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The precipitation of freshwater carbonates (tufa) along karstic rivers is enhanced by degassing of CO 2 downstream of karstic springs. However, in most karstic springs CO 2 degassing is not enough to force the precipitation of tufa sediments. Little is known about the role of dissolution of gypsum or dolomite in the hydrochemistry of these systems and how this affects the formation of tufa deposits. Here we present a monitoring study conducted over a year in Trabaque River (Spain). The river has typical karst hydrological dynamics with water sinking upstream and re-emerging downstream of the canyon. Mixing of calciumThis article is protected by copyright. All rights reserved. Tufa in Trabaque Canyon precipitates from overflow springs during high water levels. Location of the overflow springs along the canyon depends on amount of precipitation. Mixing of bicarbonate and sulphate waters caused enhanced carbonate dissolution. Incongruent dissolution of dolomite limits the precipitation of tufa sediments. Laminated tufa precipitates discontinuously and is not necessarily annual in nature.

The controls that affect the structure and timing of terminations are still poorly understood. We studied a tufa deposit from the Iberian Peninsula that covers Termination II (T-II) and whose chronology was synchronized to speleothem records. We used the same chronology to synchronize ocean sediments from the North Atlantic to correlate major climate events in a common timescale. We identify two stages within T-II. The first stage started with the increase of boreal summer integrated solar insolation, and during this stage three millennial climate oscillations were recorded. These oscillations resulted from complex ocean–atmosphere interactions in the Nordic seas, caused by the progressive decay of Northern Hemisphere ice-sheets. The second stage commenced after a glacial outburst that caused the collapse of the Thermohaline Circulation, a massive Heinrich event, and the onset of the Bipolar Seesaw Mechanism (BSM) that eventually permitted the completion of T-II. The pace of the millennial oscillations during the first stage of T-II controlled the onset of the second stage, when the termination became a non-reversible and global phenomenon that accelerated the deglaciation. During the last the two terminations, the BSM was triggered by different detailed climate interactions, which suggests the occurrence of different modes of terminations.