In the past decade, particularly since the last summary of the
subject (Calvet, 2004), the Quaternary glaciation of the Pyrenees
has been the focus of new research. Unequal progress
has been achieved on three aspects: mapping the extent of
the Pyrenean ice field, quantifying the geomorphological
impact of glaciation on the preglacial landscape and refining
the chronology of the glacial fluctuations.
Rockglaciers genesis and growth in a degrading mountaincryosphere (Southern French Alps). Presented by Monique Fort at the "Perth II: Global Change and the World's Mountains" conference in Perth, Scotland in September 2010.
Subglacial drainage in porous aquifer and sediment consolidation patterns in the glaciated valley of Andorra (Pyrenees). The poster was presented for the IAG/AIG (International Association of Geomorphologists) Regional Conference on Geomorphology Geodiversity of polar landforms which was held in Longyearbyen (Spitsbergen, Norway) on August 1-5, 2007. Conference was organised on the occasion of the International Polar Year 2007/2008 by the Association of Polish Geomorphologists.
The study of sequence stratigraphy and sedimentary system in Muglad Basiniosrjce
Application of sequence stratigraphy theory, by levels of base level cycle sequence feature analysis,
combined with core and log data, establish the sequence stratigraphic framework. The Cretaceous sedimentary
strata are divided into six two sequences and 14 third-order sequences. In sequence stratigraphy based,
combine well logging, seismic and core observation, and comprehensive analysis of each well rock type, color,
bedding and other construction phase marks. Identify the Cretaceous strata have delta, meandering fluvial
facies and braided river with three main facies. Detailed study of Cretaceous sedimentary characteristics,
identify each sedimentary microfacies, sedimentary facies sequence established in the region
Rockglaciers genesis and growth in a degrading mountaincryosphere (Southern French Alps). Presented by Monique Fort at the "Perth II: Global Change and the World's Mountains" conference in Perth, Scotland in September 2010.
Subglacial drainage in porous aquifer and sediment consolidation patterns in the glaciated valley of Andorra (Pyrenees). The poster was presented for the IAG/AIG (International Association of Geomorphologists) Regional Conference on Geomorphology Geodiversity of polar landforms which was held in Longyearbyen (Spitsbergen, Norway) on August 1-5, 2007. Conference was organised on the occasion of the International Polar Year 2007/2008 by the Association of Polish Geomorphologists.
The study of sequence stratigraphy and sedimentary system in Muglad Basiniosrjce
Application of sequence stratigraphy theory, by levels of base level cycle sequence feature analysis,
combined with core and log data, establish the sequence stratigraphic framework. The Cretaceous sedimentary
strata are divided into six two sequences and 14 third-order sequences. In sequence stratigraphy based,
combine well logging, seismic and core observation, and comprehensive analysis of each well rock type, color,
bedding and other construction phase marks. Identify the Cretaceous strata have delta, meandering fluvial
facies and braided river with three main facies. Detailed study of Cretaceous sedimentary characteristics,
identify each sedimentary microfacies, sedimentary facies sequence established in the region
The Neoproterozoic carbonate sequence on the southeastern border of the Amazon Craton is divided into three lithostratigraphic units: a basal
cap dolomite, an intermediate limestone, limestone-mudstone unit, and an upper dolarenite-dolorudite unit. Sections of the cap-carbonate were
measured from the inner shelf to the outer shelf. Carbon isotope ratios (relative to PDB) vary between − 10.5 and − 1.7‰ in cap dolomite, and
between − 5.4 and +0.1‰ in laminated limestone and mud-limestone. Limestones and mud-limestones exhibit 87Sr/86Sr ratios ranging from
0.70740 to 0.70780. A comparative isotope stratigraphy between the inner-shelf and the middle-shelf basin shows differences in carbon isotope
ratios: The cap dolomite and limestones have lower δ13C ratios on the border of the basin (inner shelf) than in the middle shelf of the basin. These
lower values can be related to shallower environmental conditions and to a stronger influence of the continental border. The 87Sr/86Sr ratios are the
same in both areas, and are consistent with seawater composition at around 600 Ma.
-Examined features ranging from valley systems in Margaritifer Sinus to inverted topography in Aeolis/Zephyria Plana
-Studied and analyzed MOLA, THEMIS-VIS, OMEGA, MOC, CRISM, HRSC, and CTX imagery
GEOLOGY OF SURINAME GOLD RUSH
https://www.researchgate.net/publication/288865395_An_explanation_to_the_geology_of_Suriname
An explanation to the geology of Suriname
October 1984
W. BosmaSalomon B. KroonenbergSalomon B. KroonenbergR.V. Van Lissa
Emond de roever
https://www.researchgate.net/publication/40160365_An_explanation_to_the_geological_map_of_Suriname
An explanation to the geological map of Suriname
January 1984
W. BosmaSalomon B. KroonenbergSalomon B. KroonenbergCissa Emond de roever
https://www.researchgate.net/publication/40160518_Igneous_and_metamorphic_complexes_of_the_GuianaShield_in_Surinam
Igneous and metamorphic complexes of the GuianaShield in Surinam
January 1983
W. BosmaSalomon B. KroonenbergSalomon B. KroonenbergK. Maas Emond de roever
https://www.youtube.com/watch?v=yJu3tat9Po4
https://www.youtube.com/watch?v=bTy87BUQyfY
https://www.facebook.com/TheMoykes/posts/10216156904223265
https://en.wikipedia.org/wiki/Suriname
https://www.vice.com/en_us/article/ppxwz9/digging-into-surinames-massive-gold-industry
An Integrated Approach to the Exploration of Fractured Reservoirs: A Challeng...Mario Prince
This is an integrated analysis of the La Luna Formation in the Chuira pop-up structure, located in the Middle Magdalena Basin (MMVB). A structural trap originally mapped with 2D seismic and later with a 3D seismic volume, was interpreted using a conventional time structure maps and depth conversion methods. In 2009, the first well drilled a sequence of calcareous rocks which produce oil in stable natural flow but with a low rate. In order to understand this potential discovery, multidisciplinary studies were conducted including a detailed geology of the La Luna Formation information from outcrops, the integration of seismic attributes, log analysis, and an exhaustive reservoir research from existing samples.
Clues of a sedimentological model for some oolite reservoirs (example of the ...Prof. Bruno R.C. Granier
Presented on March 17, 1993, on the occasion of the Petroleum Group's meeting: "Carbonate petroleum reservoirs: Models for exploration and development"
The Neoproterozoic carbonate sequence on the southeastern border of the Amazon Craton is divided into three lithostratigraphic units: a basal
cap dolomite, an intermediate limestone, limestone-mudstone unit, and an upper dolarenite-dolorudite unit. Sections of the cap-carbonate were
measured from the inner shelf to the outer shelf. Carbon isotope ratios (relative to PDB) vary between − 10.5 and − 1.7‰ in cap dolomite, and
between − 5.4 and +0.1‰ in laminated limestone and mud-limestone. Limestones and mud-limestones exhibit 87Sr/86Sr ratios ranging from
0.70740 to 0.70780. A comparative isotope stratigraphy between the inner-shelf and the middle-shelf basin shows differences in carbon isotope
ratios: The cap dolomite and limestones have lower δ13C ratios on the border of the basin (inner shelf) than in the middle shelf of the basin. These
lower values can be related to shallower environmental conditions and to a stronger influence of the continental border. The 87Sr/86Sr ratios are the
same in both areas, and are consistent with seawater composition at around 600 Ma.
-Examined features ranging from valley systems in Margaritifer Sinus to inverted topography in Aeolis/Zephyria Plana
-Studied and analyzed MOLA, THEMIS-VIS, OMEGA, MOC, CRISM, HRSC, and CTX imagery
GEOLOGY OF SURINAME GOLD RUSH
https://www.researchgate.net/publication/288865395_An_explanation_to_the_geology_of_Suriname
An explanation to the geology of Suriname
October 1984
W. BosmaSalomon B. KroonenbergSalomon B. KroonenbergR.V. Van Lissa
Emond de roever
https://www.researchgate.net/publication/40160365_An_explanation_to_the_geological_map_of_Suriname
An explanation to the geological map of Suriname
January 1984
W. BosmaSalomon B. KroonenbergSalomon B. KroonenbergCissa Emond de roever
https://www.researchgate.net/publication/40160518_Igneous_and_metamorphic_complexes_of_the_GuianaShield_in_Surinam
Igneous and metamorphic complexes of the GuianaShield in Surinam
January 1983
W. BosmaSalomon B. KroonenbergSalomon B. KroonenbergK. Maas Emond de roever
https://www.youtube.com/watch?v=yJu3tat9Po4
https://www.youtube.com/watch?v=bTy87BUQyfY
https://www.facebook.com/TheMoykes/posts/10216156904223265
https://en.wikipedia.org/wiki/Suriname
https://www.vice.com/en_us/article/ppxwz9/digging-into-surinames-massive-gold-industry
An Integrated Approach to the Exploration of Fractured Reservoirs: A Challeng...Mario Prince
This is an integrated analysis of the La Luna Formation in the Chuira pop-up structure, located in the Middle Magdalena Basin (MMVB). A structural trap originally mapped with 2D seismic and later with a 3D seismic volume, was interpreted using a conventional time structure maps and depth conversion methods. In 2009, the first well drilled a sequence of calcareous rocks which produce oil in stable natural flow but with a low rate. In order to understand this potential discovery, multidisciplinary studies were conducted including a detailed geology of the La Luna Formation information from outcrops, the integration of seismic attributes, log analysis, and an exhaustive reservoir research from existing samples.
