Journal of Paleolimnology

, Volume 60, Issue 3, pp 445–460 | Cite as

A 1600-year record of human impacts on a floodplain lake in the Mississippi River Valley

  • Richard B. Brugam
  • Samuel E. Munoz
Open Access
Original paper


In North America, land use practices of the last two centuries have strongly influenced aquatic communities and freshwater quality, but the impacts of prehistoric land use on freshwater resources remain poorly documented. Here we investigate the influence of prehistoric and historical land use on Horseshoe Lake, Illinois, USA, an oxbow lake in a floodplain of the Mississippi River that is adjacent to Cahokia, the largest prehistoric indigenous population center north of Mexico. Diatom assemblages from Horseshoe Lake’s sedimentary record track shifts in aquatic environmental conditions over the last ca. 1600 years. During the period of prehistoric population growth and agricultural intensification associated with Cahokia’s emergence (ca. 600–1200 CE), the relative abundance of Aulacoseira granulata—a planktonic diatom associated with shallow eutrophic lakes—increased. Following the abandonment of Cahokia in the 14th century CE, the diatom flora of the lake shifted from planktonic Aulacoseira taxa to the epiphytic taxa Cocconeis and Gomphonema. This shift in diatom assemblages is consistent with a reduction of nutrient inputs to the lake and/or reduced fishing pressure as prehistoric populations abandoned the area. Following the intensification of historic settlement after 1800 CE, diatom assemblages shift to epipelic species of small Staurosira and Fragilaria, indicating a reduction in aquatic macrophytes and increased turbidity. Our results document prehistoric indigenous impacts on a freshwater system beginning nearly 1000 years before European colonization of the Americas and demonstrate the antiquity of human impacts on freshwater resources in North America.


Horseshoe lake Cahokia Mississippian Floodplain Oxbow lake Diatoms Eutrophication 


Human activities exert a fundamental control on aquatic ecosystems and freshwater quality (Smith et al. 1999; Jackson et al. 2001; Dudgeon et al. 2006). Managing freshwater resources to improve water quality depends, in part, on understanding the sensitivity of aquatic ecosystems to environmental changes that occurred in the recent past and in prehistory (Smol and Stoermer 2010). At sites across North America, instrumental datasets and paleolimnological records document declines in freshwater quality beginning in the 19th and 20th centuries because of enhanced nutrient loading and pollutants (Cumming et al. 1992; Hall et al. 1997; Carpenter et al. 1998; Smol 2010). Despite the abundance of evidence documenting recent historical degradation of freshwater resources, paleolimnological records of prehistoric human impacts on aquatic ecosystems in North America are scarce. In one prominent set of studies, Ekdahl et al. (2004, 2007) demonstrated that an Iroquoian settlement around a small lake in southern Ontario, Canada caused a shift to more eutrophic conditions in the 13th century CE. Yet, whether prehistoric human impacts on freshwater ecosystems were widespread in North American remains unclear. Paleolimnological evidence from South and Central America demonstrates that indigenous populations in those regions influenced freshwater ecosystems thousands of years before European colonization (Haberyan and Horn 2005; Slate et al. 2013; Bush et al. 2016), but were similar impacts north of Mexico confined to the relatively recent past? Prehistoric populations in some areas of eastern North America, particularly in the Midwest and Southeast, were large, sedentary, and cultivated a variety of plant foods for thousands of years prior to European colonization (Smith 2009; Milner 2005), but their influence on freshwater ecosystems remains poorly documented.

In this study, we present diatom assemblages in a sedimentary record from Horseshoe Lake, Illinois (USA)—an oxbow lake that is adjacent to Cahokia, the largest prehistoric indigenous settlement north of Mexico. Because of its size and cultural prominence, Cahokia is one of the most intensively studied archaeological sites in North America, and its demographic and land use history are well-documented (Pauketat and Lopinot 1997; Milner 1998; Simon and Parker 2006; Munoz et al. 2014). We use diatom assemblages from Horseshoe Lake to examine the impacts of prehistoric populations on freshwater quality and ecosystems. We show that this large lake has been highly sensitive to human activities over the past 1600 years and exhibited signs of cultural eutrophication as early as 600 CE.

Study area

Horseshoe Lake is a large (860 ha) and shallow (3 m) oxbow lake near Saint Louis, Missouri (Fig. 1). Horseshoe Lake is in a wide section of the middle Mississippi River’s floodplain known as the ‘American Bottom’ (Milner 1998). The lake formed from a neck cut-off of the Mississippi River about 1800 years ago and developed plugs along its arms that limited its hydrological connectivity with the main channel (Hajic 1993). Several small streams originating from the loess-capped uplands to the east drain into Horseshoe Lake directly or via adjacent lakes and wetlands. In the late 19th and 20th centuries, many wetlands of the American Bottom were drained and artificial levees were constructed along the Mississippi River to encourage development and manage flood risk (Hajic 1993). Prior to the establishment of these artificial levees, high-magnitude flood events of the Mississippi River periodically deposited sediment into Horseshoe Lake (Munoz et al. 2014, 2015). Today, Horseshoe Lake is managed by the Illinois Department of Natural Resources for fishing and waterfowl hunting, and the lake’s watershed contains a mix of agricultural, industrial, and urban land use.
Fig. 1

Map of the study area in the middle Mississippi River Valley, showing: a locations of sediment cores collected from Horseshoe Lake, and Mississippian population centers (after Pauketat and Lopinot 1997), and historic (ca. 1800 CE) positions of the Mississippi River, floodplain lakes, and streams (modified from Milner 1998); b location of the study area within eastern North America, with major Mississippian population centers and area of Mississippian influence (ca. 1000–1600 CE)

During the Late Woodland (ca. 400–1050 CE) and Mississippian (ca. 1050–1350 CE) archaeological periods, the floodplain and uplands around Horseshoe Lake were populated by indigenous peoples who hunted, fished, and cultivated a variety of domesticated plant foods (Fig. 2). During the Late Woodland Period, inhabitants of the area incorporated the cultivation of indigenous seed crops of the Eastern Agricultural Complex (EAC; Smith 1987), including goosefoot (Chenopodium berlandieri), sumpweed (Iva annua), knotweed (Polygonum erectum), little barley (Hordeum pusillum), and sunflower (Helianthus annuus) into a mixed and mobile subsistence strategy (Johannessen 1984; Fortier and Jackson 2000; Koldehoff and Galloy 2006). Late Woodland peoples began cultivating maize (Zea mays subsp. mays) in conjunction with indigenous seed crops of the EAC after ca. 800 CE (Milner 1998; Simon and Parker 2006), although hunting, fishing, and foraging for wild plant foods remained important into the Mississippian Period (Fritz 1990; Lopinot 1997). During the subsequent Mississippian Period, beginning around 1050 CE, Cahokia emerged as a major political, economic, and religious center, drawing thousands of people from across the region into a hierarchically-organized, sedentary, and predominately agricultural lifestyle (Milner 1998). The area’s population size, including Cahokia and neighboring settlements, reached its height around 1200 CE, followed by a period of sociopolitical dissolution and gradual out-migration until the area was almost completely abandoned by 1350 CE. Following Cahokia’s dissolution, the area was sparsely occupied by various indigenous groups until around 1700 CE, when Euro-American farmers, fur traders, and missionaries first settled the area (Esarey 1984; Brown and Sasso 2001). Populations increased rapidly after 1800 CE as Euro-American peoples settled the area, initially establishing farms and later industries along the Horseshoe Lake’s shoreline and its watershed (Esarey 1984; Karthic et al. 2013). Given the long and well-documented demographic and land use history of the Horseshoe Lake area, we analyzed diatom assemblages in a lake’s sedimentary record to examine the influence of prehistoric and historic land use on the lake’s ecology. We hypothesize that prehistoric occupation of the lake and its watershed shifted the lake towards more eutrophic conditions, and that nutrient inputs declined following the abandonment of Cahokia.
Fig. 2

