@article{MurrayBraunReiners2018, author = {Murray, Kendra E. and Braun, Jean and Reiners, Peter W.}, title = {Toward Robust Interpretation of Low-Temperature Thermochronometers in Magmatic Terranes}, series = {Geochemistry, geophysics, geosystems}, volume = {19}, journal = {Geochemistry, geophysics, geosystems}, number = {10}, publisher = {American Geophysical Union}, address = {Washington}, issn = {1525-2027}, doi = {10.1029/2018GC007595}, pages = {3739 -- 3763}, year = {2018}, abstract = {Many regions central to our understanding of tectonics and landscape evolution are active or ancient magmatic terranes, and robust interpretation of low-temperature thermochronologic ages in these settings requires careful attention to the drivers of rock heating and cooling, including magmatism. However, we currently lack a quantitative framework for evaluating the potential role of magmatic coolingthat is, post-magmatic thermal relaxationin shaping cooling age patterns in regions with a history of intrusive magmatism. Here we use analytical approximations and numerical models to characterize how low-temperature thermochronometers document cooling inside and around plutons in steadily exhuming environments. Our models predict that the thermal field a pluton intrudes into, specifically the ambient temperatures relative to the closure temperature of a given thermochronometer, is as important as the pluton size and temperature in controlling the pattern and extent of thermochronometer resetting in the country rocks around a pluton. We identify one advective and several conductive timescales that govern the relationship between the crystallization and cooling ages inside a pluton. In synthetic vertical age-elevation relationships (AERs), resetting next to plutons results in changes in AER slope that could be misinterpreted as past changes in exhumation rate if the history of magmatism is not accounted for. Finally, we find that large midcrustal plutons, such as those emplaced at similar to 10-15-km depth, can reset the low-temperature thermochronometers far above them in the upper crusta result with considerable consequences for thermochronology in arcs and regions with a history of magmatic activity that may not have a surface expression.}, language = {en} } @article{PicoMitrovicaPerronetal.2019, author = {Pico, Tamara and Mitrovica, Jerry X. and Perron, J. Taylor and Ferrier, Ken L. and Braun, Jean}, title = {Influence of glacial isostatic adjustment on river evolution along the US mid-Atlantic coast}, series = {Earth \& planetary science letters}, volume = {522}, journal = {Earth \& planetary science letters}, publisher = {Elsevier}, address = {Amsterdam}, issn = {0012-821X}, doi = {10.1016/j.epsl.2019.06.026}, pages = {176 -- 185}, year = {2019}, abstract = {Long-term river evolution depends partly on crustal deformation, which shapes the topography crossed by rivers. On glacial timescales, ice-sheet growth and decay can produce crustal vertical motion of ∼10 mm/yr resulting from the solid Earth's adjustment to variations in ice and water loads, comparable to tectonically-driven rates in the most rapidly uplifting mountains on Earth. This process of glacial isostatic adjustment (GIA) can influence river courses and drainage basins substantially, particularly near former ice margins. We explore the extent to which GIA influenced the evolution of rivers along the United States east coast during the last glacial cycle. We compute gravitationally self-consistent GIA responses that incorporate recent constraints on the Laurentide Ice Sheet history through the last glacial build-up phase, and we connect the predicted variations in topography to abrupt changes in river dynamics recorded in the Hudson, Delaware, Susquehanna, and Potomac Rivers from 40 ka to present. To the extent that increases in sediment transport capacity imply increases in river incision rate, the GIA-driven changes in slope and drainage area are consistent with episodes of erosion and sedimentation observed in the Hudson, Delaware, and Potomac Rivers, but inconsistent with the observed accelerated river incision in the Susquehanna River at 30-14 ka. These analyses add to a growing body of evidence showing that GIA strongly influences river evolution over millennial timescales.}, language = {en} } @article{MargirierBraunGautheronetal.2019, author = {Margirier, Audrey and Braun, Jean and Gautheron, Cecile and Carcaillet, Julien and Schwartz, Stephane and Jamme, Rosella Pinna and Stanley, Jessica}, title = {Climate control on Early Cenozoic denudation of the Namibian margin as deduced from new thermochronological constraints}, series = {Earth \& planetary science letters}, volume = {527}, journal = {Earth \& planetary science letters}, publisher = {Elsevier}, address = {Amsterdam}, issn = {0012-821X}, doi = {10.1016/j.epsl.2019.115779}, pages = {11}, year = {2019}, abstract = {The processes that control long term landscape evolution in continental interiors and, in particular, along passive margins such as in southern Africa, are still the subject of much debate (e.g. Braun, 2018). Although today the Namibian margin is characterized by an arid climate, it has experienced climatic fluctuations during the Cenozoic and, yet, to date no study has documented the potential role of climate on its erosion history. In western Namibia, the Brandberg Massif, an erosional remnant or inselberg, provides a good opportunity to document the Cenozoic denudation history of the margin using the relationship between rock cooling or exhumation ages and their elevation. Here we provide new apatite (UThSm)/He dates on the Brandberg Inselberg that range from 151 +/- 12 to 30 +/- 2 Ma. Combined with existing apatite fission track data, they yield new constraints on the denudation history of the margin. These data document two main cooling phases since continental break-up 130 Myr ago, a rapid one (similar to 10 degrees C/Myr) following break-up and a slower one (similar to 12 degrees C/Myr) between 65 and 35 Ma. We interpret them respectively to be related to escarpment erosion following rifting and continental break-up and as a phase of enhanced denudation during the Early Eocene Climatic Optimum. We propose that during the Early Eocene Climatic Optimum chemical weathering was important and contributed significantly to the denudation of the Namibian margin and the formation of a pediplain around the Brandberg and enhanced valley incision within the massif. Additionally, aridification of the region since 35 Ma has resulted in negligible denudation rates since that time. (C) 2019 Elsevier B.V. All rights reserved.