Rivers provide crucial ecosystem services in water-stressed drylands. Australian dryland rivers are geomorphologically diverse, ranging from through-going, single channels to discontinuous, multi-channelled systems, yet we have limited understanding of their sensitivity to future hydroclimatic changes. Here, we characterise for the first time the geomorphology of 29 dryland rivers with catchments across a humid to arid gradient covering >1,800,000 km2 of continental eastern and central Australia. Statistical separation of five specific dominantly alluvial river types and quantification of their present-day catchment hydroclimates enables identification of potential thresholds of change. Projected aridity increases across eastern Australia by 2070 (RCP4.5) will result in ~80% of the dryland rivers crossing a threshold from one type to another, manifesting in major geomorphological changes. Dramatic cases will see currently through-going rivers (e.g. Murrumbidgee, Macintyre) experience step changes towards greater discontinuity, characterised by pronounced downstream declines in channel size and local termination. Expanding our approach to include other river styles (e.g. mixed bedrock-alluvial) would allow similar analyses of dryland rivers globally where hydroclimate is an important driver of change. Early identification of dryland river responses to future hydroclimatic change has far-reaching implications for the ~2 billion people that live in drylands and rely on riverine ecosystem services.
Rivers are lifelines in climatically variable and water-stressed drylands, the dry subhumid through hyperarid environments that cover 40–50% of the Earth’s land surface and host ~28% of the world’s population1,2. Dryland rivers are fundamentally important for human populations, providing a plethora of provisioning, regulating, supporting and cultural ecosystem services1,3. Yet dryland rivers exist in marginal environments and are threatened by declines in water availability due to the impacts of climate change (e.g. decreased rainfall, increased temperature and evapotranspiration, and greater climatic variability) and other human activities (e.g. river regulation, flow diversion and abstraction, and land use change)4,5,6. Rivers are not static conduits of water, sediment and nutrients, but adjust dynamically to a suite of internal and external drivers. Among various external drivers (e.g. tectonic activity, sea level fluctuations, climate), research has shown that late Quaternary hydroclimatic changes have driven substantial geomorphological changes to many dryland rivers globally, including during the mid to late Holocene [e.g.7,8,9,10]. Indeed, in tectonically stable settings such as continental Australia, and in reaches where rivers are free from significant bedrock influence, hydroclimatic changes are the principal driver of river response and resulting channel-floodplain geomorphology. To date, however, assessment of the potential likelihood and pathways of hydrological and geomorphological changes in dryland rivers due to future hydroclimate change have not been considered in any rigorous or systematic fashion11,12. Analyses of future changes have tended to focus solely on dryland hydrology, such as surface water availability or river flow regimes [e.g.5,13,14,15], rather than on the implications of these changes for river response and physical structure (e.g. number of channels, sinuosity, lateral stability, landform assemblages). This is a critical knowledge gap, as dryland river geomorphology provides the physical template atop which complex ecosystems and anthropogenic land uses operate and intersect16, thereby defining the range and quality of ecosystem service delivery.
In the Australian drylands, a continuum of dominantly alluvial river types extends from relatively high-energy rivers that maintain a single, continuous channel downstream, to lower energy, declining or discontinuous rivers that undergo various forms of channel breakdown, including disintegration into networks of multiple, smaller channels and/or termination on unchannelled plains termed floodouts [cf.17 Fig. 1]. In some instances, channel breakdown is associated with extensive floodplain wetlands [e.g.18] that provide ecosystem services in these water-stressed settings (e.g. wildlife habitat, water filtration and supply). Globally, other dryland river types occur, including dominantly alluvial (e.g. braided), dominantly bedrock (e.g. incised or ingrown meanders), and mixed bedrock-alluvial (e.g. anabranching/anastomosing) types19,20. In this study, these river types have not been considered, as Australian dryland rivers are not braided and are dominantly alluvial in their middle and lower reaches. Previous research has suggested that regional continua of dryland river types may be related to hydroclimatic gradients, with greater aridity leading to a greater propensity for channel breakdown21,22. To refine these concepts and identify thresholds of change relevant for Australian dryland rivers, we characterise the hydrology and geomorphology of 29 rivers draining >1,800,000 km2 of continental eastern and central Australia, and establish the hydroclimatic conditions under which different river types persist. First, we categorise Australian dryland rivers into five types using a suite of geomorphological characteristics. Second, we establish the distinct hydrological characteristics of these river types using streamflow gauge data and correlate these characteristics with catchment aridity. Third, by establishing robust and significant relationships between modern dryland river types, hydrology and catchment aridity, we define envelopes of mean catchment aridity index (AI) values for each river type. Fourth, we use downscaled global climate model projections to project future hydroclimatic changes and associated geomorphological responses. Where projections suggest that a catchment will shift outside of the envelope of aridity defined by modern climatic data, we anticipate the trajectory of geomorphological change for the trunk river in that catchment and identify the geomorphological thresholds that may be crossed. With further refinement to include a wider range of dryland river types (e.g. mixed bedrock-alluvial types), this approach will provide a quantitatively-tested method for broader, continental and global studies of dryland river sensitivity to hydroclimatic changes that may be exacerbated or compounded by other human activities, such as future river regulation, flow diversion and abstraction, and land use change. Early identification of dryland river responses to global hydroclimatic changes will have far-reaching implications for the management of dryland rivers and the maintenance of dryland river ecosystem service delivery.
