# Morphologic and morphometric differences between gullies formed in different substrates on Mars: new insights into the gully formation processes

Rishitosh K Sinha, Dwijesh Ray, Tjalling de Haas, Susan J. Conway, Axel Noblet

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Rishitosh K Sinha, Dwijesh Ray, Tjalling de Haas, Susan J. Conway, Axel Noblet. Morphologic and morphometric differences between gullies formed in different substrates on Mars: new insights into the gully formation processes. Earth Surface Dynamics, 2023, 11 (4), pp.713 - 730. 10.5194/esurf-11-713-2023. hal-04262251

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# Morphologic and morphometric differences between gullies formed in different substrates on Mars: new insights into the gully formation processes

Rishitosh K. Sinha<fnref n="1" />,<fnref n="2" />, Dwijesh Ray<fnref n="1" />, Tjalling De Haas<fnref n="3" />, Susan J. Conway<fnref n="4" />, and Axel Noblet<fnref n="4" />

Correspondence: Rishitosh K. Sinha (rishitosh@prl.res.in)

Received: 9 November 2022 – Discussion started: 21 December 2022

Revised: 13 June 2023 – Accepted: 20 June 2023 – Published: 2 August 2023

**Abstract.** Martian gullies are kilometer-scale, geologically young features with a source alcove, transportation channel, and depositional fan. On the walls of impact craters, these gullies typically incise into bedrock or surfaces modified by the latitude-dependent mantle (LDM; inferred as consisting of ice and admixed dust) and glaciation. To better understand the differences in the alcoves and fans of gullies formed in different substrates and infer the flow types that led to their formation, we have analyzed the morphology and morphometry of 167 gully systems in 29 craters distributed between 30 and 75° S. Specifically we measured length, width, gradient, area, relief, and relief ratio of the gully alcoves and fans; Melton ratio, relative concavity index, and perimeter; and form factor, elongation ratio, and circularity ratio of the gully alcoves. Our study reveals that gully alcoves formed in LDM/glacial deposits are more elongated than the gully alcoves formed in bedrock, and they possess a distinctive V-shaped cross section. We have found that the mean gradient of fans formed by gullies sourced in bedrock is steeper than the mean gradient of fans of gullies sourced in LDM/glacial deposits. These differences between gullies were found to be statistically significant and discriminant analysis has confirmed that alcove perimeter, alcove relief, and fan gradient are the most important variables for differentiating gullies according to their source substrates. The comparison between the Melton ratio, alcove length, and fan gradient of Martian and terrestrial gullies reveals that Martian gully systems were likely formed by terrestrial debris-flow-like processes. Present-day sublimation of CO₂ ice on Mars may have provided the adequate flow fluidization for the formation of deposits akin to terrestrial debris-flow-like deposits.

## 1 Introduction

Gullies are found on poleward steep slopes of about 30° latitude in both hemispheres on Mars and manifest as kilometer-scale, geologically young features (formed within the last few million years) comprising an alcove, channel, and depositional fan (Malin and Edgett, 2000; Dickson et al., 2007; Reiss et al., 2004; Schon et al., 2009). Gullies occur in a wide assortment of settings, varying from the walls and central peaks of craters to walls of valleys and steep faces of

dunes, hills, and polar pits (e.g., Balme et al., 2006; Dickson et al., 2007; Dickson and Head, 2009; Conway et al., 2011, 2015; Harrison et al., 2015). On the walls of craters, gullies are found to have incised into (1) surfaces covered by a latitude-dependent mantle (LDM; e.g., Mustard et al., 2001; Dickson et al., 2012, 2015), (2) surfaces modified by former episodes of glaciation (Conway et al., 2018; De Haas 2019a; Sinha and Vijayan, 2017), and (3) bedrock (e.g., Johnsson et al., 2014; De Haas et al., 2019a; Sinha et al., 2020). A detailed investigation of the gullies formed over these different

<footnote n="1">¹Physical Research Laboratory, Ahmedabad 380009, Gujarat, India</footnote>

<footnote n="2">²Indian Institute of Technology, Gandhinagar 382355, Gujarat, India</footnote>

<footnote n="3">³Faculty of Geoscience, Universiteit Utrecht, Princetonlaan 8a, 3584 CB Utrecht, the Netherlands</footnote>

<footnote n="4">⁴Nantes Université – Université d'Angers – Le Mans Université, CNRS UMR 6112 Laboratoire de Planétologie et Géosciences, Nantes, France</footnote>
substrates is key to understanding the intricacies of past processes by which these gullies have formed on Mars (Conway et al., 2015; De Haas et al., 2019a).

A variety of models have been proposed to explain the formation of gullies, which include (1) dry flows triggered by sublimation of CO₂ frost (e.g., Cedillo-Flores et al., 2011; Dundas et al., 2012, 2015; Pilorget and Forget, 2016; De Haas et al., 2019b), (2) debris flows of an aqueous nature (e.g., Costard et al., 2002; Levy et al., 2010; Conway et al., 2011; Johnsson et al., 2014; De Haas et al., 2019a; Sinha et al., 2020), and (3) fluvial flows (e.g., Heldmann and Melton, 2004; Heldmann et al., 2005; Dickson et al., 2007; Reiss et al., 2011). To better understand the gully formation processes, a morphometric investigation of gullies formed over different substrates needs to be undertaken at a level of detail previously not attempted.

The global distribution of gullies shows a spatial correlation with the landforms indicative of glaciation and LDM deposition on Mars (e.g., Levy et al., 2011; Dickson et al., 2015; Harrison et al., 2015; Conway et al., 2018; De Haas et al., 2019a; Sinha et al., 2020). With respect to glacial landforms, many gullies have formed into viscous flow features (VFFs) and they are found in the same latitude ranges between 30–60° (e.g., Arfstrom and Hartmann, 2005; De Haas et al., 2019a). VFFs are defined as an umbrella term for glacial-type formations covering a broad range of landforms that include lobate debris aprons (LDAs), concentric crater fills (CCFs), and lineated valley fills (LVFs) (e.g., Squyres, 1978; Levy et al., 2009a; Baker et al., 2010; Hargitai, 2014). Together, they are inferred to be similar to terrestrial debris-covered glaciers (Plaut et al., 2009). With respect to the LDM, gullies are mostly found on the pole-facing slopes of crater walls at lower mid-latitudes (30–45°) (e.g., Balme et al., 2006; Kneissl et al., 2010; Harrison et al., 2015; Conway et al., 2017), wherein the LDM is found to be dissected (e.g., Mustard et al., 2001; Milliken et al., 2003; Head et al., 2003). In the higher latitudes (> 45°), the LDM is found to be continuous (e.g., Kreslavsky and Head, 2000), and gullies are evident at both the pole- and Equator-facing slopes (e.g., Balme et al., 2006; Kneissl et al., 2010; Harrison et al., 2015; Conway et al., 2017). Gullies formed on the formerly glaciated walls of craters are fed from alcoves that do not extend up to the crater rim and appear elongated to V-shaped incision, implying gully channel incision into ice-rich, un lithified sediments (e.g., Aston et al., 2011; De Haas et al., 2019a). The alcoves, channels, and fan deposits of gullies formed within craters covered by a smooth drape of the LDM are usually found to have experienced multiple episodes of the LDM covering and subsequent reactivation of some of the pre-existing channels or formation of fresh channels within the draped LDM deposits (e.g., Dickson et al., 2015; De Haas et al., 2019a). Additionally, there are gullies that directly em anate from well-defined bedrock alcoves that cut into the crater rim in the absence of LDM and/or glacial deposits (e.g., Johnsson et al., 2014; De Haas et al., 2019a; Sinha

et al., 2020). Gullies formed in these craters have alcoves with sharply defined crests and spurs, exposing the underlying bedrock, and meter-sized boulders are found throughout the gully system (e.g., Johnsson et al., 2014; De Haas et al., 2019a; Sinha et al., 2020). Further, De Haas et al. (2015a) found that the stratigraphy of the fans whose source area was in bedrock were more boulder-rich than those fans fed by catchments in the LDM. The findings in these studies suggest that a more detailed investigation of the morphology and morphometry of the gullies formed over contrasting substrates is important for improving our understanding of the formative mechanisms of gullies.

In this work, we focus on addressing the following research questions.

1. Do the morphologies and morphometries of gully systems formed in different substrates differ (i.e., LD-M/glacial deposits and bedrock)?

2. How do the morphometric characteristics of gullies formed on Mars compare to those formed by a range of processes on Earth, and what does that tell us about the formative processes of Martian gullies?

To parameterize the morphometry, we will primarily study long profiles. Previously, only a few studies have analyzed the morphometric characteristics of the gullies by studying their long profiles (e.g., Yue et al., 2014; Conway et al., 2015; De Haas et al., 2015a; Hobbs et al., 2015). These studies have focused observations on a part of the gully system and suggested that the differences in the properties of substrate into which the gullies incise play a significant role in promoting the flows that led to gully formation. Hence, for a more detailed differentiation of the gully types and interpretation of the dominant flow type that led to gully formation on Mars, quantification of the morphometric characteristics of the entire gully system is crucial.

