The Indian Summer Monsoon from a Speleothem δ18O Perspective—A Review

As one of the most prominent seasonally recurring atmospheric circulation patterns, the Asian summer monsoon (ASM) plays a vital role for the life and livelihood of about one-third of the global population. Changes in the strength and seasonality of the ASM significantly affect the ASM region, yet the drivers of change and the varied regional responses of the ASM are not well understood. In the last two decades, there were a number of studies reconstructing the ASM using stalagmite-based proxies such as oxygen isotopes (δ18O). Such reconstructions allow examination of ASM drivers and responses, increasing monsoon predictability. In this review paper, we focus on stalagmite δ18O records from India at the proximal end of the ASM region. Indian stalagmite δ18O records show well-dated, high-amplitude changes in response to the dominant drivers of the ASM on orbital to multi-centennial timescales, and indicate the magnitude of monsoon variability in response to these drivers. We examine Indian stalagmite records collated in the Speleothem Isotope Synthesis and AnaLysis version 1 (SISAL_v1) database and support the database with a summary of record quality and regional climatic interpretations of the δ18O record during different climate states. We highlight current debates and suggest the most useful time periods (climatic events) and locations for further work using tools such as data-model comparisons, spectral analysis methods, multi-proxy investigations, and monitoring.


Introduction
The Indian summer monsoon (ISM) is part of the Asian summer monsoon (ASM) and provides ca. 70% of India's annual precipitation. Monsoon variability results in frequent floods and droughts 1.
Winter lasting from December until March; snowfall is seen only in the high-altitude Himalayan region. Winter climate is characterized by dry conditions through most of the other regions, with influence of northeasterly cold-air masses originating on the Tibetan Plateau, the "Winter monsoon". In northwest India, recycled moisture from the Atlantic, Mediterranean, and near East can be introduced by the westerlies ("Western Disturbances") [22].

2.
Summer or pre-monsoon season lasting from April to June; these are the hottest and driest months of the year with temperatures between 20 • C and 40 • C.

3.
Summer monsoon (Indian summer monsoon-ISM) or rainy season lasts from July to September; the monsoon rainfall onset is as early as the first week of June in south peninsular India gradually extending across the rest of India by the first week of July. The summer monsoon season is dominated by the southwest monsoon that delivers~70% of the total annual rainfall to India. The Meghalaya Plateau in northeast India receives exceptional amounts of precipitation at this time due to its position as the first orographic barrier for moist air masses from the Bay of Bengal [23], leading to its denomination as the "wettest place on Earth" [24]. 4.
The post-monsoon occurs during October and November; little rain falls at this time in peninsular India except in the southeast where most of the rain is brought by northeast winds that source moisture from the Bay of Bengal.
The seasonal reversal of meridional temperature and pressure gradients and associated circulation patterns which constitute the summer and winter monsoons is the most outstanding feature of Indian meteorology [25]. During the ISM period, convective rainfall dominates India's weather. A pronounced temperature gradient between Central Asia and the Indian Ocean is accompanied by a northward shift of the Intertropical Convergence Zone (ITCZ), resulting in the southeast trade winds turning westerly due to Coriolis forces as they cross the equator. These winds carry copious amounts of water from the Indian Ocean to peninsular India [1]. This southwest monsoon can be depicted as two branches: the Arabian Sea branch and the Bay of Bengal branch ( Figure 1). The Arabian Sea branch blows eastward across peninsular India and toward the Himalayas, and has a much stronger impact on peninsular India. The Bay of Bengal branch initially tracks the eastern coast and then swerves northwest at the Himalayan orographic barrier and proceeds over the Indo-Gangetic plain. Part of the Bay of Bengal branch is pushed northward along the deep meridionally oriented river valleys and onto the southern Tibetan Plateau [26]. During winter, the southward retreat of the ITCZ and parallel development of the Tibetan winter high-pressure cell results in a reversal of the wind patterns.
Two factors known to affect inter-annual ISM variability over the modern instrumental period are the El Niño-Southern Oscillation (ENSO) and Himalayan/Eurasian snow cover [1]. The Southern Oscillation is a pattern of zonal circulation in the tropics. The easterly trade winds transport cold upwelling water off the coast of Peru (Pacific Ocean) further westward. The surface water is warmed by the sun. Whichever part of the ocean is the warmest is where there is increased convection associated with the rising branch of the Walker circulation. Every 3-5 years on average, upwelling of cold waters is suppressed and El Niño conditions set in, while La Niña with a similar periodicity is characterized by warm water traveling further west than the neutral state [27], such that La Niña is associated with more convection and more rainfall in India. Satellite snow cover estimates indicate a negative relationship between snow cover (snow mass) and the ISM. Excessive snow during the preceding winter is unfavorable for the subsequent monsoon season because of delayed build-up of low-pressure cells over the continent in spring [28][29][30][31][32]. However, observations showed that the ENSO-ISM relationship [33][34][35] and the snow cover-ISM relationship [31] may be weakening in recent decades. The factors causing this weakening and the current dominant drivers of inter-annual variability are still debated.
A substantial component of ISM variability on the annual scale stems from intra-seasonal oscillations in monsoon precipitation termed active/break periods which exhibit a hierarchy of quasi periods (8-7 days, 10-20 days, and 30-60 days) [1,36]. During an "active" period, a positive rainfall anomaly is found over western and central India, and a negative rainfall anomaly is found over northeast and southeast India. During a "break" period, the signs are reversed [37,38]. Although questions remain regarding the mechanisms that drive inter-annual variability in the frequency of active/break cycles, their individual manifestations appear to be associated with the Madden-Julian Oscillation (MJO), which is the dominant driver of sub-seasonal climate variability in the pan-tropics [39]. Less is known about controls on decadal variability in the ISM. Studies suggest that solar irradiance [40] and Pacific Ocean sea surface temperature (SST) [40,41] influence ISM multi-decadal variability. cold waters is suppressed and El Niño conditions set in, while La Niña with a similar periodicity is characterized by warm water traveling further west than the neutral state [27], such that La Niña is associated with more convection and more rainfall in India. Satellite snow cover estimates indicate a negative relationship between snow cover (snow mass) and the ISM. Excessive snow during the preceding winter is unfavorable for the subsequent monsoon season because of delayed build-up of low-pressure cells over the continent in spring [28][29][30][31][32]. However, observations showed that the ENSO-ISM relationship [33][34][35] and the snow cover-ISM relationship [31] may be weakening in recent decades. The factors causing this weakening and the current dominant drivers of inter-annual variability are still debated. A substantial component of ISM variability on the annual scale stems from intra-seasonal oscillations in monsoon precipitation termed active/break periods which exhibit a hierarchy of quasi periods (8-7 days, 10-20 days, and 30-60 days) [1,36]. During an "active" period, a positive rainfall anomaly is found over western and central India, and a negative rainfall anomaly is found over northeast and southeast India. During a "break" period, the signs are reversed [37,38]. Although questions remain regarding the mechanisms that drive inter-annual variability in the frequency of active/break cycles, their individual manifestations appear to be associated with the Madden-Julian Oscillation (MJO), which is the dominant driver of sub-seasonal climate variability in the pan-tropics [39]. Less is known about controls on decadal variability in the ISM. Studies suggest that solar irradiance [40] and Pacific Ocean sea surface temperature (SST) [40,41] influence ISM multi-decadal variability.

