Hostname: page-component-857557d7f7-ksgrx Total loading time: 0 Render date: 2025-12-08T17:30:39.017Z Has data issue: false hasContentIssue false
  • English
  • Français

Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef

Published online by Cambridge University Press:  11 November 2025

Holly Muecke Open the ORCID record for Holly Muecke [Opens in a new window] ,
Scott Smithers ,
Stephanie Duce ,
Sarah Hamylton Open the ORCID record for Sarah Hamylton [Opens in a new window]  and
Emily Lazarus
Holly Muecke*
Affiliation:
Earth and Environmental Sciences, College of Science and Engineering, James Cook University, Townsville, QLD, Australia Environmental Futures Research Centre, School of Science, University of Wollongong, Wollongong, NSW, Australia
Scott Smithers
Affiliation:
Earth and Environmental Sciences, College of Science and Engineering, James Cook University, Townsville, QLD, Australia
Stephanie Duce
Affiliation:
Earth and Environmental Sciences, College of Science and Engineering, James Cook University, Townsville, QLD, Australia
Sarah Hamylton
Affiliation:
Environmental Futures Research Centre, School of Science, University of Wollongong, Wollongong, NSW, Australia
Emily Lazarus
Affiliation:
Earth and Environmental Sciences, College of Science and Engineering, James Cook University, Townsville, QLD, Australia
*
Corresponding author: Holly Muecke; Email: hqwm045@uowmail.edu.au
Rights & Permissions [Opens in a new window]

Abstract

Tropical cyclones (TC) can produce waves and water levels that markedly reshape sand cay shorelines. TC Jasper (December 2023) passed near Low Island (Low Isles, Northern Great Barrier Reef [GBF]) as a category 2 storm. Using a combination of remote sensing and ground surveys, we compare detailed, high-resolution digital terrain models created before and after TC Jasper to quantify sediment redistribution around the cay during and after the event. During TC Jasper, net transport of 8,870 m3 occurred to elongate the spits at the eastern and western ends of the cay, but the sediment volume of the cay did not significantly change. Following TC Jasper, the shoreline at Low Island returned to its modal seasonal state within six months. This accords with historical accounts of seasonal shifts in shoreline configuration driven by prevailing wind and wave regimes, as well as the relatively rapid readjustment to a modal form following episodic extreme events. Overall, the documented changes to Low Island following cyclonic events highlight the complex interplay between episodic disturbances and longer-term geomorphic stability, emphasising the importance of ongoing research into these interactions as higher-intensity cyclones increase in frequency due to climate change.

Keywords

coastal geomorphologymorphodynamicsshoreline changecycloneremote sensing

Information

Type
Research Article
Information
Cambridge Prisms: Coastal Futures , Volume 3 , 2025 , e27
Check for updates
Creative Commons
Creative Common License - CCCreative Common License - BY
This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (http://creativecommons.org/licenses/by/4.0), which permits unrestricted re-use, distribution and reproduction, provided the original article is properly cited.
Copyright
© The Author(s), 2025. Published by Cambridge University Press

Impact statement

Reef islands are globally recognised as vulnerable to climate change, particularly due to the increasing frequency and intensity of storms and TCs (Kennedy, Reference Kennedy2024). TCs can cause major changes to reef islands, including major shoreline reconfiguration due to large-scale sediment redistribution (Perry et al., Reference Perry, Smithers, Kench and Pears2014; Smithers and Hoeke, Reference Smithers and Hoeke2014). Remote sensing and three-dimensional modelling applied in this study enable detailed assessment and quantification of shoreline changes resulting from TC Jasper – a moderately sized category 2 system active in the region between 2nd–13th December 2023. Reef islands are largely composed of unconsolidated biogenic carbonate sediments produced on the surrounding reef. Reef island shoreline changes have a dynamic complexity that cannot be reduced to simple net erosion or accretion; rather, they exhibit spatial and temporal patterns of localised shoreline change, including vertical adjustments (Kench and Brander, Reference Kench and Brander2006; Webb and Kench, Reference Webb and Kench2010). This study is focussed on the Low Isles, but the findings are relevant to cays globally. The results document the distribution and magnitude of shoreline changes during and after a modest cyclone event. They also provide insights into potential reef island dynamics under climate-change-modified storm regimes, offering information useful to reef island communities and ecosystem managers.

Introduction

Reef islands are low-lying sedimentary landforms that are largely composed of unconsolidated biogenic carbonate sediments produced by organisms on the host reef platform (Gourlay, Reference Gourlay1988; Kench and Brander, Reference Kench and Brander2006; Webb and Kench, Reference Webb and Kench2010; Bonesso et al., Reference Bonesso, Cuttler, Browne, Hacker and O’Leary2020). Their formation and stability reflect the interplay of local geomorphic and environmental processes operating across time scales – from relative sea-level change over centuries to millennia to daily – decadal hydrodynamic variability, including episodic high-magnitude storms (Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019). These processes are increasingly affected by anthropogenic climate change and sea-level rise, threatening both reef islands and dependent ecosystems and communities (East et al., Reference East, Perry, Kench, Liang and Gulliver2018; Shope and Storlazzi, Reference Shope and Storlazzi2019; Matera, Reference Matera2020; Kench et al., Reference Kench, Liang, Ford, Owen, Aslam, Ryan, Turner, Beetham, Dickson, Stephenson, Vila-Concejo and McLean2023; Steibl et al., Reference Steibl, Kench, Young, Wegmann, Holmes, Bunbury, Teavai-Murphy, Davies, Murphy and Russell2024). This study documents shoreline dynamics of Low Island, a sandy cay on the Great Barrier Reef (GBF), during and immediately following the passage of tropical cyclone (TC) Jasper in December 2023. Detailed surveys prior to and following the event enable quantification of the impact of such storms on the morphology of small unconsolidated reef islands, including post-event adjustments.

TCs are rotating low-pressure systems that form between 7° and 25° north and south of the equator over oceans warmer than 27 °C (Perry et al., Reference Perry, Smithers, Kench and Pears2014; Geoscience Australia, 2022). TCs are associated with sustained gale force winds (>64 km/h) gusting up to 300 km/h, heavy rainfall, significantly increased wave heights and storm surges exceeding normal tide levels (Perry et al., Reference Perry, Smithers, Kench and Pears2014; Geoscience Australia, 2022; BOM, 2024). Although cyclones are short lived, the elevated water levels and waves they generate may exceed seasonal extremes and significantly modify the geomorphology of reefs and reef islands (Stoddart, Reference Stoddart1962; Scoffin, Reference Scoffin1993; Perry et al., Reference Perry, Smithers, Kench and Pears2014; Smithers and Hoeke, Reference Smithers and Hoeke2014; Ford and Kench, Reference Ford and Kench2016). Destructive impacts include stripping of live coral cover, damage to reef structures, and burial of living reef areas with rubble and sand (Harmelin-Vivien, Reference Harmelin-Vivien1994; Puotinen, Reference Puotinen2007; Jones et al., Reference Jones, Fisher and Bessell-Browne2019), while constructive effects include sediment production and accumulation of rubble banks and ramparts (Maragos et al., Reference Maragos, Baines and Beveridge1973). Early work on the effects of cyclones on reef islands – including studies in Jaluit Atoll in the Marshall Islands (Blumenstock, Reference Blumenstock1958), Belize (formerly British Honduras) (Stoddart, Reference Stoddart1971), Ontong Java Atoll in the Solomon Islands (Bayliss-Smith, Reference Bayliss-Smith1988) and Funafuti Atoll in Tuvalu (Maragos et al., Reference Maragos, Baines and Beveridge1973; Baines and McLean, Reference Baines and McLean1976a, Reference Baines and McLean1976b) – highlighted the complex and locally variable nature of reef island responses. Stoddart (Reference Stoddart1971) identified patterns of zonal damage, greater in smaller, narrow islands near the storm centre, causing marginal erosion, vegetation loss, and the disappearance of some cays. Bayliss-Smith (Reference Bayliss-Smith1988) underscored the cyclical formation and destruction of cays, noting that some can reform after cyclone-driven erosion if sediment supply and transport conditions are favourable. Work on Funafuti Atoll similarly demonstrated how cyclones can generate entirely new depositional features and how storm ramparts evolve through time (Maragos et al., Reference Maragos, Baines and Beveridge1973; Baines and McLean, Reference Baines and McLean1976a, Reference Baines and McLean1976b). Collectively, these studies show that high-energy cyclones can reshape reef islands. Waves and currents deliver coarse sediment onto the reef flat, where it is reworked into sand over time and may also deposit windward shingle ramparts that create sheltered low-energy zones on the reef platform (Smithers and Hoeke, Reference Smithers and Hoeke2014; Maragos et al., Reference Maragos, Baines and Beveridge1973; Baines and McLean, Reference Baines and McLean1976; Mann and Westphal, Reference Mann and Westphal2016).

Despite these early studies, significant knowledge gaps remain regarding how cyclones impact cays. Detailed high-resolution 3D datasets for cays captured within a few weeks prior to and following a cyclone, from which sediment movements can be accurately measured, are rare. As climate change modifies storm regimes, it is critical to address these uncertainties , particularly when informing management strategies (Dawson, Reference Dawson2021). More systematic and technologically advanced monitoring efforts to quantify shoreline changes and sediment dynamics, both in terms of short-term cyclone damage and long-term island resilience, are urgently needed.

