O presente trabalho tem como objectivo realizar uma
síntese da evolução paleogeográfica do Parque Nacional de Doñana,
através de uma compilação da informação previamente publicada
sobre o assunto, incluindo a descrição geral das variações climáticas
tardi-holocénicas na Península Ibérica. Dados sedimentológicos e de
microfauna de dois cores e o registo histórico de eventos energéticos
extremos em Portugal e Espanha são igualmente combinados e
discutidos no que diz respeito ao reconhecimento dos intervalos
climáticos e eventos tsunamigénicos. Os resultados mostram que a
evolução paleogeográfica do Parque Nacional de Doñana parece
certamente ligada às mudanças climáticas e à ocorrência de eventos
energéticos extremos como observado para o tsunami de 2168-2159
B.P., durante o período Sub-Atlântico

Abad, Manuel

Guerra, Liliana

Ruiz, F.

Veiga-Pires, C.

Sapientia

   Versão online: http://www.lneg.pt/iedt/unidades/16/paginas/26/30/185  Comunicações Geológicas (2014) 101, Especial III, 1461-1465 IX CNG/2º CoGePLiP, Porto 2014  ISSN: 0873-948X; e-ISSN: 1647-581X A synthesis of Doñana National Park (Spain) Late Holocene history: palaeoenvironmental evolution, climate influence, high energy events and foraminifera records  Síntese da história da Evolução Holocénica do Parque Nacional de Doñana (Espanha): evolução paleoambiental, influência climática, eventos energéticos extremos e registro de foraminíferos  L. Guerra1, C. Veiga-Pires1, F. Ruiz2, M. Abad3    © 2014 LNEG – Laboratório Nacional de Geologia e Energia IP   Abstract: The present work aims to make a synthesis of the palaeogeographical evolution of Doñana National Park, through a compilation of previously published information on this subject including the general description of Late Holocene Climatic Change in the Iberian Peninsula. Sedimentological and microfaunal data from two cores and historical records of high-energy events in Portugal and Spain are also combined and discussed in relation to the recognition of climatic intervals and tsunami events. Results show that the palaeogeographical evolution of Doñana National Park seems indeed mostly linked to Climatic Changes and occurrence of high energy events as observed for the tsunami of 2168-2159 B.P., during the Sub-Atlantic period. Keywords: Holocene, Foraminifera, Palaeogeographical Evolution, Doñana National Park, Southwestern Spain.  Resumo: O presente trabalho tem como objectivo realizar uma síntese da evolução paleogeográfica do Parque Nacional de Doñana, através de uma compilação da informação previamente publicada sobre o assunto, incluindo a descrição geral das variações climáticas tardi-holocénicas na Península Ibérica. Dados sedimentológicos e de microfauna de dois cores e o registo histórico de eventos energéticos extremos em Portugal e Espanha são igualmente combinados e discutidos no que diz respeito ao reconhecimento dos intervalos climáticos e eventos tsunamigénicos. Os resultados mostram que a evolução paleogeográfica do Parque Nacional de Doñana parece certamente ligada às mudanças climáticas e à ocorrência de eventos energéticos extremos como observado para o tsunami de 2168-2159 B.P., durante o período Sub-Atlântico. Palavras-chave: Holocénico, Foraminíferos, Evolução paleogeográfica, Parque Nacional de Doñana, Sudoeste de Espanha.      1CIMA-FCT, Universidade do Algarve, Campus de Gambelas, 8005-139 Faro, Portugal. 2Departamento de Geodinámica y Paleontología, Univ. de Huelva, Avda. Fuerzas Armadas, s/n. 21071-Huelva, Spain. 3Departamento de Geología, Univ. de Atacama, Avda. Copayapu 485, Copiapó-Chile. *Corresponding author / Autor correspondente: a40955@ualg.pt   1. Introduction Doñana National Park (DNP) is one of the largest wetlands (~500 km2) in Europe, located in southwestern Spain (Fig. 1). The Park is mainly composed of salt and freshwater marshes that include temporary ponds. These marshes are drained by several tributaries and numerous ebb tide channels, with recent and ancient banks defined by clayey levees, bioclastic and beach-like sandy ridges (Fig. 1b: Las Nuevas).  In addition, these marginal formations are locally covered by sandy ridges aligned in an NE-SW orientation nearby to the Doñana spit barrier (Fig. 1b: Vetalengua). These inner zones are protected by two littoral spit-barrier systems (Doñana and La Algaida) composed of active dunes assembled in narrow and elongated sandy strips (Rodríguez-Vidal et al., 2011). Guadalquivir fluvial regime, tidal inputs, the dominant southwesterly wave action and the southeasterly drift currents are controlling the main hydrodynamic processes within the present.  