## 2 Study sites and datasets

We characterize the morphologies and morphometries of gullies in 29 craters distributed over the Southern Hemisphere of Mars between 30° S and 75° S latitude (Fig. 1). These 29 craters are selected based on the availability of publicly released High Resolution Imaging Science Experiment (HiRISE) stereo-pair-based digital terrain models (DTMs) or the presence of suitable HiRISE stereo-pair images to produce a DTM ourselves. The HiRISE stereo-pair images are usually ~0.25–0.5 m/pixel (McEwen et al., 2007), so the DTM post spacing is ~1–2 m with vertical precision in the range of tens of centimeters (Kirk et al., 2008). Among the 29 gullied craters, publicly released DTMs are available for 25 craters (https://www.uahirise.org/hiwish/maps/dtms.jsp, last access: 18 September 2021) (Table 1). For the remaining 4 craters, we produced DTMs with the software packages USGS ISIS and BAE Systems SocetSet (Table 1) (Kirk
<table><caption>Table 1. Summary of the craters included in this study, their locations, number of gullies investigated from the crater, substrate on the crater wall in which gullies have incised, key morphological attributes of the substrate, and IDs of HiRISE imagery and digital terrain models (DTMs) used for morphological and morphometric investigation of gullies in these craters.</caption><thead><tr><th>Crater</th><th>Latitude</th><th>Longitude</th><th>No. of gullies</th><th>Substrate</th><th>Key morphological attributes</th><th>HiRISE ID</th><th>HiRISE DTM ID</th></tr></thead><tbody><tr><td>Artik</td><td>34.8° S</td><td>131.02° E</td><td>2</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_020740_1450</td><td>DTEEC_012459_1450_012314_1450_A01</td></tr><tr><td>Asimov</td><td>47.53° S</td><td>4.41° E</td><td>4</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs inside valleys</td><td>ESP_012912_1320</td><td>DTEEC_012912_1320_012767_1320_A01</td></tr><tr><td>Bunnik</td><td>38.07° S</td><td>142.07° W</td><td>8</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges</td><td>ESP_047044_1420</td><td>DTEEC_002659_1420_002514_1420_U01</td></tr><tr><td>Corozal</td><td>38.78° S</td><td>159.48° E</td><td>6</td><td>LDM/glacial deposits</td><td>Polygons, mantled alcoves/channels/fans, arcu- ate ridges, small-scale LDAs on the floor</td><td>PSP_006261_1410</td><td>DTEEC_006261_1410_014093_1410_A01</td></tr><tr><td>Dechu</td><td>42.23° S</td><td>158° W</td><td>8</td><td>LDM/glacial deposits</td><td>Polygons, mantled alcoves/channels/fans, arcu- ate ridges, small-scale LDAs on the floor</td><td>PSP_006866_1375</td><td>DTEED_023546_1375_023612_1375_A01</td></tr><tr><td>Dunkassa</td><td>37.46° S</td><td>137.06° W</td><td>5</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_032011_1425</td><td>DTEEC_039488_1420_039343_1420_A01</td></tr><tr><td>Hale</td><td>35.7° S</td><td>36.4° W</td><td>8</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, talus slope deposits</td><td>PSP_003209_1445</td><td>DTEEC_002932_1445_003209_1445_A01</td></tr><tr><td>Langtang</td><td>38.13° S</td><td>135.95° W</td><td>5</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_030099_1415</td><td>DTEEC_024099_1415_023809_1415_U01</td></tr><tr><td>Moni</td><td>46.97° S</td><td>18.79° E</td><td>5</td><td>LDM/glacial deposits</td><td>Partly infilled alcoves, mantled fan surfaces, ar- cuate ridges</td><td>ESP_056862_1325</td><td>DTEEC_007110_1325_006820_1325_A01</td></tr><tr><td>Nybyen</td><td>37.03° S</td><td>16.66° W</td><td>8</td><td>LDM/glacial deposits</td><td>Polygons, mantled alcoves/channels/fans, arcu- ate ridges</td><td>ESP_059448_1425</td><td>DTEEC_006663_1425_011436_1425_A01</td></tr><tr><td>Palikir</td><td>41.56° S</td><td>157.87° W</td><td>5</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_057462_1380</td><td>DTEEC_005943_1380_011428_1380_A01</td></tr><tr><td>Penticton</td><td>38.38° S</td><td>96.8° E</td><td>7</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_029062_1415</td><td>DTEEC_001714_1415_001846_1415_U01</td></tr><tr><td>Selevac</td><td>37.37° S</td><td>131.07° W</td><td>8</td><td>LDM/glacial deposits</td><td>Polygons, mantled alcoves/channels/fans, small-scale flows on the floor</td><td>ESP_045158_1425</td><td>DTEEC_003252_1425_003674_1425_A01</td></tr><tr><td>Raga</td><td>48.1° S</td><td>117.57° W</td><td>4</td><td>LDM</td><td>Polygons, mantled alcoves/channels/fans</td><td>ESP_041017_1315</td><td>DTEEC_014011_1315_014288_1315_A01</td></tr><tr><td>Roseau</td><td>41.7° S</td><td>150.6° E</td><td>1</td><td>LDM</td><td>Polygons, mantled alcoves/channels/fans</td><td>ESP_024115_1380/ ESP_011509_1380</td><td>ESP_024115_1380_ESP_011509_1380*</td></tr><tr><td>Taltal</td><td>39.5° S</td><td>125.8° W</td><td>7</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_037074_1400/ ESP_031259_1400</td><td>ESP_037074_1400_ESP_031259_1400*</td></tr></tbody></table>
<table><caption>Table 1. Continued</caption><thead><tr><th>Crater</th><th>Latitude</th><th>Longitude</th><th>No. of gullies</th><th>Substrate</th><th>Key morphological attributes</th><th>HiRISE ID</th><th>HiRISE DTM ID</th></tr></thead><tbody><tr><td>Talu</td><td>40.34° S 20.11° E</td><td></td><td>7</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_011817_1395</td><td>DTEEC_011817_1395_011672_1395_001</td></tr><tr><td>Triolet</td><td>37.08° S 168.02° W</td><td></td><td>4</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_047190_1425</td><td>DTEEC_023586_1425_024008_1425_A01</td></tr><tr><td>Unnamed crater</td><td>32.31° S 118.55° E</td><td></td><td>4</td><td>LDM/glacial deposits</td><td>Polygons, mantled alcoves/channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>PSP_006869_1475</td><td>DTEEC_021914_1475_022336_1475_U01</td></tr><tr><td>Unnamed crater in the Argyre basin</td><td>40.3° S 40.4° W</td><td></td><td>6</td><td>LDM/glacial deposits</td><td>Polygons, mantled alcoves/channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_032047_1395</td><td>DTEEC_012795_1395_013507_1395_A01</td></tr><tr><td>Unnamed crater in the Newton basin</td><td>38.8° S 156.8° W</td><td></td><td>5</td><td>LDM</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans</td><td>PSP_002686_1410</td><td>DTEEC_002620_1410_002686_1410_A01</td></tr><tr><td>Unnamed crater north of Corozal crater</td><td>38.53° S 159.44° E</td><td></td><td>5</td><td>LDM/glacial deposits</td><td>Polygons, mantled alcoves/channels/fans, small-scale LDAs on the floor</td><td>ESP_020884_1410</td><td>DTEEC_020884_1410_020950_1410_A01</td></tr><tr><td>Unnamed crater-1 in the Terra Sirenum</td><td>32.55° S 154.11° W</td><td></td><td>2</td><td>LDM</td><td>Mantled alcoves/channels/fans</td><td>PSP_007380_1470</td><td>DTEEC_010597_1470_007380_1470_U01</td></tr><tr><td>Unnamed crater-2 in the Terra Sirenum</td><td>38.88° S 136.36° W</td><td></td><td>6</td><td>LDM/glacial deposits</td><td>Polygons, V-shaped incisions, mantled alcoves/ channels/fans, arcuate ridges, small-scale LDAs on the floor</td><td>ESP_020407_1410</td><td>DTEEC_022108_1410_022385_1410_A01</td></tr><tr><td>Istok</td><td>45.1° S 85.82° W</td><td></td><td>8</td><td>Bedrock</td><td>Alcove cut directly into the original crater-wall material, clasts embedded into fresh deposits on fan</td><td>ESP_056668_1345</td><td>DTEEC_040607_1345_040251_1345_A01</td></tr><tr><td>Galap</td><td>37.66° S 167.07° W</td><td></td><td>8</td><td>Bedrock</td><td>Alcove cut directly into the original crater-wall material, clasts embedded into fresh deposits on fan</td><td>ESP_059770_1420</td><td>DTEEC_048983_1420_048693_1420_U01</td></tr><tr><td>Gasa</td><td>35.73° S 129.4° E</td><td></td><td>7</td><td>Bedrock</td><td>Alcove cut directly into the original crater-wall material, clasts embedded into fresh deposits on fan</td><td>ESP_057491_1440</td><td>DTEEC_021584_1440_022217_1440_A01</td></tr><tr><td>Los</td><td>35.08° S 76.23° W</td><td></td><td>7</td><td>Bedrock</td><td>Alcove cut directly into the original crater-wall material, clasts embedded into fresh deposits on fan</td><td>ESP_020774_1445/ ESP_050127_1445</td><td>DTEEC_020774_1445_ESP_050127_1445*</td></tr><tr><td>Unnamed crater-3 in the Terra Sirenum</td><td>34.27° S 165.71° E</td><td></td><td>7</td><td>Bedrock</td><td>Alcove cut directly into the original crater-wall material, clasts embedded into fresh deposits on fan</td><td>ESP_049261_1455/ ESP_049828_1455</td><td>DTEEC_049261_1455_ESP_049828_1455*</td></tr></tbody></table>

<footnote>* DTMs are produced with the software packages USGS ISIS and BAE Systems SocSet.</footnote>
<figure><img src="image_3.png" /><figcaption>**Figure 1.** Locations of craters analyzed in this study (green circles). Background: Mars Orbiter Laser Altimeter gridded data, where white is high elevation and black is low elevation; credit: MOLA Science Team/NASA/JPL.</figcaption></figure>

et al., 2008). We investigated HiRISE images of these 29 gullied craters for detailed morphological characterization of the substrate into which the crater wall gullies incise (Table 1).

