the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
Computing water flow through complex landscapes – Part 3: Fill–Spill–Merge: flow routing in depression hierarchies
Richard Barnes
Kerry L. Callaghan
Andrew D. Wickert
Depressions – inwardly draining regions – are common to many landscapes. When there is sufficient moisture, depressions take the form of lakes and wetlands; otherwise, they may be dry. Hydrological flow models used in geomorphology, hydrology, planetary science, soil and water conservation, and other fields often eliminate depressions through filling or breaching; however, this can produce unrealistic results. Models that retain depressions, on the other hand, are often undesirably expensive to run. In previous work we began to address this by developing a depression hierarchy data structure to capture the full topographic complexity of depressions in a region. Here, we extend this work by presenting the Fill–Spill–Merge algorithm that utilizes our depression hierarchy data structure to rapidly process and distribute runoff. Runoff fills depressions, which then overflow and spill into their neighbors. If both a depression and its neighbor fill, they merge. We provide a detailed explanation of the algorithm and results from two sample study areas. In these case studies, the algorithm runs 90–2600 times faster (with a reduction in compute time of 2000–63 000 times) than the commonly used Jacobi iteration and produces a more accurate output. Complete, wellcommented, opensource code with 97 % test coverage is available on GitHub and Zenodo.
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Depressions (see Lindsay, 2016, for a typology) are inwardly draining regions of a digital elevation model (DEM) that lack any outlet to an ocean or other designated base elevation. Depressions occur naturally and can be formed by glacial erosion and/or deposition (Breckenridge and Johnson, 2009), compressional and/or extensional tectonics (Reheis, 1999; Hilley and Strecker, 2005), and cratering (Cabrol and Grin, 1999). They often host lakes and wetlands by retaining water locally. Depressions may themselves contain depressions. Such regions confound algorithms for geomorphological and terrain analysis, as well as those for hydrological modeling, because many such algorithms simply route water down topographic slope following the local gradient: depressions neither fill with water nor drain.
Many hydrological models deal with the complexity of depressions by removing them. This can be done by filling the depressions with earth so that they form a flat region of landscape (e.g., Jenson and Domingue, 1988; Martz and de Jong, 1988), breaching (Martz and Garbrecht, 1998) or carving them (Soille et al., 2003) so that water flows from their lowest point through the carved channel and onward to downstream regions, or some combination of these (Lindsay and Creed, 2005b; Schwanghart and Scherler, 2017; Soille, 2004; Lindsay, 2016). This approach is justified for situations in which spatiotemporal aspects of the analysis allow depressions to be ignored or for cases in which all depressions can be considered to be data errors (Lindsay and Creed, 2005a). Historically, many DEMs were constructed from sparse data, and small data errors produced depressions, especially in flat areas (O'Callaghan and Mark, 1984). Such an assumption is no longer justified, as improved and increasingly highresolution data have become available (Li et al., 2011). Even coarseresolution data are capable of resolving realworld depressions (e.g., Riddick et al., 2018; Wickert, 2016). With this in mind, new approaches are beginning to be examined, particularly in postglacial landscapes where depressions have a significant impact on local hydrology (e.g., Lai and Anders, 2018) and therefore cannot be ignored during modeling.
FlowFill (Callaghan and Wickert, 2019) began to combat this problem by routing water across landscapes in a way that conserved water volume, creating flowrouting surfaces that could still contain real depressions. Under reasonable runoff conditions, the results show landscapes that still contain depressions and disrupted flow routes. The FlowFill method iteratively routes water from higher to lower terrain. As depressions fill, they pose an extreme challenge to such a method: since water seeks a level surface, the surface of a filled depression must eventually become flat and any fluid flowing onto the surface diffuses across it. Even for moderately sized surfaces it can take many iterations for a solver to reach steady state; we provide a theoretical analysis of this in Sect. 4.1. Runtimes for FlowFill ranged from seconds to days: large datasets quickly became unwieldy. Of those examples tested by Callaghan and Wickert (2019), the slowest was a dataset of 4 176 000 cells, which took approximately 33 h for FlowFill to process. In contrast, the Fill–Spill–Merge algorithm presented here fills a similarly sized dataset in 8.7 s.
Other authors have considered the problems of extracting nested depression hierarchies and dynamically routing water through them. However, these previous approaches are slow, inexact, or both; additionally, most previous efforts were not accompanied by source code, limiting their utility. Barnes et al. (2020) provide a more thorough literature review, which we briefly recap here. A hierarchical segmentation by Beucher (1994) did not produce a data structure on which flow could be routed. Salembier and Pardas (1994) generated a hierarchical segmentation by repeatedly simplifying source images; hydrologically speaking, this can lead to unacceptable degradation of terrain information. Arnold (2010) developed an algorithm similar to the one here but without source code; the algorithm also generates looping topologies that require correction. Wu et al. (2015) and Wu and Lane (2016) constructed depression hierarchies by first smoothing a DEM and then extracting vector contour lines from it. Wu et al. (2018) built on this approach by discretizing the DEM into a number of horizontal slices. Both approaches sacrifice exactness and the latter requires O(N^{2}) time. Cordonnier et al. (2019) used planargraph minimum spanning trees to construct a hierarchy of depressions but did not produce a data structure water can be routed on. In contrast, the Fill–Spill–Merge algorithm relies on a welldefined data structure (Barnes et al., 2020); has complete, wellcommented source code with extensive correctness tests (Barnes and Callaghan, 2019, 2020); has strong efficiency guarantees (Sect. 4.1), which are realized on actual and simulated datasets (Sect. 4.2); and provides exact answers.
To achieve this, we developed a data structure – the depression hierarchy – which represents the topologic and geographic structure of depressions. In an accompanying paper, we provide details concerning how a depression hierarchy is constructed (Barnes et al., 2020). In this paper, we explain how a depression hierarchy can be leveraged to accelerate hydrological models using a paradigm we call Fill–Spill–Merge.
Many of the techniques in this paper are based on binary tree data structures and their traversals. Although we define terms below, more complete explanations and visual examples can be found in the text for any introductory undergraduate course on data structures. We recommend Skiena (2008) and Sedgewick and Wayne (2011) as good references. In particular, a good understanding of recursion will be helpful.
2.1 Terminology
Depressions can themselves contain depressions, as shown in Fig. 1. A depression hierarchy (DH) is a data structure representing a forest of binary trees, as shown in Fig. 2a, that represents the relationships between depressions (Fig. 2a–d). Each node in the DH represents a depression. Nodes higher in the DH are depressions that themselves contain depressions; we term these metadepressions. Although the depression hierarchy could be generalized to nary trees using multiple flow direction routing, the binary simplification is sufficient to cover most use cases. A node in the DH can have several classifications.

