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HomeMy WebLinkAboutCOM 0011.000 2014-2016t DEPARTMENT OF WATER SUPPLY • COUNTY OF HAWAII 345 KEKUANAO'A STREET, SUITE 20 • HILO, HAWAII 96720 TELEPHONE (808) 961 -8050 • FAX (808) 961 -8657 November 28, 2014 Mr. William J. Aila, Jr., Chairperson and Commissioners Commission on Water Resource Management Department of Land and Natural Resources P.O. BOX 621 Honolulu, Hawai' i 96809 l xs Cn C'"i 90 N V1 Re: later Board and Department of fl'ater Supply of the County of Hatiti,ai `i 's Response to Kaloko- Honokohau National Park Service Petition to Designate Keauhois Aquifer System Area (North Kona). Hawai 'i as a Ground Water Management Area Dear Mr. Aila and Commissioners: Thank you for allowing the Water Board of the County of Hawaii ("Board ") to comment on the Petition to Designate the Keauhou Aquifer System ("Petition -) as a Ground Water Management Area, which was filed on September 13, 2013. by the National Park Service (''NPS" ). The Board respectfully opposes the Petition, as designation of the aquifer is not warranted. We therefore urge you to NOT pursue the designation process. I. INTRODUCTION h Since the Petition was filed, the Board has heard presentations and received testimony- (written and/or oral) from the NPS, Commission on Water Resource Management ("Commission ") staff, numerous representatives of stakeholders in the Kona community (public, private, and cultural), scientists in the fields of hydrology, hydrogeology, geochemistry, and biology as well as engineers, among others, as well as the Department of Water Supply's (''DWS ") staff. Since 2008, the DWS has also been closely involved in formulating and continuing the Kona Water Round Table ("KWRT' ) meetings to address the water concerns in the region and specifically within the Keauhou Aquifer system. At these KWRT meetings, presentations were made by the NPS as well as professionals in the area of ground water hydrology, anchialine ponds or pools, ground water quality management and other pertinent professions and practitioners. At each of these meetings, numerous people have attended, including members of the Board, the Commission, United States Geological Survey ("USGS'') staff, the NPS, as well as many stakeholders of North Kona. Based on the information received, the Board recognizes and believes that a strong and valid effort is in place to protect the ground water sustainability, which includes discharge into the near -shore waters, and that the scientific investigation and research does not justify- designation. Comm. No. Ref. To: ... Water, Our Most Precious Resource... Ka Wai A Kdne... P.O. Date QFE 0 1 2014 Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 2 of 12 Numerous scientists', including petitioner's own hydrologist, Paula Cutil102, stated there is no evidence that current pumping has adversely impacted resources at the park or along the coast. In fact, data from monitoring wells near or within the park indicate no increase in salinity and in some cases a decrease in salinity over the past 19 years. Rising sea level has an impact of shifting the basal lens inland; however, that does not equate to a threat to fresh water supply. It should also be noted that consumptive uses are also a public trust use of water. The following are facts regarding why each of the criteria for designation is NOT MET. II. CRITERIA NECESSARY FOR DESIGNATION TO PROCEED 1. Whether an increase in water use or authorized planned use may cause the maximum rate of withdrawal from the ground water source to reach ninety percent of the sustainable yield of the proposed water management area. %Hawai`i Revised Statutes ( "HRS ") § 174C- 44(1)1 Conclusion: CRITERIA 1 IS NOT MET. Not only is the "authorized plan use" nowhere near the ninety percent mentioned in the statutes, but there is scientific evidence that the sustainable yield number utilized by the Commission is far less than the actual sustainable yield. Discussion: .4. 6later Use and Development Plan Petitioner relies heavily on a misinterpretation of the Water Use and Development Plan of the County of Hawaii ( "WU:DP" ). The WUDP addresses a theoretical potential full build out based on the Land Use Pattern Allocation Guide ("LUPAG ") map, which only considers theoretical full build out of the entire area without regard to time. The medium growth rate projections show that in 2025. it is estimated that the water use, including agricultural use, will be approximately 18.6 million gallons per day, or about 48.9% of the sustainable yield (`'SY "). even if the SY of 38 million gallons per day (`'mgd ") is used.3 See Summary of Scientific Research on the Northern Section of'the keaarhou Aquifer System, prepared by Steve Bowles. Ph.D, Tom Nance, P.E., and . Richard Brock, Ph.D, presented to the Kona Water Roundtable on July 30, 2014 attached as Exhibit "A ". National Park Service. U.S. Department of the laterior, Water Resources Division presentation: NPS Petition for Water Management ,4rea .fiction: Scientific (Wervietir, presentation by Paula A. Cutillo, Ph.D. at the Kona Water Roundtable on August 27.2014. See Hawai 'i County Water Use and Development Plan L (August 20 10) available at: http: "www.hawai idws.org'7 %o20the0 o20water'wUdp.htm *4 Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 3 of 12 B. Sustainable Yield The current SY of 38 mgd was based on a total estimated ground water recharge of 87 mgd, while recent studies by USGS4, reported to the Commission has shown that actual ground water recharge is estimated to be approximately 77% greater or approximately, 154 mgd — four times the amount of the current SY. As our consultant for the WUDP, Jon Nishimura, explained at the Commission on Water Resource Management meeting on November 19, 2014, the use of LUPAG and associated water demand was based on a theoretical full build -out scenario where every single square foot of area was developed to its theoretical maximum extent, was never intended to be a projection of actual water use. Growth projections were also made in the WUDP to use as a guide for future planning: and based upon the medium growth rate as the most likely, to occur, it is estimated that in 2025, the water demand, including all agricultural use, will reach approximately 18.6 mgd (or 49% of SY) and further projecting that number out, it would be 25.2 mgd in 2045 (or 66% of SY), again assuming that SY is 38 mgd. C. Authorized Planned Use "'Authorized Planned Use' means the use or projected use of water by a development that has received the proper state land use designation and county development plan /community plan approvals." HRS § 17443. While the Commission has requested an abundance of data from the DWS, the statutory_ definition of Authorized Planned Use must be adhered to by the Commission. The following is the "Authorized Planned Use" as of writing this letter: Water Commitments that have land use approvals 1.14 mgd from the County (i.e., zoning, subdivision, etc,) Developer Agreements that have land use 1.21 mgd a provals from the County Vacant Service Laterals that have been paid for and 1.10 mgd installed by previous developments but are not in use because a meter has not been installed, or in some cases because development plans have changed r Open Building Permits that fall outside of the .09 mgd above categories TOTAL 1 3S4 mgd During the DWS' truncated presentation after the October 9, 2014 site visits on the Big Island, the DWS included 1.99 mgd for "other private wells." However, the Water Board and the DWS have no jurisdiction over private wells. The only non -DWS municipal wells See excerpts from USGS Scientific Investigations Report 2011-5078, "A Water - Budget Model and Assessment of Groundwater Recharge for the Island of Hawai' i, attached as Exhibit-13" hereto (hereinafter ­2011 USGS Groundwater Recharge Study "). A complete copy of the stud-, is available at: http: pubs.usgs.gov'sir 2011 5078'sir201 1- 5078.pdf Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 4 of 12 whose developments have all land use authority for full build -out are at Kukio. At full build -out Kukio's use will be approximately 0.4533 more than its existing use (this number was calculated from information obtained from an employee of Kukio). The remainder of the 1.99 mgd was given to DWS staff by Commission staff. DWS has questioned this number. DWS does not have information on the location of these irrigation wells. Whether these wells are or would be considered for a development's "authorized plan use" is highly questionable. Additionally, the Commission should NOT calculate "authorized planned use" based upon pump capacity, because: (1) there are redundant sources within the system; (2) no well would be pumped 24 hours a day; and (3) the design of the pump capacity would be much greater than actual planned use. D. Permitted Wells Petitioner is attempting to alarm the Commission by claiming that there are 51 permitted wells for production and that less than one third are reporting pumpage to the Commission. However, what Petitioner fails to understand is that some permitted wells are not in production. DWS knows that at least 26 of the 51 permitted wells not owned by them are also not in production. DWS has 14 of the listed wells, is reporting pumpage on 12 of the wells and 2 of the wells cannot be reported because the wells are not in production yet. Additionally, as a practical matter, wells are generally not pumped to their capacity, and back -up wells are standard practice as the equipment requires quite a bit of maintenance and often requires replaceme 1t which could take several months to accomplish. Therefore, total pumping capacity is always significantly higher than what is actually being used. E. Protecting Aatiti °e Hawaiian Rights and Practices Petitioner accuses both the Commission and DWS of not considering the supply of water necessary to protect the traditional and customary Native Hawaiian rights and practices. This is simply not true. The SY determination considers many factors, including ground water discharge that may affect recreational as well as aquatic and wildlife habitat (USGS Circular 1186). Though the original model may not have accounted explicitly for these issues, the recent studies that are resulting in much higher SY numbers do. 2. There is an actual or threatened water quality degradation as determined by the department of health. [HRS 4? 174C- 44(2)1 Conclusion: CRITERIA 2 IS NOT MET. To the Board "s knowledge, the Department of Health has not made any finding that there is an actual or threatened water quality degradation. See also discussion under Criteria 4. Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 5 of 12 3. Whether regulation is necessary to preserve the diminishing groundwater supply for future needs, as evidenced by excessively declining ground water levels. [HRS § 174C- 44(3)1 Conclusion: CRITERIA 3 IS NOT MET. Overall recharge is 77% higher than what was used to determine the currently used SY of 38 mgd. Discussion: The Petition references the 2011 USGS Groundwater Recharge Study that addresses climate change and refers to Timm and others (2009) and their study on rainfall estimates for the late 21't century on the Big Island. The 2011 USGS Groundwater Recharge Study projects a slight increase in precipitation for most of the Big Island, including Kona. This study also addresses the ground water recharge and estimates that the overall recharge is approximately 77% higher than what was used to determine the SY of 38 mgd. See Exhibit "B'". This section also states that the RAM methodology for determining SY did not consider these trends in rainfall and sea level. It should be pointed out that the 2011 USGS Groundwater Recharge Study does consider the climate change in determining overall recharge. Finally, the SY is not the only criteria that is being looked at by the many scientists who have come forth and shared information in determining potential impacts based on the ground water withdrawal. 4. Whether the rates, times, spatial patterns, or depths of existing withdrawals of ground water are endangering the stability or optimum development of the ground water body due to upconing or encroachment of salt water. IHRS § 174C-44(4)1 Conclusion: CRITERIA 4 IS NOT MET. There is no evidence of any danger to the aquifer due to the existing withdrawals. As the Commission witnessed and heard at the site visit at the Kahalu'u Shaft on October 9, 2014, shaft pumpage is being reduced and will be relegated to use as a back -up source in the near future. Discussion: The Petition is inaccurate and misleading. Paragraph 4 on page 33 of the Petition states that "In 2011, sodium levels in drinking water from Kahalu'u well field were as high as 185 milligrams per liter (mg /L)..." and "As of January 2013, chloride levels in Kahalu'u well field remained as high as 410 mg /L..." THESE STATEMENTS ARE INCORRECT AND MISLEADING. In 2011, the average sodium level in the Kahalu'u well field ( Kahalu'u Wells A, B, C, and D) was approximately 80 mg /L (ppm). The report presumably extracted the 185 mg/L sodium result from the DWS' 2011 Consumer Confidence Report (aka Water Quality Report). This 185 mg /L result is actually a Kahalu'u Shaft sample, and not from the Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 6 of 12 Kahalu'u well field. Also, the average chloride concentration from the Kahalu'u Wells A, B, C, and D between January 2012 and December 2012 was approximately 138 mg/L (ppm) (See http: / /www.hawiiidws .orb /7 %20the %20water /ccryaage htm). The Petition appears to total the chloride concentrations from the KahaVu wells, which is incorrect. DWS has already begun the process of reducing the pumpage of the Kahalu'u Shaft, as explained at the site visit on October 9, 2014, and the Kahalu'u Shaft will be relegated as a back -up source. There is simply no evidence that any increase in the number of pumping wells located in the vicinity of Kaloko- Honokohau would have an effect on freshwater discharge to coastal ecosystems within the Park. In fact, in the graphic shown below, which is from Paula Cutillo's presentation to the Commission on September 17 2014, shows conductivity (an indication of salinity) at a stable level from 2007 through 2011. —KAHO WELL ' —KAHO WELL 2 —KAHO WELL 3 20000 — 16000 d4. E E 12000 3 6000 p 4000 O Drc -06 0ec -07 0oc -c8 0a 09 0­10 0ec -11 0sc-12 - -KAHO WELL 2 —KAHO WELL 3 25 _ 50% E h 20 E ao °a v 15 30% la .o ��IrMfM/M�r1iMIMOr 1�//I yy �� m p 5 10% y 0 0ec -06 0ac -07 Doc -OB 0e. -09 0ec -10 Dec -11 Dec -t2 5. Whether the chloride contents of existing wells are increasing to levels which materially reduce the value of their existing uses. [HRS § 174C- 44(5)1 Conclusion: CRITERIA 5 IS NOT MET. The DWS typically attempts to blend the Kahalu'u Shaft and Kahalu'u Well water sources with each other in order to dilute the chloride concentrations. In addition, where it is physically and hydraulically possible, the higher - elevation/lower - chloride sources are blended with the Kahalu'u Shaft and Kahalu'u Well water sources. The blending cf water sources reduces the chloride levels in the water system and is done for the benefit of the community and water users, and the blending inherently increases the "value" of the water. The DWS has invested time and monies to develop additional higher- elevation/lower- chloride water sources in order to reduce the daily- pumpage from the Kahalu'u Shaft and Kahalu'u Wells. Mr. William J. Aila. Jr., Chairperson and Commissioners November 28, 2014 Page 7 of 12 Discussion: As documented, in the early 1990's Keauhou - Kamehameha Well 2 and Kalaoa Well were drilled at higher elevations, and a high - elevation water sources was discovered with significantly lower chlorides. As additional high- elevation water sources were developed, the DWS would pump and transmit the lower - chloride water to customers in the vicinity of the high - elevation sources. Recently, due to the completion of new transmission waterlines, the DWS blends the Kahalu`u Shaft and the Kahalu`u Wells' water with these higher - elevation water sources in order to dilute and decrease the chloride concentrations, thereby increasing the aesthetic and overall "value" of the water. Recent water quality analyses for chlorides in the North Kona water system has shown that this high - elevation/lower chloride water is flowing to portions of the water system that were previously- served by the Kahalu`u Shaft and Kahalu`u Wells. Thus, the "value" of the water has increased in these areas that now receive waters with lower chloride levels. 6. Whether excessive preventable waste of groundwater is occurring. [HRS §174C- 44(6)1 Conclusion: CRITERIA 6 IS NOT MET. The Petition inaccurately states the amount of single - family use. In addition, the DWS is a statewide leader in leak detection. Discussion: The Petition inaccurately states: "According to the County of Hawaii 2010 WUDP, water consumption in North Kona is 1000 alg lons per dam ep r single- family residential unit — 2 times higher than other areas of the county (Fukunaga & Associates, Inc. 2010)." The 1000 gallons per day (gpd) is per connection, which includes larger meters. The DWS has performed a recent assessment of average residential use rates in the area and has determined that accounts in typical residential subdivisions use an average of approximately 410 gpd. This is in line with what the DWS uses island -wide at 400 gpd average. See Rules and Regulations of the Department of 11 ater Slrpply, County, of flawai'i, effective October 21, 2004 (as revised) ("DWS' Rules ") available at: http://,A-w-\v.ha\,,,aiid\N,s.org/3%20about%20water/' )d%20rutes/Rules%20and%20Regulation s %20Effective %2010- 21- 04.pdf The DWS also aggressively addresses waste and conservation. An unaccounted water program has been in place at the DWS for over 20 years, and our leak detection program has been a statewide leader as evidenced by our participation with assisting the Honolulu Board of Water Supply in establishing its program. To date, DWS has installed thousands of data loggers which help to detect leaks, whether in the public water system or through customers" piping. Also, more reliable and accurate meters have been installed at our sources so that we can compare pumping and consumption more dependably. Telemetering equipment was also installed /replaced to ensure that pumps shut off when the tanks are full and do not overflow the tanks. The DWS has put in a substantial Mr. William J. Ai la, Jr., Chairperson and Commissioners November 28, 2014 Page 8 of 12 effort in determining and minimizing unaccounted water, as we realize that reducing waste is important in keeping our resources sustainable in the long run. Additionally, the DWS regularly collaborates with elementary through high school teachers to educate their students about water conservation and stewardship, both in the classroom and at our facilities. We also participate regularly in the annual statewide "Detect -a -Leak Week" campaign, where we work with local hardware stores to hand out free toilet tank leak detection tablets to customers island -wide. 7. Serious disputes respecting the use of ground water resources are occurring. [MRS 1740- 44(7)] Conclusion: CRITERIA 7 IS NOT MEC There are no disputes regarding the use of ground water resources except for this disputed Petition, which is unsupported by scientific facts. Discussion: NPS claims that it has commented on numerous "issues" with respect to ground water in the area, making it clear that NPS is the only entity, which, irrespective of scientific data, is creating these "disputes ". We believe that NPS' "issues." are being addressed and that real efforts are being made, including the addition of monitoring wells to obtain additional information within the aquifer. In fact, the DWS is currently working on a monitoring plan for its high level sources., including a component to concurrently monitor a down gradient basal source. We intend to share this information with the Commission as it becomes available. 8. Whether water development,projects that have received any federal, state, or county approval may result, in the opinion of the commission, in one of the above conditions. [MRS § 174G44(8)] Conclusion: CRITERIA 8 IS NOT MET. See discussions above. III. OTHER IMPORTANT CONSIDERATIONS 1. No Adverse Effects on the N °S NPS relies on a ground water model and analysis done in 1999 and states: "... that if all permitted wells were pumped at their maximum rate, ground water discharge at the coastline in the Park would be reduced to 47% of the 1978 rate and water levels would decline by about 0.6 ft. (Oki et al. 1999)(Figure 9)." There are more recent models and. analyses done, and the results referred to in the above paragraph are no longer valid. The Board was not presented with any evidence that freshwater Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 9 of 12 discharge to the National Park was diminished or would be diminished in the foreseeable future as described in the 1999 study. As a matter of fact, a review of the conductivity data from 2008 to 2012 from two observation wells, KAHO 2 and KAHO 3, indicated conductivity levels have dropped slightly, indicating a slight increase of freshwater (https: / /irma.nps. ov /App /Reference /Profile/2193295) NPS makes repeated references to the EA for the Palani Ranch Well (Geometrician Associates LLC 2009). The EA addresses the cumulative pumping effects on salinity increase and thermal change at the NPS inland ponds as well as coastal waters. The EA specifically addresses the orange -black damselfly, and the one completed lab test (a total of 3 were to be done) showed that the predicted salinity increase and thermal change was insignificant to the habitat of the studied damselfly. The EA also addressed mullet and other native fish that have a wide range of tolerance for salinity and will not be impacted. 2. Protecting Public Trust Resources The NPS vastly overstated the precautionary principle and omitted an essential part of the code. The Petition provides: "Pursuant to the precautionary principle, when 'the water resources in an area may be threatened by existing or proposed withdrawals or diversion of water' the Commission has a duty to designate a water management area [HRS § 174C- 41] "'. What the Petition fails to include in its quotation is the following: "When it can be reasonably determined, after conducting scientific investigations and research that the water resources in an area may be threatened by existing or proposed withdrawals or diversions of water, the commission shall designate the area ... "' The Petition's omission is not only glaring, but an indication of the Petitioner's lack of any, scientific proof that ground water withdrawals or proposed withdrawals from the Keauhou Aquifer are affecting or will affect the Kaloko- Honokohau National Historical Park. As a political subdivision of the State, DWS recognizes its duty to conserve and protect Hawai'i's natural resources. We further understand our obligation to promote the development and utilization of these resources in a manner consistent with their conservation and in furtherance of the self - sufficiency of the State. With this in mind, we also recognize that the waters of the State are held for the benefit of the citizens of the State, and that the people of the State are beneficiaries and have a right to have the waters protected for their use. The policies set forth in the Hawaii State Constitution and in the State Water Code are what guide DWS when implementing its programs and policies concerning water resources within the County of Hawaii. In furtherance of these policies, DWS remains active in its conservation efforts. To address the problems of supply and conservation of water, DWS has a rigorous leak detection program, and an active conservation education program, and also has dedicated $150,000 of its budget for its unaccounted water program for equipment maintenance and replacement. Although the DWS only provides potable water, if a customer wants a meter for irrigation/landscaping use, the DWS requires the customer execute an Irrigation Agreement /Master Landscape Water Meter Agreement, which, amongst other terms, authorizes the DWS to terminate or restrict the meters in its sole discretion. DWS may also limit or restrict water flow to all agricultural water uses in the event water service to domestic water uses is detrimentally impacted due to agricultural water use or a water shortage. See DWS" Rules. Per DWS' Rules, water commitments are based on the availability of water. In determining the availability of water, DWS considers population, projections, environmental constraints, past water usage, zoning, land use districting, water system constraints, outstanding water commitments, capital Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 10 of 12 improvement program scheduling, undeveloped available water resources, regulatory requirements of ground water control areas, and any other significant factor, including public trust principles. See Rule 5, DWS' Rules. DWS recognizes that adequate provision of water resources shall be made for the objectives set forth in the State Water Code. Although the priority of water uses has not been an issue, DWS is prepared and understands the State's policy to prioritize the provision of water resources for the "protection of traditional and customary Hawaiian rights ", the "protection and procreation of fish and wildlife, the maintenance of proper ecological balance and scenic beauty, and the preservation and enhancement of waters of the State for municipal uses, public recreation, public water supply, agriculture, and navigation." DWS continues to work to protect and improve the quality of the waters within the County of Hawai'i, and through continual monitoring and maintenance of operations strives to protect existing water from contamination and to maintain a high standard of water quality. DWS works closely with the Commission in monitoring the pumpage of its wells, and voluntarily adjusts pumpage when prudent. 3. Designation is not Necessary, Petitioner's Petition centers around the premise that without designation, the Commission has no tools to manage the aquifer. This is simply, not true. The Commission already, has the tools and does not need to rely- on a water management area.. Some of the greatest tools are the components of the Hawai `i Water Plan, which includes the Commission's Water Resource Protection Plan, the State's Water Quality- Plan, the State Water Projects Plan, the Agricultural Water Use and Development Plan, and the Counties' '\ UDPs. The Board would also like to take this opportunity to point out that the County of Hawaii was the first to update its WUDP and is currently in the process of updating it once more, including the section on the Keauh.ou Aquifer System area. Additionally, designation is NOT necessary for the Commission to regulate the location and pumpage of wells in the Keauhou Aquifer System. Existing well construction and pump installation permit processes allow opportunities for input. See Figure 1 attached hereto. In fact, through discussions with Commission staff regarding a well in Ka'u, the DWS has limited the pumping from that source. The Board is convinced that water resources are protected by multiple layers of review and enforcement currently in place at the county, state and federal levels. The Board acknowledges the successes at nearby Kohanaiki and NELHA as primary examples of this. They have not only complied with laws and regulations. but have collaboratively worked with the community- and area stakeholders to create successful ecosystems balanced with successful financial ventures. The Board believes there is and will continue to be an abundance of fresh ground water adequate to meet the needs of public trust resources for the foreseeable future. The Board echoes frustration heard within the community about the actual ability to perform Native Hawaiian practices within the Kaloko Honokohau National Park ("Park ") since it was established 36 years ago. The abundance of fresh ground water is likely to be more apparent with the proper maintenance and removal of invasive plant species within the Park. Perhaps the NPS should focus more effort and resources within the Park's boundaries prior to an exterior focus. Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 11 of 12 IV. CONCLUSION The Board, after a comprehensive assessment of the information available, finds that the Board must continue to work collaboratively with private entities, federal, state and county agencies, as well as the local community, in managing the development of the North Kona water system for the benefit of the community while collectively working to protect the Keauhou Aquifer as a public trust resource. Mr. William Tam, Water Commission Director, addressed designating all of Hawaii as a water management area by earning against letting isolated conflicts drive designation. He states: "In areas not under stress, you don't need to permit everything right now because of a conflict. There's always the danger of the tail wagging the dog, of using a water conflict to get the zoning. " It would appear to the Water Board that this particular petition could become an isolated conflict and designation would not be necessary to address the concerns of the NPS. We propose to continue to work with the Commission, NPS and community- stakeholders in making sound decisions that will be in the best interests of the community, county, and state, as well as help keep our natural public trust resources protected. We would not support a decision to designate the Keauhou Aquifer System, and therefore request again that you deny the petition. Sincerely, Water Board Chairman Quirino ,Xht�nio, Jr., Manager -Chief Engineer c: Honorable William P. Kenoi, Mayor, Iaw i`i County Honorable David Ige, Governor -Elec oft State of Hawaii Hawaii County Council Chairperson, shimoto Hawaii County Council Chairperson - Elect, Dru Kanuha Hawaii County Council members (elect) Senator Josh Green Senator Mazie Ilirono Senator Lorraine Inouve Senator Gilbert Kahele Senator Russell Ruderman Senator Brian Schatz Representative Richard Creagan Representative Tulsi Gabbard Representative Nicole Lowen Representative Mark Nakashima Representative Richard Onishi Representative Joy San Buenaventura Representative Mark Takai Environment Hatiwai 'i, Volume 24, Number 10, April 2014 Mr. William J. Aila, Jr., Chairperson and Commissioners November 28, 2014 Page 12 of 12 WELL CONSTRUCTION / PUMP INSTALLATION PERMIT PROCESS Figure 1 APPLICANT 1 CTFe? APPLICATION: APPLICATIONS) 3a - 3J c r E . M .. —T :1 al :j N iL v STAFF �E ,F -:; '. _E Y. MONTHLY ' -� BUILFTIN 1_ �: DOH �cxP - COUNIY -'I c ___ _ %�• - LUCIOCCL r DI fIS, IO ION a a PLANNING 1 . .. PUBLIC �e -I' - _ F E�� -iii _ �• �I _ _ � � 1740 13 -168 EVALUATION -- c I ,J. .- � • "- di "'. '., :NL!....- f.`h '_ _:. ':: ,: -. C�- �n HMI ,u STAFF 174C 13 -168 CONDITIONS ACTION PERNIIT(S) _ ISSUED NOTICE ___ OENV APPROVE ; -, - I .._: ._ — - - �— l M1.i c .I EJECTION R _J = JRII LFR O '. I n =. c -_ I c MITER ! - F 111, cIV E ONLY _._ ' .. -. APPLICANT---- —. __� ____1__.— C.'h!.. r., of -, tl�•.. - -. LETTER OF ASSLRANCF r— L CRWM TO AMEND, MODIFY REVOKE, SUSPEND - YES NO ' OR STAFF OR PI — _ COMPLETION nc .- -%I f _ „r:.� RE PORTISI a rrr ro.._.,- IF STAFF. N ACCEPT?: t _ , FJLf - -- ACC1-?fANCF CERIIFICAIF OF ! -I -J CNIF2M =:L - hi, �- -. DpLLEF LETTER COMPLETION 5J ACTION ! ._._ i -' ry -- e. .,x. -�caF`iE la' hArE 'F .. ^-ae' ": r• HELL E -. -' E 'WELL ORIr1TR OPERATOR IANOOWNER� !�_, Figure 1 Summary of Scientific Research on the Northern Section of the Keauhou Aquifer System Prepared by: Steve Bowles Groundwater Geologist Dr Richard Brock, Ph.D. Aquatic Resource Specialist Tom Nance, PE Hydrologist /Water Resource Engineer Dr Steve Dollar, Ph.D. Coastal Zone & Coral Reef Specialist Presented to: Kona Water Roundtable July 30, 2014 Exhibit A Preface In response to the September 13, 2013 petition filed by the Kaloko- Honokohau National Historical Park to designate the Keauhou Aquifer System as a Groundwater Management Area, four professionals prepared summaries of their ongoing work in the region. The findings of these studies come to a consistent conclusion: no evidence collected to date indicates that withdrawals of groundwater resources from the high -level and basal aquifers in the northern section of the Keauhou Aquifer System have negatively impacted basal groundwater, the ponds, and the nearshore marine waters. This document summarizes their decades of work in and around the Keauhou Aquifer System area. These collective scientific investigations and research address the issues from several perspectives: looking at the area's quantity and quality of water in the subsurface, in anchialine pools, in fish ponds and in the nearshore marine environment. This document contains all four reports. The reports are presented to the Kona Water Roundtable, a cooperative assembly of government representatives, professionals, landowners, consultants and others who share an interest and concern for the condition of the aquifer. The Roundtable is a venue to share information. The reports provide a comprehensive look at respective findings and conclusions of their ongoing research. Following are highlights of their respective findings. This is followed by a map of the region, Executive Summaries of each report and each of the full reports. Summary of Findings: Steve Bowles, Groundwater Geologist "Cumulative hydro - geologic data and field observations of the Keauhou Aquifer System obtained during the past half century support the conclusion that declaration of the Keauhou Aquifer System is not necessary at this time." "The discovery of high -level ground- water by Kamehameha Schools /KSBE in 1990 set the precedent for the subsequent development of high level ground -water by the DWS and others." "The high level ground -water system is complex with various water levels and has numerous compartments. Large quantities of high level ground -water in the south sector remain undeveloped." "Sustainable yield assumptions based upon only a basal lens inaccurately describe the complexity of ground -water occurrence in the Keauhou Aquifer System. The recharge estimates by the USGS further reduce the present accuracy of sustainable yield estimates." Steve Dollar PhD, Coastal Zone Specialist "Repetitive analyses of water chemistry in the two large fishponds in KAHO reveal no negative impacts were detected in nutrient dynamics over the last 12 years. In fact, time- course data indicate a potential reversal of pond metabolism toward a less senescent (biological aging) stage." "Based on the results, it appears that the existing development upslope of KAHO is not causing detectable input of nutrient subsidies, or reduction in groundwater flux to the ponds." 7 Tom Nance, PE, Hydrologist "High level pumpage began in 1994 and is now at about 4.0 to 4.5 MGD ... The TNWRE monitoring data (of continuous water level recording in the Kamakana well and time series salinity profiles in three others in the immediate vicinity of the National Park) establish that no impact to basal groundwater as a result of high level groundwater pumpage has been identified to date." "The discovery of fresh water under artesian pressure at depth below the basal lens in the Keopu and Kamakana deep monitor wells suggest that some or possibly even most of the high level groundwater actually flows beneath the nominally downgradient basal lens rather than into it. If discharge of high level groundwater into the basal lens is only occurring in limited amounts, then foreseeable future increases in pumpage of high level groundwater will have little or no impact on the basal lens." Richard Brock PhD, Aquatic Resource Specialist "Despite the fluctuations in concentrations of some nutrients in anchialine pools, there is no evidence of decline to pond biota connected to changes in water quality." "in the Ocean: No evidence of increased nutrients due to development when compared to adjacent control areas." "On Land: Transitory increases seen in anchialine pools but the signature is lost at the shoreline. No decline found in the pond biota connected to changes in water quality." uoogie farm image Noting Keauhou Aquifer System Area, the Kona CDP Urban Area and the National Park Steve Bowles Groundwater Geologist Findings and Conclusions Cumulative hydrogeologic data and field observations of the Keauhou Aquifer System (KAS) obtained during the past half century support the conclusion that declaration of the Keauhou Aquifer System (KAS) is not necessary at this time. The KAS as a whole is underdeveloped at this date. Early work in preparing estimates of sustainable yield is inadequate. Many of the descriptions of the hydrogeology have oversimplified the actual occurrence of the local ground- water. Further deep core drilling is needed to better under -stand the geologic elements which make up the working components of the KAS. A comprehensive water resource management plan must also be prepared and modified as knowledge through exploration continues. Findings: Our work, covering 40 years of investigation, has led us to create the findings listed in the first four items below. 1) The Keauhou Aquifer System consists of four basic units: a) North sector - high level and basal b) South sector - high level and basal 2) Likely causes of high level ground -water occurrence: a) Fault scarps covered by younger lavas b) Trachyte lava flows c) Combinations of a and b 3) Multiple water levels in the high level aquifer region of KAS indicate a complex of aquifer compartments. 4) Cold water shoreline basal springs between Keahole Point and Kaiwi Point result from: a) Deep ocean temperature intrusion b) Highly permeable shallow lavas c) Tide fluctuations and their efficiency The bullet points listed below best describe the present operating status of the KAS. • The management programs of well spacing and pumping at the Huehue Ranch and Kohanaiki well fields have had no significant direct impact on the basal lens quality at the shoreline. • The high level well pumping has had no direct impact on the basal lens in the north sector to date. • Over pumping of the Kahaluu shaft and the Kahaluu wells in the south sector has resulted in dynamic salt water encroachment which is reversible when pumping is reduced. • Water development in the north sector does not impact the south sector ground -water flow or quality. Efforts to provide a model simulation of the entire KAS are futile. • The specific migration of high level ground -water flow to the ocean is not yet defined. Evidence from the Kamakana Bore (well 3959 -01) and from well 3858 -01, (thick, dense lavas, combined with artesian flow) provides some explanation (see Tom Nance presentation). Similar evidence is also found in the Huehue wells and in wells on the north slope of Hualalai. 4 • The high level ground -water system is complex with various water levels and has numerous compartments. Large quantities of high level ground -water in the south sector remain undeveloped. • Sustainable yield assumptions based upon only a basal lens inaccurately describe the complexity of ground -water occurrence in the Keauhou Aquifer System. The recharge estimates by the USGS C[.A. Engott 2013) further reduce the present accuracy of sustainable yield estimates. The actual sustainable yield most probably lies between the two estimates. • It is important to note that all pumped water is either discharged to the atmosphere by • evapo - transpiration; • infiltration from irrigation; or • shallow disposal of storm water and wastewater. There is no discharge or runoff directly to sea in the north sector. Some extreme storm runoff does occur in the south sector. Tom Nance, PE Hydrologist /Water Resource Engineer Findings and Conclusions Using monitoring data of North Kona groundwater that TNWRE has compiled, this report addresses whether or not impacts to basal groundwater have occurred as a result of pumping the six high level groundwater wells located above Mamalahoa Highway from Kalaoa to Waiaha. High level pumpage began in 1994 and is now at about 4.0 to 4.5 MGD (Figures 2 and 3 in the report). The TNWRE monitoring data that addresses this question consists of continuous water level recording in the Kamakana well and time series salinity profiles in the Kamakana, Kaloko -2, Ooma Mauka, and Ooma Makai wells. The report presents and evaluates this data. The water levels at Kamakana and the salinity profiles at all four wells establish that no impact to basal groundwater as a result of high level groundwater pumpage has been identified to date. A key unresolved issue is whether or not the high level groundwater actually drains into the nominally downgradient basal lens in the area between Keahole Point and Kailua Town. Evidence gathered to date suggests that at least some, if not most, of the high level groundwater actually flows at depth beneath the basal le rns to discharge into the marine environment offshore. The anomalous characteristics of the basal lens suggest this: very low water levels relative to the actual ocean level; very high salinity; temperatures significantly lower than the high level groundwater; and increasing salinity in wells under modest pumping rates. The more compelling evidence is provided by the discovery of fresh water under artesian pressure at depth below the basal lens in the Keopu and Kamakana deep monitor wells. If leakage of high level groundwater into the basal lens is limited or only occurring in modest amounts, then foreseeable future increases in purnpage of high level groundwater will have little or no impact on the basal lens. With this unresolved issue, monitoring for potential impacts to basal groundwater going forward should be continued and even expanded. This expansion should include deepening the Kaloko -2 well so that possible changes to the thickness of the basal lens at this location can be tracked. Dr Steve Dollar, Ph.D. Coastal Zone & Coral Reef Specialist Findings and Conclusions This report has been prepared in response to a petition by the National Park Service (NPS) to the State Commission on Water Resource Management to designate the Keauhou Aquifer as a Groundwater Management Area. The petition asserts that present or planned future use of groundwater from the Keauhou Aquifer will reduce the flow of basal groundwater through Kaloko Honokohau (KAHO) National Historical Park, thereby causing harm to KAHO's anchialine ponds and its nearshore marine environment. This report summarizes data collected by Marine Research Consultants, Inc. during four field surveys between 2000 -2012 for the purpose of evaluating the composition of waters within two large fishponds within KAHO(Aimakapa and Kaloko) and the coastal ocean offshore of these fishponds, with particular emphasis on evaluating the contribution and fate of groundwater input. In the earlier studies (2000, 2007) Aimakapa Pond exhibited little vertical and horizontal stratification, appearing as a uniformly well -mixed system with long residence time. These conditions were characterized by near complete uptake of all inorganic nutrients entering the ponds through groundwater flux, and elevated values of organic nutrients that are the product of decomposition of organic material. This condition indicated the pond was progressing toward a terminal successional stage where the pond becomes a sediment - filled wetland. More recent studies in 2012 reveal consistent input of groundwater along the landward shoreline of the pond, resulting in steep gradients of salinity and inorganic nutrients found in groundwater. These results suggest that there has not been a detectable decrease in basal groundwater to the ponds; in fact the opposite appears to be the case. While the differences in groundwater dynamics within the ponds over the 12 -year interval of studies may reflect the relationship between sampling and tidal state, results of these studies indicate that at a minimum the fishponds are not in a cycle of uninterrupted progression toward a more senescent state. Scaling nutrients concentrations to salinity indicate that there are no nutrient subsidies to the ponds from sources other than naturally occurring groundwater. None of the data scaling inorganic nutrients to salinity within the ponds or nearshore ocean indicate substantial nutrient subsidies to groundwater that could be a result of human activities in upland areas. These results indicate that under the present scenario, the existing development upslope of KAHO is not causing detectable input of nutrient subsidies, or reduction in groundwater flux to the ponds. Rather, recent conditions in the ponds appear to represent a more open system with respect to hydraulic and nutrient fluxes. In a companion report TNWRE found no impacts to basal groundwater have been identified to date as a result of high level groundwater pumpage. While it is not resolved whether high level groundwater actually drains into the nominally downgradient basal lens, evidence gathered to date suggests that at least some, if not most, of the high level groundwater actually flows at depth beneath the basal lens to discharge into the marine environment offshore. If leakage of high level groundwater into the basal lens is limited to the modest amounts that evidence collected to date suggests, then the foreseeable future increases in pumpage of high level groundwater will have little or no impact on the basal lens. 6 If indeed pumping of high level groundwater has minimal effects on basal groundwater, then it is clear that pumping high level groundwater will also have no effect on nearshore processes influenced by basal groundwater. The results summarized in this report correspond to such a conclusion, as no negative impacts were detected in nutrient dynamics of the KAHO fishponds over the last 12 years. Dr Richard Bruck, Ph.D. Aquatic Resource Specialist Findings and Conclusions As part of the permitting process allowing the Kohanaiki development to occur, the County of Hawai'i imposed a requirement for a water quality monitoring program to insure that the quality of the ground and nearshore marine waters are not degraded as the development proceeds. This monitoring program was reviewed by federal and approved by state and county agencies. The methods follow the Hawai'i State Department of Health (DOH) Regional water quality monitoring protocols. Sampling is carried out six times a year during dry periods as well as following high rainfall events where the "trigger" initiating sampling is 1.5 inches or more of rainfall falling within a 24 -hour period. In each survey between 105 to 110 samples are collected. Samples are collected from the ocean, in brackish anchialine ponds present on the project site and from wells present In the project area. Ocean samples are collected fronting the project site as well as at control sites. Sampling comm enced in 2005 and up to present there have been 57 monitoring surveys collecting and reporting on 5,683 samples making this monitoring program the most stringent of all such non - potable monitoring programs in West Hawai'i. Findings: 1. Non - compliance with state water quality standards among parameters measured in the ocean occurs on a coast -wide basis and is not differentially greater at sample sites fronting the Kohanaiki development. Indeed, highest parameter means are found at control locations which is related to greater groundwater flow at those locations. 2. In natural undisturbed West Hawai'i environments, nutrient concentrations (which is what we measure) in the seaward flowing coastal groundwater vary tremendously through both time and space. At some locations concentrations are naturally elevated and at others they are low, but all of them hale high variability in concentrations through time. However as groundwater approaches the ocean these high concentrations decrease tremendously primarily due to dilution. 3. With development the same facts hold but coastal development will usually cause increases in some nutrient concentrations and these are seen at sample points makai of the development (primarily in anchialine pools) but again the signature continues to be lost at the shoreline. Increases in concentrations are transitory and are usually seen during the period of golf course turf establishment and once completed, concentrations decrease. Despite the fluctuations in concentrations of some nutrients in anchialine pools, there is no evidence of decline to pond biota connected to changes in water quality. This is due to: (1) these increases are usually less than the concentrations found at some completely undisturbed sites, (2) the anchialine biota have evolved in a system with this high natural variability in concentrations and are completely insensitive to it and (3) if a nutrient is in excess, adding more will not have an impact at the concentrations measured in this study. Keauhou Aquifer System Summary of Hydrogeology Findings Prepared by: Steve Bowles Groundwater Geologist Waimea Water Services 67 -1161 Mamalahoa Highway Kamuela, HI 96743 Keauhou Aquifer S Summary of Hydrogeology Findings A rarely observed event: High -level ground -water entering an uncased well bore in the uplands of Palani Ranch, Island of Haveai`i. The water level was found to stand at about 95 feet above sea level and penetrated a high -level compartment of the Keauhou Aquifer System. By Stephen P. Bowles and Waimea Water Services July, 2014 ry "r ti• s .. 4. Ij- h:eauhou Aquifer System: Hydrogeology Findings By S.P. Bowles and Waimea Water Services A Summary ExixuT E Summ"Y Cumulative hydrogeologic data and field observations of the Keauhou Aquifer System (KAS) obtained during the past half century support the conclusion that declaration of the Keauhou Aquifer System (KAS) is not necessary at this time. The KAS as a whole is underdeveloped at this date. Early work in preparing estimates of sustainable yield is inadequate. Many of the descriptions of the hydrogeology have oversimplified the actual occurrence of the local ground - water. Further deep core drilling is needed to better under- stand the geologic elements which make up the working components of the KAS. A comprehensive water resource management plan must also be prepared and modified as knowledge through exploration continues. Introduction The Keauhou Aquifer System (KAS) has been the subject of numerous studies which have resulted in a progressive accumulation of knowledge of the hydrogeology. For this review, we have divided the KAS into north and south sectors for convenience of discussion. The first drilled well (1944) for exploration was built on Hualalai road and produced brackish water to supplement the water supply from Waiaha spring. During the 1950s and early 60s construction of Kahaluu wells began in the south sector and the brackish well at Kealakehe elementary school in the north sector. These wells led to the construction of the Kahaluu Shaft and an exploration well at Kalao a (Kona Palisades). The KAS can best be described by recognizing two distinct geologic compositions, which result in a complex hydro - geologic ground -water occurrence (see attached maps). Mauna Loa lavas are generally thin bedded with numerous clinker formations and dominate the southern sector. The northern half of KAS is dominated by shallow thin bedded lavas which overlay massive trachyte flows of the Hu alalai volcano. The geology is further complicated by evidence of major slumpage of the slopes of Mauna Loa and possibly Hualalai volcanos (J. G. Moore, et al. JGU 1989). Northern Sector The emphasis for this review is with the northern sector, as water from the shallow basal lens provides the majority of the visible shoreline discharge. Initial knowledge of this sector, beginning with the brackish wells mentioned above, was assumed to be dominated by the basal lens where fresher waters float on salt water. The earliest (about 1990) estimate of sustainable yield for KAS by Mink and Lau was based on the assumption that ground - waters of the KAS occur only as a basal lens. NEL114 Injection lT ell study l 1 > In conjunction with a request by the Natural Energy Lab at Keahole Point (1970's), John F. Mink and S. P. Bowles prepared a manuscript report which included data from the DLNR well to Kona Palisades (well # 4360 -01). The well was slightly brackish and clearly tapped only the thin brackish lens. TSA Golf Course lVells (2) S. P. Bowles was contracted to evaluate the hydrology and develop two wells for the proposed TSA Golf course located adjacent to Hinalani Drive (wells # 4160 -01, 4160 -02). These wells each proved to be high yielding and brackish (chlorides @ 1000 milligrams per liter). Tide records of ocean and well levels in 4160 -02 (note: mislabeled in graph) presented below were subsequently measured by Glenn Bauer of the Commission on Water Resource Management (C WRM). Kaloko Irr. 2 Well No. 4758 -02 Tidal Response I L2 LD J is r, 3 i, 3 s tJ 341 34tt lit 738 361 us 375 378 381 3" 391 336 M JUHM Day OZ-7-9410 24-83) Kaloko Irr. 2 Well No. 4759-02 Tidal Compolmut Rcnmv 3d » .................. ....... ....... .........�.....• _.. _...... �. to- - ._ ........ ... _. ..�... __ .. ... ............ ... u-- ..----- _ ............. -------- ,_ J 1.7 D4 r. WN b I►D. 1. laid W__ 2 Kukio Resort- Huehue Ranch Wed Field (3) Drilling of water wells at about elevation 1600' for the Kukio Resort began in 1989 with HR - 1 (4559 -01) which struck the basal lens with a water level at about elevation +8'. The first water pumped contained hydrogen sulfide and more detailed chemistry showed the water to be hydrothermally altered, indicating the presence of at least gas emanating from the deep magma. The total dissolved solids exceeded the secondary standards for drinking water (appendix 1). As the well field drilling progressed, the HR wells (4459 -01, 4558 -01, and 4459 -02) all found similar water and penetrated thick, dense trachyte lava flows. At a depth of 1360', HR 3 struck a particularly thick, dense formation. A sample was dated by the Hawaii Volcanos Observatory and found to have an age of about 100,000 years by (before present). DENSE TRACHYTE BASALT POROUS OLIVINE BASALT Trachyte sample statistics including ages of various sources including the wells in the Northern sector of KAS. 1 able 1 Water W01 Localities lntersecung Trachvtc, Hualalai Volcano Localitv Lab Number Well Number Depth m Sample Interval liuchue Ranch #1 MH84 -190 4559 -01 265 -372 -326 Huehue Ranch #3 1IR3 -1373 4508 -01 315-040 418 Huehue Ranch #t5 HR -5 4558 -02 236 -467 337 -353 Kalaoa 4358 -0 4358 -01 509 -512 509 -512 Kohamild #2 2 4458-02 432484 457 -460 Puu Lani Anshulu 4850 - 011470,1490 4850 -01 0 -279 143 -146 149 -152 Keo u No sample 3957 -01 --408 No sample Tank 4 Rnulu of At- 111lnetYtrtetiW) Henitut Arnlysat. ?UU Pau Wtitu Warn u1110C lluchuc ;l K,<'aoa ►Kann' Kohsnaiki Kohsroikl Anahulu Atathulit' Nit tluchuczs iz;%rrttd Arc (ka) 110 10 3 115 117 fl, s l2$ K., 110 101 it 23d 4 4 4 1 3 4 7 3 17 i Plateau A=c (km) 1044 loll, 1059 110 1 1(15 "1 107.3 294 1,4 1 a O F 1 7 24 39 MSWD' 0.79 1.90 IOM u.>It 0.61 0.55 S K-K If L 9•F C 1 D-1 GK ' :7Ar 51.2 SU.2 57.11 481{ 54,7 64.6 lsochroa Srlresed Stay Esa:t=n At, 0w) 107- F6 3 �'A 6 to,) 1 104 6 W ' i 13 3 114 101 99 26d 9.8 91 77 3,0 2.8 9 3-1 24 5 5 13 'aAr+ 'Ar, 294.8 303.5 301 S 3012 297,0 101 0 3009 293 297A 301.5 23o 4.4 3.4 2.1 3.1 1.6 33 119 16 in 7.4 htSWD 105 0.48 160 0,91 0.84 071 160 1.1 0.52 030 F%b.OfFd' 0.40 09' 015 031 0.5� 064 02n 0.33 O.gM 0.97 Includal C Q C-0 C 1 D-M &1 C -1 C -n C-P ALL A-K %"A, 911 893 628 94.3 94.6 41.4 55 ri 97.8 100 %3 "Ar X x X X X 1'mirrred Acts (Its) smvk HueHuael Kaktm Kdun -2,i Pua Aaahulu 11'aho Pete Huchuo#3 107.2 97.3 I OrLo 113.6 103.3 95 2ul 9.8 5.9 2.0 34 53 13 Merin Man Mata Hiroo Coramcn* Isoahron age imxhmo age teoehroo "Re tsothron a nimkron a3c lsoahr on etc A 11wxs arc given at the 93% seat frianct krcl. Ages were cakulatua using an age of 28A2 Me fist Fish Canyon sanidim 1Reo w e u!, 19981 aaJ the decay oottar rrth end Isotopic abu donoos of ($titer u.