Clues of a sedimentological model for some oolite reservoirs (example of the ...Prof. Bruno R.C. Granier
Presented on March 17, 1993, on the occasion of the Petroleum Group's meeting: "Carbonate petroleum reservoirs: Models for exploration and development"
The paper that caused a bit of debate as to whether tides affect deposition in the Carboniferous Pennine Basin. Prior to this there was some evidence, but it was refuted by the main players. The tidal deposits themselves occur in discrete zones - within the TST of wide valley fills, and in mouthbar systems deposited during stillstand/ early TST.
A brief explanation on Paleo Climate of Gondwana SuperGroup. By Nitish Namdeo MSc Final Government Science College, Jabalpur. Under Guidance of Dr. Sanjay Tignath.
This is just a simple effort of laying a background of slides for new presenters. You can download, edit and present the topic. I hope you find it a bit helpful.
A "spare wheel" talk* on the occasion of JK2018, the International Symposium around the Jurassic - Cretaceous Boundary
*: to replace a talk of a registered speaker who could not attend the meeting
Similar to Recent Advances in Research on Quaternary Glaciations in the Pyrenees (20)
MESURES DE REMEDIACIÓ AMBIENTAL CONTRA ELS FENOMENS EROSIUS HÍDRICS ASSOCIAT...Fundació Marcel Chevalier
Poster per a la sessió Kick off del projecte SOLPYR (Poctefa 2023-2027) celebrada a Tremp el 29 i 30 d'abril.
Breu descipció: Al Juliol de 2015 una gran tempesta (de T~100 anys) va provocar una forta erosió a capçalera de conca, originant laves torrencials (debris flow) que amb el sediment exposat, a partir de llavors, inclusiva amb precipitacions mínimes (> 15 mm), es provocava aturades de la potabilitzadora d'aigües superficials que alimenta a Les Escaldes (15.000 hab.). Calia controlar l’enterboliment de l’aigua superficial.
Palaeoenvironmental changes in the Iberian central system during the Late-glacial and Holocene as inferred from geochemical data: A case study of the Navamuño depression in western Spain
Former cold-wet ice polythermal glaciers inferred from erratics and moraine's Schmidt Hammer ages at the Madriu valley, Principality of Andorra (SE- Pyrenees)
Mid-Late Pleistocene glacial dynamics in the Valira valleys (Principality of ...Fundació Marcel Chevalier
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.
By classifying glacial phases of the northern Iberian Peninsula fringe, four common glacial phases arise for the last glacial cycle:
A) An early Glacial Cycle 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.
Mid-Late Pleistocene glacial dynamics in the Valira valleys (Principality of Andorra). Asymmetries within the Pyrenees and correlation across the westernmost European mountain ranges.
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 (Figure 6):
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 scenario, like the southern Black Forest in Germany.
The AD Cam-Clay project takes its name from the .ad, which identifies Andorra as a country on the Internet and Clay of a recognized constitutive model and widely used in the science of soil mechanics.
The description of the objectives is structured in three sections. Type of research to be developed and the research elements. Brief explanation of the research project and conceptual model. Tools of research to use and case study.
1st) Type of research to be developed:
This project aims to enter the field of fundamental research. The project aims to develop an explanatory and predictive mathematical model. The mathematical model is based on an existing conceptual model that can be improved according to seconds the results obtained in mathematical modeling.
1b) The subject of the research: The subject of the research is a material of a geological or geomaterial nature, widely known in the Principality and geologically called "Till". In the slang of the country this geomaterial is described as "Rock in formation" or "decompose rock" due to its hardness as well as its ability to generate landslides, failures in buildings, cracks in walls, or their ability to confine groundwater. The target geomaterial is a rock and not a rock. It corresponds to a sediment deformed by the old glacier of Andorra and which has a significant amount of untreated data, under the tutelage of the Marcel Chevalier Private Foundation.
Geomaterial behaves differently depending on how it has been previously deformed (with water or without), and the place in the valley where it has been deformed as well as the depth at which it has been deformed. Numerical data on the behavior of geomaterial are known from the results pressure testing. This type of test is standardized and makes it easy to compare results incl s between distant geographical areas.
2a) Summary explanation: The project aims to develop a model that explains the values of deformation, due to the so-called preconsolidation pressure, which is observed in glacial deposits by a given from the small Andorran glacier.
2b) Conceptual model:
The dynamics are related to an accumulation of sediment and acorns at the bottom of the valley of Andorra, accompanied by a flow of groundwater generated by the melting of the ice. This water flow generates a pressure difference between the upper parts of the glacier and the discharge point at its front. In this context, the sediment at the bottom of the valley is submerged within an effort field tangential, developed by the friction exerted by the base of the glacier in displacement.
Fòssils excepcionals que requereixen excavacions excepcionals. Geoterma Pirin...Fundació Marcel Chevalier
Troballa i extracció de dos fòssils excepcionals localitzats en zones amb un alt grau de degradació, una marca de pell deixada en unes argiles per un dinosaure sauròpode i un niu d’ous de dinosaure.
Accés a l'expliació: https://www.youtube.com/watch?v=tovbPrnHh38&feature=youtu.be
Homenatge al geòleg de la Universitat de Saragossa Carlos Sancho Marcén efectuat el 7 de novembre 2019 i organitzat per la facultat de Geologia d'aquesta universitat.
New luminescence dating from glaci-fluvial & glaci-lacustrine deposits from South-Central & SE Pyrenees (Noguera Ribargozana, Noguera Pallaresa, Valira & Carol)
Extracció de mostres de sòl de 3 perfils en un transsecte
Col·locació de 3 termòmetres amb datalogguer
Tractament de les mostres obtingudes per obtenir el %CO
Fitxes descriptives + SIG + memòria
Mapes d’isovalors (contingut en CO, variació del segrest de carboni respecte el nivell del 1997)
Objectius;
Generar informació sobre l’estat actual d’un important embornal de carboni, els sòls, i els canvis a què ha estat sotmès
Aprofitar l’estat zero establert en l’estudi del 1997 per realitzar ara un nou mostreig, repetible en el futur, veure la tendència i avaluar la capacitat de segrest de CO2 atmosfèric
Publicar els resultats per tal que aquest estudi es pugui repetir en el futur i es trobi accessible per tothom
LF Energy Webinar: Electrical Grid Modelling and Simulation Through PowSyBl -...DanBrown980551
Do you want to learn how to model and simulate an electrical network from scratch in under an hour?
Then welcome to this PowSyBl workshop, hosted by Rte, the French Transmission System Operator (TSO)!
During the webinar, you will discover the PowSyBl ecosystem as well as handle and study an electrical network through an interactive Python notebook.
PowSyBl is an open source project hosted by LF Energy, which offers a comprehensive set of features for electrical grid modelling and simulation. Among other advanced features, PowSyBl provides:
- A fully editable and extendable library for grid component modelling;
- Visualization tools to display your network;
- Grid simulation tools, such as power flows, security analyses (with or without remedial actions) and sensitivity analyses;
The framework is mostly written in Java, with a Python binding so that Python developers can access PowSyBl functionalities as well.
What you will learn during the webinar:
- For beginners: discover PowSyBl's functionalities through a quick general presentation and the notebook, without needing any expert coding skills;
- For advanced developers: master the skills to efficiently apply PowSyBl functionalities to your real-world scenarios.
GraphSummit Singapore | The Art of the Possible with Graph - Q2 2024Neo4j
Neha Bajwa, Vice President of Product Marketing, Neo4j
Join us as we explore breakthrough innovations enabled by interconnected data and AI. Discover firsthand how organizations use relationships in data to uncover contextual insights and solve our most pressing challenges – from optimizing supply chains, detecting fraud, and improving customer experiences to accelerating drug discoveries.
DevOps and Testing slides at DASA ConnectKari Kakkonen
My and Rik Marselis slides at 30.5.2024 DASA Connect conference. We discuss about what is testing, then what is agile testing and finally what is Testing in DevOps. Finally we had lovely workshop with the participants trying to find out different ways to think about quality and testing in different parts of the DevOps infinity loop.
Sudheer Mechineni, Head of Application Frameworks, Standard Chartered Bank
Discover how Standard Chartered Bank harnessed the power of Neo4j to transform complex data access challenges into a dynamic, scalable graph database solution. This keynote will cover their journey from initial adoption to deploying a fully automated, enterprise-grade causal cluster, highlighting key strategies for modelling organisational changes and ensuring robust disaster recovery. Learn how these innovations have not only enhanced Standard Chartered Bank’s data infrastructure but also positioned them as pioneers in the banking sector’s adoption of graph technology.