A parent is a node, such as no. 10 and no. 12 in Fig. 2a, that represents a metadepression and whose topological descendants therefore also form depressions.

A child is a depression, such as both no. 10 and no. 1 in Fig. 2a, that geographically and topologically exists within the metadepression formed by its parent.

A leaf is a depression, such as no. 1 and no. 2 in Fig. 2a and d, that has no children. The leaves of the binary trees represent the smallest, most deeply nested depressions. If a landscape were initially devoid of water, then water flowing down slopes would begin to collect in some subset of these leaf depressions before it would begin to fill their parent depressions.

A root is a depression, such as no. 0, no. 11, and no. 12 in Fig. 2, that has no parent. This term may also refer to any node that is used as the starting point for a traversal that only considers the node and its descendants.

A descendant is a child of a given parent or the child of a child of that parent and so on. In Fig. 2a, no. 1, no. 2, no. 3, and no. 10 are all descendants of no. 12.

Every node has either no children (leaf nodes) or two children. Nodes that share a parent are siblings. In Fig. 2a, no. 1 and no. 2 are siblings, as are no. 4 and no. 5.
As depressions fill, their water surfaces eventually reach a spill elevation (Fig. 2e) at which they overflow into neighboring depressions. During this spilling, water flows from a depression into a geographically neighboring leaf depression, topologically connected by a geolink. The spill elevations in Fig. 1 are the highest points of each band of color.
Each node in the DH is associated with several properties.

Depression volume. The depression volume is the total volume of water that the depression, including all of its descendants, can contain before spilling over.

Water volume. The water volume is the total volume of water actually being stored in the depression. A parent depression will have a nonzero water volume only if both of its children are completely full and the parent itself contains some additional volume of water. In this case, the water volume will be the sum of the water volumes of the children and the additional margin of water contained within the parent (i.e., the “marginal volume” indicated in Fig. 2e). Parents whose children are not both filled with water will have a water volume equal to zero. In this way, we can use this property to determine which portions of the DH are fully or partially filled and which are the highest watercontaining nodes in any of the binary trees.

Geolinks. When a depression spills, its water passes into the subtree rooted by its sibling. However, in a full model of flow, the water would move downslope from the spill cell into whichever leaf depression of the sibling is geographically proximal to the spill cell. Geolinks are pointers from depressions higher in the DH to the leaf depressions that receive their water if they overflow. These are the dashed lines shown in Fig. 2a. Geolinks are similar to the connections used in a threaded binary tree (Fenner and Loizou, 1984).

Oceanlink. Depressions high in the mountains may overflow down escarpments to depressions far below. In this case, the depressions do not overflow into each other: the relationship is oneway. There can be multiple such escarpments, so this can happen multiple times. In such cases, each group of depressions forms a proper binary tree. However, the root of one of the trees has an oceanlink to a leaf node of the downstream binary tree. In Fig. 2, both no. 11 and no. 12 are the root nodes of a set of nested depressions. No. 12 has an oceanlink (heavy arrow) to no. 4, one of the leaf depressions of no. 11. No. 11 itself has an oceanlink to the ocean. In many of the algorithms discussed below, oceanlinked nodes are processed similarly to children.
Within the algorithm, oceanlinks and geolinks are used for different purposes: an oceanlink tells us that the depression in question has grafted onto the leaf node of another tree of the depression hierarchy, locating a route for overflowing water to eventually reach the ocean. The depression to which it is oceanlinked is considered its parent, but it is not the child of that depression because water flows only one way along an oceanlink. In Fig. 2a, depression no. 4 can be considered the parent of no. 12, but no. 12 is not the child of no. 4. This is because no. 12 is not physically contained within no. 4, but no. 12 will send all of its overflowing water to no. 4, as shown in Fig. 2b–e. No. 4 will not contain the total water volume contained within no. 12, unlike other parents. Geolinks route water within geographically adjacent depressions contained in the same metadepression.
2.2 Traversals
With these linkages in place, we can consider various ways of traversing the trees. Given a binary tree T with left and right children T.L and T.R, a breadthfirst traversal considers both T.L and T.R before considering $T.L.L$, $T.L.R$, $T.R.L$, or $T.R.R$. A depthfirst traversal, on the other hand, will consider T.L and all of its descendants before considering T.R or any of its descendants. The tree traversals we perform in this paper are all depthfirst.
Depthfirst traversals are most naturally expressed via recursion and come in three types: in order, preorder, and postorder. Let a recursive traversal function be called r(⋅) and the processing we perform on a particular node in the tree p(⋅); then the traversals are given by the following:

in order – r(T.L) then p(T) then r(T.R);

preorder – p(T) then r(T.L) then r(T.R);

postorder – r(T.L) then r(T.R) then p(T).
The Fill–Spill–Merge algorithm consists of several steps that are outlined here, depicted in Figs. 3 and 4, and shown in flowchart form in Fig. 5. This paper is also accompanied by complete, wellcommented source code; the reader may find it helpful to download this code and refer to it as an additional reference. First (Sect. 3.1), surface water needs to move downhill either to the ocean (i.e., a designated sink region or the map edge) or to collect in pit cells – the deepest points within leaf depressions. Note that the landscape may already have standing water at this stage. This operation takes place across all the cells of the DEM. Second (Sect. 3.2), water is redistributed across the depression hierarchy such that any depressions that have filled sufficiently spill over into neighboring depressions and, if both depressions are full, flood their parent to merge into a single, larger body of water within a metadepression. This operation is done without explicitly considering the cells of the DEM, which makes it very fast. Third and finally (Sect. 3.3), the water within the depression hierarchy is translated into an extent and depth of flooding across the topographic surface (DEM).
Computing a depression hierarchy (Barnes et al., 2020) is a necessary precursor to running Fill–Spill–Merge. The specific outputs from the depression hierarchy algorithm that are used in the Fill–Spill–Merge algorithm are the following.

DH is the depression hierarchy itself.

Flowdirs is a matrix of flow directions, indicating which of a cell's neighbors receives its flow. Because PriorityFlood (Barnes et al., 2014) is used to generate the depression hierarchy, flat areas are automatically resolved.