Cyclones on the GBR usually occur during the warmer months between November to April (BOM, 2024), with the greatest number typically forming during La Nina years when Coral Sea sea-surface temperatures are relatively warm (BOM, 2024). This study investigates the geomorphic impacts of TC Jasper on the shoreline morphology of Low Island, a small, vegetated sand cay located on the inner GBR shelf approximately 60 km north of Cairns. Detailed observations at Low Island, alongside historical records of seasonal and cyclone impacts dating back to the first Great Barrier Reef Expedition, offer a unique opportunity to understand processes shaping long-term shoreline dynamics on small dynamic cays globally (Moorehouse, Reference Moorehouse1936; Fairbridge and Teichert, Reference Fairbridge and Teichert1948; Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019; Spencer et al., Reference Spencer, Brown, Hamylton, McLean, Hawkins, Lemasson, Allcock, Bates, Byrne, Evans, Firth, Marzinelli, Russell, Smith, Swearer and Todd2021). The geomorphic impacts were established by:

  1. 1. generating 3D elevation models of Low Island prior to and following TC Jasper using remote sensing and ground survey data to quantify geomorphological changes caused by the cyclone.

  2. 2. comparing shoreline changes associated with TC Jasper to those produced by the historic 1934 cyclone and longer-term seasonal shoreline dynamics to better understand the relative significance of episodic high-energy events compared to shoreline adjustments driven by seasonal wave regimes

Study site

Low Isles (16.3840° S, 145.5599° E) is located 15 km northeast of Port Douglas (Figure 1). It is a low wooded-type reef island (sensu Hopley, Reference Hopley and Hopley2011; Hopley et al., Reference Hopley, Smithers and Parnell2007) comprising two geomorphic units: Low Island, a vegetated sand cay (~250 m long and 100 m wide) deposited on the north-western corner of the reef platform, and Woody Island, which consists of shingle ridges and a leeward mangrove forest located on the windward east to southeastern reef margin. This study is focussed on Low Island.

Figure 1. (a) Location of Low Isles in relation to Cairns, Townsville, Port Douglas and Wujal. Location of the Cairns WaveRider buoy marked in pink. (b) Low Isles reef platform showing the location of Low and Woody Islands. (c) Low Island captured in June 2023; the Caretaker’s residence is marked with a red circle.

Low Isles is culturally important to the Traditional Custodians, the Kuku Yalanji and Yirraganydji people, who know it as Wungkun. European heritage assets are also located at Low Isles, including the lighthouse built in 1874 (GBRMPA, 2018). Low Isles is historically significant as the site of the first scientific expedition on the GBR, the 1928–1929 Great Barrier Reef Expedition, and its subsequent status as the site for much ongoing reef and reef island research (see review by Spencer et al., Reference Spencer, Brown, Hamylton, McLean, Hawkins, Lemasson, Allcock, Bates, Byrne, Evans, Firth, Marzinelli, Russell, Smith, Swearer and Todd2021). A long history of detailed records of geomorphic changes at Low Island offers an unparalleled opportunity to understand geomorphic changes to the reef top landforms, including the mangrove forest, sand cay and shingle spits over extended timeframes. Low Isles also supports a range of critical ecological values including as a vital roosting site for endangered pied imperial pigeons and other seabirds (Brothers and Bone, Reference Brothers and Bone2012; Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019). Hundreds of tourists visit Low Isles on most days, attracted by these cultural, ecological and historical values.

Low island

Low Island is an oval-shaped vegetated sand cay with its long axis aligned east–west and mobile sandy spits at its eastern and western ends. The northern and southern shorelines include beachrock that is periodically buried and exposed (Stephenson et al., Reference Stephenson, Endean and Bennett1958; Stoddart et al., Reference Stoddart, McLean and Hopley1978; Frank and Jell, Reference Frank and Jell2006). The cay is predominantly composed of medium-to-coarse coral, mollusc and foraminifera sands (Fairbridge and Teichert, Reference Fairbridge and Teichert1948). The vegetated area of the cay is mostly 4–5.5 m above lowest astronomical tide (LAT), with the highest areas along the western and southern margins (Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019). Low Island’s vegetation has been recently described as dense or “well wooded”, including species such as Casuarina, Tournefortia, Scaevola and Ipomoea (Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019; Stoddart et al., Reference Stoddart, McLean and Hopley1978). However, Moorehouse (Reference Moorehouse1936) records the destruction of the cay’s vegetation during a cyclone in 1934, and photographs from 1945 show sparser vegetation than present (Fairbridge and Teichert, Reference Fairbridge and Teichert1948). Clearing for building construction and exotic plantings (e.g. frangipanis, hibiscus) has also modified vegetation cover.

Hydrodynamic regime

The hydrodynamic regime at Low Isles is largely a function of seasonal patterns. Southeasterly trade winds dominate from May to September. From October to April, the northwest monsoon brings heavier rainfall, weaker, more variable winds and episodic TCs. The wave climate at Low Isles is dominated by locally generated wind-driven waves as the outer GBR reef tract attenuates up to 95% of swell waves propagating from the Coral Sea (Gallop et al., Reference Gallop, Young, Ranasinghe, Durrant and Haigh2014). Waves therefore predominantly approach from the southeast and at higher tides propagate across the reef platform towards the northwest (Frank, Reference Frank2008). The closest WaveRider buoy, approximately 39 km to the south (16°43.830’S, 145°42.910′E, Figure 1), has collected wave data since 1975 (https://www.qld.gov.au/environment/coasts-waterways/beach/monitoring/waves-sites/cairns), establishing that the wave climate at Low Isles is seasonally variable. Short period (mean Tp 5.6 s) and generally larger waves (mean Hs 0.52 m, Hmax 2.0 m) prevail between May and September, whereas slightly smaller (mean Hs 0.46 m) and shorter period (Tp 4.7 s) are more typical during the NW monsoon. Importantly, however, NW monsoon conditions are more variable, with periods of much lower wave energy associated with wet season doldrums and episodic storms generating waves that may exceed 3 m. During the dry season, waves reliably approach Low Isles from the east-southeast in accord with the prevailing southeasterly trade winds, while storm waves in the wet season may approach from a broad range of directions depending on storm track geometry. The tides at Low Isles are semi-diurnal, with the highest astronomical tide (HAT) being 3.41 m above LAT (Queensland Government, 2025).

Tropical cyclone Jasper 2023

Severe TC Jasper (2–13 December 2023) peaked as a category 5 cyclone in the Coral Sea, south of the Solomon Islands, before weakening to category 1 as it approached the GBR (Figure 2) (Prasad, Reference Prasad2024). It then moved westwards, reintensifying into a category 2 cyclone before making landfall on the north Queensland coast near the township of Wujal, 57 km north-northwest of Low Isles, on 13 December (8 pm AEST, UTC + 10 h). The strongest winds, with gusts up to 130 km/h, were recorded south of the system, extending to Port Douglas and Low Isles. The cyclone rapidly weakened after landfall and was downgraded below TC intensity by midnight on 14 December. TC Jasper caused widespread impacts along the Far North Queensland coast due to heavy rainfall, high winds and storm waves (BOM, 2024).

Figure 2. (a) Track of severe tropical cyclone Jasper in relation to Low Isles (black triangle), with dates labelled from 02 to 16 December 2023. The colours of the points represent the cyclone category, determined based on central pressure (hPa). As the cyclone passed its closest point to Low Isles (some 57 km to the northwest), it was rated category 2, which equates to sustained winds of 89–117 km/h. Wave climate measured at the Cairns WaveRider buoy from 4th–20th December 2023; (b) wave direction and significant wave height (m), (c) maximum and significant wave heights (m) and (d) peak wave period (s). All data downloaded from the Bureau of Meteorology (2023).

Sustained winds above 89 km/h were recorded at Low Isles between 1:30 pm and 4:10 pm on December 13, with gusts peaking at 115 km/h at 3:30 pm (Prasad, Reference Prasad2024). At peak high tide, water levels at Low Isles were approximately 0.4 m above the predicted peak tide level (2.82 m LAT). At high tide on December 13, significant wave heights at the Cairns waverider buoy averaged 2.2 m, and the largest waves exceeded 4 m (Hmax).

As TC Jasper tracked north of Low Isles, the largest waves approached from the northeast (Figure 2). These waves propagated towards the northern shoreline of Low Island, unobstructed by the shingle ramparts and mangroves on the reef platform margin to the east and southeast. Significant wave heights above 1 m and maximum wave heights above 2 m persisted at the Cairns waverider buoy from 13 to 15 December. Winds strengthened again on 17 December, producing larger-than-normal waves for about 24 h (Hs peaking at just below 2 m and Hmax around 4 m).

Methods

Three-dimensional elevation models derived from drone imagery and RTK-GPS surveys were used to quantify the geomorphic changes at Low Island following TC Jasper.

Generation of 3D elevation models

Drone imagery acquisition

Three aerial drone surveys were conducted at Low Isles using DJI Mavic-3 (June 2023, June 2024) and Phantom 4 Pro RTK (January 2024) drones. Survey details including flight altitude, use of ground control points (GCPs), ground resolution and survey error are summarised in Supplementary Table 1.

