79
Revista de la Sociedad Geológica de España 27 (1)
ISSN (versión impresa): 0214-2708
ISSN (Internet): 2255-1379
SULFATE ISOTOPE COMPOSITIONS (δ34S, δ18O) AND STRONTIUM 
ISOTOPIC RATIOS (87Sr/86Sr) OF TRIASSIC EVAPORITES IN THE BETIC
CORDILLERA (SE SPAIN)
Composiciones isotópicas del sulfato (δ34S, δ18O) y razones isotópicas del estroncio (87Sr/86Sr) en evaporitas triásicas
de la Cordillera Bética (SE España)
Federico Ortí1, Alberto Pérez-López2, 3, Javier García-Veigas4, Laura Rosell1, Dionisio I. Cendón5 and 
Fernando Pérez-Valera6
1 Departament de Geoquímica, Petrologia i Prospecció Geològica, Universitat de Barcelona, 
C/ Martí i Franqués, s/n, 08028 Barcelona, Spain
2 Instituto Andaluz de Ciencias de la Tierra, (CSIC-Universidad de Granada), 
Avda. de las Palmeras nº4, 18100 Armilla (Granada), Spain
3 Departamento de Estratigrafía y Paleontología, Facultad de Ciencias, Universidad de Granada, 
Avda. Fuentenueva, s/n, 18002 Granada, Spain 
4 CCiTUB Centres Científics i Tecnològics, Universitat de Barcelona, 
C/ Lluís Solé i Sabarís, 1-3, 08028 Barcelona, Spain. garcia_veigas@ub.edu
5 ANSTO Australian Nuclear Science and Technology Organisation, 
Kirrawee DC, NSW 2232, Australia 
6 Dpto. de Geología, Facultad de Ciencias Experimentales, 
Campus de Las Lagunillas s/n. 23071 Jaén, Spain
Abstract: Sulfate isotope compositions (δ34S and δ18O) and strontium isotope ratios (87Sr/86Sr) of Tri-
assic evaporites in the Betic Cordillera are addressed for the first time in the present work. Isotope val-
ues have been determined in gypsum and anhydrite samples of the Germanic-type facies (Buntsandstein,
Muschelkalk and Keuper) coming from different outcrops spanning the complete Triassic Period and cor-
responding to both the Internal Zones and the External (Prebetic, Subbetic) Zones of this chain. More
precise age assignments and stratigraphic controls are often obscured because of the intense halokinetic
and tectonic deformation occurred during the Alpine Orogeny in the Betic Cordillera. Isotope values of
Triassic sulfates obtained in the present study range between 12.5 and 16.6 ‰ for δ34S, between 8.9 and
16.9 ‰ for δ18O, and between 0.707615 and 0.708114 for 87Sr/86Sr. These values, as a whole, are in
agreement with those of worldwide Triassic marine evaporites.
Key words: Isotopes, sulfate, strontium, evaporites, Triassic, Betic Cordillera.
Resumen: En este trabajo se presenta por primera vez las composiciones isotópicas del sulfato (δ34S y
δ18O) y las relaciones isotópicas del estroncio (87Sr/86Sr) en evaporitas triásicas de la Cordillera Bética.
Los valores isotópicos han sido determinados en muestras de yeso y anhidrita atribuidas a las facies
germánicas (Buntsandstein, Muschelkalk y Keuper) procedentes de diferentes áreas de la cordillera
que abarcan el Periodo Triásico completo, y que corresponden tanto a las Zonas Internas (Complejo
Alpujárride) como a las Externas (Prebético, Subbético). Debido a la intensa deformación tectónica y
halocinética ocurrida durante la Orogenia Alpina en dicha cordillera, es complicado establecer data-
ciones y controles estratigráficos precisos de las evaporitas triásicas. Los valor isotópicos obtenidos en
el presente trabajo varían entre 12,5 y 16,6 ‰ para δ34S, entre 8,9 y 16,9 ‰ para δ18O, y entre 0,707615
y 0,708114 para 87Sr/86Sr. En conjunto, los valores obtenidos son coincidentes con los asignados en la
bibliografía a las evaporitas marinas triásicas a escala global. 
Palabras clave: Isótopos, sulfato, estroncio, evaporitas, Triásico, Cordillera Bética.
Revista de la Sociedad Geológica de España, 27(1), 2014
80 ISOTOPY OF TRIASSIC EVAPORITES IN THE BETIC CORDILLERA (SPAIN)
Ortí, F., Pérez-López, A., García-Veigas, J., Rosell, L., Cendón, D.I. and Pérez-Valera, F. (2014): Sul-
fate isotope compositions (δ34S, δ18O) and strontium isotopic ratios (87Sr/86Sr) of Triassic evaporites in
the Betic Cordillera (SE Spain). Revista de la Sociedad Geológica de España, 27(1): 79-89.
The study of the isotope composition of the evaporitic and to detect possible differences among the stratigraphic
sulfates is one of the most relevant aspects for their geo- units. The values are compared with those previously
chemical and genetic characterization. The sulfate isotope reported in other Triassic domains of the Iberian Peninsula.
compositions (δ34S and δ18O) and the strontium isotope The results obtained may help to interpret the genesis of the
ratios (87Sr/86Sr) are the most commonly used geochemi- Triassic evaporites. 
cal markers to determine the marine or non-marine origin Otherwise, the dissolution of sulfates of preexisting
of the mother brines and the contribution of different water evaporite formations and their reprecipitation in newly-
types to evaporitic basins. This determination can be done formed ones is a common geologic process that has to be
by means of both the age curves of sulfur and oxygen iso- taken into account in order to elucidate the origin of the
topes in seawater sulfate and the age curve of marine mother brines. This point is particularly significant in geo-
strontium isotope ratios, which may also provide guidance logic domains containing old evaporite formations suitable
on the age of the studied sulfates if it remains unknown. to be recycled in younger lacustrine basins affected by
These curves are being continuously verified and world- intense evaporation.