Labels represent a matrix indicating the leaf depression to which each cell belongs.
By routing water according to the DH, we significantly accelerate the compute speed and ensure that the full network of depressions is a topologically correct directed tree. Each of the following subsections details one of the numbered steps along the central path of the flowchart shown in Fig. 5.
3.1 Move water downhill to pits
We route water in a similar way as standard flow accumulation algorithms (Mark, 1988; Wallis et al., 2009; Barnes, 2017), but for completeness we summarize our approach here. Flow directions for each cell have already been identified by the depression hierarchy algorithm. Each cell calculates how many of its neighbors flow into it. We call this value the cell's dependency count, as it describes the number of immediate upstream cells whose flow accumulation must be resolved before flow accumulation at the given cell can be computed. Local maxima in the DEM are identified as those cells that receive no flow from any neighbor. These local maxima are placed in a queue. Cells are then popped (i.e., noted while being removed) from this queue. The cells determine how much flow they generate locally (perhaps referring to a matrix of rainfall values, but also including existing stores of standing water) and add this to their flow accumulation value. They then add their flow accumulation to their downstream neighbor's and set their own flow accumulation value to zero. The neighbor's dependency count is then decremented. If the neighbor's dependency count has reached zero during this step, it is added to the end of the queue. This process of accumulating flow, passing it downstream, decrementing the dependency count, and adding cells to the queue continues until the queue is empty, at which point every cell on the map has been visited and any water has been moved downslope. Braun and Willett (2013) present an alternative formulation based on a depthfirst traversal, but Barnes (2019) demonstrates that a breadthfirst ordering, such as that presented here, is better suited to parallelism.
When the accumulated flow reaches the pit cell of a depression, the downhilldirected flow routing stops because there is no downhill neighbor to receive the flow. At this point, all of the flowaccumulated water in the pit cell is moved into the pit cell's associated leaf depression in the DH. That is, the water is moved out of the geographic space and into the topologic space. This then enables massconserving depression flooding via rapid Fill–Spill–Merge calculations, as detailed below.
3.2 Overflow and merge depressions
At this point, the Fill–Spill–Merge algorithm has routed all of the surface water into either the ocean or into the leaf nodes of the DH. The next step is to redistribute this water through the DH to nodes with enough volume to contain the water and to send any excess water to the ocean. This set of operations can be performed entirely in the depression hierarchy without reference to the digital elevation model.
Intuitively, the process of filling, spilling, and merging can be visualized as occurring from leaf nodes to their parents (Fig. 3). When a leaf depression initially contains more water than it can hold, the water will be redistributed by spilling over into the neighboring depression. If this neighboring depression is already full, then the excess water must pass to the parent of both the depression and its neighbor. This process continues recursively until either the supplied water is exhausted or this water reaches the ultimate parent, the ocean. In this latter case, all excess water is dropped from the model and the ocean is unaffected.
To effect the intuition developed above, we need a welldefined way to visit all of the nodes in the depression hierarchy. A postorder traversal allows us to visit both of a node's children and their descendants before calculating any quantities on the node itself. The result is that leaves get processed before their parents. However, a single traversal is insufficient: we need one traversal (the “outer traversal”) to identify nodes that have excess water and another traversal (the “inner traversal”) to distribute this water. The outer traversal may launch the inner traversal many times as it works its way up the hierarchy. Pseudocode showing these traversals is available in Sect. 6.1 and 6.2.
To efficiently redistribute water, the Fill–Spill–Merge algorithm performs nested depthfirst traversals of the DH. The outer traversal (Sect. 6.1) is postorder and considers each metadepression in turn, from the most deeply nested to the least. For each metadepression, an inner traversal (Sect. 6.2) handles its overflows by moving water to its sibling (starting by filling the sibling's descendants) and, if there is any left, passing it to the depression's parent. In this way, the outer traversal maintains an invariant (a property which is true before and after each call to a function): any metadepression it has processed does not contain an overflow. Put another way, the outer traversal finds problems and the inner traversal fixes them.
The outer traversal of the DH (which is, after all, a forest of binary trees) begins with the ocean. For each depression, the algorithm first recurses into its oceanlinks, if any, and then into the left and then right child. In the postorder portion of the traversal (which starts from the leaves and moves back up through the depression hierarchy), the algorithm identifies any depressions containing more water than they can accommodate. This process continues until the recursion returns to the ocean, at which point any additional water is assumed to be added to the ocean without impacting sea level, though this total discharge to the sea is recorded within the “ocean” depression.
When an overfilled depression is located by the outer traversal above, its water needs to be redistributed to neighboring depressions. If we call the overfilled depression D, then the water can be redistributed by starting a second inner postorder traversal at D. This inner traversal carries excess water from one depression to another until it has found a home for all of it. When we pass water into a depression, it can go to one of three places: the depression itself, its sibling, or its parent. Distributing the water to any of these places may itself cause an overflow. Therefore, the inner (preorder) traversal comprises the following steps.

Call the depression that we are currently considering B. This may be the depression we originally considered, depression D, or it may be some other depression reached during the steps detailed below. If B is overflowing, we add the overflow to the excess water the inner traversal is carrying. If B has spare capacity we add water from the excess to B until either it fills or all of the excess water the inner traversal is carrying is used.

At this point, the inner traversal can terminate if (i) there is no water left, (ii) B is the parent of D, or (iii) B was reached via an oceanlink.

Otherwise, if B has a sibling and the sibling's water volume is less than its depression volume, then start from Step 1 with the new B set as the depression pointed to by the current B's geolink.

