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19Coastal Dunes and Marshes in DonanaNational Park

Joaquın Rodrıguez-Vidal, Teresa Bardajı, Cari Zazo, Jose L. Goy, FranciscoBorja, Cristino J. Dabrio, Javier Lario, Luis M. Caceres, Francisco Ruiz, andManuel Abad

Abstract

Doñana Natural Park is a good global example of the sedimentary filling of a broad tidalestuary during the Mid-Late Holocene, after the last postglacial sea-level rise. The timing ofthis rise is not well defined yet in the Gulf of Cádiz, since the oldest evidence of coastalsedimentation, located at the right bank of the mouth of the old Guadalquivir Estuary, datesback to ca. 5,000 years ago. The first evolutionary stages of the embayment indicate anobvious marine influence, dominated by waves and storms from the SW. Since ca.4,000 years ago, protection provided by the growing coastal spit barrier of Doñana favoredthe development of a sheltered marsh dominated by tides and fluvial currents. About2,200 years ago, since the time Romans controlled the area, the estuary was dominated bymarshlands with a wide lagoon at its mouth (Lacus Ligustinus), and the current landscape ofDoñana started to form. The evolution of the last 2,000 years includes the quick andcontinuous growth of coastal barriers by longshore drift, the origin of the present-daymarshland landscape and the development of dune fields migrating inland towards thewetlands.

Keywords

Coastal dunes � Spit bar � Marshland � Holocene � Guadalquivir Basin

J. L. GoyDepartamento de Geología, Universidad de Salamanca, 37008,Salamanca, Spaine-mail: [email protected]

F. BorjaÁrea de Geografía Física, Universidad de Huelva, 21007, Huelva,Spaine-mail: [email protected]

C. J. DabrioDepartamento de Estratigrafía, Universidad Complutense, 28040,Madrid, Spaine-mail: [email protected]

J. LarioDepartamento de Ciencias Analíticas, UNED, 28040, Madrid,Spaine-mail: [email protected]

J. Rodríguez-Vidal (&) � L. M. Cáceres � F. Ruiz � M. AbadDepartamento de Geodinámica y Paleontología, Universidad deHuelva, 21071, Huelva, Spaine-mail: [email protected]

L. M. Cácerese-mail: [email protected]

F. Ruize-mail: [email protected]

M. Abade-mail: [email protected]

T. BardajíUnidad Docente de Geología, Universidad de Alcalá, 28871,Alcalá de Henares, Spaine-mail: [email protected]

C. ZazoDepartamento de Geología, Museo Nacional de CienciasNaturales (CSIC), 28006, Madrid, Spaine-mail: [email protected]

F. Gutiérrez and M. Gutiérrez (eds.), Landscapes and Landforms of Spain, World Geomorphological Landscapes,DOI: 10.1007/978-94-017-8628-7_19, � Springer Science+Business Media Dordrecht 2014

229

19.1 Introduction

Doñana Natural and National Parks constitute one of themost outstanding natural protected areas in the IberianPeninsula, as well as one of the widest lowlands. Wetlands,marshlands and dune fields cover around 1,100 km2 withinHuelva, Seville and Cádiz provinces in Andalucía. TheDoñana National Park covers more than 54,720 ha, and itsbuffer protection area, which constitutes the Natural Park,around 54,250 ha. The natural values of this privilegedlandscape have not been ignored by national or internationalbodies. It was declared Nature Reserve by the WWF in1963, National Park in 1969, Biosphere Reserve by theUNESCO in 1980, and UNESCO World Heritage Site in1994.

The present-day Doñana landscape is a clear outcome ofthe geological evolution since Late Miocene times(Fig. 19.1), and mainly since the Last Glacial Maximum(LGM). The postglacial sea-level rise, which reached itsmaximum at ca. 6,500 years BP, caused the drowning of thelower Guadalquivir River valley. Since then, littoraldynamics has largely controlled the development of thepresent landscape. The growth of littoral spit bar systems atthe mouth of the Guadalquivir Estuary induced the creationof protected marshland areas and the formation of dunesystems on top of them. Detailed analyses of spit bars, dunesystems and marshlands allow the reconstruction of thegeomorphological evolution of this particular landscape insouth-western Iberian Peninsula.