wide improved (e.g., Claypool et al., 1980; Burke et al., The Iberian Peninsula is one of the best examples of the
1982; Korte et al., 2003; Wortmann and Paytan, 2012). The scenario outlined above. Thus, Mesozoic and Cenozoic
ocean sulfate concentration and its isotope composition marine evaporite formations (Triassic, lowermost Jurassic,
have changed over time as a consequence of different Middle Jurassic, Lower Cretaceous, Upper Cretaceous,
processes: 1) continental weathering mainly affecting older Eocene, Upper Miocene) are abundant and occur in the
evaporites, 2) deposition of sulfur-bearing sediments, periphery or in the substratum of younger, non-marine
mainly evaporites, 3) volcanism and hydrothermal activity, evaporitic basins (e.g., basins of Tajo, Ebro, Duero,
and 4) changes in oceanic water circulation promoting peri- Calatayud and Teruel, and several Betic basins).
ods of oceanic anoxia and sulfide formation. In the Betic Cordillera (Fig. 1), a great number of basins
When sulfate-bearing minerals precipitate in an evap- containing evaporite formations were formed during the
oritic basin, the δ34S 18sulfate and δ Osulfate values can be Neogene in relation with the tectonic evolution of the chain.
almost coincident with those of the mother brine. Likewise, Some of these formations were marine such as those of Late
the 87Sr/86Sr ratios of the strontium incorporated (replacing Messinian age (Sorbas, Níjar and San Miguel de Salinas
Ca and as co-precipitated celestine inclusions) into these basins); many others occurred in the transition from marine
sulfate rocks reflect those of the dissolved Sr2+ in brine. to non-marine conditions such as those assigned to Late
Regarding the sulfate isotope compositions, however, the Tortonian–Lower Messinian age (Granada, Lorca, Fortuna
existence of bacterial sulfate reduction activity (BSR) in and Campo Coy basins); and some others were non-marine
some evaporitic basins might produce strong isotope frac- (Baza, Las Minas de Hellín basins). As a result of the clo-
tionation leading to the removal of the isotopically light sure of the Betic seaway during the Late Miocene, a puzzle
sulfate and the subsequent enrichment in heavy sulfate iso- of interconnected marine sedimentary basins changed their
topes of the residual brine. physiographic configuration and evolved to intramontane
The 87Sr/86Sr ratio in seawater is considered to be basins hosting evaporites in most cases. Sulfate and stron-
homogeneous due to the large difference between the stron- tium isotope variations in the evaporitic successions of these
tium residence time (several millions of years) and its basins allow to elucidate the time when each basin was
mixing time (thousands of years) (Holland, 1984). Marine closed to the seawater inflow and recycled sulfate from
87Sr/86Sr ratios over Earth’s history (Burke et al., 1982; older evaporites.
Veizer et al., 1999; McArthur et al., 2001) have fluctuated Thus, another aim of the present study is to supply data
midway between those of radiogenic continental waters which help in understanding the generalized process of
(87Sr/86Sr ~ 0.7110) and those of hydrothermally altered evaporite recycling in the Neogene formations of the Betic
oceanic basalts (87Sr/86Sr ~ 0.7030). Most of the evaporitic domain. We hope that our results can be used as a docu-
basins formed in transitional (marine to non-marine) set- ment database of the process.
tings have received different water sources (seawater,
runoff, meteoric water, hydrothermal springs, etc.). Triassic evaporite units of the Betic Cordillera
87Sr/86Sr ratios in each type of water depend on particular
chemical water-rock reactions. Strontium isotope ratios in Geological studies of Triassic materials in the Betic
a particular evaporite deposit can be used for deciphering Cordillera related to this subject have been recently focused
the marine o non-marine origin and for identifying the on stratigraphic, sedimentologic, paleogeographic, tectonic,
water sources involved. and paleontologic questions (e.g., Flügel et al., 1984;
The main aim of the present study is to provide an ini- Martín-Algarra et al., 1995; Pérez-Valera and Pérez-López,
tial compilation of isotope values of Triassic sulfates in the 2008; Pérez-López and Pérez-Valera, 2012; Pérez-López et
Betic Cordillera in order to know their range of variation al., 2012). The Triassic of the Betic Cordillera shows exten-
Revista de la Sociedad Geológica de España, 27(1), 2014
F. Ortí, A. Pérez-López, J. García-Veigas, L. Rosell, D.I. Cendón and F. Pérez-Valera 81
Fig. 1.- Geological sketch map of the main tectonic units in the Betic Cordillera (SE Spain), where the location of the sulfate samples
is indicated. Key of the last letters in the sample references: AG, Argos Reservoir; AL, Alcaudete; AR, Archidona; AT, Alicún de las
Torres; B, Brácana; CAL, Cuevas del Almanzora; CL, southeast Calasparra; CM, Cerro Molina; DLC, La Celia diapir; E, Énix; EV, El
Valle; F, Félix; FC, Fuente Camacho; FM, Fuensanta de Martos; GSP, west Calasparra; ME, Meliones spring; N, Negratín Reservoir. 
sive Germanic-type epicontinental facies both in the Exter- in thickness, have been recorded in deep wells (Meliones
nal Zones and in the Internal Zones, although Alpine facies borehole, Table 1) and diapirs (Pinoso and La Rosa diapirs,
also occur in the Internal Zones (Pérez-López and Pérez- near Jumilla; mining boreholes in the Pinoso diapir) (Ortí
Valera, 2007) (Fig. 2). However, gypsum deposits are and Pueyo, 1983; Ortí et al., 1996; Pérez-López and Pérez-
mainly present in the External Zones. Valera, 2003). Mechanical contacts, faulting, and
In the outcrops of the External Zones, a number of brecciation predominate in some of the Triassic outcrops
lithologic units making up the Triassic stratigraphy can be because intense tectonic and halokinetic deformation
identified (Fig. 3). The older materials, which can be attrib- occurred during the Alpine Orogeny (Pérez-López and
uted to the Buntsandstein facies, have only been found very Pérez-Valera, 2003). This deformation results in a variety
locally, in places (SE Calasparra) where red detrital rocks of ‘brecciated gypsum units’ and ‘brecciated outcrops’ that
with some gypsum intercalations crop out (Pérez-Valera et are difficult to correlate one to another.