# 3 Approach

## 3.1 Identification of substrate

The substrate into which the gullies have incised is identified based on the following criteria.

1. LDM/glacial deposits – any crater whose gullies incise walls that appear to be softened by the drape of smooth mantling material with polygonal cracks is inferred to have an LDM as the substrate within which gullies have incised (e.g., Mustard et al., 2001; Kreslavsky and Head, 2002; Levy et al., 2009a; Conway et al., 2018; De Haas et al., 2019a) (Fig. 2a and b). The gully alcoves on the walls of these craters may be partially to completely filled by the LDM, and in some cases, polygonized LDM materials may be seen covering the alcove walls (e.g., Christensen, 2003; Conway et al., 2018; De Haas et al., 2019a). These infilled alcoves on the crater walls are not the alcoves of gullies formed within the LDM substrate; instead, they represent the alcoves that were formed prior to the LDM emplacement epoch. Additionally, gullied craters that show evidence in the form of arcuate ridges at the foot of the walls and VFFs that cover part or the entire crater floor are inferred to have been modified by one or multiple episodes of glaciation (e.g., Arfstrom and Hartmann, 2005; Head et al., 2010; Milliken et al., 2003; Hubbard et al., 2011) (Fig. 2c). These craters host gullies that are often partially or fully covered by LDM deposits and are also inferred to incise LDM deposits.

2. Bedrock – craters where the features listed in criterion 1 (LDM/glacial deposits) are absent and where rocky material is visible extending downwards from the crater rim (Fig. 2d). This rocky material usually outcrops as spurs and can be layered or massive. The slopes can be smooth or covered with boulders, with concentrations of boulders at the slope toe.

## 3.2 Morphometric variables

The measurements we made of each gully system include alcove area, alcove perimeter, alcove length, alcove width, alcove gradient, fan area, fan length, fan width, and fan gradient (Fig. 3). In total, we derived 18 morphometric variables to characterize each gully fan and its alcove. The morphometric variables are classified into geometry, relief, gradient, and dimensionless variables (e.g., form factor, elongation ratio, and circularity ratio), and they are calculated with established mathematical equations shown in Table 2. For the gradient measurement using the DTM, the topographic profile from (1) the crest of the alcove to the apex of the fan was extracted for the alcove, and (2) the apex to the foot of the fan was extracted for the fan.

## 3.3 Gully system selection for morphometric measurements

We have selected only those gully systems for morphometric measurements in which (i) the depositional fan from an alcove–channel system is not superimposed by or interfering with the fans from the neighboring channels, (ii) there is clear association between the primary channel emanating from the alcove that extends downslope and then deposit its respective fan, (iii) no evidence of extensive cross-cutting is seen with the neighboring channels on the walls, (iv) no evidence of extensive mantling by dust/aeolian deposits is ap-
<figure><img src="image_4.png" /></figure>

**Figure 2.** Examples of morphological evidence used to identify the LDM, glacial deposits, and bedrock. (a) Smooth mantling material inferred as LDM draped on the wall of the Talu crater on the basis of polygonal cracks formed in the material. The bigger box is an expanded view of the polygons seen over the region outlined by the smaller box (HiRISE image ESP_011817_1395). (b) An infilled alcove on the wall of an unnamed crater-2 in Terra Sirenum. Polygons in the infilled material suggest presence of LDM deposits draped on the wall. The region shown in the smaller box is expanded in the bigger box to show evidence of the polygons (HiRISE image ESP_020407_1410). (c) Glaciation inferred in the Corozal crater on the basis of arcuate ridges formed at the foot of the crater wall and small-scale LDAs on the crater floor. Arrows indicate the downslope flow of LDAs on the floor (HiRISE image PSP_006261_1410). (d) Exposed fractured bedrock identified on the walls of the Istok crater within which gully alcoves have incised. The dashed lines show the gully systems that were investigated in this study (HiRISE image ESP_056668_1345). HiRISE image credit: NASA/JPL/University of Arizona.

<figure><img src="image_5.png" /></figure>

**Figure 3.** Examples of morphometric variables estimated in this work. Left panel: HiRISE DTM (Id: DTEEC_002659_1420_002514_1420) based hillshade. HiRISE DTM credit: NASA/JPL/University of Arizona. Right panel: Topographic profile: the blue profile represents the topography of gully alcove from alcove top to fan apex and the red profile represents the profile of gully fan from fan apex to fan toe.
<table><caption>Table 2. Set of morphometric variables extracted from the studied gully systems and their formulas and/or description of method.</caption><thead><tr><th>Morphometric variable</th><th>Formula and/or description of method</th><th>References</th></tr></thead><tbody><tr><td>Alcove length and width</td><td>Measured in kilometers</td><td>Tomczyk (2021)</td></tr><tr><td>Alcove area</td><td>Measured in square kilometers</td><td>Tomczyk (2021)</td></tr><tr><td>Fan length and width</td><td>Measured in kilometers</td><td>Tomczyk (2021)</td></tr><tr><td>Fan area</td><td>Measured in square kilometers</td><td>Tomczyk (2021)</td></tr><tr><td>Melton ratio</td><td>(Alcove relief)/(Alcove area<sup>-0.5</sup>)</td><td>Melton (1957)</td></tr><tr><td>Relative concavity index (RCI)</td><td>Concavity index/(maximum relief between the uppermost and lowermost points along the gully fan profile/2). Concavity index is estimated as &Sigma; (H<sub>i</sub><sup>*</sup> - H<sub>i</sub>)/N, where H<sub>i</sub><sup>*</sup> is the elevation along the straight line, H<sub>i</sub> is the elevation along the gully fan profile, N is the total number of measurement points.</td><td>Langbein (1964); Phillips and Lutz (2008)</td></tr><tr><td>Alcove gradient</td><td>Measured in degrees</td><td>Tomczyk (2021)</td></tr><tr><td>Fan gradient</td><td>Measured in degrees</td><td>Tomczyk (2021)</td></tr><tr><td>Alcove relief</td><td>Measured in kilometers</td><td>Tomczyk (2021)</td></tr><tr><td>Fan relief</td><td>Measured in kilometers</td><td>Tomczyk (2021)</td></tr><tr><td>Relief ratio (alcove and fan)</td><td>Alcove/fan relief divided by the length of the alcove/fan</td><td>Schumm (1956)</td></tr><tr><td>Alcove perimeter</td><td>Measured in kilometers</td><td>Schumm (1956)</td></tr><tr><td>Form factor</td><td>Alcove area divided by the square of the length of the alcove</td><td>Horton (1932)</td></tr><tr><td>Elongation ratio</td><td>Diameter of a circle of the same area as the alcove divided by the maximum alcove length</td><td>Schumm (1956)</td></tr><tr><td>Circularity ratio</td><td>Alcove area divided by the area of the circle having the same perimeter as the alcove perimeter</td><td>Miller (1953)</td></tr></tbody></table>

parent, and (v) no evidence of channel/fan superposition on any topographic obstacle on the walls or the floor of the crater is apparent, which may have influenced the morphometry. If in any case the fans superimpose or channels cross-cut, we have carefully demarcated the alcove-channel-fan boundary to minimize the inaccuracies in the measurements. Note that the selection of the gully systems was also constrained by the coverage of HiRISE DTMs used for morphometric analysis.

## 3.4 Statistical analysis of morphometric variables

We have two groups of gullies in our study: (1) gullies whose source areas are incised into LDM/glacial deposits and (2) gullies whose source areas are incised into the bedrock. First, for both groups, we have calculated descriptive statistics for each of the morphometric variables shown in Table 2. The significance of the difference between the values of each of the morphometric variables calculated for each group was tested using a Student's t test. To apply t tests, we have transformed the morphometric variables to remove skewness by taking their natural logarithm. The Pearson correlation analysis has been used to investigate the correlation between the selected morphometric attributes of gully alcoves and fans. We infer strong positive correlations between

variables if the correlation coefficient value is more than 0.7 and strong negative correlations if the value is less than -0.7. A very strong positive correlation between variables is inferred if the correlation coefficient is ≥ 0.9. Further, we used canonical discriminant analysis (CDA) to determine morphometric variables that provide the most discrimination between the groups of gullies. In CDA, functions are generated according to the number of groups, until a number equal to n - 1 functions is reached (n is the number of groups) (McLachlan, 2005). For the two groups of gullies in our study, there is going to be a function for which there is a standardized canonical discriminant function coefficient associated with the morphometric variable. The higher the magnitude of this coefficient for a particular morphometric variable, the higher the role of that variable in separating the groups of gullies (Conway et al., 2015). Standardization was done by dividing each value for a given variable by the maximum value.
# 4 Results

## 4.1 Morphology of gully systems

Out of the 29 gullied craters analyzed in this work, we have found that there are 24 craters influenced by LDM and/or VFFs. The remaining 5 craters have gullies incised into the exposed underlying bedrock on the wall of the crater. Below we describe the substrates identified in the studied craters and then compare the morphology of the gullies formed into those substrates.