19.2 Geographical and Geological Setting

Doñana National Park is located in the SW littoral zone ofthe Iberian Peninsula, including the lowermost reach of theGuadalquivir River. The high biodiversity found in differentecosystems make this landscape an exceptional naturalenvironment.

The present-day climatic conditions, and particularly thestrong local winds, play an instrumental role in the mor-phogenetic processes. Climate can be defined as Mediter-ranean with Atlantic influence, with a mean annual rainfallbelow 600 mm (two maxima in late autumn and spring) andan average annual temperature of around 18 �C (summermaximum can reach 35–40 �C). Prevailing winds blowfrom the SW. Winds from the SE and E are less commonbut also important since they are commonly associated withstorm events (Rodríguez-Ramírez 1998).

Regarding the geology, Doñana is located at the seawardedge of the Guadalquivir Cenozoic Basin (Fig. 19.1), whichconstitutes the foreland basin of the Betic Cordillera (Sanzde Galdeano and Vera 1992). The northern passive margin

of this basin corresponds to the Variscan Massif, againstwhich the collisional Alpine orogenic belt of the BeticCordillera develops (Fig. 19.1a).

The sedimentary marine fill of the basin has been datedon the basis of microfaunal assemblages (Sierro et al. 1996)as Late Miocene–Early Pliocene. The palaeogeographicreconstruction (Fig. 19.1b, c, and d) based on sedimentaryand palaeontological analyses shows a progressive shal-lowing of the basin, recorded by a stratigraphic successionranging from Late Miocene inner platform bioclasticsandstones to Pliocene wave- and tide-dominated deltadeposits. The Pleistocene evolution is characterized by aprogressive estuarine fill and major changes in the course ofthe main rivers (Gutiérrez-Elorza 2002).

The ca. 100–120 m sea-level drop during the LGMinduced the incision of wide valleys by the main rivers,which were subsequently flooded during the Holocene sea-level rise, becoming wide estuaries (Zazo et al. 1999;Dabrio et al. 2000). At present, most estuaries are silted upand spit bars and marshes have developed at the mouth ofthe main rivers (Fig. 19.2).

19.3 Geomorphology of Donana NationalPark

Doñana National Park exhibits a series of morphosedi-mentary units related to the progressive silting-up of theGuadalquivir Estuary after the maximum postglacial sea-level rise at ca. 6,500 cal year BP (Benavente et al. 2005).Initial vertical accretion in the estuaries changed after ca.2,700 cal year BP into growing progradational spit bars andassociated dune systems, resulting in the present-day mor-phology dominated by low-lying marshlands at the mouthof the main river valleys (Rodríguez-Ramírez et al. 2005).However, the understanding of this recent evolutionrequires a good knowledge of the Late Pleistocene historyof the lowest Guadalquivir Basin, which constitutes theinitial evolutionary stage of the geomorphological config-uration of Doñana.

19.3.1 El Abalario Dune Field

El Abalario area (Fig. 19.2) displays a NW–SE trendingelongated domal morphology that separates the lowerCenozoic Guadalquivir Basin from the Atlantic Ocean, andoutlines the headland of the spit bar system whose growthpromoted the progressive closure of the GuadalquivirEstuary.

This dome structure was caused by a progressive up-warping of underlying Pliocene–Pleistocene progradingdelta sediments, produced by the large NW–SE Torre del