al., 2000). The most common facies in the Triassic outcrops In the three superposed tectonic complexes of the Inter-
are Muschelkalk carbonates (Pérez-Valera and Pérez- nal Zones (Nevadofilábride, Alpujárride and Maláguide
López, 2008), gypsum-bearing Keuper facies (Pérez-Valera complexes; Vera, 2004), gypsum beds are only important
and Pérez-López, 2008), Norian carbonates of the Zamora- in the Alpujárride Complex (eastern sector of the chain)
nos Formation, and Rhaetian-Lower Jurassic gypsum beds (Figs. 1 and 2).
of the Lécera Fm (Gómez and Goy, 1998) correlated with Concerning the Triassic evaporites of the Betic
the Carcelén Anhydrite unit of Ortí (1987). Cordillera, few data on their isotope composition had been
The sulfate beds of these units (secondary gypsum in published until now. Accordingly, new determinations were
outcrops, anhydrite at depth) may alternate with halite carried out for the present paper with the aim to improve
intervals. Rock salt deposits, up to several hundred metres the genetic interpretations of these evaporites (Fig. 3).
Revista de la Sociedad Geológica de España, 27(1), 2014
82 ISOTOPY OF TRIASSIC EVAPORITES IN THE BETIC CORDILLERA (SPAIN)
Fig. 2.- Regional cross-section (NW-SE) showing the structure of the Betic Cordillera (Pérez-López and Pérez-Valera, 2007, modified
from Vera, 2004). The Triassic deposits constitute, in general, the main detachment level of the tectonic units. Triassic outcropping
occurs in a notably disrupted and fractured manner, and sometimes displays a mixture of different tectonic units. In this context, the
presence of ‘brecciated gypsum units’ is frequent due to tectonism and diapirism.
Materials and methods Diablo Troilite (V-CDT) standard for sulfur and to the
Vienna SMOW standard for oxygen. The analytical error
Appropriate outcrops were selected in order to have a (2σ) was ± 0.2 ‰ for δ34S and ± 0.4 ‰ for δ18O. Isotope
good representation of the most significant Triassic gyp- compositions obtained by the Standard NBS-127 were of
sum units of the External (Prebetic, Subbetic) Zones, 20.3 ± 0.1 ‰ for δ34S, and of 9.3 ± 0.2 ‰ for δ18O. 
including the ‘brecciated gypsum unit/facies’, and of the Strontium isotope ratios (87Sr/86Sr) were determined in
Internal Zones. Triassic units sampled in the External 9 samples of powdered gypsum (Table 2) containing trace
Zones mainly correspond to gypsum beds of the Jaén Keu- amounts of celestine, dolomite and/or magnesite, and in
per Group (Pérez-Lopez, 1998), especially of its upper part one anhydrite sample. All the samples were dissolved in 2
(Tables 1 and 2). However, we have also sampled gypsum mL of >18 MΩcm-1 water in order to minimize the disso-
associated with Anisian detrital rocks (Buntsandstein lution of dolomite and leaching of Sr from clays and other
facies), Ladinian carbonates (Muschelkalk facies) of the terrigenous material. Samples were left to react overnight
Cehegín Formation, and gypsum beds that overly the and then centrifuged. The supernatant was removed, taking
Norian carbonates of the Zamoranos Formation. In the care not to disturb any undissolved residue. The super-
Internal Zones, sampling was completed with a number of natant was dried, redissolved in HNO3, loaded onto
Triassic rocks of the Alpujárride Complex. Sr-Spec resin pre-conditioned columns and the eluted Sr
Mineralogical identification of 20 samples collected was finally loaded onto a Ta filament with H2O and H3PO4,
from all these Triassic outcrops of the Betic Cordillera (Fig. for TIMS (Thermal Ionisation Mass Spectrometry) analy-
1, Tables 1 and 2) was carried out by X-Ray Diffraction sis. The isotopic ratios were measured on a VG 354 TIMS
and by Scanning Electron Microscopy. Thin sections of 15 with a long term analytical precision of ± 0.000014 meas-
representative samples were prepared for petrographic ured on NBS-987 (87Sr/86Sr: 0.710288 ± 0.000014).
characterization. 87Sr/86Sr ratios were normalized to 86Sr/88Sr = 0.1194.
Secondary gypsum and anhydrite samples (16 and 3,
respectively) were selected for sulfate isotope analyses Results
(Table 2). Each sample was dissolved in distilled water,
acidified to pH 3 adding HCl and then reprecipitated as bar- Mineralogy and petrology
ium sulfate by means of a solution of BaCl2. Sulfur and
oxygen isotope compositions were analyzed by the on-line Mineral composition of sulfate samples of the Betic Tri-
method. The δ34SV-CDT was determined with a Carlo Erba assic selected for the present work is relatively
1108 Elemental Analyzer and the δ18OV-SMOW with a TC-EA homogeneous (Tables 1 and 2). Predominant sulfate is gyp-
unit, both coupled to an IRMS Thermo Finnigan Delta Plus sum, with minor amounts of celestine, which is present in
XP at the Stable Isotope Laboratory of the CCiTUB (Uni- all samples, and anhydrite in some samples. Associated car-
versitat de Barcelona). The obtained δ34S and δ18O values bonates are mainly dolomite, with minor calcite and scarce
(Table 2) are reported in ‰ relative to the Vienna Canyon magnesite. Accessory minerals are quartz, hematite and
Revista de la Sociedad Geológica de España, 27(1), 2014
F. Ortí, A. Pérez-López, J. García-Veigas, L. Rosell, D.I. Cendón and F. Pérez-Valera 83
EXTERNAL ZONES
Sample Location Rock type andmacroscopic features Texture and host material
Quarry located to Gypsum texture derived from the hydration of a precursor anhydrite rock.