At least sixteen tsunamis have been documented for the time-period between 2168-2159 B.P. (218 BC and 1900 AD) (Campos, 1991). These high-energy events had tremendous morphological effects and drastic ecological impacts in coastal areas (Borrero, 2005) and caused the deposition of sedimentary beds with characteristic textural and mineralogical features (e.g., Babu et al., 2007) (Fig. 1b and c: Cheniers). The present work aims to present a bibliographic revision of the DNP palaeogeographical evolution during the Late Holocene and to compile and integrate it with other information such as Climatic Changes as well as sedimentary and new micropaleontological data from two cores. 2. Methods A bibliographic revision was carried on in order to integrate several type of information: i) DNP paleogeographical evolution, ii) Late-Holocene Climatic phases, and iii) Artigo Curto Short Article 1462  L. Guerra et al. / Comunicações Geológicas (2014) 101, Especial III, 1461-1465  Occurrence of Tsunami events. This synthesis also aims to redraw maps of the palaeogeographical evolution of DNP (Fig. 2), based on Rodríguez-Ramírez (2008), using ArcGIS software, as well as the positioning of the sampled cores.  On the other hand, Las Nuevas area (Fig. 1b) was selected for collecting two cores, once it contains the main geomorphological features of the estuary (Fig. 1b, see Ruiz et al., 2004 for more details on sampling). Approximately 62 samples (15 g) were taken for microfossil analysis, as they were selected according to the main sedimentary changes observed in the core. These samples were washed through a 63 μm sieve to remove the mud fraction and then dried. If possible, more than 300 benthic foraminifera from each sample were picked and identified onto faunal microscope slides. The number of planktonic foraminifera in each sample was also taken into account, for latter calculation of the ratio planktonic/benthic foraminifera (individuals/gram) (Fig. 3).  Fig. 1. a) Location of Doñana National Park in the Iberian Peninsula, b) Doñana National Park main geomorphology and core sampling sites, c) Topographic profile between sampled cores C-D.  Fig. 1. a) Localização do Parque Nacional de Doñana na Península Ibérica, b) Geomorfologia geral do Parque Nacional de Doñana e locais de amostragem dos cores, c)Perfil topográfico entre os cores C-D. 3. Results and discussion 3.1. Climate and palaeoenvironmental evolution of Doñana National Park The palaeogeographical evolution of DNP has already been described by many authors, like Ruiz et al., 2010, who included numerous data obtained by Lario (1996) and Zazo et al. (1999) in several cores from DNP; as well as previous analyses of short cores by Ruiz et al. (2004). The palaeogeographical evolution of DNP presented here is further complemented with Late Holocene Climate Change phases over the Iberian Peninsula (Schütt, 2005) since the “Atlantic period” to the “SubAtlantic period to present”, and the historical records of high-energy events in Portugal and southern Spain (Galbis, 1932; Campos, 1991). Atlantic period  During the Atlantic period (8000 B.P. to 6000-5000 B.P.) the Iberian Peninsula was under the influence of the subtropical high-pressure belt in the summer months, whereas the impacts of the west wind drift shift to higher latitudes (Lamb, 1971). This period corresponds to phases 4 and 5 described by Ruiz et al. (2010) during which the Cádiz Gulf-river mouths were inundated around 6.5 cal ka (Dabrio et al., 2000) and DNP was occupied by an open lagoon, partially protected in its westernmost part by aeolian units (Zazo et al., 2008) (Fig. 2a). After this maximum transgression, the Doñana spit began to grow (Goy et al., 1996). The bottom sediments of the adjacent, quiet lagoon were composed of clayey silt (FA-3, Fig. 3) with variable bioclastic contents. Between 5100 and 4800 cal BP, there is a tsunami record causing the erosion of this spit and the deposition of aeolian sand over the new salt marsh (Fig. 2b) (Ruiz et al., 2010).  Sub Boreal period  After the end of the “postglacial climate optimum” and slight global cooling, there was a temporary southward shift of the northern hemispheric high west wind drift during the Sub-Boreal period (5000–3000 B.P.). As a result of the increasing meridional temperature gradient the circulation gained a stronger zonal component (Lamb, 1971). The west wind weather conditions now prevailing over the Iberian Peninsula between autumn and spring brought rain to all parts of it, improving the water balance. Phases 6 and 7 of Ruiz et al., 2010 are included in this period, during which the central part of the DNP was still occupied by an open lagoon, whereas the Doñana spit grew towards the southeast (Fig. 2b and 2c). There is record of one or two tsunami-like events (or very strong storms) that caused the erosion of the Doñana spit (3700-3000 B.P.; Fig. 2b) and the deposition of bioclastic, sandy-clayey silt over the lagoon bottom. In a latter period, new high-energy events induced the emersion of the very shallow, southwestern areas of the lagoon, with the deposits of bioclastic silt and sand (FA-5, Fig. 3) overlying intertidal sediments.  