230 J. Rodrıguez-Vidal et al.

Loro gravitational fault (Fig. 19.2) (Zazo et al. 2005a).Sedimentary units cropping out along the Asperillo cliff(Fig. 19.2) record the complex evolution of the area (Zazoet al. 2005a, 2008), controlled by the interaction of littoralprocesses and sea-level changes in an emergent coastalplain. Upwarping at the end of Marine Isotope Stage (MIS)-5 produced a WNW–ESE normal fault (Torre del LoroFault, Fig. 19.2), along which gravitational displacementcreated an upthrown block to the north and a downthrownblock to the south, generating a faulted sea-cliff. Threeaeolian units separated by widespread weathering surfacesand palaeosoils (U1 to U3 in Zazo et al. 1999, 2005a)accumulated in the downthrown block against the faultscarp, between the late MIS-5, under a falling sea-levelscenario, and the Last Deglaciation (chronology based onradiocarbon and OSL dating, Zazo et al. 2005a). The onsetof moist and temperate climate during the Holocene Cli-matic Optimum (9.0–6.5 cal ky BP) induced the develop-ment of a wide flat erosional surface with an iron-rich crust,at present partially destroyed. This surface is easily recog-nizable along the Asperillo cliff (Fig. 19.3) (Zazo et al.2005a, b, 2008). The development of at least four youngersemi-mobile and mobile dune systems on top of this surface(U4–U7, Zazo et al. 1999, 2005a) by W-SW winds has beeninterpreted as the result of a general aridity trend since ca.5 cal ky BP, also described in other localities from theSouthern Iberian Peninsula (Zazo et al. 1994; Santos et al.2003). The lithic workshop level (Late Neolithic–

Calcolithic; ca. 5,000 cal ky BP after Martín de la Cruzet al. 2000) found on top of this surface and coeval to thefirst aeolian unit (U4 in Zazo et al. 2005a) supports thischronology (Borja et al. 1999; Zazo et al. 2005b).

Radiocarbon dating on charcoal found with the U5aeolian unit indicates an age of ca. 2.7 cal ky BP for thisunit, coinciding with an arid period described in the regionand an increase in coastal progradation (Zazo et al. 1999;Goy et al. 2003). Archaeological remains associated withthis dune system allow one to infer that sedimentationcontinued until Roman and Medieval times. The morerecent aeolian unit U6 seems to be coeval with the 16th–17th centuries coastal watch-towers (Borja et al. 1999), andthe accumulation of the dunes corresponding to the youn-gest unit described in this area (U7 in Zazo et al. 2005a)began in the 17th century, but they are still active underwinds blowing from the SW.

19.3.2 The Donana Dune Systems

Although the dune systems reach the maximum develop-ment at El Abalario, the Doñana National Park includes thelargest active dune field in Europe. Five dune sequences(Fig. 19.4), that can be partially correlated with thosedescribed in El Abalario area, have been differentiated bymeans of geomorphological studies (Rodríguez-Vidal et al.1993; Rodríguez-Ramírez et al. 1996, 2005) (Fig. 19.4).

Fig. 19.1 a Location of the Doñana National Park within the BeticCordillera (modified from Azañón et al. 2002). Palaeogeography of the

area, b Late Tortonian, c Early Messinian, and d Early Pliocene(modified from Alonso-Zarza et al. 2002)

19 Coastal Dunes and Marshes in Donana National Park 231

Stabilized Dune SystemsThe first dune system described in the Doñana NationalPark (System I, after Rodríguez-Ramírez et al. 1996) coversthe previous topography and includes some scattered andscarcely developed parabolic dunes generated by WSWwinds. The correlation of this system with U2 dunes (afterZazo et al. 1999, 2005a) supports an age between 31 and18 ky BP.

System II is represented by extensive dunes, mainly withlong parabolic shapes that in some places grade into

transverse dunes with undulating crests (Rodríguez-Ramí-rez et al. 2005; Rodríguez-Ramírez 2011). These dunes areusually less than 100 m wide, with lengths that can reachseveral kilometres, and heights up to 80 m. Their formationis mainly related to westerly winds and their age has beenestimated for between 14 and 11.5 ky BP by correlationwith the U3 system of Zazo et al. (1999).

System III marks a change in prevailing wind directionthat turns again into WSW. Dunes show a parabolic shape,whose lateral coalescence results in an undulating

Fig. 19.2 Geomorphologicalmap of the Atlantic GuadalquivirBasin (after Zazo et al. 2005a)and location of Doñana NationalPark


transverse morphology. Their age, considered to be correl-ative to U4 dunes after Zazo et al. (1999), is constrained bythe ages of the immediately older (11 ky BP) and younger(5–4 ky BP) systems.

