Mapping landscape connectivity under tectonic and climatic forcing

Abstract. Species distribution and richness ultimately result from complex interactions between biological, physical and environmental factors. It has been recently shown for a static natural landscape that the elevational connectivity, which measures the proximity of a site to others with similar habitats, is a key physical driver of local species richness. Here we examine changes in elevational connectivity during mountain building using a landscape evolution model. We find that under uniform tectonic and variable climatic forcing, connectivity peaks at mid-elevations when the landscape reaches its geomorphic steady-state 5 and that orographic effect on geomorphic evolution tends to favour low connectivity on leeward facing catchments. Statistical comparisons between connectivity distribution and results from a metacommunity model confirm that landscape elevation connectivity explains to the first order species richness in simulated mountainous regions. Our results also predict that low connectivity areas which favour isolation, a driver for in-situ speciation, are distributed across the entire elevational range for simulated orogenic cycles. Rapid adjustments of catchment morphology after cessation of tectonic activity should reduce 10 speciation by decreasing the number of isolated regions.

SPL (Eq. 1) allows us to simulate the main geomorphic characteristics of mountainous regions, in which landscape evolution is dominated by detachment-limited erosion regime (Whipple and Tucker, 1999).
In addition to riverine processes, soil creep (approximated by a diffusion law) is used to account for semi-continuous processes of soil displacement (Tucker and Hancock, 2010;Salles et al., 2018a): (2) 5 z is the local landscape elevation and κ d is the diffusion coefficient. This formulation assumes a linear dependency of superficial sediment transport with topographic gradient.
Accounting for the two processes defined above, the equation of mass conservation driving landscape temporal evolution is expressed as: where t is time and U is the rock uplift rate. It is worth noting that the landscape evolution scenarios presented in this study neglect spatial and temporal variations in tectonic evolution and rock strength, as well as the influence of sediment characteristics on river incision.
Precipitation patterns are known to impact geomorphic evolution at local (ridge-valley) to regional (full mountain range) scales (Anders et al., 2008;Bonnet, 2009). To estimate the controls of precipitation variability on topography evolution and on 15 associated landscape connectivity, the set of landscape evolution equations presented above are coupled with a linear orographic precipitation model (Smith and Barstad, 2004). The approach already implemented in Badlands (Salles et al., 2018b) only accounts for the first-order physics of orographic precipitation and computes rainfall under idealised climatic conditions defined by a specific wind velocity and direction (Anders et al., 2008) and assumes steady, uniform, and saturated air flow (Fig. 1a).
In the study, analysis of catchment dynamics are performed using river longitudinal profiles as well as χ plots and maps. χ 20 analysis is a method of extracting information from channel profiles that attempts to compare channels with different discharges (Perron and Royden, 2013). The longitudinal coordinate χ has dimensions of length and is linearly related to the elevation (Mudd et al., 2014). The quantity χ at any channel point depends on the river network geometry and estimates the dynamic state of river basins (Willett et al., 2014): In the first one a constant precipitation (1 m/yr) is applied, then in the second, an orographic precipitation model is used with constant wind speed (0.5 m/s) coming from the South. For both scenarios, the model is forced with an initial uplift phase (uniform rate of 1 mm/yr) through the first 5 Myr. b) Approach used to compute the closeness measure (Cji) required to quantify landscape elevational connectivity (LEC) based on the topography grid (e.g.,region A) defined in panel a). Two possible paths connecting site j to i (inset) are proposed with their corresponding elevation profiles. Associated costs are computed following Eq. 6 ( L r=2 (z kr − zj) 2 ). Despite a longer length, the cost associated to the red path is smaller than that of the blue one as it travels through sites with elevations more similar to zj (adapted from Bertuzzo et al. (2016)).