Alt. GDG Cloud Southlake #33: Boule & Rebala: Effective AppSec in SDLC using ...James Anderson
Effective Application Security in Software Delivery lifecycle using Deployment Firewall and DBOM
The modern software delivery process (or the CI/CD process) includes many tools, distributed teams, open-source code, and cloud platforms. Constant focus on speed to release software to market, along with the traditional slow and manual security checks has caused gaps in continuous security as an important piece in the software supply chain. Today organizations feel more susceptible to external and internal cyber threats due to the vast attack surface in their applications supply chain and the lack of end-to-end governance and risk management.
The software team must secure its software delivery process to avoid vulnerability and security breaches. This needs to be achieved with existing tool chains and without extensive rework of the delivery processes. This talk will present strategies and techniques for providing visibility into the true risk of the existing vulnerabilities, preventing the introduction of security issues in the software, resolving vulnerabilities in production environments quickly, and capturing the deployment bill of materials (DBOM).
Speakers:
Bob Boule
Robert Boule is a technology enthusiast with PASSION for technology and making things work along with a knack for helping others understand how things work. He comes with around 20 years of solution engineering experience in application security, software continuous delivery, and SaaS platforms. He is known for his dynamic presentations in CI/CD and application security integrated in software delivery lifecycle.
Gopinath Rebala
Gopinath Rebala is the CTO of OpsMx, where he has overall responsibility for the machine learning and data processing architectures for Secure Software Delivery. Gopi also has a strong connection with our customers, leading design and architecture for strategic implementations. Gopi is a frequent speaker and well-known leader in continuous delivery and integrating security into software delivery.
GDG Cloud Southlake #33: Boule & Rebala: Effective AppSec in SDLC using Deplo...James Anderson
Effective Application Security in Software Delivery lifecycle using Deployment Firewall and DBOM
The modern software delivery process (or the CI/CD process) includes many tools, distributed teams, open-source code, and cloud platforms. Constant focus on speed to release software to market, along with the traditional slow and manual security checks has caused gaps in continuous security as an important piece in the software supply chain. Today organizations feel more susceptible to external and internal cyber threats due to the vast attack surface in their applications supply chain and the lack of end-to-end governance and risk management.
The software team must secure its software delivery process to avoid vulnerability and security breaches. This needs to be achieved with existing tool chains and without extensive rework of the delivery processes. This talk will present strategies and techniques for providing visibility into the true risk of the existing vulnerabilities, preventing the introduction of security issues in the software, resolving vulnerabilities in production environments quickly, and capturing the deployment bill of materials (DBOM).
Speakers:
Bob Boule
Robert Boule is a technology enthusiast with PASSION for technology and making things work along with a knack for helping others understand how things work. He comes with around 20 years of solution engineering experience in application security, software continuous delivery, and SaaS platforms. He is known for his dynamic presentations in CI/CD and application security integrated in software delivery lifecycle.
Gopinath Rebala
Gopinath Rebala is the CTO of OpsMx, where he has overall responsibility for the machine learning and data processing architectures for Secure Software Delivery. Gopi also has a strong connection with our customers, leading design and architecture for strategic implementations. Gopi is a frequent speaker and well-known leader in continuous delivery and integrating security into software delivery.
Removing Uninteresting Bytes in Software FuzzingAftab Hussain
Imagine a world where software fuzzing, the process of mutating bytes in test seeds to uncover hidden and erroneous program behaviors, becomes faster and more effective. A lot depends on the initial seeds, which can significantly dictate the trajectory of a fuzzing campaign, particularly in terms of how long it takes to uncover interesting behaviour in your code. We introduce DIAR, a technique designed to speedup fuzzing campaigns by pinpointing and eliminating those uninteresting bytes in the seeds. Picture this: instead of wasting valuable resources on meaningless mutations in large, bloated seeds, DIAR removes the unnecessary bytes, streamlining the entire process.
In this work, we equipped AFL, a popular fuzzer, with DIAR and examined two critical Linux libraries -- Libxml's xmllint, a tool for parsing xml documents, and Binutil's readelf, an essential debugging and security analysis command-line tool used to display detailed information about ELF (Executable and Linkable Format). Our preliminary results show that AFL+DIAR does not only discover new paths more quickly but also achieves higher coverage overall. This work thus showcases how starting with lean and optimized seeds can lead to faster, more comprehensive fuzzing campaigns -- and DIAR helps you find such seeds.
- These are slides of the talk given at IEEE International Conference on Software Testing Verification and Validation Workshop, ICSTW 2022.
The Art of the Pitch: WordPress Relationships and SalesLaura Byrne
Clients don’t know what they don’t know. What web solutions are right for them? How does WordPress come into the picture? How do you make sure you understand scope and timeline? What do you do if sometime changes?
All these questions and more will be explored as we talk about matching clients’ needs with what your agency offers without pulling teeth or pulling your hair out. Practical tips, and strategies for successful relationship building that leads to closing the deal.
Pushing the limits of ePRTC: 100ns holdover for 100 daysAdtran
At WSTS 2024, Alon Stern explored the topic of parametric holdover and explained how recent research findings can be implemented in real-world PNT networks to achieve 100 nanoseconds of accuracy for up to 100 days.
UiPath Test Automation using UiPath Test Suite series, part 6DianaGray10
Welcome to UiPath Test Automation using UiPath Test Suite series part 6. In this session, we will cover Test Automation with generative AI and Open AI.
UiPath Test Automation with generative AI and Open AI webinar offers an in-depth exploration of leveraging cutting-edge technologies for test automation within the UiPath platform. Attendees will delve into the integration of generative AI, a test automation solution, with Open AI advanced natural language processing capabilities.
Throughout the session, participants will discover how this synergy empowers testers to automate repetitive tasks, enhance testing accuracy, and expedite the software testing life cycle. Topics covered include the seamless integration process, practical use cases, and the benefits of harnessing AI-driven automation for UiPath testing initiatives. By attending this webinar, testers, and automation professionals can gain valuable insights into harnessing the power of AI to optimize their test automation workflows within the UiPath ecosystem, ultimately driving efficiency and quality in software development processes.
What will you get from this session?
1. Insights into integrating generative AI.
2. Understanding how this integration enhances test automation within the UiPath platform
3. Practical demonstrations
4. Exploration of real-world use cases illustrating the benefits of AI-driven test automation for UiPath
Topics covered:
What is generative AI
Test Automation with generative AI and Open AI.
UiPath integration with generative AI
Speaker:
Deepak Rai, Automation Practice Lead, Boundaryless Group and UiPath MVP
Encryption in Microsoft 365 - ExpertsLive Netherlands 2024Albert Hoitingh
In this session I delve into the encryption technology used in Microsoft 365 and Microsoft Purview. Including the concepts of Customer Key and Double Key Encryption.
A tale of scale & speed: How the US Navy is enabling software delivery from l...sonjaschweigert1
Rapid and secure feature delivery is a goal across every application team and every branch of the DoD. The Navy’s DevSecOps platform, Party Barge, has achieved:
- Reduction in onboarding time from 5 weeks to 1 day
- Improved developer experience and productivity through actionable findings and reduction of false positives
- Maintenance of superior security standards and inherent policy enforcement with Authorization to Operate (ATO)
Development teams can ship efficiently and ensure applications are cyber ready for Navy Authorizing Officials (AOs). In this webinar, Sigma Defense and Anchore will give attendees a look behind the scenes and demo secure pipeline automation and security artifacts that speed up application ATO and time to production.
We will cover:
- How to remove silos in DevSecOps
- How to build efficient development pipeline roles and component templates
- How to deliver security artifacts that matter for ATO’s (SBOMs, vulnerability reports, and policy evidence)
- How to streamline operations with automated policy checks on container images
Epistemic Interaction - tuning interfaces to provide information for AI supportAlan Dix
Paper presented at SYNERGY workshop at AVI 2024, Genoa, Italy. 3rd June 2024
https://alandix.com/academic/papers/synergy2024-epistemic/
As machine learning integrates deeper into human-computer interactions, the concept of epistemic interaction emerges, aiming to refine these interactions to enhance system adaptability. This approach encourages minor, intentional adjustments in user behaviour to enrich the data available for system learning. This paper introduces epistemic interaction within the context of human-system communication, illustrating how deliberate interaction design can improve system understanding and adaptation. Through concrete examples, we demonstrate the potential of epistemic interaction to significantly advance human-computer interaction by leveraging intuitive human communication strategies to inform system design and functionality, offering a novel pathway for enriching user-system engagements.