RTK-GPS surveys

Ground surveys were conducted on Low Island to georectify drone imagery and ensure digital elevation model (DEM) accuracy. These surveys used a Trimble real-time kinematic GPS (RTK-GPS) R8 base and rover. The base station operated for over six hours daily to maximise positional accuracy. Base station data were submitted to the Australian Government GPS Processing Service (AUSPOS) to correct rover-collected survey points and standardise all RTK-GPS data, achieving an accuracy of 0.014 m (x), 0.015 m (y), and 0.051 m in ellipsoidal height. Key features were mapped including the cay “toe of beach” (TOB), vegetation line, and beachrock outcrops using continuous topographic point storage (Dawson, Reference Dawson2021; Talavera et al., Reference Talavera, Vila-Concejo, Webster, Smith, Duce, Fellowes, Salles, Harris, Hill, Figueira and Hacker2021) (Figure 5). The TOB is the seaward edge of the island where the beach meets the near horizontal reef flat, often delineated by a distinct break in slope and/or change from coarser beach sediment to finer rippled sediment on the reef flat (Smithers and Hoeke, Reference Smithers and Hoeke2014; Boak and Turner, Reference Boak and Turner2005). Additionally, the location and elevation of each GCP were established using the RTK-GPS rover unit for processing of the drone images to generate orthomosaics and DEMs (Joyce et al., Reference Joyce, Duce, Leahy, Leon and Maier2018). One hundred ground validation points were taken at randomly distributed locations across the island and proximal reef flat using the validation point storage setting.

Data Preparation

All photographs and orthomosaics were aligned into the same coordinate system and georeferenced using tools within ArcGIS Pro version 3.2.1. and Agisoft Metashape version 2.1.3. The drone imagery was processed in ArcGIS Pro in a separate Ortho Mapping Workspace and Agisoft Metashape to generate orthomosaics. To correct the horizontal and vertical dimensions of the orthomosaic (Joyce et al., Reference Joyce, Duce, Leahy, Leon and Maier2018), GCP survey points collected using RTK-GPS were imported into Ortho Mapping Workspace as a point file. Each point was then manually matched to the centre of the corresponding GCPs using the manage GCPs tool.

Elevation and volume change analysis

Change in cay volume between the three elevation datasets was calculated using DEMs constructed with the same coordinate system and corrected to a common elevation datum using processed RTK-GPS data (Joyce et al., Reference Joyce, Duce, Leahy, Leon and Maier2018; Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019). Digital surface models (DSM) followed by DEMs were constructed in the ArcGIS Pro Ortho Mapping Workspace. An area of interest (AOI) was extracted using the Extract by Mask tool to exclude parts of the DEM underwater or vegetated as these areas did not return reliable data.

The Raster Calculator was used to measure pixel-by-pixel elevation change between the June 2023 and January 2024 DEMs, representing beach changes before and after TC Jasper. Net volume change was calculated using the Surface Volume Tool in ArcGIS Pro, with the TOB elevation (1.35 m LAT) as the base reference. The June 2024 DEM was excluded due to limited survey coverage from higher tides. To assess sediment movement, the shoreline was divided into four compartments based on location and geomorphic features: northern shoreline (1); eastern shoreline and spit (2); southern shoreline (3); and the western shoreline and spit (4). Volume changes were calculated per compartment to quantify net sediment transfers, and total beach volume change was derived by summing all compartments.

Monthly shoreline analysis using Sentinel-2 imagery

The drone imagery used to produce the DEMs used in this investigation was captured approximately 6 months before and after TC Jasper. Therefore, geomorphological differences established by comparing these DEMS alone cannot be fully attributed to cyclone impacts. To address this challenge, the average monthly shoreline position of Low Island was established from Sentinel-2 Level 2A imagery (available for Low Isles since 2017, averages calculated from this dataset) and compared with the same months before and after TC Jasper. This approach assumes that the differences between the average monthly and monthly post-TC Jasper shorelines reflect the cyclone’s impact. The monthly average shoreline positions were established by selecting the Sentinel-2 image for each month between January 2017 and April 2024. Although coarse (10 m pixel resolution), Lazarus et al. (Reference Lazarus, Duce, Lewis and Smithers2025) showed Sentinel-2 imagery can reliably be used to detect the TOB of even the smallest GBR cays, irrespective of tide. Images with less than 30% cloud cover and low sun glint were prioritised. In ArcGIS Pro, 50 points were manually placed around the island’s TOB to represent the shoreline position. Using the Calculate Geometry tool, the coordinates of each shoreline point were calculated and saved as x and y values in the attribute table. The x and y values for each of the 50 points were averaged across the available years to produce a monthly mean shoreline. Monthly averages were re-imported into ArcGIS Pro to visualise changes in average shoreline position for each month between 2017 to 2024. Monthly shoreline positions at Low Island for the period between June 2023 and June 2024 were established using the same approach (without the eight-year averaging). The shoreline records generated by this procedure enable shoreline positions and changes for the five months prior and post-TC Jasper to be assessed.

Results

Low Island markedly changed shape between the June 2023, January 2024 and June 2024 surveys (Figure 3), as beach sediments were redistributed around the cay’s shoreline. Shorelines derived from Sentinel-2 imagery captured 11 days before and 14 days after the passage of TC Jasper suggest significant shoreline changes were associated with this event (Figure 5c).

Figure 3. Orthomosaics and DEMs generated from field surveys. Toe of beach traces are defined using DEMs.

Geomorphic changes associated with tropical cyclone Jasper

June 2023 and January 2024: Cyclone effects

Comparison of the elevation models from June 2023 and January 2024 revealed changes to Low Island’s shoreline morphology over this interval. Key changes include erosion along the northern shoreline, particularly in the northwest corner, where extensive beach rock outcrops were exposed. Two large spits also formed at the eastern and western ends of the cay, both extending southwards over the reef flat (Figure 4.1).

Figure 4. Volumetric and planimetric changes measured at Low Island across three periods to assess the effects of and recovery after tropical cyclone Jasper. (a, c, e) Elevation change models derived from the drone imagery captured pre- and post-cyclone. In net terms, dark red areas have undergone the largest volume changes, measured in reductions in elevation (erosion depth), and dark blue areas have built up the most (vertically accreted) over this period. Values in (a) indicate net change in sediment volume for each compartment; note: up or down arrows reflect this increase or decrease in sediment volume, not direction of transport. (b, d, f) Planimetric shoreline changes of the cay’s toe of beach. Blue colour indicates shoreline accretion, red; erosion, and hatched; relative stability.

The largest loss of volume (3,245 m3) occurred on the northern cay shoreline (compartment 1) (Figure 4.1a). Erosion at the western end of compartment 1 resulted in retreat of the beach and loss of the berm, reducing the elevation in this area by as much as 1.9 m. Sand volume at compartment 2 at the eastern end of the cay decreased by 1,743 m3. However, the elevation change model shows elevation gains of up to 1.5 m in some areas of compartment 2, with the spit extending approximately 51 m across the reef flat. The southern shoreline (compartment 3) is dominated by beachrock. The volume of this compartment changed little (net loss just 188 m3). The largest changes occurred in compartment 4 at the southwest end of the cay. Volume increased by 4,342 m3 and elevations by as much as 1.6–2.1 m where a large southward curving spit formed. This western spit extends 73 m over the reef flat beyond the shoreline mapped in June 2023, covering an area of around 2,740 m2 and including almost 2,845 m3 of sediment. The volume of sediment lost from all the compartments combined between June 2023 and January 2024 was very small – just 186 m3 (Figure 4.1a).

January 2024 – June 2024: Post-cyclone recovery

The June 2024 survey provides insight into Low Island’s recovery six months after TC Jasper. The elevation change model showed accretion on the northern shoreline (Compartment 1) and the largest elevation gain (3 m) at the northwestern corner (Figure 4.2c). These trends in sediment movement are the opposite of those observed following TC Jasper. The elevation of the southern edges of both the west and eastern spits (Compartments 2 and 4) was reduced, likely due to sediment being moved back towards the cay with the trade-wind-driven waves.

June 2023 – June 2024: A return to the original shoreline position

A comparison of the DEMs from June 2023 and June 2024 indicates that the beaches of Low Island had almost completely recovered to their pre-cyclone morphology and position just six months after TC Jasper. Overall, elevation differences between the June 2023 and June 2024 elevation models were relatively small, with a general trend of erosion along the eastern shoreline and accretion along the western and northwestern shoreline. Compartments 3 and 4, on the southwestern side of the island, changed least, with elevation differences of only ±0.5 m compared to the June 2023 survey. In contrast, the largest elevation changes were observed in Compartment 1 where the northwestern corner vertically accreted by 1.4–1.6 m and the northeastern shoreline eroded by 0.9–1.2 m (Figure 4.3e).

Historical and seasonal context of Low Island’s shoreline

The average monthly shorelines from 2017 to 2024 show relatively small seasonal shifts in Low Island’s shoreline, with elongated eastern and western spits visible in February and March but not in January (Figure 5). Shorelines mapped for June 2023 to June 2024 show these spits appearing in December 2023. Sentinel-2 images were captured on 2nd and 27th December, just before and after TC Jasper passed close to Low Isles on December 13 (Figure 5). The pre-TC Jasper images show that the northern shoreline was uneroded, and eastern and western spits had not formed by 2nd December. However, the images captured on 27th December record both erosion of the northern shoreline and significant sediment redistribution to form conspicuous spits at the eastern and western ends of the cay. Energetic hydrodynamic conditions during TC Jasper are implicated as the cause of observed shoreline changes by this coincident timing.