Landscape elevational connectivity
Landscape connectivity encapsulates the combined effects of (1) landscape morphological structure and (2) the species ability to move outside its usual niche width (Tischendorf and Fahrig, 2000). As such it is both species-and landscape-specific. Here, we generalise the concept and assume that any position in the simulated mountainous landscape corresponds to a particular habitat containing a pool of adapted species able to move in a limited elevation range up and down their initial and preferred 5 habitat elevation.
We chose to map landscape connectivity and its distribution by measuring the landscape elevational connectivity (LEC) proposed by Bertuzzo et al. (2016). This metric does not account for a specific species but rather focuses on a pool of species assuming a niche width that can be a percentage of the mountain elevation range or fixed. Here, we use the bioLEC Python package to measure the LEC index (Salles and Rey, 2019). The LEC is calculated on the evolving landscape obtained from 10 Badlands at discrete time intervals and measures how easily species living in other habitats can spread and colonize a given point.
Considering a 2D lattice made of N squared cells, LEC for cell i (LEC i ) is given by where C ji quantifies the closeness between sites j and i with respect to elevational connectivity. C ji measures the cost for a given species adapted to cell j to spread and colonise cell i. This cost is a function of elevation and evaluates how often species adapted to the elevation of cell j have to travel outside their optimal species niche width (σ) to reach cell i (Fig. 1b) assuming 5 that species niche is represented by a Gaussian function of the elevation.
Estimation of C ji requires computation of all the possible paths p from j to i and is defined as the maximum closeness value along these paths. Following Bertuzzo et al. (2016), C ji is expressed as: where p = [k 1 , k 2 , ..., k L ] (with k 1 = j and k L = i) are the cells comprised in the path p from j to i.

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Eq. 6 is solved for each cell j using Dijkstra's algorithm (Dijkstra, 1959) with diagonal connectivity between cells. The approach in bioLEC is based on scikit-image Dijkstra's algorithm (van der Walt et al., 2014). For each cell j, the algorithm builds a Dijkstra tree that branches the given cell with all the cells defining the simulated region. Edge weights are set equal to the square of the difference between the considered vertex elevation (z kr ) and z j . The least-cost distance between j and i is then calculated as the minimum sum of edge weights obtained from the cells along the shortest-path (Fig. 1b). 15 Calculation of LEC values over the entire simulated region (∼1 M points in this study) is slow. Here we use the parallel strategy available in bioLEC package where Dijkstra trees for all paths are balanced and distributed over multiple processors using message passing interface (MPI). Using this approach, LEC computation on the synthetic landscapes obtained in this study is less than 4 minutes when distributed over 240 processors.

Experimental setting 20
Our experimental design consists of a 100×100 km surface at a resolution of 100 m (Fig. 1a). The initial topography is a flat area over which random noise (≤ 1 m) is applied. To estimate landscape connectivity through a complete orogenic cycle, simulations are run for 10 Myr and an uniform uplift of 1 mm/yr is applied during the first 5 Myr (e.g mountain building phase) on all surface nodes with the exception of boundary points that remain fixed over the runs (Fig. 1a). A second phase, corresponding to the cessation of tectonic activity over the remaining 5 Myr, simulates the lowering of interfluves and the 25 erosional decay of the mountain system (e.g mountain relaxation phase).
In this study and for simplicity, the SPL parameters (Eq. 1) are set constant and do not change between simulations. We assign an uniform erodibility coefficient κ e of 8.e −6 /yr and exponents m and n are set to 0.5 and 1 respectively; these exponents values are commonly used for eroding fluvial systems (Whipple and Tucker, 1999;Ferrier et al., 2013). For the hillslope processes (Eq. 2), a constant diffusion coefficient of 0.1 m/yr is chosen.

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To estimate the influence of climate on geomorphic changes and in turns on landscape connectivity, we perform two simulations ( Fig. 1a) with (1) an uniform precipitation rate of 1 m/yr over the simulated 10 Myr and (2) an orographic precipitation model considering a prevailing wind direction from the South with a wind speed of 0.5 m/s and other orographic parameters set within the range proposed by Smith & Barstad (Smith and Barstad, 2004). In both cases, simulated mountain ranges are characteristic of dendritic, erosional landscapes.

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Computation of LEC over time requires the definition of species niche width (σ). In the study conducted here, we limit our analysis to the case where all species have the same niche width at specific time assuming a ratio σ/(z max − z min ) constant.
As the landscape changes through time, the elevation range [z min , z max ] is modified and so is species niche width. Therefore, we implicitly assume that characteristic response of landscape to tectonic and climatic forces happens on temporal scale much longer than the effective evolution and adaptation of individual species (Mokany et al., 2012;Steinbauer et al., 2016).

