FIELDTRIP DOÑANA V RCANS CONGRESS mod REVfundacion.usal.es/rcans/.../2013_5thRCANS-Huelva...V RCANS INTRA‐CONGRESS FIELDTRIP: VISIT TO DOÑANA NATIONAL PARK (SEPTEMBER 25, 2013)

V RCANS INTRA‐CONGRESS FIELDTRIP: VISIT TO DOÑANA NATIONAL PARK (SEPTEMBER 25, 2013)

V RCANS INTRA-CONGRESS FIELDTRIP

VISIT TO DOÑANA NATIONAL PARK

Joaquín Rodríguez‐Vidal (Coord.) Juan José Negro

Clive Finlayson Cristino Dabrio

Francisco Borja Manuel Abad

Luis Miguel Cáceres Tatiana Izquierdo


INDEX

Introduction……………………………………………………………………………………………………... 1

Stop A: The sedimentary record of El Asperillo Cliffs……………............................... 4

Stop B: Introduction to the natural environment of the Doñana National Park…. 7

Stop C: The ecological value of La Vera and Doñana lakes………………………………… 9

Stop D: The record of tsunamis in the Doñana National Park……………………….…… 11

Stop E: Recent evolution of Doñana shoreline: Almenara watch‐tower…….……… 14

Contributing authors.……………………………………………………………………………………….. 16


1

INTRODUCTION

This visit to the Doñana National Park is carried out in collaboration with the Doñana

Biological Station (Estación Biológica de Doñana, EBD). A 4WD bus and 4WD jeeps will

be headed by specialists in the geology and biology of Doñana N.P. The visit consists on

a guided geo‐tour of about 80 km that takes ~7.5 hours and visits all the ecosystems of

Doñana (marsh, dunes, lagoon) and the main geological features that record the

Quaternary history of this National Park (tsunami and storm deposits, dune systems,

coastal retreat and progradation, recent climate and sea‐level changes; Figure 1). The

planned itinerary will go across areas that are not normally allowed for tourists.

Figure 1. Location of the cheniers and coastal spit barriers in the south of Doñana.

Doñana National Park is a lowlying area of marsh, shallow streams, and sand dunes,

that includes the Guadalquivir River Delta region where the river flows into the Atlantic

Ocean. The original area was established in 1963, UNESCO recognized it as a Biosphere

reserve in 1980 and as World Heritage Site in 1994. It is a wetland of international

importance on the list of the Ramsar Convention. The Park has a unique biodiversity

and it is considered as the largest ecological reserve in Europe. It contains a great

variety of ecosystems and shelters wildlife including thousands of European and

African migratory birds (due to its proximity to the Strait of Gibraltar), fallow deer,

San Jacinto

La Algaida

Marismilla

El Abalario

OCEANO

ATLANTICO

0 10 km

Carrizosa-Veta la Arena

Las Nuevas

VetalenguaR

ío

Guadalquivir

N

SUSTRATO PLIO-PLEISTOCEMO

MARISMAS

FASES DE CRECIMIENTODE LOS SISTEMAS DE DUNAS Y PLAYAS

CORDONES LITORALES

CHENIERS Y VETAS

España


2

Spanish red deer, wild boar, European badger, Egyptian mongoose, and endangered

species such as the Spanish Imperial Eagle and Iberian Lynx which is the most

endangered cat species of the world. The Doñana Biological Station is a reference

Research Institute in the area of Natural Resources.

The present‐day geological scenario of Doñana National Park is the final result of a

long geological evolution, with the development of a deep aquifer and numerous

geomorphological features that enhance the biodiversity. During the Holocene, this

area was configured by freshwater/brackish marshes, ponds and aeolian units, with

some marine inputs caused by high‐energy events. This variability of ecosystems was

interrupted by the Holocene transgression. At this time, Doñana National Park and the

surrounding areas were flooded and a large lagoon, later call by the romans Lacus

Ligustinus, was developed. The last 6 kyr include an increasing infilling process, with an

accelerated growth of spits and new inner marshlands and ponds. At present, the

extensive marshes of Doñana National Park present a flat topography, with some inner

depressions occupied by temporary or permanent wetlands, locally called ´lucios´. The

whole system is protected by the Doñana spit, a wide sandy barrier with active dune

systems growing toward the southeast. In addition, some “hills” (2‐3 m height) are

formed by bioclastic or sandy ridges, caused by high‐energy events during the last

5,000 years.