+JJd4W. 19771 " indicates samplts heated with it resistance furnace: other winlllm heated wrM it broad beam CO: hum t Mum critarn we those of La drug [ 19ft ` MS1YD refers to 1111x3 lum of the wrJah+cd deviates, a measure of scatter in x and y about a heat lit line t 6lrJruyrn fit"/ 1%61 S Sorps are orroned Zorn the rcgtcmxm t f. 1) including drop w otdd amc the probability of rot us drop below 0.15 (see below), or 2 i dtcy are highly inipmeue, that 13, mtnlyuW ctrors exectJ theme of the mm1 pirvw steps obtaMteA for the sarMic by a factor of �5 or mart ' Probability pmt ymtte r of dam ebau rsachwo is esalotned by sualyueal urrreminiies atoac. a value > 0 13 is considerod noetptable [e.g. Lth*4,1.19991 Excerpt from: Cousens, B.L., D. A. Clague and W.D. Sharp, 2003 Chronology, Chemistry, and Origins of Trachytes from Hualalai Volcano, Hawaii. Geochemistry Geophysics Geosystenls 4(9):1 -27. Subsequent development of these wells (which were spaced approximately 1000' apart) was placed into production with a combined estimated sustainable rate of 1.96 mgd (million gallons daily). In 2006, a major pumping test was conducted to stress the aquifer to determine how sensitive the basal lens was to pumping (appendix 1). Based on this data, the estimated sustain- able pumping rate was raised to 2.5 mgd. The average pumpage from these wells today is 1.38 mgd. Keahole to Kailua Development flan The original success of Kukio - Huehue well field continued to support the assumption that fresh basal ground -water could only be found by drilling wells above elevation 1500'. As presenter of the hydrogeology for the Keahole -to- Kailua (K -to- K) Development Plan of the county of Hawaii, S. P. Bowles recommended that potable water development for this area be developed first in the higher elevations and further, that when this pumpage reached a high point of production, that water must be imported from the south sector of the KAS. WATER RESOURCE oA DEVELOPMENT ZONE BETWEEN 1500' 8.1600' ELEVATION ,. •� 'ooa�wu�.er���r l" %IIOMwO � Y1 �} WOW NN WM IR.. _wNo Nab e 1 l' ww.. KSBE High Level Discovery (South Sector) (4) TER MAIN TO 'ORT WATER fk Y0� Q a.w ww..r O I.wM.I11�wk C NO"r.r.w REGIONAL ••• ww. waw wr WATER PLAN A � • In the meantime, in the south sector of KAS, Kamehameha Schools /Bishop Estate (KSBE) drilled a deep well from elevation 1618'. Water was struck and found to stand at elevation +278' above sea level. Following the advice of S.P. Bowles, the first well was drilled to sea level and water was found to saturate the rock to sea level indicating a very large compartment of high level ground- water. This marked the discovery of the major high level ground- waters in the KAS. Kalaoa- Honokohau Fells DWS DLNR (5) Following the strategy presented in the K -to -K Plan, the Department of Water Supply (DWS), in conjunction with the State Department of Land and Natural Resources, developed 2 wells (well 4358 -01, well 4258 -03). The average pumpage from these wells in 2013 was 0.89 mgd. Adding north sector wells, #4153 -02 and #4057 -01, brought the total to 3.67 mgd. 5 MWt PM own .YwR ' 4. .O KSBE High Level Discovery (South Sector) (4) TER MAIN TO 'ORT WATER fk Y0� Q a.w ww..r O I.wM.I11�wk C NO"r.r.w REGIONAL ••• ww. waw wr WATER PLAN A � • In the meantime, in the south sector of KAS, Kamehameha Schools /Bishop Estate (KSBE) drilled a deep well from elevation 1618'. Water was struck and found to stand at elevation +278' above sea level. Following the advice of S.P. Bowles, the first well was drilled to sea level and water was found to saturate the rock to sea level indicating a very large compartment of high level ground- water. This marked the discovery of the major high level ground- waters in the KAS. Kalaoa- Honokohau Fells DWS DLNR (5) Following the strategy presented in the K -to -K Plan, the Department of Water Supply (DWS), in conjunction with the State Department of Land and Natural Resources, developed 2 wells (well 4358 -01, well 4258 -03). The average pumpage from these wells in 2013 was 0.89 mgd. Adding north sector wells, #4153 -02 and #4057 -01, brought the total to 3.67 mgd. 5 According to information obtained during construction, it was determined that the wells penetrated several dense strata with the water level rising with increasing depth. This is further substantiated by Glenn Bauer who stated in his 2003 report, "Even though the DWS' Kalaoa Well (4358 -01) had a measured water level at 237.5± ft., msl in 1990, the bottom elevation is -57 ft., msl. When the DWS' Hualalai Well (4258 -03) was drilled 1.5 miles south of Kalaoa Well, the initial water level was 191 ± ft., msl when the bottom elevation of the well was 43 ft., msl. After an initial aquifer test was performed, the well was deepened 99 ft. to - 142 ft., msl. As a result, the water level in the well rose to 293± ft., msl. Deepening this well provides implications for ground -water flow in the high -level water body. " (Bauer, 2003, A Study of the Ground -Water Conditions in North and South Kona and South Kohala Districts Island of Hawaii, 1991 - 2002). KSBE, Kukio, Palamanui Hydrologic Budget KSBE and Kukio Resorts contracted Waimea Water Services to conduct a hydrogeology of the north Hualalai Volcano. In addition, Palamanui had requested a study for their land use appli- cation. A portion of the hydrologic budget within the KAS north sector ( units 5, 9, 10, 12, 13, 14, 15 and 16) from that study (see map) is presented is presented below. It was estimated from that study that the high level aquifer compartments receive recharge of about 10.7 mgd and the thin basal lens receives about 11.7 mgd. There is no direct runoff to the sea and the evapotranspiration is accounted for prior to estimating recharge. Average Recharge With Fop �.� Zone Recharge (Mgallyear) (MGO) a2 1 173 .474 2 770 2109 LAND a 3 248 .678 OF KAU " -� �,,, 4 1316 3.608 ` ): 5 1416 3 880 6 430 1.178 7 1912 6.238 8 28 07 0 26 .071 1 10 815 1.686 11 243 .688 12 255 .599 13 898 2.460 14 2563 7.022 15 1392 3.814 16 2753 7.542 � 1�4a. t �'�c✓r'',''�a , ° TOTAL 41199 ,,M Zone boundary t 0Inchesl boundary = 7 >0 ands 10 Inchestyr >10 and 25 Inchestyr M > 25 mcheetyr Ooma Test well (6) An exploration well (4262- 011V1) was drilled on the land of Ooma, makai of Queen Kaahumanu Highway, to explore the ground -water on that parcel. This well was the first to penetrate deep below sea level Ind led to a major discovery of decreasing temperature with depth with an increase in salinity. SALINITY (PARTS PER THOUSAND) 0 5 10 15 20 25 0 111 21) J 30 F W 40 J so 0 8 ���.. D W Z Z 7 +0 W O 811 93 100 17 18 18 TEMPERATURE (C) Previous thermal infrared studies of near shore ocean water had indicated numerous plumes of spring discharge which were assumed to discharge cold freshwater (W.A. Fischer, et al, HA- 218, 1966). The Ooma data and test results provided an alternative explanation of shallow, cold water discharge of very brackish ground -water springs. Kealakehe Wastewater Treatment Plant & Kona Kai Marina (7) Waimea Water Services was contracted to evaluate the impact of the treated wastewater discharge mauka of Queen Kaahumanu Highway. There had been implications that the wastewater was causing an algae bloom in Honokohau Harbor. Water samples were collected from spring orifice points around the edge of the man -made harbor as well as in the outgoing 7 channel. Samples were also collected from the finished treated water within the WWTP. Summaries of data are contained in appendix 2. Harbor water samples were collected for the purpose of detecting evidence of contaminants from the wastewater discharge pit of the Kealakehe WWTP located adjacent to the County Police Station. There was no conclusive evidence of the injected wastewater found in any of the samples. A water level contour map (below) was prepared in conjunction with the marina proposal which shows the anticipated direction of ground -water flow into Honokohau Harbor. Subsequent studies, using refined analytical techniques, detected evidence of the injected effluent reaching the harbor (Hunt 2008). The original plan for Kealakehe WWTP called for an injection well to be drilled to discharge the treated effluent. Dye had been injected via a test well into the water table and was never seen to discharge. As part of the study mentioned in the following paragraph, it was determined that the dye never left the bore hole. Regardless, the tidal and temperature evidence was well documented and important in under- standing the impact of the highly permeable lavas of the shallow basal aquifer. Kona Kai Ola Marina (KKOM) was proposed as an expansion of Honokohau Harbor. A series of shallow bore holes were drilled along the alignment of expansion and monitored for geology and hydrologic data. The primary purpose was to evaluate changes which might result from developing the marina and to better understand how the local ground -water was responding to tide changes. Tide changes were recorded and sample graphs are included below. J PYJ 1!!Gp F tPq �` uSPJ 76 w,w.awwni...i..wU&M.M., I:SW Jd0 y t� C ■I � NO 1s O'J19 Jwc Honokohau Wells 2 and 2A were constructed to further study the geology and hydrology as part of the KKOM project to provide a basis of water quality responses to change. The wells were built in two distinct vertical sections. An olivine basalt beach sand was struck at a depth of 80 -90 feet which continued to fill the bore. The well was sampled and cased off. A second bore was made adjacent to the i:irst bore. The sand was cased off with the new bore drilled deeper. The results of that sampling are shown below. Conductiv@y m Submeryence EC. (mfficm) 0 5 10 15 20 15 :4 0 10 20 30 40 pi 50 i E 60 70 80 90 100 35 40 • Well 2A ■ Well = -1 0025`ex 0133x As stated earlier, the evidence of cold water discharge between Keahole and Kaiwi Points accompanied by very high tidal efficiency in well water levels are likely caused by proximity to deep ocean water circulation inland. 10 The ocean bathymetry is shown in the following maps (note the North Kona Slump and Alika Slides). From B.W. Eakins, et, al., 2003, Modified by WWS, 2014 W� Bathymetry from W.W Chadwickjr, et al, 1994. Notes by WWS, 2014 12 ..r Palani Ranch lVell (8) In support of the proposed business park of the Lanihau Corporation mauka of Honokohau Harbor, a major well was built (well #4158 -03) in the uplands of Palani Ranch. The well is being placed into service with the Department of Water Supply. The water level was found to stand at about 95 feet above sea level and penetrated a high -level compartment of the KAS. Ground -water under pressure entered the uncased well bore at a depth of about 1438 feet. 13 0.0 1Q z0 34 4.0 BA 0.0 710 POW Ranch Well Dnrwdoiwn DRta 10!9611007 lam (Mt7) t 10 too 1.000 t0,o00 100,000 Sustained pumping rate of I I23gpni throughout test A long term pump test indicated that a discharge boundary was struck after 360 minutes and drawdown was calculated to sustain the pumping yield of 1,200 gallons per minute for 16 hours per day. hohanaiki (The Shores at Kohaniki) (9) The Kohanaiki resort is located just north of the Kaloko - Honokohau National Historical Park complex. Waimea Water Services was contracted to design, build and operate a water source for the purpose of providing brackish water irrigation to the project. The ground -water study was based on two existing water sampling wells and a number of anchialine ponds. Time of day water level measurements were made to observe ground -water flow direction. 14 ..riat Groundwater Flow at High Tide (7:30 Ahl, 1/9/07) Groundwater Flow at Low Tide (2:00 PM, 1/9/07) Construction water supply consisted of water furnished from an onsite brackish well for dust control and freshwater imported from the DWS potable system. Based on the initial supply, the gradient of the water table, water quality from the observation wells, and proposed irrigation water demand, WWS derived a hydrologic cycle projection for planning purposes. RD CONCENTRATE 485 GPM 21,051 mq /1 I @4 _E'LAMI 1kEi.l._11►A 1,525 GPM 7.74 mg /I COUNTY WATER 208 GPM 600 mg/I A IRRIGATION WATER 1,248 GPM 1,142 mq/I RD PRODUCT 1,040 GPM 1,250 mq/I PROJECT SCHEMATIC PROJECTED WATER QUANTITIES AND OUAUTIES 15 EVAPOTRANSPIRATED WATER 570 GPM 0 mg /I INFILTRATED WATER 678 GPM 2.102 mg A Based on the information from the Ooma test well and recognizing the very thin brackish lens (10' +/- in thickness), a well field and reverse osmosis desalting plant were constructed to develop and deliver a finished brackish water source of 1.5 mgd capacity. Brackish source wells were all built and cased to about elevation -10' to -12'. Well capacity was controlled to produce at a rate of about 200 gallons per minute (gpm). Well spacing was designed at about 400 feet between wells to prevent undue stress on the basal lens and to provide extra well capacity to allow some rest periods should there be signs of salt water encroachment. In order to meet requests from the Kaloko - Honokohau National Historic Park (KHNHP) and to provide for careful management of the ground -water resources, in addition to eight supply wells, eight additional observation wells were built. All of the wells and sample sites have been sampled for water quality since pumping began in 2008. Well Locations at Kohanaiki 16 16,000 14,000 13,000 12,000 11,000 10.000 3 9,000 a E 2 iF]0 Text a wo 5.&3a 4,000 3,000 2,000 1,000 0 11/1&2008 C m J 1 t _1 Monitoring Well chlorides Data a Production Well Pumpage 4/2/2010 811512011 1212712012 Kohanaiki Monitoring Wells Water Level Data 2010 -2011 4,600,000 4,200.000 3,900,000 3.600.000 3.300,000 3.000.000 2700.000 9 d 3,400:= 21C0,0002 6 1,500.000 1 fi00m 1,200,000 900,000 600,000 300,000 0 5111/2014 Graphs of the pumpage, tides and salinity data 17 The salt concentrate discharge from the RO plant is injected by gravity at a rate of about 450 gallons per minute (gpm) to about elevation -100 feet via a specially designed well. To determine the potential impacts of the well field pumping and the injection well, sampling is performed monthly at the following wells: • Monitoring Well 300A (4162 -005) • Monitoring Well 300B (4162 -006) • Monitoring Well 300C (4162 -007) • Monitoring Well 400 (4162 -004) • Deep Monitoring Well 401 (4161 -011) • Monitoring Well 402 (4161 -012) • Monitoring Well 201 (4161 -010) • Monitoring Well 200 (4262 -003) A deep monitor well was constructed to elevation -114 feet to observe any changes within the basal lens which might be influence by the pumping or the injection of concentrate. The data from this well is summarized in the graphs below. S Or Kohenaiki MW 4012013 Travem Data COMUmrq IfflVbe{ 10 13 20 25 30 33 40 �llgi M, . xprriew no -Onmr - .- NnaiMa - -Oarmr —.k*w so A M M �00 Kohe"ki MW 4012013 Tram" Defy • rr�ur7 -r ►tech • Jwu +wyr . vS�01MiWr -OrLlo - �.+NMMOr � - 11�NICANOr TLI00 M The top 10' of the basal lens will is sensitive to the application of water applied on the land surface within the resort area. A freshening of the lens may occur when water of lower salinity is applied in over - irrigation. It is noted that MW400 of the observation wells (4162 -004) detected fresh water leaking from a faulty valve. 18 Keopu - Doutor Coffee (10) The well bore for the Keopu project penetrated stream gravels at a depth of 960'. Subsequently, the gravels were determined by David Clague of Hawaii Volcano Observatory to consist of weathered trachyte from Hualalai volcano. The final water level was found to stand at elevation +47 feet. Located at elevation 1445 feet, just makai of Mamalahoa Highway, the Doutor Coffee well also taps high -level groundwater standing at +43' near the Keopu project. Boundary of Northern and Southern Sectors of the Keauhou Aquifer System Wells 3957 -01 and 3957 -05 mark the approximate location WWS has used to demark the approximated boundary of the extreme Hualalai trachyte lava influence on the high —level portion of KAS and the likely boundary of the Alika slides of Mauna Loa. This is not conclusive but is used to better describe some of the reasons for increasing water levels evidenced during well construction during drilling along with actual recovery of trachyte cuttings. It is a convenient point of separation between the northern and southern sectors of KAS. Kahaluu Wells, Shaft and Golf Cgurse Wells (11) Waimea Water Services has conducted a variety of studies in this complex. Efforts were been made to improve the water quality by back filling of the golf course brackish wells in addition to photographic investigations of Kahaluu wells. The high volume of ground -water flow, with a low basal head of about 4' to 5' above mean sea level, has led to a concentration of development for potable water. This pumping concentration has resulted in a dynamic increase in salinity. As shaft pumpage was reduced, the salinity in the produced water has improved. Exploration well 3657 -02, while located significantly inland and north from the producing wells, was found to be slightly brackish with a chloride salinity 400 milligrams per liter. There has been no explanation for such a salinity as the well is located inland of the producing wells. Evidence from this well may imply that the influence of the high level confining geologic structures created locally reduced flows in the basal lens. KSBE Well Field (4) As mentioned earlier, the KSBFi well field is located at the site of the first discovery of the high level ground -water aquifers in the Keauhou Aquifer system. In addition to the initial work by WWS, Tom Nance has conducted a number of well field studies. As of this date there has been no conclusive evidence as to the geologic impediments creating the high level aquifers. S.P. Bowles speculates that the cause is most likely the influence of faulting as well as the confinement of the trachyte lavas as found primarily in the north sector and, particularly where lavas have flowed over fault scarps. 19 Major coastal land slumpage has been discovered, namely, Alika 1 and Alika 2 slides and the North Kona Slump. From B.W. Eakins,et al.,2003 From W.W. Chadwick,Jr, et al., 1994 HA WA/l Alika-1 U South�"i' 1 Kone�10 %,/ i 1 13 �''•` `': •�KaLae -W� :'��'; ► r� t From B.W. Eakins,et al.,2003 From W.W. Chadwick,Jr, et al., 1994 HA WA/l pclot�: 1 + 200 is Faull 1pab 15 i Hilin 7 Loihi 4 •KaLae -E _.- __11 From J.G. Moore, et al, 1989, Notes by WWS 2014 A major fault, located inland of Kealakekua Bay, has been covered by younger lavas from Mauna Loa. Well 2753 -03, located mauka of the fault scarp, taps high level ground- water. En echelon faulting, similar to the land surface west of Kilauea volcano, may also occur along the coast line to the north of Kealakekua Bay all the way to Kaloko. 20 Alika-1 U South�"i' Kone�10 %,/ i 13 �''•` `': •�KaLae -W� :'��'; pclot�: 1 + 200 is Faull 1pab 15 i Hilin 7 Loihi 4 •KaLae -E _.- __11 From J.G. Moore, et al, 1989, Notes by WWS 2014 A major fault, located inland of Kealakekua Bay, has been covered by younger lavas from Mauna Loa. Well 2753 -03, located mauka of the fault scarp, taps high level ground- water. En echelon faulting, similar to the land surface west of Kilauea volcano, may also occur along the coast line to the north of Kealakekua Bay all the way to Kaloko. 20 Aquifer System South Boundary !see maps) It appears that the south boundary of the KAS is arbitrary. There does not seem to be any outstanding hydro - geologic reason for the boundary line. Wells 3255 -01 and 3255 -02 are drilled into the high level aquifers with water levels exceeding 400 feet above sea level near the boundary line but there is no significant change in the subsurface geology, such as a mauka -makai rift zone to demark a boundary. Hokulia- Halekii Well Complex (12) Although these projects are located outside the KAS, they are important in defining the boundary between the high -level and basal aquifers. Irrigation wells, 3056 -01 and 3156 -01 have basal water levels 1.3' and 4.0' respectively. Well 3155 -03, located about 2300 feet inland, or mauka, has a water level of +51' and produces fresh water (chlorides of 15 mg/1). The boundary between high -level and basal lens lies between these wells and appears to be the result of younger lavas flowing over a fault scarp which probably acts as an aquitard. The DWS Halekii well (3155 -02) , the Kalukalu well and the upper wells of Hokukano Ranch are all located in high level aquifer compartments with the maximum water level in well 3153- 02 exceeding 1300' above sea level. Findings Our work, covering 40 years of investigation, has led us to create the findings listed in the first four items below. 1. The Keauhou Aquifer System consists of four basic units: a. North sector - high level and basal b. South sector - high level and basal 2. Likely causes of high levee' ground -water occurrence: a. Fault scarps cover ?d by younger lavas b. Trachyte lava flows c. Combinations of a and b 3. Multiple water levels in the high level aquifer region of KAS indicate a complex of aquifer compartments. 4. Cold water shoreline basal springs between Keahole Point and Kaiwi Point result from: a. Deep ocean temperature intrusion b. Highly permeable :shallow lavas c. Tide fluctuations aid their efficiency 21 The bullet points listed below best describe the present operating status of the KAS. • The management programs of well spacing and pumping at the Huehue Ranch and Kohanaiki well fields have had no significant direct impact on the basal lens quality at the shoreline. • The high level well pumping has had no direct impact on the basal lens in the north sector to date. • Over pumping of the Kahaluu shaft and the Kahaluu wells in the south sector has resulted in dynamic salt water encroachment which is reversible when pumping is reduced. • Water development in the north sector does not impact the south sector ground -water flow or quality. Efforts to provide a model simulation of the entire KAS are futile. • The specific migration of high level ground -water flow to the ocean is not yet defined. Evidence from the Kamakana Bore (well 3959 -01) and from well 3858 -01, (thick, dense lavas, combined with artesian flow) provides some explanation (see Tom Nance presentation). Similar evidence is also found in the Huehue wells and in wells on the north slope of Hualalai. • The high level ground -water system is complex with various water levels and has numerous compartments. Large quantities of high level ground -water in the south sector remain undeveloped. • Sustainable yield assumptions based upon only a basal lens inaccurately describe the complexity of ground -water occurrence in the Keauhou Aquifer System. The recharge estimates by the USGS (J.A. Engott 2013) further reduce the present accuracy of' sustainable yield estimates. The actual sustainable yield most probably lies between the two estimates. • It is important to note that all pumped water is either discharged to the atmosphere by • evapo - transpiration; • infiltration from irrigation; or • shallow disposal of'storm water and wastewater. There is no discharge or runoff directly to sea in the north sector. Some extreme storm runoff does occur in the south sector. 22 Selected References • Bauer, G. R., 2003, A Study c f the Ground -Water Conditions in North and South Kohala Districts, Island of Hawaii, 1991-2002., DLNR -WRRC, PR - 2003 -01. • Bowles, S.P., and Mink, LA., 1980, proposed Prototype Testing Program, land Disposal by Injection Wells of Ocean Water Effluent at Seacoast Test Facility, Keahole Hawaii Island, Manuscript Report. • Eakins, B.W., Robinson, LE, IKamamatsu, T., Naka, J., Smith J.R., Takahashi E., 2003, Bathymetry Image of the Hawaiian Archipelago. USGS. • Engott, J.A., 2013, A Water - Budget Model and Assessment for the Island of Hawaii. U.S. Geological Survey Scientific (Investigations Report 2011 -5078. • Fischer, W.A., Davis, D.A., Sousa, T. M., Fresh —Water Springs of Hawaii from Infrared Images, USGS Hydrologic Investigations, Atlas HA 218. • Hunt, C., 2008, Result of Sampling of Wastewater Tracers At and Near Kealakehe WWTP, Kona, Hawaii, March 13, 2008, USGS /DOH Cooperative Program. • R.M. Towill Corportion, 1989, Keahole to Kailua Development Plan- Executive Summary Draft. Planning Department, County of Hawaii. • Stearns, H.T and MacDonald, G.A, 1942, Geology and Ground -Water Resources of Hawaii, Bulletin 9, Hawaii Division of Hydrography. • Waimea Water Services, 1996, Final Progress (March1996) Report on Effluent Discharge, Reuse and Quality, Manuscript Report, Public Works Department, County of Hawaii. Appendix 1: Huehue Well Field 1. Map of HR Wells 1 -5 2. HR Wells 1 -5 Water Chemistry Table 3. HR Wells Stress Test Report 4656 -01, Katipuleht 4657 -0,, KaupulefrLT 3 } - 4656 -02, 4aupulehi td "*' , 465&0;1, Kaupulehu 1, 4657 -03, Kaupuleht M,2_ K4658 -02 Kaupul F ? , eu ulefit e a r. — 4v$8 -02, uehue-Raocii �f4363.1,7to -19, Mera,11 P , , > _ eR c 1. 4363 -01 to -12, Lhvajima F(shenes ._.. *� : u u � _ - e a 44.63 01 to -03, DOT Keahole;i14' 1M�'.' Jot { 59 =01, Huehus Ranch 1 4463 -05 to - 07,.Nortsint " 59- Huehue RancFi,i( "63-.04, C rarao#ech -c ustTcontrol s 4 =467- 06,. -07, DOT MW13 „ '° "� 4�d- 9i�l�t ue Ranch 2 4462 =02, DOT Keatiorle -- , t - d !• • M"_'► � , 4�' _ =_ "f ti p.w . - ,° . a .,'„ - -- - .wX4. 44_ .55 8 8=,0421, Nansay P K a iki t` 446 -1 -61 Cooper ; DWS - Kahanaiki o �x °�- 461 -02, HELCO Keahole _> � - - t X4462 =05, DOT MWJ1 ' 616 fi, ao ' ti •.. i ' otech net i'a"s4363 -13,C a ;-- 4358 -01, DWS Kalaoa A 4 3 -140 , 4.6Aona -Blue 1.0_ w f. I ,�. -..: .. a- 4262 =04�to -06 Moana N 9"' - 1. `'` - 11 ' ° Kukio Resort - RO Plant at elevation 620 ft Summary of Water Quality Data provided by IUS Parameter units well well well July, 2003 well 4 well 5 "Ve"E& As m /L <0.002 <0.002 <0.002 - - - Ba m /L <0.03 <0.1 <0.1 - - - Cd m /L <0.002 <0.005 <0.005 - - - Cr m /L <0.01 <0.01 <0.01 <0.01 - - Pb m /L <0.02 0.030 0.030 - - - Hg m /L <0.0001 <0.0001 <0.0001 - - - Se m /L <0.002 <0.002 <0.002 - - - Ag mg /L <0.005 <0.01 <0.01 - - - F m /L 0.920 0.720 0.690 2.560 - Nitrate N m /L 0.780 1.470 1.400 0.850 1.070 - Turb NTU 0.300 5.800 1.500 - 2.010 - Mn m /L 0.020 0.050 0.040 - - Fe m /L 0.030 0.600 0.130 - - Na m /L 57.950 8.880 59.100 - - K m /L 12.170 12.400 6.740 27.500 - Ca m /L 21.54n ?6.?0n 7.600 - M g m /L 79.300 74.900 76.500 - - CI m /L 112.000 150.000 14.000 - - Sulfates m /L 95.000 53.800 266.000 - - sulfides mg /L 0.040 0.050 0.200 - - TDS m /L 791.000 835.000 840.000 754.000 - pH pH units 8.030 8.000 8.100 8.400 - Alk m /L CaCO3 395.000 359.000 318.000 423.000 - Hard m /L CaC04 401.000 385.000 334.000 466.000 - silica rn /L 1 90.300 1 64.000 84.000 - condu 1 1220 1 967 1300 - Huchue Ranch Well Field Aquifer Stress Tests November/December 2006 Prepared By: wa)meo waterrfervicef in( P O Box 326, Kamuela, HI 96743 Phone (808) 885 -5941 Fax (808) 885 -7851 e-mail waiono ®wws- ius.com February 2007 Summary Conclusions The water quality (as measured by specific conductance, EC) of each well remained stable for each of the testing sequences. Although there were some trends of freshening showing in HR3, this data was found to be inaccurate when compared with the operator spot sampling taken (see Appendix A). The test sequences of IM -11114, utilizing only the basal lens (HR 5 on standby), demonstrated the stability of water quality at production levels of 1.96 mgd and 2.3 mgd. Furthermore, water quality has generally remained constant in each well since pumping began in the early 1990's. The recent stress testing simply confirms this long -term observation. It is reasonable to conclude that the HR well field is capable of sustaining a pumping rate of 2.5 mgd from the basal lens. This increase in the sustainable pumpage estimate from 1.96 to 2.5 mgd will be adequate to meet the needs of Kukio Resorts, as planned, including the additional demand of Maniniowale. Regardless, water conservation is needed to maintain adequacy. Some improvement in instrumentation on HR3 is needed to insure accuracy of the records for long -term data collection. The SCADA system EC reporting should be confirmed with direct sampling periodically. Background The Huehue Ranch began its determination of groundwater resources in 1981, with a preliminary study by Island Resources. This survey was used to determine the location and feasibility of deep drilling to develop water in support of a 183 -lot subdivision on mauka Huehue land. An exploration well (HR1) was constructed at elevation 1565' in 1984 -85. Initially, the well had a relatively low yield (150 gallons per minute) and produced a poor quality of water (765 milligrams per liter dissolved solids). This result indicated that a treatment plant would be needed to consider HRl as a potable source. However, this venture proved the feasibility of developing basal groundwater as a supply for the proposed development. Based upon this success, Huehue Ranch determined that it was also possible to develop its makai land near the shore at Kukio. In 1986, plans were made for a resort development at Kukio, assisted by water resource studies indicating brackish water could be developed to supply golf course irrigation. Water demands for the mauka and makai projects were estimated at 1.52 mgd (million gallons daily) for brackish irrigation and 1.96 mgd for the combined potable supply. In 1988, HR1 was successfully deepened to increase its yield to 350 gpm. Following this improvement, the properties wE .