Timeline of cultural, land use, and demographic change in the study area: a archaeological periods of the American Bottom after Fortier et al. (2006); b subsistence strategies modified from Simon and Parker (2006), where EAC denotes the ‘Eastern Agricultural Complex’, a set of plant foods domesticated in eastern North America (see text for details); c timing of important cultural and demographic events; d human population size and density in the study area (prehistoric population levels after Milner (1998), with archaeological hiatuses from Fortier et al. (2006) representing very sparse occupations); historical populations for the study area are based on the historical census

Materials and methods

Field sampling

Four sets of sediment cores were taken across the apex of Horseshoe Lake using a Livingston piston corer in May 2012 (Fig. 1). Here, we analyze the core collected from the in-filling former thalweg of the Mississippi River (HORM12-4; 90.081279°W, 38.704767°N; water depth 1.09 m). This 578-cm-long sediment core was split longitudinally, described, photographed, sectioned into 1 cm increments and stored in Whirlpak™ bags in a refrigerator. The core analyzed in this study is the same core as the one used in the paleoecological (fossil pollen, stable carbon isotopes) and paleohydrological (grain size) reconstructions described by Munoz et al. (2014, 2015), and additional details on this sedimentary record can be found in those publications.

Chronological control

The age model for the core is the same as that used by Munoz et al. (2014), and is a modified smooth spline developed using Clam 2.2 (Blaauw 2010). The age model is based on 9 accelerator mass spectrometry 14C dates on terrestrial macrofossils, calibrated using the IntCal13 calibration curve (Reimer et al. 2013). The rise in Ambrosia pollen found by Munoz et al. (2014) was assigned the date of 1825 ± 25 CE based on McAndrews (1988). This differs slightly from the 1809 date previously assigned to the Ambrosia rise by Karthic et al. (2013) for a 73-cm-long core from Horseshoe Lake (Fig. 1). Additional details of this sediment core’s age model can be found in Munoz et al. (2014).

Diatom preparation and identification

Diatom samples were made at approximately 8-cm intervals in the core except between 64.5 and 80.5 cm where the sampling interval was 2 cm. In some core levels there were no diatom microfossils preserved. These levels were scanned for diatoms and discarded.

Diatom microfossils were prepared from the Horseshoe Lake core using a method similar to Moos et al. (2005). Approximately 0.5 gm of sediment was placed in a glass centrifuge tube. The organic matter in the sample was removed from the sediment using a solution of 50% HNO3 and 50% H2SO4. The solution was heated to 90 °C for 4 h using a block heater. The samples were removed from the block heater and allowed to cool and settle for 24 h. The acid was aspirated off and replaced with de-ionized water. This process was repeated every 24 h until the remaining acid was removed. Subsamples of the diatom suspension were dried on coverslips and mounted in Naphrax™ mounting medium, and diatoms were identified using a Leitz Laborlux microscope with a 100× oil immersion lens. Diatom preservation in the Horseshoe Lake core was highly variable so numbers counted varied from a low of 68 at 144.5 cm depth to a high of 524 at 725 cm. Diatom identification followed Siver and Hamilton (2011), Kramer (2000, 2002), Lange-Bertalot (2001), and Siver et al. (2007).

Statistical analysis

Constrained incremental sums of squares cluster analysis (CONISS)

Diatom assemblages from the Horseshoe Lake core were compared using the computer program CONISS, which performs a stratigraphically constrained cluster analysis (Grimm 1992). In contrast with ordinary cluster analysis, only stratigraphically adjacent clusters are merged. The dissimilarity metric used was chord distance.

Non-metric multidimensional scaling (NMDS)

In contrast to CONISS, Non-metric Multidimensional Scaling (NMDS) is not constrained by depth, and instead compares samples independently of depth. Minchin (1987) showed that this non-parametric method is relatively robust to variations in community models and is an appropriate choice for most ecological applications. Paleolimnologists have more frequently used Detrended Correspondence Analysis (DCA) to ordinate fossil diatoms from cores. DCA assumes that diatom taxa are organized in unimodal response functions along environmental gradients in a bell-shaped pattern. The technique is subject to an “Arch Effect,” a computational artifact in which the second ordination axis is a function of the first. DCA attempts to account for this effect by “detrending” or compressing the high and low values on the first axis. NMDS is a non-parametric method that assumes no particular response function (Minchin 1987), thereby avoiding the “Arch Effect” and modifications of ordination axes. NMDS was used by Schroeder (2016) to study the human impacts on diatom assemblages in a core from an Ohio reservoir.

Non-metric multidimensional scaling (NMDS) ordination was performed on diatom taxa using PC-Ord version 6.01 (Peck 2010). Taxa are ordinated by calculating the weighted average of the coordinates of samples containing them. This weighted average indicates which taxa are important in controlling the location of particular samples in ordination space. In our analysis, we used 24 taxa with abundances in at least 1 sample of > 5% (Table 1). This number of taxa is smaller than the total number of taxa in the dataset because many taxa from the total dataset were too rare for inclusion in the statistical analysis (Peck 2010). Members of the genus Gomphonema were summed. We used all 33 depths from the Horseshoe Lake core and used the Bray–Curtis distance metric.
Table 1

Taxa used in NMDS ordination, listed in order of abundance

Taxon number

Species name



Aulacoseira granulata

(Ehrenb.) Simonsen


Nitzschia amphibia



Fragilaria vaucheriae

(Kütz.) Petersen


Staurosira construens var. venter

(Ehrenberg) Hamilton 


Aulacoseira distans

(Ehrenberg) Simonsen


Aulacoseira ambigua

(Grunow) Simonsen


Stephanodiscus minutus



Amphora ovalis

(Kütz.) Kütz.


Sum of Gomphonema species



Cocconeis placentula



Rhopalodia gibba

(Ehrenberg) O. Müller


Aulacoseira muzzanensis

(F.Meister) Krammer


Navicula lanceolata

(C.Agardh) Ehrenb.