Diversity of Australian dryland rivers
Much of continental eastern Australia is characterised by large catchments that host perennial, intermittent or ephemeral rivers and associated wetlands. These catchments are located in a post orogenic, intracratonic setting, where denudation rates and river sediment loads are low compared to global averages. Beyond the headwaters, many rivers follow lengthy courses across piedmonts and lowland plains where bedrock outcrop is less common and alluvial river styles dominate. Owing to limited tributary inputs and declining valley slopes, many rivers undergo downstream decreases in discharge and stream power that lead to channel size declines and, in some cases, channel breakdown23. Some of these rivers are regulated to allow water storage, abstractions and altered seasonal flows, but downstream decreases in discharge and stream power, and channel size declines and breakdown can occur despite regulation23. While Australian dryland rivers display a range of dominantly alluvial styles (e.g. single channel versus multiple channel), we have defined five river types that are widely represented in the middle to lower reaches (Fig. 1; Supplementary Fig. S1). Two overarching categories are recognised: rivers with through-going channels to their catchment outlet (e.g. a lake or another river) and rivers with discontinuous channels (e.g. characterised by zones where channels lose definition or where channels terminate). Further differentiation is achieved by defining dominant river planform (sinuous, non-sinuous) and pattern (meandering, straight, anabranching/anastomosing, distributary), the nature of downstream decline in channel size after leaving valley (bedrock) confinement (maintaining, declining, or terminating), and the presence/absence and type of wetlands (see Methods, Table 1 and Supplementary Fig. S1). The five types are: Type 1 – through-going, sinuous channels that maintain size downstream; Type 2 – through-going, sinuous channels that decline in size downstream; Type 3 – through-going to discontinuous, sinuous channels that decline in size downstream; Type 4 – discontinuous, non-sinuous channels that decline in size downstream; Type 5 – discontinuous, non-sinuous channels that decline in size downstream and terminate (e.g. at a floodout) (Fig. 1).
Climatic gradient in continental eastern Australia
Approximately 78% of the Australian continent is classified as dryland24, and across the eastern half of the continent, there is a pronounced aridity gradient from humid (AI > 0.65), through dry subhumid (AI 0.65–0.5) and semiarid (AI 0.5–0.2), to arid (AI 0.2–0.05) (Fig. 2). Pronounced periods of above- and below-average rainfall combine to also make Australian hydroclimates (including river flow regimes) some of the most variable in the world25,26,27,28,29, a characteristic that persists despite the presence of dams and associated flow regulation in many catchments. In this tectonically stable setting, and especially in the middle to lower reaches where rivers are largely free from bedrock influence, these hydroclimatic variations are the key driver of river response and resulting channel-floodplain geomorphology. The relationship between climate, hydrology, and geomorphology is complex but may be expressed through various metrics including mean and peak runoff depth, flow variability, and stream power. Stream power is a function of river discharge and slope, and represents the energy exerted by water on the bed and banks of a river30. It is widely used as a quantitative measure of the potential for flow to initiate channel adjustment through erosion or deposition31,32.
Hydroclimatic controls on Australian dryland river geomorphology
To examine the links between hydroclimate and geomorphology, the five river types (Fig. 1; Table 1) have been subjected to one-way analysis of variance (ANOVA; Fig. 3) and a pairwise analysis of similarities (ANOSIM) of key variables (Fig. 4; Table 2; Supplementary Table S1). Mean catchment AI is the variable that best defines significant differences between river types (except for Types 4 and 5; see Fig. 3I). Through-going, maintaining rivers (Type 1) occur in catchments where ~65–87% of the total catchment area is classed as humid and mean catchment AI is 0.80–1.0 (Fig. 4; Supplementary Fig. S2). Through-going, declining rivers (Type 2) occur in catchments where ~7–48% of total catchment area is classed as humid and mean catchment AI is 0.45–0.78. Through-going to discontinuous, declining rivers (Type 3) occur in catchments where ~0.2–8% of the total catchment area is classed as humid and mean catchment AI is 0.30–0.46. Discontinuous, declining rivers (Type 4) have no catchment area that is humid or even dry subhumid and mean catchment AI is 0.14–0.28. Discontinuous, terminating rivers (Type 5) occur in catchments that are typically 100% arid and mean catchment AI is 0.10–0.17 (Fig. 4; Supplementary Fig. S2).
Links between climate, catchment aridity, and key hydrological variables have been established in previous research, including how the magnitude and variability of runoff and streamflow in eastern Australian rivers is strongly modulated by climatic modes (e.g. El Niño-Southern Oscillation (ENSO), Interdecadal Pacific Oscillation (IPO) and the Southern Annular Mode (SAM))25,26,27,28,29. While these inter- and multi-decadal hydroclimatic relationships are relatively well understood, the distinct trends and clusters that emerge from our analysis demonstrate, for the first time, the significant overarching control that dominant hydroclimate exerts on the geomorphology of Australian dryland rivers. There is a strong and significant positive correlation between mean catchment AI and mean annual runoff depth (Pearson’s R = 0.79, p = 0.00001), and all river types are significantly different except for Types 4 and 5 (pairwise ANOSIM, p < 0.05; Fig. 5A). There is a significant positive correlation between mean catchment AI and mean peak annual runoff depth (Pearson’s R = 0.59, p = 0.004), and all river types are significantly different except for Types 2 and 3 (pairwise ANOSIM, p < 0.05; Fig. 5B). There is a strong and significant positive correlation between mean catchment AI and bankfull gross stream power (Pearson’s R = 0.78, p = 0.001; Fig. 5C). There is a strong and significant negative correlation between mean catchment AI and coefficient of annual flow (CVaf; Pearson’s R = −0.78, p = 0.00001), and all river types are significantly different except for Types 2 and 3 (pairwise ANOSIM, p < 0.05; Fig. 5D).
