Minnesota Geological Survey (MGS) Open File Report 06-04 (Open File Reports are not subjected to conventional MGS editorial standards)
A HYDROGEOLOGIC AND MAPPING INVESTIGATION OF THE ST. LAWRENCE FORMATION IN THE TWIN CITIES METROPOLITAN AREA
Runkel, A.C., Mossler, J.H., Tipping, R.G., and Bauer, E.J. Minnesota Geological Survey 2642 University Ave W., St. Paul, Minnesota 55114-1057
EXECUTIVE SUMMARY
This report summarizes the results of a two year project conducted by the Minnesota Geological Survey to map the Upper Cambrian St. Lawrence Formation and investigate its hydrologic properties in the Twin Cities Metropolitan area (TCMA). Funding was provided by the Minnesota Department of Health. Final products are a map delivered in electronic format that can be used with Arcview 3.2 GIS software, and this informal report. Our hydrogeologic study indicates that the St. Lawrence Formation commonly has a moderate to high horizontal hydraulic conductivity across all of the study area. In conditions of shallow burial beneath younger bedrock it is most similar in the development of secondary pores and measured hydraulic properties to fractured carbonate rock aquifers. Discrete intervals with secondary pores have a high horizontal hydraulic conductivity whereas rock between these intervals are orders of magnitude lower in conductivity. The properties of the St. Lawrence Formation in a vertical direction are not as well- understood, but available data are consistent with the traditional classification of the formation as an aquitard. However, the integrity of the formation as an aquitard in a vertical direction, particularly under conditions of shallow burial such as where it is uppermost bedrock, has not been rigorously tested, and may be markedly variable across the TCMA. This is chiefly because vertical fractures play an important role in determining aquitard integrity, and the distribution of such fractures is poorly understood. Suggestions for additional research that might lead to a better understanding of aquitard integrity are made at the end of this report.
INTRODUCTION
This report summarizes the results of a two year project by the Minnesota Geological
Survey (MGS) to map the Upper Cambrian St. Lawrence Formation (Figs 1 and 2) and
investigate its hydrologic properties in the Twin Cities Metropolitan area (TCMA). Funding was
provided by the Minnesota Department of Health (MDH), and the project is informally referred
to as the “MDH-St. Lawrence Project”. The St. Lawrence Formation is a relatively fine-grained,
siliciclastic and carbonate unit that is widely considered to function as a low-permeability
1 aquitard in the Paleozoic bedrock aquifer system of southeastern Minnesota (e.g. Kanivetsky,
1978; Runkel and others, 2003). Such layers can serve to protect underlying aquifers from contamination. Minnesota state water-well construction regulations are designed to maintain the integrity of such aquitards, and therefore prohibit full penetration of the St. Lawrence Formation in an open borehole.
Despite the potential importance of the St. Lawrence Formation as an aquitard, its subcrop distribution across the TCMA, and its hydrologic properties, are poorly known compared to many other bedrock hydrogeologic units. Prior to this investigation the St. Lawrence Formation was mapped as a distinct unit only in Scott County (Olsen, 1982) and mapped in combination with the Franconia Formation elsewhere. Furthermore, the formation is widely used as a source of water to domestic wells in the TCMA, which is seemingly inconsistent with its characterization as a low-permeability aquitard. Many of these wells are constructed in a manner that is not in accordance with current MDH regulations designed to protect the integrity of aquitards. This investigation was initiated to better depict the subcrop distribution of the St.
Lawrence (Fig 1) using traditional subsurface mapping techniques, and to use this map along with hydrogeologic research to better understand the formation’s water-bearing properties. Such information will provide the basis for more effective regulatory management. John Mossler,
Emily Bauer, and Anthony Runkel produced the subcrop map of the St. Lawrence Formation, whereas Runkel and Robert Tipping conducted the hydrogeologic investigation.
SUBCROP MAP OF THE ST. LAWRENCE FORMATION
The St. Lawrence Formation is a thin, heterolithic sedimentary rock unit that occupies a position near the middle of the Paleozoic bedrock sequence of the Twin Cities basin (Fig. 2), a broad regional depression developed in Lower Paleozoic sedimentary strata in the metropolitan area
2 (Mossler, 1972). The formation was mapped where it subcrops beneath Quaternary glacial deposits and Holocene alluvium along western, northern, and eastern margins of the Twin Cities basin, an area that includes parts of Scott, Carver, Hennepin, Anoka, Chisago, Dakota, and
Washington counties (Fig. 1).
The map shown schematically in Fig. 1 was delivered to MDH in electronic format that can be used with Arcview 3.2 GIS software. It is designated MGS Open File Report 06-05 (Mossler and others, 2006). The Scott County part of the map was constructed by Anthony Runkel as part of a separate mapping project specifically for that county that was conducted at the same time as the MDH-St. Lawrence project. John Mossler was the primary mapper for the remaining part of the study area, and together with Emily Bauer compiled the final map.
Exposure of the St. Lawrence Formation in the TCMA is limited to very small outcrops in western Scott County along the Minnesota River valley, and along the St. Croix River in eastern
Washington and Chisago counties. Across most of the TCMA the St. Lawrence is buried beneath younger Paleozoic formations and unconsolidated Quaternary and Holocene sediment. Its subcrop distribution is therefore based almost entirely on subsurface mapping methods that utilized natural gamma logs, cuttings sets from water wells, engineering test borings logs, and water well construction records.
The St. Lawrence Formation is heterolithic, composed of interbedded very fine-grained sandstone, siltstone, shale, and dolostone (Fig. 3). Dolostone is more abundant in the lower one- half of the formation than in the upper one-half. The formation thickens from the northeast to the southwest across the TCMA. In northern Anoka and Washington Counties it is about 30 to 40 feet thick; in southwest Scott County it is as thick as 90 feet. An increase in thickness and
3 number of dolostone beds, and inclusion of glauconitic sandstone interbeds in the lower part of the St. Lawrence Formation largely accounts for this trend (Fig. 3).
The upper contact of the St. Lawrence Formation with the overlying Jordan Sandstone is conformable and gradational. The lower 5 to 30 feet of Jordan Sandstone is composed largely of very fine- to fine-grained feldspathic sandstone which overlies interbeds of feldspathic, very fine
grained sandstone, siltstone and shale in the upper St. Lawrence. Selecting a precise contact
between these formations in a consistent fashion from site to site can therefore be problematic.
For example, the contact between these formations occurs on natural gamma logs along a
gradual shift from relatively high to relatively low gamma counts up-section (Fig. 3). The contact
on such logs is typically chosen within the lowermost approximately five feet of this shift.
Drillers descriptions on water-well records generally indicate a downward change from relatively
soft sandstone to harder, and finer-grained (siltstone, shale, or dolostone) rock across the Jordan
Sandstone-St. Lawrence contact interval. Drill records commonly also indicate a color change,
typically from white or light gray for the Jordan Sandstone, to green, pink or red for the St
Lawrence Formation.
The basal contact of the St. Lawrence Formation with the underlying Franconia Formation is
lithically more variable than its upper contact, but in a manner that is generally predictable across
the TCMA. The contact in the northern part of the TCMA (Anoka, Chisago, and northern
Washington and Hennepin counties) is characterized by siltstone and silty dolostone in the lower
St. Lawrence overlying fine- to medium-grained sandstone of the Mazomanie Member of the
Franconia Formation. Drillers’ logs from this area typically include a description of this lithic
change, and natural gamma log curves show a distinct deflection from high gamma counts in the
feldspathic siltstone in the St. Lawrence to low gamma counts in the quartzose sandstone of the
4 Mazomanie (Fig. 3). In the central and southern TCMA area the St. Lawrence Formation
commonly overlies glauconitic and feldspathic very fine-grained sandstone of the Reno Member
of the Franconia Formation. The natural gamma log signatures for the two formations are similar
to one another, and the precise contact may be hard to ascertain without well cuttings. It is
particularly difficult to interpret geophysical logs from holes in this area where there is only a very short interval of bedrock penetrated. Additionally, the two formations interfinger, with the lower St. Lawrence Formation containing interbeds of glauconitic sandstone that are similar to the Reno member of the Franconia Formation. Scott County and southern Carver County are the most problematic areas in this regard. The contact between the two formations in those counties is picked at the base of the lowest dolostone beds, which have gamma radiation intensities lower than underlying sandstone of the Reno Member of the Franconia. This contact interval on drillers’ logs is typically expressed as a change from hard, gray or pink St. Lawrence Formation to softer, green sandstone of the Reno member, but the stratigraphic position of such a change is commonly inconsistent from record to record.
