Palaeoenvironments and Quaternary foraminifera in the Elx coastal lagoon (Alicante, Spain)

Abstract

During the Quaternary, different palaeoenvironments characterised the Elx coastal lagoon (‘Albufera d'Elx’) located in the easternmost sector of the Betic Ranges (SE Spain). Micropalaeontological and sedimentological analysis of three drilled cores allowed characterization of different sedimentary environments, including alluvial, restricted lagoon, lagoon with marine connection, shoreface, foreshore, backshore, swamp, washover fan, and back-barrier flat. A model of the evolution of this region during Marine Isotope Stage (MIS) 7 is proposed, based on chronostratigraphic correlation between the cores. Up to six transgressive episodes can be recognised, mostly represented by calcareous sandstones deposited in different sub-environments of the littoral zone. Holocene shoreface beds comprise unconsolidated sands. The occurrence of planktonic foraminifera at depths than 18 m indicates the existence of Pliocene marine beds beneath the Quaternary deposits. The data demonstrate that coastal lagoon systems have existed in this area of SE Spain since to at least the Middle Pleistocene.

Full text

Palaeoenvironments and Quaternary foraminifera in the Elx coastal lagoon
(Alicante, Spain)
Ana M
a
Bla
´zquez
a
,
*
, Juan Usera
b
a
Environmental and Marine Sciences Research Institute, Catholic University of Valencia, C/ Guillem de Castro 94, Valencia 46003, Spain
b
Departamento de Geologı
´a, Universitat de Vale
`ncia, Dr. Moliner 50, 46100 Burjassot, Valencia, Spain
article info
Article history:
Available online 24 July 2009
abstract
During the Quaternary, different palaeoenvironments characterised the Elx coastal lagoon (‘Albufera
d’Elx’) located in the easternmost sector of the Betic Ranges (SE Spain). Micropalaeontological and
sedimentological analysis of three drilled cores allowed characterization of different sedimentary envi-
ronments, including alluvial, restricted lagoon, lagoon with marine connection, shoreface, foreshore,
backshore, swamp, washover fan, and back-barrier flat. A model of the evolution of this region during
Marine Isotope Stage (MIS) 7 is proposed, based on chronostratigraphic correlation between the cores.
Up to six transgressive episodes can be recognised, mostly represented by calcareous sandstones
deposited in different sub-environments of the littoral zone. Holocene shoreface beds comprise
unconsolidated sands. The occurrence of planktonic foraminifera at depths than 18 m indicates the
existence of Pliocene marine beds beneath the Quaternary deposits. The data demonstrate that coastal
lagoon systems have existed in this area of SE Spain since to at least the Middle Pleistocene.
Ó2009 Elsevier Ltd and INQUA. All rights reserved.
1. Introduction
The Elx Depression is located in the easternmost sector of the
Betic Ranges in the southern part of the Alicante province (Spain).
The Elx coastal lagoon (l’Albufera d’Elx) is located within this
tectonic basin and currently includes the lagoons of ‘El Fondo
´d’Elx’
and ‘Salinas de Santa Pola’ (Fig. 1)(Mateu and Cuerda, 1978). Recent
work indicates the existence of a large lagoon during the late
Holocene after the Holocene sea level maximum (6000–6500 BP,
Fleming et al., 1998; Dabrio et al., 2000; Shennan, 2007), at which
time marine conditions would have extended 19 km inland from
the present coast (Bla
´zquez, 2005) and persisted until at least the
Bronze Age (second millennium B.C.). This area has been artificially
drained since the eighteenth century.
Geologically, the Elx Depression is located in the northernmost
part of the sinistral fault system defined by Montenat (1977).It
includes a subsiding syncline containing lacustrine areas between
the Santa Pola and el Molar ranges, whose axes converge pericli-
nally towards the depression. A marine Mio-Pliocene substrate
consists of sandstones, calcareous sandstones, marls, silts and clays
which outcrop in the neighbouring ranges (Caracuel et al., 2004;
Soria et al., 2005). Over these materials, alluvial fan systems were
deposited during the Pleistocene and Holocene. These extend from
the Crevillent Range towards the SE and infill the subsiding zones.
The proximal and distal parts of these systems are disconnected as
a consequence of the generalised sinking of the sector during the
Early/Middle Pleistocene (Goy et al., 1990).
The study area has subsided during the Quaternary period. The
maximum subsidence in the littoral zone is located in the ‘Salinas
de Santa Pola’, and follows an E–W direction. Landwards of this
area, maximal sinking also characterises the Vinalopo
´alluvial fan
and the ‘Fondo
´d’Elx-Crevillent’.
The main goal of this study is to reconstruct the palae-
oenvironmental conditions that occurred during the Quaternary in
the Elx lagoon (‘l’Albufera d’Elx’). Results of sedimentological and
micropalaeontological (mainly foraminiferal) investigations
completed on three drill cores (Salinas, Pinet and Mo
´rtoles, Fig. 1)
are presented. Microfossil analyses determined euryhaline species
assemblages that characterise brackish environments, and steno-
haline species assemblages that correspond to environments with
normal marine salinities. Analyses were also conducted on the
Pliocene sediments and Quaternary beaches that are exposed at the
present-day surface.
2. Previous research
There have been numerous studies in Eastern Spain involving
paleoenvironmental reconstruction of Quaternary-restricted areas
*Corresponding author.
E-mail addresses: ana.blazquez@ucv.es (A.M
a
Bla
´zquez), usera@uv.es (J. Usera).
Contents lists available at ScienceDirect
Quaternary International
journal homepage: www.elsevier.com/locate/quaint
1040-6182/$ – see front matter Ó2009 Elsevier Ltd and INQUA. All rights reserved.
doi:10.1016/j.quaint.2009.06.033
Quaternary International 221 (2010) 68–90

based on fossil foraminifera. Examples include the littoral peat bog
of Vilanova i La Geltru
´in Catalonia (Calzada, 1970), the ‘‘Mar
Menor’’ near Murcia (Mateu, 1981), and S’Albufera d’Alcu
´dia in the
Balearic Islands (Colom, 1979; Vin
˜als and Mateu, 1999). In Valencia,
papers concerning fossil foraminifera from the following areas
include: the Pen
˜ı
´scola marsh (Usera et al., 2006), the Torreblanca
marsh (Colom, 1959; Collado and Robles, 1983), the ‘‘Albufera’’ of
Valencia (Robles et al., 1985; Usera et al., 1990), the Oliva-Pego
marsh (Dupre
´et al., 1988; Mateu, 1989; Vin
˜als et al., 1989; Garcı
´a
Forner, 1997), the Xa
`bia marsh (Fumanal et al., 1993; Vin
˜als et al.,
1993; Garcı
´a Forner, 1997), and the ‘‘Albufereta d’Alacant’’ (Bla
´z-
quez and Ferrer, 2003; Ferrer et al., 2005). The ‘‘Albufera d’Elx’’ has
been studied in different works (Colom, 1959; Bla
´zquez et al., 1999;
Bla
´zquez and Usera, 2000, 2004, 2005; Bla
´zquez, 2005). The main
results have been gathered in several reviews (Usera et al., 2002;
Usera, 2003).
Previous analysis of the Quaternary succession sampled in
coastal cores indicates that the dominant foraminifera assemblage
consists of the following species: Ammonia beccarii tepida (Cush-
man), Haynesina germanica (Ehrenberg), Elphidium excavatum
(Terquem), Miliolinella eburnea (D’Orbigny), Aubignyna perlucida
(Heron-Allen and Earland) and Trichohyalus aguayoi (Bermu
´dez). In
low-salinity brackish conditions, agglutinated species such as Tro-
chammina inflata (Montagu) and Jadammina macrescens (Brady)
have been recorded. All of the species are benthic and are common
in restricted contemporary environments such as estuaries,
marshes and littoral lagoons (Murray, 1991, 2004). Connections
with the sea are inferred from the occurrence of typical marine
species, including Ammonia beccarii beccarii (Linne
´), Elphidium
crispum (Linne
´), Lobatula lobatula (Walker and Jacob), Rosalina
globularis D’Orbigny, Elphidium complanatum (D’Orbigny), Amphi-
sorus hemprichi (Ehrenberg), Asterigerinata mamilla (Williamson),
Buccella granulata (Di Napoli), Elphidium advenum (Linne
´), Elphi-
dium macellum (Fichter and Moll), Planorbulina mediterranensis
(D’Orbigny), Planorbulina variabilis (D’Orbigny), Nonion commune
(D’Orbigny), and Quinqueloculina vulgaris (D’Orbigny). These and
other species are currently dominant in the Western Mediterra-
nean infralittoral area and continental shelf (Mateu, 1970, 1974;
Colom, 1974; Bla
´zquez, 1996; Bla
´zquez et al., 1996; Usera and
Bla
´zquez, 1997). A. beccarii beccarii (Linne
´) and E. crispum (Linne
´)
are ubiquitous species.
Studies of recent tidally restricted environments are rare. One of
the lagoons studied in eastern Spain is the Torreblanca marsh,
where the following foraminifera species have been found:T. inflata
(Montagu), J. macrescens (Brady), Miliammina fusca (Brady),
T. aguayoi (Bermu
´dez), A. beccarii tepida (Cushman), Disconorbis
bulbosus (Parker), Rubratella intermedia Grell, Laminononion tumi-
dum (Cushman and Edwards), Spirillina vivipara Ehrenberg, Tur-
rispirillina sp., and aff. Physalidia sp. (Guillem, 2008). In addition,
Zaninetti (1984) analysed the foraminifera from the hyper saline
waters in the preparation salt pools in the Bras del Port salinas
(Santa Pola) and found an assemblage dominated by the species
A. beccarii tepida (Cushman), T. inflata (Montagu), J. macrescens
(Brady), Haynesina depressula (Walker and Jacob), H. germanica
(Ehrenberg), Discorbis sp. and different Miliolidae, including Mil-
iolinella? sp.
3. Material and methods
The locations of the studied cores are shown in Table 1. Cores
were sampled every 10 cm. Samples were dried and sub-samples of
100 g were treated with sodium hydroxide and hydrogen peroxide
to disaggregate them. The sediment was washed through sieves of
>0.4 mm, >0.125 mm and >0.063 mm mesh, thus yielding three
size fractions for each sample. The aim of this procedure was to
facilitate the process of picking the foraminifera shells from the
obtained residue, since the use of dense liquids (carbon tetrachlo-
ride) was successful only in very sandy carbonate-free samples,
Fig. 1. Location of the study area, geomorphological scheme and situation of the mechanical cores.
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–90 69