}, language = {en} } @article{HermanBraunDealetal.2018, author = {Herman, Frederic and Braun, Jean and Deal, Eric and Prasicek, Gunther}, title = {The response time of glacial erosion}, series = {Journal of geophysical research : Earth surface}, volume = {123}, journal = {Journal of geophysical research : Earth surface}, number = {4}, publisher = {American Geophysical Union}, address = {Washington}, issn = {2169-9003}, doi = {10.1002/2017JF004586}, pages = {801 -- 817}, year = {2018}, abstract = {There has been recent progress in the understanding of the evolution of Quaternary climate. Simultaneously, there have been improvements in the understanding of glacial erosion processes, with better parameter constraints. Despite this, there remains much debate about whether or not the observed cooling over the Quaternary has driven an increase in glacial erosion rates. Most studies agree that the erosional response to climate change must be transient; therefore, the time scale of the climatic change and the response time of glacial erosion must be accounted for. Here we analyze the equations governing glacial erosion in a steadily uplifting landscape with variable climatic forcing and derive expressions for two fundamental response time scales. The first time scale describes the response of the glacier and the second one the glacial erosion response. We find that glaciers have characteristic time scales of the order of 10 to 10,000 years, while the characteristic time scale for glacial erosion is of the order of a few tens of thousands to a few million years. We then use a numerical model to validate the approximations made to derive the analytical solutions. The solutions show that short period forcing is dampened by the glacier response time, and long period forcing (>1 Myr) may be dampened by erosional response of glaciers when the rock uplift rates are high. In most tectonic and climatic conditions, we expect to see the strongest response of glacial erosion to periodic climatic forcing corresponding to Plio-Pleistocene climatic cycles. Finally, we use the numerical model to predict the response of glacial systems to the observed climatic forcing of the Quaternary, including, but not limited to, the Milankovich periods and the long-term secular cooling trend. We conclude that an increase of glacial erosion in response to Quaternary cooling is physically plausible, and we show that the magnitude of the increase depends on rock uplift and ice accumulation rates.}, language = {en} } @article{PicoMitrovicaBraunetal.2018, author = {Pico, T. and Mitrovica, J. X. and Braun, Jean and Ferrier, K. L.}, title = {Glacial isostatic adjustment deflects the path of the ancestral Hudson River}, series = {Geology}, volume = {46}, journal = {Geology}, number = {7}, publisher = {American Institute of Physics}, address = {Boulder}, issn = {0091-7613}, doi = {10.1130/G40221.1}, pages = {591 -- 594}, year = {2018}, abstract = {Quantifying the pace of ice-sheet growth is critical to understanding ice-age climate and dynamics. Here, we show that the diversion of the Hudson River (northeastern North America) late in the last glaciation phase (ca. 30 ka), which some previous studies have speculated was due to glacial isostatic adjustment (GIA), can be used to infer the timing of the Laurentide Ice Sheet's growth to its maximum extent. Landscapes in the vicinity of glaciated regions have likely responded to crustal deformation produced by ice-sheet growth and decay through river drainage reorganization, given that rates of uplift and subsidence are on the order of tens of meters per thousand years. We perform global, gravitationally self-consistent simulations of GIA and input the predicted crustal deformation field into a landscape evolution model. Our calculations indicate that the eastward diversion of the Hudson River at 30 ka is consistent with exceptionally rapid growth of the Laurentide Ice Sheet late in the glaciation phase, beginning at 50-35 ka.}, language = {en} } @article{PrasicekHermanRobletal.2018, author = {Prasicek, G{\"u}nther and Herman, Frederic and Robl, J{\"o}rg and Braun, Jean}, title = {Glacial steady state topography controlled by the coupled influence of tectonics and climate}, series = {Journal of geophysical research : Earth surface}, volume = {123}, journal = {Journal of geophysical research : Earth surface}, number = {6}, publisher = {American Geophysical Union}, address = {Washington}, issn = {2169-9003}, doi = {10.1029/2017JF004559}, pages = {1344 -- 1362}, year = {2018}, abstract = {Glaciers and rivers are the main agents of mountain erosion. While in the fluvial realm empirical relationships and their mathematical description, such as the stream power law, improved the understanding of fundamental controls on landscape evolution, simple constraints on glacial topography and governing scaling relations are widely lacking. We present a steady state solution for longitudinal profiles along eroding glaciers in a coupled system that includes tectonics and climate. We combined the shallow ice approximation and a glacial erosion rule to calculate ice surface and bed topography from prescribed glacier mass balance gradient and rock uplift rate. Our approach is inspired by the classic application of