2. Author's personal copy
Chapter 11
Recent Advances in Research on
Quaternary Glaciations in the Pyrenees
Marc Calvet1,*, Magali Delmas1, Yanni Gunnell2, Regis Braucher3 and Didier Bourles3
´ `
1
´di-Terra, Universite de Perpignan-Via Domitia, 52 Avenue Paul Alduy, F 66860 Perpignan cedex, France
JE 2522 Me ´
2
´
UMR 5600 CNRS, Universite Lumie `re-Lyon 2, 5 avenue Pierre Mende
`s-France, 69676 Bron cedex, France
3
´,
UMR 6635 CNRS, Aix Marseille Universite BP 80, 13545 Aix-en-Provence cedex 04, France
*Correspondence and requests for materials should be addressed to Marc Calvet. E-mail: calvet@univ-perp.fr
11.1. INTRODUCTION of ice extent is only available for the eastern part of the
`
range, the Ariege catchment included. The synthesis by
In the past decade, particularly since the last summary of the Calvet (2004), who following the minimalist views of Tail-
subject (Calvet, 2004), the Quaternary glaciation of the Pyr- lefer (1985), at the time underestimated the extent of the
enees has been the focus of new research. Unequal progress ¨
Wurmian ice field, has been significantly revised
has been achieved on three aspects: mapping the extent of (Fig. 11.1). Further west, uncertainty remains concerning
the Pyrenean ice field, quantifying the geomorphological ¨
the termini of Wurmian glaciers in the Salat and Gave
impact of glaciation on the preglacial landscape and refin- d’Oloron catchments; for the last valley, the outermost gla-
ing the chronology of the glacial fluctuations. cial deposit has been described at Escot, but there is also a
Mapping of ice extent has benefited from only minor presumption that ice advance might have extended some
updates. A relatively accurate 1:100,000-scale illustration 10 km further out onto the piedmont (Gangloff et al.,
FIGURE 11.1 The Pleistocene glaciation of the Pyrenees: a cartographic synthesis. 1: Glacierised areas, a: during the Wurmian; b: during the Middle
¨
Pleistocene. 2: Main supraglacial mountain ridges and ice-catchment limits; main ice routes. 3: Possible extent of Pleistocene valley glaciers. 4: Main
transfluence cols. 5: Currently glacierised massifs containing small, residual cirque glaciers. The map is modified and updated after Calvet (2004). Note
the location of other figures mentioned in the text.
Developments in Quaternary Science. Vol. 15, doi: 10.1016/B978-0-444-53447-7.00011-8
ISSN: 1571-0866, # 2011 Elsevier B.V. All rights reserved. 127
3. Author's personal copy
128 Quaternary Glaciations-Extent and Chronology
1991). Both for small, transverse valleys and for the main 11.2. MIDDLE PLEISTOCENE GLACIATIONS
valleys, such as the Noguera Pallaresa or the Valira, the ter-
minal position of the glacier systems is also uncertain in ¨
Glaciations pre-dating the Wurmian Stage remain poorly
Spain. Work by Serrat et al. (1994) and Turu i Michels documented. Neither their number nor their spatial extent
˜ ´
and Pena Monne (2006) has claimed that these glacial ter- and precise time of formation are well established. This
mini extended ca. 10 km further than thus far accepted. This is partially ascribable to the fact that these older glaciers
is in spite of the fact that the valley cross-sections in these did not advance much further out of the crest zone than
areas are V-shaped and sometimes exhibit entrenched ¨
those during the subsequent Wurmian. It is possible that
meanders. Further, glacial landforms are either scarce or ¨
they exceeded the Wurmian maximum by 1.5 km in the
absent, and the interpretation of existing Pleistocene Carol (or Querol) valley and by 5–10 km in the case of
deposits is inconclusive. `
the Ariege glacier. Further, the last glaciation has often bur-
The impact of glacial erosion on the landscape has been ied, destroyed or reworked pre-existing older deposits.
measured through a combination of approaches: (i) qualita-
tive approaches have endeavoured to list and map all pre-
and interglacial landforms and deposits. These features
11.2.1. On the South Side of the Range
are so well preserved in some places that they necessarily The Carol catchment exhibits among the best-preserved
imply extremely limited depths of Pleistocene erosion by glacial deposit sequences of the Pyrenees (Fig. 11.2). It con-
glaciers. Relevant markers of limited glacial erosion are tains three generations of frontal and lateral moraines, each
thick weathered mantles preserved beneath glacial till or grading to the tread of a glaciofluvial terrace. Clast assem-
ice-marginal deposits, and relict erosion surfaces the Neo- blages in each terrace show distinctive weathering charac-
gene age of which have been confirmed by apatite fission- teristics. Although relative dating of these moraines would
track and (U–Th)/He dating (Gunnell et al., 2009). (ii) have suggested an age sequence bridging the Middle and
Quantitative approaches have produced mass-balance stud- Late Pleistocene, 10Be dating has provided ages of 65 ka
ies that exploit the well-preserved glacial sediment reposi- or less, suggesting that all three moraine units formed dur-
tory situated on the southern side of the Carlit massif. Based ¨
ing the Wurmian Stage (Delmas, 2009). Such a young age
on research by Delmas et al. (2009), catchment-scale glacial for deeply weathered glacial and glaciofluvial materials is
erosion depths have been estimated to have not exceeded deceptive. It suggests that the erratic boulders, sampled
5 m during the last glacial cycle. Cirque morphometry in for CRN dating, have lost significant mass through post-
Aragon (n ¼ 206; Garcıa-Ruiz et al., 2000) and in the Carlit
´ depositional rind weathering and grus formation, hence pro-
and Ariege catchments (n ¼ 1066; Delmas, 2009) has also
` viding younger than expected exposure ages. Alternatively,
provided some insight into spatial variations in erosional it implies that those same erratic boulders were embedded
intensity. However, the overwhelming conclusion is that in the moraine and have undergone post-depositional exhu-
bedrock lithology and structure are the strongest controls mation. In either case, this could explain the relatively uni-
on cirque morphology: neither climatic criteria nor the form age cluster obtained for the Carol moraines.
duration of glacier presence (estimated on the basis of cir- ´
The Gallego catchment (Fig. 11.3) has provided a puz-
que floor elevation) have provided clear-cut regional pat- ˜
zling series of OSL ages (Pena et al., 2004; Lewis et al.,
terns. Overall, even where glacial landforms pervade the ¨
2009). The large frontal moraine at Senegue was until
crest zone and convey a distinctly alpine character to the ¨
now held to represent the Wurmian glacial maximum, but
mountain scenery (Calvet et al., 2008), evidence points to moraines at Aurin, situated 2 km further down-valley, have
a relatively limited morphological imprint of glaciation yielded contrasting ages of 38 and 85 ka. They have there-
on the pre-Quaternary Pyrenean landscape. ¨
fore also been attributed to the Wurmian. Meanwhile, the
Most progress devoted to understanding Pyrenean uppermost glaciofluvial terrace deposits, Qt 5, at Sabina- ˜
Quaternary landscape evolution has been achieved through nigo, which contains glacially striated pebbles and corre-
constraining the chronology of glaciation, and particularly lates stratigraphically with terrace T2 deposits in other
¨
the last Pleistocene glacial cycle (Wurmian Stage). This is valleys in the eastern Pyrenees (Calvet, 1996), have pro-
due to the surge of in situ-produced cosmogenic radio- vided not only two ages, 155 and 156 ka, which are attrib-
nuclide (CRN) dating of glacial landforms, together with utable to marine isotope stage 6 (MIS 6; i.e. late Rissian),
optically stimulated luminescence (OSL) dating of glacio- but also two much younger ages (99 and 84 ka).
fluvial outwash deposits, and of the cross-correlation of ˜
The Valira catchment (Turu i Michels and Pena Monne, ´
these new data with existing radiocarbon ages of ice- 2006; Turu i Michels et al., 2007; Turu i Michels, 2009) is
marginal sediments. It is supported by palynological inves- reported to contain an Eemian-age sediment fill, discovered
tigations and by morphostratigraphical studies of glacial during drilling in the central valley of Andorra. Here, deeply
deposit sequences. These aspects are the main focus of this weathered moraine deposits, attributable to MIS 6, are also
review. exposed at Sant Julia de Loria and connect down-valley with
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Chapter 11 Recent Advances in Research on Quaternary Glaciations in the Pyrenees 129
FIGURE 11.2 Terminal sequence of glacier
deposits in the Carol catchment: age of frontal
¨
and lateral Wurmian moraines. 1: Pliocene or
early Pleistocene alluvium capping erosional sur-
faces. 2: Proglacial alluvial sheet (T4), deeply
weathered. 3: Alluvial sheet (T3). 4: Proglacial
alluvial sheet (T2), weathered. 5: Proglacial allu-
vial sheet (T1), poorly weathered or unweathered.