such as those from units IV and VIII from the Salinas core. However,
all samples were treated with the same methodology.
Most samples were split to obtain the minimum representative
individual number of foraminifera, which depends in each case on
the sample environment. In order to know the number of indi-
viduals that are necessary to have an appropriate estimation of the
species number in each environment, rarefaction plots were
developed for each sample. The rarefaction curves were obtained
from the Hurlbert (1971) equation, which has been discussed by
Raup and Stanley (1978), and Hayek and Buzas (1997). The result of
this equation is an estimate of species number in relation to the
number of individuals, and these estimates are the basic parame-
ters used to calculate the rarefaction curve. An asymptotic
morphology indicates that even if more individuals are picked, the
number of species will remain constant. In some samples, shells
were concentrated in one of the size fractions, and thus, all of the
size fractions were not split equally. In these cases, the size fractions
were standardised as follows: if one size fraction had been split less
times than another from the same sample, the obtained number of
individuals in the former was divided as many times as necessary to
correspond to the splitting of the latter. Unlike procedures based on
counting a fixed number of individuals in each sample, this method
allows a more reliable determination of the number of foraminifera
shells per gram, which is very useful in paleoenvironmental
interpretations.
The determination of the foraminifera assemblage was based on
the relative abundance of the dominant species. Using the fora-
minifera content, the diversity (Shannon and Wiener, 1949),
evenness (Buzas and Gibson, 1969), Fisher alpha (Fisher et al., 1943)
and Margalef richness (Magurran, 2001) were calculated.
HðSÞ¼
P
S
i¼1
P
i
log
2
P
i
E¼HðSÞ=log
2
S
a
¼N
i
=X
R¼S1=LnðnÞ
H(S): Shannon diversity index; S: number of species in each
sample; P
i
: frequency of each species; E: evenness index;
a
: Fisher
alpha index; N
i
: assemblage size; X: constant with values <1; R:
Margalef Richness and n: number of individuals.
All of these indexes are complementary. Both Margalef richness
and Fisher’s alpha values relate the number of individuals and the
number of species in each sample. Fisher’s alpha values are not
reliable in samples with less than 100 individuals. When
a
>5
the value indicates an open sea environment (Murray, 1991). The
Shannon index takes into account both the number and the
proportional abundance of species whereas the evenness index
indicates the degree of dominance of some of the species in each
sample (range: 0–1). Many authors utilise only one index (Fisher’s
alpha index is commonly employed), or they simply indicate the
number of species as a diversity measure (Garcı
´a Forner et al., 1993;
Garcı
´a Forner,1997; Usera et al., 2006). The use of several diversity
measures for this study is beneficial because different characteristics
allow for the comparison of these results with those obtained in
a wide range of other studies.
Material that could not be disaggregated was studied in thin
sections. In this case, foraminifera could be classified only at
a generic level.
Radiochronological analyses (
14
C) were carried out in Beta
Analytic (Florida), and calendar corrections were calculated. The
older samples were dated using Th/U in the ‘‘Centre d’E
´tudes et de
Recherches Aplique
´es au Karst’’ (Polytechnic Faculty of Mons,
Belgium).
4. Results and discussion
The main sedimentological and micropalaeontological results
are indicated for each core as follows.
4.1. Sedimentary units and palaeoenvironmental interpretation
4.1.1. Salinas core
A total of 101 samples were collected from the entire core, of
which 55 samples covering the Quaternary section were subjected
to micropalaeontological and sedimentological analysis (Fig. 2). On
the basis of the sedimentologic results in particular, a stratigraphic
sequence comprising nine depositional units can be established
(Fig. 3). The suborder Rotaliina dominates the core (80.35% of the
specimens picked), although the suborder Miliolina is present in
the highest proportion among all the studied cores (19.4%). Tex-
tulariina, Lagenina and Spirillinina are present as well and
respectively represent 0.05%, 0.18% and 0.02% of the total.
Three radiometric dates provide a partial chronology for the
upper part of the sequence (Table 2). The micropalaeontological
and sedimentological results of the sedimentary units are shown in
Tables 3 and 4. The palaeoenvironmental interpretation of the
analysed units in the Salinas core is shown in Fig. 2. Values of the
different diversity, abundance, evenness and richness indexes
based on the fossil foraminifer content are included.
The base of the Salinas core (Unit I, Fig. 2) was deposited in
a shelf environment, as can be deduced from the abundance of
planktonic foraminifera and the occurrence of neritic benthic
species such as Pullenia bulloides (D’Orbigny), Cassidulina laevigata
D’Orbigny and Cibicides subhaidingeri Parr (Table 3). The decrease of
the planktonic/benthonic ratio, the increase of the sand content
and the appearance of littoral species such as A. beccarii beccarii
(Linne
´)(Fig. 4), N. commune (D’Orbigny) (Fig. 4), Neoconorbina
terquemi (Rzehak) and Elphidium spp. (Table 3) indicate that the
environment becomes shallower towards the top of the unit
(Murray, 1991). The stratigraphic, sedimentologic and micro-
palaeontology characteristics correlate this unit with theMargas de
Hurchillo Formation defined by Montenat et al. (1990) and attrib-
uted by these authors to the Lower Pliocene. Bardajı
´et al. (1995)
and Soria et al. (1996) also ascribe this formation to the base of the
Pliocene, although Bardajı
´et al. (1995) placed its top at the Plio-
cene–Quaternary boundary and Soria et al. (1996) at the base of the
Lower Pliocene.
After a long erosional period, the first Quaternary sediments
were deposited (Unit II). The sequence records a decrease in the
energy levels, from a highly energetic basal episode, followed by
stream deposits as denoted by an increase in sand content (Fig. 3),
to hydromorphic soils at the top with abundant rhizotubules. The
foraminifera shells are altered by diagenesis (moulds are abundant)
and belong both to planktonic and benthic species. The absence of
autochthonous ostracods at the top of Unit II might indicate the
poor stability of the water masses. Unit III comprises a swamp
deposit, as indicated by the site’s colonisation by freshwater /
slightly brackish ostracod species (Ilyocypris gibba (Ramdohr) and
Cyprideis torosa (Jones)). Because of their good preservation, these
fossils are considered to be autochthonous.
Table 1
Location of the cores.
Core data Mo
´rtoles Pinet Salinas
UTM coordinates 30SYH089 311 30SYH079 269 30SYH086 270
Distance to the
present coastline (m)
2500 750 20
Height (m) 2 1 1
Depth (m) 31 36 30
Geomorphological
situation
Distal facies alluvial
fan Vinalopo
´)
Ancient bar Present bar
A.M
a
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´zquez, J. Usera / Quaternary International 221 (2010) 68–9070

Unit IV shows marine invasion of the previous freshwater and
terrestrial deposits. After an erosive period, grey sands with marine
fauna (Table 3) and an abundant assemblage of stenohaline fora-
minifers. This assemblage has high values for the diversity, even-
ness and richness indices (Table 4). Diversity and richness decrease
towards the top, possibly due to shallower conditions and/or to
partial sediment consolidation. Together with the micro-
palaeontological characteristics, the sedimentary and stratigraphic
data indicate that the sediments were deposited in a shoreface
environment. The conformity with the above-lying unit
Fig. 2. Stratigraphic column of the Salinas core. Palaeoenvironmental interpretation and diversity, abundance and evenness of the foraminiferal assemblages.
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–90 71

Fig. 3. Textural distribution (%) (A), % organic matter (B), % CO
3
Ca in the Salinas core. Roman numbers indicate the different sedimentary units.
Table 2
Numerical dating of the Salinas core.
*
Centre d’E
´tudes et de Recherches Aplique
´es au Karst’ at the ‘Faculte
´Polytechnique de Mons’ (Belgium).
Core Sample Depth (m) Laboratory Age Method Material dated Calibration 2 Sigma range
Salinas 4d 3 BETA-140894 671040 BP
14
C (AMS) Organic sediment 7580 BP 7620–7550 BP
Salinas 8a 7 BETA-140895 18 470 50 BP
14
C (AMS) Organic sediment 22 395–21 490 BP
Salinas 8a 7 6445
*
>400 000 BP Th/U Calcareous sandstone
A.M
a
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´zquez, J. Usera / Quaternary International 221 (2010) 68–9072