Out of 24 craters, 4 craters (i.e., Raga, Roseau, unnamed crater in Newton basin, and unnamed crater-1 in Terra Sirenum) have gullies that are only influenced by an LDM. In these craters, we have found morphological evidence of an LDM in the form of polygonized, smooth textured material on the pole-facing walls of the craters. Morphological evidence of VFFs is not evident in these craters. In these craters, the gully alcoves and gully channels appear to have been incised into the polygonized LDM material, and the gully fan deposits are mantled. A typical example of this can be found in the unnamed crater formed inside the Newton basin (Fig. 4a). The Roseau crater, in particular, contains a large number of gully systems whose alcoves and fans are extensively mantled (Fig. 4b). The remaining 20 craters out of the 24 craters contain evidence for gullies that are influenced by both LDM and glacial deposits (Table 1). The base of the pole-facing walls and the floor of the craters within which the gully systems have formed host linear-to-sinuous arcuate ridges and VFFs, respectively. Typical examples of VFFs can be found in craters of Corozal, Talu, unnamed craters in Terra Sirenum and Argyre basin, Langtang, Dechu, and Dunkassa (Fig. 4c). In majority of the gullied craters (except Raga, Roseau, and unnamed crater-1 in Terra Sirenum) influenced by LDM and glacial deposits, gully alcoves are found to have a distinctive V-shaped cross section in their mid-section (Fig. 4d and e), they do not extend up to the crater rim, and gully systems often show multiple episodes of activity, inferred by the presence of fresh channel incision on the gully fan surfaces (Fig. 4d and e).

Istok, Galap, Gasa, Los, and an unnamed crater in the Terra Sirenum contain gully systems on the pole-facing walls that are not associated with an LDM and VFFs (Table 1). The gully alcoves inside these craters have a crenulated shape and appear to have formed by headward erosion into the bedrock of the crater rim (Fig. 4f). These craters have formed large gully systems on their pole-facing walls, with brecciated alcoves, comprising of multiple sub-alcoves and hosting many clasts/boulders (Fig. 4f).

# 5 Morphometry of gully systems

Based on the criteria summarized in Sect. 3.3, we have studied 167 gullies across 29 craters for calculation of morphometric variables. Within LDM/glacial deposits, 130 gullies

<table><caption>**Table 3.** Standardized canonical discriminant function coefficients (F1) that best separate gully systems formed on LDM/glacial deposits and bedrock.</caption><thead><tr><td>Variable</td><td>F1</td></tr></thead><tbody><tr><td>Alcove perimeter</td><td>3.552</td></tr><tr><td>Alcove relief</td><td>-2.828</td></tr><tr><td>Fan gradient</td><td>1.278</td></tr><tr><td>Fan length</td><td>-1.06</td></tr><tr><td>Fan relief</td><td>1.06</td></tr><tr><td>Relief ratio (alcove)</td><td>0.971</td></tr><tr><td>Alcove width</td><td>-0.692</td></tr><tr><td>Relief ratio (fan)</td><td>-0.665</td></tr><tr><td>Alcove gradient</td><td>-0.331</td></tr><tr><td>Alcove area</td><td>-0.319</td></tr><tr><td>Alcove length</td><td>0.23</td></tr><tr><td>Relative concavity index</td><td>-0.182</td></tr></tbody></table>

are formed, and 37 gullies are formed within the bedrock. The results of morphometric calculations are summarized for visual comparison as a boxplot (Fig. 5).

The results of the Student's *t* test indicates that all of the morphometric variables in Table 2, except fan width, fan area, Melton ratio, form factor, elongation ratio, and circularity ratio, differ significantly between LDM/glacial deposits and bedrock (Fig. 5). Compared to the mean gradient of gully fans formed in LDM/glacial deposits, bedrock gully fans are steeper and possess a higher relief ratio. The interquartile range of length, relief, and perimeter of gully alcoves formed in bedrock are also higher than the interquartile range of similar variables in LDM/glacial deposits, but the gully alcoves in LDM/glacial deposits possess much higher values of length, relief, and perimeter (Fig. 5).

Pearson correlations between morphometric attributes of gully alcoves and fans formed in bedrock and LDM/glacial deposits are summarized in Fig. 6. For bedrock, there are strong positive correlations between 12 pairs of morphometric variables and strong negative correlations between 3 pairs of morphometric variables. For LDM/glacial deposits, there are strong positive correlations between 18 pairs of morphometric variables and strong negative correlations between 3 pairs of morphometric variables. Very strong positive correlations (> 0.9) are found between 9 pairs of morphometric variables for bedrock and between 4 pairs of morphometric variables for LDM/glacial deposits.

The canonical discriminant analysis reveals that the following morphometric variables best distinguish between the gully systems formed in LDM/glacial deposits and bedrock, in descending order of importance: alcove perimeter, alcove relief, fan gradient, fan relief, fan length, relief ratio (alcove), alcove width, relief ratio (fan), alcove gradient, alcove area, alcove length, and relative concavity index (Table 3). The alcove perimeter is most important in discriminating among the gully systems formed within LDM/glacial deposits and
<figure><img src="image_6.png" /></figure>

**Figure 4.** (a) LDM draped on the wall of an unnamed crater in the Newton basin. The inset shows details of the polygonal texture of the LDM (HiRISE image PSP_002686_1410). (b) Infilled gully alcoves (arrows) and mantled fan surfaces (marked by letter "f") on the wall of the Roseau crater (HiRISE image ESP_024115_1380). (c) Arcuate ridges at the foot of the crater wall and small-scale LDAs on the floor in the Langtang crater (HiRISE image ESP_030099_1415). (d) V-shaped incisions on the LDM draped walls of the Taltal crater (HiRISE image ESP_037074_1400) and (e) the Langtang crater (HiRISE image ESP_030099_1415). Note the topographic profile (A–A') that illustrates V-shaped incision of the gully channel. (f) Gully alcoves formed in the Los crater by headward erosion into the crater rim. Individual gully alcoves formed in bedrock have multiple sub-alcoves (HiRISE image ESP_020774_1445).

bedrock, and the next two most important variables are alcove relief and fan gradient. Alcove relief and fan gradient have 4/5 and 1/3 the weight of alcove perimeter, respectively. Here, the weight values indicate the discriminatory power in separating the gullies formed in LDM/glacial deposits and bedrock. The remaining variables such as fan relief, fan length, relief ratio (alcove), alcove width, and relief ratio (fan) have nearly 1/5 or greater (but less than 1/3) of the weight of alcove perimeter discriminatory power in separating the gullies formed in LDM/glacial deposits and bedrock. The variables with the smallest magnitude, alcove gradient, alcove area, alcove length, and relative concavity index have less than 1/10 the weight of the most important variable in separating the gully systems.

# 6 Discussion

## 6.1 Unique morphology and morphometry of gully systems in different substrates

We have found that the gully systems formed in LDM/glacial deposits and bedrock can, using discriminatory analysis, be distinguished from one another in terms of perimeter and relief of gully alcoves (Table 3). Additionally, we have found statistically significant differences between the perimeters and reliefs of gully alcoves formed in LDM/glacial deposits and bedrock (Fig. 5). It is likely that these differences in the perimeters and reliefs of gully alcoves formed within morphologically distinct substrates could be due to the integral nature of the surface material within which the gully alcoves have formed. In other words, it is possible that the differ-
<figure><img src="image_7.png" /></figure>

**Figure 5.** The boxplot presented here shows the interquartile range, the central horizontal bar shows median, and whiskers show the range of values of alcove/fan geometry, relief, gradient, and dimensionless variables of gullies incised into LDM/glacial deposits (pink) and bedrock (green). *P* values on the plots represent the results of the Student's *t* tests for testing the significance of difference in means of the morphometric variables between gully systems formed on LDM/glacial deposits and bedrock. *P* values in blue correspond to significant difference (with respect to a *p* value of 0.05) and those in red are non-significant.
<figure><img src="image_8.png" /><figcaption>(b) LDM/glacial deposits</figcaption></figure>

<figure><img src="image_9.png" /><figcaption>**Figure 6.** Pearson correlations between morphometric attributes of gully alcoves and fans formed in (a) bedrock and (b) LDM/glacial deposits. Values approaching either 1 or -1 have stronger correlations. Zero indicates no correlation.</figcaption></figure>

ences in the physical properties of the sediments (namely grain size, compactness etc.) within which gully alcoves have formed played a key role in erosion of the substrate, leading to differences in their morphometric variables. Below, we elaborate on the uniqueness of the substrates within which gully alcoves have formed and discuss further the relationships between the morphometric variables of the morphologically distinct gully systems.

On Mars, VFFs contain high-purity glacial ice with a debris cover (Sharp, 1973; Squyres, 1978, 1979; Squyres and Carr, 1986; Holt et al., 2008; Plaut et al., 2009; Petersen et al.,