Connectivity distribution under uniform conditions
In this first set of results, we consider a geographic domain, free of environmental gradients, under a constant precipitation rate.
As the region is uniformly uplifted at a rate of 1 mm/yr during the first 5 Myr, landscape dissection by riverine and hillslope processes leads to valleys deepening and the development of self-organized and stable large drainage basins (Fig. 2a). 15 Following the initial orogenic phase of plateau uplift and landscape incision, rivers longitudinal profiles exhibit concave upward shape, a common signature of bedrock river systems (red lines in Fig. 3b). This typical shape is a direct outcome of the detachment-limited stream power law model and is the result of the integrated effect of tectonic, climatic and bedrock erodibility. After 4 Myr of evolution, the landscape has fully adjusted to the imposed constant climatic and tectonic forcing, as shown by the increasing linearity of rivers χ-plots (blue lines in Fig. 3b) (Perron and Royden, 2013). After the cessation of uplift at From an elevational niche perspective, all connectivity (e.g., migratory) paths on a flat landscape are equal. This is not the case on a complex landscape where connectivity can only occur along a network of corridors providing species with their elevational requirements (Smith et al., 2014;Elsen and Tingley, 2015). The mapping of spatial distribution of LEC ( Fig. 2a) 25 and associated gradients of LEC ( Fig. 3a & c) reveals a migration of maximum LEC regions -during the initial orogenic phase -from highest elevations (e.g, uplifted plateau) to mid-elevations as the landscape stabilises.
This redistribution leads to two regions of maximum LEC with the highest one attributed to the symmetrical nature of the simulated synthetic landscape. During the relaxation phase, the LEC peak migrates to lower elevations as the floor of the valleys widens (Fig. 2b). After dissection of the uplifted plateau, the model predicts that higher LEC are found at intermediate We also observe that, irrespectively of the scale of observation, LEC distribution follows a similar pattern for specific time intervals even if the considered domains traverse different elevational extent. For example, the result in Fig. 2c shows similar mid-elevations maximum LEC (i.e, peak of diversity) over both valley, catchment and regional scales.  Our results show that under uniform tectonic and climatic forcing, landscape dynamic exerts a first-order control on landscape connectivity distribution which is mostly distributed at mid-elevation and peaks on highest flanks when geomorphic steady state is reached (Fig. 3a thick

Orographic effect on patterns of landscape connectivity
To explore the influence of heterogenous precipitation on connectivity, we design a new set of experiments using a coupled climate and landscape evolution model where precipitation responds through space and time to the build up of topography (i.e, orographic precipitation, Fig. 4a & b).
In this experiment, a prevailing northward directed wind condition creates specific distribution of rainfall patterns across the 5 mountain range with precipitation maxima occurring predominantly on windward facing areas. Induced changes in hydrological regime drive drainage divides migration (Fig. 5a) and the development of asymmetric topography (Roe et al., 2003;Anders et al., 2008). Topography on the leeward side (rain shadow area) is formed by tectonic uplift with limited erosion, whereas topography on the windward side is predominantly erosional. Over geological time-scales, differential distribution of rainfall influences overall topographic evolution of the simulated mountain range. First, it affects river profiles by changing concavity 10 (Roe et al., 2003) and reducing erosional rates on the drier regions. As a consequence, decrease in discharge produces steeper slopes to compensate the imposed uniform uplift rate (Fig. 4c). Orographic rain also implies continuous disequilibrium conditions (Willett et al., 2014;Whipple et al., 2016) affecting river networks through reorganization and concomitantly changing the topologies and geometries of drainage basins (Fig. 4e).
Similar to the uniform precipitation model, we observe a temporal migration of LEC maximum from the uplifted plateau 15 towards the bottom of the valleys. However, we find some specific features driven by the geomorphic responses to orographic precipitation (as shown by the LEC distribution at steady state between Fig. 2a and Fig. 4d) with a clear correlation between sites with high/low connectivity areas and windward/leeward facing catchments. It shows how uplift and its effect on regional climate influence landscapes connectivity with development of geographic connections or barriers as topography changes.
The study of two specific catchments sharing a common drainage divide highlights further these effects. In Figure 5, we 20 note that both leeward and windward catchments exhibit similar hump-shaped patterns of LEC, indicative of mid-elevation peaks, with higher connectivity on the windward facing area compared to the leeward facing one. Temporal evolution analysis through the complete orogenic cycle shows optimum landscape connectivity during the mountain building phase at mid-to high-elevations as illustrated by the broader ranges of LEC values at 2.5 Myr compared to the ones at 5.5 Myr (Fig. 5b).