the stream power law for describing a fluvial steady state but with the striking difference that, in the glacial realm, glacier mass balance is added as an altitude-dependent variable. From our analyses we find that ice surface slope and glacial relief scale with uplift rate with scaling exponents indicating that glacial relief is less sensitive to uplift rate than relief in most fluvial landscapes. Basic scaling relations controlled by either basal sliding or internal deformation follow a power law with the exponent depending on the exponents for the glacial erosion rule and Glen's flow law. In a mixed scenario of sliding and deformation, complicated scaling relations with variable exponents emerge. Furthermore, a cutoff in glacier mass balance or cold ice in high elevations can lead to substantially larger scaling exponents which may provide an explanation for high relief in high latitudes.}, language = {en} } @article{BiswasHermanKingetal.2018, author = {Biswas, R. H. and Herman, F. and King, G. E. and Braun, Jean}, title = {Thermoluminescence of feldspar as a multi-thermochronometer to constrain the temporal variation of rock exhumation in the recent past}, series = {Earth \& planetary science letters}, volume = {495}, journal = {Earth \& planetary science letters}, publisher = {Elsevier}, address = {Amsterdam}, issn = {0012-821X}, doi = {10.1016/j.epsl.2018.04.030}, pages = {56 -- 68}, year = {2018}, abstract = {Natural thermoluminescence (TL) in rocks reflects a dynamic equilibrium between radiation-induced TL growth and decay via thermal and athermal pathways. When rocks exhume through Earth's crust and cool from high to low temperature, this equilibrium level increases as the temperature dependent thermal decay decreases. This phenomenon can be exploited to extract thermal histories of rocks. The main advantage of TL is that a single TL glow curve has a wide range of thermal stabilities (lifetime 100 °C/Ma, whereas deeper traps, i.e. with higher activation energies, provide constraints on thermal histories for higher cooling rates (>300 °C/Ma). Finally, we show how the path of rock exhumation (i.e., depth vs. time) can be constrained using an inverse approach. The newly developed methodology is applied to rapidly cooled samples from the Namche Barwa massif, eastern Himalaya to suggest a trend in exhumation rate with time that follows an inverse correlation with global temperature and glaciers equilibrium altitude line (ELA).}, language = {en} } @article{DealBraunBotter2018, author = {Deal, Eric and Braun, Jean and Botter, Gianluca}, title = {Understanding the role of rainfall and hydrology in determining fluvial erosion efficiency}, series = {Journal of geophysical research : Earth surface}, volume = {123}, journal = {Journal of geophysical research : Earth surface}, number = {4}, publisher = {American Geophysical Union}, address = {Washington}, issn = {2169-9003}, doi = {10.1002/2017JF004393}, pages = {744 -- 778}, year = {2018}, abstract = {Due to the challenges in upscaling daily climatic forcing to geological time, physically realistic models describing how rainfall drives fluvial erosion are lacking. To bridge this gap between short-term hydrology and long-term geomorphology, we derive a theoretical framework for long-term fluvial erosion rates driven by realistic climate by integrating an established stochastic-mechanistic model of hydrology into a threshold-stochastic formulation of stream power. The hydrological theory provides equations for the daily streamflow probability distribution as a function of climatic boundary conditions. The new parameters introduced are rooted firmly in established climatic and hydrological theory. This allows us to account for how fluvial erosion rates respond to changes in rainfall intensity, frequency, evapotranspiration rates, and soil moisture dynamics in a way that is consistent with existing theories. We use this framework to demonstrate how hydroclimatic conditions and erosion threshold magnitude control the degree of nonlinearity between steepness index and erosion rate. We find that hydrological processes can have a significant influence on how erosive a particular climatic forcing will be. By accounting for the influence of hydrology on fluvial erosion, we conclude that climate is an important control on erosion rates and long-term landscape evolution.}, language = {en} } @article{YuanBraunGueritetal.2019, author = {Yuan, Xiaoping P. and Braun, Jean and Guerit, Laure and Rouby, D. and Cordonnier, G.}, title = {A New Efficient Method to Solve the Stream Power Law Model Taking Into Account Sediment Deposition}, series = {Journal of geophysical research : Earth surface}, volume = {124}, journal = {Journal of geophysical research : Earth surface}, number = {6}, publisher = {American Geophysical Union}, address = {Washington}, issn = {2169-9003}, doi = {10.1029/2018JF004867}, pages = {1346 -- 1365}, year = {2019}, abstract = {The stream power law model has been widely used to represent erosion by rivers but does not take into account the role played by sediment in modulating erosion and deposition rates. Davy and Lague (2009, ) provide an approach to address this issue, but it is computationally demanding because the local balance between erosion and deposition depends on sediment flux resulting from net upstream erosion. Here, we propose an efficient (i.e., O(N) and implicit) method to solve their equation. This means that, unlike other methods used to study the complete dynamics of fluvial systems (e.g., including the transition from detachment-limited to transport-limited behavior), our method is unconditionally stable even when large time steps are used. We demonstrate its applicability by performing a range of simulations based on a simple setup composed of an uplifting region adjacent to a stable foreland basin. As uplift and erosion progress, the mean elevations of the uplifting relief and the foreland increase, together with the average slope in the foreland. Sediments aggrade in the foreland and prograde to reach the base level where sediments are allowed to leave the system. We show how the topography of the uplifting relief and the stratigraphy of the foreland basin are controlled by the efficiency of river erosion and the efficiency of sediment transport by rivers. We observe the formation of a steady-state geometry in the uplifting region, and a dynamic steady state (i.e., autocyclic aggradation and incision) in the foreland, with aggradation and incision thicknesses up to tens of meters.