Figure 5. Comparison of monthly shorelines of Low Island during the cyclone year (a: June 2023 to June 2024) with the average shoreline position over the previous eight years (b: 2017–2024). (c) Satellite images from December 2nd and 27th, showing the shoreline before and after tropical cyclone Jasper. Shorelines were digitised using Sentinel-2 satellite imagery. Sentinel-2 images were not available February and March 2024, images for these months are instead from Planet Labs Satellite Imagery.

Discussion

Quantifying morphological and volumetric shoreline changes following a severe storm

Low Island’s response to TC Jasper demonstrates the sensitivity of small cays to hydrodynamic conditions that differ from prevailing conditions, with sediment redistributed across multiple shoreline compartments. Six weeks after TC Jasper, the upper northern beach remained steeply scarped. The presence of steep scarping suggests two key points: (1) sediments from the upper beach that are normally above the action of prevailing waves and currents were redistributed during TC Jasper and (2) morphological recovery of the upper beach is progressing more slowly than on the lower beach. At the northwestern corner of Low Island, the shoreline retreated up to 30 m during TC Jasper, producing erosion scarps 0.5–1.2 m high at the vegetation line. In contrast, the southern shoreline between the spits was not directly exposed to high wave action during TC Jasper and was largely unchanged.

Three key lines of evidence reinforce the interpretation of the northern beach erosion being sediment reworking and redistribution around the cay, rather than net export from the system: (1) the small net sediment loss quantified in the volumetric assessment following TC Jasper; (2) the elongation of the eastern and western spits towards the south; and (3) field observations of fresh sediment fans deposited above many of the conspicuous erosion scarps on the northern shoreline, indicating onshore sediment transport by waves. The large amount of sediment moved to create new features, including the erosion scarps and extensive spits, over just a few days demonstrates the sensitivity of cay morphology to higher-than-average wave energy. Many studies have similarly demonstrated that cyclones, as isolated events, can perform considerable geomorphic work on low-lying reef islands over very short timescales (Smithers and Hoeke, Reference Smithers and Hoeke2014). These observations are particularly timely as rising sea levels alter reef-top hydrodynamics, and a change in the frequency and intensity of TCs in a changing climate could increase cay morphodynamics.

The June 2024 survey completed approximately 6 months after TC Jasper offers valuable insights into Low Island’s geomorphological recovery. Although significant geomorphological change occurred rapidly during TC Jasper, comparison of the January and June 2024 DEMs (Figures 3 and 4) shows sediment moving from the eastern and western spits back towards the cay’s beaches, and towards Low Island’s northern shoreline, in the months following the event. The relatively rapid post-TC Jasper recovery of the shoreline morphology at Low Island under prevailing conditions is not unprecedented. Steers and Kemp (Reference Steers and Kemp1937) reported that Low Island had “practically regained its former shape” within two years of the 1934 cyclone which at Low Isles produced a storm surge conservatively estimated as approaching 2 m and significantly modified the surrounding reef (Moorehouse, Reference Moorehouse1936 – see later discussion). A comparison of the elevation models created for June 2023 and June 2024 (Figure 3) also shows that Low Island was very similar in size, shape and elevation in June before and after TC Jasper, suggesting the observed morphology is potentially the cay’s modal “winter state” and again emphasising the rapid recovery to this modal form possible under prevailing hydrodynamic conditions.

A comparison with seasonal shoreline dynamics and historical events

Understanding the relative influence of cyclone-driven events compared to seasonal shoreline processes is crucial for interpreting the long-term stability of reef islands, particularly as the frequency of more intense cyclones is projected to increase due to climate change (IPCC, Reference Lee and and Romero2023). Here, the effects of TC Jasper on Low Island are discussed and compared with seasonal and longer-term shoreline changes inferred from Sentinel-2 imagery, historical records and reports of previous cyclones.

Seasonal shoreline dynamics

Seasonal shoreline changes at Low Island have been previously documented by Stoddart et al. (Reference Stoddart, McLean and Hopley1978) and by Hamylton et al. (Reference Hamylton, McLean, Lowe and Adnan2019). Both described variations in sand deposition around the cay which coincided with seasonal changes in wind and wave directions. Similar changes to cay shape, particularly shifts in beach sediments and associated spits, are well documented elsewhere (Kench and Mann, Reference Kench and Mann2017; Mann and Westphal, Reference Mann and Westphal2014), with studies on the GBR showing that prevailing winds and incident waves drive sediment movement around reef island shorelines (Flood, Reference Flood1986; Hamylton and Puotinen, Reference Hamylton and Puotinen2015). Although these seasonal sediment shifts occur, and may vary interannually in magnitude, over longer timescales, they are generally balanced, with net island area and sediment volume remaining relatively stable (Kench and Brander, Reference Kench and Brander2006; Dawson and Smithers, Reference Dawson and Smithers2010; Costa et al., Reference Costa, Macedo and Siegle2019). This is certainly the case at Low Island, where comparisons with Spender’s (Spender, Reference Spender1930) detailed maps (1928–1929) show that, after 45 years (Stoddart et al., Reference Stoddart, McLean and Hopley1978), and 90 years (Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019), the cay’s area has changed by less than 1%.

Historical cyclone impacts: The 1934 cyclone event

Many severe cyclones have passed close to Low Isles in the past, including a system in 1934 for which detailed descriptions of the geomorphic impacts are available (Moorehouse, Reference Moorehouse1936). This cyclone made landfall near Cape Tribulation on March 12 with a reported barometric pressure of 978, corresponding to a Category 2 system (Callaghan et al., Reference Callaghan, Mumby and Mason2020). The event caused widespread destruction from storm tides and high winds. A storm tide of 9.1 m was reported at nearby Baileys Creek and a storm surge of 1.8 m was recorded at Port Douglas (Freeman et al., Reference Freeman, Velic, Colberg, Greenslade, Divakaran and Kepert2020). The cyclone struck Low Isles on 11 March, 1934, with Moorehouse (Reference Moorehouse1936, p. 40) reporting that Low Island was “considerably altered” by the event, with “much sand being taken from the windward [(eastern)] sides and deposited on the western or lee shore”. The 1934 cyclone and TC Jasper 2023 appear to have been of similar intensity and track when passing Low Isles, and they produced very similar geomorphological outcomes.

Deciphering event-driven vs. seasonal change

Interpreting the impacts of TC Jasper within the context of historical high-energy events and seasonal shoreline changes enables us to disentangle short-term storm impacts from longer-term coastal change. Comparison with the 1934 cyclone clearly demonstrates how high-energy events cause large-scale, abrupt changes, while longer-term satellite observations reveal gradual sediment deposition and reworking that enable the cay’s recovery between events. Seasonal variations in hydrodynamics, combined with episodic disturbances and tidal and El Niño–Southern Oscillation (ENSO)-related variability, drive the cay’s flux between phases of major change and slower rebuilding. Prevailing southeasterly trade winds during the dry season (May–October) gradually transport sediment to the northern side of the cay, building broader beaches and berms, whereas cyclones rapidly redistribute sediment from the exposed to more protected shores. We note that the shoreline exposed to higher wave energy may differ from that more usually affected by prevailing wind waves. During TC Jasper, erosion, scarping and onshore sand lobe deposition indicate waves approached from a more northerly bearing onto a shoreline that is normally well protected from the prevailing southeasterly wind waves. Although these waves are not exceptionally larger than those experienced windward of Low Isles during peak southeasterly trade winds (Hmax 4 m, Hmax 2 m), they are considerably bigger than those normally experienced on the sheltered northern shoreline. Elevated depths due to the storm surge would also allow these waves to work for longer and higher on the beach face, increasing the geomorphological impact of this event (Woodroffe, Reference Woodroffe2008; Smithers and Hoeke, Reference Smithers and Hoeke2014; Bernier et al., Reference Bernier, Hemer, Mori, Appendini, Breivik, de Camargo, Casas-Prat, Duong, Haigh, Howard, Hernaman, Huizy, Irish, Kirezci, Kohno, Lee, McInnes, Meyer, Marcos, Marsooli, Martin Oliva, Menendez, Moghimi, Muis, Polton, Pringle, Ranasinghe, Saillour, Smith, Tadesse, Swail, Tomoya, Voukouvalas, Wahl, Wang, Weisse, Westerink, Young and Zhang2024).

The curved eastern and western spits towards the south are characteristic features formed by both high-energy events and by wet-season wind and waves which can propagate from the north. Cyclones may accelerate their development or cause them to appear earlier in the season, as suggested by the eight-year average monthly shoreline data, which shows spits forming in February rather than December. Stoddart et al. (Reference Stoddart, McLean and Hopley1978) noted similar characteristics of these features over the 45-year period from 1929–1975 and concluded “in part they are doubtless seasonal, in part responses to random storm events” (p. 76). The Low Isles lighthouse keeper, quoted by Fairbridge and Teichert (Reference Fairbridge and Teichert1948, p. 74), further attested to the recurrence of such variations “every year with the change of season.” Hamylton et al. (Reference Hamylton, Carvalho, Duce, Roelfsema and Vila-Concejo2016) observed comparable terminal spits at multiple islands farther south on the GBR, consistent with the broader morphodynamic regime of seasonal and periodic change of reef islands described by Hamylton and Puotinen (Reference Hamylton and Puotinen2015).