Bedrock in the Twin Cities Metropolitan area is highly dissected by pre-glacial and inter- glacial stream valleys that are buried beneath subsequent layers of glacial drift, as well as the deposits of present day streams. One of the challenges of mapping bedrock geology in heavily glaciated terrains is ascertaining where buried valleys are located. This is done by contouring the elevation of the top of bedrock based on well records, engineering test borings, and bedrock
outcrops. Alignments of present day low-lying areas occupied by chains of lakes and marshes
and minor streams are helpful in determining the axis of some of the buried valleys because these
features commonly lie along them. Deep wells that bottom in Quaternary sand and gravel are
5 also useful because many are located within buried valleys and, though they do not enter bedrock, they indicate where the axes of valleys may lie.
Interpretation of the distribution of the St. Lawrence Formation in the Twin Cities area is highly dependent on the quality of data and contouring of the bedrock surface. Placement of the valleys and their width influence the distribution pattern of the formation because it commonly subcrops along valleys and bluffs. Therefore the density of well control is important in assessing accuracy of the map. In areas where there are abundant wells, there is a smaller chance for interpretive errors. The mapped width of the valleys also is affected by the amount of well control. Valleys are probably contoured wider than they actually are in areas where there is sparse control.
In much of Anoka County, the St. Lawrence Formation is present as a thin, well-indurated caprock that overlies friable sandstone (the Mazomanie Member of the Franconia Formation), analogous to the Platteville Formation caprock on top of St. Peter Sandstone elsewhere in southeastern Minnesota. Therefore, in a manner similar to the Platteville farther southeast, the St.
Lawrence caps the tops of numerous small outliers or mesas (Fig. 1). Toward the south, where the St. Lawrence Formation contains more abundant, thicker beds of dolostone, the formation commonly forms plateaus of markedly greater extent, in a manner similar to plateaus of Prairie du Chien Group dolostone that cap the Jordan Sandstone in southeastern Minnesota.
Faults are common in the Paleozoic rocks on the southeastern, northwestern, and western margins of the Twin Cities basin. They are recognized by geographically abrupt changes in the elevation of bedrock formation contacts. The faults are related to older faults within the
Proterozoic rocks of the Midcontinent rift zone that were reactivated during and after Paleozoic time. Such faults locally have a pronounced impact on St. Lawrence formation subcrop patterns.
6 HYDROGEOLOGY OF THE ST LAWRENCE FORMATION
This section of our report describes the hydrogeologic characteristics of the St. Lawrence
Formation. We use new data collected as part of the MDH-St. Lawrence project, together with data collected from a number of previous studies. Much of this earlier work is summarized in
Runkel and others (2003). Our conclusions are generally consistent with the hydrogeologic characterization of the St. Lawrence Formation presented in Runkel and others (2003, 2006).
Those reports describe the formation as a unit dominated by low- to very low matrix porosity and permeability. Variably developed secondary pores along discrete intervals that parallel bedding are of sufficiently high permeability to provide the formation with an average bulk horizontal hydraulic conductivity that is within the range of values reported for bedrock units classified as aquifers in southeastern Minnesota. Hydraulic conductivity in a vertical direction is not as well understood, but available evidence indicates that it is sufficiently low that the St. Lawrence serves as an aquitard where it is not breached by vertical fractures. The distribution of such vertical fractures is poorly known, but they are likely to be more abundant, extensive, and with larger apertures in settings where the formation is at or close to the bedrock surface, particularly near bedrock valleys, compared to where it is deeply buried by tens of feet of younger bedrock.
Evidence to support this characterization, described below, comes from multiple hydrogeologic techniques. In addition to traditional sources of data such as specific capacity tests, discrete- interval packer tests, and potentiometric data, we employed relatively new techniques of borehole geophysical and video logging to describe and measure hydrogeologic properties. We also draw heavily upon borehole, core, and outcrop descriptions of secondary pores. Selected examples of these techniques are illustrated as figures in this report, and information from 16 additional sites is illustrated in Appendix 1.
7 HYDROSTRATIGRAPHIC ATTRIBUTES
Matrix
The textural and cementation attributes of the St. Lawrence Formation and tests of its matrix
permeability are consistent with those of other Cambrian aquitards in southeastern Minnesota
(Fig. 4) (e.g. Runkel and others, 2003). The formation is composed largely of very fine-grained
sandstone, siltstone, and shale, with subordinate beds of dense, very fine-grained dolostone. Such
material has a low to very low matrix permeability. Laboratory tests of one-inch diameter
cylindrical samples indicate that siltstone, shale and carbonate beds generally range from 10-4 to
10-6 md in vertical permeability. Interbeds of very-fine grained sandstone have higher
permeability of about 10-2 to 10-4 md. Horizontal permeability is commonly about two orders of
magnitude greater than vertical (Miller and Delin, 1993).
Secondary pores
Secondary pores such as fractures and solution cavities are common in the St. Lawrence
Formation (Figures 5,6,7). Cores, video logs, caliper logs, and outcrops show that bedding plane-
parallel macropores, often referred to as bedding plane fractures, are typical of the formation. At individual sections they are clustered along discrete stratigraphic intervals of a few tens of inches or less (Fig. 5A). Vertical fractures include systematic joints that commonly penetrate for several feet or more (Figs. 6A,B), as well as nonsystematic, irregular fractures that typical extend a few
tens of inches or less (e.g. Figs 6A,D).
The degree to which secondary pores are developed in the St. Lawrence varies in a
generally predictable fashion whereby macropores are increasingly more prevalent with
increasing proximity of the formation to the bedrock surface. In conditions of relatively deep
burial by younger bedrock (50 feet or greater) secondary pores in most boreholes are typically
8 limited to discrete intervals with abundant, bedding-plane parallel openings (Figs 4 and 5A).
Vertical fractures are difficult to evaluate because of the well-known limitations on documenting such features using only vertical boreholes, but rock cores are known to contain nonsystematic vertical fractures with narrow (<1mm) apertures (Figs 4, 5A) (Runkel and others, 2003). The abundance, size and connectivity of such features cannot be confidently described. More extensive vertical fractures such as systematic joints have not been described in the St. Lawrence
Formation under conditions of deep burial. Runkel and others (2003) suggest that such joints are likely to be present at least locally, but may have relatively narrow apertures compared to shallow conditions of burial.
Outcrop and borehole observations of the St. Lawrence Formation in conditions of shallow burial by younger bedrock (less than 50 ft.)indicate that secondary pores in such conditions are more abundant , better-connected, and have larger apertures compared to conditions of deeper burial (Fig. 8). This phenomenon has been widely documented in a number of hydrogeologic studies focused on fracture flow in Paleozoic bedrock in this region of North America
(summarized in Runkel and others, 2003). Relatively extensive vertical joints with cm-scale apertures, and a dense network of nonsystematic fractures, are typical of the St. Lawrence in outcrop, and borehole observations suggest that the formation will have similar features where it subcrops beneath unconsolidated glacial deposits (Fig 6A cf. Figs 6B, C, D). A video log collected at Montgomery, Minnesota as part of this project shows what is believed to be typical expression of such features. The upper part of the open borehole penetrates the St. Lawrence
Formation at a site where it is uppermost bedrock. The video documents that bedding-plane openings are common throughout the formation, and vertical fractures with apertures greater than one cm are common. Wenck and Associates (1997), used cores, boreholes, and observations
9 of subcrop exposed by removal of overburden to describe a similarly high density of fractures in
the St. Lawrence Formation near Red Wing, Minnesota.
HYDRAULIC ATTRIBUTES
The hydraulic conductivity of the St. Lawrence Formation has not been tested as rigorously
as several other bedrock hydrogeologic units in the Twin Cities metro area, but available data
indicate it varies considerably depending on the degree of development of secondary pores.