2018). Their surfaces have been interpreted to comprise of finer, reworked debris derived from sublimation of the underlying ice (Baker et al., 2010; Plaut et al., 2009). It has been suggested that the smooth, meters-thick draping unit on the walls of formerly glaciated craters is derived from the atmosphere as a layer of dust-rich ice primarily constituted of fine-grained materials (Kreslavsky and Head, 2000; Mustard et al., 2001). The fine-grained materials are loosely packed, unconsolidated materials exhibiting low thermal inertia values (Mellon et al., 2000; Putzig et al., 2005). Typically, gulles formed within this substrate display a smooth surface
<figure><img src="image_10.png" /><figcaption>**Figure 7.** Gullies forming in glacial sediments in deglaciated terrain in the (a) Brecon Beacons, Wales, UK on Earth (© Google Earth coordinates: 51°52′59.11″ N, 3°43′33.26″ W), (b) Talu crater (https://www.uahirise.org/ESP_011817_1395, last access: 21 June 2023) on Mars, (c) Hintereisferner, Austria (© Google Earth coordinates: 46°48′54.25″ N, 10°47′8.18″ E), on Earth, and (d) Bunnik crater (https: //www.uahirise.org/ESP_047044_1420, last access: 27 July 2023) on Mars. HiRISE image credit: NASA/JPL-Caltech/University of Arizona.</figcaption></figure>

texture wherein evidence of individual clasts or meter-scale boulders is not resolvable in HiRISE images, substantiating the dominant component of fine-grained materials within the LDM (e.g., Levy et al., 2010; De Haas et al., 2015a). Additionally, it has been found that gully alcoves incised into the LDM always have a distinctive V-shaped cross section in their mid-section (Fig. 4d and e), which when compared with similar-scaled systems on Earth, also corresponds to the presence of loose sediments constituting the LDM (Conway et al., 2018). The gully alcoves with V-shaped cross sections are found to be elongated, likely indicating incision within ice-rich unlithified sediments (Aston et al., 2011). In the studied craters, we have found that gullies incised into LDM/glacial deposits do have an elongated, V-shaped cross section in their mid-sections (Fig. 4). We propose that the presence of fine-grained, loosely packed, unconsolidated materials within LDM/glacial deposits has facilitated the formation of elongated gully alcoves with perimeters and relief s relatively higher than that of gully alcoves formed in coarse-grained bedrock substrate. This is consistent with the previous studies suggesting that gullies eroding into LD-M/glacial deposits have elongated catchments (Aston et al., 2011), whereas gullies eroding into the bedrock have more amphitheater-shaped catchments (Levy et al., 2009b). For this reason, the estimated length of gully alcoves formed in LDM/glacial deposits is found to be relatively higher than that of gully alcoves formed in bedrock (Fig. 5). Furthermore, statistical analysis has revealed a significant difference between the length of gully alcoves formed in LDM/glacial

deposits and bedrock (Fig. 5). Additionally, the presence of finer-grained sediments in LDM/glacial deposits is the likely cause of the V-shape of the incision of gully alcoves investigated in this study (Aston et al., 2011). On Earth, it has been observed that V-shaped incisions through glacial ice-rich moraines have occurred during the paraglacial phase of glacial retreat (Bennett et al., 2000; Ewertowski and Tomczyk, 2015) (Fig. 7). The paraglacial phase refers to a terrestrial post-glacial period that represents the response of changing environment to deglaciation (Bennett et al., 2000; Ewertowski and Tomczyk, 2015).

The next most important difference between these two types of gullies is the mean gradient of gully fans. At the foot of the fans, mean gradient of the fans influenced by LD-M/glacial deposits is < 15° for 61 % of the studied fans. For bedrock, 84 % of the studied fans have a mean gradient > 15° at the foot of the fans. Hence, gully fans formed in bedrock are emplaced at a relatively steeper gradient than the fans formed from gullies in LDM/glacial deposits. We propose that the nature of the mobilized material can explain this difference, with the finer-grained sediments that are characteristic of the LDM/glacial type gullies being easier to mobilize and being entrained to lower slope angles than the coarser sediments found within the bedrock type gullies.

## 6.2 Evaluation of the gully formation process

On Earth, alcove–fan systems can roughly be subdivided in flood-dominated, debris-flow-dominated, and colluvial sys-
tems. Following the terminology of De Haas et al. (2015b) and Tomczyk (2021), we define these systems as follows:

1. Flood-dominated systems – these are systems dominated by fluid-gravity flows, i.e., water floods, hyper-concentrated floods, and debris floods. The fans of such systems are commonly referred to as fluvial or alluvial fans (e.g., Ryder, 1971; Blair and McPherson, 1994; Hartley et al., 2005).

2. Debris-flow-dominated systems – these are systems dominated by sediment-gravity flows, i.e., debris flows and mud flows. Irrespective of their radial extent and positional gradients, the fans aggraded by these systems can be commonly called debris-flow fans or debris fans (Blikra and Nemec, 1998; de Scally et al., 2010).

3. Colluvial systems – these are systems dominated by rock-gravity and sediment-gravity flows, with their dominant activity relating to rockfalls, grain flows, and snow avalanches (in periglacial and alpine settings). Debris flows typically constitute only a relatively minor component of geomorphic processes in such systems. The fans of these systems are also commonly known as colluvial cones or talus cones (Siewert et al., 2012; De Haas et al., 2015b).

Although these systems may be dominated by one type of geomorphic process, it is important to stress that other processes may also occur. For example, on Earth, water floods are not uncommon on many debris-flow-dominated systems, while debris-flow deposits are commonly recognized on colluvial cones.

To compare the morphometric characteristics of the Martian gully systems to terrestrial systems, we have compiled morphometric data of gully alcoves and fans across several continents, mountain ranges, climate zones, and process types on Earth. This dataset includes published data from the Himalayas, Ladakh, India (Stolle et al., 2015), the tropical Andes, Columbia (Arango et al., 2021), Spitsbergen, Svalbard (Tomczyk, 2021), British Columbia, Canada (Kostaschuk et al., 1986; Jackson et al., 1987; and newly presented data), the southern Carpathians, Romania (Ilinca, 2021), the Southern Alps, New Zealand (de Scally and Owens, 2004; de Scally et al., 2010), the North Cascade Foothills, USA, the European Alps (including Switzerland, Italy, France, and Austria), and the Pyrenees (from multiple authors compiled by Bertrand et al., 2013). The dataset comprises information from colluvial, debris-flow-dominated, and flood-dominated (also including debris flood) systems. In total, it contains 231 colluvial systems, 749 debris-flow-dominated systems, and 369 flood-dominated systems. In total, data were compiled for 1349 systems, although not all information was available for all systems, with data availability ranging from 729 sites for alcove length to all 1349 systems for Melton index and process type. Based on these

data, we have made a heatmap of the probability of conditions dominated by flood, debris flow, or colluvial systems for combinations of Melton ratio with alcove length and fan gradient to which we compare the Martian gullies (Fig. 8). We have specifically chosen the combinations of Melton ratio with alcove length and fan gradient to infer the Martian gully formative mechanism because they have been widely used in discriminating terrestrial drainage basins and fans prone to flooding from those subject to debris flows, debris floods, and floods (e.g., de Scally and Owens, 2004; Wilford et al., 2004). We have found that the Martian gullies are indeed in the debris-flow regime on Earth. Moreover, their transition is closer to the smaller and steeper colluvial cones than to the flood-dominated fans. As expected, bedrock systems in Fig. 8d and e are closer to the colluvial systems than the LDM systems.

According to the previous reports of debris-flow-like deposits found in Martian gullies (e.g., Johnsson et al., 2014; Sinha et al., 2019, 2020), the morphological attributes of debris-flow-like deposits typically include overlapping tongue-shaped lobes with embedded clasts, channels with medial deposits, and channels with clearly defined lateral levels. However, it is still not clear whether the formation of these deposits in gullies are from sublimation of CO2 ice or due to meltwater generation. De Haas et al. (2019b) showed that CO2 sublimation may lead to flow fluidization on Mars in a manner similar to fluidization by water in terrestrial debris flows – a concept supported by the recent finding of lobate deposits and boulder-rich levee formation during the present day in the Istok crater (Table 1) (Dundas et al., 2019). The formation of these morphologically similar deposits during the present day is attributed to sublimating CO2 frost, which likely produces the necessary fluidization by gas generated from entrained CO2 frost (Dundas et al., 2019). On the basis of these recent reports (De Haas et al., 2019b; Dundas et al., 2019) and based on our own findings in this study, we argue that a debris-flow-like process similar to those operated in the terrestrial gully systems has likely dominated the flow types that lead to gully formation on Mars. Present-day sublimation of CO2 ice on Mars may have provided the necessary flow fluidization for the emplacement of deposits similar to terrestrial debris-flow-like deposits (De Haas et al., 2019b).

## 7 Conclusions

This paper compares morphological and morphometric characteristics of gully alcoves and associated fans formed in LDM/glacial deposits and bedrock over walls of 29 craters between 30° S and 75° S latitudes on Mars. Out of 29 craters, 5 craters have alcove-fan systems formed within the bedrock and the remaining 24 craters have alcove-fan systems formed within LDM/glacial deposits. From our analysis of 167 gullies, we posit that gully systems formed in LDM/glacial deposits may have been similar to those in terrestrial systems, with data availability ranging from 729 sites for alcove length to all 1349 systems for Melton index and process type. Based on these
<figure><img src="image_11.png" /><figcaption>**Figure 8.** Comparison of combinations of Melton ratio with alcove length and fan gradient. The probability heat maps are based on previously published data – see text for references. The Martian gully systems formed in LDM/glacial deposits and bedrock are found to be in the debris-flow regime on Earth. The gray area shows the realm of the colluvial, debris-flow, and fluvial fans together.</figcaption></figure>

posits and bedrock differ from one another using the following lines of evidence:

- Gully alcoves formed in LDM/glacial deposits are more elongated than the gully alcoves formed in bedrock, and they possess a distinctive V-shaped cross section.

- The mean gradient of gully fans formed in bedrock is steeper than the mean gradient of fans formed from gullies in LDM/glacial deposits.

The morphological distinction reported between gullies formed in the bedrock and LDM/glacial deposits signifies that Martian gullies may have multiple formative environments. We infer that the presence of mantling material could be one of the key factors in constraining the mechanisms forming Martian gully systems and that the presence of LDM would promote the formation of elongated gully alcoves with perimeters and reliefs relatively higher than that of gully alcoves formed in coarse-grained bedrock substrate.

Based on the combinations of Melton ratio with alcove length and fan gradient, we suggest that the gully systems studied in this work were likely dominated by terrestrial debris-flow-like processes during their formation. This is consistent with the findings reported in previous studies that showed evidence of formation of deposits morphologically similar to terrestrial debris-flow-like deposits, both in the past and during the present day (e.g., Johnsson et al., 2014; Dunzas et al., 2019). The present-day sublimation of CO₂ ice on Mars is envisaged to provide the necessary flow fluidization for the emplacement of deposits similar to debris-flow-like deposits on Earth (De Haas et al., 2019b).