Low Isles is a low-wooded island with a mangrove forest behind storm-wave-deposited shingle ramparts on the windward side of the reef platform. The ramparts and the mangrove forest influence the nature of hydrodynamic processes over the reef platform. Historical descriptions, mapping and imagery indicate the elevation and extent of ramparts and mangroves over the reef platform have changed markedly over the past century, modifying wave energy accessing the cay and potentially the rate and direction of spit reworking (and shoreline recovery) between events. A broad cycle of event and recovery is nonetheless observed at Low Island, with sediment redistributed alongshore as described above.

Conclusion

Low Island is a dynamic vegetated cay. Sedimentary dynamics associated with both seasonal conditions and high-energy events have driven movements in its shoreline and position on the reef platform in the past (see Moorehouse, Reference Moorehouse1936; Hamylton et al., Reference Hamylton, McLean, Lowe and Adnan2019; Smithers, Reference Smithers2022) and will continue to do so in the future. These geomorphological patterns express the balance between episodic high-energy cyclone events and prevailing hydrodynamic conditions that drive sediment transport and deposition, where cyclones can redistribute large volumes of sediment around the cay in short time periods (days), but prevailing seasonal conditions can also produce relatively rapid recovery (months to years).

With the uncertainty of a changing climate, the future trajectory of Low Island may not follow past patterns. It is already clear that prevailing environmental conditions and episodic storm events have different geomorphologic implications for Low Island, and both prevailing environmental conditions and frequency of episodic storm events are projected to change. The application of drone imagery and high-resolution 3D elevation models in this study provides new insight into sediment redistribution at event, seasonal and interannual timescales. Such technologies can be applied to quantify volumetric change on cay beaches, improving understandings of reef island dynamics.

Open peer review

To view the open peer review materials for this article, please visit http://doi.org/10.1017/cft.2025.10017.

Supplementary material

The supplementary material for this article can be found at http://doi.org/10.1017/cft.2025.10017.

Acknowledgements

We thank the Queensland Parks and Wildlife Service (QPWS) for logistical support during fieldwork. Permission to operate a drone over Low Island was granted by the Great Barrier Reef Marine Park Authority under Part 5.4 of the Zoning Plan as a management activity.

Author contribution

Holly Muecke: Writing – original draft, review and editing, visualisation, validation, methodology, investigation, data collection, conceptualisation. Scott Smithers: Writing – original draft, review and editing, visualisation, supervision, methodology, conceptualisation, data collection. Stephanie Duce: Writing – original draft, review and editing, visualisation, supervision, methodology, investigation, conceptualisation, data collection. Sarah Hamylton: Methodology, investigation, writing – review and editing, supervision, data collection. Emily Lazarus: methodology, investigation, data collection.

Financial support

This work was supported by the Hunter Research Grant (HM) and partially funded through the partnership between the Australian Government’s Reef Trust and the Great Barrier Reef Foundation as part of the Integrated Monitoring and Reporting Program – Critical Monitoring Stage 2 (SS & SD) and the Australian Research Council (S.H. and K-L.R., Discovery Project DP210100739).

Competing interests

The authors declare no known conflicts of interest that could have influenced the work reported in this paper.

AI statement

The author used OpenAI’s ChatGPT (version GPT-4, accessed via ChatGPT Free) to assist in the development of R code for visualising wind frequency data as rose plots, plotting the track of cyclone Jasper and creating the wave plots. The tool was used interactively to refine plotting scripts (using ggplot2 and tidyverse packages), ensure appropriate handling of data and improve the clarity and consistency of visual presentation. The AI tool was not used to interpret results. All code was reviewed, tested and adapted by the author to meet the research and publication requirements. Additionally, OpenAI’s ChatGPT (version GPT-5-mini, accessed via ChatGPT Free) was used for minor language and grammar edits in the manuscript text; it did not contribute to any interpretation of results or the conclusions presented in the manuscript.