Sub Atlantic period  During the Sub-Atlantic period (3000-1500 B.P.), climate involved towards global warming (Dansgaard et al., 1969) and generally wetter conditions in central Europe. During this phase the Iberian Peninsula remained under the influence of Atlantic-cyclonic conditions (Lamb, 1971). However, generally higher temperatures resulted in deteriorating water balance conditions and an Iberian continental semi-arid climate prevailed in central Iberia. Then global cooling brought a temporary rise in humidity over the Iberian Peninsula.     Doñana National Park (Spain) Late Holocene history 1463    Fig. 2. Palaeogeographical evolution maps adapted from Rodríguez-Ramírez (2008) and showing paleogeographical environments during a) the Atlantic Climatic period, b) the Sub-Boreal Climatic period and, c)-e) the Sub-Atlantic Climatic period until present.  Fig. 2. Mapas da evolução paleogeográfica adaptados de Rodríguez-Ramírez (2008) e mostrando os ambientes paleogeográficos durante a) o período climático Atlântico, b) o período climático Sub-Boreal, c)-e) o período climático Sub-Atlântico até ao presente.  Fig. 3. Synthetic sketch correlating the two cores facies and associated paleoenvironment descriptions (Ruiz et al., 2004), with the Climatic Periods (Schütt, 2005) and the Foraminiferal ratio (this study).  Fig. 3. Esquema sintético correlacionando facies de dois cores e descrições paleoambientais associadas (Ruiz et al., 2004), com os períodos climáticos (Schütt, 2005) e ratio de foraminíferos (presente estudo).  1464  L. Guerra et al. / Comunicações Geológicas (2014) 101, Especial III, 1461-1465   The Sub-Atlantic period includes phases 8 to 10 of Ruiz et al. (2010) palaeoreconstruction, during which the southwestern part of the DNP area remained emerged, between 3000-2200 B.P., whereas the central and southern ones were occupied by a very shallow lagoon (Fig. 2c). The continuous growing of the Doñana spit and the progressive infilling induced the creation of new brackish marshes (Zazo et al., 1999) and the transition from marine conditions to more restricted scenarios (Ruiz et al., 2010). During 2200-1900 B.P. several tsunamis eroded the Doñana spit (Fig. 2c) with the creation of small washover fans constituted by aeolian sediments and bioclastic accumulation ridges over the lagoon margins (Ruiz et al., 2010).  These tsunamis may be assimilated to the historical tsunamis that devastated the southwestern Iberian coasts between 2168-2159 B.P. and 2010 B.P. (218-209 BC and 60 BC) (Campos, 1991). From 1900 B.P. to present times, there was an increasing infilling of the lagoon (Fig. 2d). This tendency was interrupted by a new introduction of marine and aeolian sediments in the southern part of the park, owing to new high-energy events (Ruiz et al., 2010). Ages of these phenomena coincide with those of an historical tsunami (1568 B.P.=382 BC; Campos, 1991). The posterior palaeoenvironmental evolution of the DNP (Fig. 2e) is marked by the creation of new wetlands with temporary ponds and the growing of the Doñana and La Algaida spits, with aeolian sands covering intertidal sediments. 3.2. Sedimentary and micropaleontological data Figure 3 illustrates the relation between the facies of cores C and D (Fig. 1), the ratio of planktonic/benthic foraminifera (n/g) along each core and an interpretation of the Holocene Climate Change phases’ on the Iberian Peninsula. The Atlantic period (Fig. 2a) is not recorded in cores C and D. During the Sub Boreal period (Fig. 2b), the planktonic/benthic foraminifera ratio reaches its highest values of 2.16 (Fig. 3) in the lower 30 cm of core D, indicating a strong marine influence and agreeing with the description of a lagoon environment by Ruiz et al. (2004). This also goes in agreement with the description of the Sub Boreal climate (see previous section). During the Sub Atlantic period (Fig. 2c-e) the planktonic/benthic foraminifera ratio shows lower values in both cores C (from 90 cm to the top) and D (from ~130 cm to the top), with some non- significant variations, indicating a more restricted environment than the latest. These results go accordingly to the description of a shallow lagoon or saltmarsh environment made by Ruiz et al. (2004). Although the facies and carbon ages concur with the sedimentary signature of high energy events and the record of the historical tsunamis respectively, no evidence of these events is found in the planktonic/benthic ratio of the cores. 