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Hydrothermal Source of Radiogenic Sr to Himalayan Rivers

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Hydrothermal Source of Radiogenic Sr to Himalayan Rivers Hydrothermal source of radiogenic Sr to Himalayan rivers Matthew J. Evans Department of Geological Sciences, Cornell University, Ithaca, New York 14853-1504, USA Louis A. Derry Suzanne P. Anderson Department of Earth Sciences, University of California, Santa Cruz, California 95064, USA Christian France-Lanord Centre des Recherches PeÂtrographiques et GeÂochimiques, BP 20, Vandouvre-les-Nancy, 54501, France ABSTRACT ment; formations III and II of the crystallines Hot-spring waters near the Main Central thrust in the Marsyandi River of central Nepal are composed of calcic gneisses and marbles have Sr concentrations to 115 mM with 87Sr/86Sr to 0.77. Small amounts of hydrothermal as well as pelitic augen gneisses, and forma- water (#1% of total river discharge) have a signi®cant impact on the solute chemistry tion I contains mainly quartzo-pelitic gneisses and the budget of radiogenic Sr in the Marsyandi. In the upper Marsyandi, river chem- and some migmatites. The Manaslu leuco- istry re¯ects carbonate weathering, with 87Sr/86Sr # 0.72. As the Marsyandi ¯ows across granite is exposed in the northeastern part of the dominantly silicate High Himalayan Crystalline terrane, both 87Sr/86Sr and [Sr] in- the drainage. Variably metamorphosed Pre- crease, associated with increases in the concentration of Na1,K1, and Cl2, all of which cambrian sedimentary rocks make up the are high in the hydrothermal waters. Cation concentrations decrease along the Lesser Lesser Himalaya, pelitic schists and minor do- 13 Himalayan reach of the river. Hot-spring dissolved CO2 has a d C value to 15.9½, lomitic carbonates in the upper formation and indicating that metamorphic decarbonation reactions contribute CO2 to the ¯uids. Hy- quartzites and schists in the lower formation. drothermal CO2 is partially neutralized in high-temperature weathering reactions, which Numerous springs are found along the Mar- generate alkalinity and yield abundant radiogenic Sr. Radiogenic hydrothermal carbonate syandi, particularly near the Main Central can form from these solutions and later weather, releasing silicate Sr but imparting car- thrust and the South Tibetan detachment. bonate characteristics to the overall water chemistry. SAMPLING AND ANALYTICAL Keywords: hot spring, alkalinity, Himalaya, strontium, geothermal system. METHODS Main stem, tributary, and spring samples INTRODUCTION Crystalline series, the Main Central thrust, and were collected in April 1997 and April 1999. The Sr ¯ux from Himalayan rivers is an im- the Lesser Himalaya sequence (Colchen et al., All water samples were ®ltered and stored in portant contributor to the Sr isotope mass bal- 1980; Upreti, 1999). The Tethyan Sedimenta- acid-washed polyethylene bottles. Cation sam- ance of the modern oceans, and Himalayan ry Series comprises a Cambrian to early Ter- ples were acidi®ed with concentrated HNO3 rivers are unusual among world rivers in that tiary stable platform sequence dominated by in the ®eld. Cations were determined by in- they have both high concentrations of Sr and shelf carbonates. The High Himalayan Crys- ductively coupled plasma±mass spectrometry high 87Sr/86Sr (Edmond, 1992). Weathering of talline series is high-grade metamorphic base- or emission spectrometry (Cornell University various silicate phases and weathering of ra- diogenic carbonates have been proposed as sources for the radiogenic Sr ¯ux in Himala- yan rivers (Palmer and Edmond, 1989; Krish- naswami et al., 1992; Derry and France- Lanord, 1996; Quade et al., 1997; Singh et al., 1998; Blum et al., 1998; Galy et al., 1999; English et al., 2000). Each of these sources has different implications for the interpretation of the marine Sr record. We have determined solute chemistry for the main stem, all major tributaries, and both hot and cold springs of the Marsyandi River in central Nepal. We ®nd that hot springs contribute signi®cant amounts of radiogenic Sr and other ions to the Mar- syandi River. GEOLOGIC SETTING The Marsyandi River ¯ows over ;150 km from its headwaters north of the Annapurna range to its con¯uence with the Trisuli River, and has a basin area of ;4800 km2 (Fig. 1). This major tributary to the Ganges River crosses the main tectonostratigraphic units that make up the Nepal Himalaya, and the shear zones that bound them. The Marsyandi Figure 1. Tectonic sketch map of Marsyandi basin, central Nepal. TSSÐTethyan Sed- imentary series; STDSÐSouth Tibetan detachment system; HHCÐHigh Himalayan ¯ows across the Tethyan Sedimentary Series, Crystalline series; MCTÐMain Central thrust; LHÐLesser Himalaya. Sampling loca- the South Tibetan detachment system, forma- tions are marked. Symbols and shading continue in following ®gures. Representative tions III, II, and I of the High Himalayan 87Sr/86Sr values for bedrock are indicated. Fm is formation. q 2001 Geological Society of America. For permission to copy, contact Copyright Clearance Center at www.copyright.com or (978) 750-8400. Geology; September 2001; v. 29; no. 9; p. 803±806; 4 ®gures; Data Repository item 2001091. 