Craticula cuspidata

(Kütz.) D.G. Mann


Unidentified Aulacoseira



Lyrella hennedyi

(W.Smith) Stickle & D.G. Mann


Aulacoseira granulata var. angustisssima

(O.Müll.) Simonsen


Cyclotella meneghiniana



Unidentified Pinnularia



Synedra rumpens



Unidentified Navicula



Surirella linearis

W. Smith 1853


Staurosira construens

Ehrenberg 1843


Sellaphora pupula


Taxon numbers are keyed to Fig. 7


Diatom assemblages are present throughout most of Horseshoe Lake’s sedimentary record (Figs. 4, 5), but we encountered poor diatom preservation in sections that were identified by Munoz et al. (2015) as sediment deposited during major flood events of the Mississippi River (Fig. 3). Here, we use sections in which diatom assemblages are well preserved to interpret limnological changes at Horseshoe Lake over the last 1600 years. Stratigraphically constrained cluster analyses based on CONISS divides the diatom assemblages from Horseshoe Lake into 4 zones numbered HORMD1 through HORMD4 (Fig. 3).
Fig. 3

Summary diagram of diatom microfossils from the Horseshoe Lake core. Diatom taxa are grouped by life form. The dendrogram shows the stratigraphically constrained incremental sums of squares (CONISS) cluster analysis used to determine diatom zone boundaries. Thin black horizontal lines indicate zone boundaries combining diatom zones and cultural periods (after Fortier et al. 2006). Gray rectangular bars indicate core regions where diatoms are not preserved. Flood deposits (blue rectangles), sediment grain size, stable carbon isotopes (δ13Corg) and a core photograph from Munoz et al. (2015) are shown in the panels to the left

Zone HORMD1 (393 cm, 390 CE)

Zone HORMD1 contains only one sample. Diatom assemblages in this sample are dominated by Aulacoseira distans (79%), a taxon that is not present in any other sample (Fig. 4). There are small percentages of Cyclotella meneghiniana and Stephanodiscus minutus. The unique diatom assemblage in this zone reflects conditions prior to intensive prehistoric settlement and/or the aquatic ecosystem shortly after the lake’s formation, but because it contains only one sample it is not used in our interpretation of the Horseshoe Lake record (below).
Fig. 4

Planktonic diatom microfossils from the Horseshoe Lake core. Thin black horizontal lines indicate diatom zone boundaries. Black rectangles on the left column (labeled “Diatoms absent”) and gray bars indicate core regions where diatoms are not preserved

Zone HORMD2 (345–45 cm, 610–1400 CE)

Core zone HORMD2 is separated from zone HORMD1 by 56 cm of sediment without identifiable diatom microfossils. This zone is also interrupted from 225 to 185 cm by another region with poor diatom preservation. After this interruption, diatom accumulation continues with the same assemblage that existed before the hiatus. That assemblage is dominated by Aulacoseira granulata (Fig. 4), a planktonic species of shallow, alkaline lakes (Brugam 1993), with abundances varying from 15 to 81%. A. granulata is accompanied by another variety of the same species, A. granulata var. angustissima. Other planktonic species that are present are Aulacoseira muzzanensis and Stephanodiscus minutus. These planktonic species are accompanied by a wide variety of epiphytic species at low abundances (Fig. 5). The most abundant of these are Cocconeis placentula and Amphora ovalis. Both of these species are moderately abundant at deeper core levels, but decline in abundance at shallower core depths until they nearly disappear at 250 cm (990 CE).
Fig. 5

Epiphytic and epipelic diatom microfossils from the Horseshoe Lake core. Thin black horizontal lines indicate diatom zone boundaries. Black rectangles on the left column (labeled “Diatoms absent”) and gray bars indicate core regions where diatoms are not preserved

Zone HORMD3 (145–57 cm, 1400–1780 CE)

Zone HORMD3 begins between 169 cm (1310 CE) and 145 cm (1410 CE) with a decline in A. granulata from 58.9 to 2.9% (Fig. 4) and a rise in total epiphytic taxa from 11.2 to 92.6% (Figs. 4, 5). Cocconeis placentula and Amphora ovalis return in higher abundances than in diatom zone HORMD2. This change represents a major shift in diatom assemblages at Horseshoe Lake from planktonic taxa to epiphytic ones (Fig. 3). The sample from 145 cm is unusual, with a high abundance of Nitzschia amphibia. Just after this sample (145–97) there is another hiatus in diatom preservation. After the hiatus, accumulation of diatoms continues with an assemblage that has high epiphytic percentages and lower planktonic species percentages (Fig. 3). This zone contains a peculiar diatom species—Lyrella hennedyi (Fig. 4)—which reaches 12.8% at 57 cm (1780 CE). This is a species generally found epipelically in marine sandy environments (Mann and Stickle 1993). Other, more common epipelic species like Staurosira construens var. venter and Staurosira vaucheriae begin to appear at this level.

Zone HORMD4 (57–1 cm, 1810–2010 CE)

This zone begins with a layer without diatom fossils. The later, fossil-containing layers have more epipelic taxa (S. construens var. venter, S. construens and Fragilaria trigona; Fig. 5). L. hennedyi percentages, however, are reduced. Cyclotella meneghiniana appears in abundance for the first time. Epiphytic taxa decline and are replaced by epipelic taxa (Fig. 5).

Ordination results

For diatom assemblages in Horseshoe Lake, NMDS ordination differentiates samples before the abandonment of Cahokia ca. AD 1350, from those deposited afterwards (Fig. 6). This result agrees with the CONISS results (Fig. 3). Samples prior to the abandonment of Cahokia have low scores on Axis 1, whereas samples from after the prehistoric abandonment of the region score higher on Axis 1. The groupings of diatom assemblages were highly significant (p = 0.001) using Analysis of Similarities (ANOSIM). The overlap among pre- and post-abandonment samples implies that shifts in communities were gradual, similar to the lagged community response observed in a reservoir in Ohio (Schroeder et al. 2016). In Horseshoe Lake, we also observe a lagged community response following historic Euro-American settlement, although the most recent samples score highly on Axis 2 (Fig. 6).
Fig. 6

Non-metric multidimensional scaling (NMDS) ordination of diatom assemblages at various core depths

The weighted averages of taxa provide insight into the distribution of individual samples, with Axis 1 defined by taxa that were abundant prior to and immediately after Cahokia’s abandonment, and Axis 2 defined by taxa that have dominated diatom assemblages since historic Euro-American settlement (Fig. 7). Planktonic taxa (Aulacoseira granulata and Stephanodiscus minutus) are most abundant in samples with Axis 1 coordinates < 0 (pre-abandonment). Epiphytic taxa (Amphora ovalis, Cocconeis placentula, Gomphonema spp. and Navicula lanceolata) are > 0 (post-abandonment). Taxa abundant following historic Euro-American settlement (Staurosira construens, S. construens var. venter, Cyclotella meneghiniana) occur at high Axis 2 values.
Fig. 7

Diagram of weighted averages of diatom species in ordination space. Numbers are keyed to taxa names in Table 1


The diatom assemblages from Horseshoe Lake’s sedimentary record are divided into three main zones, as HORMD1 contains only one sample: (1) During the period of Cahokia’s emergence, HORMD2 (610–1400 CE) is dominated by planktonic taxa – especially A. granulata; (2) Following Cahokia’s abandonment, HORMD3 (1400–1780 CE) assemblages shift from plankton to epiphytic taxa); (3) With intensification of Euro-American settlement, diatom assemblages in HORMD4 (1810–2010 CE) shift towards epipelic taxa.