Figure 2. Proposed itinerary for the Doñana N.P. visit


3

The proposed itinerary consist on seven stops, six of them inside the limits of the

protected area of Doñana (Figure 2). Stop A takes place at the Asperillo cliffs where Dr.

Cristino Dabrio and Dr. Francisco Borja will explain the origin and significance of these

Pleistocene units in relation with the recent evolution of Doñana littoral surroundings.

After the lunch at Doñana Palace, Dr. Juan José Negro will introduce us the significant

value of Doñana’s natural heritage and we will start the visit at Santa Olalla Lake and

La Vera, where Dr. Clive Finlayson and Dr. Francisco Borja will describe in depth the

geomorphological and ecological interest of these features. The itinerary penetrates

inside the Park through its marshlands to reach Vetalengua ridge, where Dr. Joaquín

Rodríguez Vidal will expound the tsunami record in Doñana. Finally, we will return to

Doñana Palace along the coast from Punta del Malandar, where Dr. Luis Miguel

Cáceres and Dr. Cristino Dabrio will explain us the dune system and the progradation

and retreat of the beaches in the Park with the help of the Almenara watch‐towers.


4

STOP A: THE SEDIMENTARY RECORD OF EL ASPERILLO CLIFFS

C.J. DABRIO, F. BORJA, C. ZAZO, J.L. GOY, E. ROQUERO, P.G. SILVA, J. LARIO, A. CABERO, C. BORJA, F. DÍAZ DEL OLMO

El Asperillo Cliffs

El Abalario area includes the most recent part of the sedimentary fill of the western

Guadalquivir basin. It records the interaction of sedimentation on a coastal plain

(including sea level changes of varying magnitudes) and upwarping of the underlying

Pliocene‐Pleistocene prograding deltaic sequence. Upwarping is probably related to

escape of over‐pressurized fluids, accompanied by dewatering, prior to (?) and during

OIS (Oxygen Isotope Stage) 5. Continued upwarping produced the large gravitational

fault of Torre del Loro (TLF) in the south‐western flank of the dome in NW–SE

direction, roughly parallel to the present coastline during OIS 5–OIS 4. El Abalario

Dome is an NW–SE elongated, elliptical–shaped topographic feature (Fig. 3).

Figure 3. Geological synthetic map of the El Abalario Dome (Zazo et al., 2005). Legend: 1, Subaerial drainage

network; 2, offshore drainage lines; 3, Drainage divide with height spots; 4, Torre del Loro Fault (TLF) lines; 5, Zone

of drainage anomaly at the dome top; 6, shallow ponds and ponded areas; 7, Lignite exploration wells; 8,

Hydrogeological exploration wells (Salvany & Custodio, 1995); 9, Petroleum exploration wells (ITGE, 1990); 10,

Geodetic bench–marks: 106 m bench‐mark corresponds to El Asperillo; 11, Plio–Pleistocene sandy coastal–plain

deposits; 12, Late Pleistocene upthrown block deposits; 13, Late Pleistocene downthrown block deposits and

Holocene dune systems; 14, Coastal active dune systems on sea–cliff; 15, Present beach deposits; 16, Marshlands (in

black: channel systems); 17, Localities.


5

This elevated area served as anchor to the Holocene spit–bars and dune systems

forming the Doñana littoral bar that eventually closed the Guadalquivir river basin

(Zazo et al., 1994; Rodríguez Ramírez et al., 1996, Zazo et al., 2005). The El Asperillo

cliff constitutes the south‐western truncated littoral flank of the dome.

