589 tocRiparian and valley-margin hardwood species of pre-colonial Piedmont forests: A preliminary study of subfossil leaves from White Clay Creek, southeastern Pennsylvania, USA

Sara J. Elliott, Christen L. Grettenberger, Michael P. Donovan, Peter Wilf, Robert C. Walter, and Dorothy J. Merritts

Article number: 19.1.2A
Copyright Paleontological Society, January 2016

Author biographies
Plain-language and multi-lingual abstracts
PDF version

Submission: 27 July 2015. Acceptance: 30 November 2015


Beginning in the seventeenth century, colonial activities such as land clearing, agriculture, and milldam construction significantly altered the landscapes, vegetation, and hydrogeomorphology of the northeastern Piedmont region, modern-day USA. Presently, weedy and non-native vegetation dominate the altered riparian zones and hill slopes where old-growth, hardwood forests once prevailed. Various studies have identified pre-settlement herbaceous wetland floras based on fruits and seeds. However, only one report provided evidence of the dominant pre-settlement woody species by using the localized signal available from subfossil leaves; that work reconstructed Maple-Ash floodplain swamp forests along valley-margins and Oak-Beech mixed forests on upper-slopes at a site in Lancaster County, southeastern Pennsylvania. Here, we investigate subfossil leaves recovered from the buried wetland soils of White Clay Creek in neighboring Chester County, Pennsylvania, providing significant new spatial data to our understanding of regional old-growth forests. The leaf assemblage, radiocarbon dated to ca. 1650, is composed of woody species with a diverse range of wetland affinities, indicating sources in both the riparian zone and surrounding lower hill slopes. Obligate and facultative-wetland species include willow (Salix spp.) and Hazel Alder (Alnus serrulata). Box Elder (Acer negundo) is the only facultative species present, while American Beech (Fagus grandifolia), the white and red oak groups (Quercus Section Quercus and Q. Section Lobatae, respectively), and Tulip Tree (Liriodendron tulipifera) comprise the identified facultative-upland taxa. These results complement and corroborate previous work and allow for greater confidence in understanding the pre-European landscape, potentially increasing the effectiveness of regional environmental restoration projects.

Sara J. Elliott. Department of Geosciences, Pennsylvania State University, University Park, PA 16802, USA; Bureau of Economic Geology, University of Texas, Austin, TX 78758, USA. This email address is being protected from spambots. You need JavaScript enabled to view it. (corresponding author)
Christen L. Grettenberger. Department of Geosciences, Pennsylvania State University, University Park, PA 16802, USA. This email address is being protected from spambots. You need JavaScript enabled to view it.
Michael P. Donovan. Department of Geosciences, Pennsylvania State University, University Park, PA 16802, USA. This email address is being protected from spambots. You need JavaScript enabled to view it.
Peter Wilf. Department of Geosciences, Pennsylvania State University, University Park, PA 16802, USA. This email address is being protected from spambots. You need JavaScript enabled to view it.
Robert C. Walter. Department of Earth and Environment, Franklin and Marshall College, Lancaster, PA 17604, USA. This email address is being protected from spambots. You need JavaScript enabled to view it.
Dorothy J. Merritts. Department of Earth and Environment, Franklin and Marshall College, Lancaster, PA 17604, USA. This email address is being protected from spambots. You need JavaScript enabled to view it.

Keywords: paleobotany; Holocene; leaves; paleoecology; restoration; milldams

Final citation: Elliott, Sara J., Grettenberger, Christen L., Donovan, Michael P., Wilf, Peter, Walter, Robert C., and Merritts, Dorothy J. 2016. Riparian and valley-margin hardwood species of pre-colonial Piedmont forests: A preliminary study of subfossil leaves from White Clay Creek, southeastern Pennsylvania, USA. Palaeontologia Electronica 19.1.2A: 1-26. https://doi.org/10.26879/589


European settlement in eastern North America was characterized by severe and rapid anthropogenic landscape modifications, including changes in stream hydrology and riparian forest ecology (Foster et al., 1998; Cogbill, 2000; Walter and Merritts, 2008; Thompson et al., 2013). Deforestation, agriculture, and milldam construction during the seventeenth through nineteenth centuries in the Piedmont region profoundly altered fluvial geomorphology, resulting in the deposition of up to several meters of fine-grained “legacy” sediments above pre-existing wetland soils along many Piedmont valley-bottoms. Through subsequent dam breaching, the once-broad wetlands were converted into incised streams with unstable banks, primarily supporting weedy and non-native vegetation (Walter and Merritts, 2008; Hartranft et al., 2011; see Appendix 1 and Elliott et al., 2013 for additional information regarding historical background). To this day, Piedmont streams carry anomalously high concentrations of suspended sediments (Walter et al., 2007; Gellis et al., 2009; Pizzuto and O’Neal, 2009; Merritts et al., 2013; Voli et al., 2013), which contribute significantly to contemporary nutrient loading in downstream watersheds such as the Chesapeake Bay. The resulting algal blooms and eutrophication are detrimental to wildlife such as marine plants, algae, and benthic organisms (Orth and Moore, 1983; Pennock et al., 1994; Boesch et al., 2001; Stanley and Doyle, 2002; Kemp et al., 2005; Kennen et al., 2010; Merritts et al., 2010a; Niemitz et al., 2013; James, 2013; Sharpley et al., 2013; Hupp et al., 2015).