¨
6: Ice-marginal sediments. 7: Wurmian till with
crested moraines; materials poorly weathered. 8:
Middle Pleistocene (MIS 6) till with physically
degraded moraines, connected to T2; materials
weathered. 9: Till with highly degraded moraines,
connected to T4 (perhaps MIS 12 or MIS 16);
materials deeply weathered. 10 : 10Be-dated sites;
note age dispersion on the more weathered
moraines. The map is after Calvet (1996, 2004),
with the geochronological data taken from
Delmas (2009).
a proglacial alluvial sheet which has yielded an OSL date of young CRN ages obtained from erratic boulders preserved on
125 ka. A much older ice front position is also reported ca. the valley slopes high above the poorly weathered and well-
10 km further down-valley at Calvinya. This gives an age ¨
preserved lateral moraines of Wurmian age (Delmas, 2009;
that is older than 350 ka (the OSL detection limit). However, Delmas et al., 2011). As in the Carol valley, the boulders also
inspection of exposed sections reveals only very rare striated show signs of post-depositional weathering, of displacement
cobbles, and sedimentological features were indicative of along fractures and even of taffoni development. Following
fluvial rather than of glacial deposition. the methodological recommendations of Putkonen and
Swanson (2003), out of the sampled population, the oldest
10
Be age was considered to be the most accurate, providing
11.2.2. On the North Side of the Range:
a resulting age of 122 ka for the deposits near Caraybat
`
Focus on the Ariege Catchment (Fig. 11.4).
`
The Ariege moraine sequence (Fig. 11.4) has raised the same Further insight into the Middle Pleistocene glaciations
issues as those in the Carol catchment, namely anomalously has been gained by examining the relative altitudes of glacial
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130 Quaternary Glaciations-Extent and Chronology
FIGURE 11.3 Age-bracketed terminal sequence
´
of glacier deposits in the Gallego catchment. 1:
High-relief landforms, razorback and hogback
ˆ
ridges. 2: aretes. 3: Tread of highest alluvial
deposits (coronas). 4: Proglacial alluvial sheets
and mantled wash pediments (weathered and rubi-
fied: Qt 5, alias T2). 5: Proglacial alluvial sheets
¨
(poorly weathered: Qt 6-7-8, alias T1). 6: Wurmian
ice-contact sedimentary units (lacustrine or flu-
vial). 7: Moraine ridges and till deposits. 8: Scoured
rock surfaces on bedrock steps. 9: Successive
¨
Wurmian ice front positions. 10: Middle Pleisto-
cene (MIS 6) ice fronts. 11: OSL and 14C-dated
sites. After the geomorphological map by Barrere `
˜
(1966) and data by Pena et al. (2004), Lewis et al.
(2009) and Jalut et al. (1992).
deposits, the advanced weathering state of which indicates even of different glacial cycles: (i) in the Tarascon basin
¨
that they are older than Wurmian. This approach has allowed `
and in the higher Ariege catchment, glacial evidence from
differentiation between generations of deposits that are leg- MIS 6 occurs as trails of weathered till deposits and erratic
acies of different stadial events within MIS 6, or perhaps boulders situated ca. 50–100 m higher than Wurmian ¨
6. Author's personal copy
FIGURE 11.4 Pleistocene glaciation in the Ariege catchment. 1: Razorback and hogback scarps in Mesozoic or Cenozoic limestone, sandstone or con-
`
glomerates of the outer Pyrenean fold belt. 2: Relict Pliocene to early Pleistocene alluvial fan deposits (formation du Lannemezan). 3: Higher alluvial
terrace T4, severely eroded. 4: Intermediate terrace, intensely weathered and rubified (Haute Boulbonne). 5: Lower terraces (generation T2), weathered
¨
and rubified (Basse Boulbonne, Vernajoul and ice-marginal terraces of Antras and Foix–Cadirac). 6: Lowermost terrace T1, of Wurmian age, unweathered
and capped by brown soils. 7: Middle Pleistocene ice boundaries; a: probable MIS 6 ice limits, grading to the T2 terraces; b: erratic boulders or residual
¨
morainic deposits dating to MIS 6 or older. 8: Wurmian maximum ice extent; the corresponding population of unweathered moraines grades to the T1
`
alluvial sheets. 9: MIS 2 ice boundaries, that is, Garrabet stadial. 10: Recessional moraines at Bompas–Arignac and Berniere (19–20 ka). 11: Recessional
`
moraines (Petches and Freychinede) dating to the Oldest Dryas. 12: Position of dated sites. Distribution of glaciofluvial deposits in the piedmont zone,
based on Hubschman (1975, 1984) and on the geological map of the Pyrenees Quaternary by Barrere et al. (2009). The ice limits and 10Be data are after
`
Delmas (2009) and the 14C ages after Jalut et al. (1982, 1992).
7. Author's personal copy
132 Quaternary Glaciations-Extent and Chronology
maximum glacial moraines. In the Foix–Montgaillard basin, 11.3. THE LAST PLEISTOCENE GLACIAL
the Antras ice-contact depositional sequence and the ice- ¨
CYCLE (WURMIAN STAGE)
`
marginal sediment body at Becq-en-Barguillere (Taillefer,
1973) represent two additional sites to which the MIS 6 max- The chronology of the Pyrenean last glacial cycle, corre-
imum ice extent can be tethered. Given these new interpre- ¨
lated with the Wurmian Stage of the Alps by most Pyrenean
tations, the ice-marginal meltwater terrace sequence at Foix– authors, has been mostly based on a large set of 14C ages
Cadirac was ascribed by Hubschman (1975, 1984) to the Ris- produced over the past 30 years, supplemented in the last
sian. This was because of the advanced state of weathering of five mostly by new 10Be and OSL ages. The image of the
its debris. However, it occurs at a lower elevation than the ¨
Wurmian chronology provided by this body of evidence
Becq and other MIS 6 benchmarks and could instead repre- is still incomplete, with contradictions between the methods
sent the legacy of a deglacial event that occurred toward the employed giving sometimes puzzling contrasts between
`
end of the MIS 6 cycle. Further down the Ariege valley, the adjacent valleys. Radiocarbon dating is usually indirect in
Foix–Cadirac terrace grades to the Basse Boulbonne (T2) that it provides an age for proglacial or ice-marginal organic
`
alluvial sheet. T2 (mapped by Barrere et al., 2009) is capped sediments whose relation to adjacent moraines is not always
by rubified soils displaying a depleted upper horizon. Char- straightforward. Even though a few terminal moraines have
acteristically evolved soils, such as this, suggest an episode been dated directly, most OSL dating raises similar prob-
of weathering and eluviation during the Eemian Stage lems. This is because sampling strategies target alluvial
(MIS 5e) climatic optimum. (ii) Erratic boulders sourced sheets that are sometimes situated several tens of kilometres
by the granitic and gneissic Aston massif have been found from the nearest ice front deposits. CRN dating, in contrast,
resting on the Mesozoic limestone and shale outcrops at Car- systematically allows direct dating of glacial landforms,
aybat, down-valley from the Antras delta and 50 m above it. whether moraines, isolated erratic boulders or ice-scoured
This boulder trail was produced by one or several ancient gla- bedrock steps. However, CRN exposure ages are, by defi-
ciers of corresponding thickness and has been tentatively cor- nition, minimum ages, with the precautions this limitation
related with elevated moraine deposits on the outer flanks of inevitably brings upon interpretation of the data.
´ ´
the Arize massif and in the Tarascon basin at Quemenailles
`
and Menties. In their lower reaches, these ice masses may
have extended as far as Pech de Varilles, at the proximal edge ¨
11.3.1. The Age of Wurmian Maximum Ice
of the Pamiers plain. At Pech de Varilles, Faucher (1937) Extent: In or Out of Phase with the Global Last
reported erratic boulders of gneiss exceeding 6 m in diame-
Glacial Maximum?
ter, sourced from the Aston massif. He hypothesised that they
were of glacial origin. However, other geologists later either The mid-latitude Pyrenean mountain range is under direct
argued that the boulders had been supplied from the under- influence of the North Atlantic weather systems. This
lying Eocene conglomerate bedrock or else ascribed them to makes the Pyrenees an ideal setting for testing whether or
unconformable Pliocene fan deposits that excavated the not mid-latitude mountain glaciation and global climatic
Eocene conglomerate and locally contain greater than 1 m- fluctuations were synchronous (Gillespie and Molnar,
sized quartzite boulders. Nevertheless, the boulders 1995; Hughes and Woodward, 2008; Thackray et al.,
described by Faucher are conspicuous by their petrography ¨
2008). The now classic view that the Wurmian Pyrenean
and provenance, by their large size, and by their extremely maximum ice extent and the global last glacial maximum
limited weathering state. They occur ca. 460 m a.s.l., that (LGM-defined as the time period between 23 and 19 ka
is, 90 m above the tread of the deeply weathered Haute Boul- cal. BP, Mix et al., 2001) did not occur simultaneously
bonne (T3) terrace, which occupies the opposite bank of the was presented in the 1980s on the basis of radiocarbon ages
`
Ariege river in the same area (Calvet, unpublished). These obtained on ice-contact lake sediments on the north side of
indications imply that this elevated erratic boulder trail is the range (Andrieu et al., 1988; Jalut et al., 1988, 1992;
of early Middle Pleistocene age and correlates, as in the Andrieu, 1991; detailed synthesis in Delmas, 2009,
Carol valley, with the older alluvial terrace T4 deposits. This pp. 96–109). This radiocarbon-based perspective on
topographical position suggests that the erratics at Pech de ¨
Pyrenean glaciation advocated a Wurmian maximum ice
Varilles are comparable to the ancient moraine deposits that extent between 70 and 50 ka. After this time, the glaciers
occur much further west at Arudy. The latter also occur at stagnated slightly up-valley from their maximal advance
elevations similar to those of the relict Pliocene to early positions before retreating to the uppermost reaches ca.