4. Conclusions Palaeogeographical evolution of Doñana NP seems mostly linked to Climatic Changes and the occurrence of high energy events. Although there is no record of the Atlantic period climate on the analyzed cores at the present work, the Sub Boreal and Sub Atlantic periods are well recorded (Fig. 2 and 3). Furthermore, although planktonic/benthic foraminifera ratios seem a reliable marine influence indicator, they do not provide information on tsunami or storm occurrence. The record of benthic foraminifera assemblages in the cores samples and at present surface samples may be an helpful assess to evidence this high-energy events. Acknowledgments This research was partially funded by Spanish–FEDER Projects CGL2012-30875, FCT Project (PTDC/CTE-GIX/110205/2009), CIMA strategic project PEst-OE/MAR/UI0350/2011, MAPFRE Foundation TSUNAONUBA Project and three Research Groups of the Andalusia Board (RNM-238, RNM-293, and RNM-349). References Babu, N., Suresh Babu, D.S., Mohan Das, P.N., 2007. Impact of tsunami on texture and mineralogy of a major placer deposit in southwest coast of India. Environmental Geology, 52, 71-80. Borrero, J.C., 2005. Field data and satellite imagery of tsunami effects in Banda Aceh. Science, 308, 1596. Campos, M.L., 1991. Tsunami hazard on the Spanish coasts of the Iberian Peninsula. Science of Tsunami Hazards, 9, 83-90. Dabrio, C.J., Zazo, C., Lario, J., Goy, J.L., Sierro, F.J., Borja, F., González, J.A., Flores, J.A., 2000. Depositional history of estuarine infill during the last postglacial transgression (Gulf of Cadiz, southern Spain). Marine Geology, 162, 381-404. Dansgaard, W., Johnsen S.J., Møller, J., 1969. One thousand Centuries of Climatic Record from Camp Century on the Greenland Ice Sheet. Science, 166, 377-381. Galbis, R.J., 1932. Catálogo sísmico de la zona comprendida entre los meridianos 58E y 208W de Greenwich y los paralelos 45º y 25º N. Dirección General del Instituto Geográfico, Catastral y de Estadística, Madrid. Goy, J.L., Zazo, C., Dabrio, C.J., Lario, J., Borja, F., Sierro, F.J., Flores, J.A., 1996. Global and regional factors controlling changes of coastlines in southern Iberia (Spain) during the Holocene. Quaternary Science Reviews, 15, 773-780. Lamb, H.H., 1971. Climates and Circulation Re-gimes Developed over the Northern Hemisphere during and since the Last Ice Age. Palaeogeography, Palaeoclimatology, Palaeoecology, 10, 125-162. Lario, J., 1996. Último y Presente Interglacial en el área de conexión Atlántico- Mediterráneo: variaciones del nivel del mar, paleoclima y paleoambientes. PhD Thesis, Universidad Complutense de Madrid (unpublished), 269 p. Rodríguez-Ramírez, 2008. Geomorfología del Parque Nacional de Doñana. Geología de Huelva: lugares de interés geológico. Universidad de Huelva, 146-151. Rodríguez-Vidal, J., Ruiz, F., Cáceres, M.A., González-Regalado, M.L., Pozo, M., Carretero, M.I., Soares, A.M., Gómez Toscano, F., 2011. Geomarkers of the 218-209 BC Atlantic tsunami in the Roman Lacus Ligustinus (SW Spain): A palaeogeographical approach. Quaternary International, 242, 201-212. Doñana National Park (Spain) Late Holocene history 1465  Ruiz, F., Pozo, M.,Carretero, M.I., Abad, M., González-Regalado, M.L., Muñoz, J.M. , Rodríguez-Vidal, J., Cáceres, L.M., Pendón, J.G., Prudêncio, M.I., Dias, M.I., 2010. Birth, evolution and death of a lagoon: Late Pleistocene to Holocene palaeoenvironmental reconstruction of the Doñana National Park (SW Spain). Lagoons: Biology, Management and Environmental Impact, 1-26. Ruiz, F., Rodríguez-Ramírez, A., Cáceres, L.M., Rodríguez Vidal, J., Carretero, M.I., Clemente, L., Muñoz, J.M., Yañez, C., Abad, M., 2004. Late Holocene evolution of the southwestern Doñana Nacional Park (Guadalquivir Estuary, SW Spain): a multivariate approach. Palaeogeography, Palaeoclimatology, Palaeoecology, 204, 47-64. Schütt, B., 2005. Late Quaternary Environmental Change on the Iberian Peninsula. Die Erde, 136, 3-14. Zazo, C., Dabrio, C.J., Goy, J.L., Lario, J., Cabero, A., Silva, P.G., Bardají, T., Mercier, N., Borja, F., Roquero, E., 2008. The coastal archives of the last 15 ka in the Atlantic-Mediterranean Spanish linkage area: Sea level and climate changes. Quaternary International, 181, 72-87. Zazo, C., Dabrio, C.J., González, A., Sierro, F.J., Yll, E.I., Goy, J.L., Luque, L., Pantaleón-Cano, J., Soler, V., Roure, J.M., Hoyos, M., Borja, F., 1999. The record of the later glacial and interglacial periods in the Guadalquivir marshlands (Mari López drilling, S. W. Spain). Geogaceta, 26, 119-122.  