Intervals lacking hydraulically significant secondary pores have low to very low hydraulic
conductivity, from about 10-4 to 10-8 ft/day, based on conversion of milidarcy values measured from laboratory tests of 1” diameter core samples. The bulk vertical conductivity of the St.
Lawrence Formation at a site in Ramsey County was calculated to be 10-4 to 10-5 ft/day on the
basis of thermal profiling, analysis of pumping tests, and hydrochemical methods (Walton and
others, 1991). Packer tests for some intervals of St. Lawrence formation as part of the same
investigation yielded a value of less than 10-3 ft/day (Fig. 4), which is consistent with the low
values measured in laboratory tests of core samples. In contrast, intervals of St. Lawrence
Formation with hydraulically connected secondary pores are several orders of magnitude higher
in conductivity. Specific capacity values from productivity tests of water-wells in the project
study area average 2.49 gal/min/ft., sufficiently high that they fall within the range of average
productivity for units designated as aquifers in the study area (Fig. 9). Borehole geophysical and
video logs support the interpretation that these measures of bulk horizontal conductivity are
achieved via flow through secondary pores. Video logs reveal water entering or exiting bedding-
plane parallel fractures with apertures of a few cm or less (e.g. Fig 7 D through I). Flowmeter,
fluid resistivity, and temperature logs have relatively sharp deflections that record the same
phenomenon of flow through thin, high permeability intervals (Figs 10, 11, 12, Appendix 1). A
10 discrete interval packer test measured bulk conductivity for an interval containing such pores at
6.7 ft/day (Fig. 4).
The increase in development of secondary pores with decreasing depth of burial beneath
younger bedrock is reflected in measures of St. Lawrence Formation productivity and hydraulic
conductivity. Water wells open to the St. Lawrence Formation in conditions of shallow burial
(less than 50 ft of overlying bedrock) have more variable and on average twice the conductivity of wells open to the formation in conditions of deep burial (Runkel and others 2006). Specific capacity data compiled for this study support the same interpretation. On average, wells that draw water from the St. Lawrence Formation where it is present in shallow conditions are nearly twice as productive as wells constructed where the unit is buried by 50 ft or more of bedrock
(Fig. 9). About three-fourths of known St. Lawrence Formation wells are constructed in such settings, over half where the formation is uppermost bedrock. This includes the high density of wells that are constructed to draw water from a buried plateau composed of St. Lawrence
Formation in southern Scott County. These wells commonly penetrate less than 20 ft of St.
Lawrence, likely drawing water from well-developed fracture networks similar to those exhibited in the video log of the formation exposed in the open borehole of the City of Montgomery
municipal well #2 (Fig 6C-F)
HYDROGEOLOGIC SYNTHESIS
Appropriate hydrogeologic classification of the St. Lawrence Formation, as an aquitard
versus as an aquifer, depends in part on whether its horizontal hydrologic attributes or whether
its vertical attributes are considered of greatest importance. For example, there is strong evidence
that the St. Lawrence Formation commonly has a moderate to high horizontal hydraulic
conductivity across all of the study area and therefore it can properly be classified as an aquifer.
11 It is a body of rock that yields water in sufficient quantity for economic use. In shallow conditions of burial it is most similar in the development of secondary pores and measured hydraulic properties to fractured carbonate rock aquifers (Runkel and others 2003, 2006).
Discrete intervals with secondary pores have a high horizontal hydraulic conductivity whereas rock between these intervals are orders of magnitude lower in conductivity.
The properties of the St. Lawrence Formation in a vertical direction are not as widely tested, but available data are consistent with the traditional classification of the formation as an aquitard. The values for vertical conductivity based on matrix permeability and bulk aquifer tests by Walton and others (1991) fall within the range of relatively low values characteristic of other
Paleozoic aquitards in southeastern Minnesota and adjacent states, such as the Eau Claire formation and lower part of the Franconia Formation (Fig. 4). The values are as much as eight orders of magnitude less than vertical hydraulic conductivity values measured for aquifers in this region. Furthermore, potentiometric data from a few sites in and near the TCMA suggest that at least some interval(s) in the St. Lawrence Formation, possibly along with the lower Jordan
Sandstone, are of sufficiently low bulk vertical conductivity to maintain distinctly different heads above and below the formation. For example, the St. Lawrence Formation separates upper Jordan from upper Franconia aquifer heads that differ by two to five feet at sites in Ramsey County
(Walton and others 1991), and in southern Dakota County (USGS on-line data for well network
CL4, 2006). The St. Lawrence formation at each of these sites is deeply buried by younger bedrock, a setting in which vertical fractures are relatively poorly developed. Flowmeter, conductivity, temperature and video logs provide additional support for the interpretation that parts of the St. Lawrence Formation can serve as an aquitard in a vertical direction (Figs. 10, 11,
12, Appendix 1). Logs collected at a number of sites within and near the study area record
12 ambient vertical flow in a borehole moving from one fracture to another. Such flow demonstrates
that the intervening interval serves as an aquitard that maintains a head differential between the
two fractures.
Given the low matrix permeability of the St. Lawrence Formation, its integrity as an
aquitard in a vertical direction is determined largely by the degree of development of vertical
fractures. If the interpretation that some intervals of the formation serve as effective aquitards in
a vertical direction is accurate, this suggests that vertical fractures are poorly connected through
the entire thickness of the formation. The available evidence indicates that the St. Lawrence
Formation may be closely analogous in hydrologic properties to the Maquoketa aquitard in
Wisconsin (Eaton, 2002; Eaton and Bradbury, 2003). According to Eaton (2002) and Eaton and
Bradbury (2003) the Maquoketa aquitard contains a relatively high transmissivity,
interconnected, but sparse fracture network embedded in a low conductivity rock matrix. The
upper interval of the aquitard is relatively densely fractured and at least locally has a good
hydraulic connection to overlying bedrock. However, a discrete interval of a few meters or less
in the lower part of the formation is resistant to the development of interconnected vertical fractures. This interval does not readily transmit head changes, and may account for the regional confining properties of the formation. Similarly, one or more relatively discrete interval(s) in the
St. Lawrence Formation may be particularly resistant to breaching by vertical fractures, as shown schematically in Figure 8.
The properties of the St. Lawrence Formation that determine aquitard integrity in a vertical sense, described above, are based on data largely collected where the formation is deeply buried by over 50 feet of younger bedrock. The integrity of the formation as an aquitard in a vertical direction in shallow conditions of burial, particularly where it is uppermost bedrock, remains
13 relatively poorly understood, and cannot be confidently characterized in a manner that is
applicable to its entire subcrop extent. Vertical fractures should be expected to be better developed and interconnected in progressively shallower conditions of burial (Fig. 8), but available information is inadequate to precisely characterize such fractures. Borehole flowmeter logs from two sites (Fig. 12) record ambient flow that indicates the presence of aquitards within the St. Lawrence even where it is present as uppermost bedrock. However, the lateral continuity of these aquitards is uncertain, and they could commonly be breached elsewhere by systematic joints or networks of nonsystematic fractures. The absence of perched water table aquifers on top of the St. Lawrence Formation in bluff-side settings along the St. Croix and Mississippi Rivers in southeastern Minnesota may reflect such breaching.
RECOMMENDATIONS FOR ADDITIONAL RESEARCH
Additional investigations of the hydrogeologic properties of the St. Lawrence Formation would support more effective groundwater management. Cherry and others (2006) and Bradbury and others (2006) provide a comprehensive overview of a number of techniques, including site- specific tests of hydraulic conductivity, potentiometric heads, and water chemistry attributes that provide important information on aquitard integrity.
Scientific test holes would allow more rigorous investigation of St. Lawrence Formation hydrologic properties, and are especially needed to evaluate aquitard integrity in shallow bedrock conditions, where the St. Lawrence Formation is known to have relatively well-developed vertical fractures, and where it is most commonly used as an aquifer. Such holes would be particularly useful for high-resolution tests of horizontal hydraulic conductivity, and for measurement of hydraulic head across discrete intervals. Such techniques have been shown to be
14 useful for identification of relatively thin intervals that account for much of an aquitards ability to provide confinement (e.g. Eaton 2002; Tipping and Runkel, 2006). Bulk vertical conductivity could also be tested through aquifer tests of the upper Franconia Formation that include networks of monitor wells open to various positions within the St. Lawrence Formation, the upper and lower parts of the Jordan Sandstone, within the upper part of the Franconia Formation.