}, language = {en} } @article{CordonnierBovyBraun2019, author = {Cordonnier, Guillaume and Bovy, Benoit and Braun, Jean}, title = {A versatile, linear complexity algorithm for flow routing in topographies with depressions}, series = {Earth surface dynamics}, volume = {7}, journal = {Earth surface dynamics}, number = {2}, publisher = {Copernicus}, address = {G{\"o}ttingen}, issn = {2196-6311}, doi = {10.5194/esurf-7-549-2019}, pages = {549 -- 562}, year = {2019}, abstract = {We present a new algorithm for solving the common problem of flow trapped in closed depressions within digital elevation models, as encountered in many applications relying on flow routing. Unlike other approaches (e.g., the Priority-Flood depression filling algorithm), this solution is based on the explicit computation of the flow paths both within and across the depressions through the construction of a graph connecting together all adjacent drainage basins. Although this represents many operations, a linear time complexity can be reached for the whole computation, making it very efficient. Compared to the most optimized solutions proposed so far, we show that this algorithm of flow path enforcement yields the best performance when used in landscape evolution models. In addition to its efficiency, our proposed method also has the advantage of letting the user choose among different strategies of flow path enforcement within the depressions (i.e., filling vs. carving). Furthermore, the computed graph of basins is a generic structure that has the potential to be reused for solving other problems as well, such as the simulation of erosion. This sequential algorithm may be helpful for those who need to, e.g., process digital elevation models of moderate size on single computers or run batches of simulations as part of an inference study.}, language = {en} } @article{YuanBraunGueritetal.2019, author = {Yuan, Xiaoping and Braun, Jean and Guerit, Laure and Simon, Brendan and Bovy, Beno{\^i}t and Rouby, Delphine and Robin, C{\´e}cile and Jiao, R.}, title = {Linking continental erosion to marine sediment transport and deposition: A new implicit and O(N) method for inverse analysis}, series = {Earth \& planetary science letters}, volume = {524}, journal = {Earth \& planetary science letters}, publisher = {Elsevier}, address = {Amsterdam}, issn = {0012-821X}, doi = {10.1016/j.epsl.2019.115728}, pages = {15}, year = {2019}, abstract = {The marine sedimentary record contains unique information about the history of erosion, uplift and climate of the adjacent continent. Inverting this record has been the purpose of many numerical studies. However, limited attention has been given to linking continental erosion to marine sediment transport and deposition in large-scale surface process evolution models. Here we present a new numerical method for marine sediment transport and deposition that is directly coupled to a landscape evolution algorithm solving for the continental fluvial and hillslope erosion equations using implicit and O(N) algorithms. The new method takes into account the sorting of grain sizes (e.g., silt and sand) in the marine domain using a non-linear multiple grain-size diffusion equation and assumes that the sediment flux exported from the continental domain is proportional to the bathymetric slope. Specific transport coefficients and compaction factors are assumed for the two different grain sizes to simulate the stratigraphic architecture. The resulting set of equations is solved using an efficient (O(N) and implicit) algorithm. It can thus be used to invert stratigraphic geometries using a Bayesian approach that requires a large number of simulations. This new method is used to invert the sedimentary geometry of a natural example, the Ogooue Delta (Gabon), over the last similar to 5 Myr. The objective is to unravel the set of erosional histories of the adjacent continental domain compatible with the observed geometry of the offshore delta. For this, we use a Bayesian inversion scheme in which the misfit function is constructed by comparing four geometrical parameters between the natural and the simulated delta: the volume of sediments stored in the delta, the surface slope, the initial and the final shelf lengths. We find that the best-fit values of the transport coefficients for silt in the marine domain are in the range of 300 - 500 m(2)/yr, in agreement with previous studies on offshore diffusion. We also show that, in order to fit the sedimentary geometry, erosion rate on the continental domain must have increased by a factor of 6 to 8 since 5.3 Ma. (C) 2019 Elsevier B.V. All rights reserved.}, language = {en} } @misc{Braun2020, author = {Braun, Jean}, title = {Response to comment by Japsen et al. on "A review of numerical modeling studies of passive margin escarpments leading to a new analytical expression for the rate of escarpment migration velocity"}, series = {Gondwana research : international geoscience journal ; official journal of the International Association for Gondwana Research}, volume = {65}, journal = {Gondwana research : international geoscience journal ; official journal of the International Association for Gondwana Research}, publisher = {Elsevier}, address = {Amsterdam}, issn = {1342-937X}, doi = {10.1016/j.gr.2018.10.003}, pages = {174 -- 176}, year = {2020}, language = {en} } @article{GebauerBraunSuaudetal.1997, author = {Gebauer, Gunther and Braun, Sebastian and Suaud, Charles and Faure, Jean M.