Diatoms in floodplain lakes

Sediments, diatoms, and other materials deposited in oxbow lakes are sourced from the lake itself (autochthonous) or its watershed (allochthonous), but during flood stages the main river channel may also deposit material in the lake (Toonen et al. 2012; Bhattacharya et al. 2016), which represents an extra-local source of allochthonous material. In a previous study of Horseshoe Lake’s sedimentary record, Munoz et al. (2015) used grain-size analysis to identify the timing of major overbank flood events of the Mississippi River (Fig. 4). Prior to the establishment of artificial levees, the Mississippi River periodically inundated the floodplain around Horseshoe Lake, depositing a layer of well-sorted and fine-grained sediment in the lake. We encountered levels in which diatom preservation was poor that correspond to levels identified by Munoz et al. (2015) as consisting mainly of suspended sediment delivered from the Mississippi River during overbank floods (Fig. 3). The absence of diatoms in these levels allows us to interpret the diatom assemblages that are present in the sediment as being primarily autochthonous. Low diatom concentrations in the extra-local allochthonous sediments are a consequence of (1) low diatom concentrations in the suspended load of floodwaters and/or (2) diatom dissolution. Diatoms are stable in sediment where the interstitial water is saturated with respect to biogenic silica (BSi), but dissolve in environments where the solubility product for BSi is not exceeded (Van Cappellen and Qui 1997a, b), so exposure of diatoms to low-silicate water may have caused them to dissolve. Throughout the remainder of this discussion, we interpret the diatom assemblages in Horseshoe Lake as being sourced primarily from the lake and its watershed.

Wiklund et al. (2010) compared modern communities of epiphytic diatoms in periodically flooded and non-flooded lakes in the Peace–Athabasca Delta in Alberta, Canada and found large differences in lake water silicate and taxon abundance between lake types. At Horseshoe Lake, we found Wiklund et al. (2010) “flood-indicator” and “non-indicator” taxa mixed together in sediment assemblages. This may be a result of comparing living communities with sediment fossil assemblages. The diatom-poor levels in the Horseshoe Lake core could result from poor preservation—not differential survival of living diatoms.

Diatom assemblages associated with prehistoric human populations

The most prominent shift in diatom assemblages at Horseshoe Lake as shown in stratigraphic diagrams, CONISS clustering, and NMDS ordination occurs in the 14th century CE, and coincides with the abandonment of Cahokia and surrounding communities in the floodplain and adjacent uplands. Diatom assemblages at this time shift from being dominated by planktonic Aulacoseira granulata to dominance by epiphytic Cocconeis and Gomphonema spp (Figs. 3, 4, 5, 7). The diatom taxa we observe before and after the prehistoric abandonment of the Horseshoe Lake area differ in their modern distributions: A. granulata is associated with shallow, eutrophic, alkaline lakes, whereas Gomphonema and Cocconeis are taxa that live on the leaf surfaces of aquatic plants (Brugam 1993; Hoaglund et al. 1982; Kilham and Kilham 1975). The observed shift in diatom assemblages is indicative of a major shift in Horseshoe Lake’s ecology when prehistoric indigenous people abandoned the area.

We interpret the dominance of A. granulata in diatom assemblages as an indicator of eutrophic conditions in Horseshoe Lake when prehistoric populations were growing and becoming increasingly agricultural. A review of the ecology of A. granulata by Kilham and Kilham (1975) found that it is common in eutrophic lakes with high pH and alkalinity, particularly in rivers and shallow floodplain lakes with high water turbulence. Kilham and Kilham (1975) classify A. granulata as meroplanktonic, depending on turbulence for periodic resuspension from the bottom sediments where it survives in a dormant state until mixed into the water column. In Sweden, Yang et al. (2016) found A. granulata to be a major part of eutrophic Lake Erken’s spring phytoplankton during warmer winters with a shorter period with ice cover because the taxon can survive in lake sediment and return to the plankton when lake turbulence increases at ice-out. In general, A. granulata is found in shallow eutrophic lakes around the world, including reservoirs in Spain (Goméz et al. 1995) and Brazil (Fontana et al. 2014), floodplain lakes in Mozambique (Sitoe et al. 2015) and shallow prairie lakes in Saskatchewan, Canada (Hall et al. 1999). In Adams Bayou, a floodplain lake in Arkansas (USA), 20th-century sediments are dominated by a group of Aulacoseira species including A. granulata, whereas Gomphonema parvulum and other epiphytic taxa were more abundant before this time. This change was interpreted as a change from a clear-water mesotrophic system to an enriched turbid system caused by an increase in local land clearance (Bhattacharya et al. 2016). The dominance of A. granulata in Horseshoe Lake’s diatom assemblages during diatom zone HORMD2 (610–1400 CE) indicates that the lake was more eutrophic during the prehistoric occupation of the area, as population densities and agricultural production increased (Milner 1998; Simon and Parker 2006; Pauketat 2009).

Eutrophication of Horseshoe Lake during the Late Woodland and Mississippian Periods is consistent with stable organic carbon isotopic (δ13Corg) measurements reported by Munoz et al. (2014) (Fig. 3). Stable carbon isotopes in lake sediments are sensitive to lake trophic status because high photosynthetic rates cause reduced isotopic discrimination among aquatic autotrophs (Hollander and McKenzie 1991; Hollander et al. 1992; Brenner et al. 1998; Meyers 2003; Belle et al. 2017; Earley et al. 2017; Mays et al. 2017). In Horseshoe Lake, Munoz et al. (2014) reported that δ13Corg values gradually increased beginning around 450 CE, and reached a stable maximum around − 23‰ from 900 to 1200 CE, tracking the development of Cahokia and inferred lake eutrophication. Following a decline when Cahokia was abandoned, δ13Corg increased again following Euro-American settlement ca. 1800 CE. In the same study, Munoz et al. (2014) also report shifts in pollen assemblages associated with prehistoric and historical deforestation that track trends in δ13Corg values. In an independent study of δ13Corg in surface sediment cores from Horseshoe Lake, Karthic et al. (2013) found δ13Corg values ranging from − 26 to − 24‰ for the historic period, confirming the patterns reported by Munoz et al. (2014).

Recently, paleolimnologists have used weighted averaging models of diatom assemblages to infer past total phosphorus concentrations in lakes (Enache et al. 2012; Reavie and Edlund 2013; Cumming et al. 2015; Reavie et al. 2017). We were unable to apply this approach to the diatom assemblages in Horseshoe Lake because of the lake’s shallow depth and the presence of epiphytic diatom taxa. As discussed by Juggins et al. (2013), epiphytic diatom taxa hinder reconstructions of total phosphorus because these taxa are sensitive to multiple environmental factors. Species composition of benthic and epiphytic communities are controlled by factors other than phosphorus, particularly the amount of light reaching the sediment surface, so quantitative reconstructions of total phosphorus levels are challenging in shallow lakes like Horseshoe Lake. Heathcote et al. (2015) encountered similar problems interpreting the paleolimnology of eutrophication in shallow Minnesota lakes, leading them to employ qualitative reconstructions of trophic status based on environmental preferences of diatom species and sediment geochemistry.

In this study, we applied a qualitative approach developed by Scheffer et al. (1993) to describe the trophic status of shallow lakes. Scheffer et al. (1993) argued that shallow lakes have alternative stable states that are controlled by nutrient concentrations. One stable state is a low-nutrient, clear-water state that enables light to penetrate to the lake bottom and encourages high macrophyte abundance; the alternative stable state has high nutrient concentrations that cause dense blooms of plankton, preventing sunlight from reaching the lake bottom (Scheffer et al. 1993). Prior work by Randsalu-Wendrup et al. (2014, 2016) demonstrated that these alternative states—and shifts between them—can be inferred using diatom assemblages in sedimentary records because diatom taxa can be classified as planktonic or epiphytic. Similar state changes have been inferred using diatom records from shallow lakes, which show shifts from epiphytic to planktonic taxa in response to more eutrophic conditions, as aquatic macrophytes are replaced by planktonic algae in response to an increase in nutrient delivery to the lake (Bhattacharya et al. 2016; Sayer et al. 2010). At Horseshoe Lake, we interpret the prominent shift in diatom assemblages in the 14th century as a shift from a eutrophic to more mesotrophic state when prehistoric populations abandoned the area and nutrient inputs to the lake from settlements and agricultural fields in the watershed declined.