Damming, sediment accumulation, and later stream incision also significantly affected the floral assemblages in the riparian zone (Voli et al., 2009; Merritts et al., 2013; Appendix 1) and the valley-margin and upslope hardwood communities (Elliott et al., 2013), producing a landscape that contrasts starkly with the sluggish, low-gradient, pre-colonial wetlands (Hilgartner and Brush, 2006; Walter and Merritts, 2008). Ultimately, the increased distance to the water table, paired with the well-drained legacy sediments, excluded native wetland species whose roots could no longer reach the water table or extract moisture from the silty soils (Shafroth et al., 2002; Stanley and Doyle, 2003). Over time, plants better adapted to dry conditions, frequently exotic species, replaced the native wetland flora (Walter et al., 2007; Walter and Merritts, 2008, figure 3c; Voli et al., 2009; Gutshall and Oberholtzer, 2011; Kim et al., 2015). Loss of the native flora and subsequent invasion of weedy species continue to have substantial impacts on ecosystem function because riparian zones, especially those rich in hardwood trees, increase bank stability, serve as important sinks for sediments and nutrients, filter pollutants, and provide habitat for native fauna (Correll et al., 1992; FISRWG, 2008; Hartranft et al., 2011; Gutshall and Oberholtzer, 2011; Macfall et al., 2014).

Potential environmental remediation of the heavily settled Piedmont, as well as historical understanding of the riparian forests that once supported native and settler populations, ultimately depend on accurate botanical knowledge of the pre-colonial landscape. Unfortunately, virtually no historical accounts provide detailed records of the lost vegetation, which is now being reconstructed using paleobotanical data from buried, prehistoric wetland (hydric) soils preserved at a handful of sites (for additional information regarding the potential benefits of paleobotanical data for environmental remediation, see Elliott et al., 2013, and Appendix 2).

Previously published fruit and seed data from the hydric soil layer at Big Spring Run in Lancaster County, Pennsylvania (Chesapeake Watershed) indicate that the pre-settlement flora was rich in herbaceous wetland species, such as Carex (sedges), Polygonum (Knotweed), and Eleocharis (spikerushes), as well as occasional woody, non-wetland taxa interpreted to be from valley-margins, including Liriodendron tulipifera (Tulip Tree) and Juglans cinerea (Butternut; Voli et al., 2009; Hartranft et al., 2011). Radiocarbon dating of the recovered fossil seeds indicated that a patchwork of wetland environments containing the aforementioned species may have been widespread from at least 3200 ybp (years before present) until the arrival of European settlers approximately 300 years ago (Voli et al., 2009). However, presumably due to biases in fruit and seed preservation (e.g., Behrensmeyer et al., 2000), the Big Spring Run data provide a very limited view of woody riparian and upslope species.

In contrast, another recent study from Denlingers Mill, also in Lancaster County and the Chesapeake Watershed, detailed valley-margin and upslope hardwood communities based on 11 recovered species of pre-settlement subfossil leaves and some fruits, dating to the early 1700s (Elliott et al., 2013). Subfossil leaves are rarely used by paleontologists because of their extreme fragility, but because they are minimally transported and temporally mixed compared to more commonly studied seeds and pollen, they can provide detailed, localized views of past landscapes that are not usually available otherwise (see Appendix 3 for additional information regarding the use of leaves versus fruits, seeds, and pollen in this research). Elliott et al. (2013) was the first study that used subfossil leaves in this region. That work concluded that Red Maple-Black Ash Swamp forests and Oak-Beech mixed hardwood forests dominated the pre-settlement valley-margin and upslope hardwood communities, respectively. Elliott et al. (2013, figure 17) also provided a detailed artist’s reconstruction of the riparian, valley-margin, and upslope pre-settlement landscape reconstructed from paleobotanical data. The results from Elliott et al. (2013) demonstrated the significance of delicate, negligibly transported subfossil leaves for localized reconstructions of pre-settlement landscapes and the need for new subfossil leaf sites, such as White Clay Creek, to improve spatial understanding.

s figure1Here, we investigate a preliminary collection of leaf subfossils from buried wetland soils located directly beneath accumulated legacy sediments on White Clay Creek, Chester County, Pennsylvania, part of the Delaware Watershed (Figure 1; Miller, 2011). We consider our findings “preliminary” because of the relatively small sample size and fragmentary nature of the material so far collected from the field site (26 of 62 specimens were identifiable; Appendix 4). Our goals are to contribute critical spatial knowledge to our overall understanding of the pre-settlement, valley-bottom Piedmont landscape, and to test the emerging consensus that the pre-colonial riparian flora was much richer in wetland-affiliated hardwood species than today. Furthermore, knowledge of the pre-settlement flora can improve the success of stream, wetland, and floodplain restoration because plant assemblages directly impact wetland and fluvial geomorphology and hydrology (Richardson et al., 2007; Macfall et al., 2014; Appendix 2).