Table 3
Main sedimentological and micropalaeontological results of the Salinas core. Reworked: derived from older strata. Resedimented: derived from contemporary environments. Both groups indicate allochthonous foraminifera.
Autochthonous: in situ assemblages.
Sedimentary units Sediment Dominant foraminiferal assemblage Taphonomy (Foram.) Other organisms CO
3
Ca
(Average %)
Organ. mat.
(Average %)
Unit IX Sand with an
interbedded layer
of grey clay
Haynesina germanica (Ehrenberg), Ammonia
beccarii tepida(Cushman)
Autochthonous. Only in the clay Continental gastropods (Helix) and
abraded marine gastropods and
bivalves
74 1
Ammonia beccarii beccarii (Linne
´), Elphidium
crispum (Linne
´), Lobatula lobatula (Walker and
Jacob), Quinqueloculina vulgaris,Buccella
granulata (Di Napoli), Quinqueloculina bicornis
(Walker and Jacob), Asterigerinata mamilla
(Williamson), Miliolinella circularis
(Bornemann) and Elphidium macellum (Fichtel
and Moll)
Allochthonous. Resedimented
Unit VIII Medium sand Ammonia beccarii tepida (Cushman), Miliolinella
eburnea (D’Orbigny), Elphidium excavatum
(Terquem) and Haynesina germanica
(Ehrenberg)
Authocthonous/Allochthonous
(Resedimented)
Plates and spines of echinoderms,
polychaetes, bryozoans, gastropods
(Hydrobia sp.) and bivalves
(Cerastoderma glaucum (Poiret)),
sponge spicules, ostracods (Cyprideis
torosa (Jones)), charophytes
(Lamprothamnium papulosum (Wallr.))
70 0.4
Ammonia beccarii beccarii (Linne
´), Lobatula
lobatula (Walker and Jacob), Elphidium
macellum (Fichtel and Moll), Quinqueloculina
bicornis (Walker and Jacob), Elphidium advenum
(Cushman), Miliolinella circularis (Bornemann),
Rosalina globularis D’Orbigny, Asterigerinata
mamilla (Williamson), Elphidium crispum
(Linne
´), Buccella granulata (Di Napoli) and
Nonion commune (D’Orbigny)
Authocthonous/Allochthonous
(Resedimented)
Unit VII Alternating silt and sand Ammonia beccarii tepida (Cushman), Haynesina
germanica (Ehrenberg), Miliolinella eburnea
(D’Orbigny) and Trichoyalus aguayoi
(Bermudez)
Autochthonous Molluscs: Cerastoderma glaucum
(Poiret), Hydrobia sp., ostracods:
Cyprideis torosa (Jones), Charophytes:
Lamprothamnium papulosum (Wallr.)
66 0.89
Ammonia beccarii beccarii (Linne
´), Lobatula
lobatula (Walker and Jacob), Elphidium advenum
(Cushman), Elphidium macellum (Fichtel and
Moll), Rosalina globularis D’Orbigny
Allochthonous. Resedimented
Unit VI Clay and silt Ammonia beccarii tepida (Cushman), Haynesina
germanica (Ehrenberg) and Miliolinella eburnea
(D’Orbigny)
Autochthonous Charophytes (Lamprothamnium
papulosum (Wallr.), gastropods
(monospecific assemblage of Hydrobia
sp.), pulmonate gastropods (Hellicella cf.
madritensis and Granopupa granum)
bivalves (Cerastoderma glaucum
(Poiret)), ostracods (Cyprideis torosa
(Jones))
42 1.3
Unit V Calcareous sand grey. Quartz,
calcite and bioclastic with
calcareous cement.
Genus Ammonia Gastropods, bivalves, bryozoans,
ostracods, spines of echinoderms.
Towards the top: increase of bioclastics.
80 0.24
Unit IV Sand. At the top: partial
consolidation
Ammonia beccarii beccarii (Linne
´), Lobatula
lobatula (Walker and Jacob), Elphidium advenum
(Cushman), Asterigerinata mamilla
(Williamson), Rosalina globularis D’Orbigny,
Elphidium macellum (Fichtel and Moll),
Elphidium excavatum (Terquem), Elphidium
crispum (Linne
´)
Autochthonous Spines and plates of echinoderms,
internal moulds of gastropods,
abundant bryozoans, marine ostracods,
fragments of abraded bivalves
84 0.3
(continued on next page)
A.M
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(V, calcareous sandstone) and the organic matter content are
suggestive of deposition as a submerged bar. The site then was
exposed as a littoral bar (Unit V), where the presence of ripple
structures indicates shallow water and the proximity of the coast-
line, probably in proximal shoreface facies. This bar probably iso-
lated the lagoonal sediments from the open sea as recorded in the
following unit (Unit VI). The establishment of coastal lagoon sedi-
ments colonised by brackish water fauna and charophytes mark
a seaward movement of the coastline. Both an organic matter
increase and a decrease in carbonate content are recorded in this
unit. The foraminifera assemblage indicates a brackish water
restricted environment (A. beccarii tepida (Cushman) (Fig. 4), H.
germanica (Ehrenberg) (Fig. 4) and M. eburnea (D’Orbigny) (Fig. 4)),
with a clear decrease of the richness and diversity indexes,
particularly towards the top (Table 4). Other organisms indicate
restricted environment as well (Table 3). The gastropod Hydrobia
tolerates a wide salinity range and the occurrence of a monospecific
Hydrobia sp. assemblage together with the foraminifera species
recorded suggests a brackish highly stressful environment. Shallow
near-shore facies are indicated in the vicinity by environment
(shore facies) the occurrence of pulmonate gastropods Hellicella cf.
madritensis and Granopupa granum (Draparnaud).
This lagoonal environment was invaded by the sea (Unit VII), as
indicated by the presence of a washover fan with alternating silts
and sands. Compared with the previous unit, the organic matter
decreased and the carbonate content increased. The foraminifera
assemblage is mixed and includes components from both the
marine and restricted environments. The specimens from the
restricted assemblage are well preserved. The theoretical number
of individuals in 50 g shows a sudden and remarkable increase,
which is characteristic of this kind of environment. Other organ-
isms that occur are typical of restricted brackish water environ-
ments (Table 3). The marine influence increases towards the top of
Unit VIII in a deposit that is characterised by medium-sized sands
(average: >93%), an increase in the carbonate fraction and
a decrease in organic matter content. It includes fossils of both
marine (echinoderm plates and spines, polychaetes, bryozoans,
sponge spicules) and brackish water organisms, including bivalves
(Cerastoderma glaucum (Poiret)), ostracods (C. torosa (Jones)),
charophytes (Lamprothamnium papulosum (Wallr.)) and gastropods
(an abundant monospecific assemblage of Hydrobia sp.). Euryhaline
foraminifera species are also present. Their tests are well preserved
and their relative abundances increase towards the top (from 15%
to 63%). Other tests are badly preserved, corresponding to the
marine species. Most of these shells are broken and larger than
0.125 mm. Towards the top of this unit, a higher proportion of
broken specimens and a smaller percentage of biogenic tests were
observed. This sediment contained the highest proportion of shells
from the suborder Miliolina. The sedimentologic, stratigraphic and
micropalaeontological data suggest a shoreface or a foreshore facies
that existed a short distance away from a restricted environment
that was the source of the euryhaline fossils. The deposit could
represent a submerged bar that was gradually closing a restricted
area.
The unconsolidated sediments in Unit IX have abundant
yellowish brown sands (average: over 94%) and include a 30-cm
bed of silts and grey clays with a remarkable increase in organic
matter. Biogenic elements are rare. The sands include tests that are
broken, show diagenesis (many internal moulds), and contain
polished and pitted surfaces. Both H. germanica (Ehrenberg) (rep-
resenting 36% of individuals) and A. beccarii tepida (Cushman) (32%
of shells) occur in the embedded silt and clay sediment. In general,
a decrease in species richness and diversity is observed. This unit is
interpreted as a backshore deposit, with the embedded clayey
sediment accumulated in its swale.
Table 3 (continued )
Sedimentary units Sediment Dominant foraminiferal assemblage Taphonomy (Foram.) Other organisms CO
3
Ca
(Average %)
Organ. mat.
(Average %)
Unit III Clay, silt and sand Lobatula lobatula (Walker and Jacob), Ammonia
beccarii beccarii (Linne
´), Nonion commune
(D’Orbigny), Neoconorbina terquemi (Rzehak)
Allochthonous. Reworked Autochthonous freshwater ostracods:
Ilyocypris gibba (Ramdohr) and
Cyprideis torosa (Jones)
62 0.44
Unit II Bottom: sand with pebbles and
gravels
Lobatula lobatula (Walker and Jacob), Ammonia
beccarii beccarii (Linne
´), Elphidium advenum
(Cushman), Elphidium macellum (Fichtel and
Moll), Neoconorbina terquemi (Rzehak), Nonion
commune (D’Orbigny)
Allochthonous. Reworked Fragments of echinoderm spines, tests
of marine ostracods
54 0.23
Towards the top: increase of the
clay fraction and carbonate
precipitation.
Unit I Silty clay. Ferruginous
concretions
Pullenia bulloides (D’Orbigny), Cassidulina
laevigata D’Orbigny, Cibicides subhaidingeri Parr,
Lenticulina sp., Bolivina punctata D’Orbigny,
Bolivina pseudoplicata (Heron-Allen)
Autochthonous Planktonic Foraminifers:
Globigerinoides ruber (D’Orbigny),
Globigerina bulloides (D’Orbigny),
Globigerinoides sacculifer (Brady),
Globigerinella siphonifera (D’Orbigny),
Globigerina apertura Cushman,
Globigerina falconensis Blow,
Turborotalia quinqueloba (Natland),
Globigerinoides conglobatus (Brady),
Globigerinoides obliquus Bolli
64 0.35
Towards the top, in addition, littoral species:
Ammonia beccarii beccarii (Linne
´), Nonion
commune (D’Orbigny), Elphidium advenum
(Cushman), Elphidium macellum (Fichtel and
Moll), Neoconorbina terquemi (Rzehak)
Towards the top: frequently broken
tests
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In summary, the Salinas core records evidence for three land-
ward movements of the coastline during the Quaternary period,
which are indicated by three kinds of environments: a) the
submerged bar of Unit IV, which outcrops from a calcareous
sandstone in Unit V; b) the shoreface or foreshore deposit of Unit
VIII; and c) the aeolian facies of Unit IX. These were separated either
by alluvial deposits with different energy levels, by swamp and
lagoonal deposits or, in the case of the materials of the top of Unit
VIII, by facies more restricted than in underlying samples.
Unit V was dated using
14
C and Th/U. The results of both
radiometric dating techniques are questionable, particularly
because of the disparity of results within a single sample.
Radiocarbon dating yielded an age of 22 395 to 21490 cal. BP, which
is clearly erroneous since at this time sea level was approximately
110 to 120 m lower than the present level (Herna
´ndez Molina et al.,
1994). Nor can the >400 000 BP age yielded by the Th/U method be
accepted, because the position of the core suggests an age younger
than MIS 5e according to previous studies (Goza
´lvez and Rossello
´,
1978; Mateu and Cuerda, 1978; Goy et al., 1993) that analysed
comparable palaeontological, geomorphological and sedimento-
logical data. This beach stratum may therefore be linked to MIS 5c,
5a or even MIS 1. This last possibility is unlikely, as the few littoral
consolidated deposits related to the Holocene rise in sea level found
in neighbouring areas, such as the Carabassı
´bed (Goy et al., 1993),
Table 4
Foraminiferal indexes corresponding to the Salinas core. Their graphical representation is shown in Fig. 2.
Sample Unit Fisher alpha Shannon–Wiener Evenness Margalef Richness N