Potentiometric data, tightly clustered stratigraphically and geographically, would also provide important information on the aquitard integrity of the St. Lawrence. Existing maps and reports that describe potentiometric data are inadequate to evaluate whether the formation by itself serves as an aquitard that separates the Jordan from upper Franconia aquifers. Tight clusters of monitor wells open to various parts of the Jordan Sandstone (and/or unconsolidated glacial deposits), St. Lawrence Formation, and the upper one-half of the Franconia Formation could provide useful insight into what part(s) of Franconia through Jordan stratigraphic interval act as an aquitard, and whether variability in geographic and geologic setting impacts the aquitard integrity of such intervals.
15 REFERENCES
Bradbury, K.R., Gotkowitz, M.B., Hart, D.J., Eaton, T.T., Cherry, J.A., Parker, B.L., and Borchardt, M.A., 2006, Contaminant transport through aquitards: Technical guidance for aquitard assessment: American Water Works Research Foundation Publication, 142 p. Cherry, J.A., Parker, B.L., Bradbury, K.R., Eaton, T.T., Gotkowitz, M.B., Hart, D.J., and Borchardt, M.A., 2006, Contaminant transport through aquitards: A state-of-the- science review: American Water Works Research Foundation Publication, 126 p. Eaton, T.T, 2002. Fracture heterogeneity and hydrogeology of the Maquoketa aquitard, southeastern Wisconsin. Ph.D. dissertation, University of Wisconsin, Madison, USA, 211 pp. Eaton, T.T., and Bradbury, K.R., 2003, Hydraulic transience and the role of bedding fractures in a bedrock aquitard, southeastern Wisconsin, USA: Geophysical Research Letters, v. 30, no. 18, p 4-1 to 4-5. Kanivetsky, R., 1978. Hydrogeologic map of Minnesota: Bedrock Hydrogeology. Minnesota Geological Survey Map Series, S-2. Miller, R.T., Delin, G.N., 1993. Field observations, preliminary model analysis, and aquifer thermal efficiency. U.S. Geological Survey Professional Paper 1530-A, 55 pp. Mossler, J.H., 1972. Paleozoic structure and stratigraphy of the Twin Cities Region. In: Sims, P.K., Morey, G.B. (eds.), Geology of Minnesota, A Centennial Volume. Publication of the Minnesota Geological Survey, pp. 485-497. Mossler, J.H., Tipping, R.G., 2000. Bedrock geology and structure of the seven-county Twin Cities Metropolitan area, Minnesota. Minnesota Geological Survey Miscellaneous Map, M-104, scale 1:125,000. Mossler, J.H., Runkel, A.C., Bauer, E. J., 2006, Subcrop of the St Lawrence Formation in the seven-county Twin Cities Metropolitan Area, Minnesota: Minnesota Geological Survey Open File Report 06-05.
16 Olsen, B.N., 1982, Bedrock Geology, in, Balaban, N.H., and McSwiggen, P. L., eds., Geologic Atlas of Scott County, Minnesota: Minnesota Geological Survey Geologic Atlas Series C-1. Scale 1:100,000. Paillet, F.L., Lundy, J., Tipping, R.G., Runkel, A.C., Reeves, L., Green, J.A., 2000. Hydrogeologic characterization of six sites in southeastern Minnesota using borehole flowmeters and other geophysical logs. U.S. Geological Survey Water-Resources Investigation Report 00-4142, 33 pp. Runkel, A.C., Tipping, R.G., Alexander, E.C., Jr., Green, J.A., Mossler, J.H., Alexander, S.C., 2003. Hydrogeology of the Paleozoic bedrock in southeastern Minnesota. Minnesota Geological Survey Report of Investigations, vol. 61, 105 pp., 2pls. Runkel, A.C., Tipping, R.G., Alexander, E.C., and Alexander, S.C., 2006, Hydrostratigraphic characterization of intergranular and secondary porosity in part of the Cambrian sandstone aquifer system of the cratonic interior of North America: Improving predictability of hydrogeologic properties: Sedimentary Geology v. 184, p. 281-304. Tipping, R.G., Runkel, A.C., Alexander, E.C., and Alexander, S.C., 2006, Evidence for hydraulic heterogeneity and anisotropy in the mostly carbonate Prairie du Chien Group, southeastern Minnesota, USA: Sedimentary Geology v. 184, p. 305-330. Walton, M., Eisenreich, S.J., Holm, N.L., Holm, T.R., Kanivetsky, R., Jirsa, M.A., Lee, H.C., Lauer, J.L., Miller, R.T., Norton, J.L., Runke, H., 1991. The University of Minnesota Aquifer Thermal Energy Storage (ATES) field test facility-system description, aquifer characterization, and results of short-term test cycles. Pacific Northwest Laboratory Report PNL-7220, UC-202, 295 pp. Wenck and Associates, Inc., 1997. Phase II: Detailed site investigation report and Phase II workplan for the hydrogeologic investigation of the proposed Red Wing ash disposal facility expansion. 36 pp.
17 FIGURE CAPTIONS
Figure 1. Schematic bedrock geologic map with locations of boreholes where flowmeter logs, video logs, or other hydrogeologic information pertinent to this investigation were collected. The subcrop distribution of the St. Lawrence Formation (pink) is based on mapping conducted as part of this project. A more detailed depiction of the St. Lawrence Formation map, which includes faults, is in the accompanying MGS Open File Report 06-05. The depiction of Cambrian versus Ordovician bedrock in this illustration is modified from Mossler and Tipping (2000). The project study area includes most of the seven-county Twin Cities Metropolitan area shown above. A description of the study area is also provided in the text of the report, and shown in the accompanying MGS Open File Report 06-05 (Mossler and others, 2006). Dashed line A-A’ is location of cross section shown in figures 2 and 8.
Figure 2. Cross-section highlighting lithic and secondary porosity attributes of Paleozoic bedrock across the Twin Cities Metro area. The focus of this investigation is the St. Lawrence Formation, which lies stratigraphically in approximately the middle of the Paleozoic bedrock package.
Figure 3. Lithic properties and representative natural gamma log signatures of the St. Lawrence Formation and adjacent stratigraphic units across the Twin Cities Metro area. Note that the St. Lawrence Formation thickens to the southwest, largely by virtue of more abundant and thicker beds of carbonate rock in its lower part. The upper and lower contacts of the St. Lawrence Formation with adjacent units are transitional, making precise, consistent identification problematic in some areas. See text for additional discussion. See Figure 1 for location of natural gamma logs.
Figure 4. Stratigraphic column showing lithic and hydrogeologic properties of a selected interval of Paleozoic bedrock in the Twin Cities Metro area. This figure is based on observations and measurements of two cores and packer tests in two boreholes from the ATES (Aquifer Thermal Energy Storage) Project site in Ramsey County. The St. Lawrence Formation lithic properties and hydraulic tests of matrix are generally similar to those of aquitards in the lower Franconia and uppermost Eau Claire Formation. The St. Lawrence Formation is of low matrix permeability, and packer tests as well as analysis of bulk vertical conductivity show correspondingly low values. However, one packer test of an upper interval of the St. Lawrence Formation (borehole BC-1) has a relatively high hydraulic conductivity comparable to known Paleozoic bedrock aquifers, reflecting contribution through secondary pores. See text for additional discussion. Hydraulic testing is from Walton and others (1991) and Miller and Delin (1993). See Figure 1 for location (shown as single borehole site with unique number 185810)
Figure 5. Representative secondary pores in cores of St. Lawrence Formation. A) Discrete intervals with large secondary pores, noted by arrows, are separated by intervals with few such pores. Video logs of boreholes described in this report show a similar distribution of secondary pores. Core is from the Waseca-Waterville area south of the Twin Cities Metro area. B) and C) Typical secondary pores in the St. Lawrence Formation. They appear to have been enlarged by solution. From ATES core AC-1, Ramsey County.