s figure2The study site is located in southeastern Pennsylvania on the eastern branch of White Clay Creek in Chester County, approximately 65 km W-SW of Philadelphia (39° 51.7’ N, 75° 47.0’ W; Figure 1, Figure 2) in the Piedmont physiographic province of the Appalachian Highlands. This region is composed of broad rolling hills and valleys underlain by both carbonate and schistose basement rock (Fenneman, 1938). The eastern branch of White Clay Creek drains through the Precambrian Cockeysville Marble, the Lower Paleozoic Wissahickon Schist, and various Lower Paleozoic gneisses (Blackmer, 2004). White Clay Creek is a 3rd order stream within the Christina River drainage system, which eventually feeds into the Delaware Bay. Land adjacent to the creek is approximately 52% open pasture, 22% agriculture, 3% residential, and 23% forested, the latter mostly in some stage of regrowth following restoration (Newbold et al., 1997).

A stratigraphic section at the study site was measured and described at the centimeter scale (Table 1) and was found to fit the composite profile of modified Piedmont streams (Walter and Merritts, 2008). Prior to examination, the stream bank was cleared, and a fresh vertical surface was exposed to ensure accurate descriptions of grain size, Munsell color, and presence or absence of cross strata and subfossils. The hydric soil layer (buried wetland), the source of all subfossils used in this study, is approximately 25 cm thick and overlies basal cobbles and schistose basement rock; it contains plant subfossils, including seeds, leaves, and twigs, especially within the lowest 7 cm. Above the hydric soil layer sit approximately 10 cm of rust-colored sandy clay, and above that lie approximately 60 cm of finely laminated, light-brown silt, in turn overlain by modern soil and vegetation.

Subfossil plant material was collected three times from October 2009 to October 2010. Blocks of the hydric soil layer that were especially fossiliferous were transported in stream water to the Sedimentology and Paleobotany laboratories at Penn State University, where they were stored in 50-50 ethanol and stream water.

Three leaf fragments, taken directly from the lower, middle, and top of the hydric soil layer, respectively (Table 1), were sent to the Center for Applied Isotope Studies at the University of Georgia for accelerator mass spectrometry (AMS, sample acronym UGAMS) radiocarbon dating (Table 2). Radiocarbon (carbon-14), with a half-life of 5,730 years, is produced in the atmosphere from the interaction of secondary cosmic ray neutrons with nitrogen-14. Radiocarbon mixes with non-radiogenic carbon, which together are assimilated by carbon molecules in living organisms. At death, carbon-14 disintegration is uncompensated, and the decay clock begins. As a general rule, the maximum duration since death can be determined to about five half-lives (ca. 30,000 years). Radiocarbon ages are reported in yr BP, which, unlike ybp, refers to the year 1950 CE as the reference date. Based on radiocarbon dating of fossil seeds and fruits, similar hydric soil layers in the Piedmont region have been dated to between 300 and 11,500 ybp (Walter and Merritts, 2008).

Leaves (and a few fruits) were cleaned of debris via alternating washes of 40% HCl (pH of ~1), to remove silicates, and Calgon liquid water softener (Reckitt Benckiser, Slough, Berkshire, England; pH of ~9) to remove organics. Acid washes were done over five to ten days. The Calgon washes involved soaking leaves and leaf fragments in a 30-50% solution for three to seven days; this product contains a polycarboxylate that prevents re-deposition of organics by interfering with the electrostatic interactions between clay particles and the leaf surface, while not destroying leaf tissue (Blockhaus et al., 1996; Traverse, 2008). The washes were repeated as necessary, up to three repetitions per sample, until the leaf surface was greater than 90% clear. We tried sonication as an alternate, rapid method for debris removal, but this unacceptably damaged the leaves.

Immediately prior to mounting, leaf fragments were dehydrated in a graded series of baths, increasing from 50% to 100% ethanol. As a final dehydration step, leaf fragments were placed in two xylene baths for five minutes each. Leaves were then mounted on glass slides using Cytoseal 280 High Viscosity Mounting Medium (Richard Allen Scientific Inc., Kalamazoo, Michigan, USA), when possible with the abaxial surface facing upwards to highlight venation. The total sample of mounted subfossil specimens was 60 leaves and two fruits. All specimens are deposited in the Earth and Mineral Sciences Museum of Pennsylvania State University (EMS; Appendix 4).

Once mounted, each sample was viewed using transmitted and epifluorescent light with both a Nikon SMZ-1500 stereomicroscope and a Nikon LV100 compound microscope (Nikon, Melville, New York, USA), an X-Cite 120 Epifluorescence Illumination Unit (EXFO Electro-Optical Engineering, Quebec City, Quebec, Canada), and an Endow GFP Longpass Emission Green Filter (Chroma Technology Number 41018, exciter HQ470/40x, diachronic Q49LP BS, emitter HQ500LP, Chroma Technology, Rockingham, Vermont, USA), then photographed using a Nikon Digital Sight DS-Ri1 camera with Nikon NIS Elements v. 3 Basic Research software. Adobe Photoshop CS5 (Adobe Systems Incorporated, San Jose, California, USA) was used to compose stacked or stitched composite images when necessary.