Síntese da história da Evolução Holocénica do Parque Nacional de Doñana (Espanha): evolução paleoambiental, influência climática, eventos energéticos extremos e registro de foraminíferos

Universidade do Algarve

 
 
 
Versão online: http://www.lneg.pt/iedt/unidades/16/paginas/26/30/185  Comunicações Geológicas (2014) 101, Especial III, 1461-1465 
IX CNG/2º CoGePLiP, Porto 2014  ISSN: 0873-948X; e-ISSN: 1647-581X 
A synthesis of Doñana National Park (Spain) Late Holocene 
history: palaeoenvironmental evolution, climate influence, high 
energy events and foraminifera records 
 
Síntese da história da Evolução Holocénica do Parque Nacional 
de Doñana (Espanha): evolução paleoambiental, influência 
climática, eventos energéticos extremos e registro de 
foraminíferos 
 
L. Guerra1, C. Veiga-Pires1, F. Ruiz2, M. Abad3 
 
  
© 2014 LNEG – Laboratório Nacional de Geologia e Energia IP  
 
Abstract: The present work aims to make a synthesis of the 
palaeogeographical evolution of Doñana National Park, through a 
compilation of previously published information on this subject 
including the general description of Late Holocene Climatic Change 
in the Iberian Peninsula. Sedimentological and microfaunal data from 
two cores and historical records of high-energy events in Portugal 
and Spain are also combined and discussed in relation to the 
recognition of climatic intervals and tsunami events. Results show 
that the palaeogeographical evolution of Doñana National Park 
seems indeed mostly linked to Climatic Changes and occurrence of 
high energy events as observed for the tsunami of 2168-2159 B.P., 
during the Sub-Atlantic period. 
Keywords: Holocene, Foraminifera, Palaeogeographical Evolution, 
Doñana National Park, Southwestern Spain. 
 
Resumo: O presente trabalho tem como objectivo realizar uma 
síntese da evolução paleogeográfica do Parque Nacional de Doñana, 
através de uma compilação da informação previamente publicada 
sobre o assunto, incluindo a descrição geral das variações climáticas 
tardi-holocénicas na Península Ibérica. Dados sedimentológicos e de 
microfauna de dois cores e o registo histórico de eventos energéticos 
extremos em Portugal e Espanha são igualmente combinados e 
discutidos no que diz respeito ao reconhecimento dos intervalos 
climáticos e eventos tsunamigénicos. Os resultados mostram que a 
evolução paleogeográfica do Parque Nacional de Doñana parece 
certamente ligada às mudanças climáticas e à ocorrência de eventos 
energéticos extremos como observado para o tsunami de 2168-2159 
B.P., durante o período Sub-Atlântico. 
Palavras-chave: Holocénico, Foraminíferos, Evolução 
paleogeográfica, Parque Nacional de Doñana, Sudoeste de Espanha. 
 