An alternative ‘top-down’ model for trophic state shifts in shallow lakes views predatory fish as playing a fundamental role in a lake’s trophic status (Hobbs et al. 2012, 2016). Using paleolimnological techniques on small shallow lakes in the Prairie Pothole region of Minnesota and South Dakota, Hobbs et al. (2012, 2016) found larger fish stocks in plankton-dominated lakes, whereas fish were absent in macrophyte-dominated lakes. This finding led Hobbs et al. (2016) to propose that changes in top-down controls were an important driver of regime shifts, and that changes in nutrient delivery need not be invoked to explain shifts in the trophic state of shallow lakes.

Indigenous populations in the study area consumed large amounts of fish for dietary protein (Milner 1998), and prehistoric fishing in Horseshoe Lake may have contributed to a shift in the lake’s trophic state. The importance of fish in the diet of prehistoric populations in the study area is indicated by the presence of fish bones, scales, and hooks in archaeological contexts (Kelly and Cross 1984; Kelly 1997; Yerkes 2005), and stable carbon isotope measurements of human bone collagen and apatite (Kellner and Schoeninger 2007). Modern experiments also demonstrate that substantial amounts of fish can be harvested with minimal energy expenditure from a Midwestern oxbow lake using a simple net (Limp and Reidhead 1979). Given the large prehistoric population that lived around Horseshoe Lake, fishing in the lake may have acted as a ‘top-down’ control that removed carnivorous taxa like bowfin (Amia calva), which is a common fish remain in archaeological contexts (Kelly and Cross 1984; Kelly 1997). Reduced populations of predatory fish would enable expansion of zooplanktivorous fish populations and an increase in phytoplankton (Hobbs et al. 2016), creating diatom assemblages similar to those observed in Horseshoe Lake when prehistoric human population densities were high. When indigenous populations declined at the end of the Mississippian Period, carnivorous fish populations in Horseshoe Lake would have recovered. This, in turn, would have increased predatory pressure on zooplanktivorous fishes, enabling proliferation of zooplanton that graze on phytoplankton, thereby resulting in clearer water and expansion of aquatic macrophytes. Although this ‘top-down’ mechanism provides a plausible explanation for the inferred shifts in trophic state at Horseshoe Lake, a decrease in nutrient inputs to the lake as a result of declining indigenous populations may also have been responsible for the inferred shifts in the lake’s ecology.

Other factors aside from prehistoric human land use, namely environmental factors affecting the climate and hydrology of the Mississippi River and its basin, may have also influenced diatom assemblages in Horseshoe Lake, although the characteristics of the observed changes around the time of abandonment of Cahokia implicate human activities. For example, the transition of the lake from a turbid eutrophic state to a more mesotrophic state in the 14th century roughly coincides with the onset of the ‘Little Ice Age’ (Mann et al. 2009), when the frequency of high-magnitude flooding on the Missouri and Upper Mississippi Rivers increased (Munoz et al. 2015), while localized drought around Cahokia became more common (Benson et al. 2009). It is possible that an increase in the frequency of overbank floods enhanced the connectivity of Horseshoe Lake with the Mississippi River and contributed to the observed transition towards a more mesotrophic state, although the mechanism responsible for this is not clear. These environmental changes associated with the Little Ice Age, however, may have influenced the decision of prehistoric populations to abandon Cahokia and the surrounding region (Benson et al. 2009; Munoz et al. 2015), reducing human impacts on Horseshoe Lake indirectly. Examining diatom assemblages from other floodplain lakes along the Mississippi River that were not as heavily settled by prehistoric populations as Horseshoe Lake could provide additional insight into the role of late Holocene climate variability on aquatic communities.

In short, evidence from fossil diatom assemblages and stable carbon isotopes indicates that, as prehistoric populations abandoned the Horseshoe Lake area in the 14th century, the lake shifted from a turbid eutrophic state to a more mesotrophic state, dominated by aquatic macrophytes. This inferred shift in trophic state was most likely the result of reduced nutrient inputs from indigenous settlements around the lake and/or the recovery of fish populations, as fishing pressure was relaxed. In either case, our data demonstrate that the ecology of a large lake in North America was substantially affected by prehistoric indigenous peoples beginning around 600 CE, nearly a millennium prior to European colonization of the Americas. Our findings add to the existing evidence of prehistoric cultural eutrophication in North America (Ekdahl et al. 2004) and demonstrate that large Mississippian population centers, which were located across much of eastern North America, also adversely influenced freshwater quality. In the case of Cahokia, human impacts on aquatic ecosystems, and on terrestrial ecosystems (Munoz et al. 2014), persisted for hundreds of years.

Diatom assemblages associated with historical settlement

In the early 19th century, diatom assemblages in Horseshoe Lake shifted from epiphytic taxa to epipelic ones of the genera Staurosira and Fragilaria, as historical settlement of the area intensified. This shift in diatom assemblages is similar to that reported in Horseshoe Lake by Karthic et al. (2013), who examined the upper meter of the lake’s sedimentary record. In the longer diatom record presented in this study, the abundance of A. granulata during the historical period is not as high as during the prehistoric occupation of the area in the Late Woodland and Mississippian Periods. These differences in diatom assemblages associated with prehistoric and historical occupations reflect, at least in part, industrialization of the area in the late 19th and early 20th century. For example, lead smelting operations on the lakeshore in the early 20th century left the uppermost sediments contaminated with heavy metals, and wastewater from a coking plant that has operated since the 1920s continues to be a large source of nitrates to the lake, both of which may influence historic diatom communities (Karthic et al. 2013). Epipelic diatoms of the genera Staurosira and Fragilaria first appear in diatom assemblages ca. 1800 CE, prior to industrialization of the area, implying that other factors also contribute to the unique diatom assemblages present in Horseshoe Lake today. Artificial levees and other hydrological alterations to Horseshoe Lake, for example, isolate the lake from the Mississippi River and maintain more consistent lake levels. Extensive aquatic macrophyte beds, which we infer to have been present following the prehistoric abandonment of the area, are no longer present on Horseshoe Lake, and may be inhibited by increased turbidity as the lake gradually fills in. In short, historical land use practices from the early 19th century onwards have markedly altered Horseshoe Lake, but these recent changes represent a second and distinct period of human influence on the lake’s freshwater ecology over the last 1600 years.


Fossil diatom assemblages in a sedimentary record collected from Horseshoe Lake, an oxbow lake in the floodplain of the middle Mississippi River, demonstrate that between 600 and 1400 CE, the lake shifted to a eutrophic state when the area was heavily occupied by prehistoric indigenous populations. After the abandonment of the area by prehistoric populations in the 14th century CE, the lake became less eutrophic and supported extensive beds of aquatic macrophytes. Beginning in the early 19th century, historic settlement of the area altered the aquatic ecosystem and adversely affected water quality. Our work implies that human activities profoundly influenced the ecology of a large lake in North America nearly a 1000 years prior to European colonization of the continent.