-re sold, leading to a planned expansion of the HR well field beginning with HR2. Meanwhile, brackish water was developed makai via the construction of the KI wells 1 -3 in 1990 and 1991. Upon completion of HR5, the properties were split, with the mauka land acquired by Makalei and the makai portion bought by Kukio Resorts, LLC. However, the financial collapse of Makalei's owner led to limited use of the HR well field, solely supplying a remaining golf course. With the eventual purchase of the HR well field by Kukio Resorts, LLC., plans were laid to install a connecting pipeline down the mountain. The pipeline was to link the HR wells to a treatment plant providing potable water to the Kukio Resort. This strategy was formed to meet increased water demand, following the addition of the Maniniowale lands, which introduced a need above original potable estimate. Recently, an additional potable supply of 0.5 mgd is needed. Kukio Resorts, LLC has continued to explore supply options to supply this increased demand. Kukio has debated the use of the concentrate reject water from the treatment plant to stretch the brackish irrigation supply. Increased pumping capacity of each HR well has been taken into serious consideration. It has long been established that wells HR1 -4 tap the basal lens, where fresh water floats on underlying salt water. This raises questions regarding the aquifer's long -term sustainable yield and its ability to maintain the quality of water produced from the basal lens. HR5's capabilities are considered individually, as it makes use of a separate resource, isolated from the salt water. It obtains water from within the rift zone of Hualalai volcano, where water is confined in dike compartments. Regardless, the quality of each HR well has been altered by the hydrothermal activity within Hualalai, thus creating a necessity for softening to produce high quality drinking water. In order to insure a long term adequacy of water supply, Kukio Resorts, LLC, decided to conduct a test of the HR well field under several different pumping combinations to explore the sensitivity of the basal aquifer to pumping stress. Stress Testing: Basal and High Level Aquifers The HR wells are spaced along a contour elevation of between 1550' and 1600' as shown in Figure 1. The wells HR2 -HR5 have a nominal installed pump capacity of 570 gpm, each with slight differences in actual rate. These variances depend on depth of setting, pump condition, et cetera. Well HRl has a nominal 350 gpm capacity due to a smaller diameter casing. An initial round of stress testing involved HRI -HR4, to study the response of the basal aquifer. HR5, being in a dike - confined unit, was excluded. The basal wells were pumped concurrently for 16 hours each day, over a five -day period. A second round of testing included the same wells, for an increased pump period (20 hours per day). This test was carried out to further stress the basal aquifer and to observe any degradation in water quality. A final round of testing included wells HR 1, 3, 4 and 5, each pumped for 20 hours per day for five days. HR2, being the southern most well, is closest to a nearby well on the lands of Kau. It was excluded to remove possible the influence by neighboring pumpage. This third test was performed not only to show an increase in the total yield by sustained pumping, but also to observe whether HR5 had a negative influence on nearby HR3. The tests were monitored continuously for flow rate (GPM) and water quality as measured by specific conductance (EC) instrumentation. This monitoring was performed remotely via the newly completed SCADA (supervisory control and data acquisition) system. In addition, to insure accuracy of the recorded quality data, each well was checked via handheld conductivity instruments. It is noted that the starting EC SCADA value for each test shows a lag in excess of 150 minutes, before reaching a quality similar to the handheld instrument. This appears to be a consequence of the instrument installation, possibly due to air entrainment or temperature. This spurious lag has been ignored in the interpretation of results. The testing was performed with a combination of wells for 16 and 20 hour days to simulate productions of 1.96 mgd and 2.36 mgd respectively. These numbers were not quite achieved to due slight differences in pump capacities. Also, the 16 -hour test was intended to run 5 days, but was cut short due to an electric company power failure. Figure 1. Well Layout for Is:ukio Potable System Round 1: 16 -hour test The following figures display water quality for each well over the 5 -day test period. The first graph shows the EC (conductance) in micro- mhos /cm (aka micro - siemens) by test day. The second graph shows pumping days superimposed in order to identify any changes in quality for the test period. The salinity of each well is expressed as total dissolved solids in mg /L and is calculated as 50% of the EC reading. Since the main purpose of the stress test was to identify any increases, the readings are not converted. Data graphs are presented in order, from the southern to northern most basal wells. List of Subsequent Figures HR2 — Figures 2 & 3 As can be seen, there were no identifiable increases in salinity after 200 minutes of pumping for the duration of the test. HR4 — Figures 4 & 5 Although the results show a baseline change in quality, the salinity reaches a steady value after 200 minutes. HRl — Figures 6 & 7 Here again, a baseline shift in quality is observed, with no real change after 200 minutes of pumping. HR3 — Figures 8 & 9 Well water shows a progressive improvement and was the freshest well from the beginning. The data shows a 20 percent improvement in quality during the 5 -day test. However, this result is believed to be an artifact of the SCADA instrumentation, as it contradicts the handheld operational data. HR 2 Pump Test. 16 hrlday 1400 1200 E 1000 u Rat) 3 >t S ban u 400 200 ._-___ 9?�G, 1137 1' 1112 AVG. 1141 AVG. 1139 AVG. 1119 , 1122 1111: 1 103 1108 1068 • 0 — AMENOW . -.. -------- � 11/20/06 11/21106 11.22)06 11123/06 Date Figure 2. HR2 Conductivity vs. Pumping Day 1200 1150 _ 1100 1050 0 1000 950 900 850 800 0 200 400 600 Time (Minutes) Figure 3. HR2 Conductivity vs. Pumping Time 1 U24106 11/25/06 11/26106 HR 2 Pump Test, 16 hrlday • SCADA I■ Mer I 800 1000 1200 * Day t' a Day 2 3' 4 X 5 E HR 4 Pump Test, 16 hr /day 1600 1400 1200 E v 1000 800 600 400 200 0 1329 .._1356_.__.�1353 ,._.13571355._..1358. _.,..1370 1357 _.1345 t AVG. 1310 AV, 1309 = AVG. 1311 AVG. 1313 = AVG 1307 • • 11/20/06 1 1121 /06 11722!06 1 1 /23106 11/24/06 11/25M6 1 1126/06 Dab Figure 4. HR4 Conductivity vs. Pumping Day 1350 F 1300 0 1250 1200 1150 HR 4 Pump Test, IS hr /day 1100 0 Time (Minutes) Figure 5. HR4 Conductivity vs. Pumping Time 800 1000 • SCADA ■ Manual • Day 1 j �. Day 2 Day 3 Day 4 z Day 5 1800 1600 1400 1200 1000 800 600 Ul 400 200 0 HR I Pump Test, 16 hr/day • 1482 1463 1495 --1530--1498 1488 • • AVG. 1449 AVG. 1429 ------- Zll!ll. 1425 1, =1111r 1-41206 11/20106 11121/06 1122/06 11/23M6 11/24106 11125/06 11/26106 Date Figure 6. HR1 Conductivity vs. Pumping Day 1500 1450 1400 1350 1300 1250 1200 1150 1100 HR I Pump Test, 16 hr /day • ADA � I • Manuel 0 200 400 600 Boo 1000 1200 Time (Minutes) Figure 7. HRI Conductivity vs. Pumping Time f * Day I 'DaY2 Day 3 Day 4 Day 5 HR 3 Pump Test, 16 hr /day 1200 10RQ E 800 600 {? 400 03 200 ''M 2 9542_m..._,.,�__..�_. 973 3 978B_____ -9594 9499 9643 9759._.. _ 982.8 • AVG. 953 • n a 1,959 o qVG. 914 u o a i AVG. 903 AVG. 892 AVG. 855 2 • 0 11120106 11121106 11/22/06 11123/06 11/24/06 1 112 5/06 1 1126106 Date Figure 8. HR3 Conductivity vs. Pumping Day HR 3 Pump Test, 16 hr /day 1000 950 900 850 800 750 • SCADAI Iis Manuel I 700 -- 0 200 400 600 Time (Minutes) Figure 9. HR3 Conductivity vs. Pumping Time 800 1000 1200 • Day 1 • Day 2 il W Day 4 j x Day 51 Round 2: 20 -hour test For the first round of testing, the quality performed under stress with remarkable stability. In response, a second test was performed adding 4 hours daily to the testing period. This 20 -hour test was designed to again explore the sensitivity of the basal lens, operating the same wells for an extended period. The results are presented in the same fashion as above. List of Subsequent Figures HR2 — Figures 10 & 11 Stable water quality was observed from this well for the duration of this round. HR4 — Figures 12 & 13 An especially large lag time was observed, and attributed to the SCADA instrumentation. However, the operator data showed stable water quality for this round of testing. HR1 — Figures 14 & 15 Water quality in the well appeared to decrease very slightly. HR3 — Figures 16 & 17 Data collected from the SCADA system again shows freshening of the well water. This again is in contradiction to the handheld data, which showed a minute increase in water conductivity. The operator data is much more credible and is used in the final interpretation of results. HR 2 Pump Test, 20 hr /day 1400 ..... _.... i A VG. 1130 AVG.1134 AVG.1129 AVG 1130 AVG 1133 1200 �� � ♦ • 1095 1099 # 19 I • 1119 1092 1082 1097 1090 1099 1110 1108 1000 E • i 800 ! a f • SCADA o %• Manual m 600 --- ------ ._ u W 400 ♦ ._....... _.._. _.._.______._____._.._.._._._., _.._.._.w..m_..._ 'K I 0 ♦ I 11/25/2006 11126/2006 11/27/2006 11/21112006 1129/2006 11 /30/2006 12J112006 Date Figure 10. HM Conductivity vs. Pumping Day HR 2 Pump Test, 20 hr /day 1200 1150 1100 E u 1050 0 z f 1000 U A u 950 .2 w 900 850 800 0 200 400 600 Boo Time (Min) Figure 11. HR2 Conductivity vs. Pumping Time 1000 1200 1400 • Day 1 ■ Day 2 Day 3 Day 4 X Day 5 ts00 1400 1200 E u 0 loon 0 L a v 800 V 4 600 w 400 200 0 11/2512006 1126/2006 11x712006 11/28/2006 11/29/2006 11/30/2006 Data Figure 12. HR4 Conductivity vs. Pumping Day HR 4 Pump Test, 20 hrlday HR 4 Pump Test, 20 hrlday 1340 1320 1300 E u 2 1260 U 1260 W 1240 1220 12/12006 1200 - 0 200 400 600 800 Time (Min) Figure 13. HR4 Conductivity vs. Pumping Time 1000 1200 1400 ♦SCADA ■ Manual Day 1' �aDay2 Day 3 Day 4 x Day 5 1800 i 1600 1400 - -� E 1200 u m 0 z 1000 —. - -- C a 0 U 800 -- urR A 600 400 — 200 0 t. 11/25/2006 11/26/2006 11127!2006 11/28/2006 11/29/2006 11/30/2006 12/1/2008 Date Figure 14. HR1 Conductivity vs. Pumping Day HR 1 Pump Test, 20 hr /day 1500 1400 1300 E u 1200 d v 1100 S V 1000 W 900 800 700 0 200 400 600 800 Time (Min) Figure 15. HRl Conductivity vs. Pumping Time HR 1 Pump Test, 20 hr /day 1000 1200 1400 ♦ SCADA ■ Manuel Day 1 a Day 2: Day 3 Day 4 !tDay5 X1.1 1000 E 800 L f 600 U uCA A m w 400 2CO HR 3 Pump Test, 20 hrfday 1112512006 1126!2006 11/21/2006 11126!2006 11!29/2006 11130/2006 Data Figure 16. HR3 Conductivity vs. Pumping Day HR 3 Pump Test, 20 hrfday 850 800 E 750 U 3 700 2 h M650 .11 550 0 200 400 600 800 Time (Min) Figure 17. HR3 Conductivity vs. Pumping Time 12/12006 1000 1200 1400 • SCADA w Manuel, L♦Day1? 0 Day 2j Day 31 Day 4' x Day 5 n960 9 9703= r, 96511 - 9714 . 7 "1 971'. 968 1 a 970 7 97081 :7 971 2 10001 .�� ��VG ♦ 744 AVG. 745 AVG 742 AVG. 752 • ♦ 1112512006 1126!2006 11/21/2006 11126!2006 11!29/2006 11130/2006 Data Figure 16. HR3 Conductivity vs. Pumping Day HR 3 Pump Test, 20 hrfday 850 800 E 750 U 3 700 2 h M650 .11 550 0 200 400 600 800 Time (Min) Figure 17. HR3 Conductivity vs. Pumping Time 12/12006 1000 1200 1400 • SCADA w Manuel, L♦Day1? 0 Day 2j Day 31 Day 4' x Day 5 Round 3: 20 -hour test (Part 2) For the final round of testing, HR5 was included. Here, the basal lens would continue to be tested, while further demonstrating the impact of pumping on water level of the HR5 compartment. These results were then compared to the performance of the water level in a basal well. The sequence again started with the southern most well, with HR2 now in standby mode. Note, under the standards of operation set forth by the state Department of Health, the reliable potable supply must be provided with the largest pumping unit on standby. In this case, any of the HR wells except HRI can be considered as a standby unit. Here again the test results are presented, first sequentially and then superimposed. List of Subsequent Figures HR4 — Figures 18 & 19 As seen with the 16 -hour tests, the quality was stable after 200 minutes for each day of the test. HRI — Figures 20 & 21 HRI, both the deepest well and the lowest pumping capacity, remained stable for the test period. It repeated its performance from the first round, with an EC of slightly more than 1500 micro -mhos JDS of 750 mg /L). HR3 — Figures 22 & 23 HR3 continued to improve in quality, according to the SCADA system, despite the increased pumping period. Here again, the operator checks independent of the SCADA monitor showed no improvement in quality. HR5 — Figures 24 & 25 HR5 has always produced some of the poorest quality, just slightly above that of HRI. The quality of the water produced remained stable, as expected, with poor quality related to the influence of the Hualalai rift zone. E 43 U LU W HR 4 Pump Test, 20 hriday 400 i -- ..._ ._.._ ..........._._� 1350 1330 ..........._ ®..134T -- ..._... 1345_.._.._.... 1350 --- ._..1349._....._._1352..,._. 1349 ...... p • q q � 200 AVG. 1305 AVG 1298 AVG 1302 AVG�130 -..._— ._.._ i 000 800 - _.__.......�.�.. �. ...__._.m___ »...._._.._._.,__ ._._....._..,.._......`�"--- 600 _ • • 400 2w 0 ----- -tea - —�-- 11130106 1211/06 1212M 12/3/06 12/4/06 1215/06 Data Figure 18. HR4 Conductivity vs. Pumping Day 1340 1320 1300 1280 1260 w 1240 1220 1200 0 200 400 600 800 Time (Min) Figure 19. HR4 Conductivity vs. Pumping Time HR 4 Pump Test, 20 hr /day 10w 1200 1400 • SCADA • Manual 1 • Day 1 IN Day 2 Day 3 j Day 4 j T LU LU HR 1 Pump Test, 20 hr/day fi00 1— 1514-1510- 1515 1512 1519 y523- 1' OMMIllkill, INWWWO '1111111" w 400 VG 1 96 TkVG 1502 AVG 1505 AVG 465 77-- 7-- 1----V 200 000 BOO 500 400 200 0 11/30/08 12/1106 12M06 1213106 Date Figure 20. HR1 Conductivity vs. Pumping Day '55" 1 1500 1450 1400 1350 1300 1250 LLI 1200 1150 1100 1050 HR 1 Pump Test, 20 hr/day 1214106 12/5106 Time (Min) Figure 21. HR1 Conductivity vs. Pumping Time SCADA ■ ManIj 68Y I wDay2 Day 3 Day 4 HR 3 Pump Test, 20 hrlday 1200 t000 ■ 970 965.4 m It 971.4 964.9w • 9729972 6E 0974,5 974 E800 .. _ ___....__.__.___......_...__.._ _ u g 800 D 400 Lu 200 D 11130106 1211/06 1212106 1213106 12/4/06 Date Figure 22. HR3 Conductivity vs. Pumping Day 730 710 690 670 S 650 U y 630 Y w 610 590 570 550 HR 3 Pump Test, 20 hr /day 12/5/06 0 200 400 600 800 1000 1200 1400 Time (Min) Figure 23. HR3 Conductivity vs. Pumping Time • KADA a Manual • Oay 1 • Day 2 Day 3 Day 4 1800 1600 1400 1200 1000 Sao 600 400 200 0 11/30106 HR 5 Pump Test, 20 hr/day 12/1/06 12M06 1213/06 12/4/06 12/5/06 Date Figure 24. HR5 Conductivity vs. Pumping Day 1600 1 1550 1500 1450 1400 1350 HR 5 Pump Test, 20 hr /day 1300 0 200 400 wo 800 1000 Time (Min) Figure 25. HR5 Conductivity vs. Pumping Time 1200 WO 1600 1800 •SCADA a Manual *Day 1 a Day 2 Day 3 Day 4 Water level trends When the mauka (upper) golf course was under construction, the brackish KI wells provided drinking water to the Kukio development. At the time, water for the initial irrigation was being supplied directly from HR5 around the clock, to keep up with the golf course grow -in. In addition to the periodic quality measurements, water level was monitored with a continuous recorder. Initially, the water level stood at +23' above sea level, and the water level records clearly show a dewatering trend. Water levels in the basal HR1 -4 wells range from elevation +5' to + 7', as they fluctuate with time of year and between years. During the 20 -hour test periods, water levels were again measured via the SCADA system. To date, the recorded levels have not been calibrated to the reference datum of mean sea level. Nonetheless, trends are evident. List of Subsequent Figures HR4 — Figures 26 & 27 The water level change: during the test period only reflects actual well drawdown at the start of each day, as the water level recovers immediately to its original level once the pump is stopped. This is typical performance for an unconfined basal lens. HR5 Figures 28 & 29 HR5 water levels behave quite differently as shown by the graphs below. Note that there is a persistent water level drop during each pumping day, and that the level continues to drop with consecutive each day, exhibiting a clear dewatering effect. This drop will continue unless the recharge to the compartment equals the pumpage, or the compartment will resume dewatering. The experience of the cycle run during the golf course start-up period indicates that this compartment could probably run for years without reaching a boundary. Again, HR5 penetrates a separate compartment from the other wells and it is an excellent standby unit for that reason. 314 312 310 308 306 LL m 304 u J e 302 3 300 298 296 294 292 11/30/06 12/1/06 12/2106 12/3/06 12/4/06 12/5/06 1216/08 Date Figure 26. HR4 Water Level vs. Pumping Day HR 4 Pump Test, 20 hrfday 312 310 308 306 304 W m m 302 J 300 298 296 294 292 HR 4 Pump Test, 20 hr /day 0 200 400 800 800 1000 1200 1400 Time (Mln) Figure 27. HR4 Water Level vs. Pumping Time • Day 1 • Day 2 Day 3 Day 4- 300 290 280 270 260 250 LL_ i 240 2 :30 3 220 210 200 190 180 170 '11130/06 12/1/06 12/2/06 12/3/06 1214106 1215/06 12/6106 Date Figure 28. HR5 Water Level vs. Pumping Day HR5 Pump Test, 20 hr /day 210 205 200 195 LL 190 J 165 180 175 170 FR25 Pump Test, 20 hr /day 0 200 400 600 800 1000 1200 1400 1600 1800 Time (Min) Figure 29. HR5 Water Level vs. Pumping Time ♦ Day 1 ■ Day 2� Day 3 Day 4 ADDendix A: Operations Water Ouaiity Data HR #3 Date Time Meter EC Level Handheld EC Handheld TDS GPM Run Hours REMARKS Start 11/25/2006 3:15 m 67058300 0.77 10.2 960.9 668.7 590 20 leak in level line Stop 11/26/2006 10:08am 67715200 0.78 10.2 970.3 673.3 590 Start 11/26/2006 2:57 pm 1 67746800 0.71 10.5 965.9 670.4 590 1 20 leak in level line Stop 11/27/2006 10:30am 68435900 0.741 10.2 971.4 674.3 590 Start 11/27/2006 2:45 pm 68469000 0.69 10.5 971 673.8 590 20 leak in level line Stop 11/28/2006 10:45am 69188500 0.75 10.2 968.1 669.6 590 Start 11/28/2006 2:51 pm 69201600 0.68 10.2 970.7 670.5 590 20 leak in level line Stop 11/29/2006 10:35am 69901100 075 10.3 970.8 673.7 590 Start 11/29/2006 2:49 pm 69907600 0.71 10.3 971.2 673.5 590 20 leak in level line Stop 11/30/2006 10 :00am 70589300 0.75 10.2 1000 695.3 590 Start 11/30/2006 2:49 pm 70648100 0.7 10.4 970 677.4 590 20 leak in level line Stop 12/1/2006 10:00am 71348000 0.69 10.3 965.4 669.7 590 Start 12/1/2006 2:49 pm 71372300 0.68 10.2 971.4 674.9 590 20 leak in level fine Stop 12/2/2006 10:00am 72049200 0.66 10.6 964.9 669.3 590 Start 12/2/2006 2:49 pm 72056400 0.65 10.7 972.9 675.4 590 20 leak in level line Stop 12/3/2006 10:00am 7276220 0.62 10.6 972.6 674.6 590 Start 12/3/2006 2:49 pm 72781200 0.62 10.7 974.5 676.3 590 20 leak in level line Stop 121406 10:00am 1 73465100 0.59 10.6 974.3 1 676.3 1 590 ADDendix A (Cont'd): Onerations Water Ouality Data H R#4 Date Time Meter EC Level Handheld EC Handheld TDS GPM Run Hours REMARKS Start 11/25/2006 3:00 pm 59664500 1.25 296.6 1,361 958.6 595 20 Stop 11/26/2006 10:24 pm 60350500 1.28 291.9 1360 959.9 595 Start 11/26/2006 2.44 pm 60367600 1.25 300 1350 951.2 595 20 Stop 11/27/2006 10:15am 61062900 1.27 232.2 1351 951.4 595 Start 1 11/27/2006 2.29 pm 1 61079500 11.28 301.8 1355 954.9 595 7t1 Qa -� V%V 44 /no /nnnB 11 /LV /LVVV 4n.nn�.r IV.VVC9114 n4 onnOnn VIVVVVVV 4 77 1.11 nn9 7 LJJ.J 4nAO IJ v nAn @ J .V cnc VJV Start 11/28/2006 2.41 pm 61814700 1.24 304.3 1343 948.4 595 20 Stop 11/29/2006 10:47am 62530400 1.28 294 1350 951.6 595 Start 11/29/2006 2.56 pm 62534300 1.28 305.4 1360 958.9 595 20 Stop 11/30/2006 10:20am 63237600 1.28 295.5 1348 949.5 595 Start 11/30/2006 2.34 pm 63273500 1.24 304.3 1350 950.7 595 Stop 12/1/2006 10.00am 63967400 1.28 296.2 1330 937.7 595 Start 1211 /2006 3.00 pm 64001100 1.28 304.3 1347 949.8 595 Stop 12/2/2006 10.37am 64703100 1.28 297 1345 947.5 595 Start 12/2/2006 2.50 pm 64716800 1.29 305 1350 951.8 595 Stop 12/3/2006 10.18am 65414300 1.29 297.8 1349 950.5 595 Start 12/3/2006 2.36am 65432300 1.29 308.3 1352 952.7 595 Stop 12/4/2006 1 10.24am 1 66141000 1.29 298.1 1349 950.5 595 Annendix A (Cont'dl: Operations Water Oualitv Data HR #1 Date Time Meter EC Level Handheld EC Handheld TDS GPM RUN HOURS REMARKS Start 11/25/2006 2:50 pm 85280700 1.28 213 1479 1047 310 20 Stop 11/26/2006 10:17am 85644600 1.48 208.8 1495 1061 310 Start 11/2612006 2:51 pm 85657300 1.371 212.4 1495 1058 310 20 Stop 11/27/2006 10:36am 86021800 1.47 208.5 1500 1063 310 Start 11/27/2006 2:34 pm 86030600 0.75 212.1 1510 1072 310 20 Sto 11/28/2006 10:39am 86412400 1.48 208.9 1519 1080 310 Start 11/28/2006 2:46 pm 86922800 1.19 212.6 1498 1061 310 20 stop 11/29/2006 10.40am 86798800 1.49 208.9 1515 1075 310 -Start 2:40 pm 86803200 1.4 213.1 1512 1070 310 20 Stop 11/30/2006 10:10am 87170400 1.49 208.9 1521 1080 310 Start 11/30/2006 2:40 pm 87193000 1.34 212.2 1508 1070 310 20 Stop 12/1/2006 10:10am 87561600 1.49 208.4 1514 1074 310 Start 121112006 2:40 pm 87574700 1.46 212.2 1510 1070 310 20 Stop 12/2/2006 10:10am 87942700 1.49 208.1 1515 1075 310 Start 12/2/2006 2:40 m 87947300 1.47 211.7 1 1512 1074 310 20 stop 12/3/2006 10:10am 88319400 1.49 208 1519 1079 310 Start 12/3/2006 2:40 m 88333400 1.17 211.3 1523 1082 310 20 Stop 12/4/2006 10:10am 88699900 1.49 208.4 1525 1083 310 Annendix A (Cont'd): Onerations Water Oualitv Data HR #2 Date Time Meter EC Level Handheld EC Handheld TDS GPM RUN HOURS REMARKS Start 11/25/2006 3:15 pm 86565300 0.95 134.2 1095 762.8 560 20 Sto 11/26/2006 10:35am 87217800 1.11 130.6 1099 767.6 560 Start Start 11/26/2006 2:37 pm 87223400 1.13 144.3 1119 779.9 560 20 Stop Stop 11/27/2006 10:22am 87887700 1.13 129.81 1092 1 763.1 1 560 Start 11/27/2006 2:22 pm 87895500 0.91 167.8 1082 1 755 560 In "' l�l�� J�V ••Nln innnn 1 1 /LO /GVVV •n.Ir_� IV.YJdlll nnr -Innn OOJ /YVVV • A 1.1 I •nn • IJV.Y I- IV7/ - I /VJ.V - UVV Start Start 11/28/2006 2:35 pm 88588200 0.85 159.3 1090 757.9 560 20 Stop Stop 11/29/2006 10:47 pm 89273000 1.11 129.9 1099 768.3 560 Start 11/29/2006 2:30am 89277500 1.1 149.91 1110 7773 560 20 Stop 11/30/2006 10:25 m 89944100 1.1 113 0.8 1106 772.7 560 HR #5 Date Time Meter EC Level Handheld EC Handheld TDS GPM Run Hours REMARKS Start 11/30/2006 3.00 pm 257425000 1.33 195.3 1372 965.6 610 20 Stop 12/1/2006 10.50am 258179000 1.42 183.4 1441 1017 610 Start 12/1/2006 2.40 pm 258282000 1.38 195.7 1397 1003 610 Stop 12/2/2006 10.20am 1.42 179.7 1436 1015 610 20 Start 12/2/2006 2.45 pm 259818000 1.41 185.2 1449 1024 610 20 Stop 12/3/2006 10.37am 259837000 1.41 178 1455 1030 610 Start 12/3/2006 2.31 pm 259045000 1.23 189.6 1366 960.2 610 20 Stop 12/4/2006 10.04am 260580000 1.41 177.2 1461 1034 610 Appendix 2: Selected Figures from the 1996 Kealakehe WWTP Report Kealakehe WWTP Effluent Reuse and Management Project FINAL PROGRESS (MARCH 1996) REPORT ON EFFLUENT DISCHARGE, REUSE, AND QUALITY by: Waimea Water Services Inc. March 1996 1 3 1 M 1000 0 1000 2000 3000 4000 5000 6007 7000 FEET I Quar� e _ o x 7 �`�; shporid 1 cr 1 80 � � 'Tank - Honokohau (; Quarry r Bay �� �► - #2 WELL at Quarry ~` Hon okohau,;'—� altu P Int `� #4 OUTLET at Harbor Nona ohau l_ S 1 Boas arbor ' #3 SPRING at Harbor Discharge Point Nat o o KZ E E No t Y WWTP EFFI UFNT - 1 a , I t* - \ A ` Radio Facility \` ,(VORTAC) TS kO tit Fawai� ' y':• Keahuo Pt, ^_ ,' Brfy N b KWWTP EFFLUENT IDENTIFIER MONITOR POINTS FIGURE 17 44 Kealakehe WWTP IMP Averages 10/30/95 to 11/24/95 Phosph. mg /I #4 Harbor 0.08 S a m #3 Spring 0.15 P I e L 0 c a t i #2 Well 0.16 0 n #1 Effluent 4.40 0.00 0.50 1.00 1.50 2.00 2.50 3.00 3.50 4.00 4.50 Units FIGURE 19 IMP PHOSPHOROUS 51 Kealakehe WWTP Averages 10/30195 to 11/24/95 Nitrogen mg /1 #4 Harbor 0.22 s a P#3 Spring 0.83 I e L 0 c a t #2 Well 1.11 I 0 n #1 Effluent 2.20 0.00 0.50 1.00 1.50 2.00 2.50 Units FIGURE 20 IMP NITROGEN 52 #4 Harbor S a m #3 Spring p I e L 0 c a t i #2 Well 0 n #1 Effluent Kealakehe WWTP IMP Averages 10/30/95 to 11/24/95 ■ Ammonia mgt! 0.000 0.020 0.040 0.060 0.080 0.100 0.120 Units FIGURE 21 IMP AMMONIA 0.140 53 Kealakehe WWTP IMP Averages 10/30/95 to 11/24/95 Chlorides mg /I #4 Harbor 17,575 S a m P #3 Spring 6,015 1 e L 0 c a t #2 Well 2,213 1 0 n #1 Effluent 1,087 0 2,000 4,000 6,000 8,000 10,000 12,000 14,000 16,000 18,000 Units FIGURE 22 IMP CHLORIDES 54 FIGURE 23 IMP TEMPERATURE 55 Kealakehe WWTP IMP Averages 10/30/95 to 11/24/95 EC seimens #4 Harbor 52.97 S a P#3 Spring 18.30 1 e L 0 c a t #2 Well 7.18 i 0 n #1 Effluent 4.33 0.00 10.00 20.00 30.00 40.00 50.00 60.00 Units FIGURE 24 IMP EC GRAPH 56 1 -8 1.6 V64 4 A T E R'1 2 L E V E 1 L E Lo 8 E V 10.6 N F E0.4 E T 0.2 0 K -WWTP OB WELL TIDE GRAPHS t013 IVA I, ELEV. FT. --4s-0B NWKAI ELFV Fr I r 1 1 1 1 1 1 i I I 1 I I 1 1 1 1 1 1 I 1 _L_L_L_1_1_1_1_1 _L_ L_ L_ L L L_ L_L_ 1_ 1_ 1_ 1_ 1_ 1 1 I -- T- i- T- T- T- 7- i-7`- 1- i-1-1 -'1 l--r -t - I - -r -� -s -I- -i - '"- r-r -r -�_r r- r-T- T- i -i -l- t I I 1 1 1 1 I 1 1 I I I 1 I r- _�_•_ + -+ - -i -i_y --�-+- - - --+ --' --1--1--1--1--1 -''- -'-� .�_ _�_ '�-`---'+-'-a' I L _ I 1. .1 1 .1 1 1 _ J 1 1 I I 1 1 ! 1 i 1 I 1 r 1 1 I t 1 1 1 I I t 1 1 1 I I 1 1 1 I 1 r 1 I r 1 1 1 1 1 1 1 1 1 I 1 1 I t 1 1 1 1 1 -y- 1 1 1 i 1 1 r I 1 1 1 i 1 I 1 1 I 1 I 1 I 1 I 1 I I 1 I I 1 1 I € I t I I 1 1 I I 1 1 I I t 1 1/3/1996 6 12 18 114/1996 6 12 18 1/5/1996 a 12 18 24 DATUHOLNt ERNE D 1 OIIIlor4mraa - 1 A, Iran �AMpn 0 X71.. -,r 5 KIM" ] 9 5 1 � A71nz l ; Q2?sr, 56�Q,xn � A !•'Ntrr. 6 5 ! 3 1 f . :, IG>n F i ONVI � � bF'rAy�l � F j'� 33 E 9 1 7_ 7 i 1 h � �I 1 wA1Rr A "w liiarlaii l i I H f i i {a.valhae J L4 V Ij K wlrl+efcu8 $,fir 1E 4.7kfi . 4 f -�-1"s 1i� Yil C1 26 c' III 491`. 1 I In •1 LO ,69 I CI, +j�j `4M H aG6 3.1 P 1! am rib L IN 12 '7+ l I:� f16 AM _i flMY9+ 6Z f0 c^3 t +� �t�l 11 97r C.a I4' 1 M14 °vwl �4� H sr� ?y L fii�i�� �� 65 FIGURE 27 M:AUKA & MAKAI OB WELL TIDAL GRAPHS OIIIlor4mraa Plana .._ _ H�iSAd h � �I wA1Rr A "w liiarlaii i {a.valhae J L4 V Ij K wlrl+efcu8 $,fir 1E �' +CI 1- . 4 f -�-1"s 1i� Yil C1 26 c' III 491`. 1 I In •1 LO ,69 I CI, +j�j 65 FIGURE 27 M:AUKA & MAKAI OB WELL TIDAL GRAPHS KEAI.A10 E WWTP - PLANT OPERATIONS DATA AI4 READINGS Pond 06 or in0umt DATE Pond *6 Pond *G Effluent Temp F Nkej kNWent I Eff u m kt k*M ENkKnt ChbrWes CMordes mgm M911 ChkxW O:None mam Mum Phosphates in V. NTU NTU 06 06 IrAwnt Eff unit Flow DIN. C otvk C ' g Foalda galons FoWDagOabn EC C Galons Galons 12- SeP495 13 14 15 16 17 18 19 20 21 22 23 24 25 28 27 28 29 30 84 6.9 2.2 84 61 3.6 84 61 3.4 84 6.9 3.5 83 6.9 3.5 84 6.9 3.1 84 7 1.5 84 7 1.9 83 6.9 2 84 6.9 2.1 84 6.8 13 82 6.9 1.4 82 6.9 1.7 82 7 12 4110 4510 4418 4630 3960 4250 4000 4300 3950 "DO 3725 4300 2886 3400 2890 3930 2850 3910 2950 3440 2900 4080 2970 4430 3300 4500 3850 4450 600 1150 850 1050 750 1150 800 1150 850 1200 800 1150 700 1150 600 1050 650 1100 750 1150 700 1100 600 1050 800 1100 8D0 1200 550 200 400 350 350 350 450 450 450 400 400 450 500 400 0.077 0.115 0.06 0.073 0.946 1.1 -0.154 0.975 1.014 -0.039 0154 0.978 -0.024 0.957 0.805 0.152 _ 1.025 0.776 0249 1.029 0.746 0.283 1.024 0.691 0333 1.028 0.788 0238 1.009 0.744 0265 0.959 0.436 0.523 0.959 DAM 0.103 1.065 0.796 0287 1.077 DAM 0273 1.033 0.814 0219 0.985 0.756 0229 0.983 0.774 _ 0209 0.982 0.768 0.214 _ 1011/1995 2 3 4 82 6,91 1.4 2950 4220 700 1150 450 500 450 450 0.067 0.075 0.074 0.070 1.021 0.7821 0.239 82 6.9i 1.5 2880 4100 600 1100 _ 1.008 0.7871 0.221 82 6.9 1.7 2570 4530 600 1050 1.025 0.4231 0.602 82 6.9 1.6 2610 4320 650 1100 1.07 0.961 0.109 1.086 0.91 0.176 6 T B 500 1.098 0.883 0215 0.077 1.092 0.815 0277 62 6.9 12 2890 4490 600 1100 1.111 0.951 0.16 9 10 82 6.9 1.1 2700 4400 650 1050 400 450 0.085 0.087 1.105: 0.378 0727 81.5 6.9 0.4 2610 4330 _ 600 1050 1.0541 1.134 -0.08 11 81.5 6.9 1.5 2720 4560 650 1100 450 0.086 0.9561 0.928 0.028 12 13 14 15 16 17 82 6.9 1.4 2680 4440 650 1100 450 400 450 460 0.085 0.086 0.079 0.090 0.9761 1.012 -0.034 _ 0.93 0.602 0.328 0.979 0.723 0.256 82 6.9 1.4 2720 4410 700 1100 0.969 0.782 0.207 82 6.9 1.5 2680 4460 _ 650 1100 0.938 0.766 0.172 81 6.9 1_1 2850 4490 650 1050 0.972 0.758 0.214 18 19 21 22 81 6.9 1.4 _ 2650 4450 600 1050 450 450 400 0.110 0.111 0.972! 0.7521 0.22 B1 6.9 1.4 2890 4460 650 1100 0.924! 0.728 0.198 0.961 0.733 0227 0.995! 0.742 0253 81 7 2 2890 4410 700 1100 0.97' 0.743 0227 23 81 6.9 2 2710 4380 650 1080 430 ____0.07_7_ 0 _ 0.959 0.751 02DO 24 81 6.9 2.3 3380 4360 700 1100 400 0.052 0.955 0.749 0206 25 81 7 1.8 2760 4350 600 1100 500 0.106 0.958 0741 0217 26 27 28 29 81 7 2 2120 4410 650 1100 450 450 0.079 0.081 0.953 0.742 0.211 _ 0154 0.743 0211 _ 0.979 0.786 0.193 81 6.9 1.9 2890 4400 650 1100 0.925 0.188 - 30 81 8.9 2 2710 1390 800 1050 - 450 --- __._...___ 0.079 0.895 _0.737 0.728 0.187 31 801 6,91 1.1 27501 4380 700 1150 450 0.095 0.929 0.498 0.431 106 IT"KE HE WWTP - PLANT OPERATIONS DATA AM READ Pond *6 kik" I I I I - --------------- 1 1 0ATK P-4 06 T-p F 7:'. -e 3) C-A..Omwt Itc cm-.t C-A..tb ,�, !tm!t MI.,11; 1.4401 CIZ 4. 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Wan-96 7 1.3 2840 4190 950 1100 460 0109 2 2 76 7 1.1 2460 4240 650 1050 400 0114 0.882 0.98 0.098 3 77 6.99 1.4 2230 3760 600 1050 450 0.148 0.879 0.91 -0.031 4 79 7.01 1.5 2170 3950 500 1050' 550 0.118 0.88 0.888 -0.008 5 77 7 1.5 2130 4160 650 1050 400 0.171 0.847 0.84 0.00 6 77 6.9 1.4 2340 4120 600 1100 500 0.127 0.842 0.838 0.004 7 77 7.9 1.3 2380 4140 600 1050 450 0.119 0.825 0.844 4019 8 77 7 1.1 2400 4200 650 1100 450 0.124 0.76 0.815 0.065 9 77 7 0.9 2400 4220 600 1050 450 0.118 0.8 0196 0.004 10 77 7.01 1.3 2390 4160 600 1050.. 450 0.132 0.773 0.744 0.029 11 77 7.03 0.9 2390 4160 650 1150 500 0.105 0.748 0.722 0.026 12 77 7.01 1.3 2400 4220 650 1050' 400 0.127 0.821 0.704 0.117 13 77 7.01 1.6 2390 4160 600 1100 500 0.113 0.78 0.795 -0.015 14 77 7 1.4 2400 4210 650 1100 450 0.11. 0.782 0162 0.02 15 77 7 0.6 2390 4146 600 1600.. 400 0.105 0.773 0.768, 0.005 16 77 7 02 2350 4130 550 960 400 0.105 23 13 0.831 0.796 0.035 17 75 7.03 1,5 2430 4150 600 1050' 450 0.102 21 12 0.856 0.79' 0.066 18 73 7,02 1.4 2340 4140 550 1100 550 0.135 22 12 0.86 O 805, 0.055 19 77 7 1.8 2330 4200 550 1000 450 0.106 22 11 0.839 0.813 0.026 20 77 7 1.4 2230 4220 550 1050' 500 0.105 0.857 0.857 21 77 7 1.3 2300 4200 600 1050' 460 0.111 0.857 0.87 •0.01 22 77 7.24 1.4 2750 3720 650 1100' 450 0.372 13 9 0.849 0.879 -0.03 23 79 7.1 0.4 2890 4060 650 1100. 450 0.161 16 9 0.823 0.85 -0.027 24 79 7.07 0.4 3520 4180 700 1050 350 0,123 18 10 0.826 0.841 4015 25 77 7 0,7 3250 4060 700 1050 350 0.203 17 9 0.825 0157 -0.032 26 77 7.01 0.6 3300 4100 700 1000' 300 0191 18 9 0.786 1168 -0.582 27 75 7 0.7 3142 4020 680 1050 370 0.11 17 9 0.807 1.19 -0.38 28 77 7,01 0.7 3220 4080 700 1100 400 0.161 17 10 0.8% 1.OL -0.194 29 77 7 0.7 2780 4000 650 1100 450 0.112 12 8 0.746 0.898, -0.152 30 78 7 0.6 2900 4080 650 1100 45 0.133 13 10 0105 0.862 0.057 31 76 7 0.9 2210 3880 600 1100 500 0.1 10 6 0.835, 1.092 -0.257 1- Feb -96 75 7 0.9 2000 4000 600 1000 400 0122 12 10 0.761 0.848 •0.087 400 2 76 7 0.7 2522 4070 650 1050 OVS 13 9 0.744 1.385 •0.641 420 3 77 7 1.6 2380 4040 630 1050 0.119 10 9 0.778 1.106 0.328 4� 76 7 0.7 2114 4000 600 1050 450 0.119 16 14 0.779 0.962 -0.183 450 5 75 7 0.9 2600 3960 600 1050 0.118 15 14 0.747 0.87 •0.123 450 6.1 76 7 0.8 2500 3740 600 1050 0.13 19 16 0.77 0.846 -0.076 7� 77 7 0.7 2690 3800 600 105 0.124 18 15 0.709 0.815 -0106 4 450 8� 77 7 0.5 2870 3860 650 1100 0.11 15 12 0.701 0.826 0.125 450 9 78 7 0.7 2545 3872 600 1050 0.12 17 14 0.709 0.838 0.129 460 10 77 7 0.7 2640 3846 600 1050 0.121 17 14 0.702 0.868 -0.16 450 11 76 7 0.8 2660 3740 600 1050 0.115 15 14 0.634 0.834 -0. 450 12 73 7 0.7 2600 3780 650 1100 0.121 16 13 0.624 0.772 -0.14 450 13 73 7 0.4 2730 4080 650 1100 0.14 17 21 0.563 0.734 -0.17 450 14 73 7 1.8 2340 3900 650 1100 0.123 20 22 0.608 0.78 •0.17 400 15 72 7.03 2 2850 36 700 1100 0.105 17 20 0.631 0.813 -0.182 450 16 72 7.05 0.9 2630 3810 650 1100 0.126 17 21 0.605 0.835 -02 450 17 72 7.1 1.8 2660 4020 650 1100 0.178 17 20 0.671 0.881 -0.21 500 18 74 7 1 2770 4030 600 11DO 0.11 17 21 0.627 0.875 500 19 74 7 0. 