Active Dune SystemsTwo active dune systems (Systems IV and V, Fig. 19.4)overlapping the previous ones and migrating across theDoñana marshlands have been described (Rodríguez-Vidalet al. 1993; Rodríguez-Ramírez et al. 2005; Rodríguez-Ramírez 2011).

System IV comprises sparse and small parabolic dunes,partially trapped by vegetation, moving towards the NE.The migration of these parabolic dunes leaves a kind ofelongated sand tracks in the interdune depressions, locallycalled ‘‘worms’’ (Fig. 19.5). The trapping effect of vegeta-tion, together with a high water-table during periods oflimited dune advance, have been suggested as the primarycauses of these ‘‘worms’’ or sand tracks (Rodríguez-Ramí-rez et al. 2005). Archaeological remains from Late Neo-lithic/Calcolithic and Roman times are covered by thesedunes, which also include post-Medieval ceramics (Borjaet al. 1999), thus suggesting an age between the 14th and17th centuries, like the U6 unit described by Zazo et al.(1999, 2005a).

System V is the most recent and active aeolian system inDoñana. It comprises large NW-migrating transverse dunes(Rodríguez-Ramírez 2011) which can be correlated with theU7 unit of Zazo et al. (2005a). These dunes partially coverthe 17th century coastal watch-towers, and they occur

associated with the beach ridges that started to progradeimmediately after the construction of these towers (Borjaet al. 1999). These relationships suggest that they started toform around the end of 17th century, continuing theiractivity under prevailing SW winds until the present time(Fig. 19.6).

19.3.3 Littoral Spit Barrier

The Holocene geological record of this littoral Atlanticregion has received increasing attention in recent years.Five morphosedimentary units separated by erosional sur-faces have been distinguished and dated (Zazo et al. 1994;Rodríguez-Ramírez et al. 1996): H1: 6,900–4,500 cal yearBP, H2: 4,200–2,600 cal year BP, H3: 2,300–1,100 cal yearBP, and H4: 1,000 cal year BP–Present. They represent thesubaerial record of the Mid-Late Holocene coastal waveaction and the dominant southeastward drift current.

The great sand barrier of Doñana grew from northwest tosoutheast, starting at the western bank of the GuadalquivirEstuary outlet (Fig. 19.2). The landward growing dune fieldcovers a wide area of this spit barrier and its oldest out-cropping beach ridge has been AMS-dated for about5,000 cal year BP (Carrizosa-Vetalarena). Its morphologi-cal arrangement, perpendicular to the WNW–ESE directionof Doñana spit barrier, together with the small size, areevidence of a short-lived but highly intense erosional event(Ruiz et al. 2005) that destroyed an earlier spit formation(H1 of Zazo et al. 1994).

Fig. 19.3 Aeolian units U2 andU3 in El Asperillo cliff (photoJ.L. Goy). Organic-rich bedswithin U3 are related to humidconditions during the lastdeglaciation. Upper surfacecorresponds to an iron-richpalaeosoil generated during theHolocene climatic optimum(Zazo et al. 2005a)


The second progradation unit (4,200–2,600 cal year BP)isolated the Guadalquivir Estuary from the sea and severalshort rivers filled the inner shore with digitated deltas. Thisis the time when marshes were first protected by the earlyDoñana spit barrier. The prevalence of fluvial activitycaused a marked biological crisis on the previous marinefauna, and frequent accumulation of organic remains (shellbeds) with ridge morphology.

During the H2 to H3 transition the mouth of the Gua-dalquivir Estuary—the ancient Roman Lacus Ligustinus—suffered the action of a great tsunami event (218–209 BC)that substantially changed the coastal landscape and pro-duced new geomorphic features (Rodríguez-Vidal et al.2011). The earthquake had probably a similar or greatermagnitude (Mw & 8.5) than the AD 1755 event (Great

Lisbon quake), also recorded in this Atlantic coast (Ruizet al. 2013). The erosion of the tsunamigenic waves focusedin the littoral spits, in which morphological evidenceremains, including cliffs and incisions. The spit barrier ofLa Algaida became an island, and the pre-Roman humansettlements were abandoned. After that, the eroded fored-unes migrated inland, in the form of transgressive blownsand sheets. The marine bioclastic sand, brought into theestuary, was accumulated in the lagoon margins, leading thedevelopment of the estuarine sandy ridges of Vetalenguaand Las Nuevas.