Figure 6. Outcrop and borehole examples of secondary pores in the St. Lawrence Formation in shallow bedrock conditions (buried by less than 50 feet of younger bedrock). A) Vertical and subvertical fractures in outcrop. Green arrows point to an extensive systematic fracture (“vertical joint”) with large aperture. Red arrows point to selected nonsystematic fractures
18 (hammer circled for scale). B) down-hole view of systematic fracture in borehole wall, C) down-hole view of rubbly, heavily fractured borehole wall, D) side-hole view of nonsystematic fractures in borehole wall, E) side-hole view of bedding plane-parallel fracture. A) near Red Wing, Minnesota. C-E from borehole video of Montgomery City Well #2 (unique number 218355) between 252.9 ft. and 269.9 ft. Borehole is about 12” diameter. Location of borehole is shown in Figure 1.
Figure 7. Examples of bedding-plane parallel secondary pores (“ bedding plane fractures”) in boreholes open to the St. Lawrence Formation in deep bedrock conditions. A) side-hole view at 339 ft in Montgomery City Well number 2 (218355) B) side view in Victoria Creamery Well (256002) at 415 ft. C) side view in Coon Rapids City Well number 11 (202965) at 191 ft. D) down-hole view in Stillwater City Well number 7 (224467) at about 260 ft. E) down-hole, and F) side view of fracture at 297 ft in Hugo test well 3 (645394). G) side view in Hasting Railroad well (255768) at 218 ft. H) side view in Inver Grove Parks well (257056) at 273 ft. I) downhole view in Chaska Test Well 2 (665714) at 355 ft. . The bedding-plane parallel pores in examples D through I actively emitted or accepted water under ambient conditions, based on observation of suspended particles in borehole video and/or geophysical flowmeter, temperature and conductivity logs. Precise scale on photographs cannot be determined, but apertures in all examples likely range from about 1 to 4 inches. Location of boreholes shown in Figure 1.
Figure 8. Schematic illustration of secondary pores in St. Lawrence Formation, comparing shallow bedrock conditions to deep bedrock conditions. Shallow bedrock conditions are characterized by a greater abundance, extent, connectivity, and aperture size of fractures and solution cavities. As a result, the hydraulic conductivity of the St. Lawrence is greater in shallow bedrock conditions, and aquitard intervals are more likely to be breached by vertical fractures.
Figure 9. Summary of productivity information for wells constructed to draw water from the St. Lawrence Formation in the study area. A) Box plots of specific capacity data comparing wells open to the St. Lawrence Formation to wells open to other Paleozoic bedrock units in the study area. Numbers in parenthesis at the top of each column are the number of wells in each category for which no measurable drawdown occurred during pumping. Such wells are highly productive but a specific capacity value cannot be calculated. B) Distribution of specific capacity values for St. Lawrence Formation wells. C) Distribution of all (643) St. Lawrence Formation wells across the study area. The distributions shown in B and C indicate that the formation yields sufficient water for domestic needs across the entire study area, but is most commonly used as an aquifer where it subcrops. The greatest density of wells, and what appears to be the most productive wells, are clustered across extensive buried plateaus of the formation in Scott County, where the St. Lawrence includes a thick dolostone-dominated interval in its lower part. Explanation of Box Plots in A): Each colored box encloses 50% of the specific capacity values with the top and bottom of the box marking the limits of 25% of the variable population. The lines extending from the top and bottom of each box mark the minimum and maximum values within a statistically acceptable range. Any value outside of this range, called an outlier, is displayed as an individual point.
Figure 10. Example of video observations and temperature and fluid resistivity logs used to document secondary pores and water movement associated with the St. Lawrence Formation. In this example water enters the borehole through a bedding plane fracture at 273 ft. in the St. Lawrence formation, travels uphole, and exits the borehole through bedding plane fractures (and possibly in intergranular fashion) in the lower part of the Jordan Sandstone. Flow pattern indicates aquitard(s) are present in the upper St. Lawrence and/or lower Jordan Sandstone. The hydraulically active bedding plane fracture in the St. Lawrence Formation at 273 ft. is shown in
19 Figure 7H. Location of borehole shown in Figure 1. Other examples of this kind of information are in Appendix 1.
Figure 11 Example of suite of geophysical logs collected to document borehole flow associated with the St. Lawrence Formation. In this example water enters the borehole at two discrete intervals (likely bedding plane fractures ) at ~337 ft and 347 ft in the upper St. Lawrence Formation, and flows downhole. Water exits the borehole at discrete intervals (likely bedding plane fractures) at ~352 ft. in the upper St. Lawrence Formation, and at three positions in the Franconia Formation and Ironton/Galesville sandstones. This flow pattern indicates the presence of an aquitard between entry and exit intervals in the St. Lawrence Formation. Other examples of this kind of information are in Appendix 1. See Runkel and others (2003, 2006) for explanation of flow-logging techniques and methods of interpretation. See Fig. 1 for location of borehole.
Figure 12 Examples of suite of geophysical logs collected to document borehole flow associated with the St. Lawrence Formation. A) Moderate downflow enters borehole at discrete interval (likely bedding plane fracture) at 138 ft. in the St. Lawrence, and exits borehole hole through a discrete interval (likely bedding plane fracture), and possibly in intergranular fashion, in the upper Franconia Formation. This flow pattern indicates the presence of an aquitard in the lower part of the St. Lawrence Formation. B) Water enters borehole at discrete interval (likely bedding plane fracture) at 221 ft in the upper part of the St. Lawrence, travels downhole, and exits at a discrete interval (likely bedding plane fracture) at 249 ft. in the upper Franconia Formation. This flow pattern indicates presence of an aquitard between the entry and exit intervals. Other examples of this kind of information are in Appendix 1. See Runkel and others (2003, 2006) for explanation of flow-logging techniques and methods of interpretation. See figure 1 for location of boreholes.
20 Isanti A Chisago Paleozoic Bedrock Anoka Ordovician 731101 Cambrian St Lawrence Fm
742803 Wright 202965 645394 Borehole with CSTL hydrogeologic data
123456 = unique well number 658157 Ramsey on County boundary 225622 224467
676433 Line of cross-section 225868 (Figure 2) 185810
Hennepin ashingt
W A'
256002 Carver 257056 665714 665713 741682 739166 Scott Dakota 255768 672729
10 miles Rice
218353 218355 235704 W ino
na C
o un t y
Figure 1 Sherburne Isanti
A Anoka
Wright on
Ramsey ashingt
Hennepin W A'
Carver Dakota Scott
Ordovician Cambrian
A A' RAMSEY COUNTY WRIGHT COUNTY HENNEPIN COUNTY WASHINGTON CO ST PAUL
DECORAH/ Quaternary unconsolidated sediment ("Glacial drift") PLATTEVILLE/ Or GLENWOOD d ovic Ca ian an mbr vici ia do n n Or ia ambr ST PETER C ST CROIX RIVER PRAIRIE DU CHIEN
Precambrian JORDAN bedrock ST LAWRENCE U D FRANCONIA (upper) FRANCONIA (lower)