We thank Jim Gowen of the Illinois Department of Natural Resources for lake access, and gratefully acknowledge Jessica Blois, Brigitta Rongstad, Grace Schellinger, Jack Williams, and Chad Zirbel for field and laboratory assistance, and Kristina Brady, Amy Myrbo, Anders Noren, and Ryan O’Grady of the National Lacustrine Core Facility (LacCore) for assistance with initial core description. We also thank Stephen Juggins of Newcastle University for help in evaluating total phosphorus reconstructions with our data, and Julie Zimmerman of Southern Illinois University at Edwardsville for discussions about Cahokia Archaeology. This work was supported by the National Geographic Society (Grant Number YEG-9008-11) and the National Science Foundation (Grant Number BCS-1333070).


  1. Belle S, Verneaux V, Mariet A-L, Millet L (2017) Impact of eutrophication on the carbon stable-isotopic baseline of benthic invertebrates in two deep soft-water lakes. Freshw Biol 62:1105–1115. CrossRefGoogle Scholar
  2. Benson LV, Pauketat TR, Cook ER (2009) Cahokia’s boom and bust in the context of climate change. Am Antiq 74:467–483CrossRefGoogle Scholar
  3. Bhattacharya R, Hausmann S, Hubeny JB, Gell P, Black JL (2016) Ecological response to hydrological variability and catchment development: insights from a shallow oxbow lake in Lower Mississippi Valley, Arkansas. Sci Total Environ 569–570:1087–1097. CrossRefGoogle Scholar
  4. Blaauw M (2010) Methods and code for ‘classical’ age-modeling of radiocarbon sequences. Quat Geochronol 5:512–518. CrossRefGoogle Scholar
  5. Brenner M, Whitmore TJ, Curtis JH, Hodell DA, Schelske CL (1998) Stable isotope (δ13C and δ15N) signatures of sedimented organic matter as indicators of historic lake trophic state. J Paleolimnol 22:205–221CrossRefGoogle Scholar
  6. Brown JA, Sasso RF (2001) Prelude to history on the eastern prairies. In: Brose DS, Cowan CW, Manifort RC (eds) Societies in eclipse: archaeology of the eastern woodlands Indians A.D. 1400–1700. Smithsonian Institution Press, Washington DC, pp 25–228Google Scholar
  7. Brugam RB (1993) Surface sample analogues of Elk Lake fossil diatom assemblages. In: Bradbury JP, Dean WE (eds) Elk Lake, minnesota: evidence for rapid climate change in the North-Central United States, Geological Society of America Special Paper, vol 276, pp 189–214Google Scholar
  8. Bush MB, Correa-Metrio A, McMichael CH, Sully S, Shadik CR, Valencia BG, Guilderson T, Steinitz-Kannan M, Overpeck JT (2016) A 6900-year history of landscape modification by humans in lowland Amazonia. Quat Sci Rev 141:52–64. CrossRefGoogle Scholar
  9. Carpenter SR, Caraco NF, Correll DL, Howarth RW, Sharpley AN, Smith VH (1998) Nonpoint pollution of surface waters with phosphorus and nitrogen. Ecol Appl 8:559–568. CrossRefGoogle Scholar
  10. Cumming BF, Smol JP, Kingston JC, Charles DF, Birks HJB, Camburn K, Dixit SS, Uutala AJ, Selled AR (1992) How much acidification has occurred in Adirondack region lakes (New York, USA) since preindustrial times? can. J Fish Aquat Sci 49:128–141. CrossRefGoogle Scholar
  11. Cumming BF, Laird KR, Gregory-Eaves I, Simpson KG, Sokal MA, Nordin RN, Walker IR (2015) Tracking past changes in lake-water phosphorus with a 251-lake calibration dataset in British Columbia: tool development and application in a multiproxy assessment of eutrophication and recovery in Osoyoos Lake, a transboundary lake in Western North America. Front Ecol Evol 3:84. CrossRefGoogle Scholar
  12. Dudgeon D, Arthington AH, Gessner MO, Kawabata ZI, Knowler DJ, Lévêque C, Naiman RJ, Prieur-Richard A-H, Soto D, Stiassny MLJ, Sullivan CA (2006) Freshwater biodiversity: importance, threats, status and conservation challenges. Biol Rev 81:163–182. CrossRefGoogle Scholar
  13. Earley SM, Waters MN, Thieme D, Smoak JM (2017) Linking biogeochemical processes and historic primary producer communities in a SE USA sinkhole lake from the mid-Holocene to present. J Paleolimnol 57:295–306. CrossRefGoogle Scholar
  14. Ekdahl EJ, Teranes JL, Guilderson TP, Turton CL, McAndrews JH, Wittkop CA, Stoermer EF (2004) Prehistorical record of cultural eutrophication from Crawford Lake, Canada. Geology 32:745–748. CrossRefGoogle Scholar
  15. Ekdahl EJ, Teranes JL, Wittkop CA, Stoermer EF, Reavie ED, Smol JP (2007) Diatom assemblage response to Iroquoian and Euro-Canadian eutrophication of Crawford Lake, Ontario, Canada. J Paleolimnol 7:233–246. CrossRefGoogle Scholar
  16. Enache MD, Charles DF, Belton TJ, Callinan CW (2012) Total phosphorus changes in New York and New Jersey lakes (USA) inferred from sediment cores. Lake Reserv Manag 28:293–310. CrossRefGoogle Scholar
  17. Esarey ME (1984) Historic Period. In: Bareis CJ, Porter JW (eds) American bottom archaeology: a summary of the FAI-270 project contribution to the culture history of the Mississippi river valley. University of Illinois Press, Urbana, pp 187–196Google Scholar
  18. Fontana L, Albuquerque ALS, Brenner M, Bonotto DM, Sabaris TPP, Pires AFS, Cotrim MEB, Bicudo DC (2014) The eutrophication history of a tropical water supply reservoir in Brazil. J Paleolimnol 51:29–43. CrossRefGoogle Scholar
  19. Fortier AC, Jackson DK (2000) The formation of a Late Woodland heartland in the American Bottom, Illinois cal AD 650-900. In: Emerson TE, McElrath DL, Fortier AC (eds) Late woodland societies: tradition and transformation across the midcontinent. University of Nebraska Press, Lincoln, pp 123–148Google Scholar
  20. Fortier AD, Emerson TE, McElrath DL (2006) Calibrating and reassessing American bottom culture history. Southeastern Archaeol 25:170–211Google Scholar
  21. Fritz GJ (1990) Multiple pathways to farming in precontact eastern North America. J World Prehist 4:387–435CrossRefGoogle Scholar
  22. Goméz N, Riera JL, Sabater S (1995) Ecology and morphological variability of Aulacoseira granulata (Bacillariophyceae) in Spanish reservoirs. J Plankton Res 17:1–16CrossRefGoogle Scholar
  23. Grimm E (1992) TILIA Software, Version 112, Illinois State MuseumGoogle Scholar
  24. Haberyan KA, Horn SP (2005) Diatom paleoecology of Laguna Zoncho, Costa Rica. J Paleolimnol 33:361–369CrossRefGoogle Scholar
  25. Hajic ER (1993) Geomorphology of the Northern American bottom as context for archaeology. Illinois Archaeol 5:54–65Google Scholar