the N of the Puente Secondary gypsum rock. Light- Gypsum components: complex net of veins, which show the same opticalcoloured, fine-grained, extinction in wide parts of the thin section; satin spar (fibrous) veins;
11-40-B Castilla bridge; tothe S of Brácana laminated gypsum clast with microcrystalline groundmass; some euhedral crystals. Small celestine
village; Granada little host material, which is crystals, with intensely corroded boundaries. The host material is formed
basin embedded in a gypsum breccia by: scattered, anhedral/subhedral crystals of dolomite (?); and few euhedralquartz crystals
Quarry located to Secondary gypsum rock. Light- Gypsum texture derived from the hydration of a precursor anhydrite rock;
the N of Fuente coloured, with diffuse banding; the texture is party recrystallized. Gypsum components: large (variable
Camacho village; the sample is a pure gypsum sizes between 0.5 and 1 mm), euhedral (prismatic sections) crystals,11-46-FC near Archidona block of alabastrine appearance, relatively oriented, with somewhat undulose optical extinction, and without
town, to the W of which is included in a anhydrite relics. Small, isolated celestine crystals. The very scarce host
Granada gypsiferous breccia material is formed by: microcrystals and coarser crystals of dolomite thatseem to replace gypsum
Mixed, heterometric gypsum texture derived from the hydration of a
precursor anhydrite rock, with the appearance of partial recrystallization.
Alicún de las Torres Secondary gypsum rock. Gypsum components: porphyroblasts, microcrystalline groundmass, and
village; to the N of Banded gypsum with dark, euhedral crystals. Porphyroblasts vary from isolated crystals to radial
12-3-AT Guadix town porphyroblastic laminae, and aggregates with undulose extinction and planar boundaries, and all they
(Guadix basin); some fine-grained, light- retain small anhydrite inclusions and seem to be partly recrystallized.
Granada province coloured laminae Celestine crystals, up to 1 mm in size, are present; they have corrodedboundaries and contain small anhydrite inclusions. The host material is
formed by dolomicrite matrix and some dolomicritic clasts scattered
throughout the thin section giving way to a diffuse lamination
Mixed, heterometric gypsum texture derived from the hydration of a
Secondary gypsum rock. precursor anhydrite rock, with the appearance of partial recrystallization.
Fuentesanta de Nodule of pink, Gypsum components (all they without anhydrite relics): unoriented,
12-17-FM Martos village; Jaén microcrystalline gypsum euhedral to subhedral crystals; some veins; microcrystalline groundmass;province; upper part including some grey carbonate large crystalline plates with undulose extinction. Small, scattered celestine
of K3 unit matrix, and sourrounded by red crystals. The host material is formed by: rectangular clasts of phyllosilicate
clay rocks; scattered, anhedral dolomite crystals; and few crystals of authigenic
quartz bearing tiny inclusions of anhydrite and gypsum
Mixed, heterometric gypsum texture derived from the hydration of a
precursor anhydrite rock. Gypsum components: large porphyroblastic
plates; fine-grained alabastrine masses; very irregular veins. The
La Celia diapir; Secondary gypsum rock. Light- porphyroblastic plates have undulose extiction and sutured contacts; theyDLC-1 Murcia province;
Keuper coloured, laminated gypsum
are poikilitic locally and contain relic inclusions of anhydrite. The host
material is formed by: abundant micrite arranged in thin, diffuse laminae;
possible pseudomorphs of precursor microselenite crystals forming
laminae; aggregates of sparitic, dark crystals of possible dolomite; hematite
crystals (20 to 60 µm in size)
Porphyroblastic gypsum texture derived from the hydration of a precursor
La Celia diapir; Secondary gypsum rock. White anhydrite rock. Gypsum components: porphyroblasts with the appearance
DLC-2 Murcia province; gypsum formed by large of large, crystalline plates; these plates are anhedral, have irregular
Keuper crystals extinction and euhedral interlocking boundaries, and bear abundantanhydrite relics. The host material is almost lacking: some scattered
micrite; few residual masses of spherulites (zeolites?)
INTERNAL ZONES
Sample Location Rock type andmacroscopic features Texture and host material
To the SE of Félix Secondary gypsum rock (clast Heterometric, recrystallized gypsum texture derived from the hydration of a
village; Almería associated with the brecciated precursor anhydrite rock. Gypsum components: coarse (up to 1 mm in size),
12-25-F province; matrix in the sample 12-26F). unoriented, euhedral-to-subhedral crystals with planar to interlocking
Alpujárride Light grey, medium-grained, boundaries, without anhydrite inclusions; some microcrystalline matrix.
Complex laminated gypsum with Small celestine crystals. The scarce host material is formed by: dolomitemillimetre-sized crystals (microsparite to sparite) arranged in diffuse laminae
Calcareous microbreccia with heterometric-sized (silt, sand and granule)
To the SE of Félix Detrital rock; microbrecciated clasts. Components: clasts of carbonates (dolostone, micritic rocks),village; Almería phyllosilicates and sandstones (quartz-arenites); isolated crystals of
12-26-F province; gypsiferous matrix. Grey andyellow tonalities, with an dolomite and quartz; gypsum cement formed by large, anhedral, poikiliticAlpujárride arenite/wacke appearance gypsum crystals; ‘hexagonal’ crystals of pyrite; tiny crystals of celestine;Complex tiny magnesite crystals that are included within the dolomite clasts;
abundant gypsum cementing preexisting porosity
Table 1.- Petrography of representative calcium sulfate samples of the Triassic outcrops in the Betic Cordillera.
Revista de la Sociedad Geológica de España, 27(1), 2014
84 ISOTOPY OF TRIASSIC EVAPORITES IN THE BETIC CORDILLERA (SPAIN)
INTERNAL ZONES
Sample Location Rock type andmacroscopic features Texture and host material
Irregular distribution of dolomite crystals and dolostone (?) clasts arranged
in diffuse lamination, in association with abundant gypsum crystals.