Distribution of Speleothem Isotopic Records in Space and Time
The spatial distribution of currently known stalagmite δ 18 O records in SISAL_v1, as well as from publications and conference abstracts (published before April 2018), from the ISM region is

Distribution of Speleothem Isotopic Records in Space and Time
The spatial distribution of currently known stalagmite δ 18 O records in SISAL_v1, as well as from publications and conference abstracts (published before April 2018), from the ISM region is shown in Figure 1. Table 1 provides a comprehensive list of published records and indicates whether the records are available in SISAL_v1. Records where we were unable to get all the required information from the original authors could not be included in SISAL_v1. Mirroring the distribution of karst in India, most stalagmite records are from the northern and northeastern Himalayas. Few records were recovered from central and southern peninsular India, and there are no known records from the northwest and the Indo-Gangetic plains. The oldest and longest published stalagmite record is from Bittoo cave in northern India covering the last 240 ka [13]. Orbital-, millennial-, and Holocene-scale records are available from the ISM region; however, most of the records are discontinuous and cover relatively brief snapshots of time ( Figure 2). Nevertheless, δ 18 O records covering time periods of climatic significance are available from north, northeastern, and peninsular India ( Figure 3). Further information on the spatio-temporal distribution of stalagmites and details on the potential for further work from these caves are given in Sections 3.1 and 3.2, while Section 3.3 provides information on the quality of the records. shown in Figure 1. Table 1 provides a comprehensive list of published records and indicates whether the records are available in SISAL_v1. Records where we were unable to get all the required information from the original authors could not be included in SISAL_v1. Mirroring the distribution of karst in India, most stalagmite records are from the northern and northeastern Himalayas. Few records were recovered from central and southern peninsular India, and there are no known records from the northwest and the Indo-Gangetic plains. The oldest and longest published stalagmite record is from Bittoo cave in northern India covering the last 240 ka [13]. Orbital-, millennial-, and Holocene-scale records are available from the ISM region; however, most of the records are discontinuous and cover relatively brief snapshots of time ( Figure 2). Nevertheless, δ 18 O records covering time periods of climatic significance are available from north, northeastern, and peninsular India ( Figure 3). Further information on the spatio-temporal distribution of stalagmites and details on the potential for further work from these caves are given in Sections 3.1 and 3.2, while Section 3.3 provides information on the quality of the records.