Otherwise, if B has no sibling or the sibling's water volume is equal to its depression volume, then start from Step 1 with the new B set as the parent of the current B, or, if B has no parent, then use the depression to which B oceanlinks.
The next step of the outer traversal, which begins one level in the DH closer to the ocean, identifies a less nested metadepression for which the inner traversal might need to be run. If this step were not supplied with information about prior water redistribution, it could cause the inner traversal to cover the same nodes repeatedly, which would be computationally wasteful. To prevent this, the inner traversal returns the ID of the final node in which it placed water: this node is the only node in the traversal with spare capacity so future traversals can begin there. Therefore, on subsequent overflows, if such a cached value is available, then the recursion skips directly to that node. This ensures that all the calls to this part of the algorithm take no more than O(N) time collectively.
The following examples use the geometry from Sect. 2 to describe a set of inner traversals, starting with the overflowing depression no. 12. Step numbers mirror those above; numbers in parentheses indicate the number of recursions – that is, the number of times that the innertraversal algorithm has returned to Step 1.
 1.
Depression no. 12 fills and overflows.
 2.
Depression no. 12's water overflows into depression no. 4, which is not full, following its geolink.
 1(r1).
Depression no. 4 acts as depression no. 12's parent via an oceanlink. The inner traversal terminates.
 1(r1).
At this point, the outer traversal moves one level closer to the ocean, and the inner traversal repeats, this time starting at depression no. 4.
 1.
Depression no. 4 fills and overflows.
 2.
Depression no. 4's water overflows into its sibling, depression no. 5, which is not full and is a leaf depression. If depression no. 5 had descendants, water overflowing from depression no. 4 would have followed a geolink to one of these.
 1(r1).
Depression no. 5 fills and overflows.
 2(r1).
Depression no. 4 is full.
 3(r1).
Depression no. 5 overflows into its parent, depression no. 11.
 1(r2).
Depression no. 11 overflows into the ocean; the inner traversal terminates.
 1(r1).
Now the outer traversal moves yet another level closer to the ocean, and the new inner traversal starts at depression no. 11.
 1.
Depression no. 11 fills and overflows.
 2.
Depression no. 11 has no sibling.
 3.
Depression no. 11 overflows into its parent, the ocean; all remaining excess water is absorbed into an infinite sink.
 1(r1).
The nowselected node is the ocean; the inner traversal terminates.
 1(r1).
At this point, the outer traversal moves one level closer to the ocean and arrives at the ocean. The outer traversal also terminates.
3.3 Flood the landscape
After water moves through the DH (Sect. 3.2, above), each node in the DH exists in one of the three following states.

Empty. The depression's water volume is equal to zero. In this case, nothing needs to be done. The depression's descendants might contain water, but the water never propagates to this level of the DH.

Full. The depression's water volume is equal to the volume of the depression itself. In this case, the depression is entirely full. If the depression's parent contains water, then the calculation of water depth is dealt with at a higher stage in the DH. If the depression's parent is empty or if the depression's parent is the ocean, then the calculation is performed at this level as described below.

Partially filled. The depression's water volume is less than its depression volume. In this case, the depth of water across the depression and all its descendants' cells must be calculated at this level so that the depression fills to an appropriate level. This is described below and indicated as the marginal volume in Fig. 2e.
The next step is to distribute this water across the DEM, appropriately flooding geographic depressions.
Given the three states described above, the algorithm locates the highestlevel nodes that contain water. It does so via a postorder traversal. Each time the traversal reaches a leaf, the algorithm notes its label and pit cell. After identifying each of these, the algorithm reverses direction, moving from child to parent so long as the parent node contains water. Call the highest waterbearing node within a tree L.
In many cases, the water volume contained within the depression will be less than the total depression volume; therefore, we must calculate what the water level in the depression will be. To do this, we pick an arbitrary pit cell within L and its descendants and then use this as a seed from which to start building a priority queue that will traverse the cells of the depression. The priority queue returns cells ordered from lowest to highest elevation. At each step through the priority queue, the algorithm checks whether the cells visited so far collectively have enough volume to hold the water. If so, the algorithm exits, having successfully defined the flooded area. If not, it continues to use the priority queue to traverse the depression cell by cell. The filling procedure is shown in pseudocode in Sect. 6.3.
To expand this brief conceptual discussion into a more formal set of steps, let us begin by calling the active cell – that is, the one that is currently being considered by the algorithm – c_{p}. This cell is initially the arbitrary pit mentioned above and is added to the priority queue. The algorithm marks c_{p}, which stands for “cell of current highest priority”, as visited; all other cells remain unvisited. The algorithm then follows these steps.

Pop c_{p} from the priority queue, call it c, and use its elevation to calculate the volume of water that can be accommodated in the set of cells processed so far (Eq. 3, below). If this volume is enough to accommodate the volume of water available, exit the loop and compute the final water level (Eq. 6, below). Otherwise, proceed to Step 2.

Add c (which was popped in Step 1) to a plain queue, which records all of the cells scanned so far; these cells will later be inundated.

Add the cells neighboring c that are not marked as visited to the priority queue if they belong to one of the descendant depressions of the one being filled. Each of these neighboring cells is then marked as visited.

