Quaternary International xxx (2018) 1e6
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High-resolution mid-Holocene Indian Summer Monsoon recorded in a stalagmite from the Kotumsar Cave, Central India Shraddha Band a, *, 1, M.G. Yadava a, Mahjoor Ahmad Lone b, **, Chuan-Chou Shen b, Kaushik Sree c, R. Ramesh a a
Geosciences Division, Physical Research Laboratory, Ahmedabad, India High-Precision Mass Spectrometry and Environment Change Laboratory (HISPEC), Department of Geosciences, National Taiwan University, Taipei, Taiwan, ROC c Department of Earth Sciences, Pondicherry University, Kalapet, Puducherry, India b
a r t i c l e i n f o
a b s t r a c t
Article history: Received 31 October 2016 Received in revised form 15 November 2017 Accepted 22 January 2018 Available online xxx
The Indian Summer Monsoon (ISM), a significant part of the global monsoon system, is driven by several climate forcing parameters. With the growing pace of global climate change scenario, there is need to focus on generating more high-resolution records of past monsoon. The ISM reconstructions from Core Monsoon Zone (CMZ) of India, which represents all-India Summer Monsoon Rainfall, are useful for a better understanding of its past variability. Such reconstructions from the CMZ are rather sparse and require detailed study based on various climate proxies. Here, we focus on the reconstruction of ISM variability during the mid-Holocene, based on stalagmite oxygen isotope ratios from the Kotumsar cave, Central India. We show that with decreasing insolation, monsoon started declining at the beginning of the mid-Holocene from 8.5 to 6.5 ka BP, which is also observed in the previous ISM reconstructions with coarser resolutions. However, a gradual increase in the rainfall is observed from 6.5 to 5.6 ka BP, a feature which is also noted in the East Asian Monsoon reconstruction from the Dongge cave. Our record mainly emphasizes on the occurrence of several abrupt weak monsoon events throughout the mid-Holocene. The occurrence of 8.2 and 5.9 ka abrupt weak monsoon events suggest that ISM variability is tightly bound to North-Atlantic Oscillation (NAO). We also demonstrate that ISM during the mid-Holocene was partly sensitive to El-Nino Southern Oscillation (ENSO), and displayed an inverse relationship. © 2018 Elsevier Ltd and INQUA. All rights reserved.
1. Introduction Speleothems, occurring in wide geographic regions and datable precisely by U-Th mass spectrometry, have proved to be important proxies for deciphering past climate changes (e.g., McDermott, 2004). Oxygen isotopic composition (d18O) is the most widely used proxy in speleothems and is primarily controlled by changes in precipitation due to amount effect in tropical and sub-tropical regions (Neff et al., 2001; Yadava et al., 2004; Lone et al., 2014; Raza et al., 2017). Therefore, speleothem form an ideal archive to reconstruct the
* Corresponding author. ** Corresponding author. E-mail addresses:
[email protected],
[email protected] (S. Band),
[email protected],
[email protected] (M.A. Lone). 1 Presently at Research Centre for Environmental Science, Academia Sinica, Taipei, Taiwan.
Indian Summer Monsoon (ISM), and is well established (Yadava and Ramesh, 1999, 2005, 2006; Yadava et al., 2004; Laskar et al., 2013; Sanwal et al., 2013; Kotlia et al., 2014; Lone et al., 2014; Allu et al., 2015; Raza et al., 2017). Although ISM on glacial-interglacial timescale shows extreme fluctuations, its variability during Holocene displays significant centennial and multi-decadal changes. Insolation plays a dominant role in controlling the variability of ISM, on orbital timescales (Leuschner and Sirocko., 2003; Kathayat et al., 2016). Whereas on centennial to millennial timescales, ISM variability is observed to co-vary with changes in the North-Atlantic circulation and ENSO (Fleitmann et al., 2003; Hong et al., 2003; Wang et al., 2005; Abram et al., 2007; Kumar and Ramesh, 2017). Steig (1999) suggested that Mid-Holocene climate changes are more complex and require high-resolution, high-quality studies from different localities. These changes are very important as the human's started wide agricultural practices during this time. Driven by changes in solar output many multi-centennial weak monsoon events in Asian monsoon have been reported to have had
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Please cite this article in press as: Band, S., et al., High-resolution mid-Holocene Indian Summer Monsoon recorded in a stalagmite from the Kotumsar Cave, Central India, Quaternary International (2018), https://doi.org/10.1016/j.quaint.2018.01.026
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S. Band et al. / Quaternary International xxx (2018) 1e6
serious consequences on cultural evolution and are in phase with North Atlantic ice-rafting (Wang et al., 2005). These prolonged droughts in ISM during the mid-Holocene are suggested to be caused by regional warming in the Indo-Pacific Warm Pool (IPWP), due to changes in the meridional overturning circulation and Walker Cell position (Prasad et al., 2014). Moreover, a negative Indian Ocean Dipole (IOD) caused by surface cooling of Arabian sea leads to weakened monsoon winds (Saraswat et al., 2013). The scarce Holocene speleothem records are either from the peripheral domain of ISM (Burns et al., 1998; Neff et al., 2001; Fleitmann et al., 2003, 2004, 2007; Shakun et al., 2007) or of different time windows from peninsular India (Yadava et al., 2004; Yadava and Ramesh, 2005; Sinha et al., 2007; Berkelhammer et al., 2010, 2012; Kotlia et al., 2014). Furthermore, there is no annual to sub-decadal ISM record from the CMZ that can help resolve the actual structure of these prolonged droughts and their controlling factors vis- a-vis their role in cultural evolution. In order to address the above issues, here we present 3000 years long Mid-Holocene speleothem based ISM variability record from Kotumsar cave located in CMZ of peninsular India. Spanning from 8.5 to 5.6 ka, the novelty of our record lies in its high resolution (sub-annual to sub-decadal) allowing us to understand the structure of prolonged weak ISM events and their role in the societal change in South Asia. Most of these significant shifts in ISM activity are observed to have occurred within few decades followed by multi-centennial prolonged droughts. 