IRONTON-GALESVILLE
EAU CLAIRE 100 ft 10 miles FINE-COARSE GRAINED SANDSTONE 0 CARBONATE MT SIMON MT SIMON VERY FINE-GRAINED SANDSTONE, SILTSTONE, SHALE Precambrian FRACTURES, OTHER CAVITIES bedrock (PROBABLE CONDUITS)
Figure 2 Southwest Metro area Northern Metro Area
665713 256002
742803
Jordan Ss
St. Lawrence Fm. Jordan Ss
G G G G G G G St. Lawrence Fm. G G St. Lawrence Fm. G G G G G G G G G G G G G G Franconia Fm. G G G G G G G Reno mbr. G G G G G G G Mazomonie mbr G Reno mbr. G Mazomonie mbr G G G G G G Franconia Fm. G G Reno mbr. G G G G G G G G G Reno mbr. G G G G
G G G G G Reno mbr. Reno mbr. G G G
G G G
FINE-COARSE GRAINED Vertical Scale Natural Gamma log SANDSTONE Gamma log scale (API units) 0 200 CARBONATE
50 ft 123456 (unique well number) VERY FINE-GRAINED SANDSTONE, SILTSTONE, SHALE
G Glauconite No horizontal scale (see Fig. 1 for location of gamma logs) Formation contacts, dashed where uncertain
Figure 3 ATES BC-1 and AC-1 Cores
Natural Gamma-ray Log
Increasing counts aphic unit d tigr a 185810 quitar Lithostr er/A t) sh sl vf f m c quif ol. A epth (f shale D
460 Oneota D
440
460 one
480 andst dan S
500 or J Macroscopic secondary porosity Plug porosity Plug permeability vertical (in md) Plug permeability horizontal (md) Packer test horizontal hydraulic conductivity (feet per day) nonsystematic, vertical fracstures/ft 0 5 0 100% 0 40% 10-6 100 10-6 100 0 7.0 520 Packer intervals
540 -4 e Fm vertical K= 10 ft/day enc wr 560 t La S
580
600
620
640 onia Fm anc r F
660
680
700
720
740 alesville Ss's on-G t on
760 Ir
780
800 e Fm 820 lair Plug sample au C E
840
860 imon Ss Mt S
Grain Size Fine to coarse-grained sandstone sh sl vf f m c Aquifer Very fine grained sandstone, siltstone, shale Aquitard sh=shale 100% sl=silt vf=very-fine Dolostone core loss SHALE f=fine 0 m=medium c=coarse Figure 4 A
B
large vug along bedding plane
C
nonsystematic vertical fractures
1 foot
Figure 5 A
Systematic vertical fracture B C D E
Figure 6 A B C
D E F G
H I
Figure 7 SHALLOW BEDROCK CONDITIONS DEEP BEDROCK CONDITIONS
systematic vertical fractures ("vertical joints")
nonsystematic vertical fractures
bedding-plane parallel secondary pores interval resistant to ("bedding plane parallel fractures") breaching by vertical fractures A A'
DECORAH/ PLATTEVILLE/ GLENWOOD
ST PETER
PRAIRIE DU CHIEN
Precambrian JORDAN bedrock ST LAWRENCE U D FRANCONIA (upper) FRANCONIA (lower)
IRONTON-GALESVILLE 100 ft 10 miles FINE-COARSE GRAINED EAU CLAIRE SANDSTONE 0 CARBONATE
VERY FINE-GRAINED SANDSTONE, MT SIMON SILTSTONE, SHALE MT SIMON
FRACTURES, OTHER CAVITIES (PROBABLE CONDUITS) Precambrian bedrock Figure 8 A CIGL CFRN CSTL CJDN OPDC all shallow deep all shallow deep all shallow deep all shallow deep all shallow deep >50 (91) (85) (6) (290) (267) (23) (21) (18) (3) (416) (71) (345) (280) (233) (47)
40 WN WDO A 30 T DR
20 ONS/MINUTE/FOO GALL
10
0 n=250 n=189 n=61 n=2800 n=2503 n=497 n=127 n=79 n=48 n=1659 n=311 n=1348 n=1164 n=923 n=241 x=2.49 x=2.38 x=2.81 x=2.81 x=3.02 x=1.84 x=2.12 x=2.57 x=1.38 x=1.58 x=2.37 x=1.40 x=2.80 x=2.90 x=2.42 s.d.=3.41 s.d.=2.92 s.d.=4.64 s.d.=3.62 s.d.=3.71 s.d.=2.97 s.d.=3.52 s.d.=4.22 s.d.=1.67 s.d.=3.07 s.d.=3.39 s.d.=2.97 s.d.=10.6 s.d.=10.89 s.d.=5.85
B C Specific capacity (gal/min/ft drawdown) .08-0.15 St Lawrence Fm wells 0.15-0.286 Isanti other wells 0.286-0.417 Chisago Ordovician 0.417-0.571 Cambrian 0.571-0.75 0.75-1 Anoka St Lawrence Fm 1-1.5 County boundary 1.5-2.5 2.5-4.286 10 miles 4.286-8 8-15 Wright 15-30 Ramse y
Hennepin ashington W
Car ver
Scott Dak ota
Rice
Figure 9 Inver Grove Heights area (IGH Parks) 257056
gamma (API units) DEPTH temperature (F) fluid resistivity (ohm-meters) video log observations IN FT.
0 300 52.3 52.8 25 30 glaical deposits 0 casing Prairie du Chien
50
100
150 Prairie du Chien Jordan Ss
BPF at 200' 200 ?
Jordan Ss BPF at 233'
St Lawrence Fm 250 ? BPF at 251.8'
Water moves uphole Water enters through BPF at 273'
St Lawrence Fm Franconia Fm 300
aquitard
flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Figure 10 City of Chaska Observation Well 665713
gamma (API units) DEPTH hole diameter (inches) station flow (gal/min) trolling flow log (gal/min) temperature (F) fluid resistivity (ohm-meters) IN FT.
0 100 200 3.0 4.0 5.0 -4 -2 0 -10 -5 0 5 57 58 59 60 16 16.5 17 bedrock surface 250 at 206'
300
Jordan Ss Casing Casing St. Lawrence Fm. 350
St. Lawrence Fm.
400 Franconia Fm.
450
500 Franconia Fm. Ironton-Galesville Ss.
550
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Figure 11 A Andover domestic well 731101 gamma (API units) DEPTH hole diameter (in.) station flow (gal/min) trolling flow log(gal/min) temperature (F) fluid resistivity (ohm-meters) IN FT.
-3 0 3 34.5 35.0 0 100 100 200 200300 4 5 6 -0.25 0 0.25 52.2 52.4 52.6 35.5
100
Glacial deposits
St. Lawrence Fm. 120
casing casing
140 St. Lawrence Fm. Franconia Fm. ? 160
B downhole flow uphole flow Blaine area Irrigation Well 742803 gamma (API units) hole diameter (in.) station flow (gal/min) trolling flow log (gal/min) temperature (F)* fluid resistivity (ohm-meters) DEPTH IN FT.
0 100 200 3.5 4.0 4.5 -1.5 -1 -0.5 0 0.5 -4 -2 0 81.7 81.9 82.1 82.3 82.5 36 37 38 Glacial deposits 200 Jordan Ss
casing Jordan Ss casing St. Lawrence Fm. 220
St Lawrence Fm. 240 Franconia Fm.
260
downhole flow uphole flow * Measured temperature about flow measurement with 30 degrees too warm due to tool tool stationary calibration error. Relative changes interpreted flow aquitard in temperature are accurate.
flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Figure 12 APPENDIX 1
Illustrated summaries of geophysical and video log information collected from boreholes open to the St. Lawrence Formation and used as basis for the descriptions and interpretations in this report. All illustrations show information collected from boreholes under ambient conditions (no pumping or injection of borehole). Locations of boreholes shown in Figure 1 of this report, and detailed locality and well construction information can be found in the County Well Index (CWI) maintained by the Minnesota Department of Health (MDH).
Abbreviations used in illustrations:
F (Fahrenheit) gal (gallons) in. (inches) API (American Petroleum Institute) (standard scale for natural gamma activity) BPF (bedding plane fracture) OPDC (Prairie du Chien Group) CJDN (Jordan Sandstone) CSTL (St. Lawrence Formation) CFRN (Franconia Formation) CIGL (Ironton and Galesville Sandstones) CECR (Eau Claire Formation) CMTS (Mt Simon Sandstone)
Andover domestic well 731101
gamma (API units) DEPTH hole diameter (in.) station flow (gal/min) trolling flow log(gal/min) temperature (F) fluid resistivity (ohm-meters) IN FT.
-3 0 3 34.5 35.0 0 100 100 200 200300 4 5 6 -0.25 0 0.25 52.2 52.4 52.6 35.5
100
Glacial deposits
St. Lawrence Fm. 120
casing casing
140 St. Lawrence Fm. Franconia Fm. ? 160
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Moderate downflow enters hole from likely BPF in CSTL at ~ 138 ft. , and exits hole through BPF and possibly in intergranular fashion in upper CFRN. This flow pattern indicates aquitard present in lower CSTL. Injection test of this hole resulted in injected water bypassing the CSTL , to exit hole in upper CFRN (injection information not shown on this illustration). Blaine area Irrigation Well 742803
gamma (API units) hole diameter (in.) station flow (gal/min) trolling flow log (gal/min) temperature (F)* fluid resistivity (ohm-meters) DEPTH IN FT.