**Data availability.** The newly generated DEM used in this work can be downloaded from https://doi.org/10.6084/m9 figshare.21717164.v1 (Sinha et al., 2022a). The measurement datasets can be downloaded from https://doi.org/10.6084/m9 figshare.21717182.v1 (Sinha et al., 2022b).

**Author contributions.** RKS, TDH, and SJC conceptualized this work. The methodology was developed by RKS, TDH, and SJC. Data curation and formal analyses were performed by RKS. TDH and AN also contributed to the collection of datasets used in this work. RKS, DR, TDH, and SJC contributed to the interpretation of the data and results. RKS wrote the original draft of this paper, which was reviewed and edited by all authors.

**Competing interests.** At least one of the (co-)authors is a guest member of the editorial board of *Earth Surface Dynamics* for the special issue “Planetary landscapes, landforms, and their analogues”. The peer-review process was guided by an independent editor, and the authors have also no other competing interests to declare.

**Disclaimer.** Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
**Special issue statement.** This article is part of the special issue "Planetary landscapes, landforms, and their analogues". It is not associated with a conference.

**Acknowledgements.** We are grateful and thank both the anonymous reviewers for thorough assessment of our paper and for providing us with constructive comments and suggestions. Thanks to the Editor (Heather Viles) and Associate Editor (Frances E. G. Butcher) at Earth Surface Dynamics for the editorial handling of the paper. We would like to thank the HiRISE team for their work in producing the images and digital elevation models used in this study; it would have been impossible without them. Rishitosh K. Sinha and Dwijesh Ray acknowledge the financial support by the Indian Space Research Organisation, Department of Space, Government of India. Susan J. Conway and Axel Noblet are grateful for the financial support from Région Pays de la Loire, project étoiles montantes METAFLOWS (convention no. 2019-14294) as well as the financial support of CNES in support of their HiRISE work. Tjalling De Haas was supported by the Netherlands Organisation for Scientific Research (NWO) (grant 016.Veni.192.001). We acknowledge the efforts of team MUTED to develop an online tool (http://muted.wwu.de/, last access: 21 June 2023) for quick identification of the spatial and multi-temporal coverage of planetary image data from Mars. All the planetary datasets used in this work are available for free download at the PDS Geosciences Node Mars Orbital Data Explorer (ODE) (https://ode.rsl.wustl.edu/mars/, last access: 21 June 2023) and https://www.uahirise.org/ (last access: 21 June 2023). The newly generated DTM s can be downloaded from https://figshare.com/articles/dataset/Self_generated_DEMs/21717164 (last access: 22 July 2023). The measurement datasets can be downloaded from https://figshare.com/articles/dataset/Measurement_data_of_gully_systems_in_the_southern_mid_latitudes_of_Mars/21717182 (last access: 22 July 2023). This work is a part of the PhD work of Rishitosh K. Sinha. Director PRL, Head of Planetary Science Division, PRL, Head of Planetary Remote Sensing Section, PRL, and Director IIT Gandhinagar are gratefully acknowledged for constant encouragement during the work.

**Financial support.** This research has been supported by the Indian Space Research Organisation, Department of Space, Government of India, Région Pays de la Loire, project étoiles montantes METAFLOWS (convention no. 2019-14294), Centre National d'Etudes Spatiales, and Netherlands Organisation for Scientific Research (NWO) (grant no. 016.Veni.192.001).

**Review statement.** This paper was edited by Frances E. G. Butcher and reviewed by two anonymous references.

## References

Arango, M. I., Aristizábal, E., and Gómez, F.: Morphometrical analysis of torrential flows-prone catchments in tropical and mountainous terrain of the Colombian Andes by machine learning techniques, Nat. Hazards, 105, 983–1012, https://doi.org/10.1007/s11069-020-04346-5, 2021.

Arfstrom, J. and Hartmann, W. K.: Martian flow features, moraine-like ridges, and gullies: terrestrial analogs and interrelationships, Icarus, 174, 321–335, https://doi.org/10.1016/j.icarus.2004.05.026, 2005.

Aston, A., Conway, S., and Balme, M.: Identifying Martian Gully Evolution, in: Martian Geomorphology, edited by: Balme, M. R., Bargery, A. S., Gallagher, C. J., and Gupta, S., Geological Society, London, Special Publications, 356, 151–169, https://doi.org/10.1144/SP356.9, 2011.

Baker, D. M. H, James W. H., and David R. M.: Flow patterns of lobate debris aprons and lineated valley fill north of Ismeniae Fossae, Mars: Evidence for extensive mid-latitude glaciation in the Late Amazonian, Icarus, 207, 186–209, https://doi.org/10.1016/j.icarus.2009.11.017, 2010.

Balme, M., Mangold, N. Et Al.: Orientation and distribution of recent gullies in the Southern Hemisphere of Mars: observations from High Resolution Stereo Camera/Mars Express (HRSC/MEX) and Mars Orbiter Camera/Mars Global Surveyor (MOC/MGS) data, J. Geophys. Res.-Planet., 111, E05001, https://doi.org/10.1029/2005JE002607, 2006.

Bennett, M. R., Huddart, D., Glasser, N. F., and Hambrey, M. J.: Resedimentation of debris on an ice-cored lateral moraine in the high-Arctic (Kongsvegen, Svalbard), Geomorphology, 35, 21–40, https://doi.org/10.1016/S0169-555X(00)00017-9, 2000.

Bertrand, M., Liébault, F., and Piégay, H.: Debris-flow susceptibility of upland catchments, Nat. Hazards, 67, 497–511, https://doi.org/10.1007/s11069-013-0575-4, 2013.

Blair, T. C. and McPherson, J. G.: Alluvial fan processes and forms, in: Geomorphology of desert environments, Springer, Dordrecht, the Netherlands, 354–402, https://doi.org/10.1007/978-94-015-8254-4_14, 1994.

Blikra, L. H. and Nemec, W.: Postglacial colluvium in western Norway: depositional processes, facies and palaeoclimatic record, Sedimentology, 45, 909–960, https://doi.org/10.1046/j.1365-3091.1998.00200.x, 1998.

Cedillo-Flores, Y., Treiman, A. H., Lasue, J., and Clifford, S. M.: CO₂ gas fluidization in the initiation and formation of Martian polar gullies, Geophys. Res. Lett., 38, L21202, https://doi.org/10.1029/2011GL049403, 2011.

Christensen, P. R.: Formation of recent Martian gullies through melting of extensive water-rich snow deposits, Nature, 422, 45–48, https://doi.org/10.1038/nature01436, 2003.

Conway, S. J., Balme, M. R., Murray, J. B., Towner, M. C., Okubo, C. H., and Grindrod, P. M.: The indication of Martian gully formation processes by slope-area analysis, in: Martian Geomorphology, edited by: Balme, M. R., Bargery, A. S., Gallagher, C. J., and Gupta, S., Geological Society, London, Special Publications, 356, 171–201, https://doi.org/10.1144/SP356.10, 2011.

Conway, S. J., Balme, M. R., Kreslavsky, M. A., Murray, J. B., and Towner, M. C.: The comparison of topographic long profiles of gullies on Earth to gullies on
Mars: a signal of water on Mars, Icarus, 253, 189–204,
https://doi.org/10.1016/j.icarus.2015.03.009, 2015.

Conway, S. J., Harrison, T. N., Soare, R. J., Britton, A. W., and
Steele, L. J.: New slope-normalized global gully density and ori-
entation maps for Mars, in: Martian Gullies and their Earth Ana-
logues, edited by: Conway, S. J., Carrivick, J. L., Carling, P. A.,
De Haas, T., and Harrison, T. N., Geol. Soc. Lond. Spec. Publ.,
467, 187–197, https://doi.org/10.1144/SP467.3, 2017.

Conway, S. J., Butcher, F. E., De Haas, T., Deijns, A. A.,
Grindrod, P. M., and Davis, J. M.: Glacial and gully erosion
on Mars: A terrestrial perspective, Geomorphology, 318, 26–57,
https://doi.org/10.1016/j geomorph.2018.05.019, 2018.

Costard, F., Forget, F., Mangold, N., and Peulvast, J. P.: Formation of recent Martian debris flows by melting of near-surface ground ice at high obliquity, Science, 295, 110–113, https://doi.org/10.1126/science.1066 https://doi.org/10.1126/science.1066698, 2002.

De Haas, T., Ventra, D., Hauber, E., Conway, S. J., and Klein-
hans, M. G.: Sedimentological analyses of Martian gullies:
the subsurface as the key to the surface, Icarus, 258, 92–108,
https://doi.org/10.1016/j.icarus.2015.06.017, 2015a.

De Haas, T., Kleinhans, M. G., Carbonneau, P. E., Rubens-
dotter, L., and Hauber, E.: Surface morphology of fans
in the high-Arctic periglacial environment of Svalbard:
Controls and processes, Earth-Sci. Rev., 146, 163–182,
https://doi.org/10.1016/j.earscirev.2015.04.004, 2015b.

De Haas, T., Conway, S. J., Butcher, F. E. G., Levy, J. S.,
Grindrod, P. M., Balme, M. R., Goudge, T. A.: Time will
tell: temporal evolution of Martian gullies and paleoclimatic
implications, Geol. Soc. Lond. Spec. Publ., 467, 165–186,
https://doi.org/10.1144/SP467.1, 2019a.