2. Regional settings The Kotumsar cave (19 000 N, 82 000 E, 35 m below ground level) is one of the many caves located in the Kanger Valley National Park, Chhattisgarh (Fig. 1 top) in Central India. It formed by the dissovati group of rocks of the lution of Kanger limestone of the Indra Mesoproterozoic era (Maheshwari et al., 2005). The lateral extent of the caves is around 330 m with chambers and passages around 20e70 m wide (Yadava et al., 2007). A narrow channel of water passes through the central part of the cave galleries which is fed at the cave entrance during the ISM season (June to September) and terminates in the middle of the cave becoming a part of the underground pathways. Small ponds are seen during the dry seasons, pre-monsoon and post-monsoon (winter), which receive cave drip water and serve as a source of life for the cave biology. Currently, the cave is open to public visit during winter. In the far interior of this cave (Fig. 1 bottom), a few stalagmite pieces were found lying horizontally within a narrow zone (~1e1.5 m of vertical space between the cave roof and the surface of ~1 m raised bedrock). A few stalagmites were recovered from this site in June 2006 CE. Around these stalagmites, layers of fresh carbonate deposition were seen due to which these were lying intact on the surface, although the surrounding was found to be dry at the time of collection. Climatic, geological and geomorphologic setup in this area has favored the formation of many other caves in the vicinity (e.g., Narayana et al., 2014). Paleomonsoon reconstruction studies based on speleothems from the Dandak (~5 km from the Kotumsar cave) spanning 3.5 ka -present (Yadava and Ramesh, 2005) and 1500e600AD (Sinha et al., 2007), and the Gupteshwar caves (~30 km apart) spanning 3.4 ka e present (Yadava and Ramesh, 2005) have been reported earlier. The nearest meteorological station, Jagadalpur, is ~5 km from the cave (Fig. 1.). To determine the moisture sources contributing to rainfall during the wet season (June to October), we carried out a Lagrangian back trajectory analysis using the HYSPLIT model (Stein et al., 2015) with NCEP Reanalysis-1 (Kalnay et al., 1996) as input to the model. We chose all the days with daily rain above 2 mm during 30years (1980e2009 CE) for the analysis. During ISM, trajectories suggest that the Arabian Sea is the major source of moisture and its
Fig. 1. Top: Map of the study area showing the location of the Kotumsar cave, Central India; bottom: Sketch of horizontal cross-sectional view of the Kotumsar cave (Yadava et al., 2007). Dotted circle shows the site of KOT-I speleothem.
isotopic composition is likely to reflect the rainout over the Western Ghats (Fig. 2).
3. Material and methods KOT-I sample is a 29.6 cm long stalagmite, composed mostly of white calcite with its outer surface covered by a grey calcitic layer (based on X-ray diffraction analyses). Sample, when cut along its growth axis, can be divided into four bands (I to IV, SI. Fig. 1) based on color and texture. In band III, distinct brown laminae, in response to incorporation of soil impurities, are observed. Very high-resolution sampling was done using Newwave Research Micromill, with the spatial resolution of 200 mm (~3e5 samples in a layer). Around 1277 subsamples were extracted from 29.6 cm long KOT-I stalagmite. Subsamples weighed ~500 mg and stable isotopes of O were measured on a Delta-V plus IRMS at the Physical Research Laboratory, Ahmedabad, India. The International standard NBS-19 was used for calibration and results are reported with respect to VPDB. The precisions (1s) of d18O and d13C measurements were ~0.09‰ and ~0.1‰ respectively. The stalagmite was sampled at six layers for U-Th dating and the measurements were carried out using a ThermoeFisher NEPTUNE multi-collector inductively coupled plasma mass spectrometer (MC-ICP-MS) at the High Precision Mass Spectrometry and Environmental Change
Please cite this article in press as: Band, S., et al., High-resolution mid-Holocene Indian Summer Monsoon recorded in a stalagmite from the Kotumsar Cave, Central India, Quaternary International (2018), https://doi.org/10.1016/j.quaint.2018.01.026
S. Band et al. / Quaternary International xxx (2018) 1e6
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deposition, from 8.4 to 6.5 ka BP, the deposition rate was slow ~0.055 mm/yr. The stalagmite growth was rapid between 6.5 and 5.6 ka BP, with the rate of ~0.23 mm/yr. The results of Hendy test (Hendy, 1971) performed on four layers of KOT-I sample are shown in SI Fig. 3. The d18O values along a layer do not show major fluctuations and also there is a poor correlation between d18O and d13C values. This ensures that the sample was precipitated under an isotopic equilibrium and can be used for paleomonsoon reconstructions.