Overall, catchments with a mean catchment AI classed as humid or dry subhumid have greater mean annual runoff depth (>40 mm a−1) and stream power (>900 W m−1), lower flow variability (CVaf < 0.9), and support through-going river types (most Types 1 and 2). Catchments with a mean catchment AI classed as semiarid or arid have lower mean annual runoff depth (<55 mm a−1) and gross stream power (<760 W m−1), greater flow variability (CVaf > 0.8), and tend to be characterised by discontinuous river types (most Type 3 rivers, and Types 4 and 5; Fig. 5). These metrics enable the identification of thresholds that define the hydroclimatic conditions that are responsible for channel (dis)continuity in these dryland rivers (i.e. through-going vs. discontinuous). There is also an intrinsic, but poorly defined, channel termination threshold causing Type 4 and 5 rivers to break down into unchannelised wetlands or floodouts.
These findings highlight the key influence of hydroclimatic conditions on the river types across our identified continuum, manifested in differences in river planform, pattern and downstream channel (dis)continuity (Fig. 1). Many Australian dryland rivers, especially Types 2, 3, 4 and 5, are characterised by downstream declines in bankfull discharge (Supplementary Fig. S1), which result from flow transmission losses associated with floodwave attenuation, evapotranspiration, or groundwater recharge23,33,34. Downstream declines in bankfull discharge are commonly associated with downstream decreases in channel slope, which collectively result in downstream decreases in stream power and sediment transport capacity, thus promoting sediment deposition. These changes may lead to a contraction of channel width and/or to channel avulsion, the process of channel relocation on a floodplain [e.g.35]. Avulsion can form new channels that may supersede the original trunk channel in single-channel rivers, or create new channels that operate in parallel with the trunk channel in multi-channelled rivers. In more arid settings, however, there is a threshold beyond which stream power becomes too low to maintain sediment transport in a defined channel. Hence, channel breakdown occurs, leading to unchannelised wetlands (Types 3 and 4) and/or floodouts without significant wetlands (Type 5), particularly where there are barriers to flow resulting from aeolian or alluvial deposits, or local bedrock outcrop17.
Recognition of these links between hydroclimates and dryland river geomorphology allows each of the five river types to be defined within a range of mean catchment AI values. Establishing these AI envelopes allows us to identify which rivers exist close to a threshold between different river types, and then use climate projections to forecast future trajectories of change for rivers subject to changing hydroclimatic conditions.
Climate change projections and impacts on Australian dryland rivers
Previous studies investigating future hydrological changes to inland Australian rivers have predicted lower stream flows resulting from warming and altered precipitation patterns36,37,38,39. Decreases in runoff in southern Australia, resulting from both reductions in winter rainfall and increased temperatures, have been projected with a high confidence38,39. These projected runoff decreases in southern Australia accord with our projections of increased future aridity in continental eastern Australia for 2070 (see Supplementary Fig. S3) under Representative Concentration Pathway 4.5 (RCP4.5; [cf.40]). RCP4.5 is a relatively moderate climate change pathway and in our study was chosen to understand which rivers are the most sensitive to conservative scenarios of future climate change. Interestingly, our modelling of future aridity under RCP8.5 suggests very similar changes in aridity over the Australian continent (Supplementary Fig. S3), likely due to increased projected rainfall across parts of northern and central Australia under RCP8.5 as well as higher projected temperatures relative to RCP4.5, thus resulting in a similar net projected change in mean catchment AI for both scenarios. Since contemporary levels of catchment aridity are closely correlated with mean and peak annual runoff depth, stream power, and flow variability (Fig. 5), and different hydroclimatic conditions are associated with distinct river types (Figs. 3, 4 and 5), we can assess how Australian dryland rivers may respond to projected hydroclimatic changes related to changing aridity indices. Given the magnitude of rainfall reductions and evapotranspiration increases projected for much of the Australian continent under RCP4.5 (Supplementary Fig. S3), many catchments will likely experience substantial aridification (Fig. 6; Supplementary Figs. S2 and S3). Particularly sensitive rivers are those that are close to a threshold of change between different river types and that therefore may be subject to significant geomorphological adjustments under these future hydroclimatic conditions.
Indeed, of the 29 rivers analysed in this study, 23 (~80%) are projected to cross a threshold to another river type due to future catchment aridification and associated changes in hydrological conditions under RCP4.5 (Fig. 6). The largest magnitude changes are likely to affect the currently through-going, maintaining rivers (Type 1) with headwaters in the Australian southeastern highlands. These highlands are projected to have some of the most severe reductions in rainfall (see Supplementary Fig. S3), likely as a result of a projected increase in the prevalence of positive phases of the Southern Annular Mode, which will shift the average track of the southern hemisphere westerlies farther south and reduce winter rainfall over southern Australia41. All four Type 1 rivers are projected to change to through-going, declining rivers (Type 2). Reduced runoff depth and stream power will likely lead to sediment deposition and downstream declines in channel size (Fig. 6). Although the Kiewa, Mitta Mitta, Upper Murray and Ovens rivers (Type 1) occupy only a small proportion of the Murray-Darling Basin (~3.8%), they currently supply a disproportionately large amount of discharge (>33%) to parts of the lower catchment. Therefore, reductions in mean annual runoff depth and downstream declines in flow will have major impacts for water users and ecosystem services in the southern Murray-Darling Basin, which is one of Australia’s most important agricultural regions. While we have not modelled the effects of future water storage, flow diversions and abstractions, and land use in these catchments, these other forms of human disturbance will likely exacerbate or compound the effects of climate change by further altering flow regimes in already highly pressured, regulated systems6.