}, title = {Die soziale Umwelt von Spitzensportlern - eine Vergleichsstudie zwischen Deutschland und Frankreich}, year = {1997}, language = {de} } @misc{GebauerBraunSuaudetal.1999, author = {Gebauer, Gunther and Braun, Sebastian and Suaud, Charles and Faure, Jean M.}, title = {Die soziale Umwelt von Spitzensportlern : ein Vergleich des Spitzensports in Deutschland und Frankreich}, series = {Schriftenreihe des Bundesinstituts f{\"u}r Sportwissenschaft}, volume = {98}, journal = {Schriftenreihe des Bundesinstituts f{\"u}r Sportwissenschaft}, publisher = {Hofmann}, address = {Schorndorf}, isbn = {3-7780-8981-1}, pages = {340 S. : graph. Darst.}, year = {1999}, language = {de} } @article{Braun2022, author = {Braun, Jean}, title = {Comparing the transport-limited and ξ-q models for sediment transport}, series = {Earth surface dynamics}, volume = {10}, journal = {Earth surface dynamics}, number = {2}, publisher = {Copernicus}, address = {G{\"o}ttingen}, issn = {2196-6311}, doi = {10.5194/esurf-10-301-2022}, pages = {301 -- 327}, year = {2022}, abstract = {Here I present a comparison between two of the most widely used reduced-complexity models for the representation of sediment transport and deposition processes, namely the transport-limited (or TL) model and the under-capacity (or xi-q) model more recently developed by Davy and Lague (2009). Using both models, I investigate the behavior of a sedimentary continental system of length L fed by a fixed sedimentary flux from a catchment of size A(0) in a nearby active orogen through which sediments transit to a fixed base level representing a large river, a lake or an ocean. This comparison shows that the two models share the same steady-state solution, for which I derive a simple 1D analytical expression that reproduces the major features of such sedimentary systems: a steep fan that connects to a shallower alluvial plain. The resulting fan geometry obeys basic observational constraints on fan size and slope with respect to the upstream drainage area, A(0). The solution is strongly dependent on the size of the system, L, in comparison to a distance L-0, which is determined by the size of A(0), and gives rise to two fundamentally different types of sedimentary systems: a constrained system where L < L-0 and open systems where L > L-0. I derive simple expressions that show the dependence of the system response time on the system characteristics, such as its length, the size of the upstream catchment area, the amplitude of the incoming sedimentary flux and the respective rate parameters (diffusivity or erodibility) for each of the two models. I show that the xi-q model predicts longer response times. I demonstrate that although the manner in which signals propagates through the sedimentary system differs greatly between the two models, they both predict that perturbations that last longer than the response time of the system can be recorded in the stratigraphy of the sedimentary system and in particular of the fan. Interestingly, the xi-q model predicts that all perturbations in the incoming sedimentary flux will be transmitted through the system, whereas the TL model predicts that rapid perturbations cannot. I finally discuss why and under which conditions these differences are important and propose observational ways to determine which of the two models is most appropriate to represent natural systems.}, language = {en} } @article{NeuharthBruneGlerumetal.2021, author = {Neuharth, Derek and Brune, Sascha and Glerum, Anne and Morley, Chris K. and Yuan, Xiaoping and Braun, Jean}, title = {Flexural strike-slip basins}, series = {Geology : a venture in earth science reporting / the Geological Society of America}, volume = {50}, journal = {Geology : a venture in earth science reporting / the Geological Society of America}, number = {3}, publisher = {American Institute of Physics}, address = {Boulder}, issn = {0091-7613}, doi = {10.1130/G49351.1}, pages = {361 -- 365}, year = {2021}, abstract = {Strike-slip faults are classically associated with pull-apart basins where continental crust is thinned between two laterally offset fault segments. We propose a subsidence mechanism to explain the formation of a new type of basin where no substantial segment offset or synstrike-slip thinning is observed. Such "flexural strike-slip basins" form due to a sediment load creating accommodation space by bending the lithosphere. We use a two-way coupling between the geodynamic code ASPECT and surface-processes code FastScape to show that flexural strike-slip basins emerge if sediment is deposited on thin lithosphere close to a strike slip fault. These conditions were met at the Andaman Basin Central fault (Andaman Sea, Indian Ocean), where seismic reflection data provide evidence of a laterally extensive flexural basin with a depocenter located parallel to the strike-slip fault trace.}, language = {en} } @article{NeuharthBruneWronaetal.2022, author = {Neuharth, Derek and Brune, Sascha and Wrona, Thilo and Glerum, Anne and Braun, Jean and Yuan, Xiaoping}, title = {Evolution of rift systems and their fault networks in response to surface processes}, series = {Tectonics}, volume = {41}, journal = {Tectonics}, number = {3}, publisher = {American Geophysical Union}, address = {Washington}, issn = {0278-7407}, doi = {10.1029/2021TC007166}, pages = {22}, year = {2022}, abstract = {Continental rifting is responsible for the generation of major sedimentary basins, both during rift inception and during the formation of rifted continental margins. Geophysical and field studies revealed that rifts feature complex networks of normal faults but the factors controlling fault network properties and their evolution are still matter of debate. Here, we employ high-resolution 2D geodynamic models (ASPECT) including two-way coupling to a surface