De Haas, T., McArdell, B. W., Conway, S. J., McElwaine,
J. N., Kleinhans, M. G., Salese, F., and Grindrod, P. M.:
Initiation and flow conditions of contemporary flows in
Martian gullies, J. Geophys. Res.-Planet., 124, 2246–2271,
https://doi.org/10.1029/2018JE005899, 2019b.

de Scally, F. A. and Owens, I. F.: Morphometric con-
trols and geomorphic responses on fans in the Southern
Alps, New Zealand, Earth Surf. Proc. Land., 29, 311–322,
https://doi.org/10.1002/esp.1022, 2004.

de Scally, F. A., Owens, I. F., Louis, J.: Controls on fan
depositional processes in the schist ranges of the South-
ern Alps, New Zealand, and implications for debris-
flow hazard assessment, Geomorphology, 122, 99–116,
https://doi.org/10.1016/j geomorph.2010.06.002, 2010.

Dickson, J. L. and Head, J. W.: The formation and evolu-
tion of youthful gullies on Mars: gullies as the latestage
phase of Mars most recent ice age, Icarus, 204, 63–86,
https://doi.org/10.1016/j.icarus.2009.06.018, 2009.

Dickson, J. L., Head, J. W., Kreslavsky, M.: Martian gullies in the southern midlatitudes of Mars: Evidence for climate-controlled formation of young fluvial features based upon local and global topography, Icarus, 188, 315–323, https://doi.org/10.1016/j.icarus.2006.11.020, 2007.

Dickson, J. L., Head, J. W., and Fassett, C. I.: Patterns of accumulation and flow of ice in the mid-latitudes of Mars during the Amazonian, Icarus, 219, 723–732, https://doi.org/10.1016/j.icarus.2012.03.010, 2012.

Dickson, J. L., Head, J. W., Goudge, T. A., and Barbieri, L.: Re-
cent climate cycles on Mars: Stratigraphic relationships between
multiple generations of gullies and the latitude dependent mantle,
Icarus, 252, 83–94, https://doi.org/10.1016/j.icarus.2014.12.035,
2015.

Dundas, C. M., Diniega, S., Hansen, C. J., Byrne, S., McEwen, A. S.: Seasonal activity and morphological changes in martian gullies, Icarus, 220, 124–143, https://doi.org/10.1016/j.icarus.2012.04.005, 2012.

Dundas, C. M., Diniega, S., McEwen, A. S.: Long-
term monitoring of Martian gully formation and evo-
lution with MRO/HiRISE, Icarus, 251, 244–263,
https://doi.org/10.1016/j.icarus.2014.05.013, 2015.

Dundas, C. M., McEwen, A. S., Diniega, S., Hansen, C. J.,
Byrne, S., and McElwaine, J. N.: The formation of gullies
on Mars today, Geol. Soc. Lond. Spec. Publ. 467, 67–94,
https://doi.org/10.1144/SP46, 2019.

Ewertowski, M. W. and Tomczyk, A. M.: Quantifica-
tion of the ice-cored moraines’ short-term dynamics in
the high-Arctic glaciers Ebbabreen and Ragnarbreen,
Petuniabukta, Svalbard, Geomorphology, 234, 211–227,
https://doi.org/10.1016/j geomorph.2015.01.023, 2015.

Hargitai, H.: Viscous Flow Features (Mars), in: Encyclo-
pedia of Planetary Landforms, Springer, New York, NY,
https://doi.org/10.1007/978-1-4614-9213-9_596-1, 2014.

Harrison, T. N., Osinski, G. R., Tornabene, L. L., Jones, E.: Global documentation of gullies with the Mars reconnaissance orbiter context camera and implications for their formation, Icarus, 252, 236–254, https://doi.org/10.1016/j.icarus.2015.01.022, 2015.

Hartley, A. J., Mather, A. E., Jolley, E., Turner, P.: Climatic controls on alluvial-fan activity, Coastal Cordillera, north- ern Chile, in: Alluvial Fans: Geomorphology, Sedimentol- ogy, Dynamics, edited by: Harvey, A. M., Mather, A. E., and Stokes, M., Geol. Soc. Lond. Spec. Publ. 251, 95–115, https://doi.org/10.1144/GSL.SP.2005.251.01.08, 2005.

Head, J. W., Mustard, J. F., Kreslavsky, M. A., Milliken, R. E., and Marchant, D. R.: Recent ice ages on Mars, Nature, 426, 797–802, https://doi.org/10.1038/nature02114, 2003.

Head, J. W., Marchant, D. R., Dickson, J. L., Kress, A. M., and Baker, D. M.: Northern midlatitude glaciation in the Late Amazonian period of Mars: criteria for the recognition of debris-covered glacier and valley glacier landsystem deposits, Earth Planet. Sc. Lett., 294, 306–320, https://doi.org/10.1016/j.epsl.2009.06.041, 2010.

Heldmann, J. L. and Mellon, M. T.: Observations of Martian gullies and constraints on potential formation mechanisms, Icarus, 168, 285–304, https://doi.org/10.1016/j.icarus.2003.11.024, 2004.

Heldmann, J. L., Toon, O. B., Pollard, W. H., Mellon, M. T., Pitlick, J., McKay, C. P., and Andersen, D. T.: Formation of Martian gullies by the action of liquid water flowing under current Martian environmental conditions, J. Geophys. Res.-Planets, 110, E05004, https://doi.org/10.1029/2004JE002261, 2005.

Hobbs, S. W., Paull, D. J., and Clarke, J. D. A.: Analysis of regional gullies within Noachis Terra, Mars: A complex relationship between slope, surface material and aspect, Icarus, 250, 308–331, https://doi.org/10.1016/j.icarus.2014.12.011, 2015.

Holt, J. W., Safaeinili, A., Plaut, J. J., Head, J. W., Phillips, R. J., Seu, R., Kempf, S. D., Choudhary, P., Young, D. A., Putzig, N. E., and Biccari, D.: Radar sounding evidence for buried glaciers
in the southern mid-latitudes of Mars, Science, 322, 1235–1238,
https://doi.org/10.1126/science.1164246, 2008.

Horton, R. E.: Drainage-basin characteristics, Trans. Am. Geophys.
Union, 13, 350–361, https://doi.org/10.1029/TR013i001p00350,
1932.

Hubbard, B., Milliken, R. E., Kargel, J. S., Limaye, A., and Souness, C.: Geomorphological characterisation and interpretation of a mid-latitude glacier-like form: Hellas Planitia, Mars, Icarus, 211, 330–346, https://doi.org/10.1016/j.icarus.2010.10.021, 2011.

Ilinca, V.: Using morphometrics to distinguish between debris flow, debris flood and flood (Southern Carpathians, Romania), Catena, 197, 104982, https://doi.org/10.1016/j.catena.2020.104982, 2021.

Jackson, L. E., Kostaschuk, R. A., and MacDonald, G. M.: Identifcation of debris flow hazard on alluvial fans in the Canaan Rocky Mountains, in: Debris flows/avalanches: process, recognition, and mitigation, edited by: Costa, J. E. and Wieczorek, G. F., Rev. Eng. Geol. vol. VII., Geol. Soc. Am., https://doi.org/10.1130/REG7-p115, 1987.

Johnsson, A., Reiss, D., Hauber, E., Hiesinger, H., and Zanetti, M.: Evidence for very recent melt-water and debris flow activity in gullies in a young mid-latitude crater on Mars, Icarus, 235, 37–54, https://doi.org/10.1016/j.icarus.2014.03.005, 2014.

Kirk, R. L., Howington-Kraus, E., Rosiek, M. R., Anderson, J. A., Archinal, B. A., Becker, K. J., Cook, D. A., Galuszka, D. M., Geissler, P. E., Hare, T. M., Holmberg, I. M., Keszthelyi, L. P., Redding, B. L., Delamere, W. A., Gallagher, D., Chapel, J. D., Eliason, E. M., King, R., and McEwen, A. S.: Ultrahigh resolution topographic mapping of Mars with MRO HiRISE stereo images: meter-scale slopes of candidate Phoenix landing sites, J. Geophys. Res.-Planet., 113, E00A24, https://doi.org/10.1029/2007JE003000, 2008.

Kneissl, T., Reiss, D., Van Gasselt, S., and Neukum, G.: Distribution and orientation of northern-hemisphere gullies on Mars from the evaluation of HRSC and MOC-NA data, Earth Planet. Sc. Lett., 294, 357–367, https://doi.org/10.1016/j.epsl.2009.05.018, 2010.

Kostaschuk, R. A., MacDonald, G. M., and Putnam, P. E.: Depositional process and alluvial fan-drainage basin morphometric relationships near Banff, Alberta, Canada, Earth Surf. Proc. Land., 11, 471–484, https://doi.org/10.1002/esp.3290110502, 1986.

Kreslavsky, M. A. and Head III, J. W.: Kilometer-scale roughness of Mars: Results from MOLA data analysis, J. Geophys. Res.-Planets, 105, 26695–26711, https://doi.org/10.1029/2000JE001259, 2000.

Kreslavsky, M. A. and Head, J. W.: Mars: nature and evolution of
young latitudedependent water-ice-rich mantle, Geophys. Res.
Lett., 29, 1419, https://doi.org/10.1029/2002GL015392, 2002.

Langbein, W. B.: Profiles of rivers of uniform discharge, U.S. Geol. Surv. Prof. Pap., 501-B, U.S. Geological Survey, 119–122, https://doi.org/10.1086/627653, 1964.

Levy, J. S., Head, J., and Marchant, D.: Thermal contraction crack polygons on Mars: classification, distribution, and climate implications from HiRISE observations, J. Geophys. Res.-Planet., 114, 01007, https://doi.org/10.1029/2008JE003273, 2009a.