Leaf specimens were described following Ellis et al. (2009), supplemented with Stearn (2004); because samples were fragmented, not all characters could be described for all specimens. Additionally, foliar trichomes found on abaxial surfaces were used to improve identifications, especially within the family Betulaceae and genera Quercus and Salix, using the Atlas of Foliar Surface Features in Woody Plants I, VIII, and IX (Hardin, 1979; Hardin and Johnson, 1985; Hardin and Bell, 1986). Noting that trichomes are typically lost during fossilization, only the presence, not the absence, of particular trichome types was used to increase taxonomic resolution.

Cleared leaf images from the Jack A. Wolfe USGS National Cleared Leaf Collection, housed at the National Museum of Natural History of the Smithsonian Institution, and from the Daniel Axelrod Cleared Leaf Collection, housed at the University of California Museum of Paleontology, Berkeley, as well as mounted leaves from PW’s York County, Pennsylvania collections (Wilf, 1997) were used as references for identification. Because it was unlikely that the pre-settlement flora contained exotic or invasive species, only species native to Pennsylvania and surrounding states were considered in this study. Classifications follow Angiosperm Phylogeny Group III (APG III, 2009).


Radiocarbon dating

Calibrated radiocarbon results for three samples collected from the base, middle and top of the fossiliferous layer indicate deposition between 311 ± 22 and 282 ± 15 yr BP (before 1950; i.e., between 1639 and 1668 C.E.; Table 2). The mean probability age for the subfossil dated from the middle portion of the hydric soil layer is temporally displaced compared to the sample from the basal layer (see Table 2 notes), possibly indicating local reworking. However, the base and top subfossils yielded identical measured 14 C ages (Table 2) and, further, each of the three samples yielded multiple intercepts on the calibrated radiocarbon curve of Reimer et al. (2013). The one intercept in common among these three samples, which agree at the 2σ level of confidence, produced tightly constrained calibrated ages shown in Table 2. For this reason, we consider all paleobotanical samples as a single, lumped assemblage. The resulting temporal averaging is minimal because the leaves were likely deposited in a short period of time around 300 +/- 20 yr BP (i.e., 1650 C.E.). No permanent European settlements existed in Pennsylvania prior to 1638 (Weslager, 1955), and the leaf layer lies immediately underneath colonial-era legacy sediments. The combined evidence indicates that the leaves were deposited immediately prior to, or during the initial stages of, European settlement in the local area. We interpret that this leaf mat horizon was deposited in a shallow pool in or near the valley margin of a widespread pre-settlement wetland.

White Clay Creek subfossil flora

The preliminary subfossil assemblage described below is composed of seven hardwood taxa with a diverse range of wetland affiliations, indicating that the leaves and occasional fruits originated from both the riparian zone and surrounding lower hill slopes. Alnus serrulata (Hazel Alder) and Salix (willow) have either wetland-obligate or facultative-wetland indicator status, meaning that they occur in wetlands 67 to 99% of the time. Acer negundo (Box Elder) is the only facultative species, signifying that it is equally likely to represent wetland and upland environments. Four taxa, namely the red and white oaks (Quercus Section Quercus, Q. Section Lobatae), Tulip Tree (Liriodendron tulipifera), and American Beech (Fagus grandifolia) are considered facultative-upland, meaning they occur in uplands 67-99% of the time and, therefore, have a reduced chance of being part of a wetland or riparian forest assemblage.

Family BETULACEAE Gray, 1821
Genus ALNUS Miller, 1754
Alnus serrulata
Aiton, 1789) Willdenow, 1805
Figure 3

s figure3Material. EMS 425002.

Description. Laminar size microphyll, length to width ratio 4:3. Laminar shape unlobed elliptic, with medial symmetry; base not preserved. Primary venation pinnate. Major secondary veins craspedodromous with excurrent attachment to midvein, spacing smoothly decreasing proximally. Intercostal tertiary veins opposite percurrent, convex or sinuous, perpendicular to midvein, angle consistent. Epimedial tertiary veins opposite percurrent, proximal course obtuse to midvein, distal course parallel to intercostal tertiary. Quaternary vein fabric irregular reticulate. Areolation moderately developed. Freely ending veinlets mostly unbranched, to 2-branched. Tooth spacing regular, tooth sinuses angular. Distal tooth flank apically concave and basally convex, tooth proximal flank convex. Leaf surface with simple stipitate glands and peltate scale trichomes, trichomes denser at vein junctions.

Discussion. The subfossil has several features of living Alnus serrulata (Hazel Alder), including strong, non-branching, regularly spaced, approximately alternate secondary veins; very thin, opposite percurrent tertiary veins (Figure 3.1); finely serrate leaf margins (Figure 3.1, 3.4); and freely ending veinlets that are usually unbranched (Figure 3.6). The subfossil leaves are similar in overall morphology to other species in the family Betulaceae, especially American Hornbeam (Carpinus caroliniana). However, the presence of both stipitate gland and peltate scale trichomes (Figure 3.2, 3.3, 3.5) indicate that it is a member of the genus Alnus (Hardin and Bell, 1986), and its regular, finely serrate teeth distinguish it from other Pennsylvania members of this genus (Rhoads and Block, 2007).