 
 
 
 
1CIMA-FCT, Universidade do Algarve, Campus de Gambelas, 8005-139 Faro, 
Portugal. 
2Departamento de Geodinámica y Paleontología, Univ. de Huelva, Avda. 
Fuerzas Armadas, s/n. 21071-Huelva, Spain. 
3Departamento de Geología, Univ. de Atacama, Avda. Copayapu 485, 
Copiapó-Chile. 
*Corresponding author / Autor correspondente: a40955@ualg.pt  
 
1. Introduction 
Doñana National Park (DNP) is one of the largest wetlands 
(~500 km2) in Europe, located in southwestern Spain (Fig. 1). 
The Park is mainly composed of salt and freshwater marshes 
that include temporary ponds. These marshes are drained by 
several tributaries and numerous ebb tide channels, with 
recent and ancient banks defined by clayey levees, bioclastic 
and beach-like sandy ridges (Fig. 1b: Las Nuevas).  In 
addition, these marginal formations are locally covered by 
sandy ridges aligned in an NE-SW orientation nearby to the 
Doñana spit barrier (Fig. 1b: Vetalengua). These inner zones 
are protected by two littoral spit-barrier systems (Doñana and 
La Algaida) composed of active dunes assembled in narrow 
and elongated sandy strips (Rodríguez-Vidal et al., 2011). 
Guadalquivir fluvial regime, tidal inputs, the dominant 
southwesterly wave action and the southeasterly drift currents 
are controlling the main hydrodynamic processes within the 
present.  
At least sixteen tsunamis have been documented for the 
time-period between 2168-2159 B.P. (218 BC and 1900 AD) 
(Campos, 1991). These high-energy events had tremendous 
morphological effects and drastic ecological impacts in 
coastal areas (Borrero, 2005) and caused the deposition of 
sedimentary beds with characteristic textural and 
mineralogical features (e.g., Babu et al., 2007) (Fig. 1b and c: 
Cheniers). 
The present work aims to present a bibliographic revision 
of the DNP palaeogeographical evolution during the Late 
Holocene and to compile and integrate it with other 
information such as Climatic Changes as well as sedimentary 
and new micropaleontological data from two cores. 
2. Methods 
A bibliographic revision was carried on in order to integrate 
several type of information: i) DNP paleogeographical 
evolution, ii) Late-Holocene Climatic phases, and iii) 
Artigo Curto 
Short Article 
1462  L. Guerra et al. / Comunicações Geológicas (2014) 101, Especial III, 1461-1465 
 
Occurrence of Tsunami events. This synthesis also aims to 
redraw maps of the palaeogeographical evolution of DNP 
(Fig. 2), based on Rodríguez-Ramírez (2008), using ArcGIS 
software, as well as the positioning of the sampled cores.  
On the other hand, Las Nuevas area (Fig. 1b) was selected 
for collecting two cores, once it contains the main 
geomorphological features of the estuary (Fig. 1b, see Ruiz et 
al., 2004 for more details on sampling). Approximately 62 
samples (15 g) were taken for microfossil analysis, as they 
were selected according to the main sedimentary changes 
observed in the core. These samples were washed through a 
63 μm sieve to remove the mud fraction and then dried. 
If possible, more than 300 benthic foraminifera from each 
sample were picked and identified onto faunal microscope 
slides. The number of planktonic foraminifera in each sample 
was also taken into account, for latter calculation of the ratio 
planktonic/benthic foraminifera (individuals/gram) (Fig. 3). 
 
Fig. 1. a) Location of Doñana National Park in the Iberian Peninsula, b) 
Doñana National Park main geomorphology and core sampling sites, c) 
Topographic profile between sampled cores C-D. 
 