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The results described above quantify the temporal and spatial evolution of landscape connectivity patterns during a complete orogenic cycle considering both uniform and orographic precipitation scenarios. In this discussion section, we build upon the work from Bertuzzo et al. (2015Bertuzzo et al. ( , 2016. First, we test the influence of different boundary and species niche width conditions on landscape connectivity. Then, we explore the relationship between landscape elevational connectivity and biodiversity using a similar metacommunity model as the one proposed in Bertuzzo et al. (2016) and discuss the possible roles of geomorphological 30 changes on patterns of species richness. By defining isolated regions as places with low connectivity, we then analyse how they evolve during simulated orogenic cycles. Normalised LEC for points belonging to the windward and leeward catchments (C1 and C2 respectively) are highlighted. The normalised LEC exhibits a typical pattern with higher values and broader ranges during mountain building phase at mid to high elevations.

Impact of forcing conditions and species niche width on connectivity mapping
In our experimental setting, we have deliberately chosen a simple model of evolving landscape similar to existing analogue and numerical models (Bonnet and Crave, 2003;Bonnet, 2009;Willett et al., 2014;Salles and Hardiman, 2016). Under such conditions, the resulting landscape is symmetric with the formation of a mountain range composed of four low angled ridges ending at the four corners of the model. In this section, we modify slightly these initial tectonic boundary conditions and presents the normalised connectivity map for the two width ratios and for the three regions.
The general pattern of geomorphological evolution under uniform precipitation is presented in Fig. 6a for the first 5 Myr and it corresponds to the mountain building phase. As for the previous cases, the evolution of the experiment involves a growth phase followed by a steady-state phase (Bonnet and Crave, 2003;Castelltort and Yamato, 2013). During the initial plateau uplift (e.g., growth phase), some topographic incisions form along the western open border of the model. As uplift continues, these incisions grow and propagate inward until there is complete dissection of the plateau (third map on the right hand side of 5 Fig. 6a). The obtained fluvial landscapes display dendritic networks and rivers longitudinal profiles present a concave upward shape characteristic of bedrock river systems (as for Fig. 3b).
To evaluate the impact of these new boundary conditions on connectivity calculation, we compute the LEC at steady state ( Fig. 6b) over the entire domain and for three quadrants (Fig. 7). In addition, we test two values of 0.1 and 0.2 respectively for the species niche width ratio (σ/(z max − z min )) defined in Eq. 6. As shown in the results (section 3) and for the Swiss 10 Alps in Bertuzzo et al. (2016), the frequency distributions of the elevation is hump-shaped regardless of the spatial extent of the considered domain (red lines representing the entire domain in Fig. 6 or three smaller regions in Fig. 7). From the results presented in Fig. 7, we find that connectivity distribution varies significantly with respect to variations of niche width σ. As the niche becomes wider (higher σ), the connectivity maps ( Fig. 6c and 7c) reveal a clear spatial pattern with valleys and mountain tops characterized by lower LEC (Bertuzzo et al., 2016). As σ increases, any point on the map is less constrained by elevational 5 barriers, and thus LEC is mostly controlled by the abundance of sites with similar elevation in the simulated domain (i.e., the elevation frequency distribution as shown by the blue lines in Fig. 6c and 7b). Bertuzzo et al. (2016) show that for very large σ, LEC becomes insensitive to elevation and elevational gradients tend to flatten out. Bertuzzo et al. (2016) have shown that when applied to real landscapes, the LEC metric predicts well the α-diversity simulated 10 by full metacommunity model. Here we perform a similar analysis on our simulated landscape and we estimate for both scenarios (uniform and orographic rain) the correlations between LEC and simulated local species richness (α diversity).

