Stalagmite growth and palaeo-climate: the numerical perspective

Abstract The growth of stalagmites can be approximated by a simple mathematical model, which depends on growth rate and equilibrium radius. These two parameters are controlled by the climate. Temperature variations derived from ice and deep-sea core data, together with models for changes in precipitation and soil cover, are used to derive stalagmite stratigraphies, which reflect the palaeo-climate variations imposed. In general, stalagmite growth is strongly correlated to temperature and the amount of carbon dioxide available in the soil. Furthermore, precipitation is correlated to the stalagmite diameter. However, several assumptions need to be made: (i) A functional relationship between temperature on the one hand and precipitation and soil cover on the other needs to be established. (ii) The kinetics of calcite dissolution and precipitation needs to be assigned, either under soil and epikarst conditions open to the atmosphere or under fractured rock conditions closed from the atmosphere. These assumptions are difficult to access from field data, and therefore a stalagmite stratigraphy can be ambiguous and not easily converted back into an unknown palaeo-climate signal.

[1]  S. Ringer,et al.  Precipitation kinetics of calcite in the system CaCO3H2OC02: The conversion to CO2 by the slow process H++HCO3− → CO2+H2O as a rate limiting step , 1997 .

[2]  K. Mosegaard,et al.  Past temperatures directly from the greenland ice sheet , 1998, Science.

[3]  D. Schrag,et al.  Hydrological conditions over the western Mediterranean basin during the deposition of the cold Sapropel 6 (ca. 175 kyr BP) , 2002 .

[4]  Walter H. F. Smith,et al.  New, improved version of generic mapping tools released , 1998 .

[5]  R. Curl.  Minimum Diameter Stalactites , 1972 .

[6]  N. Shackleton.  Oxygen isotopes, ice volume and sea level , 1987 .

[7]  J. Jouzel,et al.  Evidence for general instability of past climate from a 250-kyr ice-core record , 1993, Nature.

[8]  J. Jouzel,et al.  Extending the Vostok ice-core record of palaeoclimate to the penultimate glacial period , 1993, Nature.

[9]  K. Briffa,et al.  Seasonal temperatures in Britain during the past 22,000 years, reconstructed using beetle remains , 1987, Nature.

[10]  Wolfgang Dreybrodt,et al.  Chemical kinetics, speleothem growth and climate , 1999 .

[11]  W. Dreybrodt.  The kinetics of calcite precipitation from thin films of calcareous solutions and the growth of speleothems: Revisited , 1981 .

[12]  David L. Parkhurst,et al.  The kinetics of calcite dissolution in CO 2 -water systems at 5 degrees to 60 degrees C and 0.0 to 1.0 atm CO 2 , 1978 .

[13]  Walter H. F. Smith,et al.  Free software helps map and display data , 1991 .

[14]  P. J. Thompson,et al.  Late Pleistocene Paleoclimates of North America as Inferred from Stable Isotope Studies of Speleothems , 1978, Quaternary Research.

[15]  W. Dansgaard,et al.  Greenland palaeotemperatures derived from GRIP bore hole temperature and ice core isotope profiles , 1995 .

[16]  Andy Baker,et al.  Intra- and inter-annual growth rate of modern stalagmites , 2001 .

[17]  W. Dreybrodt.  Processes in Karst Systems , 1988 .

[18]  J. Jouzel,et al.  Climate and atmospheric history of the past 420,000 years from the Vostok ice core, Antarctica , 1999, Nature.

[19]  Andy Baker,et al.  Recent flowstone growth rates: Field measurements in comparison to theoretical predictions , 1995 .

[20]  Wolfgang Dreybrodt,et al.  Deposition of calcite from thin films of natural calcareous solutions and the growth of speleothems , 1980 .

[21]  L. N. Plummer,et al.  The solubilities of calcite, aragonite and vaterite in CO2-H2O solutions between 0 and 90°C, and an evaluation of the aqueous model for the system CaCO3-CO2-H2O , 1982 .

[22]  G. Wasserburg,et al.  The Eastern Mediterranean paleoclimate as a reflection of regional events: Soreq cave, Israel , 1999 .

[23]  S. Burns,et al.  Speleothem evidence from Oman for continental pluvial events during interglacial periods , 2001 .

[24]  E. Usdowski.  Reactions and Equilibria in the SystemsCO2-H2O andCaCO3—CO2—H2O (0°-50 °C) - A Review , 1982 .

[25]  S. Burns,et al.  Start of the last interglacial period at 135 ka: Evidence from a high Alpine speleothem , 2002 .

[26]  W. Dreybrodt,et al.  The kinetics of the reaction CO2 + H2O → H+ + HCO3− as one of the rate limiting steps for the dissolution of calcite in the system H2OCO2CaCO3 , 1996 .

[27]  N. Shackleton,et al.  The 100,000-year ice-Age cycle identified and found to lag temperature, carbon dioxide, and orbital eccentricity , 2000, Science.

[28]  T. Wigley,et al.  The effect of climate on the chemistry of carbonate groundwater , 1975 .

[29]  W. Barnes,et al.  Testing Theoretically Predicted Stalagmite Growth Rate with Recent Annually Laminated Samples: Implications for Past Stalagmite Deposition , 1998 .

[30]  A. Matter,et al.  Strong coherence between solar variability and the monsoon in Oman between 9 and 6 kyr ago , 2001, Nature.

[31]  J. Jouzel,et al.  Irregular glacial interstadials recorded in a new Greenland ice core , 1992, Nature.

[32]  B. Jones,et al.  WATEQ: A COMPUTER PROGRAM FOR CALCULATING CHEMICAL EQUILIBRIA OF NATURAL WATERS , 1973 .

[33]  W. Dreybrodt,et al.  The kinetics of calcite dissolution and precipitation in geologically relevant situations of karst areas: 2. Closed system☆ , 1985 .

[34]  N. Shackleton,et al.  Oxygen isotopes and sea level , 1986, Nature.

[35]  M. Bar-Matthews,et al.  Timing and hydrological conditions of Sapropel events in the Eastern Mediterranean, as evident from speleothems, Soreq cave, Israel , 2000 .