in coastal waters of the Humboldt Current, NE U.S. Shelf, Scotian and Newfoundland shelves, Benguela Current, East China and Yellow Seas, followed by polar regions of the East Bering and Okhotsk Seas, the Southern Ocean, enclosed bodies of water such as the Black Sea and the Mediterranean, and the west Pacific waters of the Japan seas and the Kuroshio Current. Large amounts of jelly carbon biomass that are reported from coastal areas of open shelves and semi-enclosed seas of North America, Europe, and East Asia come from coastal stranding data. Carbon export Large amounts of jelly carbon are quickly transferred to and remineralized on the seabed in coastal areas, including estuaries, lagoons and subtidal/intertidal zones, shelves and slopes, the deepsea. and even entire continental margins such as in the Mediterranean Sea. Jelly carbon transfer begins when gelatinous zooplankton die at a given "death depth" (exit depth), continues as biomass sinks through the water column, and terminates once biomass is remineralized during sinking or reaches the seabed, and then decays. Jelly carbon per se represents a transfer of "already exported" particles (below the mixed later, euphotic or mesopelagic zone), originated in primary production since gelatinous zooplankton "repackage" and integrate this carbon in their bodies, and after death transfer it to the ocean's interior. While sinking through the water column, jelly carbon is partially or totally remineralized as dissolved organic/inorganic carbon and nutrients (DOC, DIC, DON, DOP, DIN and DIP) and any left overs further experience microbial decomposition or are scavenged by macrofauna and megafauna once on the seabed. Despite the high lability of jelly‐C, a remarkably large amount of biomass arrives at the seabed below 1,000 m. During sinking, jelly‐C biochemical composition changes via shifts in C:N:P ratios as observed in experimental studies. Yet realistic jelly‐C transfer estimates at the global scale remain in their infancy, preventing a quantitative assessment of the contribution to the biological carbon soft‐tissue pump. Ocean carbon export is typically estimated from the flux of sinking particles that are either caught in sediment traps or quantified from videography, and subsequently modeled using sinking rates. Biogeochemical models are normally parameterized using particulate organic matter data (e.g., 0.5–1,000 μm marine snow and fecal pellets) that were derived from laboratory experiments or from sediment trap data. These models do not include jelly‐C (except larvaceans, not only because this carbon transport mechanism is considered transient/episodic and not usually observed, and mass