The Asperillo cliff extends for 28 km between the resorts of Mazagón and

Matalascañas (Fig. 3) with average elevations around 20 m. The cliff is being carved

into weakly cemented sandstones by the moderate energy waves of a mesotidal coast

(mean tidal range slightly above 2 m) and undergoes active retreat under

Mediterranean climate with an Atlantic influence and prevailing SW and subordinate E

and SE winds.

The cliffs expose the internal structure of the dome (Fig. 4). Sediments consist mainly

of very well sorted, medium to fine sand. Quartz grains average 80%, plagioclase and

potassium feldspars less than 10%. Biotite, tourmaline and other ferro‐magnesian

minerals are very scarce. Locally, the silt and clay fraction may reach 60% in the

topmost part of the fluviatile deposits.

Figure 4. Schematic profile showing the distribution of sedimentary units and palaeosols. Note the strong vertical

exaggeration. Distances in km from Torre de la Higuera watchtower (after Zazo et al., 1999).

Zazo et al. (1999, 2005) used sedimentary facies analysis, palaeocurrent

measurements, subsurface data from hydrological drillings, Optically Stimulated

Luminiscence (OSL) and radiocarbon measurements (AMS and conventional) to

distinguish several units and to prove that the TLF separated two palaeogeographic

domains. The upthrown tectonic block contains fluvial, marine and aeolian deposits (in

ascending stratigraphic order), whereas the downthrown block trapped aeolian

sediments and laterally discontinuous sand layers rich in organic matter, in which three


6

units (U1 to U3) were identified. A surface enriched in iron oxide fossilised the fault

trace sealing both blocks. It is covered by younger semi–mobile and mobile aeolian

dunes (U4, U5 and U6) that accumulated growing up to topographic elevations above

100 m.

The littoral aeolian sheet and wetland system of El Abalario‐Doñana

The littoral aeolian sheet of El Abalario‐Doñana supports more than 600 small ponds

(the highest density in Spain), most them seasonal. The dominant pond morphology is

rounded because they are generated after blowouts. Elongate ponds relate to inter‐

dune corridors and dune fronts. The regional aquifer contributes to the ponds during

periods of high waters, and many ponds form groups mutually interconnected. In any

other times, only the ponds placed along the zone of drainage anomalies at the dome

top (ZDA) remain connected to the aquifer, whereas the others receive water from

sub‐superficial flows only, along the semi‐permeable hydromorphic layers (Borja,

2011).

Acknowledgements Financial support from Spanish Research Projects: CGL08‐03998BTE, CGL08‐04000BTE, CGL12‐33430, and CGL2009‐

11539/BTE, Consolider‐Ingenio CSD2007‐00067‐GRACCIE, AECI‐A/017978/08. UCM Research Group 910198

(Paleoclimatology and Global Change); GEOTOP Lab. Contrib. IGCP 588, and INQUA CMP Comm. ‘Long Term Sea‐

level Changes’ F.A.

References Borja, C. (2011). Lagunas de Doñana (Huelva). Tesis Doctoral Universidad Sevilla. Dirs.: F. Díaz & F. Borja. 531 págs.

(Unp.) ITGE (1990). Introducción, Guadalquivir – Golfo de Cádiz. In: Documentos sobre la geología del subsuelo de España.

Instituto Tecnológico Geominero de España, Madrid. Rodríguez Ramírez, A., Rodríguez–Vidal, J., Cáceres, L., Clemente, L., Belluomini, G., Manfra, L., Improta, S. and De

Andrés, J.R. (1996). Recent coastal evolution of the Doñana National Park (SW Spain). Quaternary Science Reviews, 15, 803–809.

Salvany, J.M. and Custodio, E. (1995). Características litológicas de los depósitos pliocuaternarios del Bajo Guadalquivir en el área de Doñana: implicaciones hidrogeológicas. Revista Sociedad Geológica de España, 8, 21–31.