Pleistocene piedmont deposits of the Gave d’Oloron catch- 29–25 ka, depending on sites. To explain the recessional state
´
ment (Hetu and Gangloff, 1989). CRN dating was not of the Pyrenean ice cap by the time of the global LGM (which
attempted on the Pech de Varilles erratics because field evi- is broadly correlable to MIS 2), it has been argued that cli-
dence indicates that they have been exhumed from a finer matic conditions were too dry to sustain extensive ice fields
matrix and have been displaced by slope movements. on the Pyrenees. Although data are comparatively scarcer, a
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Chapter 11 Recent Advances in Research on Quaternary Glaciations in the Pyrenees 133
similar model has been proposed for the southern side of Amidst mounting uncertainty over radiocarbon ages of
the Pyrenees. In the Noguera Ribagorcana catchment
¸ ice-marginal materials, critics have begun to question the
(Fig. 11.5), the ice-marginal site of Llestui, interpreted asynchroneity of the Pyrenean glacial model. Basing their
¨
as marking a Wurmian post-maximum ice position, was reassessment on biostratigraphical and geochemical evi-
initially radiocarbon dated at 31–34 14C ka BP (Vilaplana, dence, palynologists in the late 1980s were first to challenge
1983). However, the samples were found to have been con- the view that Pyrenean glacier fluctuations were out of
taminated by inorganic carbon and later redated at 18–21 phase with the global LGM (Turner and Hannon, 1988;
14
C ka BP (Bordonau et al., 1993). For reasons of sus- Reille and Andrieu, 1995). The first CRN ages produced
pected sample contamination, the 30 14C ka BP radiocar- for glacial landforms in the Noguera Ribagorcana (Pallas
¸ `
bon age obtained from the Bassots palaeolake, which is et al., 2006) prompted a more systematic critique of radio-
ponded behind the terminal lobe of the Ribagorcana ¸ carbon ages from the Pyrenees, most of them being deemed
moraine, has also been discounted as unreliable (Bordonau unreliable and were rejected. The competing hypothesis of
i Ibern, 1992). ¨
synchroneity between the Wurmian maximum ice extent
and the global LGM was asserted. This was based on
10
Be ages of 18.1 Æ 1.9 ka obtained from a lateral moraine
of the Noguera Ribagorcana trunk glacier and 21.3 Æ 4.4 ka
¸
obtained from an erratic boulder close to the terminal lobe
(Fig. 11.5). These 10Be ages were revised to 19.2 Æ 2 of the
Noguera Ribagorcana trunk glacier and 22.6 Æ 4.7 ka,
¸
´ `
respectively, by Rodes (2008). Pallas et al. (2006) have nev-
ertheless not rejected the hypothesis that a relatively pro-
tracted ‘Pleniglacial’ might have prevailed between
before 30 ka and ca. 20 ka. This means that glacier snouts
may have been stationed far down the valleys not only dur-
ing the global LGM but also for quite some time before it.
The body of geochronological information available
today, however, provides evidence of a somewhat less static
history of glacier fluctuation, and consequently, a less seri-
ous antagonism between the in-phase and out-phase schools
of Pyrenean glaciation. The asynchroneity of maximum
advances of mountain and continental glaciers needs no
¨
longer to be challenged. The Wurmian maximum ice extent
now appears to have occurred everywhere quite early dur-
¨
ing the Wurmian Stage, irrespective of the dating methods
used to test this hypothesis. More controversial is the
relative position of ice fronts during the MIS 2 or more
accurately during the global LGM, either because of insuf-
ficient data or because of genuine variability between
valleys along the mountain range.
¨
11.3.2. Dating of Pyrenean Wurmian
Terminal Moraine Occurrences
On the Spanish side, the most abundant evidence has been
´
obtained from the Gallego catchment (Fig. 11.3). The ter-
¨
minal moraine at Senegue has yielded two OSL ages of
36 Æ 3 and 36 Æ 2 ka, respectively (Pena et al., 2004; Lewis
˜
et al., 2009). In the western part of the catchment, elevations
FIGURE 11.5 Terminal sequence of glacier deposits in the Noguera do not exceed 2.7 km. As the radiocarbon ages of 30–25 14C
¨
Ribagorcana catchment, age of the Wurmian moraines. 1: Mountain ridge.
¸ ka BP obtained from proglacial lake sediments around Tra-
¨ ¨
2: Unweathered Wurmian till or moraine. 3: Wurmian fluvio-lacustrine
¨
ice-contact deposit. 4: Wurmian ice front limits and typical U-shaped val-
´
macastilla and Pourtalet demonstrate (Garcıa-Ruiz et al.,
ley cross-profiles; 14C- and 10Be-dated sites. The map and chronological 2003; Gonza ´ lez-Samperiz et al., 2006) this area was already
´
` ´
data are after Bordonau et al. (1993), Pallas et al. (2006) and Rodes (2008). partially deglaciated in MIS 2 and cut off from transfluent
9. Author's personal copy
134 Quaternary Glaciations-Extent and Chronology
sources of northern ice spilling over the Col du Pourtalet. A data are still unpublished but they clearly confirm that
core obtained from a cirque located 2 km to the east of the ¨
the Wurmian maximum ice extent occurred much earlier
Col du Pourtalet indicates a possible readvance between than the global LGM. The ice-marginal lake sediment
24.17 and 19.25 14C ka BP. This advance would have sequence at La Massana, which formed where the Valira
occurred during MIS 2 even though ice had vacated the del Nord and Valira d’Orient glaciers separated, has been
topography at elevations situated above that site since subjected to detailed sedimentological and stratigraphical
before 19.25 14C ka BP. The position of the Gallego ice
´ analysis of its progradational deltas. AMS radiocarbon
front in MIS 2 is difficult to establish, but the 20.8 14C dates have returned ages of 25.63, 21.51 and 17.43 14C
ka BP (i.e. 24.217 ka cal. BP) radiocarbon age obtained ka BP (29031 to 27820, 24150 to 23310, 21097 to 20271
from the base of the Bubal lake deposits (Jalut et al., ka cal. BP) and indirectly confirm the presence of this lake
1992) suggests that the LGM glacier front was stationed since $ 41 ka on the basis of sedimentation rate calcula-
as much as 15 km up-valley from Senegue. ¨ tions. The lake sediments subsequently recorded a succes-
In the Cinca catchment, the maximum extent of the Ara sion of three glacier advances of diminishing intensity, all
glacier is constrained by ice-contact lake deposits at Linas ´ falling chronostratigraphically within MIS 2 (Turu i
de Broto. A 50-m drillhole here produced a mid-core AMS Michels, 2002). The maximum ice extent may have been
14
C age of 30.38 14C ka BP (Martı-Bono et al., 2002), indicat-
´ captured by a 59 Æ 1.18 21Ne ka age obtained from an
¨
ing an early age of Wurmian maximum ice extent and possi- ice-scoured bedrock surface that was sampled on the upper
ble maintenance of this advanced position until MIS 2 and flank of the glacial trough above the village of Canillo
global LGM time. In the Cinca valley, till at Salinas de Sin (Turu i Michels et al., 2004).
is associated with glaciofluvial deposits and has yielded In the eastern Pyrenees, 10Be exposure ages show that
OSL ages of 46 Æ 4, 63 Æ 6 and 71 Æ 15 ka. The Salinas expo- the MIS 2 maximum ice advance reached positions within
sure has been subjected to glaciotectonic deformation, proof ¨
a few hundred metres of the Wurmian maximum ice extent.
that it has also been overridden by the glacier since 46 ka ˆ
The frontal moraine of the Tet glacier at Mont Louis
(Lewis et al., 2009). (Fig. 11.6) has provided an age of 21.4 Æ 3.7 ka (Delmas
On the Noguera Ribagorcana (Fig. 11.5), MIS 2 ages
¸ et al., 2008), since then recalibrated as 22 Æ 3.6 ka (Delmas,
have been obtained by 10Be dating of deposits situated in 2009). However, the dated boulders belong to the innermost
the vicinity of the presumed glacier terminus (Pallas ` ˆ ¨
lobe crest of the Tet Wurmian terminal moraine sequence.
et al., 2006). The terminal lobes, however, have been signif- The two outermost lobes have so far not been dated but
icantly eroded, making it difficult to draw any firm conclu- could correspond to the sites of maximum ice extent
sions from this valley about the age of the Wurmian ¨ ¨
reached earlier during the Wurmian stage. In the Carol
maximum ice extent. In the Valira catchment, most of the catchment (Fig. 11.2), the right flank lateral moraine has
FIGURE 11.6 Terminal sequence of Wurmian ¨
ˆ
glacier deposits in the Tet catchment: age of fron-
tal and lateral moraines. 1: Quaternary incision of
valleys into the Cenozoic erosion surface of the
Col de La Perche. 2: Alluvial sheet T2, weathered
(MIS 6). 3: Proglacial alluvial sheet T1, unweath-
¨
ered and connected to the Wurmian moraines. 4:
¨
Wurmian unweathered till and moraines, with
the position 10Be exposure-dated sites. 5: Succes-
¨ ¨
sive Wurmian ice front positions. 6: Wurmian ice-
contact sedimentary units (lacustrine or fluvial).