The most dramatic change in river morphology is from a through-going, declining river (Type 2) to a more discontinuous river (Types 3 or 4). Under RCP4.5, the currently through-going, declining Campaspe, Broken, Macintyre, and Murrumbidgee rivers (Type 2) are projected to have significant increases in catchment aridity, leading to reduced discharges and stream powers and more highly variable flow regimes, thereby becoming discontinuous rivers more characterised by channel breakdown and unchannelised wetlands (Type 3). Such dramatic changes in river structure and function will decrease hydrological and sediment connectivity, with profound, long-lasting impacts on water and sediment distribution, ecosystem dynamics, and ecosystem services in rivers and floodplains that are currently heavily used for irrigated agriculture and grazing. These changes are potentially irreversible and will increase the likelihood of ecosystem collapse in these marginal environments [c.f.42]. This will likely exacerbate existing high tensions surrounding water use and storage in inland Australia, particularly in the Murray-Darling Basin where ongoing drought (2018–2020) and water resource planning changes have had severe ecological impacts, perhaps providing an insight into the future facing many of Australia’s dryland rivers43,44.
All of the currently through-going to discontinuous (Type 3) rivers except the Gwydir and Namoi are projected to become Type 4 rivers with discontinuous, declining channels (Fig. 6), likely inducing changes to many of the semi-permanent, in-channel waterholes that currently characterise many river reaches19. Catchment aridification may also impact inundation regimes in semi-permanent and intermittent floodplain wetlands associated with these rivers, likely inducing a change to more ephemeral floodplain wetlands. Potential reductions in discharge and flow frequency will be particularly profound for wetlands of national and international ecological importance (e.g. Ramsar wetlands), such as the Macquarie Marshes, Gwydir wetlands, Narran Lake wetlands, and the Great Cumbung Swamp on the lower Lachlan River. Except for the Warrego River (Fig. 6), further declines in flow may even result in many Type 4 rivers transitioning into discontinuous, terminating rivers (Type 5) with few or no significant wetlands.
Discontinuous, terminating rivers (Type 5) are projected to experience even more arid hydroclimatic conditions, most likely with even greater flow variability than at present. While there are currently no Australian dryland rivers that are characterised by the levels of aridity projected for the Hay, Todd, and Finke catchments (Fig. 6), increased flow variability may impact severely on the health of the well-developed riparian vegetation assemblages that are such a critical influence on channel processes and forms in these rivers19. There are no hyperarid regions (AI < 0.05) currently on the Australian continent, but reference to other hyperarid areas around the world (e.g. central Sahara Desert), may provide an indication of what might be expected for the small regions of Australia projected to experience hyperarid conditions by the second half of this century (e.g. lack of bank-stabilising vegetation; Supplementary Fig. S3).
In summary, greater aridification of the Australian continent is projected for the second half of this century under both moderate (RCP4.5) and business-as-usual (RCP8.5) climate change scenarios. The influence of this enhanced aridification on the hydrology, physical structure, and biogeomorphic function of Australian dryland rivers is likely to be dramatic but, until now, has not been considered in any rigorous or systematic manner. Our approach is a quantitively-tested form of ergodic reasoning with powerful application for understanding river response to future hydroclimate change, not only across continental Australia but also potentially in other drylands worldwide, as discussed below.
Developing the approach to assess river response in drylands globally
Our findings demonstrate that even under a relatively conservative future emissions scenario (RCP4.5), projected aridification and associated changes to hydrological conditions across continental eastern and central Australia are likely to lead to significant geomorphological thresholds being crossed this century. The vast majority of rivers included in this study were highly sensitive to hydroclimatic change.
While Australia possesses a number of distinctive river styles, none of these styles are necessarily unique to the continent [e.g.19]. Hence, with further development, the novel approach outlined in this study potentially could be used to assess the geomorphic sensitivity of dryland rivers globally, especially for dominantly alluvial rivers where hydroclimatic factors are the key drivers of river response. Many parts of dryland Africa, South and North America, and central and western Asia are generally projected to experience declines in surface water availability and river flow in coming decades6,13,14,45,46,47,48. As such, rivers in these regions may also respond to these hydroclimatic changes by transforming from through-going to more discontinuous river types. In southern Africa, for instance, river morphology varies across strong hydroclimatic gradients, with through-going, maintaining rivers more common in subhumid catchments, and through-going, declining and discontinuous, declining or terminating rivers more common in semiarid and arid catchments21,22. Nevertheless, along many of these rivers, varying degrees of bedrock (lithological, structural) control influence the river’s ‘degrees of freedom’; for example, resistant rocks such as dolerite or quartzite commonly crop out in river bed and banks and influence the depth of incision or extent of lateral migration that can occur in response to hydroclimatic drivers [e.g.49,50]. In drylands where there is an even higher degree of tectonic and bedrock influence on rivers (e.g. the Mediterranean and parts of the Middle East), 21st century hydroclimatic drivers will still exert an influence on river response, but may be muted or locally overridden by the non-climatic factors. For example, in steep, confined river valleys, dryland rivers may respond to hydroclimatic changes mainly by altering the magnitude of cut-and-fill cycles rather than by undergoing any pronounced changes in channel continuity while periodic, tectonically-induced rockfalls or landslides may provide the main reach-scale, long-lasting disruptions to downstream flow and sediment transfer19,51. In many regions globally, river regulation and flow abstraction can also impact on the flow regime of dryland rivers6,43, although in most cases the effect would be similar to that expected under projected future hydroclimatic change (i.e. reduced runoff and perhaps altered seasonality) and so will likely exacerbate or compound the hydrological and geomorphological changes brought about by future hydroclimate change.