Species N

Indiv. N

Indiv./50 g
1a IX 3.28 2.03 0.57 2.28 12 332 580
1b 2.78 1.53 0.46 1.96 10 280 533
2 1.95 1.08 0.38 1.42 7 168 279
3a 0.91 0.60 0.26 0.74 5 252 861
3b 3.99 2.11 0.47 3.05 22 1019 4010
3c 3.26 0.97 0.25 2.29 14 336 960
3d 6.24 3.22 0.72 3.94 22 337 1267
4a VIII 3.93 2.52 0.63 2.77 16 312 1197
4b 6.63 3.22 0.68 4.37 27 569 2246
4c 3.98 2.48 0.62 2.79 16 329 1091
4d 5.73 2.75 0.62 3.77 22 345 2529
4e 6.48 3.12 0.68 4.15 24 374 2803
4f 6.54 3.18 0.66 4.39 28 711 10 281
5a 8.27 3.38 0.68 5.14 31 504 7074
5b 7.78 3.58 0.72 4.99 31 604 8539
5c 8.51 3.69 0.73 5.34 33 529 3889
5d 8.42 3.53 0.71 5.25 32 540 7950
5e 6.70 3.47 0.73 4.40 27 566 4528
5f 4.89 2.67 0.67 3.11 16 348 1364
5g 6.77 3.75 0.82 4.24 24 324 2508
5h 5.38 3.57 0.79 3.70 23 510 8010
5i 6.10 3.98 0.86 4.07 25 453 6258
6a VII 7.42 4.08 0.80 5.07 35 1013 7978
6b 3.12 1.46 0.36 2.43 17 735 23 024
7a VI 2.97 1.84 0.46 2.32 16 656 5143
7b 3.70 2.13 0.51 2.76 18 504 1008
7c 4.12 2.24 0.54 2.95 18 344 344
9a IV 4.94 2.68 0.60 3.48 22 438 5958
9b 3.62 2.70 0.71 2.53 14 388 2954
9c 2.95 2.34 0.60 2.27 15 534 11 601
9d 3.85 2.84 0.70 2.78 17 338 4853
9e 4.92 3.22 0.70 3.56 24 658 2623
9f 3.96 2.99 0.68 3.00 21 825 6285
10a 4.07 2.88 0.70 2.88 17 283 2215
10b 4.46 2.84 0.67 3.14 19 330 4020
10c 4.09 2.76 0.67 2.89 17 289 2046
10d 4.32 2.62 0.61 3.12 20 497 9797
10e 4.32 2.58 0.59 3.17 21 576 5331
11a III 4.74 2.47 0.59 3.19 18 332 1552
11b 4.78 2.86 0.70 3.14 17 356 2473
11c 5.83 2.74 0.63 3.68 20 296 1551
11d 4.64 2.50 0.61 3.09 17 329 2008
12a II 4.73 2.82 0.69 3.13 17 177 353
12b 3.75 2.36 0.64 2.52 13 121 478
12c 4.67 2.71 0.68 3.04 16 148 148
12d 4.08 2.90 0.74 2.77 15 165 165
12e 3.08 2.34 0.74 2.01 9 68 68
12h 3.46 2.80 0.73 2.47 14 204 204
13 2.59 2.08 0.63 1.88 10 137 3981
14a 5.68 2.92 0.66 3.70 21 241 241
14b 4.86 2.74 0.65 3.29 19 259 258
14c 6.11 3.09 0.70 3.84 21 204 3099
14e 4.67 3.30 0.78 3.22 19 296 2270
14h 5.77 3.59 0.77 3.95 25 453 3561

Fig. 4. Taxa present: 1. – Lobatula lobatula (Walker and Jacob); 2. – Elphidium macellum (Fichtel and Moll); 3. – Elphidium excavatum (Terquem); 4. – Elphidium advenum (Cushman);
5. – Elphidium complanatum (D’Orbigny); 6. – Elphidium crispum (Linne
´); 7.– Rosalina globularis D’Orbig ny;8. – Nonion commune (D’Orbigny); 9. – Aubignyna perlucida (Heron-Allen and
Earland); 10. – Haynesina germanica (Ehrenberg); 11. – Ammonia beccarii tepida (Cushman); 12. – Ammonia beccarii beccarii (Linne
´); 13. – Asterigerinata mamilla (Williamson);
14. – Turrispirillina sp.; 15. – Spirillina vivipara Ehrenberg; 16. – Trichohyalusaguayoi (Bermu
´dez). Umbilical view; 17. – Trichohyalus aguayoi (Bermu
´dez). Spiral view; 18. – Trochammina
inflata (Montagu); 19. – Miliolinella eburnea (D’Orbigny); 20. – Quinqueloculina vulgaris D’Orbigny; 21. – Cornuspira involvens (Reuss); 22. – Miliolinella circularis (Bornemann).

Fig. 5. Stratigraphic column of the Pinet core. Palaeoenvironmental interpretation and diversity, abundance and evenness of the foraminiferal assemblages.
A.M
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a beach found in the ‘Serra Gelada’ (Fumanal and Ye
´benes, 1996),
and localised deposits in the Ma
´laga coast (Lario et al., 1993), show
limited diagenesis, in contrast to the material in the beach bed of
Unit V which is very cemented.
Radiocarbon dating yielded an age of 7580 cal. BP for the
uppermost foreshore/shoreface deposits. Considering that coastal
lagoon deposits, which characterise the Mediterranean Spanish
coast, are younger than 6500 BP and that their bars formed with the
Fig. 6. Textural distribution (%) (A), % organic matter (B), % CO
3
Ca in the Pinet core. Roman numbers indicate the different sedimentary units.
A.M
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stabilisation of the sea level during this epoch, it is very likely that
this age estimation is too old by several thousand years.
4.1.2. Pinet core
Analysis of 224 samples in the Pinet core resulted in the
recognition of twelve Quaternary depositional units (Fig. 5), based
on a combination of micropalaeontological and sedimentological
data (Fig. 6). Ninety-nine samples contained foraminifera. The
suborder Rotaliina dominates the core (96.98%). The suborders
Miliolina, Textulariina, Spirillinina, and Lagenina represent 2.54,
0.41, 0.04 and 0.02%, of the total, respectively.
Three radiometric dates were carried out in this core (Table 5).
Numerical age of calcareous sandstone (19b) could not be deter-
mined because previous geochemical studies indicated an open
system. The micropalaeontological and sedimentological results of
the sedimentary are provided in Tables 6 and 7.
In the Pinet core, a vertical succession of different palae-
oenvironments, which seems to correspond to coastline oscilla-
tions, was previously observed (Bla
´zquez et al., 1999; Bla
´zquez and
Usera, 2005). The basal unit corresponds to an inner shelf bottom
with sands and abundant carbonate content and is characterised by
a high diversity of species (Table 7). A gradual shallowing of the
environment is recorded above 27 m as reflected by poor shell
preservation, a general decrease in diversity, evenness and number
of specimens in 50 g and a gradual increase of carbonate content
and iron concretions in the sediment. The sedimentary and
micropalaeontological similarities to the Pliocene deposits in the
Molar Range allow the assignment of this unit to this period.
The first Quaternary deposits in this core are at 23 m (Unit II)
after a long erosive period. A littoral high-energy episode with
equigranular flat-shaped pebbles and gravels is recorded. This
deposit corresponds to a foreshore sub-environment. Scarce
biogenic rests occur in the sandy fraction. A possible back-barrier
flat could indicate a limited seaward movement of the coastline in
Unit III. In Despite an absence of foraminifers, this horizon is
interpreted as the rear end of the bar described in Unit II based on
stratigraphical data, its predominantly clayey silt texture, its
organic matter content, and its laminated carbonate precipitates,
which are more abundant at the top. In addition, there are frag-
ments of ostracods (C. torosa (Jones)). In the partially restricted
environment inferred for the top of Unit III, a washover fan,
constituting Unit IV, then invaded the coastal lagoon. Silts and clays
alternating with sands characterise this deposit. The base of the
unit is interpreted as being deposited in calm brackish waters
colonised by autochthonous foraminifera like A. beccarii tepida
(Cushman), H. germanica (Ehrenberg), H. depressula (Walker and
Jacob) or E. excavatum (Terquem). Sediments with littoral and
stenohaline foraminifera from the nearby sea were deposited in
this environment. These allochthonous (resedimented) fossils are
broken and lack external chambers. A washover fan in a restricted
environment is characterised by an increase in diversity and rich-
ness indexes, a decrease in the degree of dominance of some lagoon
species (Table 7) and, particularly, a sharp increase in the number of
individuals (Fig. 5). The absence of miliolids could be due to the fact
that chemical weathering more easily deteriorates porcellaneous
tests (Murray, 1999) or to the absence of seagrass meadows in the
surroundings (Colom, 1974).
These lagoons dried and were replaced by swamp environments
with seasonal freshwater flooding (Unit V). The occurrence of
ostracods like I. gibba (Ramdohr) indicates a lower salinity and
hence suggests that the coastline was still moving seaward. The
foraminifera found in this silty–clayey sediment with abundant
carbonate and ferruginous concretions are reworked. The same
species found in the underlying bed are present, although tapho-
nomic processes have affected both the number of species and
individuals as well as the preservation state of the tests, which are
considerably damaged. The environment becomes less stagnant
towards the top of the unit with the establishment of hydromor-
phic processes in an alluvial context, as indicated by a banded
reddish/grey colour due to the fluctuations of the water table.
Unit VI records a new landward movement of the coastline in
a back-barrier flat facies, as inferred from the occurrence of poorly
preserved marine foraminifera. They are mixed with scarce frag-
ments of ostracods from a nearby lagoon (C. torosa (Jones) and
I. gibba (Ramdohr)). Laminated carbonate deposits are also abun-
dant. Later, this small pulse vanishes in Unit VII and is again
replaced by a shallow lagoon environment colonised by foramini-
fers and ostracods from restricted low-energy brackish. Neverthe-
less a certain marine influence still persists, as indicated by the
occurrence of stenohaline species. The observed relationship
between A. beccarii tepida (Cushman) and H. germanica (Ehren-
berg), in which a decrease in the former is associated with an
increase in the latter, is difficult to explain since both are oppor-
tunistic species that have not been cultivated together. Moreover,
H. germanica (Ehrenberg) is more resistant to environmental
changes (Murray, 1991). This was observed in some Holocene beds
in the Xa
`bia lagoon (Garcı
´a Forner et al., 1993). Towards the top,
drying processes facilitating structureless carbonate deposits in
a saturated environment were observed; these processes were the
origin of the sandy textures that were found (Fig. 6). Later, this
lagoonal facies was replaced by an alluvial environment with
hydromorphic conditions (Unit VIII). These conditions involve
a decrease in the water level, a reworking of the foraminifera
characterising the previous bed and a resedimentation of the
freshwater ostracods (I. gibba (Ramdohr)) from a nearby swampy
environment.
A shallow lagoonal environment is present in Unit IX. Apart
from the higher content of organic matter, this deposit does not
show sedimentary changes compared to the previous unit. It is
characterised by the occurrence of benthonic autochthonous fora-
minifers and brackish water ostracods concentrated in ostracodites,
whose superimposed valves indicate a low-energy calm environ-
ment. E. excavatum (Terquem) and A. beccarii tepida (Cushman) are
incompatible because the latter is dominant and the former is in
a less favourable habitat. Together with these species are diage-
netically modified abraded shells derived from the reworking of
older marine horizons. The foraminifera assemblage indicates
a salinity increase towards the top of the unit, confirmed by the
establishment of a low-energy marine influence (Unit X).
Most sands in Unit X correspond to carbonate concretions, as
indicated by the carbonate proportions and a morphoscopic study.
An intermittent communication with the sea is observed. The
29 795 foraminifers extracted in this unit are characterised by
a mixing of euryhaline and stenohaline species in a similar
Table 5
Numerical dating of the Pinet core.
*
Centre d’E
´tudes et de Recherches Aplique
´es au Karst’ at the ‘Faculte
´Polytechnique de Mons’ (Belgium).
Core Sample Depth (m) Laboratory Age Method Material dated Calibration 2 Sigma range
Pinet 8 2 BETA-140892 11 640 40 BP
14
C (AMS) Organic sediment 13 450 BP 13 640–13360 BP
Pinet 19b 5.5 6442
*
– Th/U Calcareous sandstone
Pinet 67 14 6443
*
198 800 BP Th/U Carbonate
A.M
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´zquez, J. Usera / Quaternary International 221 (2010) 68–90 79

