pp 211ndash225 1991

[114] W A Berggren ldquoLate Neogene planktonic foraminiferal bios-tratigraphy of DSDP Site 357 (Rio Grande Rise)rdquo in InitialReports of the Deep Sea Drilling Project P R Supko K Perch-Nielsen R L Carlson et al Eds vol 12 pp 965ndash1001 1977

[115] W A Berggren D V Kent and J A van Couvering ldquoNeogenegeochronology and chronostratigraphyrdquo in The Chronology ofthe Geologic Record the Neogene Part 2 pp 211ndash259 BlackwellScience 1985

[116] M S Srinivasan and J P Kennett ldquoA review of Neogene plank-tonic foraminiferal biostratigraphy and evolution applicationsin the Equatorial and South Pacificrdquo Special Publications ofSEPM vol 32 pp 395ndash492 1981

[117] M S Srinivasan and J P Kennett ldquoNeogene planktonicforaminiferal biostratigraphy and evolution equatorial to sub-antarctic South Pacificrdquo Marine Micropaleontology vol 6 no5-6 pp 499ndash533 1981

[118] J P Kennett ldquoMiddle and Late Cenozoic planktonicforaminiferal biostratigraphy of the Southwest Pacific-DSDPLeg 21rdquo in Initial Reports of the Deep Sea Drilling Project EBurns J E Andrews and G J van der Lingen Eds vol 21 pp575ndash639 1973

[119] P P E Weaver and H Bergsten ldquoAssessing the accuracy offossil datum levels Globorotalia margaritae Foraminiferida a

Pliocene test caserdquo Journal of Micropalaeontology vol 9 no 2pp 225ndash231 1990

[120] T Saito L H Burckle and J D Hays ldquoLate Miocene to Pleis-tocene biostratigraphy of equatorial Pacific sedimentsrdquo in LateNeogene Epoch Boundaries pp 226ndash244 MicropaleontologyPress 1975

[121] I Raffi and J A Flores ldquoPleistocene through Miocene calcare-ous nannofossils from eastern equatorial Pacific Ocean (Leg138)rdquo in Proceedings of the Ocean Drilling Program ScienceResults vol 138 pp 233ndash286 1995

[122] I Raffi D Rio A DrsquoAtri E Fornaciari and S RocchettildquoQuantitative distribution patterns and biomagnetostratigra-phy of Middle and Late Miocene calcareous nannofossils fromequatorial Indian and Pacific Oceanrdquo in Proceedings of theOcean Drilling Program Science Results vol 138 pp 79ndash5021995

[123] J Backman and I Raffi ldquoCalibration of Miocene nannofossilevents to orbitally tuned cyclostratigraphies from Ceara RiserdquoProceedings of the Ocean Drilling Program Science Results vol154 pp 83ndash99 1997

[124] I Raffi J Backman E Fornaciari et al ldquoA review of calcareousnannofossil astrobiochronology encompassing the past 25 mil-lion yearsrdquo Quaternary Science Reviews vol 25 no 23-24 pp3113ndash3137 2006

[125] H Okada and D Bukry ldquoSupplementary modification andintroduction of code numbers to the low-latitude coccolithbiostratigraphic zonation (Bukry 1973 1975)rdquoMarine Micropa-leontology vol 5 pp 321ndash325 1980

[126] D Rio R Sprovieri and I Raffi ldquoCalcareous plankton bios-tratigraphy and biochronology of the Pliocene-Lower Pleis-tocene succession of the Capo Rossello area Sicilyrdquo MarineMicropaleontology vol 9 no 2 pp 135ndash180 1984

[127] R Thunell D Rio R Sprovieri and I Raffi ldquoLimestone-marlcouplets origin of the early Pliocene Trubi Marls in Calabriasouthern Italyrdquo Journal of Sedimentary Petrology vol 61 no 7pp 1109ndash1122 1991

[128] RThunell D Rio R Sprovieri and C Vergnaud-Grazzini ldquoAnoverview of the post-Messinian paleoenvironmental history ofthe western Mediterraneanrdquo Paleoceanography vol 6 no 1 pp143ndash163 1991

[129] A Di Stefano and G Sturiale ldquoRefinements of calcareousnannofossil biostratigraphy at the MiocenePliocene Boundaryin the Mediterranean regionrdquo Geobios vol 43 no 1 pp 5ndash202010

[130] J A Van Couvering D Castradori M B Cita F J Hilgen andD Rio ldquoThe base of the Zanclean Stage and of the Plioceneseriesrdquo Episodes vol 23 no 3 pp 179ndash187 2000