  26. Hall RI, Leavitt PR, Quinlan R, Dixit AS, Smol JP (1999) Effects of agriculture, urbanization, and climate on water quality in the northern Great Plains. Limnol Oceanogr 44:739–756CrossRefGoogle Scholar
  27. Hall RI, Leavitt PR, Smol JP, Zirnelt N (1997) Comparison of diatom, fossil pigments and historical records as measures of lake eutrophication. Freshw Biol 38:401–417. CrossRefGoogle Scholar
  28. Heathcote AJ, Hobbs JMR, Anderson NJ, Frings P, Engstrom DR, Downing JA (2015) Diatom floristic change and lake paleoproduction as evidence of recent eutrophication in shallow lakes of the midwestern USA. J Paleolimnol 53:17–34. CrossRefGoogle Scholar
  29. Hoaglund KG, Roemer SC, Rosowski JR (1982) Colonization and community structure of two periphyton assemblages with emphasis on the diatoms (Bacillariophyceae). Am J Bot 69:188–213CrossRefGoogle Scholar
  30. Hobbs WO, Hobbs JMR, LaFrançois T, Zimmer KM, Theissen M, Edlund MB, Butler MG, Hanson MA, Carlson TJ (2012) A 200-year perspective on alternative stable state theory and lake management from a biomanipulated shallow lake. Ecol Appl 22:1483–1496CrossRefGoogle Scholar
  31. Hobbs JMR, Hobbs WO, Edlund MB, Zimmer KD, Theissen KM, Hoidal N, Domine LM, Hanson MA, Herwig BR, Cotner JB (2016) The legacy of large regime shifts in shallow lakes. Ecol Appl 26:2662–2676CrossRefGoogle Scholar
  32. Hollander DJ, McKenzie JA (1991) CO2 control on carbon-isotope fractionation during aqueous photosynthesis: a paleo-pCO2 barometer. Geology 19:929–932CrossRefGoogle Scholar
  33. Hollander DJ, McKenzie JA, ten Haven JL (1992) A 200 year sedimentary record of progressive eutrophication in Lake Greifen (Switzerland): implications for the origin of organic carbon-rich sediments. Geology 20:825–828CrossRefGoogle Scholar
  34. Jackson RB, Carpenter SR, Dahm CN, McKnight DM, Naiman RJ, Postel SL, Running SW (2001) Water in a changing world. Ecol Appl 11:1027–1045CrossRefGoogle Scholar
  35. Johannessen S (1984) Paleoethnobotany. In: Bareis CJ, Porter JW (ed) American Bottom Archaeology. University of Illinois Press, Urbana, IL, pp 197–214Google Scholar
  36. Juggins S, Anderson NJ, Ramstack-Hobbs JM, Heathcote AJ (2013) Reconstructing epilimnetic total phosphorus using diatoms: statistical and ecological constraints. J Paleolimnol 49:373–390. CrossRefGoogle Scholar
  37. Karthic I, Brugam RB, Retzlaff WA, Johnson K (2013) The impact of nitrogen contamination and river modification on a Mississippi river floodplain lake. Sci Tot Environ 463(464):734–742. CrossRefGoogle Scholar
  38. Kellner CM, Schoeninger MJ (2007) A simple carbon isotope model for reconstructing prehistoric human diet. Am J Phys Anthropol 133:1112–1127. CrossRefGoogle Scholar
  39. Kelly LS (1997) Patterns of faunal exploitation at Cahokia. In: Pauketat TR, Emerson TE (eds) Cahokia: domination and Ideology in the Mississippian world. University of Nebraska Press, Lincoln, pp 69–88Google Scholar
  40. Kelly LS, Cross PG (1984) Zooarcheology. In: Bareis CJ, Porter JW (eds) American bottom archeology: a summary of the FAI-270 project contribution to the culture history of the Mississippi river valley. University of Illinois Press, Urbana, pp 215–240Google Scholar
  41. Kilham SS, Kilham (1975) Melosira granulata (Ehr) Ralfs: morphology and ecology of a cosmopolitan freshwater diatom. Verh Int Verein Limnol 19:2716–2721Google Scholar
  42. Koldehoff B, Galloy JM (2006) Late woodland frontiers in the American bottom region. Southeastern Archaeol 25:275–300Google Scholar
  43. Kramer K (2000) Diatoms of Europe vol 1: The genus Pinnularia. ARG Gantner Verlag KGGoogle Scholar
  44. Kramer K (2002) Diatoms of Europe vol 3: Cymbella. ARG Gantner Verlag KGGoogle Scholar
  45. Lange-Bertalot H (2001) Diatoms of Europe vol 2: Navicula sensu stricto, 10 Genera Separated from Navicula sensu lato, Frustulia. ARG Gantner Verlag KGGoogle Scholar
  46. Limp WF, Reidhead VA (1979) An economic evaluation of the potential of fish utilization in riverine environments. Am Antiq 44:70–78CrossRefGoogle Scholar
  47. Lopinot NH (1997) Cahokian food production reconsidered. In: Pauketat TR, Emerson TE (eds) Cahokia: domination and ideology in the Mississippian world. University of Nebraska Press, Lincoln, pp 52–68Google Scholar
  48. Mann DG, Stickle AJ (1993) Life history and systematics of Lyrella. Nova Hedwig Beih 106:43–70Google Scholar
  49. Mann ME, Zhang Z, Rutherford S, Bradley RS, Hughes MK, Shindell CA, Faluvegi G, Fenbiao N (2009) Global signatures and dynamical origins of the Little Ice Age and Medieval Climate Anomaly. Science 326:1256–1260. CrossRefGoogle Scholar
  50. Mays JL, Brenner M, Curtis J, Curtis KV, Hodell DA, Correa-Metrio A, Escobar J, Dutton AL, Zimmerman AR (2017) Guilderson TP (2017) Stable carbon isotopes (δ13C) of total organic carbon and long-chain n-alkanes as proxies for climate and environmental change in a sediment core from Lake Petén-Itzá, Guatemala. J Paleolimnol 57:307–319. CrossRefGoogle Scholar
  51. McAndrews JH (1988) Human disturbance of North American forests and grasslands: The fossil pollen record. In: Huntley B, Webb T (eds) Vegetation history. Kluwer, Dordrecht, pp 673–697CrossRefGoogle Scholar
  52. Meyers PA (2003) Applications of organic geochemistry to paleolimnological reconstructions: a summary of examples from the Laurentian Great Lakes. Org Geochem 34:261–289CrossRefGoogle Scholar
  53. Milner GR (1998) The Cahokia Chiefdom: the archaeology of a Mississippian society. Smithsonian Institution Press, Washington DC, p 240Google Scholar
  54. Milner GR (2005) The Moundbuilders: Ancient peoples of Eastern North America. Thames and Hudson, London, p 224Google Scholar
  55. Minchin PR (1987) Simulation of multidimensional community patterns: towards a comprehensive model. Vegetatio 71:145–156Google Scholar
  56. Moos M, Laird KR, Cumming BF (2005) Diatom assemblages and water depth in Lake 239 (Experimental Lakes Area, Ontario): implications of paleoclimatic studies. J Paleolimnol 24:217–287. CrossRefGoogle Scholar
  57. Munoz SE, Schroeder S, Fike DA, Williams JW (2014) A record of sustained prehistoric and historic land use from the Cahokia region, Illinois, USA. Geology 42:499–502. CrossRefGoogle Scholar