4.1. d18Odpand cave temperature An empirical relation between oxygen isotopic composition of the calcite layer (d18Ocal-VPDB) and that of the supersaturated water (d18Owater-VPDB) from which calcite precipitates at ambient temperature (T in Kelvin), is given (O'Neil et al., 1969) by the following equation: Fig. 2. Five days back trajectory estimated at 1500 m above ground level at the Kotumsar cave location, calculated by HYSPLIT (Stein et al., 2015) using the dataset from National Centre for Environmental Prediction (NCEP) reanalysis 1 (Kalnay et al., 1996). During a thirty year period (1980e2009), all those days that received rain above 2 mm were considered for the analysis (JJAS-left and October-right) with the 2244 number of trajectories.
Laboratory (HISPEC), National Taiwan University (Shen et al., 2012). The chemical separation was carried out using the protocol described in Shen et al. (2003). 4. Results Table 1 shows the U-Th ages of KOT-I stalagmite with associated errors. The age model was then constructed based on 6 ages and is shown in SI Fig. 2. The growth of the sample is from ~8.4e5.6 ka BP. The rate of growth, however, has varied during its course of the
Table 1 Uranium and Thorium isotopic compositions and Sample
Depth
Weight
238
a
(mm)
g
ppb
KOT-1 *KOT-2 *KOT-3 *KOT-4 *KOT-5 *KOT-6 *KOT-7 *KOT-8 KOT-9 KOT-10 KOT-11 *KOT-12 *KOT-13 KOT-14 KOT-15
1.5 11.5 23 38 46 62.5 78.5 103 124 168 181.5 201 227 274 276.5
0.105 0.104 0.114 0.098 0.133 0.117 0.178 0.269 0.246 0.119 0.153 0.155 0.102 0.143 0.127
244.34 80.531 78.246 73.557 84.213 74.826 77.818 95.443 86.547 101.609 117.40 321.88 114.50 120.68 93.198
Th ages of the subsamples of Kotumsar stalagmite. All errors are absolute 2s values.
232
U
ID
230
d234U
Th
ppt ±0.20 ±0.064 ±0.062 ±0.059 ±0.068 ±0.074 ±0.070 ±0.092 ±0.079 ±0.095 ±0.13 ±0.64 ±0.12 ±0.11 ±0.084
Fig. 3. d18O (dark blue) time series of KOT-I stalagmite. The stalagmite was deposited between 8.4 and 5.6 ka BP. The ages considered in the model are shown as purple filled circles. The errors are reported as 2s. The shaded orange regions demarcate abrupt decrease in ISM intensity corresponding to the North Atlantic climate changes.
79.5 1281.3 282.1 3142.0 1402.1 230.2 315.1 173.8 629.8 2063 2057.4 4581 16518 7561 763
[230Th/238U] a
activity
±1.4 ±1.5 ±1.7 ±1.8 ±1.7 ±2.7 ±2.1 ±2.7 ±2.2 ±2.3 ±2.5 ±3.7 ±2.8 ±2.1 ±2.0
0.08192 0.1386 0.2034 0.1362 0.1335 0.1517 0.10064 0.10148 0.09881 0.1012 0.1031 0.648 0.3967 0.1298 0.1195
measured ±4.5 ±5.0 ±4.1 ±7.6 ±4.1 ±4.0 ±2.7 ±1.7 ±2.1 ±34 ±4.3 ±73 ±70 ±20 ±4
622.8 688.1 693.1 684.9 686.2 696.5 696.0 696.9 700.4 715.7 706.7 409.3 719.7 674.6 684.8
c
[230Th/232Th] ppm
±0.00067 ±0.0012 ±0.0012 ±0.0017 ±0.0010 ±0.0011 ±0.00078 ±0.00057 ±0.00065 ±0.0012 ±0.0010 0.019 0.0064 0.0022 0.0010
d
4152 143.6 930 52.57 132.2 813 409.7 919 223.9 82.2 97.0 751 45.33 34.17 240.9
Age uncorrected
±237 1.3 ±15 0.67 1.1 ±15 4.7 ±11 1.6 1.6 1.0 ±25 0.76 0.59 2.5
5631 9287 13,841 9142 8948 10,153 6644 6697 6503 6603 6767 64,857 28,072 8755 7987
d234Uinitial
Age
±48 ±82 ±90 ±120 ±72 ±81 ±53 ±40 ±45 ±78 ±68 ±2545 ±510 ±156 ±72
corrected 5626 *9040 *13,785 *8476 *8690 *10,105 *6581 *6669 6391 6292 6497 *64,604 *25,903 7770 7860
c,e
±48 ±148 ±94 ±355 ±148 ±84 ±62 ±43 ±72 ±174 ±151 ±2542 ±1206 ±519 ±96
correctedb 632.8 705.9 720.6 701.5 703.3 716.7 709.1 710.1 713.2 728.6 719.8 491.2 774.2 689.6 700.1
±1.4 ±1.6 ±1.7 ±1.9 ±1.7 ±2.8 ±2.2 ±2.8 ±2.3 ±2.3 ±2.6 ±5.7 ±4.0 ±2.3 ±2.0
Chemistry was performed on 16th, Feb., and 23rd March, 2016 (Shen et al., 2003), and instrumental analysis on MC-ICP-MS (Shen et al., 2012). Analytical errors are 2s of the mean. Decay constants are 9.1705 106 yr1 for 230Th, 2.8221 106 yr1 for 234U (Cheng et al., 2013), and 1.55125 1010 yr1 for 238U (Jaffey et al., 1971). *Ages discarded from the COPRA- age model due to age reversals and high detrital Th content. a 238 [ U] ¼ [235U] 137.818 (±0.65‰); d234U ¼ ([234U/238U]activity 1) 1000. b d234Uinitial corrected was calculated based on 230Th age (T), i.e., d234Uinitial ¼ d234Umeasured X el234 *T , and T is corrected age. c 230 [ Th/238U]activity ¼ 1 el230 T þ (d234Umeasured/1000)[l230/(l230 l234)](1 eðl230 l234 TÞ ), where T is the age. d The degree of detrital 230Th contamination is indicated by the [230Th/232Th] atomic ratio instead of the activity ratio. e Age corrections for samples were calculated using an estimated initial atomic 230Th/232Th ratio of 4 ± 4 ppm. Those are the values for a material at secular equilibrium, with the crustal 232Th/238U value of 3.8. The errors are arbitrarily assumed to be 100%.