LEC as a measure of biodiversity
To do so, we use a zero-sum metacommunity model (Hubbell, 2001) where local communities (N ) are defined on an regular 2D elevation mesh. The zero-sum assumption states that each local community is saturated at all time, which means that the total number of individuals n in a particular point is constant over time. In such case and for any given time, the entire region 15 is made of a population of N · n individuals where N is equivalent to the number of points on the grid. The population number is made of different species which have different elevational niches. Each of these niches describes the competitive ability of particular species with elevation and are defined with a Gaussian function following Rybicki and Hanski (2013) (Bertuzzo et al., 2016): with f i (z) the competitive ability of species i at elevation z. The elevation z opt i is the optimal elevation for which the competitive ability equals f maxi and σ i is the niche width for species i as defined in Eq. 6. In addition to the zero-sum assumption, we suppose that all species have the same niche width σ i = σ and maximum competitive ability f maxi = f max as well as similar rates of dispersal, death and fertility.
The ecological interactions between individuals follow the same approach as the one proposed in Bertuzzo et al. (2016). For individual belonging to a new species that does not already exist in the system. This second option is probabilistically selected at every time step and allows us to model both speciation and immigration from external communities (Hubbell, 2001; Chave orographic precipitation b). The α diversity patterns result from the zero-sum metacommunity model described below. Correlations between α diversity and LEC are presented (blue dots) as well as regression and kernel density fits for each case. We also provide the resulting Pearson's coefficients for correlation between α diversity and LEC values. et al., 2002). When a competitor from a new species enters the system its optimal elevation z opt i is drawn from a uniform distribution spanning twice the relief of the system to avoid edge effects (Bertuzzo et al., 2016).
This metacommunity model is applied on the elevation grids obtained from our landscape evolution model. In all simulations, the system is initially populated by one single species and is ran until a statistically steady state is reached (∼ 10 4 generations, where a generation is N ·n time steps). As in Bertuzzo et al. (2016), we consider periodic boundaries conditions. The parameter 5 f max does not affect the system dynamics and is, without loss of generality, set to 1. Fig. 8 presents the relationships between calculated LEC and local species richness for the simulated landscapes at steady state.
Overall we have Pearson's correlations (R) >70% which is considered to be relatively strong. These results are in agreement with Bertuzzo et al. (2016) study and consolidate the idea that the LEC calculation is able to predict well the α diversity especially in the case of the uniform rainfall. Therefore if LEC captures the regional variability of communities diversity one 10 can deduce from its distribution the temporal and spatial evolution of species richness.
We provide in Fig. 9 a statistical summary of the LEC evolution for the two climatic scenarios. LEC predicts biodiversity peaks when the landscape reaches a geomorphological steady state, and maximum species richness is observed at mid-elevation ( Fig. 9a -0.7 < z/z max < 0.9) as observed in nature (Grytnes and Vetaas, 2002;Colwell et al., 2004;Brehm et al., 2007).
Interestingly, when using a coupled climate-landscape model, windward facing regions host higher biodiversities. During relaxation phase, when tectonic forcing ceases, peak in species richness shifts from mid to low-elevations (bottom graph in Fig. 9a). From the figure, we infer that mapped areas showing strong connectivity values (i.e., high LEC), within a given elevational band, have a direct effect on the biodiversity they host (Rahbek, 1997;McCain, 2007). We also hypothesise that these areas represent regions of high local species richness as local communities can be gathered from a more diverse regional pool of species that are fit to live at a similar elevation (Romdal and Grytnes, 2007).

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In summary, LEC calculation can be used to estimate in a simple way the temporal and spatial evolution of biodiversity distribution induced by changes in landscape structure over geological time. Based on LEC distribution at steady state, we found that species richness in mountainous landscapes reaches its peak at mid-elevation not only because this is where the maximum surface area available to species is located, but also because species can move up or down to accommodate climate warming or cooling respectively.

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There are many biologic and abiotic properties that drives species richness in mountainous landscapes (Hoorn et al., 2010(Hoorn et al., , 2013Giezendanner et al., 2019). For example, mountains provide species with a rich variety of environmental conditions over restricted surface areas (e.g. range of temperature, solar irradiation, wind exposure, moisture and rainfall, soils thickness and composition to cite a few). In this study, we have limited our exploration to the role of morphological changes imposed by uniform tectonic, riverine and climatic processes and we found that these changes set alone could explain to the first order the 5 biodiversity found in mountainous regions.