Fig. 1. a) Localização do Parque Nacional de Doñana na Península 
Ibérica, b) Geomorfologia geral do Parque Nacional de Doñana e locais 
de amostragem dos cores, c)Perfil topográfico entre os cores C-D. 
3. Results and discussion 
3.1. Climate and palaeoenvironmental evolution of 
Doñana National Park 
The palaeogeographical evolution of DNP has already been 
described by many authors, like Ruiz et al., 2010, who 
included numerous data obtained by Lario (1996) and Zazo 
et al. (1999) in several cores from DNP; as well as previous 
analyses of short cores by Ruiz et al. (2004). 
The palaeogeographical evolution of DNP presented 
here is further complemented with Late Holocene Climate 
Change phases over the Iberian Peninsula (Schütt, 2005) 
since the “Atlantic period” to the “SubAtlantic period to 
present”, and the historical records of high-energy events in 
Portugal and southern Spain (Galbis, 1932; Campos, 1991). 
Atlantic period 
 
During the Atlantic period (8000 B.P. to 6000-5000 B.P.) 
the Iberian Peninsula was under the influence of the 
subtropical high-pressure belt in the summer months, 
whereas the impacts of the west wind drift shift to higher 
latitudes (Lamb, 1971). This period corresponds to phases 4 
and 5 described by Ruiz et al. (2010) during which the 
Cádiz Gulf-river mouths were inundated around 6.5 cal ka 
(Dabrio et al., 2000) and DNP was occupied by an open 
lagoon, partially protected in its westernmost part by aeolian 
units (Zazo et al., 2008) (Fig. 2a). 
After this maximum transgression, the Doñana spit 
began to grow (Goy et al., 1996). The bottom sediments of 
the adjacent, quiet lagoon were composed of clayey silt 
(FA-3, Fig. 3) with variable bioclastic contents. Between 
5100 and 4800 cal BP, there is a tsunami record causing the 
erosion of this spit and the deposition of aeolian sand over 
the new salt marsh (Fig. 2b) (Ruiz et al., 2010). 
 
Sub Boreal period 
 
After the end of the “postglacial climate optimum” and 
slight global cooling, there was a temporary southward shift 
of the northern hemispheric high west wind drift during the 
Sub-Boreal period (5000–3000 B.P.). As a result of the 
increasing meridional temperature gradient the circulation 
gained a stronger zonal component (Lamb, 1971). The west 
wind weather conditions now prevailing over the Iberian 
Peninsula between autumn and spring brought rain to all 
parts of it, improving the water balance. 
Phases 6 and 7 of Ruiz et al., 2010 are included in this 
period, during which the central part of the DNP was still 
occupied by an open lagoon, whereas the Doñana spit grew 
towards the southeast (Fig. 2b and 2c). There is record of 
one or two tsunami-like events (or very strong storms) that 
caused the erosion of the Doñana spit (3700-3000 B.P.; Fig. 
2b) and the deposition of bioclastic, sandy-clayey silt over 
the lagoon bottom. In a latter period, new high-energy 
events induced the emersion of the very shallow, 
southwestern areas of the lagoon, with the deposits of 
bioclastic silt and sand (FA-5, Fig. 3) overlying intertidal 
sediments. 
 
Sub Atlantic period 
 
During the Sub-Atlantic period (3000-1500 B.P.), climate 
involved towards global warming (Dansgaard et al., 1969) 
and generally wetter conditions in central Europe. During 
this phase the Iberian Peninsula remained under the 
influence of Atlantic-cyclonic conditions (Lamb, 1971). 
However, generally higher temperatures resulted in 
deteriorating water balance conditions and an Iberian 
continental semi-arid climate prevailed in central Iberia. 
Then global cooling brought a temporary rise in 
humidity over the Iberian Peninsula. 
 
 
 
 
Doñana National Park (Spain) Late Holocene history 1463 
 
 
 
Fig. 2. Palaeogeographical evolution maps adapted from Rodríguez-Ramírez (2008) and showing paleogeographical environments during a) the 
Atlantic Climatic period, b) the Sub-Boreal Climatic period and, c)-e) the Sub-Atlantic Climatic period until present. 
 
Fig. 2. Mapas da evolução paleogeográfica adaptados de Rodríguez-Ramírez (2008) e mostrando os ambientes paleogeográficos durante a) o período 
climático Atlântico, b) o período climático Sub-Boreal, c)-e) o período climático Sub-Atlântico até ao presente. 
 
Fig. 3. Synthetic sketch correlating the two cores facies and associated paleoenvironment descriptions (Ruiz et al., 2004), with the Climatic Periods 
(Schütt, 2005) and the Foraminiferal ratio (this study). 
 
Fig. 3. Esquema sintético correlacionando facies de dois cores e descrições paleoambientais associadas (Ruiz et al., 2004), com os períodos 
climáticos (Schütt, 2005) e ratio de foraminíferos (presente estudo). 
 