Please cite this article in press as: Band, S., et al., High-resolution mid-Holocene Indian Summer Monsoon recorded in a stalagmite from the Kotumsar Cave, Central India, Quaternary International (2018), https://doi.org/10.1016/j.quaint.2018.01.026
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d18Ocal-VPDB e d18Owater-VPDB ¼ (2.78 106 / T2) e 3.39 At Jagdalpur (Fig. 1 top), the mean annual temperature is 25.5 C. Therefore, (2.78 106/T2) e 3.39 ¼ 27.8‰ Where T ~ 273 þ 25.5 K. Therefore, the mean temperature should enrich the calcite relative to the drip water by ~27.8‰ on the VPDB scale (59.57 w. r.t VSMOW). An actively growing speleothem tip and drip water (dp) associated with it were collected simultaneously during another field visit. The d18Odp and d18Ocalcite values were 2.63 ± 0.38‰ w. r.t VPDB and 28.20 w. r.t VSMOW (n ¼ 4) and 5.0 ± .15‰ (n ¼ 3), respectively (Yadava, 2002). This result ensures that at present, the conditions in the cave are likely favorable for isotopic equilibrium deposition of calcite from the drip water. In a tropical climate, large temperature variations over millennial timescales are less likely. No major changes in tectonic and geomorphologic setup have been recorded in the past few thousand years. By and large, the cave temperature may have remained constant during the deposition of the stalagmite KOT-I. 4.2. Stable isotopes of oxygen The stable isotope ratios of oxygen are shown in Fig. 3. The d18O values vary between 6 and 3‰, with an average fluctuation around 4.5‰. The oxygen and carbon isotope profiles show dense
points between 7.5 and 5.6 ka BP. This is owing to the age model, where the regularly spaced proxy record has been squeezed in the constrained time frame. The values show a depleting trend from 6.5 to 5.6 ka BP. This could be attributed to increasing rainfall, further, evident from the increased growth rate for this section of the sample. The oxygen profile also shows the episodes of periodic enrichment. 5. Discussion KOT-I is used to infer high-resolution d18O variations occurring in the mid-Holocene. In the tropics, variation in speleothem d18O is governed by the variation in the amount of rainfall (Bar-Matthews et al., 1997; Dansgaard, 1964), d18O record of KOT-I (Fig. 3) is used to reconstruct the rainfall record for a time span from 8.5 to 5.6 ka. The reconstructed record shows a gradual decline in intensity of ISM from 8.5 to 7.3 ka, followed by increasing trend from 7.3 to 5.6 ka. This decrease (between 8.5 and 5.6 ka) is attributed to the southward shift of ITCZ and decreasing (Fleitmann et al., 2003; Paillard et al., 1996) JuneeAugust insolation at 30 N. When the ITCZ shifts southwards, the land-sea temperature contrast decreases, leading to weakening of monsoon. Weaker monsoon is also recorded in Arabian sea core d18O timeseries of G. ruber (Singh et al., 2006) and abundance studies of G. bulloides (Gupta et al., 2003) and in lake records of Garhwal (Srivastava et al., 2013). Previous workers (Enzel
Fig. 4. (A) Lake El Junco grain size record (representing ENSO variability) from Galapagos islands near the equator in tropical Pacific ocean (Purple, Conroy et al., 2008). (B) Hematite-stained grain record (%) from the core MC52 from the North Atlantic (Bond et al., 1997). d18O records of the (C) Mawmulah cave (Green, Berkelhammere al., 2012), (D) the Dongge cave (red, Dykoski et al., 2005), (E) the present study (Dark blue).