2810 402 600 1100 0.102 18 2 0.587 0.862 0 20 21 0 mo 0 22 0 23 0 24 25 0 0 26 0 0 27 0 291 1 1 1 a I ( 0 108 Impact of the Use of High Level Groundwater on the Basal Lens in the ICeauhou Aquifer Prepared by: Tom Nance, PE Hydrologist Water Resource Engineer Tom Nance Water Resource Engineering 560 K1. Nimitz Hwy. - Suite 213 Honolulu, Hawaii 96817 Impact of the Use of High Level Groundwater on the Basal Lens in the Keauhou Aquifer Pre ?area for. Hawaii Island Economic Development Board P. O. Box 2159 Kamuela, Hawaii 96738 pre ? area b>: Tom Nance Water Resource Engineering 560 N. Nimitz Hwy. - Suite 213 Honolulu, Hawaii 96817 July 2014 EXECUTIVE SUMMARY Using monitoring data of Noah Kona groundwater that TNWRE has compiled, this report addresses whether or not impacts to basal groundwater have occurred as a result of pumping the six high level groundwater wells located above Mamalahoa Highway from Kalaoa to Waiaha. High level pumpage began in 1994 and is now at about 4.D to 4.5 MGD (Figures 2 and 3 in the report). The TNWRE monitoring data which address this question consists of continuous water level recording in the Kamakana well and time series salinity profiles in the Kamakana, Kaloko -2, Ooma Mauka, and Ooma Makai wells. The report presents and evaluates this data. Based on the water levels at the Kamakana Well and the salinity/ profiles at all four wells, no impact to basal groundwater as a result of high level groundwater pumpage has been identified to date. A key unresolved issue is whether or not the high level groundwater actually drains into the nominally downgradient basal lens in the area between Keahole Point and Kailua Town. Evidence gathered to date suggests that at least some, if not most, of the high level groundwater actually flows at depth beneath the basal lens to discharge into the marine environment offshore. The anomalous characteristics of the basal lens suggest this: very low water levels relative to the actual ocean level; very high salinity; temperatures significantly lower than the high level groundwater; and increasing salinity in wells under modest pumping rates. The more compelling evidence is provided by the discovery of fresh water under artesian pressure at depth below the basal lens in the Keopu and Kamakana deep monitor wells. If leakage of high level groundwater into the basal lens is limited to the modest amounts that evidence collected to date suggests, then the foreseeable future increases in pumpage of high level groundwater will have little or no impact on the basal lens. With the unresolved issue of high level groundwater leaking into or passing beneath the basal lens, monitoring for potential impacts to basal groundwater going forward should be continued and even expanded. This expansion should include deepening the Kaloko -2 well so that possible changes to the thickness of the basal lens at this locution can be tracked. o:-14-26 Table of Contents Executive Summary .......... ............................... ................ _.. ..... .. ..................... Introduction..................................................................... ............................... Groundwater Occurrence and Use in the Keauhou Aquifer ....... ............................... Hydrologic Connection Between Inland High Level Groundwater and the Nominally Downgradient Basal Lens ........................................................... ............................... Findings of Two Deep Monitor Wells ............................ ............................... Anomalous Temperature, Salinity, and Water Levels, of Basal Groundwater Between Keahole Point and Kailua Town .............................. Significance of the Natural Discharge of High Level Groundwater into or Beneaththe Basal Lens...... .......................... .................. .......... . ... ........... Monitoring Well Data Compiled by TNWRE ... ........................... ............ ....._........... Continuous Water Level Recording of Basal Groundwater at the Kamakana Monitor Well ................................................ ............................... Salinity Profiling to Track Changes in a Basal Lens ..... ............................... Salinity Profiling Results in the Kamakana Monitor Well ................... Salinity Profiling Results in the Ooma Monitor Wells ......................... Salinity Profiling Results in the Kaloko 2 Irrigation Well ..................... Future Monitoring as Pumpage of High Level Groundwater Increases .................... List of Figures Page 1 1 6 6 6 11 11 14 18 18 24 24 24 No. T i t l e Paqe 1 Location of DWS Production Wells in the Keauhou Aquifer .................. ............................... 2 2 Average Pumpage of High Level Groundwater by DWS from Kalaoa to Keopu and Years Each of the High Level Wells was Brought On Line ................... ............................... 4 3 Pumpage of DWS Wells in North Kona from 1976 through 2013 ......... ............................... 5 4 Well Locations from Keahole Point to Kailua Town .............................. ............................... 7 5 Salinity and Temperature Profile through the Water Column of the Kamakana Monitor Well on April 3, 2010 Prior to Encountering Fresh Water at Depth ........................ 8 6 Profile through the Water Column of the Kamakana Monitor Well on May 12, 2010 After Encountering Fresh Water at Depth .............................................. ............................... 9 7 Temperature in Saline Groundwater Below the Basal Lens in the Kamakana MonitorWell ........................................................................................... ............................... 10 8 Temperature Profiles in Basal Groundwater Between Keahole Point and Kailua Town ...... 13 9 Water Level in the Kamakana Monitor Well in Comparison to the Ocean Tide at KawaihaeHarbor ................................................................................... ............................... 15 10 Filtering the Semi - Diurnal Tide Using the 24 -MAV Statistic ................. ............................... 16 11 Comparison of the 24 -MAVs of Water Levels in the Kamakana Monitor Well and at KawaihaeHarbor ................................................................................... ............................... 17 12 Salinity and Temperature Profile through the Water Column of the FG -2 MonitorWell on May 4, 2014 ................................................................. ............................... 19 13 Salinity Profile Indicator Parameters ..................................................... ............................... 20 14 Salinity Trends in the Puuloa Sector of the Ewa Limestone Aquifer as Depicted by Data from the FG -2 Monitor Well ........................................................... ............................... 21 15 Comparative Salinity Profiles through the Water Column of the Kamakana Monitor Well, April 3, 2010 Versus May 22, 2014 .................................. ............................... 22 16 Trends of Salinity Indicator Parameters from Salinity Profiling in the KamakanaMonitor Well ......................................................................... ............................... 23 o:-14-26 List of Figures (continued) No. T i t I e Page 17 Salinity and Temperature Profile in the Ooma Mauka Monitor Well on May 20, 2014......... 25 18 Salinity and Temperature Profile in the Ooma Makai Monitor Well on May 20, 2014.......... 26 19 Trends of Salinity Indicator Parameters in the Ooma Mauka Monitor Well .......................... 27 20 Trends of Salinity Indicator Parameters in the Ooma Makai Monitor Well ........................... 28 21 Salinity and Temperature Profile through the Water Column of the Kaloko 2 Irrigation Well (No. 4160 -02) on May 13, 2014 .................................................... ............................... 29 22 Salinity Trends in the Water Column of the Kaloko 2 Irrigation Well .... ............................... 30 List of Tables No. T i t l e Page 1 Pumpage by DWS Basal and High Level Wells .................................... ............................... 3 2 Comparative Basal and High Level Groundwater Temperatures ......... ............................... 12 14 -26 INTRODUCTION This report has been prepared in response to a petition by the National Park Service (NPS) to the State Commission on Water Resource Management to designate the Keauhou Aquifer as a Groundwater Management Area. The petition asserts that present or planned future use of groundwater from the Keauhou Aquifer will reduce the flow of basal groundwater through Kaloko Honokohau (KAHO) National Historical Park, thereby causing harm to KAHO's anchialine ponds and its nearshore marine environment This report contains data from monitoring and production wells as compiled by Tom Nance Water Resource Engineering (TNWRE) to assess whether or not an impact to the basal lens has occurred due to ongoing groundwater use. It also presents an opinion as to whether or not the present level of monitoring can provide sufficient information to evaluate groundwater impacts as the future use of groundwater increases over present levels. GROUNDWATER OCCURRENCE AND USE IN THE KEAUHOU AQUIFER Prior to 1990, it was commonly assumed that all groundwater in the Keauhou Aquifer was basal, that is a lens of fresh and brackish water floating on saline groundwater beneath it and in dynamic equilibrium with the ocean along the shoreline. At that time, the Hawaii County Department of Water Supply (DWS) was operating six basal wells, all located in the southern part of the aquifer (shown in red on Figure 1 and listed in Table 1) and was pumping about eight (8) million gallons per day (MGD). Groundwater use by others everywhere else in the aquifer was quite modest. It amounted to pumping brackish wells at Keauhou to supplement the supply of a treated wastewater used to irrigate the Kona Country Club golf courses and use of saline groundwater for aquaculture at NELHA at Keahole Point. In 1990, first at Keauhou Well 2 (State No. 3355 -01) and soon after at the Kalaoa Well (No. 4358- 01), high level groundwater was discovered. High level groundwater stands much higher above sea level than basal groundwater. Unlike basal groundwater which is subject to increasing salinity if it is overpumped, the subsurface geologic control which creates the high level groundwater also protects it from salinity intrusion in response to pumping. As shown on Figure 2, use of high level groundwater in the Keauhou Aquifer began in 1994 with the Kalaoa Well and now includes six wells pumping between 4.0 and 4.5 MGD. All six of these wells are in the northern part of the aquifer in the area from Kalaoa to Waiaha (their locations are shown in blue on Figure 1). Use of high level groundwater has enabled DWS to reduce pumping its basal wells (Figure 3). Prior to this, DWS' basal pumpage at eight or more MGD was causing salinity issues. c_14-26 1 f w r � ` CWRM BOUNDARY OF ®KALAOA THE KEAUHOU AQUIFER 4358-Dl ®HVAb,LAI ^� 4258 -03 8HONOKOHAU 4138 -02 \ KALOKO ONOKOHAU ®QLT NATION L HISTORICAL -4057 -01 DWS' SIX ACTIVE \ PARK HIGH LEVEL ` 'MKEOPU GROUNDWATER WELLS \ _ l+� 3957 -01 sWAIAHA ;._ ■ DWS BASAL ti HOLUALOA WELL 3657 -01 / DWS' SIX ACTIVE BASAL GROUNDWATER �( WELLS 19VE DWS BASAL !HELLS IN KAHALUU -' 3557 -011 TO -05 NORTH FIGURE f LOCATION OF DWS PRODUCTION WELLS IN THE KEAUHOU AQUIFER -2- Table 1 Pumpage by DWS Basal and High Level Wells Well Average Annual Pumpage (MGD) State No. Name 1990 1994 2013 Basal Wells 3557 -05 Kahaluu Shaft 4.737 5.614 4.234 3557 -01 Kahaluu A 0.807 0.777 0.686 3557 -02 Kahaluu B 0.992 1.050 0.514 3557 -03 Kahaluu C 0.491 0.713 0.747 3557 -04 Kahaluu D 0.672 0.952 0.330 3657 -01 Holualoa 0.491 0.324 0.000 Total for Basal Wells 8190 9.430 7.040 High Level Wells 4358 -01 Kalaoa -- 0.168 0.889 4057 -01 QLT -- -- 1.299 4158 -02 Honokohau -- -- 1.648 4258 -03 Hualalai -- -- 0.000 3857 -04 Waiaha - -- 0.529 3957 -01 Keopu - -- 0.415 Total for High Level 0.000 0.168 4.251 Note: All pumpage data provided by DWS. o:_14 -26 3- 6.0 5.5 5.0 4.5 4.0 3.5 a E CL 3.0 ea 2.5 d m 02.0 d a 1.5 MW t11P 0.0 1992 1994 1996 1998 2000 2002 2004 Year Figure 2. Average Pumpage of High Level Groundwater by DWS from Kalaoa to Keopu and Years Each of the High Level Wells was Brought On Line .4- 6.0 5.5 5.0 4.5 4.0 3.5 3.0 2.5 2.0 1.5 1.0 0.5 0.0 2006 2008 2010 2012 2014 14 12 6 10 0 a� rn M 8 CL E a �a c 6 c Q m �o > 4 a 2 0 1975 Figure 3. Pumpage of DWS Wells in North Kona from 1976 through 2013 1980 1985 1990 1995 2000 2005 2010 Year ...... _ ........ _ —0 —Total of All DWS Wells in North Kona —o —Total of Basal Wells —o— Total of High Level Wells -5- 14 12 10 A 4 2 0 2015 HYDROLOGIC CONNECTION BETWEEN INLAND HIGH LEVEL GROUNDWATER AND THE NOMINALLY DOWNGRADIENT BASAL LENS The subsurface geology that :reates the high level groundwater is not known for certain, but the most likely explanation appears to be a series of poorly permeable lava flows that are in aggregate at least tens and possibly hundreds of feet thick. The information presented in the paragraphs below are the basis for this statement. Findings of Two Deep Monitor Wells Two deep monitor wells, Keopu (No. 3858 -01) and Kamakana (No. 3959 -01), have encountered fresh water under artesian pressure at depth below the basal lens and the saline groundwater below the lens (the locations of these two wells are shown on Figure 4). The comparative salinity and temperature profiles before and after encountering the fresh water at depth in the Kamakana Well illustrate this (Figures 5 and 6). Of particular note is the temperature decline and then reversal with depth in the saline groundwater zone. In combination with the unvarying salinity 500 to 950 feet below sea level, these data identify the strata confining the freshwater at depth (Figure 7). These results suggest that at least some, if not most, of the high level groundwater is flowing beneath the confining layers to the ocean at depth offshore rather than into and through the basal lens. Anomalous "Temperature, Salinity, and Water Levels of Basal Groundwater Between Keahole Point and Kailua Towr If all or even most of the high level groundwater is flowing into the nominally downgradient basal lens, this flow would constitute, by far, the largest component of recharge to the basal lens. It would be expectable that water levels in the lens would be at least two to three feet above the actual ocean level, that salinities would be of at least irrigation (brackish) quality, that salinities would be stable under at least moderate rates of pumping, and that basal water temperatures would be similar to the temperatures of the high level groundwater. In fact, basal groundwater between Keahole Point and Kailua Town exhibits none of these characteristics. Instead, occurrence of the basal groundwater can be characterized as follows: Based on a density analysis of the salinity profile in the Kamakana Well (Figure 5 prior to encountering fresh water at depth), the water level in the basal lens at this location is no more than 0.4 feet above the actual ocean level. �1 r II � W»I »,ur• ' �I r' ' 1 J OOMA M, MONITOR L-1 4 41 KAHO MONITOR WELLS 40 -01 OLT �� • 4057 -01 ...».. �"� KAMAKANA Qi PALANI + MONITOR 9 -01 3959 -01 ' KEOPU _ �� • 3957 -_0_ 1 KEOPU �• { KL{OPU 14 MONITOR © 3957 -►05 �.' 3858 -01 « , ..■.. ill ' (WAIAHA 3857 -04 NORTH FIGURE 4 GRAPHIC SCALE: WELL LOCATIONS FROM KEAHOLE 6000' 3000' 0 6000' 12000' POINT TO KAILUA TOWN -7- ( ' KEAUHOU AQUIFER- BOUNDARY' r KAU 1 � 4458 —Q1 r KA0 •2 ( ( _ '.4458-02 " KI4LAOlt' KALAOA a 1 �» 4358 -01 + OOMA MAUKA — ONITOR KALOKO .RIHUATACA1 t 2 4258 -03 ' ; --- 4160-02-- � a -" KALOKO 1 PALANI 1 Q 4158 -03 4160 -01 x'41 ,rd,2' , "' © HONOKOHAU 4158 -02 40 -01 OLT �� • 4057 -01 ...».. �"� KAMAKANA Qi PALANI + MONITOR 9 -01 3959 -01 ' KEOPU _ �� • 3957 -_0_ 1 KEOPU �• { KL{OPU 14 MONITOR © 3957 -►05 �.' 3858 -01 « , ..■.. ill ' (WAIAHA 3857 -04 NORTH FIGURE 4 GRAPHIC SCALE: WELL LOCATIONS FROM KEAHOLE 6000' 3000' 0 6000' 12000' POINT TO KAILUA TOWN -7- Figure 5. Salinity .and Temperature Profile through the Water Column of the Kamakana Monitor Well on April 3, 2010 Prior to Encountering Fresh Water at Depth Salinity (PPT) 0 5 10 15 20 25 30 35 40 0 50 100 150 200 250 300 350 400 m LL a� 450 .r 3 500 0 550 r Q 600 C) 650 700 750 800 850 900 950 1000 0 50 100 150 200 250 300 350 400 450 500 550 600 650 700 750 800 850 900 950 1000 57 59 61 63 65 67 69 71 73 Temperature (Deg F) LSalinity — Temperature -8- Figure 6. Profile through the Water Column of the Kamakana Monitor Well on May 12, 2010 After Encountering Fresh Water at Depth Salinity (PPT) 0 5 10 15 20 25 30 35 40 0 50 100 150 200 250 300 350 400 w 450 m d 500 m 0 550 $ 600 c CL 650 d 0 700 750 800 850 900 950 1000 1050 1100 57 59 61 63 65 67 69 Temperature (Deg F) Salinity — Temperature 0 50 100 150 200 250 300 350 400 450 500 550 600 650 700 750 800 850 900 950 1000 1050 1100 71 73 Figure 7. Temperature in Saline Groundwater Below the Basal Lens at the Kamakana Monitor Well 45 50 55 60 65 70 75 80 0 100 200 300 400 m 500 U. m 3 600 0 c_ r a 700 m D 800 900 1000 1100 1200 0 100 200 300 400 500 600 700 800 900 1000 1100 1200 45 50 55 60 65 70 75 80 Temperature (Deg F) — Kamakana Monitor Well Ocean Offshore -10- There are no successful salinity- dependent production wells in the basal lens between Keahole Point and Kailua Town. The very high and unstable salinity at very modest pumping rates in Palani Well (No. 4059 -01), which is located 2.6 miles in from the shoreline, is a prime example of this. Results of the Kaloko 1 and Kaloko 2 Wells (No. 4160 -01 and -02) are similar examples Temperatures at the top of the basal lens are significantly colder than the high level groundwater and these temperatures decrease with depth (Table 2 and Figure 8). Significance of the Natural Discharge of High Level Groundwater into or Beneath the Basal Lens If recharge to basal groundwater included substantial leakage from the upgradient high level groundwater, then pumpage from the array of high level groundwater production wells shown on Figures 1 and 4 would ultimately reduce the flow in the basal lens, causing at least some decline in basal water levels and a gradual increase in salinity. In this case, a monitoring well network would be critical to detecting and quantifying the impact on the basal lens. The discovery of fresh water at depth in the two deep monitor wells (Keopu and Kamakana) and characteristics of basal groundwater between Keahole and Kailua Town suggest that some or perhaps even most of the high level groundwater is not leaking into the basal lens but is instead flowing beneath the lens and discharging offshore along this section of the Keauhou Aquifer. If this interpretation ultimately proves to be the case, a monitoring well network would presumably document that little or no change to basal groundwater as a result of pumping the high level wells has occurred. MONITORING WELL DATA COMPILED BY TNWRE As shown on Figures 1 and 4, all six of DWS' active high level wells are located above Mamalahoa Highway and in a linear array from Kalaoa to Waiaha. Any impact to basal groundwater as a result of pumping these high level wells would most obviously occur in the area between Keahole Point to Kailua Town. If the high level groundwater is flowing into the basal lens, high level pumping would reduce the flowrate in the basal lens. Although the basal flowrate is not measurable directly, a reduction in its flowrate should be identifiable as a progressive lowering of the basal water level and /or as a progressive increase in salinity. Both would reflect a shrinking of the lens in response to a lesser flowrate through it. The sections following present monitoring data compiled by TNWRE which provide insight on whether such changes have been detected. - 11 - Table 2 Comparative Basal and High Level Groundwater Temperatures High Level State No. Name Temperature (of) 3857 -04 Waiaha 70.0 3858 -01 Keopu Monitor's 69.8 3957 -01 Keopu 70.0 4057 -01 QLT 68.0 4158-02 Honokohau 70.3 4258 -03 Hualalai 69.8 4358 -01 Kalaoa 73.9 0:_14 -26 -12- Basal State No. Name Temperature A 3959 -01 Kamakana 66.1 4059 -01 Palani 67.5 4160 -02 Kalako 2 64.7 - - Ooma Mauka 67,1 - - Ooma Makai 68.4 Figure 8. Temperature Profiles in Basal Groundwater Between Keahole Point and Kaiiva Town 63 64 65 66 67 68 69 70 M 10 20 30 cci 40 u- d co 3 0 50 c_ L a.+ a W a 60 80 90 100 mug 10 20 30 40 50 70 80 90 100 63 64 65 66 67 68 69 70 Temperature (deg F) —Kamakana —Ooma Mauka —Ooma Makai —HELCO Disposal Well -13- Continuous Water Level Recording of Basal Groundwater at the Kamakana Monitor Well As shown on Figure 4, the Kamakana Monitor Well (State No. 3959 -01) is located directly downgradient of DWS' Honokohau and QLT Wells (Nos. 4158 -02 and 4057 -01, respectively). These are the two most actively used of DWS' six high level production wells (refer back to Table 1 for their use rates). As such, the Kamakana Well is ideally situated to document a declining basal water level, should that be occurring. Water level recording in the Kamakana Monitor Well was begun in August 2011. Except for a 29 -day period in August- September 2012, the record is continuous through April 2014. There are three issues which complicate an interpretation of this record. First, as can be expected for basal groundwater in a highly permeable formation, there is a substantial water level response to the ocean's semi - diurnal tide. Second, there are also substantial changes to the ocean's mean water level due to large scale meteorological events and these are reflected in corresponding changes in the mean groundwater levels. Third, the datum for the elevation benchmark used to measure water levels in the Kamakana Well is not from the same datum used by NOAA for its tide gage in Kawaihae Harbor. As described below, these complications can be sorted out to determine if the basal groundwater level has declined with respect to the actual ocean level over the recording period of the Kamakana Well. Figure 9 is a comparative plot of the Kamakana water level data and the ocean level as measured by NOAA at Kawaihae Harbor (Figure 9) Except for the obvious disconnect in elevation datums, the data are difficult to interpret as presented in this manner. The semi - diurnal ocean tide in both the NOAA and Kamakana data can be filtered out by calculating their respective moving 24 -hour averages (24 -MAV), making it easier to see that most of the changes in the mean groundwater level are the result of the changes in the mean ocean level (Figures 10 and 11). When these water levels are averaged over identical periods (either as averages of the data itself or as averages of the 24- MA11s), the data establish that no decline in the basal water level relative to the actual ocean level has occurred over the August 2011 through April 2014 period. In fact, there has been a slight and gradual rise of the basal water level relative to the ocean level over this period (tally below). Comparative Mean Water Levels -14- Kamakana Kawaihae Height Year Well Tide Difference (Feet MSL) (Feet MSL) (Feet) 2011 (Aug. thru Dec.) 3.2085 0.0913 3.1172 2012 3.1552 0.0187 3.1365 2013 3.2844 0.0986 3.1858 2014 (thru 4/30) 3.2352 - 0.00.12 3.2364 -14- 4.0 3.5 3.0 2.5 2.0 J N d 1.5 m U. > 1.0 m J °1 0.5 �a 3 0.0 -0.5 -1.0 -1.5 811 Figure 9. Water Level in the Kamakana Monitor Well in Comparison to the Ocean Tide at Kawaihae Harbor ivvnn i Iuc vain IUI rXawan lac I ial vvI -15- 4.0 3.5 3.0 2.5 2.0 1.5 1.0 0.5 0.0 -0.5 -1.0 -1.5 M4 14.V 3.5 3.0 2.5 N 2.0 m 1.5 LL Z m 1.0 J 3 0.5 0.0 -0.5 -1.0 15 Figure 10. Filtering the Semi - Diurnal Tide Using the 24 -MAV Statistic ww� IT1Rj= 1 - �11 r fir• �� -�'R �T i 1 I I i k, ."AWL 1 FMO i i r r r r r 1 ����i J a ► < < � I l , iOA6. 4.0 3.5 3.0 2.5 2.0 1.5 1.0 0.5 0.0 -0.5 -1.0 -1.5 8/1/11 11/29/11 3/28/12 7 6/12 11/23/12 3/23/13 7/21/13 11/18/13 3/18/14 7/16/14 Hourly NOAA Tide Data Day and Time 24 -MAV of Tide Data -16- 5.0 4.5 Z 4.0 d 3.5 U. d 3.0 c Y A 2.5 Y c m 2.0 w J 1.5 1.0 0.5 00 Figure 11. Comparison of the 24 -MAVs of Water Levels in the Kamakana Monitor Well and at Kawaihae Harbor 24 MAV of the Kamakana Well V _ r&.A _ 24 -MAV of the Kawaihae Ocean Tide 8/1/11 11/29/11 3/28/12 7/26/12 11/23/12 3/23/13 Day and Time -17- 2.5 Nuf 1.5 CA 2 m 1.0 U. 0 0.5 0 t 0.0 3 R Y -0.5 m m J -1.0 c -1.5 I — -2.0 -2.5 7/21/13 11/18/13 3/18/14 7/16/14 �� Salinity Profiling to Track Changes in a Basal Lens In nearshore areas with very permeable strata, mean water level changes in basal groundwater as a result of changes in the flowrate through the lens are very subtle and difficult to identify, particularly in comparison to the magnitude mean level changes resulting from the varying mean ocean level Decades of monitoring by TNWRE have demonstrated that a far more effective way to monitor changes in basal groundwater is by a series of salinity profiles through the water columns of wells. The method is described below using results of the F'G -2 monitor well in the Puuloa Sector of the very permeable Ewa limestone aquifer on Oahu. Using an instrument that records data at 10 times a second, a continuous salinity profile is made through the well's water column. A typical sigmoid salinity curve is obtained which depicts the brackish basal lens and the transition zone from the basal lens above the saline groundwater below (Figure 12). If a basal lens is shrinking due to a reduced flowrate, a time sequence of salinity profiles will shift to the right and shrink upwards over time. As shown on Figure 13, two i -idicators from the salinity profile are selected to track changes over time. For the FG -2 well, these indicators are the salinity at a depth of 10 feet into groundwater and the depth to the midpoint of the transition zone, defined for the FG -2 well as the depth where the salinity is 17.5 parts per thousand (PPT). 17.5 PPT is half of seawater's 35 PPT salinity. If the lens is shrinking due to a reduced flowrate, the salinity 10 feet into water would gradually increase and the depth to the midpoint of the transition zone would gradually decrease. The two indicators parameters are graphically arrayed over the 20 -year record for FG -2 on Figure 14. Over that time, major changes to the aquifer are readily identified. Over this same 20 -year period, TNWRE has recorded groundwater levels at a number of locations in the aquifer. Other than the dramatic impact of the November 1996 storm, the water level record over this 20 year period does not identify theses changes as they are one to two orders of magnitude less than the effects of the varying mean ocean level. Salinity Profiling Results in the Kamakana Monitor Well. Salinity profiling through the basal lens in the Kamakana Monitor Well has been done 22 times since April 2010. Figure 15 depicts the first (April 3, 2010) and most recent (May 22, 2014) profiles. Using as indicators the salinity ten feet into groundwater and the depth to the midpoint of the transition zone (ie. the depth at a salinity of 17.5 PPT), the series of results for the 22 profilee is presented on Figure 16. The salinity 10 feet into water at present is essentially the same as its level in April 2010. There has been a slight decrease in the depth to the midpoint of the transition zone, an aspect that bears watching during future monitoring. -18- Figure 12. Salinity and Temperature Profile through the Water Column of the FG -2 Monitor Well on May 4, 2014 0 5 10 Sj�_INITY (�gT) 25 30 35 0 5 10 15 20 25 w 30 w w w 35 a 040 H z 45 IL w 13 50 55 60 65 70 75 76 77 78 79 80 81 TEMPERATURE (DEG F) SALINITY — TEMPERATURE -19- 0 5 10 15 20 25 30 35 40 45 50 55 60 65 70 82 Figure 13. Salinity Profile Indicator Parameters 0 5 10 SALINITY (T) 25 30 35 0 5 10 15 20 25 w 30 w LL w 35 f- Q 0 40 F- z 45 a W O 50 55 60 65 70 0 5 10 15 20 25 30 35 40 45 50 55 60 65 70 75 76 77 78 79 80 81 82 TEMPERATURE (DEG F) — SALINITY — TEMPERATURE -20- d w. Q Q d C yO Q1 E m �3 M 3 O W C O r� O tV r U- md � E 7 aM m0 t C � U! c v 'a H m 4� y C M t0 r 7 LL N (199:1) auoZ uol;lsuejl ay; ;o;ulodplW ay; o; Ja;eM O;ul 43daa lLOV- C N C3 LO h to N O ti LO N O� N N N N •- T-- r r- Udd) JOIBM o;ul 100:10 6 f4!u!IeS O - CCD N r r N N r N r N N r O cor co N N co 0 co N N rn N N r a 0 O M N r 0 0 M N r co Q r M N CD a) M N LO v r r Cl) 0) d C N .y C t`0 F- 0 c_ .0 0 c N LPL _o 'c co IL N Figure 15. Comparative Salinity Profiles through the Water Column of the Kamakana Monitor Well, April 3, 2010 Versus May 22, 2014 0 5 10 15 20 25 30 35 0 25 50 75 100 125 m 150 d m 3 175 0 c 200 CL m 225 250 275 300 325 350 i 1 1. 