Choose the lowestelevation cell in the priority queue, label it as the new c_{p}, and return to Step 1. If the priority queue is empty, then all cells in the same metadepression as c_{p} or its descendants have been visited and we are now guaranteed to have sufficient depression volume to hold all of the water.
Step 1 in this approach requires an efficient way to determine the volume of a depression below any given elevation. If we call this elevation z_{o} and the depression below the outlet contains N cells with elevations $\mathit{\{}{z}_{\mathrm{1}},{z}_{\mathrm{2}},{z}_{\mathrm{3}},{z}_{\mathrm{4}},\mathrm{\dots}\mathit{\}}$ and unit cell area, the volume of water that the depression can accommodate simply equals the sum of the depth of water in each of its cells:
Now, consider cells ${c}_{i}={c}_{\mathrm{1}},\mathrm{\dots},{c}_{N}$ in the plain queue: that is, those cells that have been visited and popped from the priority queue. We can calculate the volume of water that can be accommodated in the depression below the elevation z_{s} of the last cell c_{N} (the sill) as
where z_{i} is the elevation of cell c_{i}, and a_{i} is the area of cell c_{i}. Thus, if we keep running sums while traversing the depression, it is possible to directly calculate the volume of water the depression can hold at each point in the traversal.
Once ${V}_{\mathrm{dep},{z}_{s}}$ is greater than or equal to the volume of water in the depression, V_{w}, the plain queue contains all the cells to be flooded. At this point, the algorithm updates z_{w}, which is the water level within this depression. If ${V}_{\mathrm{w}}={V}_{\mathrm{dep},{\mathrm{z}}_{\mathrm{s}}}$, the algorithm sets z_{w}=z_{N}. If instead ${V}_{\mathrm{w}}<{V}_{\mathrm{dep},{\mathrm{z}}_{\mathrm{s}}}$, the available volume in the depression is greater than the water volume, and the algorithm calculates z_{w} in the depression as follows.
We call Eq. (6) the lakelevel equation (LLE). If all cells have a unit area, this simplifies to
The conditional usage of the LLE described above is purely for computational efficiency: if ${V}_{\mathrm{w}}={V}_{\mathrm{dep},{z}_{s}}$, its solution is that z_{w}=z_{N}.
After solving for the watersurface elevation, the algorithm pops each cell in the plain queue (${c}_{i}={c}_{\mathrm{1}},\mathrm{\dots},{c}_{N}$) corresponding to the flooded region and sets its water elevation to the computed z_{w}. This is the final step of the Fill–Spill–Merge algorithm. At this point, it outputs a file representing the topography plus water thickness across the domain (i.e., topography with depressions filled or partially filled with water).
Because Fill–Spill–Merge routes water cell by cell to the pit cells of depressions and manages an array of water depths, it can be adapted for use with groundwater models, such as that described by Fan et al. (2013).
4.1 Theory
Here we use computational complexity as a means of contrasting the expected runtime of our algorithm against previous algorithms such as FlowFill (Callaghan and Wickert, 2019). To do so, we describe a simple iterative solver similar to FlowFill whose goal is to determine an appropriate water level for a depression. The solver operates on a onedimensional domain of cells bounded by high cliffs on either side in which each cell may have a column of water. At each step, if the solver finds a discontinuity in water levels between two cells, it responds by averaging the heights of the cells' water columns. (The solver we describe is known as Jacobi's method.) The challenge we present to this solver is a direct analog of routing flow along a stretch of river with a negligible gradient and is very similar to routing flow across the surface of a lake or ocean.
For our analysis, we imagine that the system is initialized with a high column of water on the left and no water anywhere else. We call the cell with the water cell 1. We call the cells to its right 2, 3, 4, and so on. During the solver's first step, cell 1 is initialized. On its second step, cell 1 averages its height with cell 2. On the third step, cell 2 averages with cell 3 and cell 1 then averages with cell 2. On the fourth step, cell 3 averages to 4, 2 averages to 3, and 1 averages with 2. Thus, the number of cells affected at each step are 1, 2, 3, 4, and so on. Since there must be at least as many steps as there are cells, we can say that there are N steps. The total time, t_{compute}, is then
Thus, for any model (Callaghan and Wickert, 2019; Fan et al., 2013) that uses a scheme similar to our simple solver, the time required to solve the model is in O(N^{2}).
In contrast, the new algorithm runs in O(N log N) time in the worst case. Moving water downhill (Sect. 3.1) is a flow accumulation algorithm. This is known to take O(N) time (Mark, 1988), and efficient variants exist for performing flow accumulation in parallel on large datasets (Barnes, 2017) and on GPUs (Barnes, 2019), though for simplicity we do not use these techniques here. Moving water within the depression hierarchy (Sect. 3.2) requires a depthfirst postorder traversal of the entire hierarchy. This type of traversal is a foundational algorithm in computer science and takes O(N) time. Each node in this traversal has the potential to overflow, which also results in a depthfirst traversal, thereby requiring up to O(N) time. However, by using a jump table that persists between calls to the overflow function, we ensure that it is able to identify the target of the overflow in amortized constant time; that is, the function is able to skip over fully filled depressions. Finally, the algorithm floods the digital elevation model from the pit cells up. This requires a depthfirst postorder traversal, which calls a flooding function (Sect. 3.3) on select subtrees of the DH. The depthfirst traversal takes O(N) time, as described above. The priority queue used for flooding nominally takes O(N log N) time in the worst case for floatingpoint data and O(N) time in the worst case for integer data (Barnes et al., 2014). However, with specialized data structures the time can be reduced to O(N) for both floatingpoint and integer data (Barnes et al., 2014). Most real datasets consist of many small depressions whose cell counts N_{cellsindep} are much smaller than the total number of cells in the digital elevation model. Therefore, the actual time for this step is O(N_{dep}N_{cellsindep}), where N_{dep} is the total number of depressions and N_{dep}N_{cellsindep} can be much less than N. Because the worstcase time complexity of any operation is O(N), this bounds the time of the algorithm as a whole. However, to reduce the potential for bugs, we use the C++ standard library's O(Nlog N) priority queue in our implementation at the cost of reduced performance.
To put this in more concrete terms, consider a long stretch of lowgradient river. Such a feature poses a lower bound on the time of our simple solver. North America's Red River of the North runs for 885 km with a gradient that is often on the order of 0.03 m km^{−1}. On a 90 m grid of floatingpoint data, the river would be 9833 cells long. Our simple (Jacobi) solver would then take an estimated 97 million time units to reach a solution, whereas the new solver that we describe in this paper would take 9833 time units, a speedup of 10 000 times. Our empirical results, which are presented below, support both the theory and this expected value.