  58. Munoz SE, Gruleya KE, Massiea A, Fike DA, Schroeder A, Williams JW (2015) Cahokia’s emergence and decline coincided with shifts of flood frequency on the Mississippi River. Proc Natl Acad Sci USA 112:6319–6324. CrossRefGoogle Scholar
  59. Pauketat TR (2009) Cahokia: Ancient America’s Great City on the Mississippi. Viking, New York, p 162Google Scholar
  60. Pauketat TR, Lopinot NH (1997) Cahokian population dynamics. In: Pauketat TR, Lopinot NH (eds) Cahokia: domination and Ideology in the Mississippian world. University of Nebraska Press, Lincoln, pp 103–123Google Scholar
  61. Peck JE (2010) Multivariate analysis for community ecologists: step-by-step using PC-ORD. MJM software design, gleneden beach, Oregon, USA, 162 ppGoogle Scholar
  62. Randsalu-Wendrup L, Conley DJ, Carstensen J, Hansson L-A, Brönmark C, Fritz SC, Choudhary P, Routh J, Hammarlund D (2014) Combining limnology and palaeolimnology to investigate recent regime shifts in a shallow, eutrophic lake. J Paleolimnol 51:437–448. CrossRefGoogle Scholar
  63. Randsalu-Wendrup L, Conley DJ, Carstensen J, Fritz SC (2016) Paleolimnological records of regime shifts in lakes in response to climate change and anthropogenic activities. J Paleolimnol 56:1–14. CrossRefGoogle Scholar
  64. Reavie ED, Edlund MB (2013) Assessing the performance of a diatom transfer function on four Minnesota lake sediment cores: effects of training set size and sample age. J Paleolimnol 50:87–104. CrossRefGoogle Scholar
  65. Reavie ED, Edlund MB, Andresen NA, Engstrom DR, Leavitt PR, Schottler S, Cai M (2017) Paleolimnology of the Lake of the Woods southern basin: continued water quality degradation despite lower nutrient influx. Lake Reserv Manag 33:369–385. CrossRefGoogle Scholar
  66. Reimer PJ et al (2013) IntCal13 and Marine13 radiocarbon age calibrations curves, 0–50,000 years cal BP. Radiocarbon 55:1869–1887. CrossRefGoogle Scholar
  67. Sayer CD, Burgess A, Kari K, Davidson TA, Peglar S, Yang H-D, Rose N (2010) Long-term dynamics of submerged macrophytes and algae in a small and shallow, eutrophic lake: implications for the stability of macrophyte-dominance. Freshw Biol 55:565–583. CrossRefGoogle Scholar
  68. Scheffer M, Hosper SH, Meijer ML, Moss B, Jeppesen E (1993) Alternative equilibria in shallow lakes. Trends Ecol Evol 8:275–279CrossRefGoogle Scholar
  69. Schroeder LA, Martin SC, Kerns GJ, McLean CE (2016) Diatom assemblages in a reservoir sediment core track land-use changes in the watershed. J Paleolimnol 55:17–33. CrossRefGoogle Scholar
  70. Simon ML, Parker KE (2006) Prehistoric plant use in the American Bottom: new thoughts and interpretations. Southeastern Archaeol 25:212–257Google Scholar
  71. Sitoe SR, Risberg J, Norström E, Snowball I, Holmgren K, Achimo M, Mugabe J (2015) Paleo-environment and flooding of the Limpopo River-plain, Mozambique, between AD 1200–2000. CATENA 126:105–116. CrossRefGoogle Scholar
  72. Siver PA, Hamilton PB (2011) Diatoms of North America: the freshwater Flora of Waterbodies on the Atlantic Coastal plain. ARG Ganter Verlag KGGoogle Scholar
  73. Siver PA, Hamilton PB, Stachura-Sucholes K, Kocioleck JP (2007) Diatoms of North America: the freshwater Flora of Cape Cod. ARG Gantner Verlag KGGoogle Scholar
  74. Slate JE, Johnson TC, Moore TC (2013) Impact of pre-Columbian agriculture, climate change, and tectonic activity inferred from a 5700-year paleolimnological record from Lake Nicaragua. J Paleolimnol 50:139–149. CrossRefGoogle Scholar
  75. Smith BD (1987) The independent domestication of indigenous seed-bearing plants in eastern North America emergent horticultural economies of the Eastern Woodlands. In: Keegan WF (ed), Emergent horticultural economies of the eastern woodlands. Southern Illinois University at Carbondale, Center for Archaeological Investigation, Occasional Paper, vol 7, pp 3–47Google Scholar
  76. Smith BD (2009) Resource resilience, human niche construction, and the long-term sustainability of pre-Columbian subsistence economies in the Mississippi River Valley corridor. J Ethnobiol 29:167–183CrossRefGoogle Scholar
  77. Smith VH, Tilman GD, Nekola JC (1999) Eutrophication: impacts of excess nutrient inputs on freshwater, marine, and terrestrial ecosystems. Environ Pollut 100:179–196CrossRefGoogle Scholar
  78. Smol JP (2010) The power of the past: using sediments to track the effects of multiple stressors on lake ecosystems. Freshwat Biol 55:43–59. CrossRefGoogle Scholar
  79. Smol JP, Stoermer EF (eds) (2010) The diatoms: applications for the environmental and earth sciences. Cambridge University Press, CambridgeGoogle Scholar
  80. Toonen WH, Kleinhans MG, Cohen KM (2012) Sedimentary architecture of abandoned channel fills. Earth Surf Process 37:459–472. CrossRefGoogle Scholar
  81. Van Cappellen P, Qui L (1997a) Biogenic silica dissolution in sediments of the Southern Ocean I: solubility. Deep-Sea Res II 44:1109–1129CrossRefGoogle Scholar
  82. Van Cappellen P, Qui L (1997b) Biogenic silica dissolution in sediments of the Southern Ocean II: kinetics. Deep Sea Res II 44:1129–1149CrossRefGoogle Scholar
  83. Wiklund JA, Bozinovski N, Hall RI, Wolfe BB (2010) Epiphytic diatoms as flood indicators. J Paleolimnol 44:25–42. CrossRefGoogle Scholar
  84. Yang Y, Stenger-Kovács C, Padisák J, Pettersson K (2016) Effects of winter severity on spring phytoplankton development in a temperate lake (Lake Erken, Sweden). Hydrobiologia 780:47–57. CrossRefGoogle Scholar
  85. Yerkes RW (2005) Bone chemistry, body parts, and growth marks: evaluating Ohio Hopewell and Cahokia Mississippian seasonality, subsistence, ritual, and feasting. Am Antiq 70:241–265CrossRefGoogle Scholar

Copyright information

© The Author(s) 2018

Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (, which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.

Authors and Affiliations

  1. 1.Department of Biological SciencesSouthern Illinois University EdwardsvilleEdwardsvilleUSA
  2. 2.Department of Marine and Environmental Sciences, Marine Science CenterNortheastern UniversityNahantUSA
  3. 3.Department of Civil and Environmental EngineeringNortheastern UniversityBostonUSA

Personalised recommendations