A comparative analysis of bedform fields along the submarine flanks of insular volcanoes, characterized by different morpho‐structural settings, volcanic and meteo‐marine regimes (Vanuatu, Kermadec, Bismark, Madeira and Aeolian archipelagos), is presented here to provide insights on the size distribution, morpho‐dynamic and genesis of such bedforms. Two main types of bedforms are recognized according to their size, location and preconditioning/triggering processes. Small‐scale bedforms have wavelengths of tens to hundreds of metres and wave heights of metres. Because of their small‐size, they are typically not recognizable at water depths greater than 400 m from vessel‐mounted bathymetric surveys. However, few examples of small‐scale bedforms are reported from upper volcanic flanks, where steep gradients commonly hinder their formation. Their recognition is mostly limited to the thalweg of shallow and flat‐bottomed channels that carve the insular shelf on slope gradients <15°. Small‐scale bedforms are mostly related to erosional–depositional processes due to sedimentary gravity flows that are often the result of a cascading effect between volcanic and non‐volcanic processes (for example, flood discharges and retrogressive landslides). Large‐scale bedforms occur at all water depths, having wavelengths of hundreds/thousands of metres and wave heights up to few hundreds of metres. The origin of large bedforms is more difficult to ascertain, especially if only bathymetric data are available. Some diagnostic criteria are presented to distinguish between bedforms associated with landslide deposits and those associated with density currents. In this latter case, relevant sediment sources and slope gradients (<8°) are key factors for bedform development. Erosional–depositional bedforms are typically related to eruption‐fed density flows formed during large caldera collapses or to large turbidity flows. Bedforms generated by turbidity flows are often observed in the lower volcanic flanks, where an abrupt decrease of gradients is present, often matching a change from confined to unconfined settings. In summary, this study provides insights to interpret bedforms in modern and ancient marine volcaniclastic settings elsewhere.

中文翻译：

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岛屿火山海底侧翼的床型：从高分辨率海底调查中获得的新见解

此处介绍了对岛屿火山海底侧翼的床型场的比较分析，其特征在于不同的形态结构设置、火山和海洋海洋制度（瓦努阿图、克马德克、俾斯麦、马德拉和伊奥利亚群岛），以提供有关大小的见解这种床型的分布、形态动力学和成因。根据其大小、位置和预处理/触发过程，可识别两种主要类型的床型。小尺度海床的波长为数十至数百米，波高为数米。由于它们的体积小，在超过 400 m 的水深下，通常无法通过安装在船上的测深测量来识别它们。然而，在火山上部侧翼很少报道小规模床型的例子，那里陡峭的梯度通常阻碍了它们的形成。他们的识别主要限于浅平底渠道的thalweg，这些渠道在坡度<15°的坡度上雕刻岛架。由于沉积重力流，小规模的床型主要与侵蚀沉积过程有关，而沉积重力流通常是火山和非火山过程（例如，洪水排放和后退滑坡）之间的级联效应的结果。大规模的床形出现在所有水深，波长可达数百/数千米，波高可达数百米。大型床型的起源更难确定，尤其是在只有测深数据可用的情况下。提出了一些诊断标准来区分与滑坡沉积物相关的床型和与密度流相关的床型。在后一种情况下，相关的沉积物来源和坡度（<8°）是底床发育的关键因素。侵蚀沉积床型通常与大火山口坍塌期间形成的喷发密度流或大浊度流有关。在较低的火山侧翼经常观察到由浊流产生的床形，那里梯度突然下降，通常与从受限环境到非受限环境的变化相匹配。总之，这项研究为解释其他地方现代和古代海相火山碎屑环境中的床形态提供了见解。在较低的火山侧翼经常观察到由浊流产生的床形，那里梯度突然下降，通常与从受限环境到非受限环境的变化相匹配。总之，这项研究为解释其他地方现代和古代海相火山碎屑环境中的床形态提供了见解。在较低的火山侧翼经常观察到由浊流产生的床形，那里梯度突然下降，通常与从受限环境到非受限环境的变化相匹配。总之，这项研究为解释其他地方现代和古代海相火山碎屑环境中的床形态提供了见解。