References

Australian Government and Geoscience Australia (2022) Tropical cyclone & severe wind. https://www.ga.gov.au/education/natural-hazards/tropical-cyclone-and-severe-windGoogle Scholar
Baines, GB and McLean, R (1976a) Re-Surveys of 1972 Hurricane Rampart of Funafuti Atoll, Ellice Islands, Vol. 7. AUSTRALIA: CONTROL PUBL PTY LTD 14 ARCHERON ST, DONCASTER VIC 3108, pp. 36–37.Google Scholar
Baines, GB and McLean, RF (1976b) Sequential studies of hurricane deposit evolution at Funafuti atoll. Marine Geology 21(1), M1–M8.Google Scholar
Bayliss-Smith, TP (1988) The Role of Hurricanes in the Development of Reef Islands, Ontong Java Atoll, Solomon Islands. The Geographical Journal 154(3), 377. https://doi.org/10.2307/634610.Google Scholar
Bernier, NB, Hemer, M, Mori, N, Appendini, CM, Breivik, O, de Camargo, R, Casas-Prat, M, Duong, TM, Haigh, ID, Howard, T, Hernaman, V, Huizy, O, Irish, JL, Kirezci, E, Kohno, N, Lee, J-W, McInnes, KL, Meyer, EMI, Marcos, M, Marsooli, R, Martin Oliva, A, Menendez, M, Moghimi, S, Muis, S, Polton, JA, Pringle, WJ, Ranasinghe, R, Saillour, T, Smith, G, Tadesse, MG, Swail, V, Tomoya, S, Voukouvalas, E, Wahl, T, Wang, P, Weisse, R, Westerink, JJ, Young, I and Zhang, YJ (2024) Storm surges and extreme sea levels: Review, establishment of model intercomparison and coordination of surge climate projection efforts (SurgeMIP). Weather and Climate Extremes 45, 100689. https://doi.org/10.1016/j.wace.2024.100689.Google Scholar
Blumenstock, DI (1958) Typhoon effects at Jaluit atoll in the Marshall Islands. Nature 182(4645), 1267–1269.Google Scholar
Boak, EH and Turner, IL (2005) Shoreline Definition and Detection: A Review. Journal of Coastal Research 214, 688–703. https://doi.org/10.2112/03-0071.1.Google Scholar
Bonesso, JL, Cuttler, MVW, Browne, N, Hacker, J and O’Leary, M (2020) Assessing Reef Island sensitivity based on LiDAR-derived morphometric indicators. Remote Sensing 12(18). https://doi.org/10.3390/rs12183033.Google Scholar
Brothers, N and Bone, C (2012) Torresian Imperial pigeon Ducula spilorrhoa monitoring, population trends and species suitability as an indicator of environmental changes. Corella 36(3), 69–75.Google Scholar
Bureau of Meteorology and Commonwealth of Australia (2024) Tropical Cyclone Knowledge Centre. http://www.bom.gov.au/cyclone/tropical-cyclone-knowledge-centre/ (accessed 15 June 2025).Google Scholar
Callaghan, DP, Mumby, PJ and Mason, MS (2020) Near-reef and nearshore tropical cyclone wave climate in the Great Barrier reef with and without reef structure. Coastal Engineering 157, 103652.Google Scholar
Costa, MB, Macedo, EC and Siegle, E (2019) Wave refraction and reef island stability under rising sea level. Global and Planetary Change 172, 256–267. https://doi.org/10.1016/j.gloplacha.2018.10.015.Google Scholar
Dawson, JL (2021) Multi-decadal shoreline morphodynamics of a shelf-edge reef island, Great Barrier reef: Implications for future island persistence. Geomorphology 392, 107920. https://doi.org/10.1016/j.geomorph.2021.107920.Google Scholar
Dawson, JL and Smithers, SG (2010) Shoreline and beach volume change between 1967 and 2007 at Raine Island, Great Barrier reef, Australia. Global and Planetary Change 72(3), 141–154. https://doi.org/10.1016/j.gloplacha.2010.01.026.Google Scholar
East, HK, Perry, CT, Kench, PS, Liang, Y and Gulliver, P (2018) Coral reef island initiation and development under higher than present sea levels. Geophysical Research Letters 45(20), 11265–11274.Google Scholar
Fairbridge, RW and Teichert, C (1948) The low isles of the Great Barrier reef: A new analysis. The Geographical Journal 111(1/3), 67–88. https://doi.org/10.2307/1789287.Google Scholar
Flood, PG (1986) Sensitivity of coral cays to climatic variations, southern Great Barrier reef, Australia. Coral Reefs 5(1), 13–18. https://doi.org/10.1007/BF00302166.Google Scholar
Ford, MR and Kench, PS (2016) Spatiotemporal variability of typhoon impacts and relaxation intervals on Jaluit atoll, Marshall Islands. Geology 44(2), 159–162. https://doi.org/10.1130/g37402.1.Google Scholar
Frank, TD (2008) Late Holocene island reef development on the inner zone of the northern Great Barrier reef: Insights from low isles reef. Australian Journal of Earth Sciences 55(5), 669–683. https://doi.org/10.1080/08120090801982835.Google Scholar
Frank, TD and Jell, JS (2006) Recent developments on a nearshore, Terrigenous-influenced reef: Low isles reef, Australia. Journal of Coastal Research 22(3 (223)), 474–486. https://doi.org/10.2112/03-0127.1.Google Scholar
Freeman, J, Velic, M, Colberg, F, Greenslade, D, Divakaran, P and Kepert, J (2020) Development of a tropical storm surge prediction system for Australia. Journal of Marine Systems 206, 103317. https://doi.org/10.1016/j.jmarsys.2020.103317.Google Scholar
Gallop, SL, Young, IR, Ranasinghe, R, Durrant, TH and Haigh, ID (2014) The large-scale influence of the Great Barrier reef matrix on wave attenuation. Coral Reefs 33, 1167–1178.Google Scholar
GBRMPA and Commonwealth of Australia (2018) Low Islet Lightstation and Low Island Heritage Register.Google Scholar
Gourlay, MR (1988) Coral cays: Products of wave action and geological processes in a biogenic environment. Presented at the 6th International Coral Reef Symposium 2, 491–496.Google Scholar
Hamylton, SM, Carvalho, RC, Duce, S, Roelfsema, CM and Vila-Concejo, A (2016) Linking pattern to process in reef sediment dynamics at lady Musgrave Island, southern Great Barrier reef. Sedimentology 63(6), 1634–1650. https://doi.org/10.1111/sed.12278.Google Scholar
Hamylton, SM, McLean, R, Lowe, M and Adnan, FAF (2019) Ninety years of change on a low wooded island, Great Barrier reef. Royal Society Open Science 6(6), 181314. https://doi.org/10.1098/rsos.181314.Google Scholar
Hamylton, SM and Puotinen, M (2015) A meta-analysis of reef island response to environmental change on the Great Barrier reef. Earth Surface Processes and Landforms 40(8), 1006–1016. https://doi.org/10.1002/esp.3694.Google Scholar
Harmelin-Vivien, M. L. (1994). The effects of storms and cyclones on coral reefs: A review. Journal of Coastal Research, 211–231. http://www.jstor.org/stable/25735600Google Scholar
Hopley, D (2011) Reef classification by Hopley (1982). In Hopley, D (ed), Encyclopedia of Modern Coral Reefs: Structure, Form and Process. Springer Netherlands, pp. 850–854. https://doi.org/10.1007/978-90-481-2639-2_132Google Scholar
Hopley, D, Smithers, SG and Parnell, K (2007) The Geomorphology of the Great Barrier Reef: Development, Diversity and Change. Cambridge: Cambridge University PressGoogle Scholar
IPCC (2023) Sections. In Lee and, H and Romero, J (eds), Climate Change 2023: Synthesis Report. Contribution of Working Groups I, II and III to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change. Core Writing Team. Geneva, Switzerland: IPCC, pp. 35–115. https://doi.org/10.59327/IPCC/AR6-9789291691647Google Scholar
Jones, R, Fisher, R and Bessell-Browne, P (2019) Sediment deposition and coral smothering. PLoS One 14(6), e0216248. https://doi.org/10.1371/journal.pone.0216248.Google Scholar
Joyce, KE, Duce, S, Leahy, SM, Leon, J and Maier, SW (2018) Principles and practice of acquiring drone-based image data in marine environments. Marine and Freshwater Research 70(7), 952–963.Google Scholar
Kench, P and Brander, R (2006) Response of reef island shorelines to seasonal climate oscillations: South Maalhosmadulu Atoll, Maldives. Journal of Geophysical Research 111. https://doi.org/10.1029/2005JF000323.Google Scholar
Kench, PS and Brander, RW (2006) Wave processes on coral reef flats: Implications for reef geomorphology using Australian case studies. Journal of Coastal Research 22(1), 209–223. https://doi.org/10.2112/05A-0016.1.Google Scholar
Kench, PS, Liang, C, Ford, MR, Owen, SD, Aslam, M, Ryan, EJ, Turner, T, Beetham, E, Dickson, ME, Stephenson, W, Vila-Concejo, A and McLean, RF (2023) Reef islands have continually adjusted to environmental change over the past two millennia. Nature Communications 14(1), 508. https://doi.org/10.1038/s41467-023-36171-2.Google Scholar
Kench, PS and Mann, T (2017) Reef Island evolution and dynamics: Insights from the Indian and Pacific oceans and perspectives for the Spermonde archipelago. Frontiers in Marine Science 4. https://doi.org/10.3389/fmars.2017.00145.Google Scholar
Kennedy, DM (2024) A review of the vulnerability of low-lying reef island landscapes to climate change and ways forward for sustainable management. Ocean & Coastal Management 249, 106984.Google Scholar
Lazarus, E, Duce, S, Lewis, S and Smithers, S (2025) The Reef Island geomorphic activity assessment: A new approach to quantify cay geomorphic change. Global and Planetary Change 247, 104743. https://doi.org/10.1016/j.gloplacha.2025.104743.Google Scholar
Mann, T and Westphal, H (2014) Assessing Long-Term Changes in the Beach Width of Reef Islands Based on Temporally Fragmented Remote Sensing Data. Remote Sensing 6(8), 6961–6987. https://doi.org/10.3390/rs6086961.Google Scholar
Mann, T and Westphal, H (2016) Multi-decadal shoreline changes on Takú Atoll, Papua New Guinea: Observational evidence of early reef island recovery after the impact of storm waves. Geomorphology 257, 75–84. https://doi.org/10.1016/j.geomorph.2015.12.028.Google Scholar
Maragos, JE, Baines, GB and Beveridge, PJ (1973) Tropical cyclone Bebe creates a new land formation on Funafuti atoll. Science 181(4105), 1161–1164.Google Scholar
Matera, J (2020) Bridging traditional and scientific knowledge of climate change: Understanding change through the lives of small island communities. Human Ecology 48(5), 529–538.Google Scholar
Moorehouse, FW (1936) The cyclone of 1934 and its effect on low isles with special observations on Porites. Report to the Great Barrier Reef Committee 4, 37–44. https://espace.library.uq.edu.au/view/UQ:689165/ID_2291112190003131_v4x.pdf?dsi_version=768401b2d93854ed075fa8fb04be0d25.Google Scholar
Perry, CT, Smithers, SG, Kench, PS and Pears, B (2014) Impacts of cyclone Yasi on nearshore, terrigenous sediment-dominated reefs of the central Great Barrier reef, Australia. Geomorphology 222, 92–105. https://doi.org/10.1016/j.geomorph.2014.03.012.Google Scholar
Prasad, V (2024) Severe Tropical Cyclone Jasper (02U): 2–17 December 2023. Tropical Cyclone Environmental Prediction Services, Bureau of Meteorology. https://www.bom.gov.au/cyclone/history/jasper23.shtml.Google Scholar
Puotinen, ML (2007) Modelling the risk of cyclone wave damage to coral reefs using GIS: A case study of the Great Barrier reef, 1969–2003. International Journal of Geographical Information Science 21(1), 97–120. https://doi.org/10.1080/13658810600852230.Google Scholar
Queensland Government. (2025). Queensland Tide Tables (Maritime Safety Queensland) 2010–2025. The State of Queensland (Department of Transport and Main Roads). https://www.msq.qld.gov.au/tides/tide-tables.aspxGoogle Scholar
Scoffin, TP (1993) The geological effects of hurricanes on coral reefs and the interpretation of storm deposits. Coral Reefs 12, 203–221.Google Scholar
Shope, J and Storlazzi, C (2019) Assessing morphologic controls on Atoll Island alongshore sediment transport gradients due to Future Sea-level rise. Frontiers in Marine Science 6. https://doi.org/10.3389/fmars.2019.00245.Google Scholar
Smithers, SG (2022) Low Isles Erosion: Assessment of Shoreline Mobility, Beach Erosion and Potential Temporary Actions to Protect Vulnerable Assets (Unpublished) Prepared for. Queensland Parks and Wildlife Service / Great Barrier Reef Marine Park Authority.Google Scholar
Smithers, SG and Hoeke, RK (2014) Geomorphological impacts of high-latitude storm waves on low-latitude reef islands — Observations of the December 2008 event on Nukutoa, Takuu, Papua New Guinea. Geomorphology 222, 106–121. https://doi.org/10.1016/j.geomorph.2014.03.042.Google Scholar
Spencer, T, Brown, BE, Hamylton, SM and McLean, RF (2021) ‘A close and friendly alliance’: Biology, GEOLOGY and the GREAT BARRIER reef expedition of 1928–1929. In Hawkins, SJ, Lemasson, AJ, Allcock, AL, Bates, AE, Byrne, M, Evans, AJ, Firth, LB, Marzinelli, EM, Russell, BD, Smith, IP, Swearer, SE, and Todd, PA (eds), Oceanography and Marine Biology: An Annual Review, Vol. 59, pp. 89–138.Google Scholar
Spender, M (1930) Island-reefs of the Queensland coast. Part III. The Labyrinth. The Geographical Journal 76(4), 273–293. https://doi.org/10.2307/1783721.Google Scholar
Steers, JA and Kemp, FE (1937) The Coral Islands and associated features of the Great Barrier reefs (continued). The Geographical Journal 89(2), 119–140. https://doi.org/10.2307/1786122.Google Scholar
Steibl, S, Kench, PS, Young, HS, Wegmann, AS, Holmes, ND, Bunbury, N, Teavai-Murphy, TH, Davies, N, Murphy, F and Russell, JC (2024) Rethinking atoll futures: Local resilience to global challenges. Trends in Ecology & Evolution 39(3), 258–266.Google Scholar
Stephenson, W, Endean, R and Bennett, I (1958) An ecological survey of the marine fauna of low isles, Queensland. Marine and Freshwater Research 9(2), 261–318. https://doi.org/10.1071/MF9580261.Google Scholar
Stoddart, DR (1962) Catastrophic storm effects on the British Honduras reefs and cays. Nature 196(4854), 512–515. https://doi.org/10.1038/196512a0.Google Scholar
Stoddart, DR (1971) Coral Reefs and Islands and Catastrophic Storms, Applied Coastal Geomorphology. London: Macmillan, pp. 155–197Google Scholar
Stoddart, DR, McLean, RF and Hopley, D (1978) Geomorphology of Reef Islands, northern Great Barrier reef. Philosophical Transactions of the Royal Society of London. Series B, Biological Sciences 284(999), 39–61.Google Scholar
Talavera, L, Vila-Concejo, A, Webster, JM, Smith, C, Duce, S, Fellowes, TE, Salles, T, Harris, D, Hill, J, Figueira, W and Hacker, J (2021) Morphodynamic controls for growth and evolution of a rubble Coral Island. Remote Sensing 13(8), 1582.Google Scholar
Webb, AP and Kench, PS (2010) The dynamic response of reef islands to sea-level rise: Evidence from multi-decadal analysis of island change in the Central Pacific. Global and Planetary Change 72(3), 234–246. https://doi.org/10.1016/j.gloplacha.2010.05.003.Google Scholar
Woodroffe, CD (2008) Reef-island topography and the vulnerability of atolls to sea-level rise. Global and Planetary Change 62(1), 77–96. https://doi.org/10.1016/j.gloplacha.2007.11.001.Google Scholar
Figure 0