Table 6
Main sedimentological and micropalaeontological results of the Pinet core. Reworked: derived from older strata. Resedimented: derived from contemporary environments.
Both groups indicate allochthonous foraminifera. Autochthonous: in situ assemblages.
Sedimentary
units
Sediment Dominant foraminiferal assemblage Taphonomy
(Foram.)
Other organisms CO
3
Ca
(Average %)
Organ. mat.
(Average %)
Unit XII Sand. Isolated
intercalation of
clay and silt
Ammonia beccarii beccarii (Linne
´),
Elphidium macellum (Fichtel and Moll),
Lobatula lobatula (Walker and Jacob),
Rosalina globularis D’Orbigny and
Asterigerinata mamilla (Williamson)
Allochthonous.
Resedimented
Marine ostracods, fragments of
molluscs: gastropods and bivalves,
like Cerastoderma sp., Plates and
spines of echinoderms
70 0.3
Unit XI Calcareous sandstones Encrusting algae (Melobesia) and
fragments of plates of echinoderms,
molluscs: gastropods and bivalves,
bryozoans.
82 0.02
Unit X Silt and clay. Fragments of
calcareous sandstones.
Ferruginous concretions.
Ammonia beccarii tepida (Cushman),
Haynesina germanica (Ehrenberg) and
Elphidium excavatum (Terquem)
Autochthonous Brackish water ostracods (Candona sp.,
Cyprideis torosa (Jones)) and marine
species
82 0.55
Rosalina globularis D’Orbigny, Elphidium
complanatum (D’Orbigny), Elphidium
macellum (Fichtel and Moll), Triloculina
rotunda D’Orbigny, Triloculina trigonula
(Lamarck), Triloculina oblonga
(Montagu)
Allochthonous.
Resedimented
Unit IX Clay and silt Elphidium excavatum (Terquem),
Ammonia beccarii tepida (Cushman),
Aubignyna perlucida (Heron-Allen and
Earland) and Haynesina germanica
(Ehrenberg)
Autochthonous Ostracods (Candona sp., Cyprideis torosa
(Jones))
46 0.96
Unit VIII Clay and silt. Carbonate
precipitation towards the
top. Ferruginous
concretions.
Ammonia beccarii beccarii (Linne
´),
Elphidium excavatum (Terquem),
Asterigerinata mamilla (Williamson),
Lobatula lobatula (Walker and Jacob),
Bolivina sp. and Brizalina sp.
Allochthonous.
Reworked
Fragments of echinoderms, bivalves,
planktonic foraminifers (Globigerina sp.,
Globorotalia sp.). Autochthonous
ostracods: Ilyocypris gibba (Ramdohr)
and Candona sp.
46 0.8
Unit VII Clay and silt. Carbonate
precipitation and
ferruginous concretions
towards the top
Ammonia beccarii tepida (Cushman),
Haynesina germanica (Ehrenberg) and
Elphidium excavatum (Terquem)
Autochthonous Ostracods: Cyprideis torosa (Jones) 56 0.43
Ammonia beccarii beccarii (Linne
´),
Lobatula lobatula (Walker and Jacob),
Nonion commune (D’Orbigny), Rosalina
globularis D’Orbigny
Allochthonous.
Resedimented
Unit VI Sand and silt. Clay
increasing towards the top
Ammonia beccarii beccarii (Linne
´),
Lobatula lobatula (Walker and Jacob),
Elphidium crispum (Linne
´), Elphidium
macellum (Fichtel and Moll), Elphidium
complanatum (D’Orbigny),
Asterigerinata mamilla (Williamson),
Rosalina globularis D’Orbigny and
Nonion commune (D’Orbigny)
Allochthonous.
Resedimented
Plates and spines of echinoderms,
sponge spicules, calcareous algae,
bryozoans and molluscs (bivalves and
gastropods). Autochthonous ostracods:
Cyprideis torosa (Jones) and Ilyocypris
gibba (Ramdohr)
46 0.47
Unit V Clay and silt. Carbonate
precipitation. Ferruginous
concretions
Ammonia beccarii beccarii (Linne
´),
Lobatula lobatula (Walker and Jacob),
Elphidium complanatum (D’Orbigny),
Rosalina globularis D’Orbigny, Nonion
(D’Orbigny), Elphidium macellum
(Fichtel and Moll) and Elphidium
excavatum (Terquem)
Allochthonous.
Reworked
Freshwater, Ilyocypris gibba (Ramdohr),
and brackish, Cyprideis torosa (Jones)
ostracods, charophytres oogonia
(Lamprothamnium papulosum (Wallr.)).
Bivalves
40 0.44
Unit IV Alternating sand
and silty clay
Ammonia beccarii tepida (Cushman),
Haynesina germanica (Ehrenberg),
Haynesina depressula (Walker and
Jacob), Elphidium excavatum (Terquem)
Autochthonous Fragments of molluscs (bivalves and
gastropods), spines of echinoderms,
sponge spicules, bryozoans, marine
ostracods, planktonic foraminifers
(Orbulina sp.)
54 0.4
Ammonia beccarii beccarii (Linne
´),
Elphidium crispum (Linne
´), Lobatula
lobatula (Walker and Jacob), Rosalina
globularis D’Orbigny, Elphidium
complanatum (D’Orbigny) and Nonion
commune (D’Orbigny)
Allochthonous.
Resedimented
Unit III Sand. Silt and clay towards
the top
Brackish, Cyprideis torosa (Jones)
ostracods,
56 0.4
Unit II Coarse sand with pebbles
and gravels
70 0.15
A.M
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preservation state. A. beccarii tepida (Cushman), H. germanica
(Ehrenberg) and E. excavatum (Terquem) are dominant at the base.
Starting at a depth of 8 m, stenohaline species become more
frequent. From 7 m up to the top, a euryhaline species assemblage
consisting of A. beccarii tepida (Cushman) and H. germanica
(Ehrenberg) with the occasional addition of A. perlucida (Heron-
Allen and Earland) (Fig. 4) is noted. This is reflected in the richness
and diversity indexes and in the number of species in each sample.
The test diameters of the euryhaline species are abundant both in
the >0.063 mm and in the >0.125 mm size fractions, whereas those
of stenohaline species are always over 0.125 mm. The latter show
transport signs including broken chambers, particularly in the
latter fractions. Most are filled and coveredby carbonate accretions,
especially in the deposits with the richest carbonate content. These
micropalaeontological data indicate a lagoon with marine
connection.
The landward movement of the coastline is indicated by the
deposition of Unit X following an erosive episode. This unit is
a beach bed constituted by calcareous sandstone with high
carbonate content. The base of this unit is characterised by abun-
dant encrusting algae (Melobesia), echinoderm plate fragments,
gastropods, bivalves, bryozoa, and benthonic foraminifera. Towards
the top, the calcareous sandstone becomes much more detrital and
rich in quartz and calcareous algae, and in general the fossil content
decreases significantly.
Unit XII is interpreted as a backshore environment, perhaps in
a dune facies, although no crossed lamination was observed in the
consolidated fragments. Nevertheless, the presence of greyish
interbedded silts and clays (without autochthonous fossils)
suggests quiet-water sedimentation in a dune slack. There are
stenohaline foraminifera species that become less abundant
towards the top, as reflected by a (very irregular) decrease in the
number of individuals in 50 g, and in the diversity, richness and
evenness indexes. Ooliths are considered to be sedimentologic
indicators of the Tyrrhenian II marine transgression in the Medi-
terranean (Goy et al., 1993). Their abundance in this unit (especially
at the top, 80% in sample 4) suggests this age for the unit or indi-
cates, at least, the geographical proximityof outcrops from this age.
In summary, the data from this core suggest that on three
occasions during the Quaternary, the coastline was located in
a more landward position than the present shore. Two of these
periods saw the deposition of back-barrier flat facies, one linked to
a previous foreshore deposit and the other to a shoreface envi-
ronment capped with backshore sediments. In relation to the
position of the Pinet core (Table 1), two of these three phases
involve the sea being located more than 750 m landward compared
to its present position. Assemblages of stenohaline foraminifers
occur during these episodes, with diversity, richness and evenness
values varying in a substantial way according to the action of
taphonomic processes, both biostratinomic and fossil diagenesis.
Interbedded with the landward movements, seaward movements
of the coastline are observed, as reflected by continental sedi-
mentation either in the alluvial context of hydromorphic soils with
occasional associated swamp environments or in lagoons.
With respect to the age of these sediments, the location of the
core indicates that the beach capping of the series likely corre-
sponds to MIS 5e or 5c (Tyrrhenian II or III, Goza
´lvez and Rossello
´,
1978). The similarity of the colour and the facies of this material
with a beach bed exposed a few metres away from the core (Goy
et al., 1993), together with the absence of ooliths, in this zone
marking the MIS 5e, suggest attribution to MIS 5c. The continuity
and gradual transition found in the underlying sediments in coastal
lagoon facies, with or without marine influence, seem to indicate
that these two deposits correspond to the same interglacial. It is
likely that the beach corresponding to Tyrrhenian II (MIS 5e), if it
was preserved at this point, was located a few metres landward
from the position of this core. The radiometric dating (Th/U) of
carbonate concretions from sample 67 (Unit VII) yielded an age of
198800 BP. Although the radiometric dates are questionable, this
age might be valid since it is a semi-open geochemical system
(Centre d’E
´tudes et de Recherches Aplique
´es au Karst’ at the ‘Fac-
ulte
´Polytechnique de Mons’ (Belgium)). On this basis the sedi-
ments between 23 m and 9 m might be ascribed to the Middle
Pleistocene. The radiocarbon (
14
C) dating of 13 450 cal. BP from the
organic sediment from the interdune depression (swale) is thus
very questionable and clearly does not relate to a former sea level,
which at this time was significantly below present.
4.1.3. Mo
´rtoles core
A micropalaeontological and sedimentological study of 231
samples indicates twelve Quaternary depositional units (Figs. 7
and 8). Only 16 samples near the top of the core contained foramin-
ifers. The suborder Rotaliina is dominantand represents 94.55%of the
total, although in the top layers the suborder Spirillinina (5.26%)
represents a significant proportion of the total, as do Textulariina
(0.08%) and Miliolina (0.11%) to a lesser degree.
Two radiometric dates were measured from this core. The data
are shown in Table 8. The micropalaeontological and sedimento-
logical results for the sedimentary units, from the bottom to the
top, are shown in Tables 9 and 10.
Reddish clays, silts, and sands characterise Unit I (Fig. 7). At the
base, sands represent up to 60% of the deposit, and pebbles and
gravels are also present. The average carbonate proportion in the
unit is 50%. In general, the carbonate content decreases with
proportion of sands except at the base, which is siliceous. In
contrast, the organic matter content, although low and fluctuating,
increases towards the top of the unit and varies between 0.11 and
0.33%. Carbonate is present particularly between samples 215 and
205, whereas ferruginous concretions occur in the whole unit.
Samples with the highest proportion of silts and clays are greyish-
coloured with reddish interbedded layers due to surface fluctua-
tions of the water table. There is no fossil content except for some
foraminifers reworked from previous marine beds with very
abraded diagenesis-modified tests (abundant internal moulds) fil-
led with carbonate and in a poor preservation state. Thus, this unit
corresponds to an alluvial environment.
Unit II comprises a 9-cm-thick bed of calcareous sands modified
by diagenesis, comprising algal remains (Melobesia) and corals of
Table 6 (continued )
Sedimentary
units
Sediment Dominant foraminiferal assemblage Taphonomy
(Foram.)
Other organisms CO
3
Ca
(Average %)
Organ. mat.
(Average %)
Unit I Fine sand with sandstone
fragments. Pebbles in the
base. Carbonate
precipitation towards the
top. Ferruginous
concretions
Ammonia beccarii beccarii (Linne
´),
Elphidium crispum (Linne
´), Nonion
commune (D’Orbigny), Elphidium
advenum (Cushman), Rosalina globularis
D’Orbigny, Lobatula lobatula (Walker
and Jacob), and Asterigerinata mamilla
(Williamson)
Autochthonous.
Diagenized
Plates and spines of echinoderms,
fragments of molluscs: bivalves and
scaphopods (Dentalium), marine
ostracods, tests of bryozoans
74 0.3
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–90 81