To the SW of Enix Components: anhedral, dirty carbonate crystals; coarse, euhedral to
village; Almería Gypsiferous dolostone, with the subhedral gypsum crystals often with undulose extinction, which
12-27-E province; appearance of a grey, laminated poikilitically include carbonate crystals and clasts, to which they replace
Alpujárride gypsum rock locally. These gypsum crystals, which have not anhydrite relics, behave as a
Complex cement with an anhedral-to-blocky texture; tiny celestine and pyrite
crystals; clasts of quartz-arenites; clasts of other siliceous rocks and
particles
Quarry in the Sierra Dense, recrystallized gypsum texture, which originally was derived from
de Almagro, to the the hydration of a precursor anhydrite rock. Gypsum components: euhedral
N of Cuevas de Secondary gypsum rock. (prismatic sections) and subhedral, unoriented gypsum crystals with
12-29-CAL Almanzora village; Massive bed of white, sacaroid variable size (up to 1 mm) and without anhydrite relics, whose boundaries
Almería province, (medium-grained) gypsum are from planar (blocky texture) to sutured; and very scarce gypsum
Alpujárride groundmass. Relatively large celestine crystals are present, which appear to
Complex be corroded by gypsum. The host material is formed by scattered, anhedralto subhedral dolomite crystals
Microsparitic-to-sparitic, xenotopic dolostone formed by heterometric
dolomite crystals arranged in diffuse lamination. A vein system formed by
Quarry in the Sierra transparent, euhedral (prismatic sections) to subhedral gypsum crystals is
de Almagro, to the present; these crystals behave as a cement and have not anhydrite
N of Cuevas de Gypsiferous (gypsum veins) inclusions. Those parts of the dolostone in close relation with the gypsum
12-30-CAL Almanzora village; dolostone, with the appearance veins display coarse dolomite crystals, which in turn are associated with
Almería province; of light-coloured, massive, very coarse gypsum crystals; many other parts of the rock show gypsum crystals
Alpujárride pure marble or alabaster rock isolated or forming small clusters; all these parts probably represent
Complex preexisting porosity which was later cemented by gypsum and largedolomite crystals. Some celestine and quartz crystals are present as well as
prismatic crystals of Na-silicate (with almost straight optical extinction, and
with several types of twins)
Table 1.- (continuation) Petrography of representative calcium sulfate samples of the Triassic outcrops in the Betic Cordillera.
clays (clay mineralogy was not identified in the present The celestine crystals in the gypsum samples have
work). variable size, from tens of µm up to1 mm. The growth
The petrographic study of selected thin sections is sum- timing of these crystals is not readily determined.
marized in Table 1. Gypsum is secondary (derived from the Presently, small amounts of celestine precipitate in asso-
hydration of precursor anhydrite) in all the samples, and its ciation with gypsum in both marine and non-marine
textures vary largely from unaltered to strongly recrystal- modern evaporite environments. In some of the studied
lized. samples celestine might have been late diagenetic given
Non-recrystallized gypsum textures are only present in that they contain tiny inclusions of anhydrite, which in
some samples of the External Zones. These little modified most cases was a burial (late) diagenetic product. In gen-
textures show a number of petrographic components, some eral, the celestine crystals exhibit boundaries that are
of them preserving anhydrite relics: porphyroblastic crystals, corroded by the hosting secondary gypsum, suggesting
either isolated or in groups; microcrystalline groundmass that celestine was affected by (was formed prior to) the
(alabastrine matrix); euhedral to subhedral crystals, in which final hydration of anhydrite into secondary gypsum.
prismatic sections are predominant; large crystalline plates Whatever the case, the abundance of celestine is very low.
with contact boundaries ranging from planar to interpene- Presumably, such a low content and the low solubility of
trated; and fibrous (satin spar) veins. Many gypsum textures SrSO4 suggest that celestine has no influence on the stron-
combine several of these components. Recrystallized tex- tium isotope determination.
tures are evidenced by progressive changes from these
components to a homogeneous texture formed by coarse, Sulfate isotope compositions (δ34S, δ18O) and strontium
euhedral crystals either aligned or unoriented, in which isotope ratios (87Sr/86Sr)
anhydrite relics are totally absent. These recrystallized tex-
tures are preferentially observed in samples of the Internal Sulfur isotope compositions (δ34Ssulfate) of Triassic
Zones, given the metamorphism they have undergone. evaporites of the Betic Cordillera determined in the pres-
Carbonate associated with secondary gypsum is mainly ent study range between 12.5 and 16.6 ‰ averaging 14.9
dolomite, either forming discontinuous laminae or as irreg- ± 1.0 ‰. The corresponding oxygen isotope compositions
ularly distributed masses within the rock. Anhydrite (δ18Osulfate) exhibit a wider range, from 8.9 to 16.9 ‰ with
samples coming from boreholes show a marked recrystal- an average value of 12.6 ± 2.1 ‰ (Table 2). Strontium iso-
lized texture, which is formed by coarse crystals with tope counterparts range between 0.707615 and 0.708114
interpenetrated contact boundaries. (Table 2).
Revista de la Sociedad Geológica de España, 27(1), 2014
F. Ortí, A. Pérez-López, J. García-Veigas, L. Rosell, D.I. Cendón and F. Pérez-Valera 85
Fig. 3.- Triassic stratigraphy in the Betic External Zones (modified from Pérez-López, 1998), where the units hosting evaporites are
shown and the situation of the sulfate samples is indicated. These evaporites contain associated deposits of anhydrite and salt, which are
known from boreholes. Legend: 1: Gypsum/anhydrite 2: Nodular gypsum and clay; 3: Lutite/marl; 4: Sandstone; 5 Marly limestone
and marl 6: Limestone; 7: Dolostone; 8: Carniolar carbonate 9: Red claystone and conglomerate. Schema out of scale.