processes (SP) code (FastScape) to conduct 12 models of major rift types that are exposed to various degrees of erosion and sedimentation. We further present a novel quantitative fault analysis toolbox (Fatbox), which allows us to isolate fault growth patterns, the number of faults, and their length and displacement throughout rift history. Our analysis reveals that rift fault networks may evolve through five major phases: (a) distributed deformation and coalescence, (b) fault system growth, (c) fault system decline and basinward localization, (d) rift migration, and (e) breakup. These phases can be correlated to distinct rifted margin domains. Models of asymmetric rifting suggest rift migration is facilitated through both ductile and brittle deformation within a weak exhumation channel that rotates subhorizontally and remains active at low angles. In sedimentation-starved settings, this channel satisfies the conditions for serpentinization. We find that SP are not only able to enhance strain localization and to increase fault longevity but that they also reduce the total length of the fault system, prolong rift phases and delay continental breakup.}, language = {en} } @article{WolfHuismansBraunetal.2022, author = {Wolf, Sebastian G. and Huismans, Ritske S. and Braun, Jean and Yuan, Xiaoping}, title = {Topography of mountain belts controlled by rheology and surface processes}, series = {Nature : the international weekly journal of science}, volume = {606}, journal = {Nature : the international weekly journal of science}, number = {7914}, publisher = {Nature portfolio}, address = {Berlin}, issn = {0028-0836}, doi = {10.1038/s41586-022-04700-6}, pages = {516 -- 521}, year = {2022}, abstract = {It is widely recognized that collisional mountain belt topography is generated by crustal thickening and lowered by river bedrock erosion, linking climate and tectonics(1-4). However, whether surface processes or lithospheric strength control mountain belt height, shape and longevity remains uncertain. Additionally, how to reconcile high erosion rates in some active orogens with long-term survival of mountain belts for hundreds of millions of years remains enigmatic. Here we investigate mountain belt growth and decay using a new coupled surface process(5,6) and mantle-scale tectonic model(7). End-member models and the new non-dimensional Beaumont number, Bm, quantify how surface processes and tectonics control the topographic evolution of mountain belts, and enable the definition of three end-member types of growing orogens: type 1, non-steady state, strength controlled (Bm > 0.5); type 2, flux steady state(8), strength controlled (Bm approximate to 0.4-0.5); and type 3, flux steady state, erosion controlled (Bm < 0.4). Our results indicate that tectonics dominate in Himalaya-Tibet and the Central Andes (both type 1), efficient surface processes balance high convergence rates in Taiwan (probably type 2) and surface processes dominate in the Southern Alps of New Zealand (type 3). Orogenic decay is determined by erosional efficiency and can be subdivided into two phases with variable isostatic rebound characteristics and associated timescales. The results presented here provide a unified framework explaining how surface processes and lithospheric strength control the height, shape, and longevity of mountain belts.}, language = {en} } @article{BraunGemignanivanderBeek2018, author = {Braun, Jean and Gemignani, Lorenzo and van der Beek, Pieter A.}, title = {Extracting information on the spatial variability in erosion rate stored in detrital cooling age distributions in river sands}, series = {Earth surface dynamics}, volume = {6}, journal = {Earth surface dynamics}, number = {1}, publisher = {Copernicus}, address = {G{\"o}ttingen}, issn = {2196-6311}, doi = {10.5194/esurf-6-257-2018}, pages = {257 -- 270}, year = {2018}, abstract = {One of the main purposes of detrital thermochronology is to provide constraints on the regional-scale exhumation rate and its spatial variability in actively eroding mountain ranges. Procedures that use cooling age distributions coupled with hypsometry and thermal models have been developed in order to extract quantitative estimates of erosion rate and its spatial distribution, assuming steady state between tectonic uplift and erosion. This hypothesis precludes the use of these procedures to assess the likely transient response of mountain belts to changes in tectonic or climatic forcing. Other methods are based on an a priori knowledge of the in situ distribution of ages to interpret the detrital age distributions. In this paper, we describe a simple method that, using the observed detrital mineral age distributions collected along a river, allows us to extract information about the relative distribution of erosion rates in an eroding catchment without relying on a steady-state assumption, the value of thermal parameters or an a priori knowledge of in situ age distributions. The model is based on a relatively low number of parameters describing lithological variability among the various sub-catchments and their sizes and only uses the raw ages. The method we propose is tested against synthetic age distributions to demonstrate its accuracy and the optimum conditions for it use. In order to illustrate the method, we invert age distributions collected along the main trunk of the Tsangpo-Siang-Brahmaputra river system in the eastern Himalaya. From the inversion of the cooling age distributions we predict present-day erosion rates of the catchments along the Tsangpo-Siang-Brahmaputra river system, as well as some of its tributaries. We show that detrital age distributions contain dual information about present-day erosion rate, i. e., from the predicted distribution of surface ages within each catchment and from the relative contribution of any given catchment to the river distribution. The method additionally allows comparing modern erosion rates to long-term exhumation rates. We provide a simple implementation of the method in Python code within a Jupyter Notebook that includes the data used in this paper for illustration purposes.