4.2 Computational performance
We have implemented the algorithm described above in C++17 using the Geospatial Data Abstraction Library (GDAL) (GDAL Development Team, 2016) to read and write data. There are 1003 lines of code, 46 % of which are or contain comments. The code can be acquired from https://github.com/rbarnes/Barnes2020FillSpillMerge (last access: 6 February 2021) and Zenodo (Barnes and Callaghan, 2020; https://doi.org/10.5281/zenodo.3755142). The code contains extensive unit and endtoend tests, which leverage both deterministic and random testing; the code passes a total of 214 990 test assertions and achieves 97 % test coverage. The missed lines flag emergency situations that can only arise if there is a logic error, so they (in theory) cannot be reached.
Tests were run on the Comet machine of the Extreme Science and Engineering Discovery Environment (XSEDE) (Towns et al., 2014). Each node of the machine has 2.5 GHz Intel Xeon E52680v3 processors with 24 cores per node and 128 GB of DDR4 DRAM. Code was compiled using GNU g++ 7.2.0 with full optimizations enabled.
We ran two sets of scaling tests, one on actual data and one on synthetic data. On actual data, our scaling tests cover datasets spanning 3 orders of magnitude in terms of their number of cells, as shown in Table 1. The R package GuessCompx (AgenisNevers et al., 2019) shows that an O(Nlog N) scaling relationship gives the best fit to the data, which agrees with the theory.
To more precisely demonstrate performance, we run Fill–Spill–Merge on synthetic landscapes of various sizes generated using RichDEM's Perlin noise random terrain generator (Barnes, 2018). Multiple landscapes are generated and timed at each size to smooth timing variation due to both the data and fluctuations in the testing environment. This results in Fig. 6, which again shows that the performance data give a good fit to an Nlog N function.
4.3 Model intercomparison
Given a depression hierarchy data structure, Fill–Spill–Merge provides an efficient method to route water across any surface while taking depressions into account. Furthermore, Fill–Spill–Merge can be used to assess which depressions are most important in daytoday or seasonal changes to the hydrologic system. For example, small depressions will become flooded and spill over even with relatively small amounts of water reaching them, while larger depressions may not be completely filled. These depressions impact the hydrologic connectivity of the landscape (Callaghan and Wickert, 2019). If standing water is retained between invocations of Fill–Spill–Merge and new water added at each invocation, the algorithm can be used to simulate the movement of water across landscapes; we will explore this further in future work.
We have compared Fill–Spill–Merge with a prior algorithm, FlowFill, at the same two sites used by Callaghan and Wickert (2019): a reach of the Sangamon River in Illinois (Fig. 7) and the Río Toro basin in Argentina (Fig. 8). Like Fill–Spill–Merge, FlowFill can be used to route water across a landscape while preserving real depressions, but the latter algorithm is significantly slower (Table 2). The two selected study sites provide very different landscapes for testing the performance of the algorithm. The Sangamon River site is located in Illinois, USA, at 39.97^{∘} N, 88.72^{∘} W. It is a lowrelief, postglacial landscape containing many closed depressions, which may impact hydrologic connectivity as a function of runoff (Lai and Anders, 2018). It furthermore contains a grid of roads and associated embankments whose elevations are significant when compared to regional relief and impact water flow paths and storage. Callaghan and Wickert (2019) resampled the 0.76 m resolution lidar DEM (Illinois Geospatial Data Clearinghouse, 2020) to 15 m resolution for analysis and manually removed several road bridges using GRASS GIS (Neteler et al., 2012) to prevent artificial pooling behind these; here we use the same modified DEM to enable a direct comparison between the algorithms. The Río Toro site is located mainly in Salta Province, Argentina, around 24.5^{∘} S, 65.8^{∘} W. This site exhibits more rugged fluvially sculpted topography (Hilley and Strecker, 2005). Callaghan and Wickert (2019) resampled the 12 m TanDEMX DEM of this region (Krieger et al., 2013; Rizzoli et al., 2017) to 120 m resolution. Here we use this same resampled DEM for comparison. The runoff depths used at each of the two study sites were selected to show a range of water levels present in the depressions. The depths shown were therefore scaled based on the amount of water required to completely fill depressions in the landscape.
As shown in Table 2, wall times using Fill–Spill–Merge ranged from 0.227 to 0.243 s for the Sangamon River site and 0.300 to 0.319 s for the Río Toro site. This compares with times ranging from 20 to 643 s and 31 to 155 s, respectively, for FlowFill. These times for both sites correspond to a reduction in wall time of 86–2645 times using FSM. Since FlowFill was run with 24 processors, this translates to a reduction in compute time of 2064–63 480 times. Considering that each of these example DEMs is quite small relative to modern fullresolution lidarderived elevation datasets or continentalscale 30 m DEMs (Table 1), this speedup and its associated O(Nlog N) scaling provide a significant advantage for topographic analysis and solving associated problems in hydrology and geomorphology.
Although both FlowFill and Fill–Spill–Merge route water downslope, flooding depressions based on the quantity of available water, our FSM results differ in some ways from those of FlowFill (Callaghan and Wickert, 2019). In both Figs. 7 and 8, Fill–Spill–Merge flooded some depressions more deeply than FlowFill did and flooded some depressions with less water. At both study sites, the differences between the two algorithms are minimized at the extreme high and extreme low starting runoff values. For the highest runoff values, this is because both algorithms successfully fill all depressions in the landscape so that no differences are possible. For the lowest runoff values, both algorithms simulate only a small amount of water filling any depression so that significant differences between the two algorithms are not possible. The biggest differences are therefore seen for moderate starting runoff values, when depressions contain substantial water volumes but are still only partially filled. One possible cause of these discrepancies is FlowFill's asymptotic approach to an equilibrium water level, which may prevent small volumes of water from reaching the depression to which they belong. On the other hand, depressions with a narrow outlet could be especially prone to being overfilled by FlowFill because its cellbycell algorithm could dynamically dam this outlet, routing additional water into the depression. Both of these possibilities are further linked to the fact that FlowFill dynamically evolves a landpluswater flowrouting surface, whereas Fill–Spill–Merge routes flow just over the land surface. These differences make FlowFill more useful for understanding temporal changes in surface water distribution, while Fill–Spill–Merge provides a more accurate snapshot of surface hydrology under equilibrium conditions.