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et al., 1999; Laskar et al., 2013; Ramesh, 2001; Staubwasser et al., 2003) have shown that there was an increase in monsoon rainfall from 6.3 to 5.5 ka. The evidence of this variability was also seen in the northern hemisphere where there was an advance in alpine glaciers and strengthening of westerlies in North Atlantic and Siberia (Meeker and Mayewski, 2002). Our results are consistent with previous studies and marks 8.5e7 ka as a time of declining monsoon rain. There is a brief period of enhanced monsoon condition between 7.3 and 6.6 ka followed by a weaker monsoon period stretching from 6.6 to 6.5 for a span of 100 years. However, the overall trend of weakening (8.5e7 ka) and strengthening (7e5.6 ka) of monsoon during the mid-Holocene is punctuated by series of abrupt megadrought events spanning 70e100 years. Previous studies have attributed occurrence of megadrought events to the weakening of the North-Atlantic circulation (Fleitmann et al., 2003; Hong et al., 2003; Wang et al., 2005). In Fig. 4, we compared our record with Hematite-stained grain record (%) from the core MC52 from the North Atlantic (Bond et al., 1997). Our observation shows that in addition to 8.2 and 5.9ka Bond events, weakening of monsoon is also found during the abrupt cold periods (7.7, 7.3, 6.5 and 5.7 ka) reconstructed from the sediment core. The Occurrence of such drought events is also seen in the speleothem records from the Dongge (Dykoski et al., 2005) and Mawmullah caves (Berkelhammer et al., 2012). A recent study from Lake Ximenglongtan, southwest China (Ning et al., 2017), also recorded series of weak ISM events coinciding with our observations. The study suggests that the occurrence of such drought events may correspond to the reduced total solar irradiance (TSI) in addition to cooling of the North Atlantic climate and the ENSO in the equatorial Pacific Ocean. The Weakening of the North Atlantic circulation, owing to reduced total solar irradiance, leads to cooling of the northern Indian Ocean, one of the major monsoon drivers (Pausata et al., 2011). This, in turn, reduces the precipitation over Indian subcontinent as evident from our stalagmite record. On the other hand, strengthening of ENSO also affects ISM intensity by modulating the Walker circulation. During the peak ENSO episodes, the Pacific warm water pool shifts eastward, shifting the descending arm of Walker circulation towards Indian subcontinent. As a result, an anticorrelation is observed between ISM and ENSO. During the strong ENSO events, weakening of ISM is observed (Webster et al., 1998). This relation is also observed in the instrumental records and the AOGCM simulations coupled with insolation changes due to orbital parameters for the Holocene period (Webster et al., 1998; Kumar et al., 1999; Liu et al., 2000). Conroy et al. (2008), used grain size distributions (% silt, sand and clay), C/N ratio of the lacustrine sediment core raised from the Lake El Junco, in Galapagos islands near the equator in the tropical Pacific Ocean to characterize ENSO variability during the Holocene period. Based on the increased percentage of silt and low C/N ratio, the study inferred an increase in the frequency of ENSO episodes during the mid-Holocene. Our record, when compared with Lake El Junco grain size record, shows some of the weak ISM periods coinciding with the strong ENSO events (Fig. 4 A and E). Comparison of ISM with the North Atlantic circulation and the ENSO index to understand the mechanism of these abrupt changes would lead to over simplification of the rather complex climate process. Hence the factors governing abrupt changes in ISM in the core monsoon region of India requires further investigation. 6. Conclusion A stalagmite from Central India was used to reconstruct variations in the past monsoon rainfall between 8.5 and 5.6 ka. A gradual decrease in the monsoon in response to a decrease in insolation
5