The late progradation units (H3 and H4) produced aconsiderable growth of beach and dune reaches, the retreatof cliffs, and the gradual fill of the Guadalquivir Estuary. Inthe Doñana spit barrier these phases are recorded by the

Fig. 19.4 Dune systems (I–V, after Rodríguez-Ramírez 1998) andspit bars (H3 and H4, La Marismilla and San Jacinto) in Doñana

National Park (Google Earth image: 2013 Digital Globe and 2013Instituto de Cartografía de Andalucía)


strands of La Marismilla (H3) and San Jacinto (H4)(Fig. 19.4).

Today, the longshore drift is becoming stronger, anderosion is increasing at the end of San Jacinto strand. Hookswith NE orientation are being formed, encroaching into theGuadalquivir channel (Rodríguez-Ramírez et al. 1996).

19.3.4 Marshland

The Doñana marshlands are located in the area onceoccupied by the former Guadalquivir Estuary, forming avast silt–clay plain of approximately 2000 km2. TheNational Park also includes the entire fluvio-tidal complex.Although it is essentially a natural marsh, anthropogenicactions have modified the dynamics of some fluvial chan-nels that supply it with fresh water. This environment ischaracterized by a monotonous plain at less than 3 m a.s.l.

in the entire area, with small topographic irregularities(Fig. 19.7). Old levees stand out at the banks of the maintidal and fluvial channels, which isolate them from the restof the plain and constitute the most elevated sectors of themarsh. These levees retain the fresh water of the rain, whichfloods the lowest zones, isolating the marshland from thesea. The degraded levees form rounded and elongated rid-ges locally known as vetas. The low-lying zones that remainflooded for longer periods throughout the year are calledlucios, which constitute, together with the semi-blockedfluvio-tidal channels (caños), the low marsh (Rodríguez-Ramírez 1998).

Furthermore, within the silt–clay plain, there are somerather continuous long ridges, made up of sandy or shellydeposits, corresponding to relict beaches (Rodríguez-Ramírez and Yáñez-Camacho 2008). These are thin andnarrow accumulations generated either by intense erosionalevents such as storms or tsunamis, or as a result of the

Fig. 19.5 Active dune systemsin Doñana National Park. SystemV (foreground) is overlappingsystem IV (photo by L.Menanteau)

Fig. 19.6 Active aeolian dunessurrounding the 17th centurycoastal watch-tower in Doñanacoast (photo by M. Abad)


reworking of the deposits accumulated by these events(Rodríguez-Vidal et al. 2011). The oldest of these ridges arethose of Carrizosa and Vetalarena, with ages between 5,000and 4,000 years BP (Ruiz et al. 2005), and the most recentones are Vetalengua and Las Nuevas (2200–1900 year BP).

19.4 Evolution and Conclusions

The lower Guadalquivir River valley became a large estuaryas a result of the postglacial sea-level rise, which wasprogressively silted up by fluvial sediment supply. Aggra-dation was favoured by the growth of littoral spit barsduring Holocene times that eventually blocked the riverflow. Changes in littoral dynamics and sea-level variationswhich occurred since the LGM are the main factors thathave controlled the geomorphological evolution of the area.

During the LGM the coastline in the SW Iberian Pen-insula was located at 120 m below the present sea-level,with wide and deep valleys excavated by the main rivers.As the sea advanced over the coast during the subsequentpostglacial rise, the coastline acquired an uneven mor-phology with large inlets, estuaries and headlands. Theestuarine deposits accumulated in the main valleys of thearea indicate that the succeeding sea-level rise occurred intwo phases: an initial rapid rise (7.0–5.7 mm/year) between13,000 and 6,500 cal year BP, and a subsequent decelera-tion phase (2.6–0.9 mm/year) (Dabrio et al. 2000; Boskiet al. 2001; Lario et al. 2002; Zazo et al. 2008). This two-fold sea-level history caused a general change from verticalaggradation to lateral progradation recorded in severalestuaries of the area (Dabrio et al. 2000; Zazo et al. 2008).Climatically induced sea-level changes during the Holocenehighstand marked the alternation between progradational

Fig. 19.7 General (a1, b1) and local (a2, b2) views of Doñana marshland during wet and dry seasons. Landsat images elaborated by LAST-EBD (CSIC) (photos by C. Finlayson)


and erosional phases (Rodríguez-Ramírez et al. 1996; Goyet al. 2003; Zazo et al. 2008).