The mapping and geochronological data are after
Delmas et al. (2008) and Delmas (2009).
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Chapter 11 Recent Advances in Research on Quaternary Glaciations in the Pyrenees 135
been dated with great precision by three samples: as early as 29–25 14C ka BP, and no post-maximum ice front
22.9 Æ 2.7, 22.1 Æ 3.4 and 21.7 Æ 2.8 ka (Delmas, 2009). position corresponding to MIS 2, for example, similar to the
ˆ
However, as in the case of the Tet moraine sequence, the Garrabet frontal system, has been clearly identified. The
dated lateral moraine connects with a frontal lobe that is sit- interpretations of Jalut et al. (1992) and Reille and Andrieu
uated ca. 0.6 km up-valley from the Vinyola terminal lobe. (1995), respectively, have diverged on these issues.
The dated lateral moraine is therefore not the oldest in the Accordingly, a discussion of their respective merits in the
¨
Wurmian sequence. Finally, the small Malniu glacier, context of this review seems timely. Assuming first that
which remained disconnected from the Carol trunk valley the 38.4 Æ 2 14C ka BP age obtained at the Biscaye site
throughout the Wurmian stage, has yielded 10Be ages of
¨ by Mardonnes and Jalut (1983) is invalid and should be
76.5, 42.3 and 40.6 ka. The post-maximum Malniu frontal replaced by the AMS 14C ages obtained by Reille and
lobe, which is situated 0.5 km further up-valley, provided Andrieu (1995) from glaciolacustrine clays at the Lourdes
an age of 21.3 ka, which accords with the 23.9 ka age of a ¨
1 terminal moraine site, a Wurmian maximum ice extent
coeval lateral moraine preserved on the valley side (Pallas ` older than 20.025 14C ka BP (22486 to 21562 ka cal. BP)
et al., 2010). appears correct, with vacation of the piedmont zone
Among the north-facing glacial catchments, only the between 16.67 and 14.46 14C ka BP. New 10Be exposure
`
Ariege basin has recently delivered new data (Delmas, data from the Gave de Pau catchment have been obtained
2009; Delmas et al., 2011). Results, which largely rely on from morainic boulders situated at the Ossen diffluence site,
10
Be exposure ages, confirm the classic view of asynchro- immediately above the town of Lourdes. However, with
neity between mountain glaciation and the continental ice- five Lateglacial and Holocene ages and another of
sheet record and are broadly compatible with existing 53.5 Æ 38 ka, results remain inconclusive (Rodes, 2008).
`
¨
results from the Spanish catchments. The Wurmian maxi- Likewise, the moraine sequence at Aucun has yielded four
10
mum ice extent (Fig. 11.4) is constrained by two CRN ages Be ages ranging between 13 and 10 ka. All these ages,
that suggest two glacier advances of comparable extent: a however, are suspiciously young for this small glacier,
81.4 Æ 14.6 ka age obtained from an erratic boulder in the which at that time was disconnected from the Gave de
vicinity of the terminal moraine and a younger age of Pau trunk valley glacier. At the time, as shown by the posi-
34.9 Æ 8.5 ka obtained on the mid-valley lateral moraine `
tion of the lateral moraines at Argeles-Gazost (Barrere `
`
at Larcat. The Ariege glacier advanced to within 2 km of et al., 1980), this larger glacier still descended to elevations
the town of Foix. The older age is in good agreement with below 400 m a.s.l. and to positions less than 10 km from the
the 91.4 Æ 2.4 ka U–Th age obtained for the stalagmite floor ¨
outermost Wurmian ice front at Lourdes. Assuming now,
in the prehistoric cave at Niaux, which occurs 8 km up-val- instead, that the chronology advocated for the Wurmian ¨
ley and is just slightly older than the Niaux glacial deposits maximum ice extent by Mardonnes and Jalut (1983) is
(Sorriaux, 1981, 1982; Bakalowicz et al., 1984). The MIS 2 `
valid, it is feasible that the Argeles-Gazost and Aucun
maximum extent ice front has not been directly dated, but moraine ridges could define the post-maximum glacier
its position almost certainly coincides with the Garrabet position during MIS 2 peak.
frontal moraine, which is located 8 km up-valley from the If these local insights are assembled into a more coher-
¨
Wurmian terminal moraine. It has two recessional fronts ent Pyrenean-scale picture, it appears that the Wurmian ¨
`
at Bompas–Arignac and Berniere, respectively. This chro- maximum ice extent occurred somewhat earlier than the
nology was established indirectly by a surface exposure age global LGM, perhaps with glaciers advancing out of the
with a strong component of nuclide inheritance (31.2 ka) on crest zone to similar positions repeatedly during MIS 5d,
the bedrock step of the Tarascon basin and by the age of an 5b and 4. By definition, all 10Be ages are minimal exposure
adjacent erratic boulder resting directly on the dated bed- ages and thus cannot precisely date the moraine ridges that
rock-step surface (16.7 ka). Such a conjunction suggests have been sampled. Caution, therefore, must be exercised
so far unreported ice recessions and readvances, that is sta- when determining the exact number and position of glacier
dials, within the Pyrenean last glacial cycle. Other bedrock advances and retreats. For example, the MIS 2 ice fronts
steps have yielded exposure ages of 19 ka, for example, on a have only been positively identified in the eastern, more
scoured rock exposure situated 2.5 km up-valley from Gar- Mediterranean part of the mountain range: for example,
rabet. These ages equate to a $ 19 ka age for the Berniere ` ˆ `
in the Tet, Carol, Malniu, Ariege, Valira and Ribagorcana ¸
frontal lobe and provide the timing of the deglaciation valleys. It further appears that, in this region, MIS 2 ice
increment that followed the Garrabet stage. ¨
fronts also nearly reached the Wurmian maximum glacier
So far, no new data have been produced that might help positions. The MIS 2 ice fronts reached those positions at
to update the radiocarbon-dated terminal lobes of the the time of, or just before, the global LGM (i.e. between
Garonne, Gave de Pau and Gave d’Ossau catchments 23–19 ka cal. BP, Mix et al., 2001). In the western catch-
(Fig. 11.1). In these western tracts of the Pyrenean range, ments (Garonne, gave de Pau, Gave d’Ossau, Gallego),
the glaciers are thought to have receded to the upper valleys which are under greater direct influence from Atlantic
11. Author's personal copy
136 Quaternary Glaciations-Extent and Chronology
weather conditions, MIS 2 appears to have coincided 19.25 14C ka BP (i.e. 22–23 ka cal. BP; Gonzalez-Samperiz
´ ´
instead with a recessional period. It is too soon to decide et al., 2006); at the Col de Lhers (Fig. 11.4), it occurred
whether such contrasts should be ascribed to methodologi- ca. 22–20 14C ka BP (Jalut et al., 1982, 1992) and probably
cal artefacts inherent in the dating techniques used, or likewise at the Col de Puymorens.
whether the observed differences in glacier behaviour along After those events, glacier ice rapidly vacated most Pyr-
the strike of the mountain range truly reflect palaeoclimatic enean valleys, although it did not necessarily undergo a
differences. Far from being implausible, such differences ˆ
steady or uniform decline. In the Tet catchment, for exam-
could indeed have been controlled over the western Medi- ple, four moraine systems, both lateral and frontal, form a
terranean by the Balearic low atmospheric pressure centre, regular sequence receding back into the crest zone. Degla-
which may have been more active than Atlantic weather ciation also affected cirques, at least in the south-eastwards
systems during MIS 2 because of the southerly position ˆ
facing Tet catchment. For example, fossil peat exposed at
¨
of the Polar Front at the time (Florineth and Schluchter, the Grave-Amont site (elevation: 2150 m) has yielded three
14
2000; Hughes and Woodward, 2008). C ages that cluster around 20 ka cal. BP (from top to bot-
tom: 20.25–19.87, 19.204–18.666 and 20.26–19.37 ka cal.