Levy, J. S., Head, J. W., Marchant, D. R., Dickson, J. L., and Morgan, G. A.: Geologically recent gully-polygon relationships on Mars: Insights from the Antarctic Dry Valleys on the roles of permafrost, microclimates, and

water sources for surface flow, Icarus, 201, 113–126,
https://doi.org/10.1016/j.icarus.2008.12.043, 2009b.

Levy, J. S., Head, J. W., Dickson, J. L., Fassett, C. I., Morgan, G. A., and Schon, S. C.: Identification of gully debris flow deposits in Protonilus Mensae, Mars: Characterization of a water-bearing, energetic gully-forming process, Earth Planet. Sc. Lett., 294, 368–377, https://doi.org/10.1016/j.epsl.2009.08.002, 2010.

Levy, J. S., Head, J. W., Marchant, D. R.: Gullies, polygons and mantles in Martian permafrost environments: cold desert landforms and sedimentary processes during recent Martian geological history, Geol. Soc. Lond. Spec. Publ., 354, 167–182, https://doi.org/10.1144/SP354.10, 2011.

Malin, M. C. and Edgett, K. S.: Evidence for recent groundwater seepage and surface runoff on Mars, Science, 288, 2330–2335, https://doi.org/10.1126/science.288.5475.2330, 2000.

McEwen, A. S., Eliason, E. M., Bergstrom, J. W., Bridges, N. T., Hansen, C. J., Delamere, W. A., Grant, J. A., Gulick, V. C., Herkenhoff, K. E., Keszthelyi, L., Kirk, R. L., Mellon, M. T., Squyres, S. W., Thomas, N., and Weitz, C. M.: Mars reconnaissance orbiter's high resolution imaging science experiment (HiRISE), J. Geophys. Res.-Planets, 112, E05S02, https://doi.org/10.1029/2005JE002605, 2007.

McLachlan, G. J.: Discriminant analysis and statistical pattern recognition, John Wiley and Sons, ISBN 0-471-69115-1, 2005.

Mellon, M. T., Jakosky, B. M., Kieffer, H. H., and Christensen, P. R.: High-resolution thermal inertia mapping from the Mars global surveyor thermal emission spectrometer, Icarus, 148, 437–455, https://doi.org/10.1006/icar.2000.6503, 2000.

Melton, M. A.: An analysis of the relations among elements of climate, surface properties, and geomorphology, in: Vol. 11, Department of Geology, Columbia University, New York, https://doi.org/10.7916/d8-0rmg-j112, 1957.

Miller, V. C.: A quantitative geomorphic study of drainage basin characteristics in the Clinch Mountain area, Virginia and Tennessee, in: Vol. 3, Columbia University, New York, https://doi.org/10.1086/626413, 1953.

Milliken, R. E., Mustard, J. F., and Goldsby, D. L.: Viscous flow features on the surface of Mars: observations from high-resolution Mars Orbiter Camera (MOC) images, J. Geophys. Res., 108, 5057, https://doi.org/10.1029/2002JE002005, 2003.

Mustard, J. F., Cooper, C. D., and Rifkin, M. K.: Evidence for recent climate change on Mars from the identification of youthful near-surface ground ice, Nature, 412, 411–414, https://doi.org/10.1038/35086515, 2001.

Petersen, E. I., Holt, J. W., and Levy, J. S.: High ice purity of Martian lobate debris aprons at the regional scale: evidence from an orbital radar sounding survey in Deuteronilus and Protonilus Mensae, Geophys. Res. Lett., 45, 11595–11604, https://doi.org/10.1029/2018GL079759, 2018.

Phillips, J. D. and Lutz, J. D.: Profile convexities in bedrock and alluvial streams, Geomorphology, 102, 554–566, https://doi.org/10.1016/j geomorph.2008.05.042, 2008.

Pilorget, C. and Forget, F.: Formation of gullies on Mars by debris flows triggered by CO₂ sublimation, Nat. Geosci., 9, 65–69, https://doi.org/10.1038/ngeo2619, 2016.

Plaut, J. J., Safaeinili, A., Holt, J. W., Phillips, R. J., Head III, J. W., Seu, R., Putzig, N. E., and Frigeri, A.: Radar evidence for ice in lobate debris aprons in the mid-
northern latitudes of Mars, Geophys. Res. Lett., 36, L02203,
https://doi.org/10.1029/2008GL036379, 2009.

Putzig, N. E., Mellon, M. T., Kretke, K. A., and Arvid-
son, R. E.: Global thermal inertia and surface properties of
Mars from the MGS mapping mission, Icarus, 173, 325–341,
https://doi.org/10.1016/j.icarus.2004.08.017, 2005.

Reiss, D., Van Gasselt, S., Neukum, G., and Jaumann, R.: Absolute dune ages and implications for the time of formation of gullies in Nirgal Vallis, Mars, J. Geophys. Res.-Planets, 109, E06007, https://doi.org/10.1029/2004JE002251, 2004.

Reiss, D., Hauber, E., Hiesinger, H., Jaumann, R., Trauthan, F., Preusker, F., Zanetti, M., Ulrich, M., Johnsson, A., Johansson, L., Olvmo, M., Carlsson, E., Johansson, H. A. B., and McDaniel, S.: Terrestrial gullies and debris-flow tracks on Svalbard as planetary analogs for Mars, in: Analogs for Planetary Exploration, edited by: Garry, W. B. and Bleacher, J. E., Geol. Soc. Am. Spec. Pap. 483, Geol. Soc. Am., 165–175, https://doi.org/10.1130/2011.2483(11), 2011.

Ryder, J.: Some aspects of the morphometry of paraglacial allu-
vial fans in South-central British Columbia, Can. J. Earth Sci., 8,
1252–1264, https://doi.org/10.1139/e71-114, 1971.

Schon, S. C., Head, J. W., and Fassett, C. I.: Unique chronostrati-
graphic marker in depositional fan stratigraphy on Mars: Evi-
dence for ca. 1.25 Ma gully activity and surficial meltwater ori-
gin, Geology, 37, 207–210, https://doi.org/10.1130/g25398a.1,
2009.

Schumm, S. A.: Evolution of drainage systems and slopes in badlands at Perth Amboy, New Jersey, Geol. Sco. Am. Bull., 67, 597–646, https://doi.org/10.1130/0016-7606(1956)67[597:EODSAS]2.0.CO;2, 1956.

Sharp, R. P.: Mars: Fretted and chaotic terrains, J. Geophys. Res., 78, 4073–4083, https://doi.org/10.1029/JB078i020p04073, 1973.

Siewert, M. B., Krautblatter, M., Christiansen, H. H., and Eck-
erstorfer, M.: Arctic rockwall retreat rates estimated using
laboratory-calibrated ERT measurements of talus cones in
Longyeardalen, Svalbard, Earth Surf. Proc. Land., 37, 1542–
1555, https://doi.org/10.1002/esp.3297, 2012.

Sinha, R., Ray, D., De Haas, T., Conway, S. J., and No-
blet, A.: Self generated DEMs, figshare [data set],
https://doi.org/10.6084/m9 figshare.21717164.v1, 2022a.

Sinha, R., Ray, D., De Haas, T., Conway, S. J., and No-
blet, A.: Measurement data of gully systems in the
southern mid latitudes of Mars, figshare [data set],
https://doi.org/10.6084/m9 figshare.21717182.v1, 2022b.

Sinha, R. K. and Vijayan, S.: Geomorphic investigation of craters in Alba Mons, Mars: implications for Late Amazonian glacial activity in the region, Planet. Space Sci., 144, 32–48, https://doi.org/10.1016/j.pss.2017.05.014, 2017.

Sinha, R. K., Vijayan, S., Shukla, A. D., Das, P., and Bhattacharya, F.: Gullies and debris-flows in Ladakh Himalaya, India: a potential Martian analogue, Geol. Soc. Lond. Spec. Publ., 467, 315–342, https://doi.org/10.1144/SP46, 2019.

Sinha, R. K., Ray, D., De Haas, T., and Conway, S. J.: Global documentation of overlapping lobate deposits in Martian gullies, Icarus, 352, 113979, https://doi.org/10.1016/j.icarus.2020.113979, 2020.

Squyres, S. W.: Martian fretted terrain: Flow of erosional debris, Icarus, 34, 600–613, https://doi.org/10.1016/0019-1035(78)90048-9, 1978.

Squyres, S. W.: The distribution of lobate debris aprons and sim-
ilar flows on Mars, J. Geophys. Res.-Solid, 84, 8087–8096,
https://doi.org/10.1029/JB084iB14p08087, 1979.

Squyres, S. W. and Carr, M. H.: Geomorphic evidence for the distribution of ground ice on Mars, Science, 231, 249–252, https://doi.org/10.1126/science.231.4735.249, 1986.

Stolle, A., Langer, M., Blöthe, J. H., and Korup, O.: On predicting debris flows in arid mountain belts, Global Planet. Change, 126, 1–13, https://doi.org/10.1016/j.gloplacha.2014.12.005, 2015.

Tomczyk, A. M.: Morphometry and morphology of fan-
shaped landforms in the high-Arctic settings of cen-
tral Spitsbergen, Svalbard, Geomorphology, 392, 107899,
https://doi.org/10.1016/j geomorph.2021.107899, 2021.

Wilford, D. J., Sakals, M. E., Innes, J. L., Sidle, R. C., and Bergerud, W. A.: Recognition of debris flow, debris flood and flood hazard through watershed morphometrics, Landslides, 1, 61–66, https://doi.org/10.1007/s10346-003-0002-0, 2004.

Yue, Z., Hu, W., Liu, B., Liu, Y., Sun, X., Zhao, Q., and Di, K.: Quantitative analysis of the morphology of martian gullies and insights into their formation, Icarus, 243, 208–221, https://doi.org/10.1016/j.icarus.2014.08.028, 2014.