Spatial Distribution of Caves and Potential for Paleoclimate Studies
Information on north and northeast Indian caves is provided by Gebauer [62][63][64][65][66][67][68][69][70] and Breitenbach and Gebauer [71] and a number of other publications [72][73][74][75][76][77]. In comparison to the Himalayan region, very limited information is available on the caves from peninsular India. Based on publications and field visits conducted by one or more authors of this paper, karst caves in peninsular India are mainly found in the Proterozoic Mahanadi, Kaladgi, and Cuddapah basins. Dandak, Jhumar, Gupteshwar, Kailash, and Kotumsar caves are a part of the Mahanadi basin. Additional information on caves from the Mahanadi basin can be found in References [78][79][80]. This region is worth exploring further; however, the current disturbed political conditions prevent this. Akalagavi cave formed in the limestone and dolomite formations of the Kaladgi basin on the west coast of India. Several other caves from the same karst region were explored. Akalagavi and one other cave are currently dripping; however, no further stalagmites (apart from Reference [50]) suitable for paleoclimate work were identified from this region. Belum, Valmiki, Munagamanu, and Nakarallu caves are located in the Cuddapah basin. Dar et al. [81] published a comprehensive review of the Cuddapah karst region from peninsular India. This region is worth exploring further for paleoclimate records. Several caves are protected as tourism and temple caves. Bora cave is a part of the Eastern Ghats Mobile Belt of Precambrian age. It is a large, open, airy cave and is unlikely to be suitable for paleoclimate work. No other caves are reported from this region. Baratang cave is located in limestone formations of Cenozoic age in the Andaman Island in the Bay of Bengal. Figure 2 shows the temporal distribution of stalagmite δ 18 O records from India in SISAL_v1. Table 1 provides information on records published from this region, including those records not currently in the SISAL database. Orbital-scale records are available from Bittoo cave [13] from north India and Belum cave [54] from peninsular India. Mawmluh cave [16,17,46] from the northeast currently covers the Last Glacial Maximum, and Heinrich stadials. Records from peninsular Valmiki cave covers the later phase of Heinrich event 1 [50] and the last deglaciation [49]. Bittoo [13], Kalakot [44], and Timta [15] caves from north India and Mawmluh [16,17,46] cave from northeast India cover the Bølling-Allerød (BA) and Younger Dryas (YD) periods. Sahiya [10,12] cave from north India, Mawmluh [45] and Umsynrang [61] caves from northeast India, and Kotumsar [57] cave from peninsular India cover significant periods of the Holocene. The other published records in Table 1 cover brief snapshots during the last 5000 years.

Quality of the Records
The interpretation of a δ 18 O time series strongly depends on the temporal resolution and chronological precision of the stalagmite record. Keeping this in mind, the quality of the records can be assessed based on a few objective parameters such as speleothem form, mineralogy, age control, sampling density (resolution), and cave monitoring, which aids in the interpretation of the δ 18 O signal. The SISAL database provides information on all these parameters and aids in the selection of appropriate stalagmite δ 18 O records to reconstruct ISM variability on different timescales. One further parameter, i.e., age uncertainty envelopes on records, needs to be discussed since statistical comparability between records is hampered by the lack of uncertainty information in publications and the lack of knowledge of the difference in uncertainty envelopes when using different age models. Only a few samples are dated from a stalagmite, and various age models are then employed to derive an age for each measured data point. Age modeling techniques (e.g., [82][83][84][85]) propose methods to calculate uncertainties between dated points allowing for continuous error propagation and the true uncertainty envelope of a time series to be established. This is yet to be done for the SISAL records; this paper on Indian stalagmites only considers individual age errors (uranium-thorium or radiocarbon ages) for the records.
The longest Indian record (ca. 240 ka) is from Bittoo cave, a composite record of ten stalagmites [13]. Replication of δ 18 O patterns by multiple stalagmites from the same cave greatly increases the confidence in the climatic signal. However, the record shows multiple hiatuses that limit the availability of δ 18 O values for certain climate states.
Global-scale climate events such as the Heinrich, BA, YD, 4.2 ka, and the Little Ice Age (LIA) events typically lasted for 50-1000 years. When detectable, the amplitude of δ 18 O excursions of these events is low (~0.5 to 2 ) compared to variability over orbital time scales. Identification of such events requires tight age control and high confidence in the climatic influence on the δ 18 O record. The Bittoo [13], Kalakot [44], Timta [15], and Mawmluh [16,17] cave records provide measurements of δ 18 O covering the BA and YD periods. The Bittoo and Timta cave stalagmites from north India provide better age control ( Figure 6 in Section 5.2.) than the Kalakot record. The Bittoo and Mawmluh cave records also provide δ 18 O measurements of multiple Heinrich stadials. The Valmiki cave record [50] from peninsular India covers the later part of Heinrich I, but is not replicated by a second Valmiki cave record [49] and needs to be treated with caution ( Figure S4 in Supplementary Materials). The Valmiki stalagmites are composed of aragonite rather than calcite. Under equilibrium conditions, aragonite should have δ 18 O values 0.8 more enriched than calcite at 25 • C [86]. This 0.8 offset in δ 18 O records between calcite and aragonite stalagmites has to be taken into account when comparing δ 18 O records over large spatial scales. Stalagmites composed entirely of aragonite have several benefits, such as a tendency to contain high uranium concentrations and high growth rates which provide high-resolution records with tight age control (see Reference [87]), and are being increasingly studied. However, at present, less is known about conditions governing δ 18 O in aragonitic stalagmites compared to calcitic stalagmites.
The Mawmluh cave δ 18 O records are supported by robust monitoring studies [23,88] that significantly increase confidence in the interpretation of the stalagmite δ 18 O records from this cave. However, there is lack of replication in the Mawmluh cave records [16,17,45] over short time periods and they must be treated with caution when examining millennial and shorter-time-scale events ( Figure 6 in Section 5.2.). The Mawmluh cave record covering the 4.2 ka event, KM-A [45], provides sufficient age control with low errors of ±40 to 60 years. A new stalagmite δ 18 O record from Mawmluh cave covering the same time period [89] with even lower age errors of ±13 years shows a similar onset date for the 4.2 ka event as KM-A (4.071 to 4.049 ka BP), but with one-third the δ 18 O amplitude measured in the KM-A record and with different nominal termination patterns for the 4.2 ka event. Figure 2B indicates that Sahiya [10], Wah Shikhar [11], Dandak [9], Jhumar [11], and Munagamanu [47] cave records provide δ 18 O data of all or part of the LIA beginning around 750 to 450 years BP (1200 to 1500 Common Era (CE)) [90,91]. The Sahiya cave record is characterized by tight age control (errors of ±40 years over the LIA period) and replicate δ 18 O records for significant time periods [10,12], making it a reliable climate record to examine the LIA for north India. The high-resolution Dandak and Jhumar cave records from peninsular India provide the most reliable record of the LIA for this region [9,11,43]. Although the chronology of the Jhumar cave record is not independently well constrained, its replication with the Dandak cave record from the same region provides confidence in its interpretation. With age errors of ±200 years, the Wah Shikhar cave record from the northeast provides limited age control for examining the LIA. The chronology of the Munagamanu cave record is fairly robust, but shows mixed calcite and aragonite mineralogy which hampers interpretation of the LIA δ 18 O record. Care needs to be taken with mixed calcite-aragonite samples, because the cause of variation in the δ 18 O record may be due to climatic/environmental factors, or changes in mineralogy, or a combination of both.