BP; Delmas, 2005; Delmas et al., 2008). The reliability of
11.3.3. Evidence of Rapid Deglaciation from these ages is reinforced by the fact that they were obtained
from well-preserved Sphagnum. This material was free
the end of the global LGM from graphite contamination from the Palaeozoic schist
The stages of ice recession are only known for certain val- outcrops present in the catchment (this was verified by
leys, and it is not yet possible to produce a coherent synthe- X-ray diffraction analysis of the matrix) and with no possi-
sis for the entire Pyrenean range. Evidence of a first ˆ
ble hard-water effect. In the Tet catchment, the Llat reces-
recessional stage is provided by frontal moraines situated sional moraine (2200 m a.s.l.) has yielded a 10Be age of
only a short distance behind the MIS 2 maximum ice 18.4 Æ 2.3 ka (Delmas et al., 2008; Delmas, 2009). Like-
advance fronts, with additional evidence of significantly wise, the small Malniu catchment exhibits a recessional
thinner glaciers merely lining the valley floors (Delmas, moraine, with a 10Be age of 18.2 Æ 0.5 ka, situated on the
`
2009). In the Ariege catchment (Fig. 11.4), the ice field `
2200 m a.s.l. contour (Pallas et al., 2010). Further west,
was dismembered into disjunct trunk and tributary valley in the Valira catchment, valley glaciers and the Massana
`
glaciers, with, for example, the Courbiere, Vicdessos and moraine-dammed lake seem to have persisted until 17.5
14
Lauze glaciers forming disconnected, self-contained sys- C ka BP (Turu i Michels, 2002), and the lower lateral
tems. In the Cabanes basin, the glacier rapidly melted to moraine at Engolaster has returned a 10Be age of
half of its thickness. During this time, a number of new 18.077 Æ 1.31 ka (Turu i Michels et al., 2004; Turu i
ice-contact lakes and deltas also formed, such as at Michels, 2009). Along the Noguera Ribagorcana, the snout
¸
Ascou–Goulours and Axiat–Senconac on the trunk valley of an 8-km-long valley glacier reaching an elevation of
right flank, and at Niaux and Surba on the trunk valley left 1560 m a.s.l. formed the Santet moraines, with a mean
flank. The frontal moraines of this period are situated at 10
Be age of 13.7 Æ 0.9 ka (the oldest boulder being
Bompas–Arignac (19.1 Æ 3.8 ka, a 10Be exposure age 16.1 Æ 2.8 ka: Pallas et al., 2006). Rodes (2008) has recali-
` ´
obtained indirectly from a ice-scoured bedrock step just brated the Santet ages to 14.6 Æ 1.1 and 17 Æ 0.7 ka, respec-
down-valley from the Bompas-Arignac ice front) and at tively. Meanwhile, in the upper subcatchment of
Berniere (18.8 Æ 1.3 ka, 10Be age obtained on an erratic
` the Noguera de Tor, which is the main tributary to the
boulder). The corresponding exposure ages are in remark- ¨
Noguera Ribagorcana river, the Redo d’Ayguestortes lake,
¸
able agreement with the 19.1 Æ 1.6 ka U–Th age from the dammed by a frontal moraine at an elevation of 2110 m a.s.
younger stalagmite floor that seals the glacial deposits l. was ice free by 13.47 Æ 0.06 14C ka BP (Copons and Bor-
trapped in the Niaux cave (Sorriaux, 1981, 1982; Bakalo- donau, 1996).
wicz et al., 1984). This evidence also heralds the end of gla- In the north-facing catchments of the Pyrenees, valley
cial sedimentation at this site, with the cave becoming glaciers several kilometres long appear to have persisted
abandoned above the level of glacier activity. until, or even readvanced during, the Oldest Dryas Sta-
ˆ ˆ
A similar story emerges from the Tet ice field, with the Tet `
dial. This is well observed in the Ariege catchment at
glacier snout receding ca. 2.5 km from the Mont Louis termi- Freychine ` des, where a 4- to 6-km-long glacier tongue
nal lobe to the site of the Borde frontal moraine (Fig. 11.6). persisted until 13 14C ka BP ($16 ka cal. BP) alongside
Three 10Be exposure ages from the Borde moraine have indi- an ice-marginal lake (Jalut et al., 1982, 1992). This has
cated that recession occurred ca. 18.1 Æ 3.9, 19.4 Æ 2.5 or since been confirmed by CRN dating, with a bedrock-
21.1 Æ 3.1 ka (Delmas et al., 2008; Delmas, 2009). This step 10Be exposure age of 14.4 Æ 1.1 ka (Delmas, 2009;
period also coincided with the disappearance of major trans- `
Delmas et al., 2011). In the upper Ariege catchment,
fluence cols: at the Col du Pourtalet, this occurred before the Petches recessional moraine sequence (Fig. 11.4)
12. Author's personal copy
Chapter 11 Recent Advances in Research on Quaternary Glaciations in the Pyrenees 137
has been age-bracketed by a 10Be age from the Ax bed- ¨
the Wurmian could soon arise from systematic CRN dating
rock step of 15.4 Æ 3.4 ka (Delmas, 2009; Delmas et al., of vertical profiles in exposures of glaciofluvial outwash
2011). This implies the presence of a 26-km-long valley deposits and of terminal moraines. This would advanta-
glacier during the Oldest Dryas Stadial. It was well sup- geously complement, for example, in the Carol and Ariege `
plied by tributary valleys descending from the elevated valleys, the rather haphazard dating of scattered erratic
crest zone and feeding into the trunk valley just 5 km boulders (out of a population of heterogeneous and thus
from its terminus. At the Puymorens col, the lateral inconclusive CRN ages, a single boulder has provided a
moraine of a comparatively shorter glacier that des- suitable age of 122 ka, Delmas et al., 2011). The last glacial
cended to the carol valley yielded three 10Be ages around cycle, in contrast, has been increasingly well constrained
`
15 ka (Pallas et al., 2010). through the use of multiple chronometers. Glaciers during
¨
the Wurmian appear to have behaved in a more erratic, non-
11.3.4. The Last Glacial Bastions: Moraines in uniform manner than previously believed, particularly by
¨
‘mono-glacialists’ according to whom the ‘Wurm’ cycle
the Crest Zone Cirques consisted of a single episode of ice advance followed by
The chronology of the cirque glaciers is quite variable and a single episode of ice retreat (Taillefer, 1985). Neverthe-
depends on their altitude and their position within the less, the asynchroneity between the Pyrenean mountain gla-
mountain mass. As a result, it still remains difficult to pro- cial chronology and the global LGM seems confirmed. An
duce a definitive synthesis on the latest Pleistocene cirque ¨
important interstadial within the Wurmian has been
glaciation of the Pyrenees. In the central Pyrenees, residual `
revealed in the Ariege catchment, with glaciers having
glaciers still exist on the most elevated massifs, and evi- extended repeatedly to approximately the same positions
dence that some of these grew during the Little Ice Age during stadial advances and interstadial recessions. MIS
has ushered in the idea, still poorly investigated, of a ‘neo- 2, which coincided with significant post-maximum read-
glacial’ resurgence during the Holocene (Gellatly et al., vances to the outermost terminal moraines in the eastern
1992). Other cirques, however, were ice free by the time part of the Pyrenees, remains poorly represented in the
of the Oldest Dryas as demonstrated, for example, by paly- ´
western half of the range (Gallego, Garonne, Gave de
nostratigraphy in the cirques of the Madres massif (Reille `
Pau). In the Ariege basin, perhaps because it is located in
and Lowe, 1993). In good agreement with 10Be ages the transition zone between east and west, MIS 2 moraines
obtained from bedrock steps, most cirques in the south-east- ¨
stand distinctly within the earlier Wurmian maximum ter-
ern Pyrenees were almost entirely deglaciated by the mini. It remains too early to confirm whether this east-to-
Allerd Interstadial (Delmas, 2005, 2009), at a time when west gradient is a genuine signal reflecting differences in
the tree-line rose rapidly to altitudes of 1800 m a.s.l. on glacier response to palaeoclimatic differences, or whether
north-facing slopes (Reille and Andrieu, 1993). Neverthe- it is the consequence of insufficient or insufficiently precise
less, in conditions locally favoured either by snow drifts radiometric age brackets. Regional climatic differences cer-
ˆ
or by limited insolation, such as in the Tet (i.e. upper Grave) tainly became quite sharp after the onset of the latest Pleis-
valley, some small glaciers persisted or reformed during the tocene deglacial stage, and have remained so as a function
Younger Dryas Stadial, as attested by a 11.6 Æ 1.8 ka, 10Be- of topographical setting and local conditions. Finally,
dated moraine (Delmas et al., 2008; Delmas, 2009). This although ice receded rapidly everywhere after the global
appears to have also occurred in the Lorri valley above Puy- LGM, the detailed chronology of cirque glaciation is still
morens, supported by a 10Be age of 11.8 Æ 0.6 ka (Rodes, ´ difficult to unravel because of its geographical variability.
2008; Pallas et al., 2010). More surprising are the 10Be ages
` More work on these aspects is expected in the coming years.
of 10.4 Æ 1.2 and 10.3 Æ 1.8 ka (Pallas et al., 2006), recali-
`
brated to 11 Æ 1.3 and 11 Æ 1.9 ka (Rodes, 2008), that have
´
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