was observed between 8.5 and 7.3 ka, followed by a steady increase in the ISM intensity between 6.3 and 5.6 ka. During the midHolocene, the overall trend of monsoon is punctuated by abrupt megadrought events spanning 70e100 years. Comparison with north-Atlantic oscillations and ENSO events shows a strong teleconnection between the climate systems. Based on the present study we conclude that in addition to the insolation changes, the ISM variability during mid-Holocene was modulated by abrupt cooling episodes of the north-Atlantic and increased frequency in the ENSO. Acknowledgments We thank N$B.Vaghela (PRL) for technical support, and the Indian Space Research Organization e Geosphere Biosphere Programme for funding. We thank P. Gautam and A. C. Narayana, Central University of Hyderabad, for help with mineralogy of some sub-samples. U-Th dating was supported by grants from Taiwan ROC MOST (104-2119-M-002-003, 105-2119-M-002-001) and the National Taiwan University (105R7625). Appendix A. Supplementary data Supplementary data related to this article can be found at https://doi.org/10.1016/j.quaint.2018.01.026. References Abram, N.J., Gagan, M.K., Liu, Z., Hantoro, W.S., McCulloch, M.T., Suwargadi, B.W., 2007. Seasonal characteristics of the Indian Ocean Dipole during the Holocene epoch. Nature 445 (7125), 299e302. Allu, N.C., Tiwari, M., Yadava, M.G., Dung, N.C., Shen, C.-C., Belgaonkar, S.P., Ramesh, R., Laskar, A.H., 2015. Stalagmite d18O variations in southern India reveal divergent trends of Indian summer monsoon and East Asian summer monsoon during the last interglacial. Quat. Int. https://doi.org/10.1016/ j.quaint.2014.12.014. Bar-Matthews, M., Ayalon, A., Kaufman, A., 1997. Late quaternary paleoclimate in the Eastern Mediterranean Region from stable isotope analysis of speleothems at Soreq Cave. Isr. Quat. Res. 47, 155e168. https://doi.org/10.1006/ qres.1997.1883. Berkelhammer, M., Sinha, A., Mudelsee, M., Cheng, H., Edwards, R.L., Cannariato, K., 2010. Persistent multidecadal power of the Indian Summer Monsoon. Earth Planet. Sci. Lett. 290 (1e2), 166e172. Berkelhammer, M., Sinha, A., Stott, L., Cheng, H., Pausata, F., Yoshimura, K., 2012. An Abrupt Shift in the Indian Monsoon 4000 Years Ago, Climates, Landscapes, and Civilizations, pp. 75e88. Bond, G., Showers, W., Cheseby, M., Lotti, R., Almasi, P., Priore, P., Cullen, H., Hajdas, I., Bonani, G., et al., 1997. A pervasive millennial-scale cycle in North Atlantic Holocene and glacial climates. Science 278 (5341), 1257e1266. Burns, S.J., Matter, A., Frank, N., Mangini, A., 1998. Speleothem-based paleoclimate record from northern Oman. Geology 26 (6), 499e502. Cheng, H., Edwards, R.L., Shen, C.C., Polyak, V.J., Asmerom, Y., Woodhead, J., €tl, C., Wang, X., 2013. Improvements in 230 Hellstrom, J., Wang, Y., Kong, X., Spo Th dating, 230 Th and 234 U half-life values, and UeTh isotopic measurements by multi-collector inductively coupled plasma mass spectrometry. Earth Planet Sci. Lett. 371, 82e91. Conroy, J.L., Overpeck, J.T., Cole, J.E., Shanahan, T.M., Steinitz-Kannan, M., 2008. pagos Holocene changes in eastern tropical Pacific climate inferred from a Gala lake sediment record. Quat. Sci. Rev. 27 (11), 1166e1180. Dansgaard, W., 1964. Stable isotopes in precipitation. Tellus 16, 436e468. https:// doi.org/10.1111/j.2153-3490.1964.tb00181.x. Dykoski, C.A., Edwards, R.L., Cheng, H., Yuan, D., Cai, Y., Zhang, M., Lin, Y., Qing, J., An, Z., Revenaugh, J., 2005. A high-resolution, absolute-dated Holocene and deglacial Asian monsoon record from dongge cave, China. Earth Planet Sci. Lett. 233 (1), 71e86. Enzel, Y., Ely, L.L., Mishra, S., Ramesh, R., Amit, R., Lazar, B., Rajaguru, S.N., Baker, V.R., Sandler, A, 1999. High-resolution Holocene environmental changes in the Thar Desert, Northwestern India. Science 284 (80), 125e128. https://doi.org/10.1126/ science.284.5411.125. Fleitmann, D., Burns, S.J., Mudelsee, M., Neff, U., Kramers, J., Mangini, A., Matter, A., 2003. Holocene forcing of the Indian monsoon recorded in a stalagmite from southern Oman. Science 300, 1737e1739. https://doi.org/10.1126/ science.1083130. Fleitmann, D., Burns, S.J., Neff, U., Mudelsee, M., Mangini, A., Matter, A., 2004. Palaeoclimatic interpretation of high-resolution oxygen isotope profiles derived from annually laminated speleothems from Southern Oman. Quat. Sci. Rev. 23
Please cite this article in press as: Band, S., et al., High-resolution mid-Holocene Indian Summer Monsoon recorded in a stalagmite from the Kotumsar Cave, Central India, Quaternary International (2018), https://doi.org/10.1016/j.quaint.2018.01.026