While our approach has been based around Australian dryland rivers with flow gauging records, this may not be essential. Climate-hydrology-geomorphology relations established for gauged rivers could be used to make predictions for nearby ungauged rivers in the same hydroclimatic region. In southeastern Australia, for example, all the gauged Type 1 rivers that form part of our dataset (e.g. Kiewa, Mitta Mitta, Upper Murray and Ovens rivers) are projected to become Type 2 rivers under future hydroclimatic change (Fig. 6). Modelling of future mean catchment aridity index for other nearby rivers that are classified as Type 1 based on their geomorphology can be undertaken even if they are ungauged, as the robust climate-hydrology-geomorphology relationships have been established using data from the gauged rivers. Alternatively, indirect approaches to discharge estimation in dryland rivers52 could be used to generate supporting hydrological or hydraulic information to help establish modern climate-hydrology-geomorphology relations across hydroclimatic gradients, as has been done successfully for different dryland rivers worldwide (e.g.10,22,53). By applying ergodic reasoning, these relations could then be used as the basis for predicting river response under altered hydroclimates.
In summary, beyond the continental Australian setting, our approach will need to be expanded to include a wider diversity of dryland rivers (e.g. additional alluvial, bedrock, and mixed-bedrock alluvial types), and to account for a fuller suite of climatic and non-climatic (e.g. lithological/structural, tectonic, anthropogenic) controls on river response. Nevertheless, careful regional- or continental-scale application to a range of gauged and ungauged dryland rivers may still provide the basis for making valuable insights into potential threshold river responses to 21st century hydroclimatic changes.
Forecasting the responses of dryland rivers to climate-driven hydrological changes is critical due to the importance of geomorphology for the range and quality of ecosystem services in these marginal environments1. Dryland rivers sustain many unique and threatened ecosystems and help support the livelihoods of approximately 2 billion people who live in the world’s drylands1,2. Given heightened concern over the likelihood of a global average temperature rise of >1.5 °C by the end of the century54,55, major changes to hydroclimates and river geomorphology are likely to occur within a few generations. Our approach to forecasting likely geomorphological changes in Australian dryland rivers has the potential to be applied to other gauged and ungauged dryland rivers globally, including in regions where there is a wider diversity of river styles and additional controls that may influence river response to hydroclimatic changes. As such, further development of our approach may provide a key tool to identify thresholds of river response in otherwise poorly monitored systems, and may provide advance warning of such changes to inform water resource development, adaptation, and other management strategies.
Large river catchments in continental eastern and central Australia straddle different climate zones from humid through to arid (Fig. 2). The rivers included in this study in some cases have humid upper reaches, but all have drylands (subhumid through arid climates) consisting of between 10 and 100% of their catchment areas. A framework was developed to categorise river types based on their geomorphological characteristics. The rivers analysed were the Kiewa, Mitta Mitta, Ovens, Upper Murray, Broken, Campaspe, Goulburn, Macintyre, Murrumbidgee, Avoca, Condamine-Balonne, Castlereagh, Gwydir, Lachlan, Loddon, Macquarie, Namoi, Wimmera, Bulloo, Cooper Creek, Diamantina, Georgina, Paroo, Warrego, Allungra Creek, Finke, Hay, Todd, and Woodforde. Although dryland river types fall along a continuum19,20, we use five geomorphological characteristics to define five dryland river types (Fig. 1; Table 1; see also Supplementary Fig. S1). These geomorphological characteristics were derived using Google Earth satellite imagery and a 30 m Shuttle Radar Topography Mission (SRTM) digital elevation model (DEM):
longitudinal continuity of channels (through-going, discontinuous);
nature of reduction in channel width downstream of the end of major bedrock confinement (maintaining, declining, terminating);
dominant river planform (sinuous, non-sinuous);
dominant river pattern (single-thread (meandering, straight), multi-thread (anabranching, anastomosing, distributary));
presence/absence of wetlands, and where present, type of wetlands (e.g. permanent, intermittent, ephemeral).
Aridity and hydrology
Aridity has been expressed according to the Aridity Index (AI), defined as mean annual precipitation (PPT) divided by potential mean annual evapotranspiration (PET56). AI data were sourced from the datasets compiled by Trabucco and Zomer, (200957), available from the Consultative Group for International Agriculture Research Consortium for Spatial Information (CGIAR-CSI) GeoPortal (http://www.csi.cgiar.org). Hydrology data were sourced from the New South Wales Department of Primary Industries Office of Water, the Victorian Department of Environment, Land, Water and Planning Water Measurement Information System, the Queensland Government Water Monitoring Information Portal, and the Northern Territory Water Resources Data and Information Centre. Gauges were chosen as near as possible to the end of bedrock confinement on each river (i.e. usually in the transition from the upper to middle reaches) and each had at least 30 years of continuous flow records, except for the Finke River and Allungra Creek gauges that had 13 and 16 years of flow records, respectively (Table 3). It should also be noted that the Hay River does not have a suitable gauge (the only gauges in the catchment are on small headwater creeks) and was not included in hydrological analysis, but was included for catchment aridity analyses.
Hydrological variables were calculated from these flow records using standard methods. Mean annual runoff depth was calculated by dividing mean annual discharge (megalitres; ML) by catchment area (km2). Mean annual peak runoff depth was calculated by dividing mean annual peak discharge (ML) by catchment area (km2). Coefficient of variation of annual flow (CVaf) was calculated by dividing the standard deviation of mean annual discharge by mean annual discharge. Mean floodplain slope was derived by calculating an average slope of the alluvial plain downstream of each river’s emergence from bedrock confinement using a 30 m SRTM DEM. Gross bankfull stream power is the product of bankfull discharge (m3 s−1), channel slope (m m−1), and the specific weight of water-sediment mixture (given the low suspended loads of most Australian rivers, this was assumed constant at 9800 N m-3). Gross bankfull stream power was calculated for the trunk channel at gauge locations that provided a ratings table necessary to estimate bankfull discharge; these data were only available for 14 of the 29 rivers and so there were not enough data points from each of the river types for robust analysis of similarities (ANOSIM) (see below and Fig. 5C). Channel slope data used for gross stream power estimation were calculated by dividing the local floodplain slope – calculated using 3–5 km transects along the floodplain at each gauge location using a 30 m SRTM DEM – by the channel sinuosity value measured over the same reach. The relationships between aridity and specific hydrological variables (mean annual runoff depth [annual discharge normalised for catchment area], mean annual peak runoff depth, and coefficient of variation of annual flow) were then analysed using basic linear regressions.
