dc.description.abstract
[eng] Many sediment-covered mountain areas affected by the growth of
Pleistocene glaciers are over-consolidated. Palaeoglacial conditions are
deduced from glacial consolidation and site investigations. Geomorphological
evidence on the glacial extent and history is in this Thesis used as a framework
for hydro-mechanical flow simulations in the valley glacier of Andorra and the
lower Isère glaciated valley. From the effects observed within the fossil record
of ancient glaciated valleys, a reliable reconstruction of palaeo-glacier’s
thickness is possible when former ice-tonges overlayed porous aquifers,
because subglacial erosion was mitigated by the subglacial water pressure
limiting subglacial till formation. Records of minimum preconsolidation values
indicate a buoyant surging glacier. For palaeoglacier reconstruction, the glacial
valley geomorphology is clue providing the palaeogeographical calibration for
further hydrogeomechanical calculations, especially at successive glacial
stages during the deglaciation. A modern analogue, the Hansbreen sub-polar
glacier, helps to set up a conceptual model allowing a better understanding of
the glaciology of the two studied former valley glaciers, comparable to a
polythermal glacier type.
Tills and glaciolacustrine deposits from Andorra’s main valley and its
principal tributary of La Massana allow for reliable local deglaciation patterns
between GS-9 (40 ka b2k) and the Holocene Optimum (9.3–5.5 b2k). However,
from the palaeoenvironmental data of the Pyrenees, deglaciation started
sooner, and aridity affected the size of the glaciers from GS-10, resetting the
valley glacier conditions ahead of GI-7. This affected the mainly prominent
glacier-ice transfluence pass in the Pyrenees and the extension of the ice
tongues on both sides of the mountain belt between GI-9 and GI-7, also during
GS-5.2 and GI-5.1. During and posteriorly Heinrich event H4, aridity did not
favour the development of valley glaciers in Andorra until stadial GS-7; however, glaciers in the Pyrenees progressed during the following Heinrich
event (H3).
Using geochemical data (Al, Ti, Ca, K, P), a basic limnological study permits
a palaeoenvironmental interpretation in Andorra by adding data from stable
carbon isotope (δ13C) from bulk carbon samples and AMS dates. Results show
four unreported inland δ13C cycles linked to low water levels in the ice-dammed
lake of Andorra (La Massana palaeolake). At the beginning of each cycle,
enhanced δ13C bulk carbon values are found (> -23‰), a proxy of abrupt
shifting from Type-C3 to Type-C4 vegetation. The beginning of the LGM and
Heinrich events H3 and H2 were marked by enhanced δ13C values interpreted
as a product of strong climate change that boosted aridity. The retrieval period
towards δ13C depleted values (< -23‰) spans 4,500±500 years.
In Andorra, the beginnings of H3 and H2 events were relatively dry, and the
second half of the climate was moist. The first evidence of sediments coming
from the motion of a temperate-base glacier in the Pyrenees was from stadial
GI-3. Moist conditions suddenly stopped at the beginning of Heinrich event 2
and returned at the end of H2. This moisture behaviour during H2 on the
southern slopes of the Pyrenees is the opposite of the wet-to-dry conditions
described in NW Iberia. Conversely, the H1 event had a wet-to-dry structure
coast to coast of Iberia, including in the SE Pyrenees (Andorra).
A transition from single-phase-like glacier advances (NW Iberia) to
multiphase glacier advances (SE Pyrenees) was due to a change from coldbased
glaciers to temperate-based glaciers. However, glacier sensibility to
global changes increases through time toward NW Iberia. The Last Maximum
Ice Extent and the Global LGM did not concur in places experiencing
multiphase glacier advances. Indeed both extreme behaviours do not
correspond to the same type of glaciers. Polar-type glaciers in NW Iberia are in
this Thesis invoked, while tempered or polythermal were frequent in NE Iberia.
Abrupt glacier advances and quick glacier recession in Andorra are
interpreted as surges from a mass-imbalanced glacier. Two kinds of surge
events are distinguished from available data in the Pyrenees, those surges
produced by overfed ice tongues fed by short-lived cold spells (in GS-2b and
H1) and those surges produced by buoyant melting ice tongues within the glaciated valley (between stadials GS-5/GI-4, stadials GI-3/GS-3 and stadials
GS-2.1b/GS-2.1a) by a warm moist climate. The winter solar rate increase (GI-3
and GS-5.1) and the evidence of polythermal-type glaciers matched.
Conversely, summer insolation increases and wet-ice type oversaturated
glaciers and surges at GS-2a concurred. In Andorra the snow-overfed glacier
surges correlate with the decreasing winter insolation during GS-2b. In Iberia,
the LGM would be placed between 23-17.5 ka and glaciers spread, linked to
both wet westerlies from the North Atlantic and moisture supply of
Mediterranean influence, reaching almost the eastern side of the Central
Pyrenees, leading us to suppose an NW-NE seesaw climatic relationship
across Iberia almost since GS-5.1. The oscillations of the oceanic thermal front
promoted wet/dry westerly winds crossing over the Pyrenees, pushing back the
Mediterranean influence towards the East.
By classifying glacial phases of the northern Iberian Peninsula fringe, four
common glacial phases arise for the last glacial cycle:
A An early LGC starting at MIS 5d having a recessional period during MIS
5c. Cold-type glaciers are expected to have existed in some of the extreme NW
of the Iberian mountains until Termination 1.
B The Last Maximum Ice Extent occurred mainly during MIS 5a – MIS 4.
An asymmetrical glacier recession during MIS 3 was related to an increase in
eastward aridity.
C Significant glacier fluctuations during the MIS 3 – MIS 2 hinge, the
appraisal of temperated-polythermal type of glaciers accompanied by a
generalised moisture increase entailing valley glaciers to surge.
D Side-to-side mountain range-scale deglaciation dissymmetry in MIS 2.
The widespread expansion of tempered-polythermal type glaciers during the
LGM period and Termination 1 had a proportional expansion to the available
moisture.
The final deglaciation is characterised by relictual cirque glaciers
disappearing during GS-1. In Andorra, a general rise in local river base levels
occurred until the Holocene Optimum.
Unravelling the afore-cited glacial phases and unexpected research allows
for a tesselated mapping of the SW continental Europe concerning part, or all of
the LGC glacial phases outlined above:
1 – Areas where glaciers were prevalent during MIS 2, like the Iberian
Central System, the NW and S French Massif Central, the NW Jura and the
maritime Alps.
2 – Areas having a far-flung end moraine produced in a previous glacial
phase (MIS 6 or posterior) showing stability until the MIS 2, as for ice
caps/fields from the southern half of the Galicia mountains.
3 – Areas of pseudo-pleniglacial or apparent-pleniglacial condition, despite
previous glacier recessions phases (albeit challenging to identify), as in most of
the northern slope of the Pyrenees.
4 – Areas of multiphase glacier advances, like most of the southern slope of
the Pyrenees, most of the Cantabrian Mountains, the half north of the Galicia
mountains, the High Atlas, Sierra Nevada and the SW French Massif Central,
the western Alps and the Vosges.
5 – Areas where glaciers were present from the LGM until Termination-I, like
the northern Iberian range and Sanabria in Iberia. Nevertheless, other mountain
ranges have a Type 5 glaciation’s scenario, like the southern Black Forest in
Germany.
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