Dynamic of geomorphic-driven isolation
From the LEC values, one can derived geomorphic-driven isolation by finding spatial regions of low LEC compared to their surrounding areas. Here, we apply an approach similar to a depression-filling algorithm (Barnes and Lehman, 2013) using the LEC values instead of the elevation. Isolated areas in that sense, represent depressions or inwardly-draining regions of the LEC 10 map which have no outlet. To prevent coalescence of these isolated regions (i.e, small depressions within bigger ones), one can apply a threshold on the filling limit of the LEC map. Increasing such threshold produces a smaller number of isolated regions but with larger areas.
In Fig. 10, we evaluate through time these areas of low LEC values (normalised LEC below 20%) and analyse series of metrics: mean LEC, mean area and mean elevation. Our results show that the competition between mountain-building and 15 erosion increases the number of isolated regions during the orogenic phase (Fig. 10a). Orographic precipitation fosters faster isolation than the uniform precipitation model (red lines trends in Fig. 10a) especially on the steeper and drier leeward sides (rain shadow zones) of the drainage divides (Fig. 10b). For the uniform rain model, we observe a decrease in the average area of these isolated regions concomitant with catchments stabilisation and emergence of the steady state (light grey line in Fig. 10a top graph). For both precipitation scenarios, the cessation of tectonic activity at 5 Myr results in a rapid decrease in 20 the number of isolated regions associated with an initial episode of augmentation of mean area that last no more than 250,000 years. We attribute this peculiar effect to the fast widening of valleys high-and mid-elevation zones related to the adjustment of catchments morphology and induced by the advective slope retreat predominant across the valley heads (Pelletier, 2011). Hence, our model predicts an increase in isolation during the mountain building phase, and a decrease during the relaxation phase. 25 Based on the results from section 4.2 and as high LEC regions represent -to the first order -places of higher biodiversity, we could take the argument further and propose that low LEC areas should potentially correspond to places where species get trapped into isolated refuges and such ecological niches should favour speciation and endemism.
Not surprisingly, it has been found that the potential for isolation increases in more topographically diverse areas (Ali and Aitchison, 2014;Gillespie and Roderick, 2014). In recent years, several studies have shown that isolation induced by uplift 30 and climatic processes plays a central part in shaping biodiversity (Wang et al., 2009;Craw et al., 2015) and mapping of geomorphic-driven low landscape connectivity could potentially highlight these areas of speciation hotspots. Therefore the LEC calculation could provide an efficient way to identify and manage regions of higher conservation value. Studies have predicted higher endemism at higher elevation as a consequence of increasing isolation with elevation (Steinbauer et al., 2016(Steinbauer et al., , 2018. We see similar trend with high-elevation zones less connected from each other and statistically smaller than lower-elevation ones. However, our results also suggest that low connectivity regions form fragmented patches that are distributed across the entire elevational range during an orogenic cycle (z mean in Fig. 10a). Several other parameters and mechanisms not accounted for in this study will promote spatial variations in speciation rates including temperature or 5 biotic interactions (Emerson and Kolm, 2005;Brown, 2014). Nevertheless, it shows that when considering the morphological complexity of mountainous landscapes over geological time, zones of low connectivity are not distributed continuously over elevation gradients and the associated isolated regions will likely be found at different elevations. Therefore the prediction of increasing endemism with higher elevation might not always be the rule.

Conclusions
This paper presents a methodology to quantify landscape connectivity under tectonic and climatic forcing. Over geological time scales (million years), tectonics and surface processes conspire to transform flat regions into complex dissected moun-5 tainous landscapes. We used the landscape elevational connectivity (LEC) to measure the connectivity between sites of similar elevations (Bertuzzo et al., 2016). We show that this abiotic parameter is able to account for up to 80% of the α diversity predicted by a zero-sum metacommunity model (Hubbell, 2001;Rybicki and Hanski, 2013) and therefore it could potentially explain the first order distribution of biodiversity found in mountainous regions (Ali and Aitchison, 2014;Steinbauer et al., 2018). In the future, we can easily improve the predictive capacity of this metric by integrating fitness parameters other than 10 elevation.
From the LEC calculation, one can quantify the role of geomorphology on landscape connectivity and topography-driven isolation. As the periodicity of isolation and connection dictates evolutionary outcomes, understanding of this dynamic might be used to test models of biological diversification, and to understand species distribution and biodiversity patterns through time. Our results suggest that peaks in species richness for mountainous landscapes can be derived from the analysis of the 15 dynamic organisation of geomorphic features as they evolved in response to tectonic, climatic and erosion processes. These features might be inferred from physiographic metrics such as χ maps, in-situ observations, river longitudinal profiles or landscape evolution modelling. We also found that geomorphic-driven isolation has the potential to increase rates of speciation over the entire elevational range. This is an important outcome that could potentially lead to reassessment of the spatial viability of existing conservation sites and could help us improve future conservation planning, policy and practice (Mokany et al., 2012). 20 Code and data availability. The results and data presented and discussed in this paper were simulated using Badlands model and the connectivity maps were obtained from bioLEC Python package. All the model outputs were visualised using Python Matplotlib library for standard graphics, Seaborn data visualization library for statistical graphics and the Paraview software (V 5.2.0) from Kitware, Sandia National Labs and CSimSoft for 3D graphics and 2D maps.
Author contributions. T.S., development of the code, design of the experiment, output analysis, and manuscript writing; P.R., output analysis