0 25 50 75 100 125 150 175 200 225 250 275 300 325 350 0 5 10 15 20 25 30 35 Salinity (PPT) L=May 2014 —April 20101 -22- t0 r d 7 LL (;aad) /4iuileS ldd 916 W J04BM O;ui y ;dap LO C) Lo LO 't Iq M M N N r- LO O A v r N r Cl) M r ('7 ti O aM-' M N_ w C co E rn � 3 N tU O Na0+ N t6 M Q r N Q� r N O a) N m O r N O CO (O IT N O 00 to v N 04 N r r r Udd) Ja;eM O;ul;aad 01 A4iwIeS i I 1 1 L I I I i i I 1 CO) N Salinity Profiling Results in the Ooma Monitor Wells. Locations of the two Ooma monitor wells are shown on Figure 4. Although they have not been profiled as frequently as the Kamakana Monitor Well, their record starts in November 2002, a longer period of time than for the Kamakana well. Its most recent salinity and temperature profiles are shown on Figures 17 and 18. Trends of salinity (10 feet into water) and lens thickness (depth to 17.5 PPT salinity) are shown on Figures 19 and 20. Over the 12 -year period of record, the salinities 10 feet into water are the same or slightly fresher than in November 2002 and the depths to the midpoint of the transition zone are essentially unchanged. The closely spaced sequence of profiles in May 2009 and again in May 2014 were done to see the effect on the profiles of the semi - diurnal tide. For nearshore wells such as the two at Ooma, that effect is relatively significant, creating significant variability in the indicator parameters. Salinity Profiling Results in the Kaloko 2 Irrigation Well. The Kaloko 2 irrigation well only penetrates about 18 feet into groundwater, not deep enough to reach the midpoint of the transition zone (Figure 21). In lieu of this, the salinity at varying depths into groundwater have been tracked (Figure 22). No trend of increasing salinity in this 'Nell has occurred since the first salinity profile done in March 1996. FUTURE MONITORING AS PUMPAGE OF HIGH LEVEL GROUNDWATER INCREASES So far, monitoring data of the basal lens as complied by TNWRE has not shown an impact of high level groundwater pumpage on the nominally downgradient basal lens. However, there is still an unresolved question on whether the natural discharge of groundwater is into or beneath the basal lens. Also, it is virtually certain that high level groundwater pumpage will increase in the future. A number of new wells in production are foreseeable, including Palani 1 (No. 4158 -03), Keopu 4 (No. 3957 -05), another QL,f well, and another well near Waiaha. Greater use of the Keopu Well (No. 3957 -01) will be made possible with transmission imp,ovements in the Mamalahoa corridor to be completed as a part of outfitting the Keopu 4 Well. Similarly, greater use of the Waiaha Well (No. 3857 -04) will occur with completion of a nearby mauka- to -makai transmission corridor. In light of the foreseeable increase in high level groundwater pumpage, it is reasonable to ask if current ongoing monitoring will adequately detect changes to basal groundwater resulting from this use. Recommendations for groundwater monitoring going forward are as follows: Continue salinity profiling and water level recording in the Kamakana Monitor Well. It is ideally located downgradient of present and foreseeable future high level groundwater pumping. Drill the Kaloko 2 irrigation well at least 400 feet deeper and convert it to a permanent monitoring well with continuous water level recording and salinity profiling. The recommended depth will completely portray the basal lens and transition zone and also the temperature reversal at depth. As with the Kamakana Well, the well is ideally located. It is downgradient of DWS' Hualalai Well -24- 0 10 20 30 40 a� m U. L d .r 3 50 0 c L 60 70 80 90 100 63 64 65 66 67 68 Temperature (Deg F) —Salinity —Temperature Figure 17. Salinity and Temperature Profile in the Ooma Mauka Monitor Well on May 20, 2014 0 5 10 Salin% (PPT) 20 25 30 -25- 0 10 20 30 40 50 60 70 80 90 100 69 0 3 6 9 12 u. m 15 0 c_ t CL 18 21 24 27 30 Figure 18. SaEnity and Temperature Profile in the Ooma Makai Monitor Well on May 20, 2014 0 5 10 Salini% (PPT) 20 25 30 0 3 6 9 12 15 18 21 24 27 30 64 65 66 67 68 69 70 Temperature (Deg F) Salinity — Temperature, -26- 20 18 16 IL 14 a m i 12 3 0 10 m m LL 0 8 �c U 6 4 2 0 9/1/2002 8/31/2004 8/31/2006 8/30/2008 8/30/2010 Date --o— Salinity 10 Feet into Water —1— Depth at 17. 5 PPT Salinity ) Figure 19. Trends of Salinity Indicator Parameters in the Ooma Mauka Monitor Well -27- 50 45 40 q 35-S M U) 300- 25 as A 20 3 0 C 15 m 0 10 5 0 8/29/2012 8/29/2014 20 18 16 14 12 H CL CL .2� 10 .0 y 8 4 2 0 9/1/2002 8/31/2004 8/31/2006 8/30/2008 8/30/2010 Date Salinity 5 Feet into Water - -Depth at 17. 5 PPT Figure 20. Trends of Salinity Indicator Parameters in the Ooma Makai Monitor Well -28- 50 45 40 F4 35-S m w, 300. r: 25 L d 20 O 4d C 15 a d 10 5 0 8/29/2012 8/29/2014 Figure 21. Salinity and Temperature Profile through the Water Column of the Kaloko 2 Irrigation Well (No. 4160 -02) on May 13, 2014 Salinity (PPT) 1.75 1.80 1.85 190 1.95 2.00 0 1 2 3 4 5 6 7 8 d i g 3 0 c 10 z a+ CL 11 0 12 13 14 15 16 17 18 2.05 64.56 64.60 64.64 64.68 64.72 Temperature (Deg F) Salinity —Temperature -29- 0 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 64.76 64.80 O O to 0 LO 0 U'j 0 U') 0 0 O O co co t- co to Ul) LO CV r r V-: r T-: r r V.: V: V-: . . . . . . . . . CD M co Q U) (0 O Im U-) 0 a` O (Y) O O O co C) O O co- - ----- -------- co O co co co co 0 LAO O .... ............................ .......... LO Ul) O U') O LO 0 LO 000 O O O 00 llq h (P Co IQ Up co V- Udd) ANIMS (D 0 LL Lo f cr) (No. 4258 -03) and the soon to be put into service Palani Well (No. 4158 -03). It is also directly upgradient of KAHO. The water levels and periodic salinity profiles in both the Kamakana and Kalaoa 2 Wells would enable an accurate depiction of potential changes in the basal lens downgradient of pumpage of the high level aquifer between Kalaoa and Waiaha. Continue periodic salinity profiling in the Ooma monitor wells. Although these wells are not ideally located, their records predate the start of pumpage in the high level aquifer and are useful in that respect. -31 - SUMMARY OF RESULTS FROM THE KOHANAIKI WATER QUALITY MONITORING PROGRAM Prepared by: Dr Richard Brock, Ph.D. Aquatic Resource Specialist Environmental Assessment, LLC 12:32 Lunalilo Home Road Honolulu, Hawaii 96825 SUMMARY OF RESULTS FROM THE KOHANAIKI WATER QUALITY MONITORING PROGRAM Richard Brock, Ph.D. Environmental Assessment, LLC 1232 Lunalilo Home Road Honolulu, Hawaii 96825 June 2014 EAC Report No. 2014 -09 TABLE OF CONTENTS Page 1.0 Background ........................................................ ............................... 1 1.1 The Monitoring Program .............................. ............................... 1 2.0 Results 2.1 Compliance with State St,-�ndards ................. ............................... 2 2.2 Pre- Development Water Quality ................... ............................... 2 2.3 Water Quality with Development .................. ............................... 3 2.4 Changes in Marine Water Quality ................. ............................... 4 3.0 Observations on Salinity and Anchialine Biota .. ............................... 5 4.0 Literature Cited ................................................... ............................... 5 List of Tables Table 1. Table of parameter means from 2005 through 2013 for wells. anchialine pools and shoreline stations ..................... 6 Table 2. Results of the Wilcoxon 2- Sample Test comparing pre- construction to during construction parameter means for marine sampl, .-s .......................... ............................... 7 Table 3. Results of the Wilcoxon 2- Sample Test comparing marine parameter means from control sites to those from sites fronting the development ........... ............................... 8 List of Figures Figure 1. Map showing the approximate locations of water quality monitoring sites .......................................... ............................... 9 Figure 2. Plot of nitrate nitrogen measured four sites from 2005 through June; 2007 .................... ............................... 10 Figure 3. Plot of orthophosphorous measured at four sites from 2005 through June; 2007 .................... ............................... 11 Figure 4. Plot of nitrate nitrogen measured at four sites in the 2005 - 2013 period .......................... ............................... 12 Figure 5. Plot of orthophosphorous measured at four sites in the 2005 - 2013 period .......................... ............................... 13 Figure 6. Mean nitrate nitrogen in all sampled anchialine pools from 2005 through 2013 .................. ............................... 14 Figure 7. Mean orthophosphorous in all sampled anchialine pools from 2005 throug=h 2013 .................. ............................... 15 Figure 8. Mean opae'ula shrimp counts in anchialine pools from 2005 through 2013 ............................ ............................... 16 SUMMARY OF RESULTS FROM THE KOHANAIKI WATER QUALITY MONITORING PROGRAM R. Brock, Ph.D. 1.0 Background 1.1 The Monitoring Program As part of the permitting process allowing the Kohanaiki development to occur, the County of Hawai'i imposed a requirement for a water quality monitoring program to insure that the quality of the ground and nearshore marine waters are not degraded as the development proceeds. This monitoring program was approved by federal, state and county agencies and the methods follow the Hawai'i State Department of Health (DOH) Regional water quality protocols (HAR Chapter 11- 54- [6]d). Samples are handled as per USEPA protocols and follow procedures outlined in Standard Methods (1999). Samples are analyzed at the University of Washington's School of Oceanography Marine Chemistry Laboratory that specializes in low level nutrient analysis. Sampling is carried out six times a year during dry periods as well as following high rainfall events where the "trigger" initiating sampling is 1.5 inches or more of rainfall falling within a 24- hour period. In each survey between 105 to 110 samples are collected which includes replicates for quality assurance /quality control purposes. Samples are collected from the ocean, in brackish anchialine ponds present on the project site and from wells present in the project area. Eight marine samples are collected along transects that commence at the shoreline at extend 500 m seaward. Four marine transects have been established away from the project site to serve as control sites (one fronting Wawaloli Beach, 1.2 km north of the project site and three transects to the south established offshore of the Kaloko- Honokohau National Historical Park (or KAHO). Five marine transects have been set up fronting the Kohanaiki project site. Thus on each survey, 32 marine samples are from control sites and 40 marine samples come from the waters fronting the Kohanaiki project site. On land samples are drawn from 14 wells, 16 anchialine ponds and one reservoir all located on the project site. Figure 1 shows the approximate locations of the marine transects as well as the pond and well sample sites. Four surveys (from April through June 2005) were undertaken prior to the commencement of construction. Site grading commenced in September 2005 and more recently construction is ongoing. Over this period of time 57 water quality monitoring surveys have been completed with eleven of them occurring following high rainfall events. Golf course construction was undertaken in the June 2007 through May 2009 period and the "grow -in" period establishing the golf course turf was finished in October 2009. Since the completion of golf course grow -in, 32 surveys have been done and through the January 2014 period 5,683 water quality samples have been analyzed and reported on. This report summarizes the findings of this monitoring program through January 2014. FACT: Because the Kohanaiki project site is directly north of the KAHO, the water quality monitoring program is the most stringent of all such non - potable monitoring programs in West Hawaii (i.e., frequency of sampling, numbers of samples). 2.0 Results 2.1 Compliance with State Standards The state DOH has water quality standards that apply to marine waters. There are no state water quality standards for anchialine pools or for coastal (non - potable) monitoring wells. In the preconstruction period 32 marine transects were completed finding that fronting the project site the rate of non - compliance was 28% among the parameters and for control site transects the rate of non - compliance was 52 %. In the during construction period 461 transects have been completed and for those transects .sampling waters offshore of the development the rate of non- compliance is 42% and for control site transects the rate of non - compliance is 60 %. What are the findings telling us? Non - compliance is commonplace for all parameters in the pre- and during construction periods. More non - compliance occurs at the control stations than at stations fronting the development and the greatest geometric means (which are used to determine compliance) are found at control sites for all parameters. These findings are related to the greater groundwater escapement to the sea fronting some control site transects. Fact: Compliance /non - compliance among parameters occurs on a coast -wide basis and is not differentially greater at stations fronting the development. 2.2 Pre - Development Water Quality The following generalizations have been noted at Kohanaiki as well as at other West Hawai'i sites prior to much development: (1) nutrient concentrations are elevated in mauka groundwater and as groundwater flows towards the sea, the concentrations decrease due to mixing with intruding seawater. (2) However, biological activity and physical processes in anchialine pools may modify nutrient concentrations both up and down but (3) as the groundwater approaches and enters the sea, concentrations decrease very rapidly because ocean water has low concentrations of these parameters. These decreases are primarily due to simple dilution. Figure 2 shows the concentrations of the nutrient nitrate nitrogen (nitrate -N or NO,) over the first three and a half years prior to the start of golf course construction in a mauka monitoring well adjacent to the property boundary at Kohanaiki and also in two anchialine pools seaward of this well and finally at the shoreline seaward of the two ponds. Figure 3 show the changes in orthophosphorous (ortho -P or PO4) over the same time period and sample locations. Fact: In natural undisturbed environments, nutrient concentrations vary tremendously 2 through both time and space. At some locations concentrations are naturally elevated and at others they are low, but all of them have high variability in concentrations through time. This is reflected in the well data as given in Figures 2 and 3 and is most evident in static monitoring wells relative to coastal wells developed for water withdrawal. 2.3 Water Quality with Development The same facts continue to hold with development but with the following caveat: coastal development will usually cause increases in some nutrient concentrations and these are seen at sample points makai of the development. At Kohanaiki most of these makai sample points are located in the anchialine pools present on the project site. To expect development not to cause change is denying common sense. Figure 4 is a continuation of Figure 2 showing the changes in concentration of NO3 to the present time. Again, the concentrations are generally greater in the mauka well and decrease moving towards the ocean but occasional increases occur in the anchialine pools and these are related to the development and sometimes to high rainfall events. Figure 5 is a continuation of Figure 3 and shows these changes for PO4 at the same locations up to the present time. Figure 5 again demonstrates the greater fluctuation in the concentration of PO4 in the mauka well and to a lesser extent at sample points makai due to dilution. Golf course "grow -in" temporarily increased the concentration of NO3 in some of the anchialine pools as shown in Figure 6 but the concentrations measured have no impact on biota. Why? There are three reasons: (1) the changes are often less than those found at some non - developed Kona sites, (2) when nutrients are in excess (as is the case for much of Kona's groundwater), adding more does not cause a response and (3) the increases may be large but quickly decrease. If NO3 is in excess as during "grow -in ", it will readily move through soil horizons with irrigation water down to the seaward flowing groundwater below and into the anchialine pools. However phosphorus does not readily move but binds with the soil. This is evident in Figure 7 where there are no identifiable increases in PO, above earlier "preconstruction" peaks in the "grow -in" period. Table 1 presents the mean concentrations of important nutrient parameters in the groundwater over the 2005 -2014 period at Kohanaiki as it moves from the mauka boundary of the project site to the shoreline. Nitrate -N, Ortho -P and Total -P all show decreases as the groundwater approaches the shoreline. Similarly in the preconstruction period, Total -N showed the same decrease moving from inland to shoreline sample points. However today in the anchialine pools there is a —3% increase of Total -N which may be related to the restoration activities occurring in some pools. As expected, salinity increases with proximity to the shoreline. Ammonia -N increases because it is a product of organism metabolism and the anchialine pools have a complex community of organisms nevertheless ammonia -N concentrations like all of the others decrease with proximity to the ocean. Fact: With development, the decrease in nutrient concentrations in groundwater as measured at inland wells, anchialine pools and seaward to the shoreline seen previously continue to hold with some transitory increases occurring in the anchialine pools but the signature continues to be lost at the shoreline. Despite the fluctuations in concentrations of some nutrients in anchialine pools, there is no evidence of decline to pond biota connected to changes in water quality (Figure 8). 2.4 Changes in Marine Water Quality The question, "Has the quality of the ocean waters fronting the Kohanaiki project site been negatively impacted by the development ?" is addressed in Table 2 examining the means of important nutrient parameters in two time periods, before the commencement of construction and in the during the construction period. The data are examined using the Wilcoxon 2- Sample Test and the results are presented in Table 2. Referring to Table 2, the during construction means for ammonia -N, total -P, salinity and turbidity are all significantly greater than are the preconstruction means. The preconstruction means for nitrate -N and total -N are significantly greater than the during construction means for those two parameters and the means for ortho -P and dissolved silica show no significant differences. These data suggest that the activities occurring at Kohanaiki could be increasing the concentrations of some nutrient parameters. Another approach to determine if the activities on the Kohanaiki project site are having a negative impact to the quality of the adjacent marine waters is to examine the means of important nutrient parameters as sampled from the marine control sites and compare these means to those from the sample sites fronting Kohanaiki. Table 3 presents the results of the Wilcoxon 2- Sample Test addressing the question, "Are there significant differences among the mean parameter concentrations for samples collected at control transects relative to those collected fronting the project site ? ". Referring to Table 3, all of the important nutrient parameters have significantly greater mean concentrations at the marine control site transects relative to the Kohanaiki transects except for salinity which is significantly greater (by 0.953 ppt) offshore of Kohanaiki. FACT: Despite significant changes in concentrations of some water quality parameters over time offshore of the Kohanaiki project site, these changes are small relative to the mean concentrations measured at the marine control sites. In no case is there any evidence to suggest that the changes in water quality parameters are having any negative impact to the resident reef species. KOHANAIKI WATER QUALITY SUMMARY: What have the impacts been? In the Ocean: areas. No evidence of increased nutrients due to development when compared to adjacent control 4 On Land: Transitory increases seen in anchialine pools but the signature is lost at the shoreline. No decline found in the pond biota connected to changes in water quality. 3.0 OBSERVATIONS ON SALINITY AND ANCHIALINE BIOTA There is concern that water withdrawals from the Keauhou aquifer for consumption and irrigation may, at some point in the future, cause an increase in the salinity of the anchialine pools and fishponds at the KAHO. These increases in salinity could have a negative impact on some of the aquatic resources at KAHO and elsewhere. After more than forty years of observations on salinity and anchialine biota along the Kona coast, Big Island residents should be aware of the following observations: Most Kona coast anchialine ponds have salinities in the range from 5 to 13 ppt (parts per thousand). For comparative purposes ocean salinity is 34 -35 ppt and freshwater is 0 ppt. 2. Most of the common aquatic native anchialine species (like opae'ula) are found in a wide range of salinities (from —1 ppt to —30 ppt). There are a few native species found in anchialine pools (like the orangeback damselfly and some emergent vegetation) that do not tolerate higher salinity water (above 8 ppt for the damselfly). However, all of these species are found in many other brackish water habitats in the Hawaiian Islands. 4. The rarest of the unusual anchialine shrimp species (6 -7 species) are found exclusively in higher salinity anchialine systems (usually above 15 ppt). Some of these species are known from one or two locations only in the Hawaiian Islands and are not found anywhere else. On the Kona coast, ponds with salinities greater than 15 ppt are relatively rare. Any increase in salinity of the Kona coast anchialine ponds would increase the available habitat for these rare species. 4.0 Literature Cited Standard Methods. 1999. Standard methods for the examination of water and wastewater. 20'" edition. American Health Assoc., Washington, D.C. Port City Press, Baltimore, Md. 1325 p. TABLE 1. Table of means for parameters measured over the 2005 through 2013 period in nine wells located in proximity to the mauka boundary of the Kohanaiki project site (n =290), in 16 anchialine pools (n =971) located makai of most of the development and at five marine shoreline stations (n =289) at Kohanaiki showing the decrease in mean parameter concentrations with proximity to the ocean. All parameter means are in ug/L unless otherwise shown, ppt = parts per thousand. SALINITY LOCATION NO3 NH4 TN PO4 TP (ppt) Mauka Wells (n =290) 1215 19 1952 95 156 7.779 Anch. Pools (n =971) 1077 42 2013 60 119 12.758 Shoreline (n =289) 45 4 173 8 16 33.948 6 TABLE 2. Results of the Wilcoxon 2- Sample Test examining the means of important nutrient parameters in the marine waters fronting the Kohanaiki project site in two time periods: Preconstruction (n -163) and During Construction (n= 2,160). The question being addressed is, "Are there any significant differences between the preconstruction means of parameters to those collected in the during construction time period ? ". All means are in ug/L unless otherwise noted, NTU Nephelometric Turbidity Units. During Preconstruction Construction Parameter Mean (n =163) Mean (n =2160) Significantly Different? Nitrate -N 11.38 10.38 YES (P <0.0001) Interpretation: During Construction means is significantly less Ammonia -N 2.43 3.22 YES (P <0.009) Interpretation: During Construction means is significantly greater Total -N 146.30 131.62 YES ( <0.0001) Interpretation: During Construction mean is significantly less Ortho -P 5.62 5.18 NO Interpretation: No significant differences Total -P 12.14 13.07 YES (P <0.0001) Interpretation: During Construction mean is significantly greater Si 399.42 248.21 NO Interpretation: No significant differences Salinity (ppt) 34.191 34.685 YES (13<0.0001) Interpretation: During Construction mean is significantly greater Turbidity (NTU) 0.08 0.11 YES (P <0.0001) Interpretation: During Construction mean is significantly greater VA TABLE 3. Results of the Wilcoxon 2- Sample Test examining the means of important nutrient parameters in the marine waters fronting the Control Sites (n= 1,764) and the Kohanaiki project site (n= 2,323) addressing the question, "Are there significant differences among the mean parameter concentrations for samples collected at control transects relative to those collected fronting the project site ? ". All means are in ug/L unless otherwise noted. Mean Kohanaiki Control Sites Transect Means Parameter (n =1764) (n =2323) Significantly Different? Nitrate -N 34.93 10.45 YES (P <0.0001) Interpretation: Control Site means are significantly greater Ammonia -N 6.00 3.16 YES (P <0.0001) Interpretation: Control Site means are significantly greater Total -N 164.20 132.65 YES (P <0.0001) Interpretation: Control Site means are significantly greater Ortho -P 8.97 5.21 YES (P <0.0001) Interpretation: Control Site means are significantly greater Total -P 17.40 13.00 YES (P <0.0001) Interpretation: Control Site means are significantly greater Si 955.60 258.82 YES (P <0.0001) Interpretation: Control Sit-. means are significantly greater Salinity (ppt) 33.698 34.651 YES (P <0.0001) Interpretation: Kohanaiki ' Transect mean are significantly greater Turbidity (NTU) 0.17 0.11 YES (P <0.0001) Interpretation: Control Site means are significantly greater 8 tl N' wa wa!011 8, p;h 7 18 Heau 2p b M 141 1 vVeRyDa-, 4 IN 0 Wag K61— Wall 200 wen )(02 Val V�13 Pia P141 VVMON K04 )PIOSIM P12 MO 1(D5 *wall Peg P82 KOP Wu'F 0, P72 POO 101 P40 VMl 302 -PP0 . Well 301 Wawahiw wo i-k P28 P13 YMIA02 7 `, a�'� S%WlAlOt- MIDO *1CIF) <' Vc*. Kaloko Pt FIGURE 1Map, of the Kohanaiki project site Showing on-site sample locations, marine sample sites offshore 5'j. as well as for the marine control sites. \1\ Approximate scale I cm= 195m. I ' 'k ib k" IT o it o k a kdu� I B (�y m TIOr rn 5000 Z W 4000 C9 O 3000 Z 2000 Q of F- 1000 z 0 Al Well 200 P139 (Pi — — — — P141 (Pi — — • Station c i I \ DATE FIGURE 2. Plot of nitrate nitrogen from 2005 through June 2007 at four Kohanaiki sites: Well 200, Pond 139, Pond 141 and shoreline (site 9). 10 rn 100 2 U) 60 O T- 11_ O f- OC 20 O 1 1 DATE Well 200 P139 (Pond) - - - - -- P141 (Pond) — Station 9 (Marine) FIGURE 3. Plot of orthophosphorous from 2005 through June 2007 at four Kohanaiki sites: Well 200, Pond 139, Pond 141 and shoreline (site 9). 11 800( 6000 rn Z W 0 400C O W H z N 200C z Well 200 PI39(Pond) - - - - -- P141 (Pond) — — — Station 9 (Marine) I �: II ` Il ' •1 1 I l 1 I 11 _ l• l I 1 •[- FIGURE 4. Plot of nitrate nitrogen from 2005 to present at four Kohanaiki sites; Well 200, P -139, P-141 and shoreline (site 9). Note the variability in Welt 200 decreases once water withdrawals for ir- rigation commence (December 2008). Two closest irrigation wells are about 55 and 130 m away from monitoring Well 200. 12 200 180 160 140 Q 120 a 100 U) O 80 Z 60 O 40 20 a Well 200 P138(Pond) - - - - -- P141 (Pond) — — Station 9 (Marine) TN yl t j\+ Vt /�I 1 ll 1 til APR06 A4M APR07 APR08 AP6 APR10 APR11 APR12 APR13 APR14 FIGURE & Plot of orthophosphorous from 2005 to present at four Kchanaiki sample sites: Well 200, Pond 139, Pond 141 and shoreline (site 9). Unlike nitrate nitrogen, variability with orthophos- phorous does not appear to be af%cted by the operation of nearby irrigation wells. 13 0U W S 40 00 Z W a O f— Z W Q Of H Z Z 'tt d 30 00 20 10 � rn 0 0 v O 00 1 APROS APROB APR07 VMS AP AM APR10 APR11 AP 12 APR13 APR14 DATE FIGURE 6. Plot of mean nitrate nitrogen by date in all sampled anchialine pools at Kohanaiki from 2005 to present (n=934). Also shown are the start of golf course construction (June 2007) and the completion of golf course "grow -in" in October 2009. 14 7 O a v7 O Q- 0 t- o! O t 100 60 Eja 20 ti o 0 0 = U O P 0 APRO$ AP 07 A 08 A 09 APR10 AP 11 AP 12 APR13 AP 14 DATE FIGURE 7. Plot of mean orthophosphorous by date in all sampled anchialine pools at Kohanaiiki from 2005 to present (n =934). Also shown are the start of golf course construction (June 2007) and the completion of the golf course "grow-in" in October 2009. Note that golf course construction and "grow -in" do not appear to influence the variability in orthophosphorous concentrations due to its affinity to bind with soil. 15 2' IT 21 C) 11 ti � 11 a CO 1 H O 1, a1" i Z L 2 DATE FIGURE 8. Plot of mean opaeN la shrimp counts by date in anchialine pools at Kobanaiki from 2005 through 2013. Also shown is the fitted regression line to those data having almost no slope (b= - 0.00097) that does not differ significantly from zero indicating no significant change has occurred in shrimp abundance albeit the fit of the line is poor (r= 0.03). 16 i � i • k •• • • IDS jPW • APR05 APR08 APR07 AAA APR09 APR10 APR11 APR12 APR13 DATE FIGURE 8. Plot of mean opaeN la shrimp counts by date in anchialine pools at Kobanaiki from 2005 through 2013. Also shown is the fitted regression line to those data having almost no slope (b= - 0.00097) that does not differ significantly from zero indicating no significant change has occurred in shrimp abundance albeit the fit of the line is poor (r= 0.03). 