Revista de la Sociedad Geológica de España, 27(1), 2014
86 ISOTOPY OF TRIASSIC EVAPORITES IN THE BETIC CORDILLERA (SPAIN)
BETIC EXTERNAL ZONES
Age range Sample Coordinate Location (Province1) δ34S‰ δ18O‰ 87Sr/86Sr Lithofacies/(unit) Mineralogy2 Ref.3
Upper Triassic? 11-40-B 37º 12’ 15’’ S Brácana (GR) 14.0 12.1 Laminated secondary gypsum03º 56’ 25’’ (brecciated units) gyp (cel, q) a
Upper Triassic? 11-44-B 37º 12’ 05’’ S Brácana (GR) 13.6 11.8 Alabastrine secondary gypsum03º 56’ 29’’ (brecciated units) gyp (cel, q) a
Norian? 11-46-FC 37º 06’ 18’’ N Fuente Camacho (GR) 15.4 12.8 Alabastrine secondary gypsum04º 16’ 04’’ (Keuper, K5 unit?) gyp (cel, dol, cal) a
Norian? 11-50-AR 37º 04’ 56’’ S Archidona (MA) 14.5 11.5 Alabastrine secondary gypsum04º 22’ 31’’ (Keuper, K5 unit?) anh (dol, gyp) a
Anisian 12-1-CL 38º 12’ 22’’ SE Calasparra (MU) 14.7 13.7 0.708114 Nodular secondary gypsum (Bunt-01º 38’ 10’’ sandstein) gyp (q, anh, cel ) *
Upper Triassic? 12-3-AT 37º 29’ 17’’ Alicún de las Torres (GR) 15.0 11.6 0.707615 Laminated secondary gypsum03º 08’ 03’’ block gyp, cel *
Upper Triassic? 12-4-AT 37º 29’ 18’’ Laminated secondary gypsum03º 08’ 03’’ Alicún de las Torres (GR) 15.8 16.7 0.707896 (brecciated units) gyp (mgs, cel) *
Carnian-Norian 12-6-N 37º 33’ 51’’ N Bácor (GR) 15.2 11.2 0.707857 Laminated secondary gypsum gyp (anh, dol, mgs,2º 57’ 35’’ (Keuper) cel) *
Carnian-Norian 12-7-N 37º 33’ 51’’ N Bácor (GR) 15.6 13.5 Laminated secondary gypsum2º 57’ 34’’ (Keuper) gyp, cel *
Carnian 12-15-AL 37º 35’ 13’’04º 09’ 06’’ W Alcaudete (J) 16.2 12.3
Laminated secondary gypsum
(Keuper, K1 unit) gyp (anh, dol, cel) *
Carnian-Norian 12-6-N 37º 33’ 51’’ N Bácor (GR) 15.2 11.2 Laminated secondary gypsum gyp (anh, dol, mgs,2º 57’ 35’’ (Keuper) cel) *
Carnian-Norian 12-7-N 37º 33’ 51’’ N Bácor (GR) 15.6 13.5 Laminated secondary gypsum2º 57’ 34’’ (Keuper) gyp, cel *
Norian 12-18-FM 37º 38’ 24’’03º 55’ 06’’ Fuensanta de Martos (J) 15.4 16.9
Laminated secondary gypsum (K5
unit) gyp, cel *
Rhaetian 12-21-CM 37º 48’ 09’’ Laminated secondary gypsum 03º 44’ 11’’ Puente Tablas (J) 14.8 10.0 0.707757 (Carcelén Anhydrite unit) gyp (anh, dol, cel) *
Ladinian-Carnian 12-22-AG 38º 10’ 15’’01º 43’ 24’’ Argos (MU) 16.4 13.5 0.707720
Laminated gypsum (uppermost 
part of Muschelkalk) gyp, cel *
Upper Triassic? 12-24-ME 36º 59’ 13’’ W Antequera 04º 44’ 50’ Meliones borehole (MA) 14.8 13.6 0.707985 Anhydrite core (923 m depth)
anh, dol (q, mgs,
cel) *
Carnian DLC-1 38º 26’ 25.3’’ 01º 32’ 10.5’ La Celia diapir (MU) 14.5 10.7
Laminated secondary gypsum gyp (anh, cal, cel, q,
(Keuper) hem, mgt) *
Carnian DLC-2 38º 26’ 25.3’’ Megacrystalline secondary gypsum01º 32’ 10.5’ La Celia diapir (MU) 14.6 10.8 (Keuper) gyp (anh, mgt) *
Upper Triassic GSP-1 38º 13’ 45’’01º 42’ 47’’ Calasparra (MU) 15.4 14.6
Laminated secondary gypsum
(Keuper) Gyp b
Upper Triassic GSP-2 38º 13’ 45’’01º 42’ 47’’ Calasparra (MU) 13.8 12.4
Laminated secondary gypsum
(Keuper) Gyp b
Upper Triassic Montealegre del Castillo 13.8 Laminated secondary gypsum(ALB) (Keuper) Gyp d
Upper Triassic S2-168.3 m 38º 23’ 31’’ Pinoso diapir borehole01º 1’ 30’’ (ALI) 12.5 11.5 Laminated anhydrite (Keuper) Anh c
Upper Triassic S2-318.8 m 38º 23’ 31’’ Pinoso diapir borehole01º 1’ 30’’ (ALI) 15.8 10.9 Laminated anhydrite (Keuper) Anh c
Rhaetian-lower- 39º 5’ 16.60’’
most Jurassic 1242 m 01º 18’ 12.70’’ Carcelén borehole (ALB) 16.3 12.6
Nodular anhydrite 
(Anhydrite Zone) Anh c
Rhaetian-lower- 39º 5’ 16.60’’ Nodular anhydrite 
most Jurassic 1247 m 01º 18’ 12.70’’ Carcelén borehole (ALB) 14.8 13.9 (Anhydrite Zone) Anh c
Rhaetian-lower- 39º 5’ 16.60’’ Massive anhydrite 
most Jurassic 1522 m 01º 18’ 12.70’’ Carcelén borehole (ALB) 14.8 9.7 (Anhydrite Zone) Anh c
Rhaetian-lower- 1525 m 39º 5’ 16.60’’ Carcelén borehole (ALB) 13.3 10.2 Nodular anhydrite most Jurassic 01º 18’ 12.70’’ (Anhydrite Zone) Anh c
Upper Triassic 1948 m 39º 5’ 16.60’’01º 18’ 12.70’’ Carcelén borehole (ALB) 13.9 8.9 Massive anhydrite (Keuper) Anh c
Upper Triassic 1949 m 39º 5’ 16.60’’01º 18’ 12.70’’ Carcelén borehole (ALB) 13.5 9.0 Massive anhydrite (Keuper) Anh c
Middle Triassic 1184.8 m 39º 1’ 37.5’’0º 14’ 25.7’’ Jaraco-1 borehole(V) 16.6 11.5
Nodular anhydrite
(Muschelkalk) Anh c
BETIC INTERNAL ZONES
Age range Sample Coordinate Location (Province) δ34S‰ δ18O‰ 87Sr/86Sr Lithofacies/(unit) Mineralogy Ref.