Table 7
Foraminiferal indexes corresponding to the Pinet core. Their graphical representation is shown in Fig. 3.
Sample Unit Fisher alpha Shannon–Wiener Evenness Margalef richness N

Species N

Indiv. N

Indiv./50 g
2 XII 3.19 2.90 0.87 2.12 10 70 797
4 6.97 3.25 0.83 3.53 15 53 1828
7 3.45 2.95 0.89 2.21 10 59 793
11 4.43 3.00 0.84 2.67 12 62 875
12 3.62 3.45 0.96 2.41 12 96 1865
13 3.92 3.64 0.89 2.81 17 296 7383
14 3.46 3.57 0.94 2.47 14 194 15
15 5.81 3.52 0.77 3.91 24 356 12 444
23 X 5.68 3.63 0.79 3.87 24 383 17 240
24b 5.78 3.43 0.75 3.91 24 361 15 225
25b 5.25 3.55 0.78 3.65 23 414 17 054
26b 3.09 1.22 0.31 2.38 16 545 5901
27b 5.82 3.85 0.82 4.02 26 502 4452
28b 5.72 3.70 0.80 3.93 25 446 4400
29 4.35 2.90 0.64 3.26 23 852 21 352
30b 2.31 1.66 0.46 1.83 12 412 20 959
31b 1.58 1.01 0.29 1.35 11 1669 41 560
32b 1.45 1.21 0.38 1.21 9 729 24 896
33b 3.18 1.78 0.44 2.46 17 664 10 830
34b 1.70 1.18 0.34 1.43 11 1106 41 298
35b 2.19 2.26 0.61 1.79 13 826 10 012
36a 3.09 3.27 0.80 2.41 17 754 6223
36b 3.50 3.16 0.72 2.76 21 1409 23 344
37 1.71 2.03 0.55 1.47 13 3457 96 168
38a 2.82 1.48 0.37 2.24 16 820 3538
38b 1.77 0.90 0.24 1.51 13 2759 25 257
39a 1.59 1.16 0.34 1.36 11 1589 3713
(39b) IX 0.90 0.76 0.27 0.78 7 2197 3741
(40a) 0.63 0.90 0.39 0.53 5 1833 2516
(40b) 0.90 0.95 0.37 0.76 6 712 571
(40c) 0.38 0.89 0.56 0.29 3 984 792
(41a) 0.55 0.97 0.49 0.45 4 807 874
(41b) 0.25 0.27 0.27 0.15 2 679 587
(41c) 0.39 0.35 0.22 0.30 3 850 694
(42a) 0.55 0.26 0.13 0.45 4 815 388
(42b) 1.30 0.71 0.24 1.09 8 620 229
(43b) 1.50 0.37 0.12 1.25 9 601 245
52 VII 2.20 1.62 0.47 1.73 12 323 219
54 5.20 2.97 0.83 2.86 13 47 34
59b 4.93 2.98 0.69 3.37 21 279 6583
63 0.92 0.81 0.51 0.64 4 23 133
65 0.98 0.75 0.29 0.82 7 444 2180
67b 1.59 1.19 0.38 1.31 10 471 4936
69 2.27 1.83 0.48 1.86 15 1083 28 815
71 1.27 1.20 0.40 1.07 9 697 13 049
73b 3.01 1.60 0.41 2.30 16 437 286
75 4.37 2.59 0.62 3.05 19 264 668
77b VI 2.98 2.47 0.67 2.21 13 230 3938
79 3.58 2.52 0.62 2.66 17 410 4307
81 3.16 2.25 0.56 2.42 16 496 18 708
83 1.56 1.53 0.51 1.26 8 259 1028
85 3.51 2.81 0.89 2.14 9 42 43
87b 3.43 2.52 0.63 2.55 16 362 3369
89a 5.91 3.39 0.71 4.15 28 668 2399
90a V 4.67 3.15 0.79 3.04 16 139 132
91 3.13 2.88 0.87 2.10 10 73 76
92b 7.74 3.59 0.92 3.66 15 46 45
95 4.16 2.93 0.73 2.86 16 190 531
97 IV 4.99 2.69 0.57 3.67 26 911 7339
99 4.41 2.90 0.62 3.39 26 1590 168 094
100b 4.33 2.97 0.63 3.35 26 1759 103 953
102 4.97 3.37 0.72 3.66 26 925 105 364
104 3.00 2.92 0.75 2.30 15 441 4725
106 1.03 1.23 0.53 0.82 5 131 1157
120b I 2.91 2.19 0.55 2.29 16 705 1475
122 6.51 2.70 0.63 3.80 19 114 257
124 4.38 3.14 0.79 2.94 16 165 94
126 5.73 3.67 0.77 4.03 27 633 4296
128a 4.97 3.05 0.69 3.44 21 335 1171
129 4.76 3.13 0.68 3.49 24 730 2084
A.M
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´zquez, J. Usera / Quaternary International 221 (2010) 68–9082

the species Cladocora caespitosa (Linne
´), that unconformably over-
lies Unit I. Thin section analysis suggests a complex diagenetic story
with ulterior dissolution and infilling processes in a continental
phreatic or vadose environment.
Similar facies to those found in Unit I were recorded in Unit III.
A structureless carbonate precipitate (between 13 and 14 m)
might indicate, on the one hand, a lateral migration of the anterior
channel and lower energy conditions or, on the other hand,
a reduction in the sedimentary supply from the alluvial fan. The
assemblage of these beds is reworked.
A new and significant landward movement of the coastline is
apparent by littoral episode represented by calcareous sandstone
(Unit IV). It contains abundant biogenic rests and small flat pebbles
at its base. Internal and external moulds of bivalves and even of
a pulmonate gastropod (Eobania cf. vermiculata (Mu
¨ller)) occur at
the top. Study of the thin sections shows a finer grain size and
abundant large fragments of algae (Melobesia), rests of bivalves,
echinoderm plates and benthonic foraminifera (including
Ammonia) in the basal samples. The top of this unit is a thin 1-mm-
thick carbonate layer. In general, the grain size increases towards
the top while the marine micropalaeontological content becomes
less abundant. The sedimentary and micropalaeontological char-
acteristics of the calcareous sandstone seem to indicate emerged
conditions, probably linked to backshore environments, with an
intense calcareous cement precipitation. This hypothesis is sup-
ported by the reddish colour of the sediment resulting from
oxidative processes, the presence of the external mould of Eobania
cf. vermiculata (Mu
¨ller) and the occurrence, towards the top, of
a calcareous bed with a 1-mm-thick laminar internal structure.
Nevertheless, smaller grain sizes and increased micro-
palaeontological content were observed in the basal beds, which
might indicate a foreshore facies.
A new seaward movement of the coastline is recorded by Unit V,
in which laminar flooding mechanisms together with carbonate
formation and oxidation linked to possible sporadic flood episodes
is inferred. These distal alluvial facies were replaced by lagoonal
environments (Unit VI), which appear for the first time in this core
at a depth of 8 m, probably corresponding to the beginning of the
‘Albufera d’Elx’ of MIS 1. They consist of grey silts and clays with
a foraminiferal assemblage constituted by A. beccarii tepida
(Cushman), H. germanica (Ehrenberg), A. perlucida (Heron-Allen
and Earland), Trichoyalus aguayoi (Bermudez), and T. inflata (Mon-
tagu) (Fig. 4). As a whole, in the uppermost metres of the core, there
is an alternation of alluvial environments in distal fan facies with
both stream and laminar flood processes (Units VII, IX and XI) and
lagoon-reducing environments (Units VI, VIII, X and XII) charac-
terised by autochthonous brackish water foraminifera. Other fossils
including ostracods (C. torosa (Jones)), charophyte oogonia
(L. papulosum (Wallr.)), and gastropoda (Hydrobia sp.) (Table 9)
confirm the restricted environments in the different units.
Considering that the core is derived from the contact area
between the Vinalopo
´river fan and the ‘‘Albufera d’Elx’’ (the
current ‘‘Salinas’’ of Santa Pola), the paleoenvironmental changes
recorded in the uppermost 8 m could be due to changes in alluvial
and marine processes. Both the sedimentary characteristics and the
thickness of the alluvial layers separating the two deepest lagoonal
beds (Unit VII) suggest an advance of the fan over the previous
lagoonal facies of Unit VI.
Radiometric Th/U dating of the shoreface sediment at 9m
yielded an age of 146500 BP, but the result is uncertain, as it
corresponds to a time of marine regression in the Quaternary
chronology. As for the age of the younger sediments, radiocarbon
dating of organic sediment in the second lagoonal bed, at 3m
(sample 18), yielded an age of 10 220 cal. BP. Considering the
problems observed with the radiocarbon data method and the
nature of these organic sediments (1% organic matter), the upper-
most 8 m of the core is considered as upper Holocene, given the
basal erosive surface (9 m) and its correlation with the erosive
surface associated with the eustatic minimum in the south of the
basin (Soria et al., 1999)(Fig. 9). From a biostratigraphic view, the
Table 7 (continued )
Sample Unit Fisher alpha Shannon–Wiener Evenness Margalef richness N