Regional Patterns in Speleothem Oxygen Isotope Records and Their Climatic Interpretations
To assess how well δ 18 O stalagmite reflects local rainfall changes at any given cave site, local calibration with measurements of rainfall, temperature, and δ 18 O rainfall , in addition to drip water δ 18 O, is required. However, such observations are limited in space and time. General circulation models (GCMs) can be used to aid the interpretation of δ 18 O records (e.g., [92][93][94]). Individual GCMs can produce different results because parameterization of tropical convection differs significantly among models; thus, multi-model analyses are more useful for such diagnoses [95]. Using this multi-model approach, Midhun and Ramesh (2016) analyzed output from Swing2, and found that simulations nudged with observed wind fields show better skill at reproducing the spatio-temporal pattern of rainfall amount and δ 18 O rainfall . They suggested that the improvements were due to the role of large-scale atmospheric dynamics on ISM rainfall and, hence, on δ 18 O rainfall . An increasing number of recent studies produce similar results suggesting that it is large-scale circulation rather than local rainfall amount that controls δ 18 O rainfall in the ISM region (e.g., References [96,97]). δ 18 O rainfall is further modified in its journey from the surface to the drip site in the cave and during precipitation of the stalagmite [88].
Paleoclimate data-model comparisons were used to investigate orbital-millennial time-scale controls on δ 18 O stalagmite and, hence, on δ 18 O rainfall (e.g., [98,99]). These studies suggest that large-scale circulation coupled with a largely common moisture source direction and upstream rainout can explain the pattern of δ 18 O variability in proxy records across the ISM region from Oman and into China.
Limited local calibration efforts are described further in the subsections below from the three ISM regions, i.e., north, northeastern, and peninsular India. However, past climate states are likely to have varied and circulation patterns may have been different from today. Here, we address the current level of understanding and existing debates.

North India
Paired analysis of Global Network of Isotopes in Precipitation (GNIP) δ 18 O rainfall data collected at Delhi and low-level wind trajectory patterns show that δ 18 O variability in northern India is linked to periods of strong (weak) ISM circulation [10]. Strong (weak) ISM periods are characterized by an enhanced (reduced) flux of isotopically depleted Bay of Bengal moisture and reduced (enhanced) flux of isotopically enriched Arabian Sea moisture [10]. As stalagmites are ultimately fed by rainwater, δ 18 O stalagmite reflects such changes in ISM circulation dynamics. This interpretation hinges on strong seasonality and the premise that effective precipitation is positive only during the ISM, but negative during the rest of the year [10]. However, seasonality changes in the past might have altered this climate state, thus complicating the interpretation of δ 18 O stalagmite . For example, a negative δ 18 O excursion found in multiple stalagmites from north India is interpreted to be a result of stronger winter Western Disturbances and weaker ISM circulation during all or part of the LIA (e.g., References [55,56,60]). However, the influence of Western Disturbances on stalagmite δ 18 O records is debated (see Section 5). In most scenarios, it is thought that winter season infiltration is minimal and does not contribute significantly to the δ 18 O budget of infiltrating waters [10,88].
Phase correspondence of stalagmite δ 18 O records from this region with millennial events thought to have been triggered in the North Atlantic [12,15] and the bipolar seesaw pattern observed in ice core records [13] constitute strong evidence for an impact of hemispheric-scale circulation on stalagmite δ 18 O records. Rapid positive excursions in the Bittoo stalagmite δ 18 O record corresponding to events identified in the North Greenland Ice Core Project (NGRIP) ice core record~55 ka, at a time when Antarctic ice cores showed low-amplitude warming suggests dominant Northern Hemisphere forcing at the millennial scale in this region [13]. Phase correspondence with Northern Hemisphere summer insolation (NHSI), with abrupt and high-amplitude (~4 ) negative δ 18 O excursions in the Bittoo cave stalagmite, suggests direct insolation forcing of the ISM [13]. Furthermore, the well-dated MIS 5 and MIS 3 portions of the Bittoo cave record show no visible phase difference with its counterparts in the East Asian monsoon (EAM) domain [8,100] indicating that speleothem δ 18 O variations are broadly in phase in the peripheral ISM and EAM domains.