Figure 1. (a) Location of Low Isles in relation to Cairns, Townsville, Port Douglas and Wujal. Location of the Cairns WaveRider buoy marked in pink. (b) Low Isles reef platform showing the location of Low and Woody Islands. (c) Low Island captured in June 2023; the Caretaker’s residence is marked with a red circle.

Figure 1

Figure 2. (a) Track of severe tropical cyclone Jasper in relation to Low Isles (black triangle), with dates labelled from 02 to 16 December 2023. The colours of the points represent the cyclone category, determined based on central pressure (hPa). As the cyclone passed its closest point to Low Isles (some 57 km to the northwest), it was rated category 2, which equates to sustained winds of 89–117 km/h. Wave climate measured at the Cairns WaveRider buoy from 4th–20th December 2023; (b) wave direction and significant wave height (m), (c) maximum and significant wave heights (m) and (d) peak wave period (s). All data downloaded from the Bureau of Meteorology (2023).

Figure 2

Figure 3. Orthomosaics and DEMs generated from field surveys. Toe of beach traces are defined using DEMs.

Figure 3

Figure 4. Volumetric and planimetric changes measured at Low Island across three periods to assess the effects of and recovery after tropical cyclone Jasper. (a, c, e) Elevation change models derived from the drone imagery captured pre- and post-cyclone. In net terms, dark red areas have undergone the largest volume changes, measured in reductions in elevation (erosion depth), and dark blue areas have built up the most (vertically accreted) over this period. Values in (a) indicate net change in sediment volume for each compartment; note: up or down arrows reflect this increase or decrease in sediment volume, not direction of transport. (b, d, f) Planimetric shoreline changes of the cay’s toe of beach. Blue colour indicates shoreline accretion, red; erosion, and hatched; relative stability.

Figure 4

Figure 5. Comparison of monthly shorelines of Low Island during the cyclone year (a: June 2023 to June 2024) with the average shoreline position over the previous eight years (b: 2017–2024). (c) Satellite images from December 2nd and 27th, showing the shoreline before and after tropical cyclone Jasper. Shorelines were digitised using Sentinel-2 satellite imagery. Sentinel-2 images were not available February and March 2024, images for these months are instead from Planet Labs Satellite Imagery.

Supplementary material: File

Muecke et al. supplementary material

Muecke et al. supplementary material
Download Muecke et al. supplementary material(File)
File 371.4 KB

Author comment: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R0/PR1

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr1 [Opens in a new window]
Holly Muecke [Opens in a new window] School of Science, University of Wollongong, Australia
Revision round: 0
Role: author

Comments

No accompanying comment.

Review: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R0/PR2

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr2 [Opens in a new window]
Reviewer_1
Date of review:  23 July 2025
Revision round: 0
Role: reviewer
Recommendation/decision: major-revision

Conflict of interest statement

Reviewer declares none.

Comments

Overall comments: This is a nicely conducted study within the constraints of data/image availability. It reports on the effects of what was actually a quite low Cat (2) cyclone on a vegetated sand cay in the northern GBR. The data presented (on sign wave heights etc – which arguably should be the first part of the Results) actually seem to show that significant wave heights during the event were not that much higher than during seasonal events (see Fig 2 v SI Fig 1). Instead, the main difference appears to be direction of wave approach which are different to the seasonal approaches. The net effect of the TC was quite modest with island shoreline readjustments reflected mainly as a slug of sediment moving around to, especially, the SW side. However, the majority of this material seems to have been reworked back in a relatively short period after the event.

Perhaps a key point here is that this was not a major cyclone event (e.g., Cat 4/5). The real take home message to me thus seems like it should be that lower Cat cyclones do geomorphic work, perhaps especially where they impact islands from directions outside those of normal seasonal wave approaches, but that recovery can be quite fast. This nuance does not seem to come through in the impact/abstract but I feel needs to. This maybe then also leads to the need for a stronger discussion of/ comparison to what major TC events have been shown to do to islands (Bebe and others) - so a clearer comparison that these big events can do a lot of geomorphic work and indeed lead to island-building. This would to me give the paper a bit more depth and would more fully support what might be the useful contribution here that minor events are mainly exacerbating or modifying islands slightly outside seasonally shifting shoreline patterns, but that these are recoverable. However, if as some models suggest TC intensity not frequency will increase the implications under climate change may be severe.

Other comments/points.

L19 add year to date please.

L19 “calcium carbonate sands” or gravels or mixtures depending on location.

L21 “exhibit spatial and temporal patterns of localised shoreline change,” reference to Kench & Brander 2006 would be useful here as one good example.

The terms reef island, sand cay and just cay are all used on the first page. I would suggest some consistency would help and explain how a sand cay differs from a reef island.

Abstract might useful also explain how the post-event changes compared to the seasonal changes that usually occur – this is alluded to methodologically, but no finding is summarised. Indeed, coming back to this point now having read the whole paper this is really important to be clear about because 1) the magnitude of change was actually quite small and 2) the event seems to have caused a response more because of the unusual direction of wave approach than the sign wave heights, and 3) most sediment seems to have returned during later seasonal wave exposure.

I think also in the abstract that it would be worth emphasising that this was a Cat 2 event. A reasonable amount of sediment movement seems to have occurred despite this and so the fact that there was a noted geomorphic response is relevant and could be mentioned in terms of what a major event might do.

L50 “the values they support”. Do you mean services, functions, people? Values seems the wrong term here.

L52 “geomorphic impacts”. Could you expand since this is quite a generic term.

L146. Some of the material in here and the plotted data (Fig. 2) seem really to be results not background material to me in the sense that this section is reporting significant wave heights etc during the event. I wonder if this should be moved to the results section. Indeed, there may be merit in that because it would allow a clearer comparison with the normal season wave height/direction data. My reading of this data is that significant wave heights were not really much above those occurring during parts of the wet season, but the main difference was the direction of approach. A revised combination of Fig 2 and SI fig 1 may be useful here. I feel this is important and should perhaps be emphasised more strongly in e.g., abstract. Sign wave height is important but also direction of approach. Thus, during high energy events, even relatively modest (Cat 2) ones the different direction of wave approach can lead to meaningful sediment remobilisation. On L330 the point is made “when exposed to higher-than-average wave energy”. Actually as noted above wave heights were not (to my reading) much above those that are shown in SI fig 1 – so again it seems that it is perhaps the direction of high wave approach that is more important here. Significantly, and this is supported by later parts of the discussion, the amount of actual long-term change to the main part of the island “structure” seems quite limited – these lower magnitude cyclone events are either exacerbating season events or causing short-term sediment transfer of material from the beaches but this neutralises over quite short periods when the season winds move.

L228 “try to tease out”, and L232 “may have been brought about by the cyclone”. This concerningly now all sounds less certain in terms of event attribution than implied earlier in the paper.

Fig 3 – the image for June 2024 appears actually to still show the same body of sediment sitting to the SW of the island. This was traced around in Jan 2024 but not in June 2024. To me it seems a slight matter of interpretation about whether this body of moved sand has actually gone. This feeds through into Fig 4. I know the interpretation is based on toe of beach surveys but actually, and although perhaps now sitting a a very slightly lower elevation, that body of sediment in the SW block is still there (Fig. 3 – June 2024)

Fig 4 – as someone who is red-green colour blind this colour scheme is not easy to interpret. The authors might think about perhaps a blue to green scheme.