Climate data and future climate projections
ArcMap v.10.2 software was used for catchment scale analyses of AI, precipitation, and future climate model outputs. Gridded modern AI data were clipped to each study subcatchment and the proportional aridity was calculated with exported cell counts of each unique AI value in the sub-catchment (cells equivalent to ~1 km by ~1 km). Weighted mean catchment AI was also calculated from this output.
To derive future precipitation and potential evapotranspiration, we used outputs from 16 downscaled global climate models (GCMs) that were part of the Intergovernmental Panel on Climate Change’s (IPCC) Fifth Coupled Model Intercomparison Project, (CMIP558). These models are BCC-CSM1–1, CCSM4, CNRM-CM5, GFDL-CM3, GISS-E2-R, HadGEM2-AO, HadGEM2-CC, HadGEM2-ES, INMCM4, IPSL-CM5A-LR, MIROC-ESM-CHEM, MIROC-ESM, MIROC5, MPI-ESM-LR, MRI-CGCM3, and NorESM1-M. The outputs used were from model runs assuming Representative Concentration Pathway (RCP) 4.5. RCPs are named according to the radiative forcing of greenhouse gases expected for 2100 depending on various scales of emissions reductions (RCP2.6, 4.5, 6, 8.5)40. RCP4.5 is a relatively moderate future pathway in which emissions peak around 2040 and then decline with a radiative forcing of 4.5 W m−2 above pre-industrial values by 210040. RCP4.5 was chosen to understand which dryland river catchments were most sensitive to even relatively moderate scenarios of future climate change. Future aridity under RCP8.5 was also modelled to understand the difference between scenarios (see Supplementary Fig. S3). Due to projected increases in rainfall over parts of northern and central Australia under RCP8.5 relative to RCP4.5, projected net change in AI over the Australian continent is very similar for both RCP4.5 and RCP8.5 (Supplementary Fig. S3). Future projected precipitation is an output from the CMIP5 models. Mean annual temperature (Tmean) and annual temperature range (Trange) were the outputs used in conjunction with solar radiation (RA) to model future potential evapotranspiration (PET) using the Hargreaves-Samani equation (Eq. (1)59,60,61):
The Hargreaves-Samani equation was used to calculate the modern AI used in this study57 and therefore was also used for the future projections. It has been shown to perform nearly as well as the common FAO Penman method but requires substantially less parametrisation with more readily available data62. Future projected precipitation was then divided by modelled future potential evapotranspiration to provide future AI values across Australia.
Multivariate analysis of variables associated with river types
The five river types were compared across various hydrological and geomorphological variables using a multivariate approach in Primer v663. Data for 11 variables were collected (Table 2; Figs. 3 and 4), but bankfull gross stream power was not included in statistical tests as data were not available to calculate gross stream power for all gauges. One-way Analysis of Variance (ANOVA) tests were also performed to determine the difference between river types for each variable. Tukey’s honest significant difference (HSD) test determined which groups were significantly different from one another at p < 0.05. Results are presented in Fig. 3. Analysis of similarities (ANOSIM) and pairwise tests among all combinations of river types were performed on a resemblance matrix based on Euclidean distances, and based on 9999 permutations. R statistics were calculated for each pairwise comparison, where R values closer to 1 indicate greater differences between two compared groups63. Significance was determined where p < 0.05 (Supplementary Table S1). Based on the resemblance matrix, a non-parametric multidimensional scaling (nMDS) plot was constructed to visually represent the similarity among rivers; each point on the figure represents a single river, with points closer together being more similar to one another on the measured variables, and points farther apart being more dissimilar (Fig. 4).
Modern aridity index data are publicly available from Trabucco and Zomer’s (2009) Global Aridity Index (Global-Aridity) and Global Potential Evapo-Transpiration (Global-PET) Geospatial Database. Published online, available from the CGIAR-CSI GeoPortal at: http://www.csi.cgiar.org. Downscaled global climate model projection data are publicly available from WorldClim – Global Climate data at: www.worldclim.org/. The data that support the findings of this paper are available from the corresponding author upon reasonable request.
Millennium Ecosystem Assessment (MEA) Ecosystems and Human Well-being: Wetlands and Water (World Resources Institute: Washington, DC) (2005).
Van der Esch, S. et al. Exploring future changes in land use and land condition and the impacts on food, water, climate change and biodiversity: Scenarios for the Global Land Outlook. (PBL Netherlands Environmental Assessment Agency, The Hague) (2017).
Costanza, R. et al. The value of the world’s ecosystem services and natural capital. Nature 387, 253–260 (1998).
Pekel, J.-F., Cottam, A., Gorelick, N. & Belward, A. S. High-resolution mapping of global surface water and its long-term changes. Nature 540, 418–422 (2016).
Rodell, M. et al. Emerging trends in global freshwater availability. Nature 557, 651–659 (2018).
Best, J. Anthropogenic stresses on the world’s big rivers. Nat Geosci 12, 7–21 (2019).
Schumm, S. A. The Fluvial System. (Wiley, New York) (1977).
Nanson, G. C. & Tooth, S. Arid-zone rivers as indicators of climate change, In: Singhvi, A.K. and Derbyshire, E. (Eds.), Paleoenvironmental Reconstructions in Arid Lands, 175–216 (Balkema, Rotterdam) (1999).