[131] A Caruso M Sprovieri A Bonanno and R Sprovieri ldquoAstro-nomical calibration of the SerravallianTortonian Case Pelacanisection (Sicily Italy)rdquo Rivista Italiana di Paleontologia e Strati-grafia vol 108 no 2 pp 297ndash306 2002

[132] M Sprovieri A Caruso L M Foresi et al ldquoAstronomicalcalibration of the upper Langhianlower Serravallian record ofRas il-Pellegrin section (Malta Island Central Mediterranean)rdquoRivista Italiana di Paleontologia e Stratigrafia vol 108 no 2 pp183ndash193 2002

[133] M Sprovieri A Bellanca A Neri et al ldquoAstronomical cal-ibration of late Miocene stratigraphic events and analysisof precessionally driven paleoceanographic changes in theMediterranean basinrdquoMemorie della Societa Geologica Italianavol 54 pp 7ndash24 1999


[134] A Bellanca A Caruso G Ferruzza et al ldquoTransition frommarine to hypersaline conditions in the Messinian TripoliFormation from themarginal areas of the central Sicilian BasinrdquoSedimentary Geology vol 140 no 1-2 pp 87ndash105 2001

[135] A Vazquez R Utrilla I Zamarreno et al ldquoPrecession-relatedsapropelites of the Messinian Sorbas Basin (South Spain)paleoenvironmental significancerdquo Palaeogeography Palaeocli-matology Palaeoecology vol 158 no 3-4 pp 353ndash370 2000

[136] A W H Be ldquoAn ecological zoogeographic and taxonomicreview of recent planktonic foraminifersrdquo in Oceanic Micropa-leontology A T S Ramsey Ed pp 1ndash101 Academic Press NewYork NY USA 1977

[137] B Luz and Z Reiss ldquoStable carbon isotopes in Quaternaryforaminifers from the Gulf of Aqaba (Etlat) Red Seardquo UtrechMicropaleontological Bulletins vol 30 pp 129ndash140 1983

[138] C Pujol and C V Grazzini ldquoDistribution patterns of liveplanktic foraminifers as related to regional hydrography andproductive systems of theMediterranean SeardquoMarineMicropa-leontology vol 25 no 2-3 pp 187ndash217 1995

[139] R G Fairbanks and P H Wiebe ldquoForaminifera and chloro-phyll maximum vertical distribution seasonal succession andpaleoceanographic significancerdquo Science vol 209 no 4464 pp1524ndash1526 1980

[140] R G Fairbanks M Sverdlove R Free P H Wiebe and A WH Be ldquoVertical distribution and isotopic fractionation of livingplanktonic foraminifera from the Panama Basinrdquo Nature vol298 no 5877 pp 841ndash844 1982

[141] E J Rohling andWW C Gieskes ldquoLate Quaternary changes inMediterranean intermediate water density and formation raterdquoPaleoceanography vol 4 no 5 pp 531ndash545 1989

[142] F J Sierro J A Flores I Zamarreno et al ldquoMessinianpre-evaporite sapropels and precession-induced oscillations inwestern Mediterranean climaterdquo Marine Geology vol 153 no1ndash4 pp 137ndash146 1999

[143] A W H Be and D S Tolderlund ldquoDistribution and ecology ofliving planktonic foraminifera in surface waters of the Atlanticand Indian Oceansrdquo in The Micropaleontology of Oceans BM Funnel and W R Riedel Eds pp 105ndash149 CambridgeUniversity Press London UK 1971

[144] C Hemleben M Spindler and O R Anderson ModernPlanktonic Foraminifera Springer New York NY USA 1989

[145] A W H Be G Vilks and I Lott ldquoWinter distribution ofplanktonic foraminifera between the Grand Banks and theCaribbeanrdquoMicropaleontology vol 17 pp 31ndash42 1971

[146] R J W Van Leeuwen ldquoSea-floor distribution and Late Quater-nary faunal patterns of planktonic and benthic foraminifers inthe Angola Basinrdquo Utrecht Micropaleontological Bulletins vol38 p 287 1989

[147] B Malmgren and J P Kennett ldquoBiometric analyses of phe-notypic variation Globigerina bulloides and Globigerina falco-nensis in the southern Indian Oceanrdquo Journal of ForaminiferalResearch vol 7 pp 130ndash148 1977