L414 “Low Island is a dynamic unvegetated cay”. I am confused. I assume you mean vegetated and that the peripheral margins are dynamic?

Review: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R0/PR3

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr3 [Opens in a new window]
Reviewer_2
Date of review:  28 August 2025
Revision round: 0
Role: reviewer
Recommendation/decision: major-revision

Conflict of interest statement

Reviewer declares none.

Comments

The manuscript titled “Effects of Tropical Cyclone Jasper at Low Island, Northern Great Barrier Reef” presents a timely and relevant case study of storm impacts on reef islands. The study is interesting and overall well-written, with clear field and remote sensing data collection and strong potential to contribute to our understanding of how unconsolidated reef islands respond to cyclonic events. This manuscript presents a valuable and well-executed dataset, and the results—particularly the documentation of shoreline and sediment reorganization without major net loss—are important for coastal geomorphology and island resilience research.

However, the manuscript in its current form requires major revision before it can be considered for publication in Coastal Futures. The abstract and introduction are at times too superficial and informal, lacking quantitative context and broader scientific framing beyond Low Isles papers. The study objectives are presented in a way that feels too site-specific and method-oriented, rather than highlighting the transferrable scientific contributions to reef island geomorphology worldwide. In fact, specific objective 2 is questionably an objective achieved by this study (it was not a dense discussion… it was good but not to be an objective of the paper). The results are promising and supported by clever figures (e.g., Figure 5), but the description is often too brief, missing detail/depth. Similarly, the discussion is somewhat repetitive (in relation to results) and site-focused.

In summary, this paper provides an important dataset and addresses a significant event, but revisions are necessary to strengthen the framing, add substance to the results and discussion, and elevate the study from a descriptive case study of Low Isles to a contribution with broader relevance. Below I provide more specific comments to support the improvement of the manuscript.

Specific comments

Line 19: Please clarify — Dec 2–13 of which year?

Line 27: This seems to be intended as the paper’s objective, but it could be improved. As the authors highlight in the importance statement, the focus should be more on island responses to storm activity rather than simply “examining shoreline changes in Low Isles.” While I personally find Low Isles interesting, other readers may not, and the objective needs to be framed more in terms of advancing scientific understanding rather than describing a single case study.

Line 32–33: Results are said to be compared to seasonal shoreline changes… but then what? Could the authors provide a bit more detail about their findings here?

Line 52: “impacts of high energy storm events”.. after this maybe add “on small unconsolidated reef islands”?

Line 54–58: This section reads as very basic TC background. I suggest using this space instead to build a stronger case for TC impacts on reef systems: e.g., coral breakage, sediment generation, sediment transport, and subsequent island morphological change.

Line 66–68: This is a long sentence. It is understandable, but worth revising for clarity.

Line 70–72: The authors touch briefly here on what I mentioned above, but I suggest opening the paragraph with this point. Also, a citation is needed.

Line 85: ENSO should be defined on first use: El Niño–Southern Oscillation (ENSO). The paragraph is acceptable, but it reads more like a study area description than the close of the introduction.

Line 90–97: This section ties back to my earlier comment about the objective being too site-specific. The objective does not have to be limited to Low Isles; it can be reframed for broader relevance. Also, the two listed “specific objectives” read more like methods than scientific objectives.

Abstract and Introduction: The writing is generally fine, but at times it feels informal and somewhat superficial. Stronger, more consistent arguments would help — for example, including quantitative values, case examples from other cyclone events, and clear take-home conclusions rather than simply “previous studies also observed shoreline changes.” This would help build a more compelling narrative that supports later discussion.

Line 99: Low Isles is described as “a low wooded island” — but aren’t there two islands? Please clarify.

Line 140: The sentence about wave periods and heights is confusing and the parentheses messy. Also, “larger wave height” is unclear — please revise.

Line 142: waves are smaller by 4 cm? Hmax is actually higher.

Line 147: I recommend calling TC Jasper instead of TCJ.

Line 158: Use “wave height” instead of “wave sizes.”

Line 160: Use “waverider” instead of “wave-rider.” Please check consistency throughout the manuscript.

Line 164: After introducing “significant wave height,” use the shorthand Hs consistently throughout.

Drone imagery acquisition section: While Table 1 provides some information, this section could benefit from more methodological detail: e.g., number of GCPs, survey error, etc. Also, regarding DEM generation: my understanding is that angled imagery (not strictly nadir/perpendicular) is required. If perpendicular imagery was used for a specific reason, please explain. If I’m mistaken, disregard this comment.

Line 213: The Talavera citation is unclear here. Also, ensure consistent naming of TC Jasper throughout.

Line 239–241: The Excel processing description is unnecessary. I suggest removing the sentence about grouping monthly files in Excel and starting instead with: “The x and y values for each of the 50 points were averaged…”

Line 252: Agreed — and the figures (which should be cited more often in the text) present very interesting results. I recommend merging this short paragraph with the previous one.

Line 258: occurred due to? TC Jasper. Also, Figure 7?

Line 282: The finding that sediment was rearranged across island compartments with minimal net loss is very interesting.

Jan–Jun 24 and Jun 23–Jun 24 sections: These deserve a more detailed description, with values presented as in the Jun 23–Jan 24 section. Avoid superficial descriptions.

Figure 5: This is a clever and effective figure — I really like it. However, as noted above, the accompanying results section (3.2) could provide more detailed interpretation.

Section 4.1 title: Consider revising to something more like “Morphological and volumetric changes following a severe storm”.

Line 311–321: This entire paragraph reads more like results. Given the short length of the paper, it feels repetitive. At the same time, I missed some of this detail while reading the actual results section. Also, the discussion of Jasper’s storm waves (height, direction), the track crossing the reef and exposing Low Isles, and the resulting morphology changes should be expanded here.

Line 329: Delete “short” — “just a few days” is clearer.

Line 330: “Many studies” — please cite specific examples to strengthen the discussion. Without references, the manuscript risks reading as a site-specific report rather than a contribution of broader relevance.

Line 333: The statement about an “increase in frequency and intensity of storms” needs a citation. Note that evidence for this is not uniform: for example, Chand et al. (2019) found statistically significant decreasing trends in both seasonal TC frequency (∼−0.115 year−1) and severe TC frequency (∼−0.112 year−1) over Australia, with >95% confidence. https://doi.org/10.1002/wcc.602

Line 375: Please correct the citation year.

Line 378: Consider merging sections to avoid so many breaks — the current structure interrupts the flow.

Line 406: While the mangroves on Low Wooded Island clearly protect Low Island from SE waves, the spits appear to be a response to diffraction of high NE waves around the island.

Recommendation: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R0/PR4

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr4 [Opens in a new window]
Alex Enriquez School of Geosciences, University of South Florida, United States
Date of review:  28 August 2025
Revision round: 0
Role: Handling Editor
Recommendation/decision: major-revision

Comments

Dear authors,

Both reviewers have recommended a major revision of your manuscript. After re-reading your paper alongside the reviewers’ comments, I agree with their recommendation. The feedback provided is constructive and will improve the clarity and discussion of an already very interesting paper.

One particular suggestion is to contextualize the wave height of the tropical cyclone in comparison with seasonal storms, which will aid in the interpretation of your results. They also note that the manuscript can use more discussion of the results.

I look forward to receiving your revised manuscript.

Decision: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R0/PR5

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr5 [Opens in a new window]
Colin Whittaker [Opens in a new window] Faculty of Engineering, UBC Institute for the Oceans and Fisheries, Canada
Revision round: 0
Role: Editor in Chief
Recommendation/decision: major-revision

Comments

No accompanying comment.

Author comment: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R1/PR6

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr6 [Opens in a new window]
Holly Muecke [Opens in a new window] School of Science, University of Wollongong, Australia
Revision round: 1
Role: author

Comments

No accompanying comment.

Review: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R1/PR7

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr7 [Opens in a new window]
Chris Perry [Opens in a new window] Geography, University of Exeter, United Kingdom of Great Britain and Northern Ireland
Date of review:  13 October 2025
Revision round: 1
Role: reviewer
Recommendation/decision: accept

Conflict of interest statement

None

Comments

I feel that the authors have done a good job of responding to the reviews and that the M/s is now reading very well.

Recommendation: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R1/PR8

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr8 [Opens in a new window]
Alex Enriquez School of Geosciences, University of South Florida, United States
Date of review:  20 October 2025
Revision round: 1
Role: Handling Editor
Recommendation/decision: accept

Comments

Reviewer 1 recommended acceptance of the manuscript. Reviewer 2 declined the second review.

I have reviewed the authors’ responses to both reviewers and examined the revised manuscript. The authors addressed all the comments (major and minor) raised by both reviewers. After re-reading the paper, I have no additional comments, concerns, or suggestions. I therefore recommend that the paper be accepted for publication.

Decision: Effects of tropical cyclone Jasper at Low Island, northern Great Barrier Reef — R1/PR9

Published online by Cambridge University Press:  11 November 2025
DOI: https://doi.org/10.1017/cft.2025.10017.pr9 [Opens in a new window]
Colin Whittaker [Opens in a new window] Faculty of Engineering, UBC Institute for the Oceans and Fisheries, Canada
Revision round: 1
Role: Editor in Chief
Recommendation/decision: accept

Comments

No accompanying comment.