Zazo, C., Dabrio, C.J., Borja, F., Goy, J.L., Lézine, A.M. Lario, J., Polo, M.D., Hoyos, M. and Boersma. J.R. (1999). Pleistocene and Holocene aeolian facies along the Huelva coast (southern Spain): climatic and neotectonic implications. Geologie en Mijnbouw, 77, 209–224.

Zazo, C., Mercier, N., Silva, P.G., Dabrio, C.J., Goy, J.L., Roquero, E., Soler, V., Borja, F., Lario, J., Polo, M.D. and Luque, L. (2005). Landscape evolution and geodynamic controls in the Gulf of Cadiz (Huelva coast, SW Spain) during the Late Quaternary. Geomorphology, 68, 269‐290.


7

STOP B: INTRODUCTION TO THE NATURAL HERITAGE OF THE DOÑANA N. P.

J.J. NEGRO

The Natural Area of Doñana extends over 106,047 hectares and includes Doñana

National and Natural Parks. It is located on the SW Atlantic coast of the Iberian

Peninsula in the Municipal District of Almonte (Huelva). It is one of the most important

protected areas of Andalusia and the largest ecological reserve in Europe. The

geographical situation of Andalusia, as a bridge between Europe and North of Africa,

offers the possibility for European researchers to study many Iberian and African

species. This space has been catalogued as Area of Special Protection for Birds (ZEPA),

Site of Communitarian Importance (LIC ES0000024; 112,355.29 hectares), Biosphere

Reserve (77,260 hectares, since 1980), World Heritage Site (since 1994), RAMSAR site

(111,645.81 hectares, since 1982) and has been qualified as Important Area for the

Steppe Birds in Andalusia (ZIAE 2). The wealth of its aquatic and terrestrial ecosystems

(beaches, dunes, marshlands, scrubland, pine tree forests, streams, lagoons, etc.)

endow its unique characteristics to house a large amount of species, amongst which

some emblematic ones can be highlighted, such as the Iberian lynx and the Imperial

eagle. The marshland can be highlighted as a stopping, breeding and wintering site for

thousands of European, Iberian and African birds, making it an ecosystem with a high

ecological value.

Doñana includes four large ecosystems: the beach, the dunes, scrub‐woodland, and

marshes. Within these, 21 different biotopes have been described, the following 11 of

which are particularly important for their uniqueness in an European context: Scirpus

maritimus marsh, saltmarsh, seasonal lakes, marsh channels, permanent lagoons, the

scrub‐marsh ecotone (known locally as the "vera"), mobile dunes, Mediterranean

woodland, juniper forest, heathland and maquis. The flora includes 803 species of

vascular plants, including 48 endemics to Spain, and four to the Doñana area. The

fauna includes 41 ant species, seven freshwater fish, 30 estuarine fish, 12 amphibians,

19 reptiles and 29 mammals. The avifauna is outstanding, with 361 species

representing 70% of all the species present in Europe. Of these, 119 species breed

regularly in Doñana. In winter, up to 700.000 waterbirds concentrate in the marshes,

making Doñana one of the most important European wetlands. Doñana and its

surroundings provide one of the last strongholds in Europe for the Marbled Teal,

White‐headed Duck and Crested Coot.

Doñana Biological Reserve (ICTS‐RBD), situated in the hearth of Doñana National Park,

is managed by Doñana Biological Station (EBD), a research institute belonging to the

Spanish Council for Scientific Research (CSIC). It consists of two estates, the Doñana

Biological Reserve, which extends over 6,794 hectares, and the Guadiamar Biological


8

Reserve, extending over 3,214 hectares. The scientific and administrative affairs are

managed by EBD. At the same time, the legally appointed director of the EBD, in

accordance with the Doñana Law 91/1978 and the Royal Decree 97/2005, is

responsible for coordinating all research projects undertaken in the Doñana Natural

Area. ICTS‐RBD´s main aim is to provide the space and the necessary technical facilities

so that research of the highest standard can be carried out by internal as well as

external users in the facilities of the Doñana ecosystems. This area is legally protected

from direct or uncontrolled human activity. Only researchers and technicians are

allowed to enter the park, which is a great advantage for research development.