Northeast India
Back trajectory analysis shows that the Bay of Bengal is the dominant source of moisture for northeast India [23]. Two years of observation reveal a trend toward lighter δ 18 O in the late ISM in connection with temporal variations in river runoff into the Bay of Bengal that may contribute up to 25% of observed changes in δ 18 O of precipitation in this region [23]; however, this requires further verification. Rainfall data [23] were used to validate a synthetic multi-decadal δ 18 O time series generated from an isotope-enabled general circulation model (GCM) (after Reference [101]) by Berkelhammer et al. [45]. The synthetic time series suggests that there is significant negative correlation between δ 18 O and rainfall amount only when the late ISM rainfall (October in addition to July, August, and September (JAS)) is included, suggesting that the amount effect is a result of a prolonged ISM rainfall season [45]. The studies suggest that more positive stalagmite δ 18 O values from the region may indicate early monsoon onset or early withdrawal, or both, in addition to changes in and at moisture source and transport pathways.
Instrumental data show that, in contrast to central peninsular India, rainfall amounts in northeast India are relatively unaffected by ENSO dynamics [23]. Despite this, El Niño years are marked by more positive δ 18 O values in a sub-annually resolved, 50-year-long aragonite stalagmite δ 18 O record from Mawmluh cave [14]. Back trajectory analysis [14] indicates that, during Central Pacific El Niño events, moisture transport distance to northeast India is reduced, resulting in more positive rainwater δ 18 O values; this response can be detected by the weak but significant positive correlation between this stalagmite δ 18 O and central Pacific SSTs. In addition, the δ 18 O record shows significant correlation with Pacific decadal variability.
Glycerol dialkyl glycerol tetraethers (GDGTs) [46], δ 13 C, and ice-volume-corrected δ 18 O [17] measured from stalagmites in this region give additional information on the controls on δ 18 O variation. The ice-volume-corrected δ 18 O suggests that ice volume and SST changes account for only one-fourth (~1 ) of the δ 18 O change from the glacial to deglacial, whereby the larger part is attributable to change in ISM strength [17]. Similarly, the temperature reconstruction given by the stalagmite GDGT record indicates little temperature change in this region during the YD event. This suggests that δ 18 O variation is not controlled by local temperature change, but by larger circulation changes triggered by a distal North Atlantic event [46]. The coupled analysis of δ 18 O and δ 13 C further indicates that the δ 18 O variation between the BA and into the YD may be more representative of reduced seasonality of rainfall and more proximal rainfall source during the YD associated with a weaker ISM [17].
On orbital time scales, the Umsynrang Holocene δ 18 O record shows an inverse relationship with insolation. The period of maximum rainfall and enhanced seasonality corresponds to the Holocene Thermal Maximum observed in Europe [61].

Peninsular India
Monsoon trajectory analysis [57] suggests that the Arabian Sea (and probably continental recycling) is the dominant source of moisture for the monsoon rainfall period (June, July, August, and September (JJAS)) while the Bay of Bengal, the Indian Ocean, and continental recycling are minor sources that play a role only during the remaining months. The Jhumar cave δ 18 O record overlaps with the instrumental period and shows a significant inverse relationship with a regional (18- [11]. Similarly, there is significant inverse relationship (R 2 = −0.38) between decadally averaged Akalagavi stalagmite δ 18 O (measured at annual resolution) and the regionally averaged instrumental rainfall amount data (n = 89) [51]. These two studies suggest that at least some of the variance in stalagmite δ 18 O results from changes in the amount of regional and upstream rainfall. This interpretation was also used to explain past variation in stalagmite δ 18 O from this region on millennial and orbital time scales. For example, stalagmite δ 18 O records from this region suggest that the Medieval Warm Period (MWP) was a wet period, while the early LIA was characterized by multi-decadal droughts [9,11]. A comparison of Dandak cave from peninsular India with Wah Shikhar cave located in northeast India suggests that the period from 550 to 250 years BP was marked by higher-frequency and/or amplitude break events which cumulatively generated a negative precipitation anomaly over Central India [11]. It was subsequently found that the δ 18 O record from northeast India is controlled by multiple factors other than the amount effect [23,45]. The Kotumsar δ 18 O record similarly shows that there was a gradual decrease in the amount of rainfall from 8500 to 7300 years BP followed by an increasing trend from 7300 to 5600 years BP [57]. A very limited number of records cover ISM dynamics in peninsular India during brief time windows older than the Holocene [49,50,54]. An aragonite stalagmite record from Valmiki cave indicates wetter climate during Termination 1a (~14,800 years BP) [50] and during the later phase of Heinrich event 1 [50], pending replicate measurements and verification.

Discussion
The available stalagmite δ 18 O data in SISAL show that regional ISM responses differ in terms of sensitivity and timing. Better understanding of regional dynamics causing stalagmite δ 18 O variation allows examination of specific aspects of the monsoon such as rainfall amount, source and path changes, and changes in length of the season. Such regional paleoclimate records provide valuable information to test the ability of climate models to predict changes in the ISM in response to different forcing mechanisms and climate states. Based on the availability of stalagmite records from India, the following discussion sections examine regional ISM variability in response to volcanic/solar forcing during the LIA, North Atlantic, and orbital-insolation drivers.