}, language = {en} } @article{ActisAgnettaAharonianetal.2011, author = {Actis, M. and Agnetta, G. and Aharonian, Felix A. and Akhperjanian, A. G. and Aleksic, J. and Aliu, E. and Allan, D. and Allekotte, I. and Antico, F. and Antonelli, L. A. and Antoranz, P. and Aravantinos, A. and Arlen, T. and Arnaldi, H. and Artmann, S. and Asano, K. and Asorey, H. G. and Baehr, J. and Bais, A. and Baixeras, C. and Bajtlik, S. and Balis, D. and Bamba, A. and Barbier, C. and Barcelo, M. and Barnacka, Anna and Barnstedt, J{\"u}rgen and de Almeida, U. Barres and Barrio, J. A. and Basso, S. and Bastieri, D. and Bauer, C. and Becerra Gonzalez, J. and Becherini, Yvonne and Bechtol, K. C. and Becker, J. and Beckmann, Volker and Bednarek, W. and Behera, B. and Beilicke, M. and Belluso, M. and Benallou, M. and Benbow, W. and Berdugo, J. and Berger, K. and Bernardino, T. and Bernl{\"o}hr, K. and Biland, A. and Billotta, S. and Bird, T. and Birsin, E. and Bissaldi, E. and Blake, S. and Blanch Bigas, O. and Bobkov, A. A. and Bogacz, L. and Bogdan, M. and Boisson, Catherine and Boix Gargallo, J. and Bolmont, J. and Bonanno, G. and Bonardi, A. and Bonev, T. and Borkowski, Janett and Botner, O. and Bottani, A. and Bourgeat, M. and Boutonnet, C. and Bouvier, A. and Brau-Nogue, S. and Braun, I. and Bretz, T. and Briggs, M. S. and Brun, Pierre and Brunetti, L. and Buckley, H. and Bugaev, V. and Buehler, R. and Bulik, Tomasz and Busetto, G. and Buson, S. and Byrum, K. and Cailles, M. and Cameron, R. A. and Canestrari, R. and Cantu, S. and Carmona, E. and Carosi, A. and Carr, John and Carton, P. H. and Casiraghi, M. and Castarede, H. and Catalano, O. and Cavazzani, S. and Cazaux, S. and Cerruti, B. and Cerruti, M. and Chadwick, M. and Chiang, J. and Chikawa, M. and Cieslar, M. and Ciesielska, M. and Cillis, A. N. and Clerc, C. and Colin, P. and Colome, J. and Compin, M. and Conconi, P. and Connaughton, V. and Conrad, Jan and Contreras, J. L. and Coppi, P. and Corlier, M. and Corona, P. and Corpace, O. and Corti, D. and Cortina, J. and Costantini, H. and Cotter, G. and Courty, B. and Couturier, S. and Covino, S. and Croston, J. and Cusumano, G. and Daniel, M. K. and Dazzi, F. and Deangelis, A. and de Cea del Pozo, E. and Dal Pino, E. M. de Gouveia and de Jager, O. and de la Calle Perez, I. and De La Vega, G. and De Lotto, B. and de Naurois, M. and Wilhelmi, E. de Ona and de Souza, V. and Decerprit, B. and Deil, C. and Delagnes, E. and Deleglise, G. and Delgado, C. and Dettlaff, T. and Di Paolo, A. and Di Pierro, F. and Diaz, C. and Dick, J. and Dickinson, H. and Digel, S. W. and Dimitrov, D. and Disset, G. and Djannati-Ata{\"i}, A. and Doert, M. and Domainko, W. and Dorner, D. and Doro, M. and Dournaux, J. -L. and Dravins, D. and Drury, L. and Dubois, F. and Dubois, R. and Dubus, G. and Dufour, C. and Durand, D. and Dyks, J. and Dyrda, M. and Edy, E. and Egberts, Kathrin and Eleftheriadis, C. and Elles, S. and Emmanoulopoulos, D. and Enomoto, R. and Ernenwein, J. -P. and Errando, M. and Etchegoyen, A. and Falcone, A. D. and Farakos, K. and Farnier, C. and Federici, S. and Feinstein, F. and Ferenc, D. and Fillin-Martino, E. and Fink, D. and Finley, C. and Finley, J. P. and Firpo, R. and Florin, D. and Foehr, C. and Fokitis, E. and Font, Ll. and Fontaine, G. and Fontana, A. and Foerster, A. and Fortson, L. and Fouque, N. and Fransson, C. and Fraser, G. W. and Fresnillo, L. and Fruck, C. and Fujita, Y. and Fukazawa, Y. and Funk, S. and Gaebele, W. and Gabici, S. and Gadola, A. and Galante, N. and Gallant, Y. and Garcia, B. and Garcia Lopez, R. 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J. and Hassan, T. and Haubold, T. and Hauser, M. and Hayashida, M. and Heller, R. and Henri, G. and Hermann, G. and Herrero, A. and Hinton, James Anthony and Hoffmann, D. and Hofmann, W. and Hofverberg, P. and Horns, D. and Hrupec, D. and Huan, H. and Huber, B. and Huet, J. -M. and Hughes, G. and Hultquist, K. and Humensky, T. B. and Huppert, J. -F. and Ibarra, A. and Illa, J. M. and Ingjald, J. and Inoue, S. and Inoue, Y. and Ioka, K. and Jablonski, C. and Jacholkowska, A. and Janiak, M. and Jean, P. and Jensen, H. and Jogler, T. and Jung, I. and Kaaret, P. and Kabuki, S. and Kakuwa, J. and Kalkuhl, C. and Kankanyan, R. and Kapala, M. and Karastergiou, A. and Karczewski, M. and Karkar, S. and Karlsson, N. and Kasperek, J. and Katagiri, H. and Katarzynski, K. and Kawanaka, N. and Kedziora, B. and Kendziorra, E. and Khelifi, B. and Kieda, D. and Kifune, T. and Kihm, T. and Klepser, S. and Kluzniak, W. and Knapp, J. and Knappy, A. 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P. and Videla, M. and Vincent, P. and Vink, J. and Vlahakis, N. and Vlahos, L. and Vogler, P. and Vollhardt, A. and Volpe, F. and Von Gunten, H. P. and Vorobiov, S. and Wagner, S. and Wagner, R. M. and Wagner, B. and Wakely, S. P. and Walter, P. and Walter, R. and Warwick, R. and Wawer, P. and Wawrzaszek, R. and Webb, N. and Wegner, P. and Weinstein, A. and Weitzel, Q. and Welsing, R. and Wetteskind, H. and White, R. and Wierzcholska, A. and Wilkinson, M. I. and Williams, D. A. and Winde, M. and Wischnewski, R. and Wisniewski, L. and Wolczko, A. and Wood, M. and Xiong, Q. and Yamamoto, T. and Yamaoka, K. and Yamazaki, R. and Yanagita, S. and Yoffo, B. and Yonetani, M. and Yoshida, A. and Yoshida, T. and Yoshikoshi, T. and Zabalza, V. and Zagdanski, A. and Zajczyk, A. and Zdziarski, A. and Zech, Alraune and Zietara, K. and Ziolkowski, P. and Zitelli, V. and Zychowski, P.