[148] W Krijgsman F J Hilgen A Negri J R Wijbrans andW J Zachariasse ldquoThe Monte del Casino section (NorthernApennines Italy) a potential TortonianMessinian boundarystratotyperdquo Palaeogeography Palaeoclimatology Palaeoecologyvol 133 no 1-2 pp 27ndash47 1997

[149] S J Schenau A Antonarakou F J Hilgen et al ldquoOrganic-richlayers in the Metochia section (Gavdos Greece) evidence for asingle mechanism of sapropel formation during the past 10MyrdquoMarine Geology vol 153 no 1ndash4 pp 117ndash135 1999

[150] G M Filippelli F J Sierro J A Flores et al ldquoA sediment-nutrient-oxygen feedback responsible for productivity vari-ations in Late Miocene sapropel sequences of the westernMediterraneanrdquo Palaeogeography Palaeoclimatology Palaeoe-cology vol 190 pp 335ndash348 2003

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Atmospheric SciencesInternational Journal of



considered one of the best tools to gain high-resolutionchronostratigraphy in different depositional environments(continental marginal marine and deep sea) The presenceof high-frequency cycles in deep-sea records and their tuningto the astronomical curve provide an accurate chronologyfor the stratigraphic events recognized through the studiedsedimentary successions Applications of cyclostratigraphyresulted in the construction of an accurate AstronomicalTuned Neogene Time Scale (ATNTS 2004) for the Qua-ternary Pliocene and late and middle Miocene [3 42ndash44 53ndash61] The classic high frequency cyclicity recognizedin most of the late Neogene Mediterranean sedimentaryrecord is manifested by the alternation of homogeneousmarl and sapropel (or sapropel equivalent) horizons pro-moted by astronomical forcing [3] In this paper since thesuccession investigated does not show rhythmic litholog-ical patterns the proposed cyclostratigraphic reconstruc-tion is mainly based on the quantitative distribution pat-terns of climate-sensitive planktonic foraminifera taxa (eg[62ndash66])

The aim of this paper is (i) to present an biostratigraphyfor the Messinian-early Zanclean of the Hole 953C basedon quantitative data of planktonic foraminifera (previousstudies by [67 68] are to be considered inadequate for thisresearch) (ii) to compare the bioevents recognized withthose occurring in other astronomically calibrated sections(iii) to recognize other cyclic patterns for using as furthercontrol of the obtained astronomical calibration

2 Material and Methods

21 Site Description During Ocean Drilling Program Leg157 four sites (Site 953 to 956 see [70]) were drilled in thevolcaniclastic apron of Gran Canaria in the Canary IslandArchipelago (North-Eastern Atlantic) (Figure 1) ODP Hole953C is situated at 28∘391015840012N 15∘081015840670W 68 kmnortheastof GranCanaria 90 kmwest of Fuerteventura and 98 km eastof Tenerife at water depth of 35778m It is the most distallylocated site on the flanks of Gran Canaria and thus seemsto have been spared some of the major slumped intervalsand unconformities present at Sites 954 955 and 956 Therecovered sedimentary succession spans the interval from themiddle Miocene to Holocene and the dominant nonvolcaniclithologies were divided into seven major units and threesubunits (see [69]) The present study focuses on a 5111mthick succession from the Unit III embracing cores 18R to13R from 34689 to 29578mbsf (Figure 1) and representingthe Messinian-early Zanclean time interval Core recoverywas generally over 50 and mainly consisting of gray tobrownish-gray clayey nannofossil ooze interbedded withminor graded nannofossil clay-silt foraminifer lithic silt andsands and foraminifer sands

22 Sample Preparation and Micropaleontological Analysis

221 Foraminifera Samples for foraminiferal analysis weredisaggregated in normal water and washed through a 63 120583msieve The residues were oven dried at 40∘C Qualitative

and quantitative planktonic foraminiferal analyses were per-formed using a stereoscopic microscope on 170 samples(average spacing 20 cm) The samples were divided with amicrosplitter to obtain unbiased aliquots with about 300planktonic foraminifera They were (1) picked (2) mountedonto faunal slides (3) determined at specific and supraspe-cific level and (4) counted (200ndash300 specimens) from thelarger than 125 120583m fraction of the washed residue to collectquantitative faunal data The assemblages are usually abun-dant and generally well preserved although at times they arepoor Very few samples show a very scarce faunal content

Raw data of microfossils were transformed into percent-ages over the total abundance and percentage abundancecurves were plotted Species with phylogenetic affinities andsimilar environmental significance were also grouped tobetter interpret distribution patterns