1464  L. Guerra et al. / Comunicações Geológicas (2014) 101, Especial III, 1461-1465 
 
 
The Sub-Atlantic period includes phases 8 to 10 of 
Ruiz et al. (2010) palaeoreconstruction, during which the 
southwestern part of the DNP area remained emerged, 
between 3000-2200 B.P., whereas the central and southern 
ones were occupied by a very shallow lagoon (Fig. 2c). 
The continuous growing of the Doñana spit and the 
progressive infilling induced the creation of new brackish 
marshes (Zazo et al., 1999) and the transition from marine 
conditions to more restricted scenarios (Ruiz et al., 2010). 
During 2200-1900 B.P. several tsunamis eroded the 
Doñana spit (Fig. 2c) with the creation of small washover 
fans constituted by aeolian sediments and bioclastic 
accumulation ridges over the lagoon margins (Ruiz et al., 
2010).  
These tsunamis may be assimilated to the historical 
tsunamis that devastated the southwestern Iberian coasts 
between 2168-2159 B.P. and 2010 B.P. (218-209 BC and 
60 BC) (Campos, 1991). 
From 1900 B.P. to present times, there was an 
increasing infilling of the lagoon (Fig. 2d). This tendency 
was interrupted by a new introduction of marine and 
aeolian sediments in the southern part of the park, owing 
to new high-energy events (Ruiz et al., 2010). Ages of 
these phenomena coincide with those of an historical 
tsunami (1568 B.P.=382 BC; Campos, 1991). The 
posterior palaeoenvironmental evolution of the DNP (Fig. 
2e) is marked by the creation of new wetlands with 
temporary ponds and the growing of the Doñana and La 
Algaida spits, with aeolian sands covering intertidal 
sediments. 
3.2. Sedimentary and micropaleontological data 
Figure 3 illustrates the relation between the facies of cores C 
and D (Fig. 1), the ratio of planktonic/benthic foraminifera 
(n/g) along each core and an interpretation of the Holocene 
Climate Change phases’ on the Iberian Peninsula. 
The Atlantic period (Fig. 2a) is not recorded in cores C 
and D. During the Sub Boreal period (Fig. 2b), the 
planktonic/benthic foraminifera ratio reaches its highest 
values of 2.16 (Fig. 3) in the lower 30 cm of core D, 
indicating a strong marine influence and agreeing with the 
description of a lagoon environment by Ruiz et al. (2004). 
This also goes in agreement with the description of the Sub 
Boreal climate (see previous section). 
During the Sub Atlantic period (Fig. 2c-e) the 
planktonic/benthic foraminifera ratio shows lower values in 
both cores C (from 90 cm to the top) and D (from ~130 cm 
to the top), with some non- significant variations, indicating 
a more restricted environment than the latest. These results 
go accordingly to the description of a shallow lagoon or 
saltmarsh environment made by Ruiz et al. (2004). 
Although the facies and carbon ages concur with the 
sedimentary signature of high energy events and the record 
of the historical tsunamis respectively, no evidence of these 
events is found in the planktonic/benthic ratio of the cores. 
4. Conclusions 
Palaeogeographical evolution of Doñana NP seems mostly 
linked to Climatic Changes and the occurrence of high 
energy events. Although there is no record of the Atlantic 
period climate on the analyzed cores at the present work, the 
Sub Boreal and Sub Atlantic periods are well recorded (Fig. 
2 and 3). Furthermore, although planktonic/benthic 
foraminifera ratios seem a reliable marine influence 
indicator, they do not provide information on tsunami or 
storm occurrence. The record of benthic foraminifera 
assemblages in the cores samples and at present surface 
samples may be an helpful assess to evidence this high-
energy events. 
Acknowledgments 
This research was partially funded by Spanish–FEDER 
Projects CGL2012-30875, FCT Project (PTDC/CTE-
GIX/110205/2009), CIMA strategic project PEst-
OE/MAR/UI0350/2011, MAPFRE Foundation 
TSUNAONUBA Project and three Research Groups of the 
Andalusia Board (RNM-238, RNM-293, and RNM-349). 
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Síntese da história da Evolução Holocénica do Parque Nacional de Doñana (Espanha): evolução paleoambiental, influência climática, eventos energéticos extremos e registro de foraminíferos

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