16 EFFECTS OF GROUNDWATER ON FISHPONDS AND COASTAL OCEAN OF THE KALOKO- HONOKOHAU NATIONAL HISTORICAL PARK Prepared by: Dr Steve Dollar.. Ph.D. Coastal Zone & Coral Reef Specialist Marine Research Consultants, Inc. 1039 Waakaua PI Honolulu, Hawaii 96822 EFFECTS OF GROUNDWATER ON FISHPONDS AND COASTAL OCEAN OF THE KALOKO - HONOKOHAU NATIONAL HISTORICAL PARK Prepared for: Hawai' I Island Economic Development Board Prepared by: Marine Research Consultants, Inc. 1039 Waakaua PI Honolulu, HI 96822 July 2014 EXECUTIVE SUMMARY This report has been prepared in response to a petition by the National Park Service (NPS) to the State Commission on Water Resource Management to designate the Keauhou Aquifer as a Groundwater Management Area. The petition asserts that present or planned future use of groundwater from the Keauhou Aquifer will reduce the flow of basal groundwater through Kaloko Honokohau (KAHO) National Historical Park, thereby causing harm to KAHO's anchialine ponds and its nearshore marine environment. This report summarizes data collected by Marine Research Consultants, Inc. during four field surveys between 2000 -2012 for the purpose of evaluating the composition of waters within two large fishponds within KAHO(Aimakapa and Kaloko) and the coastal ocean offshore of these fishponds, with particular emphasis on evaluating the contribution and fate of groundwater input. In the earlier studies (2000, 2007) Aimakapa Pond exhibited little vertical and horizontal stratification, appearing as a uniformly well -mixed system with long residence time. These conditions were characterized by near complete uptake of all inorganic nutrients entering the ponds through groundwater flux, and elevated values of organic nutrients that are the product of decomposition of organic material. This condition indicated the pond was progressing toward a terminal successional stage where the pond becomes a sediment - filled wetland. More recent studies in 2012 reveal consistent input of groundwater along the landward shoreline of the pond, resulting in steep gradients of salinity and inorganic nutrients found in groundwater. These results suggest that there has not been a detectable decrease in basal groundwater to the ponds; in fact the opposite appears to be the case. While the differences in groundwater dynamics within the ponds over the 12 -year interval of studies may reflect the relationship between sampling and tidal state, results of these studies indicate that at a minimum the fishponds are not in a cycle of uninterrupted progression toward a more senescent state. Scaling nutrients concentrations to salinity indicate that there are no nutrient subsidies to the ponds from sources other than naturally occurring groundwater. None of the data scaling inorganic nutrients to salinity within the ponds or nearshore ocean indicate substantial nutrient subsidies to groundwater that could be a result of human activities in upland areas. These results indicate that under the present scenario, the existing development upslope of KAHO is not causing detectable input of nutrient subsidies, or reduction in groundwater flux to the ponds. Rather, recent conditions in the ponds appear to represent a more open system with respect to hydraulic and nutrient fluxes. KAHO POND /MARINE WATERS PAGE 1 IMPACT SUMMARY In a companion report TNWRE found no impacts to basal groundwater have been identified to date as a result cf high level groundwater pumpage. While it is not resolved whether high level groundwater actually drains into the nominally downgradient basal lens, evidence gathered to date suggests that at least some, if not most, of the high level groundwater actually flows at depth beneath the basal lens to discharge into the marine environment offshore. If leakage of high level groundwater into the basal lens is limited to the modest amounts that evidence collected to date suggests, then the foreseeable future increases in pumpage of high level groundwater will have little or no impact on the basal lens. If indeed pumping of high level groundwater has minimal effects on basal groundwater, then it is clear that pumping high level groundwater will also have no effect on nearshore processes influenced by basal groundwater. The results summarized in this report correspond to such a conclusion, as no negative impacts were detected in nutrient dynamics of the KAHO fishponds over the last 12 years. KAHO POND /MARINE WATERS PAGE 2 IMPACT SUMMARY 1. PURPOSE This report has been prepared in response to a petition by the National Park Service (NPS) to the State Commission on Water Resource Management to designate the Keauhou Aquifer as a Groundwater Management Area. The petition asserts that present or planned future use of groundwater from the Keauhou Aquifer will reduce the flow of basal groundwater through Kaloko Honokohau (KAHO) National Historical Park, thereby causing harm to KAHO's anchialine ponds and its nearshore marine environment. This report contains data collected by Marine Research Consultants, Inc. during four field surveys between 2000 and 2012 for the purpose of evaluating the composition of waters within two large fishponds (Aimakapa and Kaloko), as well as the coastal ocean, with particular emphasis on evaluating the contribution and fate of groundwater input. This report provides a summary of these data, and also presents an opinion as to the effects of potential alteration of groundwater fluxes on the condition of the fishponds and adjoining coastal ocean. Examination of the list of publications and studies provided by the NPS relating to KAHO does not include any materials that address these issues. Hence, the results and conclusions presented below provide the sole evaluation of the effects of groundwater input in the KAHO fishponds. 2. BACKGROUND The National Parks and Recreation Act of 1978 provided for the establishment of the Kaloko - Honokohau National Historical Park to preserve the integrity of the many archaeological features and fishponds found in the area. Kaloko Pond and Aimakapa Pond are large brackish bodies of water separated from the ocean by a man -made basaltic rock wall at Kaloko, and a sand beach berm at Aimakapa. The rock wall at Kaloko Pond has recently been reconstructed, and the new wall incorporates channels which afford a direct connection between the pond and ocean. Water in the ponds is brackish, consisting of a mixture of low salinity groundwater, and seawater. As a result, water chemistry in the ponds can potentially be influenced by changes in groundwater composition and runoff of surface water. Leaching of materials such as fertilizer nutrients, pest control agents or other materials originating from anthropogenic activities to groundwater could potentially alter pond water chemistry. In addition, as pond water exchanges with ocean water in the nearshore marine area, there is also potential for alteration of marine water chemistry owing to changes in groundwater composition. Such alterations in water chemistry can, in turn, provide the potential to affect the structure of marine biotic communities in the nearshore area. KAHO FISHPOND -OCEAN PAGE 3 SUMMARY of GROUNDWATER IMPACTS In 2000, 2007 and 2012 Marine Research Consultants, Inc. had the opportunity to conduct investigations of these systems as part of the planning process for several different proposed upland development projects. All of these studies used identical methodologies allowing the resulting data to serve as a time - course analysis to determine how water chemistry has changed over the 12 -year period. During this time, upland development proceeded. Thus, the time - course analysis can serve as a tool for evaluating the effects of existing land development makai of KAHO on the functional aspects of the fishponds. Based on these changes in the past, it is possible to predict the potential future effects to the composition of the marine and pond environments. Of particular interest is assessing the nutrient dynamics and associated metabolic activity of the Aimakapa Pond. As this pond is essentially sealed from direct contact with the ocean, the metabolic function of the pond is directly linked to groundwater flux and composition. As a result, Aimakapa Pond is the area with the most potential for changes associated with alteration of groundwater from activities upslope of KAHO. 3. METHODS Water sampling protocols consisted of collecting surface and bottom water along transects through the center of fishponds from the most landward edges to the most seaward edges. Sampling was continued in the nearshore ocean from the shoreline adjacent to the ponds to a distance offshore considered to be beyond the major influences of land. Constituents measured included all listed in Chapter 11 -54, Hawaii Administrative Rules, Water Quality Standards, Department of Health, State of Hawaii. These constituents included various forms of dissolved nutrients (nitrogen and phosphorus), chlorophyll a (C'hl a), turbidity, dissolved oxygen, pH and salinity. Evaluation of the marine biological community was conducted by qualitative reconnaissance surveys along the length of the area comprising the marine portion of the Kaloko - Honokohau Nalional Historical Park from the shoreline out to the 10 meters (30 feet) depth contour. Information gathered during the surveys included abundance estimates of the dominant flora and fauna, as well as observations on the factors that affect these biotic assemblages. 4. RESULTS Concentrations of twelve chemical constituents in surface and bottom water samples from Kaloko and Airrakapa Ponds and the offshore ocean from the four survey years are plotted as functions of distance from the shorelines in Figures 2 -9. These plots show several major patterns of horizontal stratification of water chemistry constituents in the ponds and ocean. One of the most obvious differences is the KAHO FISHPOND -OCEAN PAGE 4 SUMMARY of GROUNDWATER IMPACTS dissimilarity between patterns in Aimakapa and Kaloko Ponds and the ocean. Aimakapa pond is separated from the ocean by a fairly wide ( -20 m) continuous sand berm which is not very permeable to exchange between the pond and the ocean. Such impermeability is apparent in the sharp, nearly vertical gradients at the shoreline of many of the water chemistry constituents shown in Figures 2 -9. Compared to the sand berm bounding Aimakapa Pond, the rock wall that separates Kaloko Pond from the ocean is highly permeable, and exchange of water between the ocean and pond is enhanced by flushing channels (makahas) constructed into the wall. Hence, the gradation in the water chemistry constituents between pond and ocean are less distinct in Kaloko compared to Aimakapa Pond, and the gradients within Kaloko Pond are more continuous between pond and ocean compared to Aimakapa (Figures 2 -9). It should be noted that these direct connections between the pond and ocean eliminate Kaloko Pond from the designation of "anchialine" which requires that no such connections exist. While both ponds contain thick sediment bottoms, there is a substantial difference in the quality of the sediment. Bottom composition of Aimakapa Pond consists of soft flocculent silty mud that is easily penetrable for at least one meter. Bottom composition of Kaloko Pond is a hard sand /mud mixture that is largely covered with marine algae, primarily the introduced species Acanthophora specifera. Sand /mud bottoms in both ponds were distinctly anaerobic beneath the surface layer as evidenced by the strong odor of H2S when the bottom was even slightly disturbed. 4.1 Patterns of Salinity in the Ponds and Ocean During all sampling events, salinity within the two ponds showed very different patterns of horizontal gradations from the ocean to the shoreward sides of the ponds (Figure 2). In Aimakapa Pond, average salinity during the four surveys was 12.64 +0.43 %o (part per thousand). These data indicate that the water in the pond consists of about 36% groundwater and 64% ocean water. In addition, salinity in Aimakapa is remarkable constant over the entire area of the entire pond as well as through the water column. In addition, salinity was nearly constant over the 12 -year interval of sampling. There is however, a slight trend of freshening over time, with the 2012 samples exhibiting the lowest salinities. The constancy of salinity through both time and space in Aimakapa Pond is clearly evident in Figure 2. The overall pattern of salinity in Kaloko Pond was substantially different than in Aimakapa. Average salinity in the fishpond during the four increments of sampling 24.81 %o± 6.11. As Kaloko Pond is "connected" to the ocean, the variability in salinity is a result of sampling at various stages of tide, and is also likely a response to the various stages of construction of the rock wall separating the pond from the ocean. As can be seen in Figure 2, all of the samplings of Kaloko Pond exhibited a pattern of KAHO FISHPOND OCEAN PAGE 5 SUMMARY of GROUNDWATER IMPACTS increasing salinity with decreasing distance from the shoreline, indicating gradient of mixing between seawater and groundwater. The overall patterns of salinity, with the lowest values in 2007 and the highest in 2000 do not suggest any consistent pattern with respect to time as a function of groundwater input into the pond. Comparing values of salinity within Aimakapa Pond to salinities of anchialine pools located in KAHO indicate that salinity in the fishpond is within the range of salinity in water in three representative pools water (8- 14%o), while the salinity in Kaloko Pond is substantially higher than anchialine pools (Table 1). These comparisons again point to the open circulation between Kaloko Pond and the ocean. Nearshore ocean waters in West Hawaii are typified by a pattern of decreasing salinity with distance from shore. This gradient is indicative of low salinity groundwater entering the ocean near the shoreline and mixing with high salinity ocean water. While this was the general pattern observed on the KAHO transect sites in 2007 and 2012, a somewhat unusual result in the 2000 data is that the lowest salinities in the ocean samples were not found nearest to the shoreline off of either fishpond. Rather, the lowest salinities were measured in surface ocean samples approximately 25 -50 m offshore (Figure 2). Such a result suggests that the majority of groundwater flow to the ocean may be around the pond boundaries, rather than through the shoreline barriers that separate the ponds from the ocean. Horizontal and vertical stratification of salinity in the ocean samples was evident at all stations during all surveys. Beyond 25 -50 m from shore, with increasing distance from shore, salinity increased at all stations in both surface and bottom water, while at all sampling stations, surface salinity was lower than the corresponding bottom sample. These gradients indicate that mixing of groundwater entering the ocean does not completely homogenize the water column, with a surface layer of lower salinity water overlying a water column of ocean water. 4.2 Patterns of Nutrients in the Ponds and Ocean As with salinity, the patterns o-f dissolved nutrients vary considerably between ponds. The patterns prescribed by the concentrations of dissolved Silica (Si) on transects are essentially a mirror image of salinity during all surveys (Figure 3). These mirror image patterns reflect the two orders of magnitude difference in concentrations of Si between groundwater and ocean water. In addition, the mirror image of Si and salinity indicates that Si is a "conservative" tracer, in that it is not utilized to any measurable extent by biotic or chemical reactions within the ponds and ocean. As a result, there is the same large variation in patterns of concentration of Si between the ponds, and same degree of stratification of Si as was evident in salinity. KAHO FISHPOND -OCEAN PAGE 6 SUMMARY of GROUNDWATER IMPACTS In addition to Si, the other nutrient found in high concentrations in groundwater relative to ocean water is nitrate nitrogen (NO3-). While the concentrations of NO3 in the 2000 and 2007 surveys were consistently low (below 0.5 pM) across the entire sampling transect, substantially different patterns occurred in both 2012 surveys (Figure 4). During the two most recent surveys, concentrations of NOT at the inshore end of the pond exhibited peak values with rapidly decreasing concentrations to the center region of the pond (Figure 4). The magnitude of the gradients was different between the February and November 2012 surveys, with peak values of about 13 NM in February and 50 pM in November. However, the location in the pond where the concentrations dropped to previously measured levels of NO3 of less than 1 pM occurred at nearly the same place during both surveys (- 150 m from the shoreline). The pattern of the other major inorganic nutrient, phosphate phosphorus (P043 -) exhibits a similar pattern, with highest values at the shoreward edge of Aimakapa Pond wand sharply decreasing values up to the center of the pond (Figure 5). These steep horizontal gradients of NO3 and P043-, as well as depressed salinity, suggest the possibility of a qualitatively different level of groundwater input at the mauka shoreline of Aimakapa Pond in 2012 relative to past surveys. While these changes between years may be result of an increase in the overall magnitude of groundwater flux into the ponds (although not likely), it is more likely that influx varies as a result of water level in the ponds. It has been shown that Aimakapa Pond responds to tidal fluctuations (damped relative to the ocean cycle in both magnitude and time) which push pond water inland during flood tides and draw groundwater into the ponds during ebbing tidal cycles (Tom Nance, personal communication). As pond salinity was higher in 2000 and 2007 relative to 2012 (Figure 7), the distinct differences in nutrient gradients between these years may be a reflection of when samples were collected relative to tidal state. However, while there is a distinctly higher input flux of NO3- and P043- along the mauka shoreline of Aimakapa during 2012, the incoming inorganic plant nutrients are almost completely taken up within the shoreward half of the pond (Figure 4). In sum, there are no indications of reduction of groundwater flux into Aimakapa Pond over the last 12 years, and in fact the opposite appears true. Kaloko Pond also shows distinct gradients of NO3 and P043 , with an overall similar pattern to Aimakapa Pond. While the peak values of NO3 occurred in 2012 in Aimakapa, the peaks in Kaloko occurred in 2007 corresponding to minimum values of salinity (Figures 4 and 5. In contrast to the steeply declining concentrations of NO3 down to very low values before the center of Aimakapa Pond, gradients were less steep and extended further toward the ocean end of Kaloko Pond. Gradients of other forms of nitrogen and phosphorus show distinctly different patterns of distributions than NO3- and P043-, particularly in Aimakapa Pond. During all four of the sampling events, total nitrogen (TN) is relatively constant across the entirety of KAHO FISHPOND -OCEAN PAGE 7 SUMMARY of GROUNDWATER IMPACTS Aimakapa Pond. The majority on TN exists as total organic nitrogen (TON) (Figure 7), rather than either NO3- or ammonium (NHa +) (Figure b). In the 2012 surveys, concentrations of TON mirror 1403 with lowest values at the inshore end of the pond, and elevated values in the seaward portion of the pond. In particular, during the November 2012 survey, the sharp elevation in concentrations of TON occur at the sampling station approximately 150 m from the shoreline, which is the same location that concentrations of NOT dropped to low values. The same patterns are evident for total phosphorus (TP) and total organic phosphorus (TOP) (Figure 8). Total organic nitrogen and phosphorus are the end products of decomposition of organic material, while the inorganic nutrients NOT and P043 -, as well as NHa+ are the nutrients taken up by plants during photosynthetic activity. The considerably different patterns of distributions of these nutrient components in Aimakapa Pond over the last 12 years suggest a shift in metabolic function over time. During the earliest survey in 2000, virtually all of the nitrogetn and phosphorus in Aimakapa Pond was in the form an organic form (TON, TOP), with essentially no NOT and P043- present. Such a distribution indicates that the pond was in a decaying state, proceeding toward anoxic conditions. During both 2012 surveys, the metabolic functioning of Aimakapa appears to have shifted toward a more "open" system. High input of low salinity water containing high concentrations of inorganic nutrients found in groundwater is evident along the inland shoreline of the pond. These concentrations decrease with distance seaward until the approximate center of the pond, where concentrations approach the levels found in 2000. TON mirrors the pattern of nutrients indicating gradients of progressive uptake and metabolic processes from the mauka edge toward the center of the pond. Hence, the recent data showing steep gradients of nutrients within Aimakapa Pond indicate that the entire :system has not remained a completely heterotrophic system removing nutrients from the water column, while adding back end products of metabolic decomposition. Rather, the apparent increase in groundwater now results in indications that at least part of the pond is a more open system with respect to metabolic cycling somewhat reversing he progression toward an anoxic system. It may be however, that the differences between nutrient gradients in different sampling years is a response to sampling during different phases of the tidal cycle, with nutrient fluxes into the pond more pronounced during ebbing tides. In any case, the time - course evaluation indicates that there is not a progressing decomposition of the ponds during the 12 -year interval of sampling. Plots of Chlorophyll a reveal substantially elevated values throughout the water column in Aimakapo in 2000 (Figure 9). The close tracking of Chl a and turbidity in this survey indicates that the high values are not the result of resuspension of bottom sediment. Chlorophyll a and turbidity are also elevated in surface and bottom waters KAHO FISHPOND -OCEAN PAGE S SUMMARY of GROUNDWATER IMPACTS of Kaloko Pond relative to ocean water, but without the anomalous values in bottom water during 2000 (Figure 9). 4.3 Conservative Mixing Analysis A useful treatment of water chemistry data for interpreting the extent of material input from land is application of a hydrographic mixing model. In the simplest form, such a model consists of plotting the concentration of a dissolved chemical species as a function of salinity. Comparison of the curves produced by such plots with conservative mixing lines provides an indication of the origin and fate of the material in question. Figures 10 -12 show plots of concentrations of nutrient constituents as functions of salinity for Aimakapa and Kaloko ponds, anchialine pools and ocean water samples collected in the KAHO during the four sampling surveys in 2000, 2007 and 2012. In addition, nutrient concentrations and salinity from data collected in three monitoring wells within the KAHO boundaries are also shown. Each plot in Figures 10 -12 also show two conservative mixing lines that were constructed by connecting the end member concentrations of open ocean water and averaged high -level groundwater concentrations from the DWS Honokohau Well (4158 -03), and averaged basal groundwater Kaloko Irrigation Well (4160 -02) (Well data provided by TNWRE). If the parameter in question displays purely conservative behavior (no input or removal from any process other than physical mixing), data points should fall on, or very near, the conservative mixing line. If, however, external material is added to the system through processes such as leaching of fertilizer nutrients to groundwater, data points will fall above the mixing line. If material is being removed from the system by processes such as uptake by biotic metabolic processes, data points will fall below the mixing line. It is also important to note that since nutrient concentrations are scaled to salinity, the effects of tidal state are not a factor in interpreting data on source or sinks. Dissolved Si represents a check on the model as this material is present in high concentration in groundwater, but is not a major component of fertilizer. In addition, Si is not utilized rapidly within the nearshore environment by biological processes. It can be seen in Figure 10 that all of the data points from Aimakapa and Kaloko Ponds, the three anchialine pools, and the ocean fall very close to the conservative mixing line for Si. Such agreement indicates that the end members used to construct the lines are representative of the system. The only data set that deviates from the linear pattern falling near the conservative mixing lines is for Monitoring Well 1, with anomalously low values in samples collected in 2000 and 2001. The lack of curvature in the linear arrays of data points also indicate that there is no detectable uptake of KAHO FISHPOND -OCEAN PAGE 9 SUMMARY of GROUNDWATER IMPACTS Si within the pond and marine system, and no other sources of Si other than groundwater. The plot of NO3 versus salinity reveals distinctly different results than plot of Si (Figure 10). Plots of concentrations of NO3 versus salinity in Aimakapa Pond show a distinct nearly vertical line extending from the point of intersection with the mixing line (data from November 2012) to the X -axis with a NOT concentration of essentially zero. This linear array illustrates the process described in the section above where groundwater containing high levels of NO3- relative to seawater enters Aimakapa Pond at the mauka shoreline. With mixing of the groundwater into the pond, NO3 is rapidly stripped by biotic uptake. The orientation of data points from both of the surveys in 2012 along the same linear array suggests the same degree of removal of nutrients relative to salinity is occurring within the pond. The arrays of NO3 data points for Kaloko Pond are substantially different than for Aimakapa (Figure 10). At the low salinity end of the plots, at salinities less than 15 700, all data points fall on the conservative mixing lines, indicating that concentrations in the pond at these sampling points consists exclusively of mixing of groundwater and ocean water. At salinities higher than 15 %o, data points all lie beneath the mixing lines, with concentrations of N 03 decreasing steadily to very low values to a salinity of approximately 30 %o. These patterns delineate uptake of NOT by biotic processes within the main body of Kaloko Pond. As with the smooth linear array of data points of decreasing value with increasing salinity in Aimakapa, the relatively smooth curve prescribed by the data points in Kaloko indicate that there are no other sources or sinks of NOT within the pond. Salinities above about 30 %o represent samples from the nearshore ocean, which show a slight increase in concentration relative to pond waters. Such an increase suggests that groundwater may be entering the ocean from other entry points than through the ponds. Concentrations of NO3- in the anchialine pools scaled to salinity lie on, or slightly above the conservative mixing lines. The position of these points indicates that the same processes of NO3- uptake occurring in the two large fishponds is not occurring in the anchialine pools. Rather, groundwater nutrients remain in essentially the same concentration while in the anchialine pool as in the submarine aquifer. Such a difference in nutrient cycling in the smaller anchialine pools relative to the fishponds is a result of far more rapid flushing and turnover rate of water in the pools. Concentrations of NOT in monitoring wells are generally above the conservative mixing lines, suggesting an external source of NO3 other than naturally occurring groundwater. Phosphate phosphorus (P043 -1 is also a major component of fertilizer and sewage effluent, but is usually not found to leach to groundwater to the extent of NOT, owing to a high absorptive affinity of phosphorus in soils. The curves defined by the plotted data of P043- as a function of salinity are similar to NO3 although the concentrations KAHO FISHPOND -OCEAN PAGE 10 SUMMARY of GROUNDWATER IMPACTS differ by an order of magnitude (Figure 11). In addition, data points from the shoreward end of Aimakapa Pond occur above the mixing lines, indicating a source Of P043- that is not completely naturally occurring groundwater. However, the near - vertical linear array of data points indicates rapid uptake of POa 3- beyond the shoreward edge of the pond. The distribution of data points in Kaloko Pond also reflects mixing of groundwater and ocean water along with uptake by biotic activity within the pond, although the magnitude of uptake is less than in Aimakapa Pond (Figure 11). Concentrations of POa 3 scaled to salinity in the anchialine pools all fall near the conservative mixing lines indicating that there are no external sources of POa 3- to the anchialine pools from sources other than naturally occurring groundwater. Similar to anchialine pools, the scaled concentrations of POa 3 for monitoring wells 2 and 3 fall on the conservative mixing lines, while most data points for well 1 lies below the mixing lines. The other form of dissolved inorganic nitrogen, NHa +, shows a reversed pattern of distribution relative to conservative mixing lines when concentrations are plotted as functions of salinity. It can be seen in Figure 11 that the conservative mixing lines are nearly flat with nearly similar concentrations in groundwater and ocean water. The occurrence of nearly all of the data points from all water sources lying above the mixing lines indicates that the observed concentrations of NHa+ are not a result of mixing of groundwater and ocean water. Rather, these concentrations are the result of either input from another source, or as is more likely the case, from in -situ metabolic processes within the ponds. Because total organic nitrogen and phosphorus (TON and TOP) occur in very low concentrations in both open ocean water and high level groundwater, the mixing lines for these constituents are essentially flat (Figure 12). The occurrence of data points of TOP and TON far above the mixing lines reflects the metabolic cycling conversion of inorganic nutrients to organic nutrients by metabolic cycling of nutrients in the Aimakapa Pond ecosystem. Products of metabolic decomposition of organic material include organic nitrogen (TON) and organic phosphorus (TOP). Owing to low circulation and flushing of the majority of Aimakapa Pond, and no apparent uptake by biotic function, these organic nutrients remain in the water column. Contrary to Aimakapa Pond, the data points of TOP and TON in Kaloko versus salinity fall near the mixing lines, indicating that the level of organic decomposition and /or flushing of the pond is not occurring. Within the anchialine pools and monitoring wells, TON and TOP occur at very low levels, supporting the observation that rapid water exchange through the pools and wells prevents accumulation of the products of organic metabolism. Two major points can be made to summarize the results of the mixing analyses. First, and most importantly, there are no indications of significant input to any of the ponds of inorganic nutrients from sources other than naturally occurring groundwater. None KAHO FISHPOND -OCEAN PAGE 11 SUMMARY of GROUNDWATER IMPACTS of the data points scaling inorganic nutrients to salinity within the ponds or nearshore ocean indicate substantial nutrient subsidies to groundwater that could be a result of human activities in upland areas. The constituents that show substantial elevations in the ponds (NH4 +, TON and TOP) are not the direct result of nutrient loading, but rather byproducts of metabolic cycling coupled with long residence time (slow water exchange) within the ponds. The second major point that is illustrated by the nutrient data and mixing plots is that during the most recent samplings in 2012 Aimakapa Pond exhibited a far more detectable pattern of active groundwater flux than in previous surveys. At the inland shoreline of the pond, input of low salinity, high nutrient groundwater was clearly evident during both of the 2012 surveys. Such input was not present in earlier surveys utilizing identical sampling mE4hods. While the nutrient inputs were rapidly taken up within the shoreward half of the pond, the input of groundwater suggests a more active circulation than in the ipast. While the process responsible for these differences in input over a decadal period are not readily decipherable, it is clear that there is no indication of increased senescence of Aimakapa Pond. Rather, these data indicate that the pond may be stabilizng the trend of tending toward a system completely dominated by decomposition and infilling of sediment. While not included in the present data presentation, past investigations of the KAHO area have included comparisons of the nutrient dynamics occurring in the fishponds to the effects of discharges o" water from the Natural Energy Laboratory of Hawaii at Keahole Point. These comparisons indicate that subsidies to groundwater of NOT and PO4 -3 are far greater at NELHA than in the Kaloko- Honokohau area as a result of high concentrations in deep seawater that is discharged into disposal trenches along the shoreline. 