found a westward flow induced by the wind stress with velocities between 5 and 18 cm s 1 and a maximum transport in July–August (\citealp{Zavala_Hidalgo_2003}).
Lagrangian results presented here are in agreement with the ensemble-mean Lagrangian circulation sustained by the instantaneous HyCOM-GOM10.04 velocity from 1994 through 2014, depicted for example in figure 1 of \citet{Duran_2018}. In that figure, the ensemble-mean distribution of a passive tracer moves westward over the Yucatan shelf. The ensemble averaging is taken over a series of different initial conditions spanning 1994-2014. Blue tracer reaches the furthest towards the west at the location where cLCS deform as chevrons towards the west, and where the climatological attraction is weakest. This is in excellent agreement with the 2018 trajectory simulation presented here, where trajectories originating in the Yucatan shelf move across cLCS where the climatological strength of attraction is weakest and where they deform as chevrons towards the west (Fig. \ref{521863}). Thus, the existence of a predominant pathway connecting the eastern Yucatan shelf and the Bay of Campeche becomes clear. Different experiments supporting a persistent along-slope Lagrangian link between the Yucatan shelf and the Campeche shelf,  including the 2018 simulation presented here (Fig. \ref{581122}), the ensemble-mean tracer distribution from an instantaneous velocity spanning 1994 through 2014, and cLCS computed from a 1994-2014 climatological velocity \citep{Duran_2018}. Trajectories computed directly from the climatological velocity are also in good agreement with this pattern, although when initiated in the Campeche pool of cool water and integrated backward in time, trajectories move westward closer to the coast, where strongly-attracting cLCS align with the coastline, thus confirming the cLCS's strong attraction (Fig. \ref{521863}).