Six prograding spit bar systems have been identified inthe southern Iberian Peninsula (H1 to H6, Goy et al. 2003;Zazo et al. 2008), punctuated by short periods of limitedprogradation or erosion, that have been correlated with anincreased aridity during Bond events (Zazo et al. 2008).Nevertheless, in the Guadalquivir Estuary area, only fourphases have been described (Zazo et al. 1994; Rodríguez-Ramírez et al. 1996, 2005), and only the two most recentones crop out in Doñana area (Dabrio et al. 2000; Goy et al.2003; Rodríguez-Ramírez et al. 2005; Zazo et al. 2008).

Identification of beach ridges on spit bars in Doñana is ahard task due to both the fine grain size that favours aeolianreworking, and the occurrence of superimposed dunes.Archaeological remains (Menanteau 1979; Borja et al.1999), the scarce available outcrops of former shorelines, aswell as data from drill cores obtained in the Guadalquivirmarshlands (Ruiz et al. 2005) and radiocarbon dating (Larioet al. 1995; Rodríguez-Ramírez et al. 1996; Rodríguez-Ramírez and Yáñez-Camacho 2008; etc.), allow thereconstruction of the geomorphological evolution in severalphases:• Between MIS-5 and MIS-4 (El Asperillo Cliff). Upwar-

ping of El Abalario area induced, on one hand, thesouthward deviation of Guadalquivir River, and on theother hand, vertical displacement on the Torre del LoroFault, favouring the development of the first dunesystems.

• Deglaciation: Rapid sea-level rise (7.0–5.7 mm/year)between 13,000 and 6,500 cal year BP.

• Holocene Climatic Optimum (ca. 6,500 cal year BP). Thesea-level reached the maximum highstand, resulting inthe development of wide estuaries at the mouth of themain rivers. Wet and temperate climate favoured theformation of an iron-rich palaeosoil on an erosional sur-face in El Abalario area.

• First spit bar progradation phase (6,500–4,500 cal yearBP). Although there are no exposed remains, data fromdrill cores reveal that the Doñana littoral barrier wasalready growing between 5,500 and 5,400 cal year BP.The chenier of Carrizosa-Vetalarena (ca. 5,000 cal yearBP) may be the result of the catastrophic destruction ofthis early spit bar. Prevailing winds form the WSWcaused the growth of U4 dune system.

• Second spit bar progradation phase (4,200–2,600 cal yearBP). Fluvial dominance in the Guadalquivir Estuaryresulted in biological crisis and the development of theRoman Lacus Ligustinus. Pre-Roman settlement at LaAlgaida (Guadalquivir Estuary left bank) indicates thatH2 spit bar already existed at that time.

• Third (2,300–1,100 cal year BP) and Fourth (1,000–Present) spit bar progradation phases. By these twophases the estuary was definitively closed from the opensea. Acceleration in progradation of H3 and H4 spit barswas coeval to cliff retreat upstream the longshore currentat El Asperillo. Dune systems IV and V are correlative toH3 and H4 spit bars, as well as San Jacinto-La Marismillastrands, respectively.

Acknowledgments This work has been supported by MICINN-FEDER Projects CGL2010-15810, HAR2011-23798, CGL2012-33430, CGL2012-378, HAR2012-36008, and Excellence Project of theAndalousia Board (SEJ-4770) funded by the EU. It is a contribution toINQUA-CMP and Working Group UCM 910198 (Palaeoclimatologyand Global Change).

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[world geomorphological landscapes] landscapes and landforms of spain || coastal dunes and marshes...

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