Woodward, J. C., Williams, M. A. J., Garzanti, E., Macklin, M. G. & Marriner, N. From source to sink: Exploring the Quaternary history of the Nile. Quat Sci Rev 130, 3–8 (2015).
Hesse, P. P. et al. Palaeohydrology of lowland rivers in the Murray-Darling Basin, Australia. Quat Sci Rev 200, 85–105 (2018).
Lane, S. N. 21st century climate change: Where has all the geomorphology gone? Earth Surf Process Landf 38, 106–110 (2013).
Fryirs, K. A. River sensitivity: A lost foundation concept in fluvial geomorphology. Earth Surf Process Landf 42, 55–70 (2017).
Nijssen, B., O’Donnell, G. M., Hamlet, A. F. & Lettenmaier, D. P. Hydrologic sensitivity of global rivers to climate change. Clim Change 50, 143–175 (2001).
Milly, P. C. D., Dunne, K. A. & Vecchia, A. V. Global pattern of trends in streamflow and water availability in a changing climate. Nature 438, 347–350 (2005).
De Wit, M. & Stankiewicz, J. Changes in surface water supply across Africa with predicted climate change. Science 311, 1917–1921 (2006).
Brierley, G. J. & Fryirs, K. A. Eds. River Futures: An Integrative Scientific Approach to River Repair (Island Press, Washington DC) (2008).
Tooth, S. Floodouts in central Australia. In: Miller, A. J. & Gupta, A. (Eds.), Varieties of Fluvial Form, 219–247 (Wiley, Chichester) (1999).
Tooth, S. & McCarthy, T. S. Wetlands in drylands: geomorphological and sedimentological characteristics, with emphasis on examples from southern Africa. Prog Phys Geogr 31, 3–41 (2007).
Tooth, S. & Nanson, G. C. Distinctiveness and diversity of arid zone river systems. In: Thomas, D. S. G. (Ed.), 3rd edn. Arid Zone Geomorphology: Process, Form and Change in Drylands, 269–300 (John Wiley & Sons: Chichester) (2011).
Tooth, S. Dryland Fluvial Environments: Assessing Distinctiveness and Diversity from a Global Perspective, In Shroder, J. and Wohl, E. E. (Eds.) Treatise on Geomorphology 9, 612–644 (Academic Press) (2013).
Grenfell, S. E., Grenfell, M. C., Rowntree, K. M. & Ellery, W. N. Fluvial connectivity and climate: A comparison of channel pattern and process in two climatically contrasting fluvial sedimentary systems in South Africa. Geomorphology 205, 142–154 (2014).
Larkin, Z. T., Ralph, T. J., Tooth, S. & McCarthy, T. S. The interplay between extrinsic and intrinsic controls in determining floodplain wetland characteristics in the South African drylands. Earth Surf Process Landf 42, 1092–1109 (2017).
Ralph, T. J. & Hesse, P. P. Downstream hydrogeomorphic changes along the Macquarie River, southeastern Australia, leading to channel breakdown and floodplain wetlands. Geomorphology 118, 48–64 (2010).
Peel, M. C., Finlayson, B. L. & McMahon, T. A. Updated world map of the Köppen-Geiger climate classification. Hydrol Earth Syst Sci Discuss 4, 439–473 (2007).
McMahon, T. A., Finlayson, B. L., Haines, A. & Srikanthan, R. Runoff variability: a global perspective. IASH-AISH 168, 3–11 (1987).
McMahon, T. A., Peel, M. C., Vogel, R. M. & Pegram, G. G. S. Global streamflows - Part 3: Country and climate zone characteristics. J Hydrol 347, 272–291 (2007).
McMahon, T. A., Murphy, R. E., Peel, M. C., Costelloe, J. F. & Chiew, F. H. S. Understanding the surface hydrology of the Lake Eyre Basin: Part 2-Streamflow. J Arid Environ 72, 1869–1886 (2008).
Verdon, D. C., Wyatt, A. M., Kiem, A. S. & Franks, S. W. Multidecadal variability of rainfall and streamflow: Eastern Australia. Water Resour Res 40, 1–8 (2004).
Peel, M. C., McMahon, T. A. & Finlayson, B. L. Continental differences in the variability of annual runoff-update and reassessment. J Hydrol 295, 185–197 (2004).
Brierley, G.J., Fryirs, K.A. Geomorphology and River Management: Applications of the River Styles Framework (Blackwell Publications: Oxford) (2005).
Chang, H. H. Minimum stream power and river channel patterns. J Hydrol 41, 303–327 (1979).
Yochum, S. E., Sholtes, J. S., Scott, J. A. & Bledsoe, B. P. Stream power framework for predicting geomorphic change: The 2013 Colorado Front Range flood. Geomorphology 292, 178–192 (2017).
Knighton, A. D. & Nanson, G. C. Flow transmission along an arid zone anastomosing river, Cooper Creek, Australia. Hydrol Process 8(2), 137–154 (1994).
Pietsch, T. J. & Nanson, G. C. Bankfull hydraulic geometry; the role of in-channel vegetation and downstream declining discharges in the anabranching and distributary channels of the Gwydir distributive fluvial system, southeastern Australia. Geomorphology 129, 152–165 (2011).
Slingerland, R. & Smith, N. D. River avulsions and their deposits. Annu Rev Earth Planet Sci 32, 257–285 (2004).
Hughes, L. Climate change and Australia: Trends, projections and impacts. Austral Ecol 28, 423–443 (2003).
Chiew, F. H. S. & McMahon, T. A. Modelling the impacts of climate change on Australian streamflow. Hydrol Process 16, 1235–1245 (2002).