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(7e8), 935e945. Fleitmann, D., Burns, S.J., Mangini, A., Mudelsee, M., Kramers, J., Villa, I., Neff, U., AlSubbary, A.A., Buettner, A., Hippler, D., Matter, A., 2007. Holocene ITCZ and Indian monsoon dynamics recorded in stalagmites from Oman and Yemen (Socotra). Quat. Sci. Rev. 26 (1e2), 170e188. Gupta, A.K., Anderson, D.M., Overpeck, J.T., 2003. Abrupt changes in the Asian southwest monsoon during the Holocene and their links to the north Atlantic ocean. Nature 421 (6921), 354e357. Hendy, C., 1971. The isotopic geochemistry of speleothemsdI. The calculation of the effects of different modes of formation of the isotopic composition of speleothems and their applicability as palaeoclimatic indicators. Geochem. Cosmochim. Acta 35, 801e824. https://doi.org/10.1016/0016-7037(71)90127-X. Hong, Y.T., Hong, B., Lin, Q.H., Zhu, Y.X., Shibata, Y., Hirota, M., Uchida, M., Leng, X.T., Jiang, H.B., Xu, H., Wang, H., 2003. Correlation between Indian Ocean summer monsoon and North Atlantic climate during the Holocene. Earth Planet Sci. Lett. 211 (3), 371e380. Jaffey, A.H., Flynn, K.F., Glendenin, L.E., Bentley, W.T., Essling, A.M., 1971. Precision measurement of half-lives and specific activities of U 235 and U 238. Phys. Rev. C 4 (5), 1889. Kalnay, E., Kanamitsu, M., Kistler, R., Collins, W., Deaven, D., Gandin, L., Iredell, M., Saha, S., White, G., Woollen, J., et al., 1996. The ncep/ncar 40-year reanalysis project. Bull. Am. Meteorol. Soc. 77 (3), 437e471. €tl, C., Edwards, R.L., Zhang, H., Li, X., Yi, L., Kathayat, G., Cheng, H., Sinha, A., Spo Ning, Y., Cai, Y., Lui, W.L., 2016. Indian monsoon variability on millennial-orbital timescales. Sci. Rep. 6, 24374. Kotlia, B.S., Singh, A.K., Joshi, L.M., Dhaila, B.S., 2014. Precipitation variability in the Indian Central Himalaya during last ca. 4,000 years inferred from a speleothem record: impact of Indian summer monsoon (ISM) and Westerlies. Quat. Int. https://doi.org/10.1016/j.quaint.2014.10.066. Kumar, K.K., Rajagopalan, B., Cane, M.A., 1999. On the weakening relationship between the Indian monsoon and ENSO. Science 284 (5423), 2156e2159. Kumar, P.K., Ramesh, R., 2017. Revisiting reconstructed Indian monsoon rainfall variations during the last ~25 ka from planktonic foraminiferal d18O from the Eastern Arabian Sea. Quat. Int. 443, 29e38. Laskar, A.H., Yadava, M.G., Ramesh, R., Polyak, V.J., Asmerom, Y., 2013. A 4 kyr stalagmite oxygen isotopic record of the past Indian Summer Monsoon in the Andaman Islands. Geochem. Geophys. Geosyst. 14, 3555e3566. https://doi.org/ 10.1002/ggge.20203. Leuschner, D.C., Sirocko, F., 2003. Orbital insolation forcing of the Indian Monsoonea motor for global climate changes? Palaeogeogr. Palaeoclimatol. Palaeoecol. 197 (1), 83e95. Liu, Z., Kutzbach, J., Wu, L., 2000. Modeling climate shift of El nino variability in the Holocene. Geophys. Res. Lett. 27 (15), 2265e2268. Lone, M.A., Ahmad, S.M., Dung, N.C., Shen, C.-C., Raza, W., Kumar, A., 2014. Speleothem based 1000-year high resolution record of Indian monsoon variability during the last deglaciation. Palaeogeogr. Palaeoclimatol. Palaeoecol. 395, 1e8. https://doi.org/10.1016/j.palaeo.2013.12.010. Maheshwari, A., Sial, A.N., Guhey, R., Ferreira, V.P., 2005. C-isotope Composition of Carbonates from Indravati Basin, India : Implications for Regional Stratigraphic Correlation, pp. 603e610. McDermott, F., 2004. Palaeo-climate reconstruction from stable isotope variations in speleothems: a review. Quat. Sci. Rev. 23, 901e918. https://doi.org/10.1016/ j.quascirev.2003.06.021. Meeker, L.D., Mayewski, P.A., 2002. A 1400-year high-resolution record of atmospheric circulation over the North Atlantic and Asia. Holocene 12, 257e266. https://doi.org/10.1191/0959683602hl542ft. Narayana, A.C., Yadava, M.G., Dar, F.A., Ramesh, R., 2014. The spectacular Belum and Borra caves of eastern India. In: Kale, V.S. (Ed.), Landscapes and Landforms of India. Springer, Netherlands, pp. 189e194. Neff, U., Burns, S.J., Mangini, A., Mudelsee, M., Fleitmann, D., Matter, A., 2001. Strong coherence between solar variability and the monsoon in Oman between 9 and 6 kyr ago. Nature 411 (6835), 290e293. Ning, D., Zhang, E., Sun, W., Chang, J., Shulmeister, J., 2017. Holocene Indian Summer Monsoon variation inferred from geochemical and grain size records from Lake Ximenglongtan, southwestern China. Palaeogeogr. Palaeoclimatol. Palaeoecol. 487, 260e269. O'Neil, J.R., Clayton, R.N., Mayeda, T.K., 1969. Oxygen isotope fractionation of divalent metal carbonates. J. Chem. Phys. 30, 5547e5558. Paillard, D., Labeyrie, L., Yiou, P., 1996. Macintosh program performs timeseries analysis, Eos. Trans. Am. Geophys. Union 77 (39), 379e379.