Figure 5.


9

STOP C: THE ECOLOGICAL VALUE OF LA VERA AND DOÑANA LAKES

C. FINLAYSON

Zones of high physiographical diversity at small spatial scales generate rich ecological

diversity, generally referred to as ecotones. This often occurs where topographical

changes occur across small distances but they can happen in other scenarios. In the

low‐lying ground of the Coto Doñana a major ecotone exists where the ground water

that has filtered into the dune systems surfaces at its interface with the substrate of

the marismas – the large marshlands of the Guadalquivir River. This ecotone is known

locally as La Vera and is a veritable inland coastline which runs for many kilometres in a

roughly north‐south direction.

Figure 6.

The ecological richness of La Vera varies between seasons and years but is always high.

During the dry summer months (July‐September) it is – alongside the lakes with

permanent water – an area that concentrates many species which come to drink in the

receding water holes. They are also a source of concentration of predators which hunt

the animals which are dying inside the drying pools or others which are gathered to

drink. La Vera and the Doñana lakes thus concentrate a variety of species at this time

including Fallow Deer Dama dama, Red Deer Cervus elaphus and Wild Boar Sus scrofa;

predators that regularly hunt here are the endangered Iberian Lynx Lynx pardina as

well as raptors, particularly Black Kite Milvus migrans, Red Kite Milvus milvus and the


10

endangered Spanish Imperial Eagle Aquila adalberti. In late summer, from late August

to late October, these zones attract many trans‐Saharan passerine migratory birds

which arrive from northern Europe and use the area as a stop‐over ahead of the

crossing of the Sahara Desert. Typical species include Northern Wheatear Oenanthe

oenanthe and Pied Flycatcher Ficedula hypoleuca.

In wet winters, when the marismas flood, many animals concentrate in La Vera where

there is dry ground. This provides a different kind of concentration, of waterfowl and

wading birds, as well as the mammalian herbivores, which attracts predators. At this

time Marsh Harriers Circus aeruginosus are particularly numerous. The receding waters

during the spring see La Vera at its best. The Cork Oak Quercus suber and other trees

which are scattered in linear fashion along it attract vast numbers of birds that will

nest on the trees and, from here, radiate out to forage in the marshes and along La

Vera itself. These large nesting colonies are known famously as “La Pajarera” and the

species that nest in these trees include the kites and eagles as well as Spoonbills

Platalea leucorodia, Grey Herons Ardea cinerea, White Storks Ciconia ciconia and

Black‐crowned Night Herons Nycticorax nycticorax.


11

STOP D: THE RECORD OF TSUNAMIS IN THE DOÑANA NATIONAL PARK

J. RODRÍGUEZ‐VIDAL, M. ABAD

Between 218 and 209 BC, the western coasts of Iberia suffered the impact of a

historical tsunami, with an epicentre probably located in the Atlantic Ocean near the

Cape St. Vincent area (SW Portugal). Palaeogeographical changes in the River

Guadalquivir estuary, the ancient Roman Lacus Ligustinus, have been recorded in

erosional and depositional landforms, both stratigraphically and as landscape relicts.

The tsunamigenic waves (run‐up of 5 m) and their subsequent backwash eroded the

previous littoral spits transversally, generating rectilinear cliffs and incisions. The

littoral foredunes were also eroded and reactivated as transgressive dunes over the

edge of the marshes. Former coastal sediments (520‐100 BC) generated overwash

deposits, ebb tide deltas and sand sheets within the estuary, as well as a subsequent

bioclastic beach on the lagoon shore, defining the post‐tsunami (130 BC‐ 80 AD)

estuarine shoreline (Roman lagoon). Some coastal pre‐Roman (7th to 3rd centuries BC)

human settlements were abandoned, and later, in the Roman period (1st century AD),

saltworks were installed.

Figure 7. Geographical location of the study area, Holocene morphosedimentary features and core sites (CM, DR, GR, HR) in the Guadalquivir estuary (Doñana marshlands).