Chiew, F. H. S., Young, W. J., Cai, W. & Teng, J. Current drought and future hydroclimate projections in southeast Australia and implications for water resources management. Stoch Environ Res Risk Assess 25, 601–612 (2011).
CSIRO and Bureau of Meteorology (BoM). Projections: Atmosphere and the land, Climate Change in Australia. Information for Australia’s Natural Resource Management Regions: Technical Report (2015).
van Vuuren et al. The representative concentration pathways: An overview. Clim Change 109, 5–31 (2011).
Shi, G., Ribbe, J., Cai, W., Cowan, T. & Nin, E. An interpretation of Australian rainfall projections. Geophys Res Lett 35, 1–6 (2008).
Harris, R. M. B. et al. Biological responses to the press and pulse of climate trends and extreme events. Nat Clim Chang 8, 579–587 (2018).
Kingsford, R. T. Ecological impacts of dams, water diversions and river management on floodplain wetlands in Australia. Austral Ecol 25, 109–127 (2000).
Connell, D. & Grafton, R. Q. Water reform in the Murray-Darling Basin. Water Resour Res 47, 1–9 (2011).
Nash, L. L. & Gleick, P. H. Sensitivity of streamflow in the Colorado Basin to climatic changes. J Hydrol 125, 221–241 (1991).
Shongwe, M. E. et al. Projected Changes in Mean and Extreme Precipitation in Africa under Global Warming. Part I: Southern Africa. J Clim 22, 3819–3837 (2009).
Schewe, J. et al. Multimodel assessment of water scarcity under climate change. Proc Natl Acad Sci USA 111, 3245–3250 (2013).
Seager, R. et al. Projections of declining surface-water availability for the southwestern United States. Nat Clim Chang 3, 482–486 (2013).
Tooth, S. et al. Controls on the genesis, sedimentary architecture, and preservation potential of dryland alluvial successions in stable continental interiors: insights from the incising Modder River, South Africa. J Sediment Res 83, 541–561 (2013).
Keen-Zebert, A. et al. Late Quaternary floodplain reworking and the preservation of alluvial sedimentary archives in unconfined and confined river valleys in the eastern interior of South Africa. Geomorphology 185, 54–66 (2013).
Macklin, M. G., Tooth, S., Brewer, P. A., Noble, P. L. & Duller, G. A. T. Holocene flooding and river development in a Mediterranean steepland catchment: the Anapodaris Gorge, south central Crete, Greece. In: J.C., Woodward, P.A., Brewer, M.G., Macklin and S., Tooth (Eds), Advances in Palaeoflood Science, Special Issue of Glob Planet Change, 70, 35–52 (2010).
Bjerklie, D. M. Estimating the bankfull velocity and discharge for rivers using remotely sensed river morphology information. J Hydrol 341, 144–155 (2007).
Li, J., Tooth, S. & Yao, G. Cascades of sub-decadal, channel-floodplain changes in low-gradient, non-vegetated reaches near a dryland river terminus: Salar de Uyuni, Bolivia. Earth Surf Process Landf 44, 490–506 (2019).
IPCC. Climate Change 2014: Synthesis Report. Contribution of Working Groups I, II and III to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change, IPCC (2014).
Hoegh-Guldberg, O. et al. Impacts of 1.5 °C global warming on natural and human systems. In: Masson-Delmotte, V. et al. (Eds.) Global warming of 1.5 °C. An IPCC Special Report on the impacts of global warming of 1.5 °C above pre-industrial levels and related global greenhouse gas emission pathways, in the context of strengthening the global response to the threat of climate change, sustainable development, and efforts to eradicate poverty (2018).
United Nations Environment Programme (UNEP) World Atlas of Desertification (Edward Arnold: London) pp 15–45 (1992).
Trabucco, A. & Zomer, R. J. Global Aridity Index (Global-Aridity) and Global Potential Evapo-Transpiration (Global-PET) Geospatial Database., CGIAR Consortium for Spatial Information. Available from the CGIAR-CSI GeoPortal at: http://www.csi.cgiar.org (2009).
Hijmans, R. J., Cameron, S. E., Parra, J. L., Jones, G. & Jarvis, A. Very high resolution interpolated climate surfaces for global land areas. Int J Climatol 25, 1965–1978 (2005).
Hargreaves, G. H. & Samani, Z. A. Estimating potential evapotranspiration. J Irrig Drain Div – Am Soc Civ Eng 108, 225–230 (1982).
Hargreaves, G. H. & Samani, Z. A. Reference crop evapotranspiration from temperature. Appl Eng Agric 1, 96–99 (1985).
Hargreaves, G. H. & Allen, R. G. History and evaluation of Hargreaves evapotranspiration equation. J Irrig Drain Div – Am Soc Civ Eng 129, 53–63 (2003).
Heydari, M. M., Tajamoli, A., Ghoreishi, S. H., Darbe-Esfahani, M. K. & Gilasi, H. Evaluation and calibration of Blaney–Criddle equation for estimating reference evapotranspiration in semiarid and arid regions. Environ Earth Sci 74, 4053–4063 (2015).
Clarke, K. R. & Gorley, R. N. PRIMER v6: User Manual/Tutorial. PRIMER-E: Plymouth (2006).
Z.L. was supported by an Australian Postgraduate Award Scholarship and Macquarie University postgraduate research funds. The authors wish to thank the two anonymous reviewers, an anonymous Editorial Board Member, and Mikiko Fujita for supportive comments on the initial submission that helped to shape the final version of the paper.
The authors declare no competing interests.
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Larkin, Z.T., Ralph, T.J., Tooth, S. et al. Identifying threshold responses of Australian dryland rivers to future hydroclimatic change. Sci Rep 10, 6653 (2020). https://doi.org/10.1038/s41598-020-63622-3
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