Hazel Alder is native to eastern North America, ranging from Texas to northwest Maine, New Brunswick, and Quebec (United States Department of Agriculture, 2011). It is considered to be an obligate wetland species that grows best at stream margins and in other wet areas including swamps and bogs, although it may also grow on well-drained upland soils (Rhoads and Block, 2007; United States Department of Agriculture, 2011). This species has a rapid growth rate and a high fire tolerance; adult individuals reach a maximum height of approximately nine meters (United States Department of Agriculture, 2011).

Family FAGACEAE Dumortier, 1829
Genus FAGUS Linnaeus, 1753
Fagus grandifolia
Ehrhart, 1788
Figure 4

s figure4Material. EMS 425003, EMS 425004 (Figure 4.1-3, 4.7), EMS 425005 (Figure 4.5).

Description. Lamina elliptic, unlobed, medially symmetrical. Primary venation pinnate. Major secondary veins craspedodromous, attachment to midvein excurrent, spacing regular. Intercostal tertiary veins opposite percurrent, sinuous or occasionally concave, acute to the midvein, angle consistent. Epimedial tertiary veins opposite percurrent, proximal course perpendicular to midvein, distal course parallel to intercostal tertiaries. Quaternary vein fabric mixed percurrent. Areolation moderately developed. Tooth spacing not visible. Distal tooth flank concave; proximal tooth flank flexuous; sinus rounded. Principal vein present. Surface puberulent; trichomes unicellular simple and solitary, with higher densities along major veins and at vein junctions.

Discussion. Observed features that are characteristic of Fagus grandifolia (American Beech) leaves include: regularly spaced secondary veins and opposite-percurrent, low-gauge tertiary veins (Figure 4.1, 4.2); teeth with slightly rounded apices and rounded sinuses that occur approximately once per secondary vein (Figure 4.5); and unicellular, simple, solitary trichomes concentrated along major veins and vein junctions (Figure 4.3, 4.4, 4.7). The subfossils appear similar to other Pennsylvania species of Fagaceae, including Quercus muhlenbergii (Chinkapin Oak)and Castanea dentata (Chestnut), but they are distinguishable from trichome types and tooth morphology. The leaf surface of C. dentata generally lacks the simple trichomes seen in F. grandifolia, and it instead may possess fasciculate trichomes not seen in the latter (Hardin and Johnson, 1985). Additionally, leaves of F. grandifolia lack the incurved teeth of Q. muhlenbergii (Rhoads and Block, 2007).

American Beech is native to eastern North America, ranging from Texas, Oklahoma, and Minnesota, east to the Florida panhandle, and north to Quebec, with isolated populations in Utah (United States Department of Agriculture, 2011). Adult individuals typically measure 20-24 m in height (Coladonato, 1991) and frequently reproduce asexually, forming patches or colonies (Rhoads and Block, 2007). The species is considered to be facultative-upland, but it also grows well in valley-bottoms, generally in moist soils (Coladonato, 1991; Rhoads and Block, 2007; United States Department of Agriculture, 2011).

Genus QUERCUS Linnaeus, 1753
Quercus Section Lobatae Loudon, 1830
Figure 5

s figure5Material. EMS 425010, EMS 425011 (Figure 5.1-4, 5.6), EMS 425012-425013.

Description. Lobe apices acuminate, angle acute. Inferred major secondary veins craspedodromous; fimbrial vein present, exterior tertiaries looped. Quaternary and higher-order vein fabric random to regular reticulate. Areolation well-developed; freely ending veinlets mostly one-branched. Leaf surface with a few small trichomes on the secondary veins. Stomata randomly oriented, guard cell junctions in T-configuration.

Discussion. These fragments are interpreted as asymmetrical lobe tips with acute apices, fimbrial veins, and marginal irregularities at likely sites of bristle-teeth that were broken off during preservation (Figure 5.1). Only a few, small trichomes persist on the secondary veins (Figure 5.3, 5.4). Stomata are randomly oriented (Figure 5.2, 5.3), and the junction of two guard cells of an individual stoma creates a characteristic T-shape (Figure 5.5, 5.6). These features collectively indicate membership in the red oak group (Quercus Section Lobatae) and, in Pennsylvania, exclude the unlobed species Q. phellos (Rhoads and Block, 2007); however, species-level identification is not possible. The ten species in the red oak group that are native to Pennsylvania vary widely in their environmental preferences (Rhoads and Block, 2007; United States Department of Agriculture, 2011), and without further resolution, these subfossils do not refine environmental interpretation. With the exception of Q. ilicifolia, a shrub, the Pennsylvania species are trees reaching adult heights of 20 -30 meters (Rhoads and Block, 2007).

Quercus Section Quercus Linnaeus, 1753
Figure 6

s figure6Material. EMS 425006-425007, EMS 425008 (Figure 6.2), EMS 425009.

Description. Acute, retuse, lobe apices. Primary venation not preserved. Inferred major secondary vein craspedodromous. Fimbrial vein present. Exterior tertiary veins looped or terminating at margin. Quaternary to 6th -order vein fabric irregular reticulate.