Here we leverage the depression hierarchy data structure (Barnes et al., 2020) to route flow through surface depressions in a realistic yet efficient manner. In comparison to previous approaches, such as Jacobi iteration, the new algorithm runs in loglinear time in the input size and is accompanied by extensively commented source code. This computationally efficient algorithm may help us to better understand hydrologic connectivity and water storage across the land surface, and it is an important step forwards in recognizing the importance of depressions as realworld features in digital elevation models.
6.1 MoveWaterInDepHier
6.2 OverflowInto
6.3 FillDepressions
Complete, wellcommented source code, an associated makefile, and correctness tests are available from https://github.com/rbarnes/Barnes2020FillSpillMerge (last access: 12 February 2021) and Zenodo (Barnes and Callaghan, 2020).
KLC and ADW conceived the problem. RB conceived the algorithm and developed initial implementations. KC and RB completed, debugged, and tested the algorithm. All authors contributed to the preparation of the paper.
The authors declare that they have no conflict of interest.
Richard Barnes was supported by the Department of Energy's Computational Science Graduate Fellowship (grant no. DEFG0297ER25308) and, through the Berkeley Institute for Data Science's PhD Fellowship, by the Gordon and Betty Moore Foundation (grant GBMF3834) as well as by the Alfred P. Sloan Foundation (grant 20131027).
Kerry L. Callaghan was supported by the National Science Foundation under grant no. EAR1903606, the University of Minnesota Department of Earth Sciences Junior F Hayden Fellowship, the University of Minnesota Department of Earth Sciences H.E. Wright Footsteps Award, and startup funds awarded to Andrew Wickert by the University of Minnesota.
Empirical tests and results were performed on XSEDE's Comet supercomputer (Towns et al., 2014), which is supported by the National Science Foundation (grant no. ACI1053575). Portability and debugging tests were performed on the Mesabi machine at the Minnesota Supercomputing Institute (MSI) at the University of Minnesota (http://www.msi.umn.edu last access: 6 February 2021).
The Deutsches Zentrum für Luft und Raumfahrt (DLR) provided 12 m TanDEMX DEM coverage of the Río Toro catchment via proposal DEM_GEOL1915 awarded to Taylor Schildgen, Andrew Wickert, Stefanie Tofelde, and Mitch D'Arcy. Jingtao Lai and Alison Anders provided a copy of their Sangamon River DEM.
This collaboration resulted from a serendipitous meeting at the Community Surface Dynamics Modeling System (CSDMS) annual meeting, which RB attended on a CSDMS travel grant.
This research has been supported by the U.S. Department of Energy–Krell Institute (grant no. DEFG0297ER25308), the National Science Foundation Office of Advanced Cyberinfrastructure (grant no. ACI1053575), the Gordon and Betty Moore Foundation (grant no. GBMF3834), the Alfred P. Sloan Foundation (grant no. 20131027), and the National Science Foundation Division of Earth Sciences (grant no. EAR1903606).
This paper was edited by Wolfgang Schwanghart and reviewed by Daniel Hobley and one anonymous referee.
AgenisNevers, M., Bokde, N. D., Yaseen, Z. M., and Shende, M.: GuessCompx: An empirical complexity estimation in R, arXiv [preprint], arXiv:1911.01420v1, 2019. a
Arnold, N.: A new approach for dealing with depressions in digital elevation models when calculating flow accumulation values, Prog. Phys. Geogr., 34, 781–809, https://doi.org/10.1177/0309133310384542, 2010. a
Barnes, R.: Parallel nondivergent flow accumulation for trillion cell digital elevation models on desktops or clusters, Environ. Modell. Softw., 92, 202–212, https://doi.org/10.1016/j.envsoft.2017.02.022, 2017. a, b
Barnes, R.: rbarnes/richdem: Zenodo DOI Release, Software, Zenodo, https://doi.org/10.5281/zenodo.1295618, 2018. a
Barnes, R.: Accelerating a fluvial incision and landscape evolution model with parallelism, Geomorphology, 330, 28–39, https://doi.org/10.1016/j.geomorph.2019.01.002, 2019. a, b
Barnes, R. and Callaghan, K.: Depression Hierarchy Source Code, Zenodo, https://doi.org/10.5281/zenodo.3238558, 2019. a
Barnes, R. and Callaghan, K.: FillSpillMerge Source Code, Zenodo, https://doi.org/10.5281/zenodo.3755142, 2020. a, b, c
Barnes, R., Lehman, C., and Mulla, D.: Priorityflood: An optimal depressionfilling and watershedlabeling algorithm for digital elevation models, Comput. Geosci., 62, 117–127, https://doi.org/10.1016/j.cageo.2013.04.024, 2014. a, b, c
Barnes, R., Callaghan, K. L., and Wickert, A. D.: Computing water flow through complex landscapes – Part 2: Finding hierarchies in depressions and morphological segmentations, Earth Surf. Dynam., 8, 431–445, https://doi.org/10.5194/esurf84312020, 2020. a, b, c, d, e, f, g
Beucher, S.: Watershed, Hierarchical Segmentation and Waterfall Algorithm, in: Mathematical Morphology and Its Applications to Image Processing, edited by: Viergever, M. A., Serra, J., and Soille, P., Springer Netherlands, Dordrecht, vol. 2, 69–76, https://doi.org/10.1007/9789401110402_10, 1994. a
Braun, J. and Willett, S. D.: A very efficient O(n), implicit and parallel method to solve the stream power equation governing fluvial incision and landscape evolution, Geomorphology, 180–181, 170–179, https://doi.org/10.1016/j.geomorph.2012.10.008, 2013. a
Breckenridge, A. and Johnson, T. C.: Paleohydrology of the upper Laurentian Great Lakes from the late glacial to early Holocene, Quaternary Res., 71, 397–408, https://doi.org/10.1016/j.yqres.2009.01.003, 2009. a
Cabrol, N. A. and Grin, E. A.: Distribution, classification, and ages of Martian impact crater lakes, Icarus, 142, 160–172, 1999. a
Callaghan, K. L. and Wickert, A. D.: Computing water flow through complex landscapes – Part 1: Incorporating depressions in flow routing using FlowFill, Earth Surf. Dynam., 7, 737–753, https://doi.org/10.5194/esurf77372019, 2019. a, b, c, d, e, f, g, h, i, j, k
Cordonnier, G., Bovy, B., and Braun, J.: A versatile, linear complexity algorithm for flow routing in topographies with depressions, Earth Surf. Dynam., 7, 549–562, https://doi.org/10.5194/esurf75492019, 2019. a
Fan, Y., Li, H., and MiguezMacho, G.: Global Patterns of Groundwater Table Depth, Science, 339, 940–943, https://doi.org/10.1126/science.1229881, 2013. a, b
Fenner, T. I. and Loizou, G.: Loopfree Algorithms for Traversing Binary Trees, BIT, 24, 33–44, https://doi.org/10.1007/BF01934513, 1984. a
GDAL Development Team: GDAL – Geospatial Data Abstraction Library, Open Source Geospatial Foundation, available at: http://www.gdal.org (last access: 6 February 2021), 2016. a