12

The Vetalengua ridge is characterized by a large lateral extension and a narrow width

(20‐30 m). Thickness (5‐70 cm in most cases) decreases landward, usually covering

previous marsh and lagoon facies. They display an erosive base, with vegetation

remains and intraclasts of the underlying sediments in the basal lag. In the upper part,

bioclasts are in most cases fragmented and arranged in thick laminae or displaying a

disorganized disposition. Textural analysis allows delimiting subfacies with a bimodal

grain‐size distribution and poor sorting in both cases.

Figure 8. Core profiles showing lithofacies and calibrated ages of shells

These deposits are constituted by bioclasts included in a greenish to greyish silty‐sandy

matrix. In general, facies exhibit fining‐upward sequences, passing from basal fine

sands to very fine sands with important contribution of silt near the top. Quartz is the

main component (up to 70% in most cases), accompanied by secondary percentages of

phyllosilicates and feldspars. Molluscs represent an important proportion (10‐40% dry

weight) of the sediment. Shell debris and disarticulated bivalve shells of euryhaline

(mainly C. edule) and marine (mainly A. tuberculata, Donax vittatus and Spisula solida)

are abundant. Gastropods are represented by freshwater (Gyraulus laevis, Melanopsis)

and marine (Rissoa, Lemintina, Hinia) specimens. Fragments of barnacles, scaphopods

and bryozoans are also frequent. Microfauna is well represented with 50‐500

individuals/g of brackish ostracods (Cyprideis torosa, Loxoconcha elliptica) and

foraminifera (Ammonia tepida, Haynesina germanica), together with marine

specimens of both groups (Basslerites berchoni, Carinocythereis whitei, Urocythereis

britannica, A. beccarii, E. crispum).

These ridges show numerous features described in tsunamigenic deposits: a) an

erosional base; b) occurrence of intraclast and plant remains near the base; c) finer

sediments towards the top; d) presence of higher sand percentages (near the Doñana

spitbarrier) in relation to the underlying sediments; e) changes in the clay mineral

composition; f) strong changes of fauna in relation to the underlying layers; g)


13

presence of numerous marine species of both macro and microfauna with evidence of

reworking. Consequently, a tsunamigenic origin is attributed to these beds.

Figure 9. Morphosedimentary formations of Vetalengua area and DR core. 1‐2, interpretative cross‐section of Vetalengua ridge during Roman time


14

STOP E: RECENT EVOLUTION OF DOÑANA SHORELINE: ALMENARA WATCH‐TOWERS

L.M. CÁCERES, J. RODRÍGUEZ‐VIDAL, M. ABAD

Several defensive towers (Torres de Almenara) were constructed in the late 16th and

early 17th century along the main beaches to prevent the pirate attacks. Some towers

remain actually, whereas others have been destructed by erosion processes and

human activities. Nevertheless, the precise location of all of them was situated in an

anonymous text of 1756 and a nautical map of 1770, both cited by Menanteau (1979).

The difference between the 1756‐1770 situations and the present‐day location permits

to estimate the average progradation ratios in these beaches.

Once reached the transgressive maximum (Flandrian Maximun) around 6500 years BP,

the Huelva coast experienced a progressive stabilization recorded in the backward

movement of the interfluvials sectors with cliff generation, as well as in the

progradation of the estuaries. This tendency has been steady until the present time as

it is possible to be observed by means of historical constructions like the Almenara

watch‐towers. The advance or retreat movements of the littoral of Huelva are

represented in Figure 10 where these constructions are still preserved. The absolute

values and the annual mean rates for the last two and a half centuries are also

indicated. At a first glance, it is possible to establish two sectors with different trends.