Discussion. These fragments are characterized by an entire margin with a fimbrial vein, and a retuse, asymmetrical lobe apex (Figure 6.1). Secondary veins terminate at the lobe apex, and exterior tertiary veins are looped with inconsistent vein angles. Trichomes are uncommon but can be seen scattered across the leaf surface. Species native to Pennsylvania within the white oak group (Quercus Section Quercus) generally have rounded lobe apices, distinguishing them from the bristle-tipped red oak group (Q. Section Lobatae; Rhoads and Block, 2007). The subfossil specimens are inferred from their preserved venation asymmetry to represent rounded lobe apices, indicating both that they belong to the white oak group and that they cannot be Q. muhlenbergii (Chinkapin Oak), which is toothed and unlobed or shallow-lobed (Rhoads and Block, 2007). The apparently glabrous leaf surface suggests that the fragments may represent Q. alba (White Oak), however, due to the small amount of tissue preserved, the specimens cannot definitively be identified to species level.

Seven species within the white oak group are native to Pennsylvania and occur within a broad range of environments (Rhoads and Block, 2007; United States Department of Agriculture, 2011). The majority of species, including Quercus alba (White Oak), Q. macrocarpa (Bur Oak), Q. stellata (Post Oak), Q. prinoides (Dwarf Chestnut Oak), Q. muhlenbergii (Chinkapin Oak) and Q. montana (Chestnut Oak), are generally found in non-wetland communities such as hill slopes, ridges, and dry to moist woodlands (Rhoads and Block 2007; United States Department of Agriculture, 2011). However, Swamp White Oak (Quercus bicolor), has a similar leaf morphology to the non-wetland species, but occurs in very different habitats, being frequently found along rivers, on the edges of swamps, and in forested wetlands (Snyder, 1992).

With the exception of Q. prinoides, which is usually a shrub, white oak group species are trees growing to approximately 20-30 meters in height (Rhoads and Block, 2007). These species vary in their tolerance to shade, salinity, and fire (United States Department of Agriculture, 2011), as well as their wetland indicator statuses (Rhoads and Block, 2007; United States Department of Agriculture, 2011). Therefore, no environmental interpretations were based on these subfossils.

Family MAGNOLIACEAE Jussieu, 1789
Genus LIRIODENDRON Linnaeus, 1753
Liriodendron tulipifera Linnaeus, 1753
Figure 7

s figure7Material. EMS 425015 (Figure 7.1-7.2), EMS 425014 (Figure 7.3).

Description. Samara, elongate, tip mucronate, at the basal seed cavity curving upward and thickened, forming a ridge (Figure 7.2).

Discussion. Liriodendron tulipifera (Tulip Tree) samaras superficially resemble those of various species of ash (Fraxinus spp.). However, ash samaras are flat and unridged, unlike those of L . tulipifera and the subfossils, which are curved and ridged (Figure 7.2; McCutchen, 1977; Rhoads and Block, 2007).

Tulip Tree is native to the eastern half of the United States, with isolated populations in Texas. This species has a fast growth rate, and adult individuals typically reach 24-36 meters in height (Rhoads and Block, 2007; United States Department of Agriculture, 2011). Tulip Tree is considered to be a facultative-upland species. It grows well in moist, well drained, neutral to acidic soils and prefers mesic environments (Beck, 1990). It cannot tolerate very wet or dry soils, is shade intolerant, and generally appears early in succession (Beck, 1990; United States Department of Agriculture, 2011).

Family SALICACEAE Mirbel, 1815
Genus SALIX Linnaeus, 1753
Salix spp.
Figure 8

Material. EMS 425022 (Figure 8.1), EMS 425017-425020, EMS 425021 (Figure 8.2, 8.4), EMS 425023 (Figure 8.3), EMS 425024-525027.

s figure8Description. Lamina unlobed, medially symmetrical. Apex straight, angle acute. Base convex to straight, angle acute. Primary venation pinnate. Major secondary veins semicraspedodromous, spacing and angle inconsistent, attachment to midvein excurrent. Intersecondary veins less-than-one per intercostal area, proximal course acute to midvein, distal course reticulating. Intercostal tertiary veins convex, opposite percurrent to irregular reticulate, obtuse to midvein. Epimedial tertiary veins opposite percurrent to reticulate. Areolation poorly to moderately developed, freely ending veinlets mostly one branched. Tooth spacing regular to irregular, tooth sinuses rounded. Teeth salicoid; principal veins present. Leaf surface without trichomes preserved, possibly glabrous.

Discussion. The subfossils have distinctive salicoid teeth, consisting of one round, dark, non-deciduous seta attached to the tooth apex (Figure 8.4; Hickey and Wolfe, 1975), that place them confidently in Salicaceae. Only two genera of Salicaceae are native to Pennsylvania (Salix, willows, and Populus, cottonwoods and aspens; Rhoads and Block, 2007), and these are readily distinguished because Populus leaves are generally about as wide as they are long, whereas Salix leaves are typically at least two times longer than they are wide (Rhoads and Block, 2007), as seen in the subfossils (Figure 8.1-3). The specimens display both regularly and irregularly spaced teeth. The teeth also vary in orientation and size.