0 100 200 3.5 4.0 4.5 -1.5 -1 -0.5 0 0.5 -4 -2 0 81.7 81.9 82.1 82.3 82.5 36 37 38 Glacial deposits 200 Jordan Ss
casing Jordan Ss casing St. Lawrence Fm. 220
St Lawrence Fm. 240 Franconia Fm.
260 downhole flow uphole flow * Measured temperature about 30 degrees too warm due to tool calibration error. Relative changes flow measurement with aquitard tool stationary in temperature are accurate. interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters borehole at discrete interval (likely BPF) at 221' in upper part of CSTL, travels downhole, and exits at discrete interval (likely BPF) at 249' in upper CFRN. Flow pattern indicates presence of aquitard in interval between entry and exit . City of Chaska Observation Well 665713
gamma (API units) DEPTH hole diameter (inches) station flow (gal/min) trolling flow log (gal/min) temperature (F) fluid resistivity (ohm-meters) IN FT.
0 100 200 3.0 4.0 5.0 -4 -2 0 -10 -5 0 5 57 58 59 60 16 16.5 17 bedrock surface 250 at 206'
300
Jordan Ss Casing Casing St. Lawrence Fm. 350
St. Lawrence Fm.
400 Franconia Fm.
450
500 Franconia Fm. Ironton-Galesville Ss.
550
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters borehole at two discrete intervals (likely BPF's) at ~337' & 347' in upper CSTL, and flows downhole. Water exits at discrete intervals (likely BPF's) at ~352' in upper CSTL, and at three positions in CFRN and CIGL. This flow pattern indicates presence of aquitard between entry and exit intervals in CSTL. Borehole conditions may have been altered by drilling mud originating from neaby borehole. City of Chaska Test Well #2 665714
gamma (API units) DEPTH hole diameter (in.) station flow (gal/min) video log observations trolling flow (gal/min) temperature (F) fluid resistivity (ohm-meters) IN FT. 5 6.5
0 100 200 5 6 7 -0.25 0 0.25 -10 -5 0 57.75 58 58.25 14 16 18 bedrock surface 300 300 at 217'
Jordan Ss casing casing St. Lawrence Water entering at BPF at ~330' and flowing downhole Fm. 350 350 BPF at 355', water exiting?, BPF at 361' diminished downflow St. Lawrence below this depth Fm. BPF at 375' Franconia Fm. 400 400
hole contains 450 450 drilling mud
500 500 downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpetation overview: Water enters borehole through BPF at ~330' at approx. contact between CJDN and CSTL, and flows downhole.Water exits through two BPFs, at 355' and 375', in CSTL. Remaining downflow exiting lower in borehole (CFRN). Flow pattern indicates interval of lower CJDN/upper CSTL between water entry and exit is an aquitard. Borehole conditions may have been altered by drilling mud originating from neaby borehole. Video collected prior to this testing showed markedly stronger downflow. Drilling mud in lower part of borehole likely diminished downflow. BPF at approx 355' is shown in Fig 7I Cologne area, Hans Hagen Homes 739166
gamma (API units) DEPTH hole diameter (in.) station flow (gal/min) trolling flow (gal/min) temperature (F)* fluid resistivity (ohm-meters) IN FT.
-1 -0.5 0 100 200 300 3.5 4.0 4.5 0 -6 -4 -2 0 83 83.2 83.4 83.6 17.2 17.6 18 18.4
Glacial deposits
St. Lawrence Fm. 200 casing casing
St. Lawrence Fm.
Franconia Fm. 250
300
350
Franconia Fm. Ironton/Galesville Ss
300 400 300
downhole flow uphole flow
* Measured temperature about flow measurement with aquitard 30 degrees too warm due to tool tool stationary calibration error. Relative changes interpreted flow flow abruptly enters/exits in temperature are accurate.
flow gradually (intergranularly?) enters or exits
Interpretation overview: Ambient conditions show downflow entering hole through BPFs at ~220' and 240' in CSTL and at ~275' upper CFRN, and exiting hole in CIGL, perhaps largely at a BPF near hole bottom. Injected water in this borehole appeared to exit entirely in CIGL, with bypass of all CFRN and CSTL. (Injection data not shown on this illustration).
Ironton-Galesville Ss.
Eau Claire Fm. City of Cologne Test Well #1 741682
DEPTH IN FT. gamma (API units) hole diameter (in.) station flow (gal/min) trolling flow log (gal/min) temperature (F)* fluid resistivity (ohm-meters) bedrock surface at 215' 0 100 200 6.2 6.3 6.4 -4 -2 0 -1.5 -1 -0.5 0 82.9 83 17 17.2 17.4 casing casing casing 250 St Lawrence Fm. Franconia Fm.
300 hole continues to CMTS, to 710+ ft. downflow continues to CMTS,
downhole flow uphole flow * Measured temperature about 30 degrees too warm due to tool calibration error. Relative changes in temperature are accurate. flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters borehole through two, closely spaced, discrete intervals (likely BPFs) at ~250' in CSTL, flows downhole, exiting in CMTS. Coon Rapids Municipal Well #11 202965
gamma (API units) DEPTH hole diameter (in.) Observations of CSTL on video log IN FT.
0 200 15 20 25 30 35 Glacial deposits
140
St. Lawrence Fm.
160
180
casing BPF at 191' St. Lawrence Fm.
200 Franconia Fm. sandstone "washout" in upper CFRN
220
Interpretation overview: Video and caliper logs show BPF in lower CSTL. This BPF is shown in Figure 7C. City of Greenfield Test Well 658157
gamma (API units) DEPTH caliper log (inches) station flow (gal/min) trolling flow (gal/min) temperature (F) fluid resistivity (ohm-meters) IN FT.
0 100 200 3.0 4.0 5.0 0 0.5 1 0 1.5 3 57 57.25 57.5 13 14 15 16 17 18 bedrock surface 240 at 216''
Jordan Ss casing casing St. Lawrence Fm 260
280
St. Lawrence Fm
300 Franconia Fm.
320
340
360
380
400
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters hole through BPF at ~328' in upper CFRN, flows uphole, and exits through BPF at 270' in upper CSTL. This flow pattern indicates aquitard present in upper CFRN or, more likely, lower to middle CSTL. Pumping of this hole at approx. 5 gal/min, resulted in at least 99% of yield emitted from the BPF in the upper CFRN (pumping data not shown on this illustration) Hastings area Railroad well 255768
gamma (API units) hole diameter (in.) station flow (gal/min) video log observations trolling flow log (gal/min) temperature (F) fluid resistivity (ohm-meters) DEPTH of CSTL IN FT.
bedrock surface 0 100 200 300 6.0 7.0 8.0 9.0 10.0 -1 60 61 62 20 21 22 23 24 25 26 27 28 29 30 at 5' 0 1 2 3 0 1 200 casing Jordan Ss Water exiting St. Lawrence through BPF at 218' Fm. BPF at 231.9' St. Lawrence 250 Fm.
Franconia Fm.
300
350
400 Franconia Fm.
Ironton-Galesville Ss.
450
Ironton-Galesville Ss.
Eau Claire Fm.
500
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters hole intergranularly through CIGL, through two BPFs at ~ 305' and 280' in upper CFRN and one BPF at ~252' in lower CSTL. This water travels uphole, where about half of flow exits through BPF in upper CSTL at 218 '. Remaining uphole flow exits through hole in casing higher in well. Flow pattern indicates that interval of CSTL between BPFs with entering and exiting water is an aquitard. BPF at 218' is shown in figure 7G. Hugo Test Well 3, 645394
gamma (API units) DEPTH hole diameter (in.) video log observations IN FT.
0 100 200 5 10 15
Glacial deposits
Prairie du Chien Gp 100
casing
150
200 Prairie du Chien Gp
Jordan Ss. Water moves downhole (emitted from OPDC/CJDN above) 250
Jordan Ss Water enters through BPF's at 274'7" & 271'
St. Lawrence Fm. 300 Water exits through BPF at 297.1 ft
aquitard
flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters borehole from OPDC and CJDN, travels downhole, and exits through BPF at ~297' in upper CSTL. Flow pattern suggests aquitard in upper CSTL/lower CJDN. BPF at ~297' is shown in Fig 7E. Inver Grove Heights area (IGH Parks) 257056
gamma (API units) DEPTH temperature (F) fluid resistivity (ohm-meters) video log observations IN FT.