Pausata, F.S., Battisti, D.S., Nisancioglu, K.H., Bitz, C.M., 2011. Chinese stalagmite [delta] 18O controlled by changes in the Indian monsoon during a simulated Heinrich event. Nat. Geosci. 4 (7), 474e480. Prasad, S., Anoop, A., Riedel, N., Sarkar, S., Menzel, P., Basavaiah, N., Krishnan, R., € hl, U., 2014. Prolonged monsoon droughts and Fuller, D., Plessen, B., Gaye, B., Ro links to Indo-Pacific warm pool: a Holocene record from Lonar Lake, central India. Earth Planet Sci. Lett. 391, 171e182. Ramesh, R., 2001. High resolution Holocene monsoon records from different proxies: an assessment of their consistency. Curr. Sci. 81, 1432e1436. Raza, W., Ahmad, S.M., Lone, M.A., Shen, C.C., Sarma, D.S., Kumar, A., 2017. Indian summer monsoon variability in southern India during the last deglaciation: evidence from a high resolution stalagmite d18O record. Palaeogeogr. Palaeoclimatol. Palaeoecol. 485, 476e485. Sanwal, J., Kotlia, B.S., Rajendran, C., Ahmad, S.M., Rajendran, K., Sandiford, M., 2013. Climatic variability in Central Indian Himalaya during the last ~1800 years: evidence from a high resolution speleothem record. Quat. Int. 304, 183e192. https://doi.org/10.1016/j.quaint.2013.03.029. Saraswat, R., Lea, D.W., Nigam, R., Mackensen, A., Naik, D.K., 2013. Deglaciation in the tropical Indian Ocean driven by interplay between the regional monsoon and global teleconnections. Earth Planet Sci. Lett. 375, 166e175. Shakun, J.D., Burns, S.J., Fleitmann, D., Kramers, J., Matter, A., Al-Subary, A., 2007. A high-resolution, absolute-dated deglacial speleothem record of Indian Ocean climate from Socotra Island, Yemen. Earth Planet. Sci. Lett. 259 (3e4), 442e456. Shen, C.C., Cheng, H., Edwards, R.L., Moran, S.B., Edmonds, H.N., Hoff, J.A., Thomas, R.B., 2003. Measurement of attogram quantities of 231Pa in dissolved and particulate fractions of seawater by isotope dilution. Anal. Chem. 75, 1075e1079. Shen, C.C., Cheng, H., Edwards, R.L., Hsieh, Y.T., Gallet, S., Chang, C.C., Li, T.Y., Lam, D.D., Kano, A., Hori, N., SpVotl, C., 2012. High resolution and high precision carbonate 230Th dating by MC-ICP-MS with SEM protocols. Geochem. Cosmochim. Acta 99, 71e86. Singh, A., Kroon, D., Ganeshram, R., 2006. Millennial-scale variations in productivity and omz intensity in the eastern Arabian sea. J. Geol. Soc. India 68 (3), 369. Sinha, A., Cannariato, K.G., Stott, L.D., Cheng, H., Edwards, R.L., Yadava, M.G., Ramesh, R., Singh, I.B., 2007. A 900-year (600 to 1500 A.D.) record of the Indian summer monsoon precipitation from the core monsoon zone of India. Geophys. Res. Lett. 34 https://doi.org/10.1029/2007GL030431. Srivastava, P., Kumar, A., Mishra, A., Meena, N.K., Tripathi, J.K., Sundriyal, Y., Agnihotri, R., Gupta, A.K., 2013. Early Holocene monsoonal fluctuations in the Garhwal higher Himalaya as inferred from multi-proxy data from the malari paleolake. Quat. Res. 80 (3), 447e458. Staubwasser, M., F, S., P.M, G., M, S., 2003. Climate change at the 4.2 ka BP termination of the Indus valley civilization and Holocene south Asian monsoon variability. Geophys. Res. Lett. 30, 1425. https://doi.org/10.1029/2002GL016822. Steig, E.J., 1999. Mid-Holocene climate change. Science 286 (5444), 1485. Stein, A.F., Draxler, R.R., Rolph, G.D., Stunder, B.J.B., Cohen, M.D., Ngan, F., 2015. NOAA's HYSPLIT atmospheric transport and dispersion modeling system. Bull. Am. Meteorol. Soc. 96 (12), 2059e2077. https://doi.org/10.1175/BAMS-D-1400110.1. Wang, Y., Cheng, H., Edwards, R.L., He, Y., Kong, X., An, Z., Wu, J., Kelly, M.J., Dykoski, C.A., Li, X., 2005. The Holocene Asian monsoon: links to solar changes and north Atlantic climate. Science 308 (5723), 854e857. Webster, P.J., Magana, V.O., Palmer, T.N., Shukla, J., Tomas, R.A., Yanai, M.U., Yasunari, T., 1998. Monsoons: processes, predictability, and the prospects for prediction. J. Geophys. Res.: Oceans 103 (C7), 14451e14510. Yadava, M.G., 2002. Stable Isotope Systematics in Cave Calcites: Implications to Past Climatic Changes in Tropical India. Unpubl. (Ph. D. thesis). Devi Ahilya Vishwavidyalaya, Indore, India, p. 175. Yadava, M.G., S, K.S., S, I.B., Ramesh, R., 2007. Evidence of early human occupation in the limestone caves of Bastar, Chhattisgarh. Curr. Sci. 92. Yadava, M.G., Ramesh, R., 1999. Speleothems-Useful proxies for past monsoon rainfall. J. Sci. Ind. Res. (India) 58, 339e348. Yadava, M.G., Ramesh, R., Pant, G.B., 2004. Past monsoon rainfall variations in peninsular India recorded in a 331-year-old speleothem. Holocene 14 (4), 517e524. Yadava, M.G., Ramesh, R., 2005. Monsoon Reconstruction from Radiocarbon Dated Tropical Indian Speleothems, vol. 1, pp. 48e59. Yadava, M.G., Ramesh, R., 2006. Stable oxygen and carbon isotope variations as monsoon Proxies : a comparative study of speleothems from four different locations in India. J. Geol. Soc. India 68, 461e475.
Please cite this article in press as: Band, S., et al., High-resolution mid-Holocene Indian Summer Monsoon recorded in a stalagmite from the Kotumsar Cave, Central India, Quaternary International (2018), https://doi.org/10.1016/j.quaint.2018.01.026