Willows (Salix spp.) are difficult to identify to the species level using leaves alone because a large amount of hybridization occurs between species, and because the typical species-level diagnostic features are not preserved here, such as leaf attachment, catkin morphology, and branching patterns (Argus, 2006). The samples might represent a single or multiple Salix species. Salix species are widely distributed across the world and are generally affiliated with wetland conditions, but they can also grow in drier, upland environments. However, only one willow species native to Pennsylvania, the Prairie Willow (S. humilis), is a facultative-upland species (United States Department of Agriculture, 2011). That species has variable leaf form, but it frequently has entire margins (Rhoads and Block, 2007) and a tomentose abaxial leaf surface (Argus, 2006; Rhoads and Block, 2007), causing it to appear hairier than many other taxa within the genus. Because the subfossils appear quite different from S. humilis in these and other characteristics, we infer that the prehistoric willows were affiliated with a wetland environment.

Family SAPINDACEAE Jussieu, 1789
Genus ACER Linnaeus, 1753
Acer negundo Linnaeus, 1753
Figure 9

Material. EMS 425016 (Figure 9.1-3)

s figure9Description. Inferred lateral leaflet, petiolulate, lamina unlobed, ovate, medially asymmetrical with basal width asymmetry. Laminar size nanophyll, length to width ratio 2:1. Base angle obtuse, base shape convex. Apex angle acute, apex shape acuminate. Primary venation pinnate. Major secondary veins semicraspedodromous, irregularly spaced, angle decreasing proximally on one side, attachment to midvein excurrent. Intercostal tertiary veins irregular reticulate. Epimedial tertiary veins reticulate. Higher-order venation indistinct. Tooth spacing irregular with one order of teeth; principal veins present. Tooth sinuses angular to slightly rounded; both distal and proximal flanks basally convex and apically concave. Trichomes simple, restricted to midvein, secondary veins, and leaf margins, increasing in density approaching tooth bases, with no hairs directly above the tooth apex.

Discussion. As seen in the subfossil (Figure 9), Acer negundo (Box Elder) is characterized by asymmetrical, irregularly toothed to shallow-lobed, petiolulate lateral leaflets and simple trichomes that occur only along the midvein, secondary veins, and at leaf margins. Juvenile Acer negundo leaflets may be mistaken for poison ivy (Toxicodendron radicans; United States Department of Agriculture, 2011). Leaflet morphology in both species can be highly variable, making them difficult to distinguish, and both species have marginal trichomes. However, unlike the subfossil, poison ivy leaflets that are toothed usually only have a single or few irregularly-sized teeth, and these have straight or convex, not acuminate, flanks.

Box Elder is a fast-growing, short-lived tree that reaches an average height of approximately 18 meters (United States Department of Agriculture, 2011; Overton, 1990). It has a broad geographic range throughout the eastern two-thirds of the United States and Canada, with isolated populations as far south as Guatemala (Overton 1990). It is considered to be a facultative species with a slight affiliation to wetlands (United States Department of Agriculture, 2011). Acer negundo may grow in nearly any soil type but is frequently found in relatively flat areas near streams (Overton, 1990).


This study identifies seven hardwood taxa that inhabited the Piedmont wetlands and valley-margins surrounding White Clay Creek before European settlement in eastern North America. Based on previous work (Walter and Merritts, 2008; Voli et al., 2009; Elliott et al., 2013), we hypothesized that the pre-settlement assemblage would represent the riparian and lower-slope hardwood tree communities and be rich in obligate and facultative-wetland species. Although multiple wetland tree species are indeed represented at White Clay Creek, the paleofloral assemblage also contains facultative-wetland, facultative, and facultative-upland species, indicating leaf litter input from multiple topographic sources. Additionally, nearly all the species in the pre-settlement assemblage are not present at the site today, which is dominated by weedy vegetation, indicating that anthropogenic activities significantly altered the floral communities in this region.

Paleocommunity interpretation and comparison

The White Clay Creek floral assemblage, at face value, does not match any single modern-day forest community. Presumably, the identified taxa represent the preservational mixing of more than one forest type. However, when combined with previously published data from similar nearby sites (Table 3), it becomes possible to fit the data into reconstructions of pre-settlement forest communities.

Walter and Merritts (2008) hypothesized that the modern, single-channel, meandering streams in the northeastern United States seen today were once the locations of broad, tussock-sedge wetlands. The fossil fruit and seed assemblage from Big Spring Run, rich in herbaceous wetland plants (Voli et al., 2009), lends support to this hypothesis. These environments were apparently dominated by herbaceous, wetland-obligate species such as Carex, Polygonum, Eleocharis, Scirpus, Najas, and Brasenia (Voli et al., 2009). However, even though this type of community generally has few shrubs and is entirely devoid of trees (Westervelt et al., 2006), Voli et al. (2009) also reported remains of woody upland taxa including Liriodendron tulipifera (Tulip Tree) and Juglans cinerea (Butternut), suggesting some input from local slope environments. From the Denlingers Mill site, Elliott et al. (2013) expanded the pre-settlement interpretation by recovering more valley-margin to upslope species, including Fraxinus nigra (Black Ash), Acer rubrum (Red Maple), Platanus occidentalis (American Sycamore), Ostrya virginiana (Eastern Hophornbeam), Betula lenta (Sweet Birch), Acer spicatum (Mountain Maple), and Castanea dentata (American Chestnut).