Furthermore a semiquantitative analysis from the largerthan 63 120583m fraction was carried out on all samples in orderto pinpoint the actual position of the bioevents

Benthic foraminifera were also counted to determineplanktonbenthos ratio which is expressed as P = 100 lowast[P(P + B)] (eg [71])

222 Calcareous Nannofossil Standard smear-slides wereprepared for the nannofossil analyses for the intervals encom-passing the principal bioevents (from core 17R Section 3 tocore 13R Section 5) Qualitative analyses on a total of 30samples have been performed byDr Baldassini N (SienaUni-versity) to determine additional biohorizons and bioevents toimprove the biostratigraphic resolution

3 Micropaleontological Data

Theanalysis of the planktonic foraminiferal fauna allowed theidentification of 45 taxa which sometimes were grouped intocategories on the basis of morphological phyletic or ecologi-cal affinities The categories are (Table 1) Dentoglobigerina gr(D altispira altispiraD altispira globosa)Globigerinita gr (Gglutinata G uvula) Globigerinoides obliquus gr (G bollii Gcf elongatus G emeisi G extremus G obliquus) Globigeri-noides quadrilobatus gr (G quadrilobatusG trilobusG sac-culifer)Globoturborotalita decoraperta gr (G cf apertura Gdecoraperta) Globorotalia menardii gr (G menardii G mul-ticamerata) Neogloboquadrina gr (N acostaensis N pachy-dermaN dutertrei humerosaN dutertrei blowi)Orbulina gr(O bilobataO suturalisO universa) and Sphaeroidinellopsisseminulina gr (S seminulina paenedehiscens S seminulinaseminulina) Most of the categories are self-explaining butthe labelling of some of them needs further explanation

Figure 2 shows the quantitative distribution of thosespecies (or categories) which generally display frequencieshigher than 15 The main components are Globoturboro-talita nepenthes and Neogloboquadrina gr which are contin-uously present throughout the investigated interval reachingmaxima frequencies of 90 and 80 respectively

Neogloboquadrina gr includes also small-sized speci-mens sometimes under poor preservation conditions thatwere difficult to distinguish Different coiling directions of


28∘N

29∘N

350

340

330

320

310

300

Dep

th (m

bsf)

Hole 953C

Cor

e

Reco

very

Uni

t

Lith

olog

y

13R

14R

15R

16R

17R

18R

III


2000

9553000

3000

956

2000

2000

1000

1000

Fu

953

954

GranCanaria

Tenerife

16∘W 15

∘W

16∘W 15

∘W

27∘N

28∘N

29∘N

27∘N


295

300

305

310

315

320

325

330

335

340

345

350

Dep

th (m

bsf)

1314

1518

1716

6CC

CC

CC

CC

CC

12345

1234

1234

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12

12

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6

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ODP Hole 953C

C3n2r

C3n3nC3n3r

C3n4n

C3An

C3r

LO

LROSD

100

50 200 00 20 0 5 0 10 150 0 2 20 0 30 0 020 040 090 060 0 5 060 3030 0 40 00

ldquoFOrdquo

Den

toglo

bige

rina

gr

G fa

lcone

nsis

Glob

iger

inita

gr

Gob

liquu

s gr

G q

uadr

iloba

tus g

r

G ju

anai

G m

mar

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ae

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G ci

baoe

nsis

G sc

itula

G m

enar

dii g

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G m

iotu

mid

a

G d

ecor

aper

ta gr

G n

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thes

N a

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ensis

N p

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derm

a

Orb

ulin

a gr

Spha

eroi

dine

llops

is s

gr

119875 ()















multicamerata






Orbulina bilobata
























4 Biostratigraphy


























Insolationminus +

War

mc

old

Neog

lobo

quad

rinid

s

Glob

igerin

oide

sSicily

Marl

Diatomite

Sapropel

Marl

Diatomite

Sapropel

Marl

MarlDiatomite

Sapropel

Gavdos















11solution)




800

494

504

514

524

534

544

554

564

574

584

594

604

614

624

634

644

654

664

674

684

694

704

714

0 007400 5200 40 1000295

300

305

310

315

320

325

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335

340

345

350

355

360

365

370

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6cc 12

cc

12

3cc

123

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123

12

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6

13

Dep

th (m

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Core

Secti

on

14

15

16

17

18cc

cc19

20

ODP Hole 953C

Polar

ity

Chro

n

C3r

C3An

C3Ar

C3n4n

C3n3r

C3n3n

C3n2r


4

14

59

101315

22

23

28

29

34

35

383940414243

(a)