803 Figure 2. Marsyandi main stem, tributary, and spring chemistry. Concentrations in micromoles/kg (mM). Note scale break on all vertical axes to accom- modate high concentra- tions in hot-spring waters. Shading corresponds to map units in Figure 1 and symbols follow its key. Downstream distance measured from Khangsar Khola. K, Na, and Cl are particularly anomalous in hot springs and clearly af- fect main-stem chemistry down to its con¯uence with Trisuli River. and University of California, Santa Cruz), and 54 thermal ionization mass spectrometer increase occurs within the High Himalayan anions were determined by ion chromatogra- (Cornell). Spring waters and some river wa- Crystallines, concurrent with the increase in phy (Cornell and Centre des Recherches PeÂ- ters were spiked with an enriched 84Sr tracer [Sr]. Each of the lithologic units in the Mar- trographiques et GeÂochimiques [CRPG]). Sr and [Sr] was determined by isotope dilution. syandi basin has distinct Sr characteristics that isotope ratios were analyzed on a VG Sector Separate samples were reacted under vacu- are re¯ected in tributary streams from mon- um with H3PO4, and the evolved CO2 was olithologic catchments. Tethyan tributaries measured for determination of d13Cona have high Sr concentrations (;4.5 mM) and modi®ed VG 602D mass spectrometer. The low 87Sr/86Sr, near 0.72. Tributaries from for- 18 87 86 d O and dD values from H2O were deter- mations II and III have similar Sr/ Sr at mined for six spring samples by CO2 equil- 0.721, but much lower [Sr] (;0.6 mM). For- ibration and reduction over hot uranium, re- mations II and III contain abundant marbles, spectively (CRPG). and as in the Tethyan reach, these carbonates strongly control the riverine Sr in both the RESULTS AND DISCUSSION main stem and tributaries. Formation I tribu- Main Stem and Tributary Chemistry taries are radiogenic (87Sr/86Sr 5 0.744) with Within the Tethyan series Ca, Mg, and Sr dilute [Sr] (ø0.5mM). Lesser Himalayan concentrations1 are high in both the tributaries streams have [Sr] of only ;0.3 mM but very and main stem, re¯ecting carbonate weather- high 87Sr/86Sr ratios (to 0.87). ing (Figs. 2 and 3). Within the High Himala- yan Crystalline and Lesser Himalaya series Spring Chemistry these ions show overall decreases in concen- Five hot (;30±55 8C) springs and two cold tration, except for main-stem [Sr], which in- springs along the Marsyandi were sampled. creases in formation I. Levels of K, Na, and Hot springs are Cl rich (Fig. 2) with total dis- Cl in the Marsyandi and its tributaries are rel- solved solid (TDS) values of 800±7000 mg/ atively low upstream of the South Tibetan de- L. Cold springs have higher Ca/Na and Ca/Cl tachment, but increase two to tenfold overall ratios but are much more dilute (TDS ø 300± within the High Himalayan Crystallines. [Na], 600 mg/L) and closely resemble nearby trib- [Cl], and [K] in Lesser Himalayan tributaries utaries. Sr in the hot springs is consistently are mostly relatively dilute. Measured and cal- more radiogenic and concentrated than in both culated alkalinities are similar and range from the main stem and tributary values at the same ø1500 to 1800 mM for the main stem; the position along the Marsyandi; the hot springs highest values are in the Tethyan series. de®ne a Sr source distinct from the tributaries, The 87Sr/86Sr values for the main stem of with 87Sr/86Sr ranging from 0.736 to 0.768 Figure 3. A: Sr concentrations in waters. the Marsyandi increase downstream from Note vertical axis break for hot-spring sam- and [Sr] from 15 to 115 mM (Fig. 3). The two ples. Numbers give d13C (in per mil) of dis- 0.719 to 0.733 (Fig. 3) and the majority of this cold springs sampled near the South Tibetan 87 solved CO2 in hot-spring samples. B: Isoto- detachment are much less radiogenic ( Sr/ pic ratio of dissolved Sr, symbols as in 1GSA Data Repository item 2001091, Water 86Sr 5 0.712) and concentrated ([Sr] 5 6±3 Figure 1. Compared to tributaries, hot chemistry data, is available on request from Docu- springs in formation I of High Himalayan ments Secretary, GSA, P.O. Box 9140, Boulder, CO mM) than their warmer counterparts and re- 13 Crystallines have ;100 times more Sr, and 80301-9140, [email protected], or at www. semble Tethyan tributaries. The d C of dis- are more radiogenic. geosociety.org/pubs/ft2001.htm. solved inorganic carbon in the sampled 804 GEOLOGY, September 2001 tion of hot-spring alkalinity that is derived from carbonate versus silicate sources. The fraction of hot-spring alkalinity present as Na* and K necessarily represents a minimum es- timate of the silicate-derived alkalinity ¯ux from the springs. The positive d13C values (10.48½ to 15.9½) in spring water CO2 imply that some of the dissolved CO2 (alkalinity) is derived from metamorphic decarbonation reactions (Shieh and Taylor, 1969; Friedman and O'Neil, 1977).
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