4.4 Effects to the Nearshore Marine Environment Coral reef ecosystems have adapted to grow in low nutrient marine waters. So a reduction in flux of nutrients through reduced groundwater flux will have no effect on offshore marine systems. Even if changes in groundwater flux results in an increase in nutrients, it is also unlikely that there would be any effects to the nearshore marine environment. Data reveal that groundwater nutrients were retained within a surface layer, with no exposure to the benthos. Circulation within the area is rapid enough to prevent phytoplankton blooms. These results indicated that even with long -term input of high nutrient subsidies, there are no negative effects to the receiving environment. 5. DISCUSSION and CONCLUSIONS The purpose of this data review is to provide the information to make valid estimates of the potential for impact to the marine and pond environments at Kaloko KAHO FISHPOND -OCEAN PAGE 12 SUMMARY of GROUNDWATER IMPACTS Honokohau National Historical Park, and possibly NELHA, from upland development involving increased use of potable basal groundwater. To summarize, it is generally accepted that one of the large fishponds within the Kaloko - Honokohau National Historical Park function in a similar manner to smaller anchialine ponds that occur on the west coast of Hawaii. By definition anchialine ponds are surface exposures of the water table with no direct connection to the ocean that contain brackish water which is a mixture of seaward flowing groundwater and landward flowing seawater. Anchialine ponds in early successional stages usually have sediment -free bottoms which allow for relatively rapid exchange of water. It is important to note that healthy anchialine ponds are NOT nutrient limited systems, and contain high concentrations of plant nutrients. The excess nutrients do not lead to algal dominated water columns (at least until late stages of pond senescence, as a result of a balance between short residence time of water within the ponds, and production and consumption by pond biota. Rapid flux of water through the ponds, and grazing by resident populations prevent plankton buildup within the water column. In the later stages of the anchialine pond cycle, infilling by sediment reduces the rate of water exchange and the balance between production and consumption is lost. Ultimately, in the last stages of pond senescence infilling is complete and ponds transition to wetlands. During surveys of Aimakapa Pond conducted in 2000 and 2007 restricted groundwater flow into Aimakapa Pond was borne out by the near complete lack of both vertical and horizontal gradients within the ponds. Such lack of detectable inputs suggested that the pond is essentially a closed system which was accumulating sediment and metabolic decay products which cannot be naturally flushed from the enclosed pond basin. Continued metabolic activity would produce increasing sediment deposition which would elevate rates of nutrient release from sediment decomposition, which would in turn allow for increased phytoplankton growth. During surveys in 2012, evidence of groundwater input at stations within the inshore half of Aimakapa Pond was detected as steep horizontal gradients of salinity and inorganic nutrients found in groundwater. These results suggest that Aimakapa Pond may be experiencing either increased groundwater input, or at least not a decrease in groundwater input relative to a decade earlier. As the existing developments in the areas upslope of the KAHO ponds have been in place for the last decade, water quality in the ponds changes can be assumed to be influenced by the present level of development upslope from the KAHO ponds. In a companion report TNWRE found no impacts to basal groundwater have been identified to date as a result of high level groundwater pumpage. A key unresolved issue is whether or not the high level groundwater actually drains into the nominally downgradient basal lens in the area between Keahole Point and Kailua Town. KAHO FISHPOND -OCEAN PAGE 13 SUMMARY of GROUNDWATER IMPACTS Evidence gathered to date suggests that at least some, if not most, of the high level groundwater actually flows at depth beneath the basal lens to discharge into the marine environment offshore. If leakage of high level groundwater into the basal lens is limited to the modest amounts that evidence collected to date suggests, then the foreseeable future increases in pumpage of high level groundwater will have little or no impact on the basal lens. If indeed pumping of high level groundwater has minimal effects to basal groundwater, it is clear that pumping high level groundwater will have no effect on nearshore processes influencE�d by basal groundwater. The results summarized in this report correspond to such a conclusion, as no negative impacts were detected in nutrient dynamics of the KAHO fishponds over the last 12 years. In fact, time - course data indicate a potential revE >rsal of pond metabolism toward a less senescent stage. As this time period includes the addition of upslope development and pumpage of high level groundwater it can be concluded that these activities do not represent a negative influence, and there is no reason to expect this pattern to change in the future. KAHO FISHPOND -OCEAN PAGE 14 SUMMARY of GROUNDWATER IMPACTS fec'a 1000 S00 f°-' 1000 500 neteia FIGURE 1. Aerial images of Aimakapa (left) and Kaloko Fishponds at Kaloko - Honokohau National Historical Park on West Coast of the Island of Hawaii. Yellow lines in each photo represent sampling transects extending through the length of the ponds and into the coastal ocean. 35 30 A/MAKAPA Q POND 25 H z Q 20 W 15 OCEAN --l- FEB 2012 SURFACE -0- FEB 2012 BOTTOM - f-- 2007 SURFACE - E]- 2007 BOTTOM -4- 2000 SURFACE -0. 2000 BOTTOM -A NOV 2012 SURFACE - A- NOV 2012 BOTTOM 10 ' -300 -200 -100 0 100 200 300 400 500 M1 RGES Q. a 25 z -J 20 d W 15 KALE POh 00 00 -100 0 100 200 300 400 500 DISTANCE FROM SHORE (m) FIGURE 2. Plots of salinity in Aimakapa Pond (top) and Kaloko Pond (bottom) and adjacent offshore ocean as fur ctions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in February and November). Shoreline is represented by green vertical line; positive values indicate distance seaward from the shoreline in the ocean; negative values ridicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figures 1. 700-- -- 600 - -- 500 ANk 400 U 300 co 200 A/MAKAPA POND 100 0 a--- _ -200 -100 0 700 M 500 400 Q U 300 J_ U) 200 100 M KALOKO nntin 0- FEB 2012 SURFACE -0- FEB 2012 BOTTOM 2007 SURFACE E3- 2007 BOTTOM --*— 2000 SURFACE -e- 2000 BOTTOM --� NOV 2012 SURFACE - d- NOV 2012 BOTTOM r O - - - - - -- 100 200 300 400 500 -200 -100 0 100 200 300 400 500 DISTANCE FROM SHORE (m) FIGURE 3- Plots of silica in Aimakapa Pond (top) and Kaloko Pond (bottom) and adjacent ocean as functions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in february and november). The shoreline is represented by the green vertical line; positive values indicate distance seaward from the shoreline in the ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure 1 60 50 AIMAKAP'A �-. POND 1 40 - p- z -�- ' � Q W 30 ' -0 Q -p- ' - A 20 - A- NOV 2012 BOTTOM 10 O , 0 50 .1 30 W F- 20 Z 10 -200 -100 f ot- -200 0 100 OCEAN K1I11 -F FEB 2012 SURFACE - p- FEB 2012 BOTTOM -�- 2007 SURFACE - E} 2007 BOTTOM -0 2000 SURFACE -p- 2000 BOTTOM - A NOV 2012 SURFACE - A- NOV 2012 BOTTOM 300 400 500 -100 0 100 200 300 400 500 DISTANCE FROM SHORE (m) FIGURE 4. Plots of nitrate nitrogen in Aimaka a Pond (top) and Kaloko Pond (bottom) and adjacent ocean as functions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in February and November. The shoreline is represented by the green vertical line; positive values indicate distance seaward from the shoreline in this ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure 1. 5.0 4.5 4.0 3.5--- W 3.0 Q 2.5 2.0 O 1.5 0- 1.0 - 0.5 0.0 E, K11 W 3.0 CL 2.5 W Q 2.0 W 1.5 0 1.0 CL 0.5 0 0 -• ;A WO I 0i i0 i -9- FEB 2012 SURFACE - E} FEB 2012 BOTTOM f 2007 SURFACE - 0- 2007 BOTTOM --*- 2000 SURFACE -®- 2000 BOTTOM -A NOV 2012 SURFACE - �- NOV 2012 BOTTOM OCEAN 200 300 4100 500 -200 -100 0 100 200 300 400 500 DISTANCE FROM SHORE (m) FIGURE 5. Plots of phosphate phosphorus in Aimakapa Pond (top) and Kaloko Pond (bottom) and adjacent ocean as functions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in February and November). The shoreline is represented by the green vertical line; positive values indicate distance seaward from the shoreline in the ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure 1. Z3 10 g Z 6 O 2 2 4 Q 0q -!- FEB 2012 SURFACE -0- FEB 2012 BOTTOM --*-- 2007 SURFACE - 0- 2007 BOTTOM -�- 2000 SURFACE © A/MAKAPA 2000 BOTTOM 12 ;'; POND - a NOV 2012 BOTTOM 10 Z 8 , d ; � 6 d O 4 -- ------------ 2 v 0 - -- -200 -100 0 14-- _ - -- KALOKO 12 - POND o , ; Z3 10 g Z 6 O 2 2 4 Q 0q -!- FEB 2012 SURFACE -0- FEB 2012 BOTTOM --*-- 2007 SURFACE - 0- 2007 BOTTOM -�- 2000 SURFACE -B- 2000 BOTTOM -A NOV 2012 SURFACE - a NOV 2012 BOTTOM OCEAN 100 200 300 400 500 -.200 -100 0 100 200 300 400 DISTANCE FROM SHORE (m) FIGURE 6. Plots of ammonium nitrogen in Aimakapa Pond (top) and Kaloko Pond (bottom) as functions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in February and November). The shoreline is represented by the green vertical line-, positive values indicate distance seaward from the shoreline in the ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure1. 500 120 100 80 - z W 60 -- O J 40 O I— 20- 1 �i 30 z 20-- O J 0 10 I A/MAKAPA POND 11 11 1 e ° w L N :I -4110- FEB 2012 SURFACE - (} FEB 2012 BOTTOM f 2007 SURFACE - o- 2007 BOTTOM -4- 2000 SURFACE -Q- 2000 BOTTOM -A NOV 2012 SURFACE - &- NOV 2012 BOTTOM OCEAN low 1 100 200 300 400 500 100"! 4 P --W OCEAN JKALOKOPOND 0 -200 -100 0 100 200 300 400 DISTANCE FROM SHORE (m) FIGURE 7. Plots of Total Organic Nitrogen in Aimakapa Pond (top) and Kaloko Pond (bottom) and the adjacent ocean as functions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in February and November). The shoreline is represented by a green vertical line; positive values indicate distance seaward from the shoreline in the ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure 1. 500 �.d 1.6 , M! 1.2 o- 1.0 0.8 O Q 0.6 p 0.4 0.2- r _ -200 -100 0 KALOKO POND ; o Q ►, ©. rLl V L 41t � OCEAN T_ 100 200 -f- FEB 2012 SURFACE -0- FEB 2012 BOTTOM 2007 SURFACE - o- 2007 BOTTOM -♦- 2000 SURFACE - �- 2000 BOTTOM -+- NOV 2012 SURFACE - d- NOV 2012 BOTTOM 300 400 OCEAN ei -T T - - - , 7 . T T ---- -T i -.200 -100 0 100 200 300 400 500 DISTANCE FROM SHORE (m) FIGURE 8. Plots of Total Organic Phosphorus in Aimakapa Pond (top) and Kaloko Pond (bottom) and adjacent ocean as functions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in February and November. Shoreline is represented byy green vertical line; positive values indicate distance seaward from the shoreline in the ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure 1. g 7 AIMAKAPA 6 POND 5 [L 4 O J 3 �.d 1.6 , M! 1.2 o- 1.0 0.8 O Q 0.6 p 0.4 0.2- r _ -200 -100 0 KALOKO POND ; o Q ►, ©. rLl V L 41t � OCEAN T_ 100 200 -f- FEB 2012 SURFACE -0- FEB 2012 BOTTOM 2007 SURFACE - o- 2007 BOTTOM -♦- 2000 SURFACE - �- 2000 BOTTOM -+- NOV 2012 SURFACE - d- NOV 2012 BOTTOM 300 400 OCEAN ei -T T - - - , 7 . T T ---- -T i -.200 -100 0 100 200 300 400 500 DISTANCE FROM SHORE (m) FIGURE 8. Plots of Total Organic Phosphorus in Aimakapa Pond (top) and Kaloko Pond (bottom) and adjacent ocean as functions of distance from the shoreline measured in 2000, 2007 and 2012 (sampled in February and November. Shoreline is represented byy green vertical line; positive values indicate distance seaward from the shoreline in the ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure 1. 70- A/MAKAPA -- POND 60 50 J � , J 40 ' e , �- 30 ' O ' b O 20 - ' J 0 i U 10- 0-1 10 J m 8 ca 6 O 4 W O = 2 U X -200 -100 0 100 O KALOKO y% POND -f- FEB 2012 SURFACE -0- FEB 2012 BOTTOM -- m 2007 SURFACE - o- 2007 BOTTOM f 2000 SURFACE -®- 2000 BOTTOM NOV 2012 SURFACE - a NOV 2012 BOTTOM OCEAN 200 300 400 500 -200 -100 0 100 200 300 400 500 DISTANCE FROM SHORE (m) FIGURE 9. Plots of Chlorophyll a in Aimakapa Pond (top) and Kaloko Pond (bottom) as functions of distance from the shoreline measured in 001, 2007 and 2012 (sampled in February and November). The shoreline is represented by the green vertical lines; positive values indicate distance seaward from the shoreline in the ocean; negative values indicate distance inland from the shoreline in the ponds. For locations of sampling transects, see Figure 1.. 1 1 CC- I ON mac., 500 C �- 400 Q U J 300 _ 200 100 110 100 90 t 80 70 Z 60 w Q 50 40 z 30 20 10 0 o . E3 1 • EB AIMAKAPA 2012 ■ AIMAKAPA 2007 ♦ AIMAKAPA 2000 Q FEB KALOKO 2012 0 KALOKO 2007 0 KALOKO 2000 A NOV AIMAKAPA 2012 NOV KALOKO 2012 ♦ ANCHIALINE POOLS 2012 Q MONITORING WELL 1 Q MONITORING WELL 2 0 O 5 10 15 20 25 30 35 5 10 15 20 25 30 35 SALINITY (ppt) FIGURE 10. Mixing plots showing Silica (top) and nitrate nitrogen as functions of salinity in Aimakapa and Kaloko Fishponds, anchialine pools and the adjacent ocean during four sampling periods (2000, 200i', Feb. 2012 and Nov. 2012). Also shown are data from three KAHpO Monitoring wells. Solid line is conservative mixing line connecting endpoint concen- trations from the open ocean and high level groundwater from the DWS Honokohau Well (4158 -03), while dashed line is conservative mixing line connecting open ocean concen- trations to basal groundwater sampled from the Kaloko Irrigation Well (4160 -02). 5.5 5.0 4.5 4.0 3.5 H 3.0 r 2.5 2.0 0 1.5 o- 1.0 0.5 0.0 • FEB AIMAKAPA 2012 ■ AIMAKAPA 2007 ♦ AIMAKAPA 2000 O 0 FEB KALOKO 2012 O KALOKO 2007 0 KALOKO 2000 • NOV AIMAKAPA 2012 A NOV KALOKO 2012 ♦ ANCHIALINE POOLS 2012 0 0 A`` Q 0 MONITORING WELL 1 Q` 0 MONITORING WELL 2 00 t13 1 0 CAM O 5 10 15 20 25 30 35 10 A O � A&N AA E3 � $ D Z 6 � O ♦ p Z) O V 13 13 O 4 � O 0 O a 2 0 0° o� oo C9 O E3 111711 o 0 5 10 15 20 25 30 35 SALINITY (ppt) FIGURE 11. Mixing plots showing Phosphate phosphorus (top) and Ammonium nitrogen as functions of salinity in Almakapa and Kaloko Fishponds, anchialine pools wells and the adjacent ocean during four sampling periods (2000, 2007, Feb. 2012 and Nov. 2012). Also shown are data from KAHO monitoring wells. Solid line is conservative mixing line connecting endpoint concentrations from the open ocean and high level groundwater from the DWS Honokohau Well (4158 -03), while dashed line is conservative mixing line connecting open ocean concentrations to basal groundwater sampled from the Kaloko IrrigationWell (4160 -02). doff, 180 G 160 Z 140 U 120 Z 100 80 Q 60 40 O ~ 20 X 20 CL 15 U_ Z � 10 W O J H 5 O Cpl �r i 0 A, • AIMAKAPA 2012 ■ AIMAKAPA 2007 ♦ AIMAKAPA 2000 Q KALOKO 2012 O KALOKO 2007 Q KALOKO 2000 • NOV AIMAKAPA 2012 • NOV KALOKO 2012 ANCHIALINE POOLS 2012 Q MONITORING WELL 1 Q MONITORING WELL 2 ■ ■, ■ AL _ ��_••J� AL 5 10 15 20 25 30 35 5 10 15 20 25 30 35 SALINITY (ppt) FIGURE 12. Mixing plots showing Total Organic Nitrogen (top) and Total Organic Phosphorus (bottom) functions of salinity in Almakapa and Kaloko Fishponds, anchialine pools and the adjacent ocean during four :sampling periods (2000, 2007 Feb. 2012 and Nov. 2012). Also shown are data from three KAHO monitoring wells. Solid tine is conservative mixing line connecting endpoint concentrations from the open ocean and high level groundwater from the DWS Honokohau Well (4158 -03), while dashed line is conservative mixing line connecting open ocean concentrations to basal groundwater sampled from the Kaloko Irrigation Well (4160 -02). A Water- Budget Model and Assessment of Groundwater Recharge for the Island of Hawaii KailuF Captain Co 1ja- Scientific Investigations Report 2011 -5078 U.S. Department of the Interior U.S. Geological Survey F:Y6161t b A Water- Budget Model and Assessment of Groundwater Recharge for the Island of Hawaii By John A. Engott Scientific Investigations Report 2011 -5078 U.S. Department of the Interior U.S. Geological Survey U.S. Department of the Interior KEN SALAZAR, Secretary U.S. Geological Survey Marcia K. McNutt, Director U.S. Geological Survey, Reston, Virginia: 2011 This report and any updates to it are available online at: http://pubs.usgs.gov/sir/2011/5078/ For more information on the USGS —the Federal source for science about the Earth, its natural and living resources, natural hazards, and the environment, visit http: / /www.usgs.gov or call 1 -888- ASK -USGS For an overview of USGS information products, including maps, imagery, and publications, visit http: /Avww.usgs.gov /pubprod To order this and other USGS information products, visit http: / /store.usgs.gov Any use of trade, product, or firm names is for descriptive purposes only and does not imply endorsement by the U.S. Government. Although this report is in the public domain, permission must be secured from the individual copyright owners to reproduce any copyrighted materials contained within this report. Suggested citation: Engott, J.A., 2011, A water - budget model and assessment of groundwater recharge for the Island of Hawaii: U.S. Geological Survey Scientific Investigations Report 2011 -5078, 53 p. Executive Summary Concern surrounding increasing demand for groundwa- ter on the Island of Hawai `i, caused by a growing population and an increasing reliance on groundwater as a source for municipal and private water systems, has prompted a study of groundwater recharge on the island using the most current data and accepted methods. This report documents the development of a daily water- budget model for computing groundwater recharge for the entire Island of Hawaii and the application of the model to estimate mean recharge for various land -cover and rainfall conditions. The development of a submodel for the Kona area and the application of the model to estimate historical groundwater recharge in the Kona area during the period 1984 -2008 also are documented. Recharge estimates from this study are compared to recharge estimates used by the State of Hawaii Commission on Water Resource Management (CWRM) in setting the sustainable yields (maximum allow- able pumping rates) of Hawai `i aquifer systems in the 2008 version of the Water Resource Protection Plan (2008 WRPP). Groundwater Recharge on Hawaii Estimated mean annual recharge on the Island of Hawaii is 6,594 million gallons per day, which is about 49 percent of mean annual rainfall. Recharge is highest on the windward slopes of Mauna Loa, below the tradewind inversion, and low- est on the leeward slopes of Kohala and Mauna Kea (fig. ES 1). Local recharge maxima also occur on (1) the higher eleva- tions of windward Kohala, (2) windward Mauna Kea below the tradewind inversion, (3) windward Kilauea, (4) the middle elevations of southeastern Mauna Loa, and (5) the lower middle elevations of leeward Mauna Loa and southwestern Hualalai, in the Kona area. Local recharge minima also occur on (1) Mauna Kea and Mauna Loa, above the tradewind inver- sion, (2) the northern tip of Kohala, (3) leeward Kilauea, (4) the southern tip of Mauna Loa, and (5) the northwestern slopes of Mauna Loa and Hualalai. In 18 of the 24 aquifer systems on the island, mean annual recharge estimated in this study for baseline conditions was higher than the recharge estimates used in the 2008 WRPP Im (fig. ES2). Baseline conditions for this study were 2008 land cover and mean annual rainfall from the period 1916 -1983. The higher recharge estimates for most areas in this study generally are attributable to differences in the methods used to estimate runoff and ET, the inclusion of fog interception in this study, and the shorter time step used in this study. Sub- stantially lower estimates of recharge were calculated for the Mahukona, Waimea, and Haw! aquifer systems -38, 34, and 29 percent lower, respectively. These lower estimates mainly are due to much higher ET estimates in this study compared to the 2008 WRPR This may be cause for concern, because these particular areas are experiencing a growth in development and a related growth in water demand. For the drought simula- tion performed in this study, the estimates of recharge for all three of these aquifer systems were substantially less than the sustainable yields of the aquifer systems set by CWRM. Recent projections of change in rainfall owing to effects of ongoing climate change generally indicate a slight increase in islandwide rainfall, and estimates of annual recharge in the late 21 st century are higher than baseline estimates for every aquifer system, except `Anaeho`omalu. On average, these aquifer- system recharge estimates are higher by about 8 per- cent compared to baseline estimates. Recharge in the Kona Area (1984 -2008) For the Kona submodel, the period 1984 -2008 was bro- ken into five subperiods to simplify calculation: 1984 -1988, 1989 -1993, 1994 -1998, 1999 -2003, and 2004 -2008. Ground- water recharge was highest during 2004 -8 and lowest during 1999 -2003 (fig. ES3). Estimated mean annual recharge during 1999 -2003 was only 50 percent of estimated recharge during 2004 -8. These extremes coincided with the periods of lowest and highest mean rainfall, respectively. On a monthly basis, average recharge during the entire 1984 -2008 period was highest in January and lowest in August; however, no clear seasonal pattern is discernible. Spatially, the highest recharge occurred in a belt about 4 miles wide running parallel to the coast about 2 miles inland. 40 A Water- Budget Model and Assessment of Groundwater Recharge for the Island of Hawai'i from the Intergovernmental Panel on Climate Change (IPCC) Fourth Assessment Report (2007). Late - 21st - century projections for specific rain -gage stations are published online (Timm and others, 2009). In general, precipitation is projected to increase slightly for most areas of the island. Projected late- 21st - century rainfall changes from Timm and others (2009) were applied to each rainfall - variability zone in the water- budget model (table 9), except for zone 7, an area for which no climate - change projections were published. The effect of climate change on pan evaporation was analyzed for each pan- evaporation zone by developing a linear regression of historical pan evaporation versus historical rainfall for stations in each zone (table 10). For this particular analysis, pan- evaporation and rainfall data were normalized by dividing the annual or monthly observed values by the mean values for the particular pan- evaporation or rain -gage station published in Ekern and Chang (1985) or Giambelluca and others (1986), respectively. For the linear regression, a basic assumption was made that annual or monthly periods of mean pan evaporation should correspond to annual or monthly periods of mean rainfall. Hence, each regression line was forced through the point (1,1) on the plot of normalized pan evaporation versus normalized rainfall. The equation for each regression line is given by PANI (PAN)... - 1 = a(P/P.. - 1) (15 ) where PAN = pan evaporation [L], (PAN)m,,,, = mean pan evaporation [L], a = slope of the regression line [dimensionless], P = rainfall [L], and Pm,.„ = mean rainfall [L]. Solving equation 15 for pan evaporation (PAN) yields: PAN = (a(P /P,,,«„ - 1) + 1)(PAN),,,,,,, (16) Late- 21st - century mean pan evaporation in each pan- evaporation zone was estimated by using equation 16 and the following variable definitions: Table 9. Parameters used for the simulation of late -21 st- century rainfall conditions on the Island of Hawaii. [See figure 6 for locations of rainfall - variability zones; column (A) is the ratio of mean seasonal rainfall from Timm and others (2009) to the mean seasonal rainfall derived from Giambelluca and others (1986); columns (B), (C), and (D) are estimated rainfall- change factors based on the means and lower and upper margins of the 95- percent statistical confidence interval for a six -model ensemble for the late 21st century from Timm and others (2009); columns (E), (E), and (G) are the factors used to adjust mean rainfall in each rainfall - variability zone in the water - budget model to simulate late 21st century climate; SKN, state key number, NWS ID, National Weather Service cooperative identification number, HVNP HQ, Hawaii Volcanoes National Park headquarters; -, no data given in Timm and others (2009)] Rainfall- Rain -gage NWS Mean Mean Lower 95% Upper 95% Overall Overall Overall variability station and ID rainfall change confidence confidence adjustment adjustment adjustment zone SKN adjustment factor change change factor for factor for lower factor for upper factor (B) factor factor mean change 95% confidence 95% confidence (A) (C) (D) (E) = (A) x (B) change Mange (F) = (A) x (C) (G) = (A) x (D) Wet Season (November to April) I HIM 168 511339 1.070 - - - 1.070 1.070 1.070 2 Pa'auilo 221 517312 0.996 1.033 0.852 1.214 1.029 0.849 1.209 3 HVNP HQ 54 511303 1.056 1.028 0.890 1.166 1.086 0.940 1.232 4 N5'hlehu 14 516588 0.998 1.027 0.860 1.195 1.025 0.858 1.193 5 Kulani Mauka 76 515018 0.975 - - - 0.975 0.975 0.975 6 H81ualoa 70 511557 1.089 1 .012 0.799 1 .226 1.102 0.870 1.335 7 No estimates for this zone - - - - 1 .000 1.000 1.000 Dry Season (May to October) 1 Hawi 168 511339 1.014 1.040 0.818 1.261 1.054 0.829 1.279 2 Pa'auilo 221 517312 0.941 1.070 0.839 1.300 1.007 0.790 1.224 3 HVNP HQ 54 511303 1.011 - - - 1.011 1.011 1.011 4 Kapitpala Ranch 36 513300 1.009 1.039 0.867 1.212 1.048 0.875 1.223 5 K01ani Mauka 76 515018 0.847 - - - 0.847 0.847 0.847 6 1461ualoa 70 511557 1.097 1.044 0.843 1.244 1.145 0.924 1.364 7 No estimates for this zone - - - - 1.000 1.000 1.000