(b)

(c)

(d)(e)

(f)

Ain el beidasection


A20

A21

A22

A23

A24

A25

A26

A27

B1

B2

B3

B4

B5

B6

B7

B8

B9

C3r




AEB32

AEB33AEB34AEB35

AEB37

AEB38

AEB36

AEB39

AEB40

AEB41

AEB42

AEB43

484 Ma


Louljasections

La04 11 solution

[68 65]









Figure 5





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology





28∘N

29∘N

350

340

330

320

310

300

Dep

th (m

bsf)

Hole 953C

Cor

e

Reco

very

Uni

t

Lith

olog

y

13R

14R

15R

16R

17R

18R

III


2000

9553000

3000

956

2000

2000

1000

1000

Fu

953

954

GranCanaria

Tenerife

16∘W 15

∘W

16∘W 15

∘W

27∘N

28∘N

29∘N

27∘N


295

300

305

310

315

320

325

330

335

340

345

350

Dep

th (m

bsf)

1314

1518

1716

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ODP Hole 953C

C3n2r

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C3n4n

C3An

C3r

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100

50 200 00 20 0 5 0 10 150 0 2 20 0 30 0 020 040 090 060 0 5 060 3030 0 40 00

ldquoFOrdquo

Den

toglo

bige

rina

gr

G fa

lcone

nsis

Glob

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inita

gr

Gob

liquu

s gr

G q

uadr

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tus g

r

G ju

anai

G m

mar

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G m

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G ci

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G sc

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G m

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G m

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mid

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G d

ecor

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ta gr

G n

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N a

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ensis

N p

achy

derm

a

Orb

ulin

a gr

Spha

eroi

dine

llops

is s

gr

119875 ()















multicamerata






Orbulina bilobata
























4 Biostratigraphy


























Insolationminus +

War

mc

old

Neog

lobo

quad

rinid

s

Glob

igerin

oide

sSicily

Marl

Diatomite

Sapropel

Marl

Diatomite

Sapropel

Marl

MarlDiatomite

Sapropel

Gavdos















11solution)




800

494

504

514

524

534

544

554

564

574

584

594

604

614

624

634

644

654

664

674

684

694

704

714

0 007400 5200 40 1000295

300

305

310

315

320

325

330

335

340

345

350

355

360

365

370

12345

6cc 12

cc

12

3cc

123

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123

12

12345

6

13

Dep

th (m

bsf)

Core

Secti

on

14

15

16

17

18cc

cc19

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ODP Hole 953C

Polar

ity

Chro

n

C3r

C3An

C3Ar

C3n4n

C3n3r

C3n3n

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4

14

59

101315

22

23

28

29

34

35

383940414243

(a)

(b)

(c)

(d)(e)

(f)

Ain el beidasection


A20

A21

A22

A23

A24

A25

A26

A27

B1

B2

B3

B4

B5

B6

B7

B8

B9

C3r




AEB32

AEB33AEB34AEB35

AEB37

AEB38

AEB36

AEB39

AEB40

AEB41

AEB42

AEB43

484 Ma


Louljasections

La04 11 solution

[68 65]









Figure 5





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology















multicamerata






Orbulina bilobata
























4 Biostratigraphy


























Insolationminus +

War

mc

old

Neog

lobo

quad

rinid

s

Glob

igerin

oide

sSicily

Marl

Diatomite

Sapropel

Marl

Diatomite

Sapropel

Marl

MarlDiatomite

Sapropel

Gavdos















11solution)




800

494

504

514

524

534

544

554

564

574

584

594

604

614

624

634

644

654

664

674

684

694

704

714

0 007400 5200 40 1000295

300

305

310

315

320

325

330

335

340

345

350

355

360

365

370

12345

6cc 12

cc

12

3cc

123

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12345

123

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12345

6

13

Dep

th (m

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Core

Secti

on

14

15

16

17

18cc

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ODP Hole 953C

Polar

ity

Chro

n

C3r

C3An

C3Ar

C3n4n

C3n3r

C3n3n

C3n2r


4

14

59

101315

22

23

28

29

34

35

383940414243

(a)

(b)

(c)

(d)(e)

(f)

Ain el beidasection


A20

A21

A22

A23

A24

A25

A26

A27

B1

B2

B3

B4

B5

B6

B7

B8

B9

C3r




AEB32

AEB33AEB34AEB35

AEB37

AEB38

AEB36

AEB39

AEB40

AEB41

AEB42

AEB43

484 Ma


Louljasections

La04 11 solution

[68 65]