Species N

Indiv. N

Indiv./50 g
131a 4.46 2.17 0.50 3.18 20 391 2270
132a 2.87 1.82 0.48 2.19 14 375 3922
133a 1.90 1.64 0.47 1.56 11 618 12 322
134a 2.74 1.62 0.43 2.13 12 451 3090
136 3.12 2.00 0.51 2.36 15 381 3889
137b 3.75 1.97 0.47 2.78 18 451 3286
139 4.99 2.95 0.65 3.54 23 497 7329
141 5.15 2.81 0.61 3.66 24 537 13 425
143 5.35 2.89 0.63 3.74 24 470 7008
145 5.43 3.35 0.73 3.77 24 447 10 780
147 5.98 3.23 0.65 4.31 29 1060 25 539
148 5.62 3.46 0.73 3.99 27 679 17 865
149b 5.84 3.12 0.66 4.03 26 495 9656
151 5.94 3.27 0.67 4.25 30 922 18 802
152a 5.94 3.23 0.65 4.29 31 1089 26 872
153 4.73 3.02 0.66 3.47 24 749 9283
155 4.27 2.94 0.77 2.77 14 109 954
157 4.29 2.46 0.55 3.19 22 716 11 149
159 4.01 2.52 0.58 2.98 20 582 8091
161 6.23 2.90 0.60 4.33 29 648 11 975
163 3.70 2.88 0.68 2.80 19 624 10 578
165 3.98 2.63 0.62 2.93 19 467 8453
166 5.01 2.94 0.68 3.40 20 266 2550
167 3.63 2.56 0.63 2.68 17 388 3958
168 3.79 2.44 0.60 2.76 17 331 3940
170 3.82 3.07 0.79 2.67 15 190 986
172 4.01 2.76 0.64 2.98 20 582 5558
174 3.16 2.62 0.67 2.38 15 363 4666
176 3.69 2.97 0.73 2.71 17 367 2394
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–90 83

Fig. 7. Stratigraphic column of the Mo
´rtoles core. Palaeoenvironmental interpretation and diversity, abundance and evenness of the foraminiferal assemblages.
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–9084

abundance of T. aguayoi and its behaviour as an acme zone might
support this hypothesis (Usera et al., 2002).
4.2. Depositional model for the study area
Based on chronostratigraphic correlation of the drill cores, an
evolution model for this area is proposed (Fig. 9).
A marine regression, possibly corresponding to MIS 12, is indi-
cated by a continental deposit with a thick crust of channelled facies
at its top, on which waterlogged soils were deposited. Subsequently,
marine inundation, perhaps associated with MIS 11, is suggestedby
the deposition of first foreshore and then restricted environment
facies that formed in lagoonal environments.
A subsequent lowering of sea level, perhaps in MIS 10, is sug-
gested by a thick alluvial bed, located between 25.5 m and 18 m
a.s.l. in Mo
´rtoles core. The next transgressive phase deposited
a beach facies with abundant corals C. caespitosa (Linne
´). This facies
is recorded in Mo
´rtoles core at 18 m a.s.l. and may relate to MIS 9,
although Zazo et al. (2003) point out the occurrence of these corals in
younger materials. This core is located in the centre of the syncline
separating the Santa Pola and el Molar anticlines and thus belongs to
the coastal sector where the highest sinking rates are recorded. This
maximal subsidence compared to the surrounding areas could
Fig. 8. Textural distribution (%) (A), % organic materia (B), % CO
3
Ca en el sondeo Mo
´rtoles. Roman numbers indicate the different sedimentary units.
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–90 85

explain the preservation of this bed in this core andits absence in the
Pinet core, since the latter is located in the northern flank of the
Molar anticline, which is an area with less subsiding. The palae-
ontological characteristics of the bed point suggest a sea warmer
than the present one at this time. However,since MIS 11 was warmer
than MIS 5e, which is thought to have been tropical (Burckle,1993), it
could also be attributed to this latter stage as well. A new marine
regression is recorded at 17.5 m a.s.l. in the Pinet core and is
attributed to MIS 8. It was characterised by a basal swamp layer
colonised by the freshwater ostracod I. gibba (Ramdohr), thus indi-
cating deposition at some distance from the sea.
A thick lagoonal deposit located between 15 m and 10 m a.s.l
represents a marine highstand in MIS 7. The foraminifera indicate
a shallow brackish water environment with a connection to the sea.
The structureless carbonate precipitation towards the topof this unit
is related to the saturation and drying of the basin, and is probably
linked to the withdrawal of the sea. This environment seems to
correspond inland to a layer of waterlogged soils formed in a topo-
graphic depression and a high oscillating water table. The marine
regression of MIS 6 involves the drying of the lagoonal environments,
the loss of the marine influence and, later, the establishment of
a generalised hydromorphic soil in the study area. In addition, in the
innermost zone channelled facies occur. A thick alluvial bed, most
likely coming from the Molar Range and also with basal channel
bottoms, was deposited towards the coast.
The Tyrrhenian depositslocated in the study areacorrespond with
the overlapping beds in the Pinet quarry, located to the north of the
Molar Range. Goy et al. (1993) identified up to three Tyrrhenian beds
attributedto episodes TII, TIIIand TIV(?): the oldestone is remarkable
because of the substantial presence of ooliths (Zazo et al., 2003). The
analysis of the cores in this study showed a lack of sedimentologic
indicators of TII in this area. On the basis of this finding and the
stratigraphic correlations carried out among the different columns,
marine MIS5c is proposed as theoldest Tyrrhenianepisode preserved
in the core points for the coast of the Elx Depression.
A slight fall in sea level may correspond to MIS 5d as indicated
by a lagoonal bed located above 7.5 m a.s.l. (Pinet core); it was
a shallow environment characterised by assemblages of benthic
foraminifera and brackish water ostracods, which can even be
described as ostracodites. Marine foraminifers gradually invaded
this restricted environment, which is a sign of a new sea level rise.
The climax of the transgression is located in the beach layers
described at 2.5 m a.s.l. on the coast (Pinet core) and at 7.5 m
a.s.l. inland (Mo
´rtoles core), with the latter corresponding to the
backshore facies of the former, which is interpreted as a shoreface
sub-environment. Care should be taken not to over-interpret these
changes, since changes in facies environment may not require
a vertical change in sea level, especially if sediment supply is varied.
This transgressive phase is not represented in the most littoral
sequence (Salinas core) due to a possible fault located between the
Pinet and Salinas cores (Fig. 9), which could have caused sinking of
the coastal sector.
MIS 5b is represented by the erosion surface located on the coast
at 8.5 m a.s.l. Above this erosive signal, a new approximation of
the sea level is suggested by the deposit of a shoreface bed ascribed
to MIS 5a. The marine transgression corresponding to MIS 5a was
preserved in the Salinas core, first in a very sandy shoreface deposit,
probably with a submarine bar morphology (Unit IV), and later in
a shallower environment (Unit V) where it was consolidated. The
sedimentary characteristics and the similarity with Unit III of the
Pinet quarry, which is considered to be Tyrrhenian IV(?) (Goy et al.,
1993), suggests assignment of this unit to MIS 5a. The position of
the beach of the Salinas core, lower than the Pinet one, suggests
that the maximal action of the intra-Tyrrhenian fault took place
between MIS 5c and 5a. The sediment is unlikely to be Holocene in
age due to the strong diagenesis of this material (Goy et al., 1986;
Lario et al., 1993; Fumanal and Ye
´benes, 1996). According to several
authors, the sea level during MIS 5a did not reach the present
height (Chappell and Shackleton, 1986; Zazo, 1999), so its occur-
rence at this point (20 m from the present coastline) would be the
consequence of the aforementioned sinking of the most littoral
sector. Nevertheless, other authors defend a higher position for this
sub-stage in the Mediterranean (Zazo et al., 1997).
After this transgressive maximum, a generalised regression (MIS
4, 3 and 2) with hardly any sedimentary record is preserved. The
continental platform next to the study area shows a weak average
slope (0.32%) during this time, and the coastline was probably
located some 40 km off its current position in ‘La Marina’. There-
fore, in this topographically plain area it is possible that erosionwas
produced especially in the form of small abundant shallow chan-
nels that affected this zone. The Holocene rise in sea level caused
these channels to flood and, in the more continental areas, the
sedimentation of the fan deposits preserved at 6 and 7 m a.s.l. in
the Mo
´rtoles core. These sediments were attributed to the transi-
tion between the uppermost Pleistocene and the middle Holocene
when the sea level reached close to its present position. The gentle
slope of this area might explain the low thickness of the continental
formations related to this period.
The Holocene highstand is recorded in the coastal lagoon
environments as washover fan deposits in the Salinas core. These
environments were associated with the occurrence of a neigh-
bouring bar located to the east, which would have isolated these
restricted environments. Subsequently, when the sea level
continued to rise, this bar ceased to be effective. At this time,
benthic stenohaline organisms coming from an open marine sandy
environment started to penetrate into the lagoon. The relative
increase in benthic foraminifers from restricted waters indicates
a more active bar towards the top of the series.
The Holocene maximum in the Elx Depression sub-basin
resulted in the sea level reaching a more landward position than its
present one, as the deposit recorded in the Salinas core between
1 m and 4.5 m a.s.l. seems to indicate. The sea level advance was
probably interrupted by the obstacle of the series of bars of the
Tyrrhenian episode. This bed may correlate with the shoreface
facies, which several authors (Fumanal and Ferrer,1998; Ferrer and
Bla
´zquez, 1999) have linked to the Santa Pola Holocene deposit,
dated by Goy et al. (1993) at 3290 BP. Towards the top of the Salinas
deposit, more restricted conditions were observed. The sea water
characteristics were probably very similar to the present ones, as
inferred from the occurrence of the same benthic foraminifera
species currently colonising the shoreface environment and the
inner shelf of the Valencian coasts (Bla
´zquez, 1996; Usera and
Bla
´zquez, 1997). A very extensive post-Flandrian lagoonal facies
(Bla
´zquez, 2005) was identified during the upper Holocene.
The thickness of the Quaternary sedimentation might reflect the
subsidence rate experienced by the sector currently occupied by
Table 8
Numerical dating of the Mo
´rtoles core.
*
Centre d’E
´tudes et de Recherches Aplique
´es au Karst’ at the ‘Faculte
´Polytechnique de Mons’ (Belgium).
Core Sample Depth (m) Laboratory Age Method Material dated Calibration 2 Sigma range
Mo
´rtoles 18 2.7 BETA-140890 9040 40 BP
14
C (AMS) Organic sediment 10 220 BP 10240–10 180 BP
Mo
´rtoles 68 9 6444* 146 500 BP Th/U Carbonated sediment
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–9086

