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Other external factors also influence the bathymetry, e.g. Kirschner et al., 2010 Celerier, 1988 Sclater and Christie, 1980). In addition, during sediment deposition, the bathymetry itself changes due to different processes, such as the loading of accumulated sediments, thermal subsidence acting on extended continental crust, or subsidence or uplift induced by mantle dynamics (dynamic topography) or sea level changes (e.g. The numerous oceanic deep-drilling campaigns that occurred over the past decades have the potential to constrain such reconstructions, but this is not the case when part of the information has been eroded and/or reworked during geological time by other tectonic or climatic processes. Reconstructing past topographies and bathymetries is fundamental for paleoclimate and paleo-ice-sheet simulations (e.g. Nevertheless, simulating and reconstructing past climatic conditions can bring useful hints as to how the future climate might evolve and also help in narrowing the range of likely long-term carbon emissions trajectories. Going back to those times (or even before), it is likely that the tectonic setting responsible for other boundary conditions, such as oceanic gateways, elevation of mountain ranges, continental margin expansion, and the location and extent of continental masses themselves, differed from that of the present-day (e.g. larger than 400 ppm for atmospheric CO 2, can only be found for times prior to 3 million years ago (e.g. GHG concentrations higher than present-day or future levels, i.e. It allows for the testing of the response of the Earth's climate under different but realistic atmospheric greenhouse gas (GHG) concentrations (e.g. At this point, the exercise becomes difficult, and this is when reconstructing past climates becomes important. Golledge et al., 2015 DeConto and Pollard, 2016). Projecting to such timescales implies designing corresponding realistic carbon emission trajectories, and so far millennial-scale emissions trajectories are just extension of existing emission scenarios beyond 2100 (e.g. Their main response has yet to be observed and is likely to happen beyond the 21st century, which is encouraging climatologists to project changes on longer timescales that cover centuries to millennia into the future (e.g. Colleoni et al., 2018 b Noble et al., 2020), despite already showing evidence of changes over the past few decades ( Caesar et al., 2021). the deep ocean, the carbon cycle, and the ice sheets and glaciers, react more slowly to climate changes (e.g. However, some of the climatic variables, e.g. The Coupled Model Intercomparison Project (CMIP), now ending phase 6 ( Eyring et al., 2016), has been producing a large amount of climate projections that extend to 2100. the Shared Socio-economical Pathways by Riahi et al., 2017). Ongoing climate changes are urging the scientific community to project future climate evolution in response to carbon emission trajectories (e.g. PALEOSTRIP has been designed to be modular and to allow users to insert their own implementations. In the following, we detail the physics embedded within PALEOSTRIP, and we show its application using a drilling site (1D), a transect (2D), and a map (3D), taking the Ross Sea (Antarctica) as a case study. It includes 3D flexural isostasy, 1D thermal subsidence, and possibilities to correct for prescribed sea level and dynamical topography changes. As such, all physical parameters can be modified from the GUI. PALEOSTRIP comes with a graphical user interface (GUI) to facilitate computation of sensitivity tests and to allow the users to switch all the different processes on and off and thus separate the various aspects of backtracking.
#Flex2d geodynamics reference software
To fill this gap, we present PALEOSTRIPv1.0, a MATLAB open-source software designed to perform 1D, 2D, and 3D backtracking of paleo-bathymetries. The geological community lacks a complex open-source tool that allows for community implementations and strengthens research synergies. 10.Paleo-bathymetric reconstructions provide boundary conditions to numerical models of ice sheet evolution and ocean circulation that are critical to understanding their evolution through time. Estimate of three-dimensional flexural-isostatic response to unloading: Rock uplift due to late Cenozoic glacial erosion in the western United States. Quantitative Modeling of Earth Surface Processes.