The Little Ice Age (LIA)
Temperature reconstructions across the globe generally indicate a cooling trend beginning around 750-450 BP (1200-1500 CE) (interspersed with periods of warmth) and continuing into the nineteenth century that is referred to as the Little Ice Age [90,91]. Solar and/or volcanic forcings coupled with ocean-atmosphere feedbacks were used to explain the LIA cooling trend (e.g., References [102,103]). Paleoclimate studies used stalagmite δ 18 O records to understand ISM variation during the LIA. Rehfeld et al. [104] used the Akalagavi [51] and Dandak [9] records to examine the relationship between ISM and EAM using complex networks. Chen et al. [105] used the Dandak [9] and Dharamjali [56] records along with a number of other proxy records across the ASM region to suggest a "wet-North and dry-South" pattern during the LIA. A similar conclusion was reached by Dixit and Tandon [106], who use several proxy records from the ISM region to discuss the hydroclimate of the Holocene. This section examines the LIA period using stalagmite δ 18 O records available in SISAL_v1.
The precise onset and culmination of the LIA is still debated [107]. Here, we will nominally use the regionally demarcated LIA period from 370-70 BP (1580-1880 CE) [91]. The Sahiya cave δ 18 O record [10] shows the best age control over this time period ( Figure 4); however, the amplitude of δ 18 O variation is low (0.5 ). Z-scores calculated for the Sahiya cave δ 18 O record ( Figure 5) indicate that there is a distinct positive δ 18 O anomaly over the LIA period in this record covering the last 2000 years. The Wah Shikhar and Jhumar cave records show higher-amplitude δ 18 O changes (1-2 ) over the LIA period, but with limited age control.  [10], Wah Shikhar [11], Jhumar [11], and Dandak [9] cave records are shown along with their U-Th age errors.  [10]. Age in years CE is given on the x-axis. The y-axis gives the δ 18 O in ‰VPDB. The LIA period is nominally demarcated from 1580 to 1880 CE [91].
These records suggest regional differences in responses to circulation changes during the LIA (Figures 3 and 4). While ISM rainfall in peninsular India was reduced, northeast India experienced  [10], Wah Shikhar [11], Jhumar [11], and Dandak [9] cave records are shown along with their U-Th age errors.   [10], Wah Shikhar [11], Jhumar [11], and Dandak [9] cave records are shown along with their U-Th age errors. These records suggest regional differences in responses to circulation changes during the LIA (Figures 3 and 4). While ISM rainfall in peninsular India was reduced, northeast India experienced  [10]. Age in years CE is given on the x-axis. The y-axis gives the δ 18 O in VPDB. The LIA period is nominally demarcated from 1580 to 1880 CE [91].
These records suggest regional differences in responses to circulation changes during the LIA (Figures 3 and 4). While ISM rainfall in peninsular India was reduced, northeast India experienced an increase in monsoon season length and changes in moisture source and path (see Section 4). The Sahiya record from north India suggests that LIA dynamics did not produce significant changes in ISM rainfall δ 18 O. However, three lines of evidence suggest that further work is required in the north Indian region.

1.
Other types of records from the north Indian region (such as lake core records) suggest changes in ISM rainfall amount in north India during the LIA (e.g., [106] and references therein).

2.
If changes in circulation during the LIA are a result of active/break dynamics as suggested by Dixit and Tandon [106], the northeast and north Indian cave records should respond with δ 18 O excursions in the same direction as a result of stronger Bay of Bengal branch of precipitation.

3.
If changes in circulation during the LIA are a result of a weaker ISM and stronger Western Disturbances as suggested by Kotlia et al. [60] and Sanwal et al. [56], then there needs to be unambiguous evidence of Western Disturbances influencing cave stalagmite δ 18 O records (either through seasonal drip water δ 18 O changes or cave ventilation changes) at present or in the past (e.g., through investigation in spatially separated stalagmite records and climate modeling).

North Atlantic Forcing
Ice-rafted debris deposited during past glacial times in the North Atlantic region indicate the release of large pulses of fresh water affecting the thermohaline circulation and causing global climate fluctuations during so-called Heinrich stadials [108,109]. The YD stadial (12,679 years BP to~11,550 a BP) occurred abruptly at the end of the BA interstadial and is thought to have been caused by a sudden decrease in the thermohaline circulation caused by fresh water from the North American region during the current interglacial [110][111][112][113]. Arabian Sea ocean sediment records of upwelling intensity [114][115][116] are consistent with reduction in ISM during these Heinrich stadials and the YD [117]. Pausata et al. used an isotope-enabled atmospheric GCM to show that a sudden increase in the sea ice extent in the North Atlantic region during a Heinrich stadial could lead to cooling of the Northern Hemisphere, reduced precipitation over the Indian basin, and weakening of the ISM. The precipitation was isotopically heavier over India at this time [99].
The Bittoo cave record [13] is characterized by more positive δ 18 O values during nearly all stadials compared to interstadials, consistent with the modeling results given by Pausata et al. [99]. Unlike the LIA, this pattern of more positive δ 18 O is replicated by other shorter records from north and northeast India [15][16][17]44] (Figure 3). The Bittoo and Mawmluh cave records suggest that Heinrich stadials are responsible for higher-amplitude changes in the ISM than the YD stadial in north and northeast India ( Figure 6). However, the transition into and out of the Heinrich stadials is not as distinct as the transition into the YD at~12.7 ka in the north Indian Bittoo [13], Timta [15], and Kalakot [44] records ( Figure 6). The Kalakot cave record does not show the negative excursion for the BA seen in the other records. The magnitude of change in δ 18 O from the BA to the YD period is~2 in this region. Though the northeast Indian cave records indicate the BA-YD excursions with tight age control, the δ 18 O records from Mawmluh cave do not replicate well with each other over the BA-YD transition. The magnitude of δ 18 O transition from BA to YD is lower than in the north Indian cave records at~1 . The Younger Dryas (YD) and Heinrich events 1 and 2 [118] are indicated by yellow bars. Bölling-Allerød (BA) is indicated by a grey bar. The BA-YD transition is marked at 12.8 ka BP in the figure (GISP2 [119]). Bittoo [13], Kalakot [44], Timta [15], and Mawmluh [16,17] records are shown along with their U-Th age errors.