Despite the physical and historical similarities, there is limited overlap in represented species among the three floras (Table 3). These differences do not necessarily indicate that the sites represent dissimilar forest communities. Instead, they more likely provide snapshots across a similar paleo-landscape, from the inundated wetlands to the drier upper hill slopes, due to varying paleotopography and the contrasting taphonomic pathways of the plant organs (Appendix 3). We note that Denlingers Mill is located in a narrow, geologically-incised part of the valley. An unusual feature of Denlingers Mill not seen at White Clay Creek is a bedrock spur immediately overhanging the leaf layer that presumably was also present in the past, when it supported many of the trees there preserved; this interpretation accounts for the significant representation of upslope species at that site (Elliott et al., 2013).

Based on all available paleobotanical data, the regional valley-margin and lower-slope hardwood communities were probably most similar to either a Red Maple-Tussock Sedge wooded marsh or a Red Maple-Black Ash deciduous swamp forest, which in modern environments both frequently border tussock sedge meadows (Fike, 1999; Westervelt et al., 2006). The most likely analog candidate is the Red Maple-Black Ash swamp forest because it typically has a sedge-dominated understory, and in addition to the two dominant namesake species, this community frequently contains Betula spp., Quercus spp., and Salix spp. as canopy taxa and Alnus serrulata as understory vegetation (Westervelt et al., 2006). Today, this forest community type can be found in the Northern Piedmont, High Allegheny Plateau, and Central Appalachians ecoregions (Westervelt et al., 2006).

The regional pre-settlement upper-slope forest community was probably most similar to either a modern day Northern Piedmont Mesic Oak-Beech Forest or a Red Oak-American Beech Forest. The Mesic Oak-Beech forest is dominated by Liriodendron tulipifera, Fagus grandifolia, and Betula lenta; and, to a lesser extent, Quercus rubra and Q. alba; it is common on gently sloping hills in the Piedmont physiographic province (Westervelt et al., 2006). The Red Oak-American Beech forest, on the other hand, is a broadly defined community that also occurs on mesic sites, but it is rather variable in composition, with dominant canopy species such as Quercus spp., F. grandifolia, and Acer rubrum, and typical subcanopy species including B. lenta, L. tulipifera, and Ostrya virginiana (Fike, 1999; Westervelt et al., 2006).

Comparison to the modern White Clay Creek flora

Although all seven identified taxa reported here from White Clay Creek are hardwood species native to Pennsylvania, only Liriodendron tulipifera is present in the area today. Instead, weedy species dominate the local riparian vegetation. The area immediately adjacent to the stream, up to three meters from the bank, has no trees or small shrubs. Common taxa in this strip include Jewelweed (Impatiens capensis) and species of Rubus and Solidago (Figure 2). Farther from the stream bank (three to fifteen meters), the vegetation is composed almost entirely of brambly taxa, and although some tree species are present (e.g., L. tulipifera, Fraxinus americana, and exotics such as Ulmus parvifolia and Styphnolobium japonicum), many individuals have been either purposely girdled by humans or are choked with blackberry brambles. This type of vegetation is typical of highly disturbed environments and close proximity to roads and residential areas. All tree species present are either non-native or have facultative-upland affiliations, i.e., L. tulipifera and F. americana. No woody wetland taxa are present, probably due to the well-drained soil and the large (>1 m) distance between the topsoil and the water table.


The White Clay Creek flora contributes to our overall understanding of the pre-settlement valley-bottom and lower-slope environments by reinforcing results from previously studied paleobotanical sites in southeastern Pennsylvania and through the addition of new species thus far not represented elsewhere, including Acer negundo (Box Elder) and Alnus serrulata (Hazel Alder). Species from at least two different communities, a valley-bottom wetland and an upper slope, are represented in the subfossil assemblage, and nearly all the recovered taxa are absent from the weedy, mostly non-native vegetation present at the study site today. This change is attributed primarily to the results of European settlement in the region, specifically the construction, use, and abandonment of tens of thousands of milldams, as well as to subsequent land use.

The White Clay Creek flora provides a preliminary view of the pre-European settlement forests of Chester County and, in combination with emerging data from other sites, shows which native tree species were once present and could potentially be restored in the area. Restoration efforts that make use of direct paleobotanical evidence for the hardwood species that are best adapted to the landscape should hold the greatest potential for long-term success in the region, including a reduction in legacy sediment loads that cause eutrophication in fragile, downstream estuaries such as Delaware Bay and Chesapeake Bay.


We thank I. Grettenberger for assistance with field work and S. Little, M. Carvalho, and R. Coope for help in developing sample cleaning and identification methods. We also thank our colleagues at the Stroud Water Research Center, especially L. Kaplan and A. Aufdenkampe, for their support during our field work activities on White Clay Creek. Funding supporting this work came from the P.D. Krynine Memorial Fund of the Penn State Department of Geosciences and a Geological Society of America Student Research Grant (to CLG), and the David and Lucile Packard Foundation (to PW). This research partially completed requirements for a Masters in Geosciences for CLG at Pennsylvania State University, 2011.


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