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Barriendos, Mariano; Llasat, M. C.

doi:10.1023/a:1026327613698

Cited by 83 publications

(15 citation statements)

References 24 publications

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“…Period 2 comprises of a 20-years flood cluster at the end of the 18th century (large floods: 1776, 1783, 1787, 1795). This flood cluster coincides climatically with the "Malda Anomaly" (1760-1800) described for the Western Mediterranean as a period of high inter-annual hydrological variability (floods and droughts, [77]. In this high variability rainfall pattern, large floods occurred predominantly (>70%) in the autumn due to Mediterranean associated mesoscale convective systems [76].…”

Section: Information Content Of Palaeoflood Datasupporting

confidence: 79%

Extreme Floods in Small Mediterranean Catchments: Long-Term Response to Climate Variability and Change

Benito

Moya

Medialdea

et al. 2020

Water

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Climate change implies changes in the frequency and magnitude of flood events. The influence of climate variability on flooding was evaluated by an analysis of sedimentary (palaeofloods) and documentary archives. A 500-year palaeoflood record at Montlleó River (657 km2 in catchment area), eastern Spain, revealed up to 31 palaeofloods with a range of discharges of 20–950 m3 s−1, and with at least five floods exceeding 740–950 m3 s−1. This information contrasts with the available gauged flood registers (since year 1971) with an annual maximum daily discharge of 129 m3 s−1. Our palaeoflood dataset indicates flood cluster episodes at (1) 1570–1620, (2) 1775–1795, (3) 1850–1890, and (4) 1920–1969. Flood rich periods 1 and 3 corresponded to cooler than usual (about 0.3 °C and 0.2 °C) climate oscillations, whereas 2 and 4 were characterised by higher inter-annual climatic variability (floods and droughts). This high inter-annual rainfall variability increased over the last 150 years, leading to a reduction of annual maximum flow. Flood quantiles (>50 years) calculated from palaeoflood+gauged data showed 30%–40% higher peak discharges than those using only instrumental records, whereas when increasing the catchment area (1500 km2) the discharge estimation variance decreased to ~15%. The results reflect the higher sensitivity of small catchments to changes on flood magnitude and frequency due to climate variability whereas a larger catchment buffers the response due to the limited extent of convective storms. Our findings show that extended flood records provide robust knowledge about hazardous flooding that can assist in the prioritization of low-regret actions for flood-risk adaptation to climate change.

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Section: Information Content Of Palaeoflood Datasupporting

confidence: 79%

Extreme Floods in Small Mediterranean Catchments: Long-Term Response to Climate Variability and Change

Benito

Moya

Medialdea

et al. 2020

Water

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“…Despite the fact that this group appears to coincide with intense cold in the Iberian mountains (González-Trueba et al, 2008;García-Ruiz et al, 2014;Gómez-Ortiz et al, 2018), the smaller number of floods might also be consistent with the dry period between 1650 and 1715 (Domínguez-Castro et al, 2010;López-Blanco et al, 2016). There is a higher degree of coincidence between the Dalton Minimum and a period of abundant floods in the Jarama valley, which is in agreement with the abundant floods and precipitation in Andalucía (Rodrigo et al, 2008;Rodrigo, 2018), Cataluña (Maldá anomaly), (Barriendos and Llasat, 2003) and the Tagus River (Benito et al, 2003). This timing coincides with other similar studies reported in Europe (Brázdil et al, 1999;Glaser el al., 2010).…”

Section: Interpretation Of the Temporal Sequence Of Floodssupporting

confidence: 53%

“…First, there are palaeoclimatic and palaeohydrological reconstructions, which are useful for deducing the temporal variability in precipitation and floods during the last 500 years in Europe (Brázdil et al, 2006;Glaser et al, 2010) and Spain (Barriendos and Coeur, 2004; Barriendos and Rodrigo, 2006;Rodrigo and Barriendos, 2008). A complete study of floods in Cataluña from the 14th century was conducted by Llasat et al, 2005, which is also associated with the Maldás wet oscillation, situated within the Dalton phase of the LIA (Barriendos and Llasat, 2003). Flood intensities associated with the wet phases of the LIA in different Spanish areas were studied by Rodrigo et al, 2000 andRodrigo et al, 2018 in Andalucía and by Benito et al, 2003;Uribelarrea et al, 2003;Uribelarrea et al, 2004 andBullón, 2011 in the Tagus and Jarama-Tagus River basins.…”

Section: State Of the Art And Contextualizationmentioning

confidence: 99%

Little Ice Age, Palaeofloods and human adaptation on the Jarama River (Tajo Basin, Central Spain) from documentary proxy data

Bullón

2020

CIG

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This research assesses the close relationship between river history and human adaptation by combining the study of the migration of channels on the floodplain, the temporal distribution of floods, and human adaptation to the fluvial environment during the Little Ice Age (LIA) period on the Jarama River section situated between the mouths of two tributaries, the Henares and Manzanares. The methodology consists of the employment of abundant documentary records from the 14th to 19th centuries related to the response of society to hydrological dynamics within changing river patterns. The management and delimitation of land ownership, along with the readjustments and modifications therein, allow the inference of the changes that have taken place in the river throughout history. These changes include meander cut-offs, the abandonment of a channel fragment and aggradation in the alluvial plain, all of them located in different areas within the study area and with different historical timeframes. A relationship exists between changes in fluvial dynamics and the times of the greater abundance of floods. An initial change in the alluvial plain occurred in the Middle Ages as a result of the abandonment of the medieval channel and the creation of a new channel. The second change occurred between the 15th and 17th centuries and affected the properties on the right-hand bank of the river. Since the 18th century, the abandonment of and reduction in meanders and the aggradation at the Manzanares-Jarama mouth have created a new alluvial plain of the river. The different phases of the LIA defined herein coincide with much of the palynological and dendrochronological research conducted in other areas of the southwestern fringe of Europe. From the historical point of view, critical changes appear to be associated with some LIA phases. Furthermore, the progressive transformation of communal lands into public or private property could be promoted by the intense floods recorded since the 15th century. The Maunder and Dalton Minimums occurred together with an increase in the area assigned for agriculture on the alluvial plain; this land use type continued to grow during the 19th and 20th centuries.

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“…Moister conditions on the IP during this phase of the LIA (1500-1750 AD) are documented by the increase in flood frequency in the Tagus River watershed (Benito et al 2003a;Moreno et al 2008), reaching maximum frequency and intensity during the sixteenth century, and archaeological records (Ferrio et al 2006) in the Ebro Basin. The occurrence of arid conditions during the late eighteenth century correlates with the so-called Maldá Anomaly in NE Spain (Barriendos and Llasat 2003)…”

mentioning

confidence: 99%

Climate changes and human activities recorded in the sediments of Lake Estanya (NE Spain) during the Medieval Warm Period and Little Ice Age

et al. 2009

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Untitled

Cited by 83 publications

References 24 publications

Extreme Floods in Small Mediterranean Catchments: Long-Term Response to Climate Variability and Change

Extreme Floods in Small Mediterranean Catchments: Long-Term Response to Climate Variability and Change

Little Ice Age, Palaeofloods and human adaptation on the Jarama River (Tajo Basin, Central Spain) from documentary proxy data

Climate changes and human activities recorded in the sediments of Lake Estanya (NE Spain) during the Medieval Warm Period and Little Ice Age

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