Figure 5





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology









4 Biostratigraphy


























Insolationminus +

War

mc

old

Neog

lobo

quad

rinid

s

Glob

igerin

oide

sSicily

Marl

Diatomite

Sapropel

Marl

Diatomite

Sapropel

Marl

MarlDiatomite

Sapropel

Gavdos















11solution)




800

494

504

514

524

534

544

554

564

574

584

594

604

614

624

634

644

654

664

674

684

694

704

714

0 007400 5200 40 1000295

300

305

310

315

320

325

330

335

340

345

350

355

360

365

370

12345

6cc 12

cc

12

3cc

123

cc

12345

123

12

12345

6

13

Dep

th (m

bsf)

Core

Secti

on

14

15

16

17

18cc

cc19

20

ODP Hole 953C

Polar

ity

Chro

n

C3r

C3An

C3Ar

C3n4n

C3n3r

C3n3n

C3n2r


4

14

59

101315

22

23

28

29

34

35

383940414243

(a)

(b)

(c)

(d)(e)

(f)

Ain el beidasection


A20

A21

A22

A23

A24

A25

A26

A27

B1

B2

B3

B4

B5

B6

B7

B8

B9

C3r




AEB32

AEB33AEB34AEB35

AEB37

AEB38

AEB36

AEB39

AEB40

AEB41

AEB42

AEB43

484 Ma


Louljasections

La04 11 solution

[68 65]









Figure 5





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology




















Insolationminus +

War

mc

old

Neog

lobo

quad

rinid

s

Glob

igerin

oide

sSicily

Marl

Diatomite

Sapropel

Marl

Diatomite

Sapropel

Marl

MarlDiatomite

Sapropel

Gavdos















11solution)




800

494

504

514

524

534

544

554

564

574

584

594

604

614

624

634

644

654

664

674

684

694

704

714

0 007400 5200 40 1000295

300

305

310

315

320

325

330

335

340

345

350

355

360

365

370

12345

6cc 12

cc

12

3cc

123

cc

12345

123

12

12345

6

13

Dep

th (m

bsf)

Core

Secti

on

14

15

16

17

18cc

cc19

20

ODP Hole 953C

Polar

ity

Chro

n

C3r

C3An

C3Ar

C3n4n

C3n3r

C3n3n

C3n2r


4

14

59

101315

22

23

28

29

34

35

383940414243

(a)

(b)

(c)

(d)(e)

(f)

Ain el beidasection


A20

A21

A22

A23

A24

A25

A26

A27

B1

B2

B3

B4

B5

B6

B7

B8

B9

C3r




AEB32

AEB33AEB34AEB35

AEB37

AEB38

AEB36

AEB39

AEB40

AEB41

AEB42

AEB43

484 Ma


Louljasections

La04 11 solution

[68 65]









Figure 5





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology





800

494

504

514

524

534

544

554

564

574

584

594

604

614

624

634

644

654

664

674

684

694

704

714

0 007400 5200 40 1000295

300

305

310

315

320

325

330

335

340

345

350

355

360

365

370

12345

6cc 12

cc

12

3cc

123

cc

12345

123

12

12345

6

13

Dep

th (m

bsf)

Core

Secti

on

14

15

16

17

18cc

cc19

20

ODP Hole 953C

Polar

ity

Chro

n

C3r

C3An

C3Ar

C3n4n

C3n3r

C3n3n

C3n2r


4

14

59

101315

22

23

28

29

34

35

383940414243

(a)

(b)

(c)

(d)(e)

(f)

Ain el beidasection


A20

A21

A22

A23

A24

A25

A26

A27

B1

B2

B3

B4

B5

B6

B7

B8

B9

C3r




AEB32

AEB33AEB34AEB35

AEB37

AEB38

AEB36

AEB39

AEB40

AEB41

AEB42

AEB43

484 Ma


Louljasections

La04 11 solution

[68 65]









Figure 5





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology





Figure 5





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology





Figure 6








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology








6 Conclusion

































Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology














Acknowledgments


References


































































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology

















































































































































Volume 2013


Volume 2013

ISRN Paleontology


Geochemistry


Journal of

ISRN Geophysics







ISRN Oceanography






Geophysics





ISRN Meteorology


Meteorology


Advances in



Mining


Journal of


ISRN Geology




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