Orbital Forcing
Battisti et al. [19] used an isotope-enabled Atmospheric GCM to examine the differences between the high and low summer insolation phases (corresponding to 218 and 207 ka BP, respectively) with a 100-W/m 2 difference between the two at 30° N for June-July-August. They showed δ 18 O difference between the high and low insolation phases of between 4 to 6‰ in north and northeast Indian region. The Bittoo cave record [13] shows a ~6‰ shift in δ 18 O between the low insolation phase of MIS 6 and the high insolation phase of MIS 5 (Figure 7). Similarly, the 30-ka-long Mawmluh [16] cave record shows a ~6‰ difference between the low insolation phase of MIS 2 and the high insolation phase of MIS 1. This suggests that models capture the large-amplitude changes in δ 18 O on orbital time scales seen in stalagmite δ 18 O records from north and northeast India. Furthermore, the Mawmluh cave record of ~30 ka shows no visual phase difference with the Bittoo cave record with similar magnitude of δ 18 O change, strongly suggesting that, on orbital time scales, ISM variation is in phase with solar insolation in north and northeast India. These results support the argument of direct insolation forcing of ISM change [13]. More enriched δ 18 O during glacial periods MIS 4 and MIS 2 in comparison to interglacial periods MIS 3 and MIS 1 suggests that ice volume changes influence the ISM, supporting a previous study from Xiabailong cave from the ISM Figure 6. SISAL_v1 ISM stalagmite δ 18 O records covering millennial events over the last deglaciation. The Younger Dryas (YD) and Heinrich events 1 and 2 [118] are indicated by yellow bars. Bölling-Allerød (BA) is indicated by a grey bar. The BA-YD transition is marked at 12.8 ka BP in the figure (GISP2 [119]). Bittoo [13], Kalakot [44], Timta [15], and Mawmluh [16,17] records are shown along with their U-Th age errors.

Orbital Forcing
Battisti et al. [19] used an isotope-enabled Atmospheric GCM to examine the differences between the high and low summer insolation phases (corresponding to 218 and 207 ka BP, respectively) with a 100-W/m 2 difference between the two at 30 • N for June-July-August. They showed δ 18 O difference between the high and low insolation phases of between 4 to 6 in north and northeast Indian region. The Bittoo cave record [13] shows a~6 shift in δ 18 O between the low insolation phase of MIS 6 and the high insolation phase of MIS 5 (Figure 7). Similarly, the 30-ka-long Mawmluh [16] cave record shows a~6 difference between the low insolation phase of MIS 2 and the high insolation phase of MIS 1. This suggests that models capture the large-amplitude changes in δ 18 O on orbital time scales seen in stalagmite δ 18 O records from north and northeast India. Furthermore, the Mawmluh cave record of~30 ka shows no visual phase difference with the Bittoo cave record with similar magnitude of δ 18 O change, strongly suggesting that, on orbital time scales, ISM variation is in phase with solar insolation in north and northeast India. These results support the argument of direct insolation forcing of ISM change [13]. More enriched δ 18 O during glacial periods MIS 4 and MIS 2 in comparison to interglacial periods MIS 3 and MIS 1 suggests that ice volume changes influence the ISM, supporting a previous study from Xiabailong cave from the ISM region [120]. While the Bittoo and Mawmluh cave records provide much needed information regarding long-term ISM forcings, the hiatuses in the record prevent comprehensive analysis of the relative dominance of different forcing mechanisms. The Umsynrang record [61] from northeast India is the only record that covers the entire Holocene from India (but is not in SISAL_v1). The record shows a peak at ~9 ka BP with progressive increase in δ 18 O of ~1‰ across the Holocene matching modeling studies by LeGrande and Schmidt [18] and Battisti et al. [19], which calculate a 1‰ increase in rainfall δ 18 O associated with a 27-W/m 2 decrease in summer insolation over the Holocene. The records from Figure 8 cover parts of the Holocene. The Mawmluh cave record from northeast India similarly shows an increasing δ 18 O trend with decreasing insolation; however, it peaks at ~8.5 ka BP. The Sahiya δ 18 O cave record [12] from north India also follows the insolation curve during its 5000 years of growth. The peninsular Indian cave record is formed of two stalagmites from Kotumsar cave (KOT [57] and NK record given in the Supplementary Materials of this paper, Figures S1-S3 and Tables S1,S2) and the coupled Dandak [9] and Jhumar [11] cave records; however, the long-term trend seen in the other records is not as clear from this region.  [13] and Mawmluh [16] cave records are shown along with their U-Th age errors. Hiatuses in the Bittoo cave record are marked. Marine isotope stages (MIS) are demarcated by grey and white bars. The insolation curve in W/m 2 at 20 • N is shown in blue [121].
The Umsynrang record [61] from northeast India is the only record that covers the entire Holocene from India (but is not in SISAL_v1). The record shows a peak at~9 ka BP with progressive increase in δ 18 O of~1 across the Holocene matching modeling studies by LeGrande and Schmidt [18] and Battisti et al. [19], which calculate a 1 increase in rainfall δ 18 O associated with a 27-W/m 2 decrease in summer insolation over the Holocene. The records from Figure 8 cover parts of the Holocene. The Mawmluh cave record from northeast India similarly shows an increasing δ 18 O trend with decreasing insolation; however, it peaks at~8.5 ka BP. The Sahiya δ 18 O cave record [12] from north India also follows the insolation curve during its 5000 years of growth. The peninsular Indian cave record is formed of two stalagmites from Kotumsar cave (KOT [57] and NK record given in the Supplementary Materials of this paper, Figures S1-S3 and Tables S1,S2) and the coupled Dandak [9] and Jhumar [11] cave records; however, the long-term trend seen in the other records is not as clear from this region.