Upper Triassic? 12-25-F 36º 52’ 10’’ Secondary gypsum block  (breccia- gyp (cel, dol, anh)02º 38’ 38’’ SE Félix (AL) 15.9 14.9 ted unit, Alpujárride Complex) cal, q *
Upper Triassic? 12-26-F 36º 52’ 10’’ SE Félix (AL) 15.8 16.1 Secondary gypsum matrix  (brec- gyp (q, dol, pyr) ru,02º 38’ 38’’ ciated unit, Alpujárride Complex) cel, mgs, mus, chl *
Upper Triassic? 12-27-E 36º 52’ 26’’02º 37’ 16’’ SW Enix (AL) 16.0 16.3
Laminated grey, secondary gypsum
bed (Alpujárride Complex) gyp (dol, cel) q, mus *
Upper Triassic? 12-29-CAL 37º 21’ 29’’ Cuevas del Almanzora (AL) 15.4 14.2 0.707744 Sacaroid white, secondary gypsum gyp (dol, cel) Q,01º 52’ 38’’ bed (Alpujárride Complex) anh?, pyr? *
Upper Triassic? 12-30-CAL 37º 21’ 29’’ Cuevas del Almanzora (AL) 15.1 14.3 Crystalline, secondary gypsum bed dol (gypsum veins)01º 52’ 38’’ (Alpujárride Complex) mus *
Upper Triassic? 12-33-EV 37º 19’ 20’’ El Valle (AL) 15.2 12.1 0.707819 Crystalline, secondary gypsum anh (gyp, q, mgs,02º 34’ 28’’ block (Nevadofilábride Complex) cel) *
Upper Triassic? 12-35-EV 37º 19’ 20’’02º 34’ 28’’ El Valle (AL) 15.4 10.8
Crystalline, anhydrite rock (Neva-
dofilábride Complex) anh (mgs, cel, dol) *
1 Province: AL Almería, ALB Albacete, ALI Alicante, GR Granada, J Jaén, MA Málaga, MU Murcia, V Valencia
2 Mineralogy: anh anhydrite, cal calcite, cel celestine, chl chlorite, dol dolomite, hem hematite, mgs magnesite, mgt magnetite, mus muscovite, pyr pyrite, q quartz, ru rutile
3 Ref. Reference: a García-Veigas et al. (2013); b Gibert et al. (2007); c Utrilla et al. (1992); d Gómez Alday et al. (2004); *: this work.
Table 2.- Location, isotope values (δ34S and δ18O of sulfate; 87Sr/86Sr ratios), and main features of the studied sulfate samples. Pro-
vince key: AL, Almería; ALB, Albacete; ALI, Alicante; GR, Granada; J, Jaén; MA, Málaga; MU, Murcia; V, Valencia. Data from the
present work (*) and from the literature (a, b, c).
Revista de la Sociedad Geológica de España, 27(1), 2014
F. Ortí, A. Pérez-López, J. García-Veigas, L. Rosell, D.I. Cendón and F. Pérez-Valera 87
Discussion during the Rhaetian stage. Strontium isotope data from the
Betic evaporites in the present study are in the range with
Besides the former determinations, other isotopic val- those expected for Triassic marine evaporites (Fig. 5). The
ues (δ34S 18sulfate, δ Osulfate) available in the literature (Utrilla sample assigned to the Buntsandstein facies shows the
et al., 1992; Gómez-Alday et al., 2004; Gibert et al., 2007, highest ratio (sample 12-1-CL; 87Sr/86Sr: 0.708114; Tables
García-Veigas et al., 2013) of Triassic sulfates coming from 1 and 2) while the sample attributed to the uppermost part
the central and eastern sectors of the Betic Cordillera of the Muschelkalk carbonates (sample 12-22-AG;
(Pinoso diapir and Montealegre del Castillo outcrops, 87Sr/86Sr: 0.707720; Tables 1 and 2) falls within the gen-
Carcelén and Jaraco-1 boreholes; Calasparra outcrops; out- eral Triassic range. Significant isotopic differences were
crops in surrounding areas of the Granada basin) are not observed between samples from the External Zones and
included in Tables 1 and 2. Thus, values ranging from 12.5 the Internal Zones (Fig. 6).
to 17 ‰ for δ34S and from 9 to 17 ‰ for δ18O are the most
commonly found in the Triassic evaporites of the Betic
domain (Fig. 4). As a whole, these sulfur and oxygen iso-
tope values are similar to those reported for the
northwestern domain of the Iberian Range (Alonso-
Azcárate et al., 2006; Iribar and Ábalos, 2011) and for the
Catalan Coastal Ranges and the Pyrenean Chain (Utrilla et
al., 1992). All these results are also similar to the values
referred to in the literature for marine Triassic sulfates
(Claypool et al., 1980; Cortecci et al., 1981; Rick, 1990;
Fanlo and Ayora, 1998; Longinelli and Flora, 2007;
Boschetti et al., 2011). The only sample analysed assigned
to the Buntsandstein facies is in the range of the Keuper
values. The two samples assigned to the Muschelkalk
facies show higher δ34S values, close to 16.5 ‰, while the Fig. 5.- 87Sr/86Sr variations for the Permian-Triassic marine sedi-
corresponding δ18O data fit well with the Triassic range. mentary rocks (after Burke et al., 1982, Veizer et al., 1999, and
Korte et al., 2003), with indication of the 87Sr/86Sr values of the
studied samples (dotted lines in the Buntsandstein and Muschel-
kalk samples; area comprised between dotted lines in the Keuper
samples).