Firstly, the western sector, where progradation prevails, is characterized by the large

advances of the coast as those occurred in Isla Canela or in the Punta Umbría‐Punta

Arenilla spits. In this sector, the development of spits and barrier islands has forced the

Flandrian shoreline to move progressively seawards. On the other hand, in the eastern

sector prevails an erosive coast with cliffs in which retreats of as much as 300 m are

recorded (Asperillo). However, in the most eastern sector of Doñana a large coastal

progradation is produced by means of the formation of the large spit system of

Doñana. Erosion in Mazagón and La Hoguera watch‐tower has softened this old

promontory with the result of a progressive movement of the erosive‐sedimentary

inflexion point towards the east, where is now located at Zalabar watch‐tower. In this

sense, erosive processes have been transferred towards areas that were initially

progradating and promote the growing of the end of the spit de Doñana.

The rates of advance or backward movement are regulated by the cyclonal or

anticyclonal activity, which influences directly in marine dynamics. These climatic

cycles regulate the availability of sedimentary supply and therefore, the growth of

beaches, sandy barriers, as well as the cliff backward movement. In the last decades,

different alterations in the coast have modified their natural dynamics and therefore,

they have broken the existing balance. Especially showy are the groynes located in the

fluvial mouths, which cause retention of sediments to the west and deficit and erosion to

the east.


15

Figure 10. Sedimentary and erosive balance in the section Guadalquivir‐Guadiana, from present and historic dates.

“Torres de Almenara” are been used as shoreline indicators.


16

CONTRIBUTING AUTHORS

M. ABAD. Departamento de Geodinámica y Paleontología. Universidad de Huelva. Avda. 3 de Marzo,

s/n 21071 Huelva ([email protected])

C. BORJA. Departamento de Geografía Física y Análisis Geográfico Regional. Universidad de Sevilla. C/

María de Padilla, s/n. 41004‐Sevilla. Spain ([email protected])

F. BORJA. Departamento de Historia II y Geografía, Facultad de Humanidades, Universidad de Huelva,

21007 Huelva, Spain ([email protected])

A. CABERO. Departamento de Ciencias Analíticas, Facultad de Ciencias. Universidad Nacional de

Educación a Distancia. 28040‐Madrid, Spain ([email protected])

L.M. CÁCERES. Departamento de Geodinámica y Paleontología. Universidad de Huelva. Avda. 3 de

Marzo, s/n 21071 Huelva ([email protected])

C.J. DABRIO. Departamento de Estratigrafía–UCM, Universidad Complutense, 28040–Madrid, Spain

([email protected])

F. DÍAZ DEL OLMO. Departamento de Geografía Física y Análisis Geográfico Regional. Universidad de

Sevilla. C/ María de Padilla, s/n. 41004‐Sevilla. Spain ([email protected])

C. FINLAYSON. The Gibraltar Museum. 18‐20 Bomb House Lane, PO Box 939, Gibraltar (UK)

([email protected])

J.L. GOY. Departamento de Geología, Facultad de Ciencias, Universidad, 37008–Salamanca, Spain

([email protected])

J. LARIO .Departamento de Ciencias Analíticas, Facultad de Ciencias. Universidad Nacional de Educación

a Distancia. 28040‐Madrid, Spain ([email protected])

J.J. NEGRO. Estación Biológica de Doñana, CSIC. c/ Americo Vespucio s/n, 41092 Isla de la Cartuja,

Sevilla, Spain ([email protected])

J. RODRÍGUEZ‐VIDAL. Departamento de Geodinámica y Paleontología. Universidad de Huelva. Avda. 3

de Marzo, s/n 21071 Huelva ([email protected])

E. ROQUERO Departamento de Edafología, ETS I. Agrónomos, Universidad Politécnica, 28040–Madrid,

Spain ([email protected])

P.G. SILVA Departamento de Geología, Facultad de Ciencias, Universidad, 37008–Salamanca, Spain

([email protected])

C. ZAZO Departamento de Geología, Museo Nacional de Ciencias Naturales–CSIC, 28006–Madrid, Spain

([email protected])

FIELDTRIP DOÑANA V RCANS CONGRESS mod REVfundacion.usal.es/rcans/.../2013_5thRCANS-Huelva...V RCANS INTRA‐CONGRESS FIELDTRIP: VISIT TO DOÑANA NATIONAL PARK (SEPTEMBER 25, 2013)

Documents