the Vinalopo
´alluvial fan. However, on the coast, this subsidence
was moderate, as indicated by the preservation on the surface and
in a parallel arrangement of three of the possible palaeobars that
closed this ancient lagoonal area.
Nevertheless, the depositional model proposed for the study
area is limited by the results of the radiochronological analyses,
many of which were rejected due to their lack of correspondence
with the Quaternary chronology. The materials dated were not
Table 9
Main sedimentological and micropalaeontological results of the Mo
´rtoles core. Reworked: derived from older strata. Resedimented: derived from contemporary environments.
Both groups indicate allochthonous foraminifera. Autochthonous: in situ assemblages.
Sedimentary units Sediment Dominant foraminiferal assemblage Taphonomy
(Foram.)
Other organisms CO
3
Ca
(Average %)
Organ. mat.
(Average %)
Unit XII Clay and silt. Ferruginous
concretions
Trichohyalus aguayoi (Bermudez),
Spirillina vivipara Ehrenberg, Rubratella
intermedia Grell, Turrispirillina sp.,
Elphidium excavatum (Terquem),
Miliolinella eburnea (D’Orbigny) and
Cornuspira involvens (Reuss)
Autochthonous Brackish water bivalves and
gastropods (Hydrobia sp.)
52 1.3
Unit XI Clay and silt. Ferruginous
concretions
Ammonia cf. beccarii beccarii (Linne
´),
Elphidium cf. crispum (Linne
´), Nonion cf.
commune (D’Orbigny), Elphidium cf.
macellum (Fichtel and Moll)
Allochthonous.
Reworked
62 0.65
Unit X Clay and silt. Ferruginous
concretions
Ammonia beccarii tepida (Cushman),
Trichohyalus aguayoi (Bermudez),
Haynesina germanica (Ehrenberg),
Elphidium excavatum (Terquem) and
Physalidia ? sp.
Autochthonous Charophytes (Lamprothamnium
papulosum (Wallr.) Valves of
the ostracod Cyprideis torosa
(Jones).
64 0.6
Unit IX Clay and silt. Carbonate
precipitates. Ferruginous
concretions
Ammonia cf. beccarii beccarii (Linne
´),
Nonion cf. commune (D’Orbigny)
Allochthonous.
Reworked
56 0.4
Unit VIII Clay and silt Ammonia beccarii tepida (Cushman),
Trichohyalus aguayoi (Bermudez) and
Trochammina inflata (Montagu).
Autochthonous Ostracods (Cyprideis torosa
(Jones)) and charophyte
oogonia Lamprothamnium
papulosum (Wallr.).
52 0.6
Unit VII Clay with sand towards
the top Ferruginous
concretions
Ammonia cf. beccarii beccarii (Linne
´),
Asterigerinata cf. mamilla (Williamson),
Nonion cf. commune (D’Orbigny), etc
Allochthonous.
Reworked
Fragments of the ostracod
Cyprideis torosa (Jones)
36 0.08
Unit VI Clay and silt. Ferruginous
concretions
Ammonia beccarii tepida (Cushman),
Haynesina germanica (Ehrenberg),
Aubignyna perlucida (Heron-Allen and
Earland), Trichoyalus aguayoi
(Bermudez) and Trochammina inflata
(Montagu)
Autochthonous Valves of the ostracod Cyprideis
torosa (Jones), charophytes
Lamprothamnium papulosum
(Wallr.).
66 0.4
Unit V Clay with sand. Iron and
carbonate precipitates.
78 0.38
Unit IV Calcareous sandstones.
Towards the top: increasing
grain size and decreasing
proportion of the marine
palaeontological content.
Benthic foraminifera belonging to
suborder Rotaliina and to genus
Ammonia
Autochthonous Encrusting algae (Melobesia),
bivalves, plates of echinoderms.
At the top: impressions,
internal and external moulds of
bivalves and a pulmonate
gastropod (Eobania cf.
vermiculata (Mu
¨ller))
60 0.4
Unit III Alternating silty clay with
sand and interbedded
carbonate crusts.
Ferruginous concretions
Ammonia cf. beccarii beccarii (Linne
´),
Elphidium cf. crispum (Linne
´), Lobatula
cf. lobatula (Walker and Jacob),
Neoconorbina cf. terquemi (Rzehak),
Elphidium cf. macellum (Fichtel and
Moll), Nonion cf. commune (D’Orbigny),
Rosalina cf. globularis D’Orbigny,
Hanzawaia cf. boueana (D’Orbigny),
Pullenia cf. bulloides (D’Orbigny),
Cassidulina cf. laevigata D’Orbigny,
Elphidium cf. complanatum (D’Orbigny),
Cancris cf. auricula (Fichtel and Moll)
Allochthonous.
Resedimented
64 Between 0.3
and 0.6
Unit II Calcareous sandstones Coral: Cladocora caespitosa
(Lı
´nne
´)
90 0.1
Unit I Alternating silty clay with
sand and interbedded
carbonate crusts and basal
pebbles. Ferruginous
concretions
Ammonia cf. beccarii beccarii (Linne
´),
Nonion cf. commune (D’Orbigny),
Elphidium cf. crispum (Linne
´), Lobatula
cf. lobatula (Walker and Jacob),
Neoconorbina cf. terquemi (Rzehak)
Allochthonous.
Reworked
50 Between
0.08 and 0.33
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–90 87

ideal. Furthermore, in the cores nearest sea level, and especially
during the Holocene, it is difficult to establish whether the
changes in sedimentation are due to vertical changes in sea level
or to changes in the coastal sedimentary dynamics. However, the
interpretations of the sediments studied are in agreement with
the geomorphological and tectonic behaviour determined in the
previous studies mentioned above, based on the materials on the
surface.
5. Conclusions
The results of this study indicate the following conclusions:
A. beccarii tepida (Cushman), H. germanica (Ehrenberg),
E. excavatum (Terquem) and T. aguayoi (Bermudez) were the main
foraminifera species colonising the lagoonal environments from
the Middle Pleistocene to the Holocene in the Elx coastal lagoon
(‘l’Albufera d’Elx’).
In the littoral sequence of the Elx Depression, a series of deposits
were chronostratigraphically identified and ascribed to MIS 1–7.
Older deposits observed towards the base of the cores are ascribed
to MIS 8–12. Nevertheless, this depositional model is limitedby the
radiochronological analyses results, many of which were rejected
due to their lack of correspondence with the Quaternary
chronology.
Six transgressive episodes can be recognised, mostly in the form
of calcareous sandstones originating in different sub-environments
of the littoral system. The material of the shoreface Holocene beds
is unconsolidated sands. The abundance and taxonomic
Table 10
Foraminiferal indexes corresponding to the Mo
´rtoles core. Their graphical representation is shown in Fig. 4.
Sample Unit Fisher alpha Shannon–Wiener Evenness Margalef Richness N

Species N

Indiv. N

Indiv./50 g
1 XII 0.80 1.02 0.44 0.67 6 419 5840
2 1.37 1.06 0.35 1.14 9 464 5904
3 1.21 1.22 0.43 1.00 7 395 6304
4 1.00 0.36 0.14 0.83 6 403 6448
9 X 0.57 1.04 0.52 0.47 4 623 19 280
10 0.38 0.97 0.61 0.29 3 1019 46 912
11 0.34 0.86 0.54 0.26 2 2124 22 576
19 VIII 0.50 1.01 0.64 0.38 3 202 404
20 0.35 0.94 0.94 0.22 2 110 220
49 VI 0.38 0.31 0.31 0.23 2 71 568
50 0.31 0.41 0.41 0.19 2 182 1456
51 0.45 0.30 0.19 0.34 3 368 2944
52 0.45 0.25 0.16 0.34 3 356 2848
53 0.70 0.34 0.17 0.56 4 211 844
54 0.49 0.24 0.15 0.37 3 231 3696
55 0.67 0.27 0.13 0.54 4 253 8096
Fig. 9. Correlation of the cores and proposed palaeoenvironmental interpretation.
A.M
a
Bla
´zquez, J. Usera / Quaternary International 221 (2010) 68–9088

composition of planktonic foraminifera indicates the occurrence of
marine Pliocene beds below a depth of 18 m in the littoral sector of
the Elx Depression, which constitutes the base of the Quaternary
sedimentation.
In the Holocene brackish lagoons, the appearance of T. inflata
(Montagu) in the most continental areas indicates lower water
salinity, possibly in the context of a vegetated marsh. High
proportions of the porcellaneous species M. eburnea (D’Orbigny),
indicating a higher salinity, were noted in those beds correspond-
ing to locations closer to the sea or with a greater marine influence.
The sediments showed a seaward movement of the lagoonal
environments during multiple regressive sub-stages and a land-
ward development of those environments during the transgressive
episodes. The strongest eustatic falls involved erosive processes
that gave rise to stratigraphic discontinuities in the continental
area.
On the basis of the current morphology of the coast, it can be
deduced that subsidence has become less active since the last
interglacial period, at least in the littoral sector. This has favoured
the preservation on the surface (above the present sea level) of
a system of bars associated with the different Tyrrhenian episodes,
which were arranged parallel to the current coastline. Considering
the depth of the consolidated deposit of the Salinas core attributed
to MIS 5a, a sinking rate of 0.1 mm/a is inferred in the littoral area of
the Elx Depression.
Acknowledgments
The authors are grateful to Prof. Alfonso Ye
´benes, from the
‘Universidad de Alicante’, for his collaboration in the stratigraphic
interpretation of the Salinas core and to Prof. Fernando Robles (from
the ‘Universitat de Vale
`ncia’) for the taxonomic determination of
the gastropods. The authors also thank the critical review of paper
for the Dr. Jorge Guillem from the ‘Universitat de Vale
`ncia’ and the
Dr. Carmen A
´lvarez, from the ‘Universidad Cato
´lica de Valencia’.
Thanks are also due to Dr. Antony Long (Editor), Dr John Cann,
and an anonymous reviewer for their valuable comments, which
greatly improved this article. This publication has been partially
supported by Projects GV/2009/129 and UCV/2009-006-001.
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