Future Directions
Two decades of stalagmite δ 18 O-based reconstructions of the ISM from India showed that past variability of the ISM lies beyond the boundaries suggested by the short instrumental records. Solar insolation changes, dynamics in the North Atlantic region, and Pacific Ocean SSTs affect the ISM on different time scales. Models are able to replicate the large-amplitude δ 18 O changes seen in the limited stalagmite records over orbital time scales; however, further work is required to test models against the increasing number of millennial-and shorter-time-scale events now available from the ISM region. Systematic comparison of stalagmite records with models is an effective test of the ability of individual models to predict future changes in the ISM [2]. The significant advances made in this field indicate fruitful future directions of research, including the following: 1. The use of uranium-thorium dating methods coupled with the strong seasonality of the monsoon allow for high-resolution records with high dating precision. This allows for precise age control on the timing of events and, in turn, gives significant insight into the pathway of distal forcings on the ISM. However, this requires consistency in age model creation, which will be an important next step for the SISAL Working Group. 2. There is less information available on multi-decadal variability of the ISM and on the frequency of variability within different climate states. The age control provided by stalagmites coupled with high growth rates allows for the generation of more information on this variability through different methods of spectral analysis. This was explored only to a limited extent in the current records, only to conclude with a range of plausible mechanisms. Increased interaction between the paleoclimate and atmospheric sciences communities will be required to narrow down the plausible physical mechanisms and pathways of forcings. 3. Databases such as SISAL allow examination of regional patterns in records highlighting the sub-regional differences in responses of the ISM to forcings. At present, this is somewhat handicapped by the lack of long-term rainfall δ 18 O and cave monitoring studies. While δ 18 O gives information on large-scale circulation changes, other stalagmite-based records like trace-element ratios (such as Mg/Ca and U/Ca) can form powerful paleo-aridity indicators  [10,12], Mawmluh [45], Kotumsar (KOT [57], NK (Supplementary Materials)), Dandak [9], and Jhumar [11] cave records are shown along with their U-Th age errors. The insolation curve in W/m2 at 20 • N is shown in blue [121].

Future Directions
Two decades of stalagmite δ 18 O-based reconstructions of the ISM from India showed that past variability of the ISM lies beyond the boundaries suggested by the short instrumental records. Solar insolation changes, dynamics in the North Atlantic region, and Pacific Ocean SSTs affect the ISM on different time scales. Models are able to replicate the large-amplitude δ 18 O changes seen in the limited stalagmite records over orbital time scales; however, further work is required to test models against the increasing number of millennial-and shorter-time-scale events now available from the ISM region. Systematic comparison of stalagmite records with models is an effective test of the ability of individual models to predict future changes in the ISM [2]. The significant advances made in this field indicate fruitful future directions of research, including the following: 1.
The use of uranium-thorium dating methods coupled with the strong seasonality of the monsoon allow for high-resolution records with high dating precision. This allows for precise age control on the timing of events and, in turn, gives significant insight into the pathway of distal forcings on the ISM. However, this requires consistency in age model creation, which will be an important next step for the SISAL Working Group.

2.
There is less information available on multi-decadal variability of the ISM and on the frequency of variability within different climate states. The age control provided by stalagmites coupled with high growth rates allows for the generation of more information on this variability through different methods of spectral analysis. This was explored only to a limited extent in the current records, only to conclude with a range of plausible mechanisms. Increased interaction between the paleoclimate and atmospheric sciences communities will be required to narrow down the plausible physical mechanisms and pathways of forcings.

3.
Databases such as SISAL allow examination of regional patterns in records highlighting the sub-regional differences in responses of the ISM to forcings. At present, this is somewhat handicapped by the lack of long-term rainfall δ 18 O and cave monitoring studies. While δ 18 O gives information on large-scale circulation changes, other stalagmite-based records like trace-element ratios (such as Mg/Ca and U/Ca) can form powerful paleo-aridity indicators providing information on local changes in rainfall. This not only provides information on local climate change, but also on the sub-regional ISM response to distal forcings. Quantitative reconstruction of rainfall using δ 18 O was attempted [122], and this approach is worth testing over modern instrumental time scales. A recent study suggests that calcium isotope ratios can also be used for quantitative reconstruction of rainfall [123].
These steps should significantly improve the predictability of ISM variability, which is the ultimate aim of such paleoclimate investigations.