Fig. 4.- Plot of the sulfate isotope composition (δ34S vs δ18O) of
the studied samples. 
The 87Sr/86Sr variations for the Phanerozoic marine sed- Fig. 6.- Plot of the 87Sr/86Sr vs δ34S values of the studied samples.
imentary rocks (Burke et al., 1982; Veizer et al., 1999; Ext.: External Zones; Int.: Internal Zones.
Korte et al., 2003) record a marked increase from values
close to 0.706900 during the Late Permian to 0.708200 at Strontium isotope ratios reported for Keuper evaporites
the end of the Early Triassic. A progressive drop occurs of the Cameros Basin, in the Northern sector of the Iberian
during the Middle Triassic to values close to 0.707600 at Range (Alonso-Azcárate et al., 2006), are within the lower
the end of the Ladinian stage, although some small differ- part of the range obtained in the present work (0.707615 –
ent trends have been reported between the Tethys and the 0.708114). 
mid-European Muschelkalk Sea values (Korte et al., 2003). A brief reference can be made to the interest of these
Most of the Late Triassic time period, to which the Keuper data regarding the origin of the Neogene evaporite forma-
facies corresponds, is characterized by a progressive radio- tions in the Betic domain. Two factors should be
genic enrichment with a 87Sr/86Sr trend from 0.707600 to considered: (1) the chemical recycling of Triassic sulfates
0.707800 followed by a one-off increase to ~ 0.708200 at into the Neogene ones, and (2) the nature of the mother
the end of the Norian stage, and a final drop to ~ 0.707800 brines from which the Neogene evaporites precipitated.
Revista de la Sociedad Geológica de España, 27(1), 2014
88 ISOTOPY OF TRIASSIC EVAPORITES IN THE BETIC CORDILLERA (SPAIN)
Thus, some of the Neogene evaporites have sulfates cha- Burke, W.H., Denison, R.E., Hetherington, E.A., Koepnick, R.B.,
racterized by δ34S values suggesting direct recycling of Nelson, H.F. and Otto, J.B. (1982): Variation of seawater
87 86
Triassic sulfates in meteoric waters (14-16 ‰) as well as Sr/ Sr throughout Phanerozoic time. Geology, 10: 516-519. 
progressively higher values (up to 20-21 ‰) interpreted as Claypool, G.E., Holser, W.T., Kaplan, I.R., Sakai, H. and Zak, I.
derived from several stages of recycling of the Triassic sul- (1980): The age curves of sulfur and oxygen isotopes in
fates in the Baza basin (Gibert et al., 2007). Other Neogene marine sulfate and their mutual interpretation. Chemical Geol-
evaporites show increasing δ34S values from the base (20- ogy, 28: 199-260.
22 ‰) to the top (near 16-17 ‰) indicating a change in the Cortecci, G., Reyes, E., Berti, G. and Casati, P. (1981): Sulfur and
mother brines from initially marine (as demonstrated by oxygen isotopes in Italian marine sulfates of Permian and Tri-assic ages. Chemical Geology, 34: 65-79.
other geochemical indicators also) to isotopically depleted,
non-marine waters, in which dissolved sulfate probably Fanlo, I. and Ayora, C. (1998): The evolution of the Lorraineevaporite basin: Implications for the chemical and isotope
comes from the recycling of Triassic evaporites to the top. compositions of the Triassic ocean. Chemical Geology, 146:
In this group, the evaporite units of the Granada basin (Gar- 135-154.
cía-Veigas et al., 2013) and some of the evaporite units of Flügel E., Flügel-Kahler E., Martin, J.M. and Martín-Algarra, A.
the Lorca and Fortuna basins (Playà et al., 2000) are (1984): Middle Triassic reefs from Southern Spain. Facies, 11:
included. Other Neogene evaporites show intermediate 173-218.
δ34S values (14-19 ‰) suggesting continuous mixing of García-Veigas, J., Cendón, D.I., Rosell, L., Ortí, F., Torres Ruiz,
marine and meteoric water, as in the Las Minas-Camaril- J., Martín, J.M. and Sanz, E. (2013): Salt deposition and brine
las basin (Hellín Gypsum unit; Moragas et al., 2011). evolution in the Granada Basin (Late Tortonian, SE Spain).
Palaeogeography, Palaeoclimatology and Palaeoecology,
Conclusions 369: 452-465.
Gibert, L., Ortí, F. and Rosell, L. (2007): Plio-Pleistocene lacus-
1) The isotope values of Triassic sulfates of the Betic trine evaporites of the Baza Basin (Betic Chain, SE Spain).
Cordillera obtained in the present study range between 12.5 Sedimentary Geology, 200: 89-116.
and 16.6 ‰ for δ34S, between 8.9 and 16.9 ‰ for δ18O, and Gómez, J.J. and Goy, A. (1998): Las unidades litoestratigráficas
between 0.707615 and 0.708114 for 87Sr/86Sr. These val- del tránsito Triásico-Jurásico en la región de Lécera (Zara-
ues confirm the marine origin of the Triassic evaporite goza). Geogaceta, 23: 63-66. 
formations in this geological domain. Gómez-Alday, J.J., Castaño, S. and Sanz, D. (2004): Origen geo-
2) Significant isotopic differences were not observed lógico de los contaminantes (sulfatos) presentes en las aguas
between sulfates from the External Zones and the Internal subterráneas de la Laguna de Petróla (Albacete, España).
Zones, although the number of samples studied in the Inter- Resultados preliminares. Geogaceta, 35: 167-170.
nal Zones was much lower than in the External Zones. Holland, H.D. (1984): The Chemical Evolution of the Atmospheres
3) The isotopic data of the Triassic sulfates can con- and Ocean. Princeton University, Princeton N.J., 583 p. 
tribute to a better understanding of the origin, either marine Iribar, V. and Ábalos, B. (2011): The geochemical and isotopic
or recycled from older formations, of the Neogene evapor- record of evaporite recycling in spas and salterns of the BasqueCantabrian basin, Spain. Applied Geochemistry, 26: 1315-
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