0 300 52.3 52.8 25 30 glaical deposits 0 casing Prairie du Chien
50
100
150 Prairie du Chien Jordan Ss
BPF at 200' 200 ?
Jordan Ss BPF at 233'
St Lawrence Fm 250 ? BPF at 251.8'
Water moves uphole Water enters through BPF at 273'
St Lawrence Fm Franconia Fm 300
aquitard
flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters through BPF at 273' in CSTL, travels uphole, exiting through BPFs and possibly in intergranular fashion in CJDN. Flow pattern indicates aquitard(s) in upper CSTL and/or lowermost CJDN. BPF at ~273' shown in figure 7H. Mccarrons Lake #3 (St Paul Water Utility) 225868
gamma (API units) hole diameter (in.) Observations of CSTL on video log DEPTH IN FT.
0 bedrock surface 200 12 13 14 15 at 139'
440
Jordan Ss 460
BPF at CJDN/CSTL contact, 468' St. Lawrence Fm. 480
St. Lawrence Fm. 500
Franconia Fm.
520
Interpretation overview: Video log shows BPF at approximately the Jordan-St Lawrence contact Medina area domestic well 676433
DEPTH station flow (gal/min) gamma (API units) IN FT. hole diameter (in.) trolling flow (gal/min) temperature (F) fluid resistivity (ohm-meters)
0 1 2 0 100 200 3.75 4.0 4.25 -.0625 0 .0625 .125 53 53.5 54 20 24 28 32 36 40 360 bedrock surface at 307'
380 Jordan Ss. casing casing
St. Lawrence Fm. 400
420
St. Lawrence Fm. Franconia Fm. 440
460
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretaion overview: Some apparent inconsistency in trolling versus station flow logs, and very low flow velocities, making two interpretations possible at this site. Favored interpretation (shown with dashed interpretation line above) is that water enters through four discrete intervals (likely BPFs) in upper CFRN and lower 2/3 of CSTL, flows uphole, and exits through discrete interval (likely BPF) at about the CSTL-CJDN contact. This flow pattern indicates that upper part of CSTL is an aquitard. An alternative interpretation, supported largely by the trolling log, is that water enters through discrete interval (likely BPF) in upper CFRN, flows uphole, and exits through four discrete intervals (likely BPFs) in the St Lawrence Fm and CSTL/CJDN contact. The two interpretations are similar to one another in that both indicate presence of discrete intervals with ambient flow in the CSTL. City of Montgomery #1 218353
gamma (API units) DEPTH hole diameter (in.) Observations of CSTL on video log IN FT.
0 300 10 16 22
Glacial Drift Prairie du Chien Gp Jordan Ss 250 casing
300
Jordan Ss Possible BPF at 325' St Lawrence Fm
350 Possible BPF at 360' Possible BPF at 363'
Possible BPF at 380' St Lawrence Fm Possible BPF at 387' Possible BPF at 396' 400 Franconia Fm
450
500
Franconia Fm Ironton/Galesville Ss
550
Interpretation overview: Abrupt, vertically discrete increases in borehole diameter in CSTL indicate likely BPFs, especially at 380 and 396 ft. Secondary pores difficult to assess on video log because borehole walls largely covered with sediment/microbial matter. Borehole was flowmeter logged, but no unequivocal flow measured in borehole atany level, which may reflect large diameter of borehole. Video log showed no evidence of flow.
Ironton-Galesville Ss.
Eau Claire Fm. Montgomery # 2, 218355
No gamma, caliper, nor any other geophysical log. Drilling log and video only
Stratigraphic picks based on drilling log and video log:
0-254 Q 254-341 CSTL 341-475 CFRN 475-563 CICE 563-617 CECR
Observations of CSTL from video log:
253’ Casing bottom
253’-270’ Heavily fractured, “rubbly”, CSTL from approx 253’ (casing bottom) to 270’. Includes bedding plane fractures; vertical, irregular fractures (nonsystematic) with narrow apertures, and systematic vertical joints with cm-scale apertures.
270’ Prominent BPF with inch-scale aperture and perhaps subtle evidence of flow
270’-333’ borehole appears relatively smooth, although mostly down-hole view only (few side- views of borehole wall). Possible BPF at 295’.
333’ Prominent vertical fracture/joint with aperture extending at least a few ft along borehole wall.
339’ BPF, and rubbly CSTL
Several of the features described above are shown in Figures 6B-E and 7A.
Prior Lake Test Well B 672729
GAMMA DEPTH hole diameter (in.) station flow (gal/min) ambient troll (gal/min) temperature (F) fluid resistivity (ohm-meters) IN FT.
58.6 58.8 59 18.5 19 19.5 bedrock surface 0 100 200 4.0 5.0 6.0 -8 -6 -4 -2 0 2 -5 0 5 at 124' 400 casing casing St Lawrence Fm.
Franconia Fm. 450
500
Franconia Fm. 550
Ironton-Galesville Ss.
600
Ironton-Galesville Ss. Eau Claire Fm. 650
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters borehole through discrete interval (likely BPF) at ~425' in lowermost CSTL, and at 3 positions between 450' and 500' in upper CFRN, flows downhole, and exits intergranularly and through discrete intervals (likely BPFs) in CIGL and possibly in uppermost CECR. This flow pattern indicates aquitard in middle to lower CFRN. City of Stillwater #7 224467
gamma (API units) DEPTH hole diameter (in.) Observations of CSTL on video log IN FT.
0 200 8 10 12 200 bedrock surface at 119'
220
Jordan Ss
240 St. Lawrence Fm.
water too murky to clearly see casing borehole/casing above ~ 259' 260 St. Lawrence Fm. water clears, with visible flow, and BPFs, 259'-263'
Franconia Fm.
280
300
320
340
aquitard
flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Video log shows BPFs in lower CSTL, with visible flow that appears to enter borehole and flow downhole. BPFs at ~260' shown in Fig 7D. Vadnais Station A, 225622
gamma (API units) DEPTH hole diameter (in.) Observations of CSTL on video log IN FT.
10 0 100 200 14 bedrock surface at 216' 300
Prairie du Chien Gp 350 Jordan Ss
400
Jordan Ss Possible BPF at 437' St. Lawrence Fm. 450
St. Lawrence Fm.
Franconia Fm.
500
550
Interpretation overview: Video log shows no certain secondary pores in CSTL, only possible BPF at 437'. Caliper log indicates BPF in CSTL at 450'. Flowmeter logged, but no unequivocal flow measured in borehole at any level, which may reflect large diameter of borehole Victoria Creamery 256002
gamma (API units) DEPTH Observations of CSTL on video log IN FT.
0 200
bedrock surface at 349'' 360
380 Jordan Ss casing BPF, 389.5'
400 St. Lawrence Fm.
BPFs, 410'-416'
420
St. Lawrence Fm. BPFs, 430'-431'
440
460 Franconia Fm.
480
Interpretation overview: Video log shows BPFs in CSTL. No visible flow noted. BPF at 415' shown in figure 7B Winona area domestic well 235704
gamma (API units) hole diameter (in.) station flow (gal/min) DEPTH IN FT.
0 100 200 0 10 20 -1 -0.5 0 bedrock surface 200 at 32'
Prairie du Chien Gp static water static water level level Jordan Ss 250
300
Jordan Ss
St. Lawrence Fm. 350
St. Lawrence Fm.
Franconia Fm. 400
450
500
Franconia Fm. 550 Ironton-Galesville Ss.
downhole flow uphole flow
flow measurement with aquitard tool stationary interpreted flow flow abruptly enters/exits
flow gradually (intergranularly?) enters or exits
Interpretation overview: Water enters borehole through discrete intervals (likely BPFs) in CJDN and at ~335' in uppermost CSTL, flows downhole, and exits through discrete intervals in lowermost CSTL (~380') and CFRN. Flow pattern indicates that inverval of CSTL between entry and exits of water is an aquitard. Modified from Paillet and others (2000).