}, title = {Design concepts for the Cherenkov Telescope Array CTA an advanced facility for ground-based high-energy gamma-ray astronomy}, series = {Experimental astronomy : an international journal on astronomical instrumentation and data analysis}, volume = {32}, journal = {Experimental astronomy : an international journal on astronomical instrumentation and data analysis}, number = {3}, publisher = {Springer}, address = {Dordrecht}, organization = {CTA Consortium}, issn = {0922-6435}, doi = {10.1007/s10686-011-9247-0}, pages = {193 -- 316}, year = {2011}, abstract = {Ground-based gamma-ray astronomy has had a major breakthrough with the impressive results obtained using systems of imaging atmospheric Cherenkov telescopes. Ground-based gamma-ray astronomy has a huge potential in astrophysics, particle physics and cosmology. CTA is an international initiative to build the next generation instrument, with a factor of 5-10 improvement in sensitivity in the 100 GeV-10 TeV range and the extension to energies well below 100 GeV and above 100 TeV. CTA will consist of two arrays (one in the north, one in the south) for full sky coverage and will be operated as open observatory. The design of CTA is based on currently available technology. This document reports on the status and presents the major design concepts of CTA.}, language = {en} } @unpublished{AcharyaActisAghajanietal.2013, author = {Acharya, B. S. and Actis, M. and Aghajani, T. and Agnetta, G. and Aguilar, J. and Aharonian, Felix A. and Ajello, M. and Akhperjanian, A. G. and Alcubierre, M. and Aleksic, J. and Alfaro, R. and Aliu, E. and Allafort, A. J. and Allan, D. and Allekotte, I. and Amato, E. and Anderson, J. and Ang{\"u}ner, Ekrem Oǧuzhan and Antonelli, L. A. and Antoranz, P. and Aravantinos, A. and Arlen, T. and Armstrong, T. and Arnaldi, H. and Arrabito, L. and Asano, K. and Ashton, T. and Asorey, H. G. and Awane, Y. and Baba, H. and Babic, A. and Baby, N. and Baehr, J. and Bais, A. and Baixeras, C. and Bajtlik, S. and Balbo, M. and Balis, D. and Balkowski, C. and Bamba, A. and Bandiera, R. and Barber, A. and Barbier, C. and Barcelo, M. and Barnacka, Anna and Barnstedt, J{\"u}rgen and Barres de Almeida, U. and Barrio, J. A. and Basili, A. and Basso, S. and Bastieri, D. and Bauer, C. and Baushev, Anton N. and Becerra Gonzalez, J. and Becherini, Yvonne and Bechtol, K. C. and Tjus, J. 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T. and de Naurois, M. and de Oliveira, Y. and de Ona Wilhelmi, E. and de Souza, V. and Decerprit, G. and Decock, G. and Deil, C. and Delagnes, E. and Deleglise, G. and Delgado, C. and Della Volpe, D. and Demange, P. and Depaola, G. and Dettlaff, A. and Di Paola, A. and Di Pierro, F. and Diaz, C. and Dick, J. and Dickherber, R. and Dickinson, H. and Diez-Blanco, V. and Digel, S. and Dimitrov, D. and Disset, G. and Djannati-Ata{\"i}, A. and Doert, M. and Dohmke, M. and Domainko, W. and Prester, Dijana Dominis and Donat, A. and Dorner, D. and Doro, M. and Dournaux, J-L. and Drake, G. and Dravins, D. and Drury, L. and Dubois, F. and Dubois, R. and Dubus, G. and Dufour, C. and Dumas, D. and Dumm, J. and Durand, D. and Dyks, J. and Dyrda, M. and Ebr, J. and Edy, E. and Egberts, Kathrin and Eger, P. and Einecke, S. and Eleftheriadis, C. and Elles, S. and Emmanoulopoulos, D. and Engelhaupt, D. and Enomoto, R. and Ernenwein, J-P and Errando, M. and Etchegoyen, A. and Evans, P. and Falcone, A. and Fantinel, D. and Farakos, K. and Farnier, C. and Fasola, G. and Favill, B. and Fede, E. and Federici, S. and Fegan, S. and Feinstein, F. and Ferenc, D. and Ferrando, P. and Fesquet, M. and Fiasson, A. and Fillin-Martino, E. and Fink, D. and Finley, C. and Finley, J. 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F. and Vallania, P. and Vallejo, G. and van Driel, W. and van Eldik, C. and Vandenbrouke, J. and Vanderwalt, J. and Vankov, H. and Vasileiadis, G. and Vassiliev, V. and Veberic, D. and Vegas, I. and Vercellone, S. and Vergani, S. and Veyssiere, C. and Vialle, J. P. and Viana, A. and Videla, M. and Vincent, P. and Vincent, S. and Vink, J. and Vlahakis, N. and Vlahos, L. and Vogler, P. and Vollhardt, A. and von Gunten, H. P. and Vorobiov, S. and Vuerli, C. and Waegebaert, V. and Wagner, R. and Wagner, R. G. and Wagner, S. and Wakely, S. P. and Walter, R. and Walther, T. and Warda, K. and Warwick, R. and Wawer, P. and Wawrzaszek, R. and Webb, N. and Wegner, P. and Weinstein, A. and Weitzel, Q. and Welsing, R. and Werner, M. and Wetteskind, H. and White, R. and Wierzcholska, A. and Wiesand, S. and Wilkinson, M. and Williams, D. A. and Willingale, R. and Winiarski, K. and Wischnewski, R. and Wisniewski, L. and Wood, M. and Woernlein, A. and Xiong, Q. and Yadav, K. K. and Yamamoto, H. and Yamamoto, T. and Yamazaki, R. and Yanagita, S. and Yebras, J. M. and Yelos, D. and Yoshida, A. and Yoshida, T. and Yoshikoshi, T. and Zabalza, V. and Zacharias, M. and Zajczyk, A. and Zanin, R. and Zdziarski, A. and Zech, Alraune and Zhao, A. and Zhou, X. and Zietara, K. and Ziolkowski, J. and Ziolkowski, P. and Zitelli, V. and Zurbach, C. and Zychowski, P.}, title = {Introducing the CTA concept}, series = {Astroparticle physics}, volume = {43}, journal = {Astroparticle physics}, number = {2}, publisher = {Elsevier}, address = {Amsterdam}, organization = {CTA Consortium}, issn = {0927-6505}, doi = {10.1016/j.astropartphys.2013.01.007}, pages = {3 -- 18}, year = {2013}, abstract = {The Cherenkov Telescope Array (CTA) is a new observatory for very high-energy (VHE) gamma rays. CTA has ambitions science goals, for which it is necessary to achieve full-sky coverage, to improve the sensitivity by about an order of magnitude, to span about four decades of energy, from a few tens of GeV to above 100 TeV with enhanced angular and energy resolutions over existing VHE gamma-ray observatories. An international collaboration has formed with more than 1000 members from 27 countries in Europe, Asia, Africa and North and South America. In 2010 the CTA Consortium completed a Design Study and started a three-year Preparatory Phase which leads to production readiness of CTA in 2014. In this paper we introduce the science goals and the concept of CTA, and provide an overview of the project.}, language = {en} }