GEBCO: General Bathymetric Chart of the Oceans (GEBCO), GEBCO_08 grid, version 20100927, http://www.gebco.net (last access: 6 February 2021), 2010. a
Hilley, G. E. and Strecker, M. R.: Processes of oscillatory basin filling and excavation in a tectonically active orogen: Quebrada del Toro Basin, NW Argentina, GSA Bulletin, 117, 887–901, https://doi.org/10.1130/B25602.1, 2005. a, b
Illinois Geospatial Data Clearinghouse: Illinois Height Modernization (ILHMP), available at: https://clearinghouse.isgs.illinois.edu/data/elevation/illinoisheightmodernizationilhmplidardata (last access: 6 February 2021), 2020. a, b
Jenson, S. and Domingue, J.: Extracting Topographic Structure from Digital Elevation Data for Geographic Information System Analysis, Photogrammetric Engineering and Remote Sensing, 54, 1–5, 1988. a
Krieger, G., Zink, M., Bachmann, M., Bräutigam, B., Schulze, D., Martone, M., Rizzoli, P., Steinbrecher, U., Walter Antony, J., De Zan, F., Hajnsek, I., Papathanassiou, K., Kugler, F., Rodriguez Cassola, M., Younis, M., Baumgartner, S., LópezDekker, P., Prats, P., and Moreira, A.: TanDEMX: A radar interferometer with two formationflying satellites, Acta Astronautica, 89, 83–98, 2013. a, b
Lai, J. and Anders, A. M.: Modeled Postglacial Landscape Evolution at the Southern Margin of the Laurentide Ice Sheet: Hydrological Connection of Uplands Controls the Pace and Style of Fluvial Network Expansion, J. Geophys. Res.Earth, 123, 967–984, https://doi.org/10.1029/2017JF004509, 2018. a, b, c
Li, S., MacMillan, R., Lobb, D. A., McConkey, B. G., Moulin, A., and Fraser, W. R.: Lidar DEM error analyses and topographic depression identification in a hummocky landscape in the prairie region of Canada, Geomorphology, 129, 263–275, https://doi.org/10.1016/j.geomorph.2011.02.020, 2011. a
Lindsay, J. and Creed, I.: Removal of artifact depressions from digital elevation models: towards a minimum impact approach, Hydrol. Process., 19, 3113–3126, https://doi.org/10.1002/hyp.5835, 2005a. a
Lindsay, J. B.: Efficient hybrid breachingfilling sink removal methods for flow path enforcement in digital elevation models: Efficient Hybrid Sink Removal Methods for Flow Path Enforcement, Hydrol. Process., 30, 846–857, https://doi.org/10.1002/hyp.10648, 2016. a, b
Lindsay, J. B. and Creed, I. F.: Removal of artifact depressions from digital elevation models: Towards a minimum impact approach, Hydrol. Process., 19, 3113–3126, https://doi.org/10.1002/hyp.5835, 2005b. a
Mark, D.: Modelling in Geomorphological Systems, chap. Network models in geomorphology, John Wiley & Sons, Las Vegas, Nevada, 73–97, 1988. a, b
Martz, L. W. and Garbrecht, J.: The treatment of flat areas and depressions in automated drainage analysis of raster digital elevation models, Hydrol. Process., 12, 843–855, https://doi.org/10.1002/(SICI)10991085(199805)12:6<843::AIDHYP658>3.0.CO;2R, 1998. a
Martz, L. W. and de Jong, E.: CATCH: A FORTRAN program for measuring catchment area from digital elevation models, Comput. Geosci., 14, 627–640, https://doi.org/10.1016/00983004(88)900180, 1988. a
MNDNR – Minnesota Department of Natural Resources: Lake Bathymetric Outlines, Contours, Vegetation, and DEM, available at: https://gisdata.mn.gov/dataset/waterlakebathymetry (last access: 6 February 2021), 2014. a
MNGEO – Minnesota Geospatial Information Office: LiDAR Elevation Data for Minnesota, available at: http://www.mngeo.state.mn.us/chouse/elevation/lidar.html (last access: 6 February 2021), 2019. a
Neteler, M., Bowman, M. H., Landa, M., and Metz, M.: GRASS GIS: A multipurpose open source GIS, Environ. Modell. Softw., 31, 124–130, https://doi.org/10.1016/j.envsoft.2011.11.014, 2012. a
O'Callaghan, J. and Mark, D.: The extraction of drainage networks from digital elevation data, Comput. Vision Graph., 28, 323–344, https://doi.org/10.1016/S0734189X(84)800110, 1984. a
Reheis, M.: Highest PluvialLake Shorelines and Pleistocene Climate of the Western Great Basin, Quaternary Res., 52, 196–205, https://doi.org/10.1006/qres.1999.2064, 1999. a
Riddick, T., Brovkin, V., Hagemann, S., and Mikolajewicz, U.: Dynamic hydrological discharge modelling for coupled climate model simulations of the last glacial cycle: the MPIDynamicHD model version 3.0, Geosci. Model Dev., 11, 4291–4316, https://doi.org/10.5194/gmd1142912018, 2018. a
Rizzoli, P., Martone, M., Gonzalez, C., Wecklich, C., Tridon, D. B., Bräutigam, B., Bachmann, M., Schulze, D., Fritz, T., Huber, M., et al.: Generation and performance assessment of the global TanDEMX digital elevation model, ISPRS J. Photogramm., 132, 119–139, 2017. a, b
Salembier, P. and Pardas, M.: Hierarchical morphological segmentation for image sequence coding, IEEE T. Image Process., 3, 639–651, https://doi.org/10.1109/83.334980, 1994. a
Schwanghart, W. and Scherler, D.: Bumps in river profiles: uncertainty assessment and smoothing using quantile regression techniques, Earth Surf. Dynam., 5, 821–839, https://doi.org/10.5194/esurf58212017, 2017. a
Sedgewick, R. and Wayne, K.: Algorithms, AddisonWesley, Boston, USA, 4 edn., 2011. a
Skiena, S. S.: The Algorithm Design Manual, Springer, New York, USA, 2008. a
Soille, P.: Optimal removal of spurious pits in grid digital elevation models, Water Resour. Res., 40, 1–9, https://doi.org/10.1029/2004WR003060, 2004. a
Soille, P., Vogt, J., and Colombo, R.: Carving and adaptive drainage enforcement of grid digital elevation models, Water Resour. Res., 39, 1366, https://doi.org/10.1029/2002WR001879, 2003. a
Towns, J., Cockerill, T., Dahan, M., Foster, I., Gaither, K., Grimshaw, A., Hazlewood, V., Lathrop, S., Lifka, D., Peterson, G. D., Roskies, R., Scott, J. R., and WilkinsDiehr, N.: XSEDE: accelerating scientific discovery, Comput. Sci. Eng., 16, 62–74, 2014. a, b
Wallis, C., Watson, D., Tarboton, D., and Wallace, R.: Parallel flowdirection and contributing area calculation for hydrology analysis in digital elevation models, in: Preceedings of the 2009 International Conference on Parallel and Distributed Processing Techniques and Applications, Las Vegas, Nevada, available at: https://digitalcommons.usu.edu/cee_facpub/2533/ (last access: 6 February 2021), 2009. a
Wickert, A. D.: Reconstruction of North American drainage basins and river discharge since the Last Glacial Maximum, Earth Surf. Dynam., 4, 831–869, https://doi.org/10.5194/esurf48312016, 2016. a
Wu, Q. and Lane, C. R.: Delineation and quantification of wetland depressions in the Prairie Pothole Region of North Dakota, Wetlands, 36, 215–227, 2016. a
Wu, Q., Liu, H., Wang, S., Yu, B., Beck, R., and Hinkel, K.: A localized contour tree method for deriving geometric and topological properties of complex surface depressions based on highresolution topographical data, Int. J. Geogr. Inf. Sci., 29, 2041–2060, https://doi.org/10.1080/13658816.2015.1038719, 2015. a
Wu, Q., Lane, C. R., Wang, L., Vanderhoof, M. K., Christensen, J. R., and Liu, H.: Efficient Delineation of Nested Depression Hierarchy in Digital Elevation Models for Hydrological Analysis Using LevelSet Method, J. Am. Water Resour. As., 55, 354–368, https://doi.org/10.1111/17521688.12689, 2018. a